report 59: geology and mineralization of the ......copper–gold volcanogenic massive sulfides,...
TRANSCRIPT
DEPARTMENT OF MINERALS AND ENERGY
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
REPORT59
GEOLOGY AND MINERALIZATIONOF THE PALAEOPROTEROZOICBRYAH AND PADBURY BASINS
WESTERN AUSTRALIA
by F Pirajno S A Occhipinti and C P Swager
GOVERNMENT OFWESTERN AUSTRALIA
REPORT 59
GEOLOGY AND MINERALIZATIONOF THE PALAEOPROTEROZOICBRYAH AND PADBURY BASINSWESTERN AUSTRALIA
byF Pirajno S A Occhipinti and C P Swager
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
Perth 2000
MINISTER FOR MINESThe Hon Norman Moore MLC
DIRECTOR GENERALL C Ranford
DIRECTOR GEOLOGICAL SURVEY OF WESTERN AUSTRALIADavid Blight
Copy editor D P Reddy
REFERENCEThe recommended reference for this publication isPIRAJNO F OCCHIPINTI S A and SWAGER C P 2000 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury
Basins Western Australia Western Australia Geological Survey Report 59 52p
National Library of AustraliaCataloguing-in-publication entry
Pirajno Franco 1939ndashGeology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
BibliographyISBN 0 7309 6653 4
1 Geology Structural mdash Western Australia mdash Bryah Basin2 Geology Structural mdash Western Australia mdash Padbury Basin3 Mines and mineral resources mdash Western Australia mdash Bryah Basin4 Mines and mineral resources mdash Western Australia mdash Padbury Basin5 Bryah Region (WA)6 Padbury Region (WA)I Swager C PII Occhipinti S A (Sandra Anne)III Geological Survey of Western AustraliaIV Title (Series Report (Geological Survey of Western Australia) 59)
5531099413
ISSN 0508ndash4741
Grid references in this publication refer to the Australian Geodetic Datum (AGD84)
Printed by Optima Press Perth Western Australia
Copies available fromInformation CentreDepartment of Minerals and Energy100 Plain StreetEAST PERTH WESTERN AUSTRALIA 6004Telephone (08) 9222 3459 Facsimile (08) 9222 3444wwwdmewagovau
Cover photographFerruginous shale of the Millidie Creek Formation with a well-developed pencil cleavage 25 km northwest of Fraser Well(BRYAH AMG 651660)
iii
Contents
Abstract 1Introduction 1Regional tectonic setting 3Geology stratigraphy and geochronology 4
Peak Hill Schist and Marymia Inlier 5Bryah Group 6
Karalundi Formation 6Narracoota Formation 7
Peridotitic and high-Mg basalt association 7Intrusive rocks and layered intrusions 7Mafic and ultramafic schist 8Metabasaltic hyaloclastite 9Felsic schist 9Volcaniclastic rocks 10Carbonated and silicified metavolcanic rocks 11Jasperoidal chert 11Geochemistry of the Narracoota Formation 11
Ravelstone Formation 16Horseshoe Formation 16
Padbury Group 17Labouchere Formation 18Wilthorpe Formation 19
Beatty Park and Heines Members 19Robinson Range Formation 20Millidie Creek Formation 20Unassigned units of the Padbury Group 21
Structure 21D1 structures 23D2 structures 23D3 structures and their relationship to D2 structures 25D4 structures 25
Metamorphism 25Structural synthesis 27Mineralization 32
Gold deposits 33Peak Hill Jubilee and Mount Pleasant deposits 39Harmony deposit 41Labouchere Nathans and Fortnum deposits 41Wembley deposit 42Wilgeena deposit 43Durack St Crispin and Heines Find prospects 43Ruby Well group 43Mikhaburra deposit 43Wilthorpe deposit 43Cashman deposit 44
Volcanogenic copperndashgold deposits 44Supergene manganese deposits 44Iron ore 45Talc 45Discussion 45
Tectonic model and conclusions 46Acknowledgements 48References 49
Appendix
Gazetteer of localities 52
Plate
Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
iv
Figures
1 Stratigraphy of the former lsquoGlengarry Basinrsquo 22 Simplified geology of the Bryah Padbury and Yerrida Basins 43 Rotated orthoclase porphyroblast Peak Hill Schist 54 Partially recrystallized mylonite Peak Hill Schist 55 Peak Hill Schist mylonite from the Hangingwall Sequence 56 Outcrop of quartz mylonite Peak Hill Schist 67 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric 68 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt) 89 Basaltic hyaloclastite Narracoota Formation 9
10 Mafic volcaniclastic rock Narracoota Formation 1011 Volcanic breccia intersected in diamond drillhole BD1 1012 Total alkali versus silica diagram for rocks the Narracoota Formation 1313 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the
Narracoota Formation 1414 Geochemical characteristics of the Narracoota Formation rocks 1415 Geochemical discriminant plots for Narracoota Formation 1516 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation 1617 Schematic stratigraphy of the Horseshoe Formation 1718 Major regional structures in the Bryah and Padbury Groups 2219 Simplified geological map of the Bryah and Padbury Groups 2420 Selected hypothetical cross sections through the Bryah and Padbury Groups 2721 Model of the structural development of the BryahndashPadbury Group succession 2922 New model of the structural development of the BryahndashPadbury Group succession 3123 New model for the structural development of the BryahndashPadbury Group succession
and the Peak Hill Schist 3224 Schematic north-northwest to south-southeast cross section from the Bangemall Basin
into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins 3325 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins 3626 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet 3827 Albite porphyroblasts in mylonitic schist at Mount Pleasant 3928 The Mine Sequence schist 4029 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit 4030 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and
Marker quartzite unit 4031 Diagrammatic cross section of the Harmony ore zones 4132 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and
deformed Despair Granite 4433 Sketch illustrating a conceptual model for the origin of precious and base metal
deposits in the BryahndashPadbury and Yerrida Basins 4534 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and
Padbury Basins within the context of the Capricorn Orogen 46
Tables
1 Stratigraphy of the Bryah and Padbury Groups 32 Representative chemical analyses of the Narracoota Formation 123 Magnesium numbers for the Narracoota and Killara Formations 134 Selected geochemical parameters for the Narracoota Formation 135 Sequence of deformation events in the Bryah and Padbury Basins 236 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic
minerals of the Bryah Group and deformation fabrics 287 Gold production and remaining resources in the Bryah and Padbury Groups 348 Mineral production and remaining resources in the Bryah and Padbury Groups 359 Mineral deposits and occurrences in the Bryah and Padbury Basins 36
Digital dataset (in pocket)
Whole-rock geochemical analyses of Narracoota Formation rocks (narracootacsv)
1
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Geology and mineralization of thePalaeoproterozoic Bryah and Padbury
Basins Western Australia
by
F Pirajno S A Occhipinti and C P Swager
AbstractThe Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collision zonebetween the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains a succession of maficand ultramafic rocks of mid-oceanic ridge basalt to oceanic plateau affinity overlain by clastic andchemical sedimentary rocks The Bryah Basin was formed during back-arc sea-floor spreading andrifting on the northern margin of the Yilgarn Craton The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of the Bryah Basin as a forelandstructure resulting from either the c 1800 Ma oblique collision of the Pilbara and Yilgarn Cratons(Capricorn Orogeny) or the c 2000 Ma collision of the Glenburgh terrane and the Yilgarn Craton(Glenburgh Orogeny)
Important mineral deposits are contained in both basins and include mesothermal orogenic goldcopperndashgold volcanogenic massive sulfides manganese and iron ore The origin of the goldmineralization is related to metamorphism and deformation linked to the Capricorn Orogeny at c 18 GaThe formation of other deposits is related to pre-orogenic syngenetic processes
KEYWORDS Bryah Basin Padbury Basin Palaeoproterozoic stratigraphy geochemistry maficrocks ultramafic rocks mineralization mesothermal deposits gold
IntroductionIn early 1994 the Geological Survey of Western Australia(GSWA) commenced fieldwork to reassess the geologyand mineralization of the Palaeoproterozoic GlengarryBasin as part of a program of new mapping initiativesThe Glengarry Basin as defined by Gee and Grey (1993)constitutes the western part of the greater Palaeo-proterozoic Nabberu Province which in the east includesthe Earaheedy Basin (Bunting et al 1977 Hall andGoode 1978 Gee 1990)
The new mapping initiative resulted in the reappraisalof the geology tectonic evolution and mineralizationof the Glengarry Basin which is now recognized toconsist of three main geotectonic units the BryahPadbury and Yerrida Basins As a result the volcano-sedimentary rocks of the former lsquoGlengarry Grouprsquo arenow divided into the Bryah and Yerrida Groups (Fig 1 andTable 1) characterized not only by different lithologiesbut also by different regional structures metamorphismand mineral deposit types Some formations previouslyassigned to the lsquoGlengarry Grouprsquo have been reassigned
to the Padbury Group (Martin 1992) In additionthere is evidence to suggest that the economicallyimportant lsquoPeak Hill Metamorphic Suitersquo previouslyconsidered to be part of the lsquoGlengarry Grouprsquo (Gee1987) constitutes a separate unit the Peak Hill Schistderived from a protolith of probable Archaean ageConsequently the previous nomenclature (lsquoGlengarryGrouprsquo and lsquoGlengarry Basinrsquo) is no longer used Detailsof the old and new stratigraphy are presented in Figure 1and Table 1 and discussed in later sections The revisedstratigraphy of the former lsquoGlengarry Basinrsquo is presentedin Occhipinti et al (1997) Details of the stratigraphy andstructure of the lower Padbury Group are presented inMartin (1998)
The Bryah and Padbury Basins lie within the ROBINSON
RANGE and PEAK HILL 1250 000 sheets (MacLeod 1970Elias and Williams 1980 Gee 1987) and the north-western and northeastern corners of the BELELE andGLENGARRY 1250 000 sheets (Elias 1982 Elias et al
Capitalized names refer to standard 1100 000 map sheets unless otherwisespecified
2
Pirajno et al
1982) The Bryah and Padbury Groups (Fig 2) make upthe western part of the former lsquoGlengarry Basinrsquo andare now interpreted to have developed in rift and forelandbasins respectively (Martin 1994 Pirajno 1996 Pirajnoet al 1996 Pirajno et al 1998b) The Yerrida Group(Fig 2) makes up the eastern part of the former lsquoGlengarryBasinrsquo and includes two subgroups the Windplainand Mooloogool Subgroups (Fig 2 Table 1) whichdeveloped in sag and rift basins respectively (Pirajno et al1995ab 1996) The geology and mineralization ofthe Yerrida Basin are described in a separate Report(Pirajno and Adamides 2000) The Bryah Group isin faulted contact with the Yarlarweelor gneiss complexthe Marymia Inlier of the Archaean Yilgarn Cratonand the Palaeoproterozoic Yerrida Group The contactbetween the Bryah and the Yerrida Groups is along anortheasterly trending high-angle reverse fault (the GoodinFault)
Based on structural and metamorphic criteria the areaoccupied by the Bryah and Padbury Groups and thePeak Hill Schist can be regarded as a single domainIn this Report where appropriate this domain is referred
to as the BryahndashPadbury Basin The geology newstratigraphy geochronological constraints structureand metamorphism of the Bryah and Padbury Groups arediscussed The geochemistry of the volcanic componentof the Bryah Group and mineral deposits of the Bryahand Padbury Basins are also summarized A tectonicoverview and proposed model for the geodynamicevolution of the Bryah and Padbury Basins withinthe framework of the Capricorn Orogen conclude thereport
Work in the BryahndashPadbury area involved 125 000-scale mapping to produce 1100 000-scale geologicalmaps Geological mapping was carried out using125 000-scale colour aerial photography (availablefrom the Western Australian Department of LandAdministration) aeromagnetic images (400 m line-spacedcollected by GSWA in 1994) and Landsat TM imagesResults of geological mapping were integrated withpetrographic geochemical and geochronology studiesDuring this work a total of 1450 rock samples werecollected of which 776 were thin-sectioned and 136geochemically analysed In addition logging of diamond
Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
Gee (1987)P
AD
BU
RY
BA
SIN
GR
OU
PG
LEN
GA
RR
Y B
AS
ING
RO
UP
Millidie Creek Formation
Robinson Range Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Narracoota Volcanics
Karalundi Formation
Doolgunna Formation
Johnson Cairn Shale
Thaduna Greywacke
Juderina Formation
Maraloou Formation
Crispin Conglomerate
Finlayson Sandstone
Peak Hill Metamorphics
GLE
NG
AR
RY
BA
SIN
GR
OU
P
Maraloou Formation
Thaduna Greywacke
Narracoota Volcanics
Doolgunna Formation
Johnson Cairn Shale
Juderina Formation(Finlayson SandstoneMember)
YE
RR
IDA
BA
SIN
GR
OU
P
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Peak Hill Schist
BR
YA
H B
AS
ING
RO
UP
PA
DB
UR
Y B
AS
ING
RO
UP
TE
CT
ON
IC C
ON
TA
CT
Millidie Creek Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Karalundi Formation
Ravelstone Formation
Narracoota FormationMaraloou Formation
Killarra Formation(Bartle Member)
Doolgunna Formation
Thaduna Formation
Juderina Formation
170100
Gee and Grey (1993) Occhipinti et al (1997) Pirajno et al (1998b this study)
Robinson RangeFormation
Unconformity
Unconformity
Johnson CairnFormation
NOTE New or redefined units (Occhipinti et al 1997)
(Finlayson and BubbleWell Members)
ARCHAEAN BASEMENT
FMP409a
3
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
drillcore (1100 m) and several visits to prospects andoperating mines considerably enhanced our knowledge ofthe geology of the area Most of the mapped areas werealso included in a regional regolith geochemical samplingprogram covering the PEAK HILL ROBINSON RANGE andGLENGARRY 1250 000 sheets (Subramanya et al 1995Bradley et al 1997 Crawford et al 1996)
Interim accounts of the structural and stratigraphicrelations of the BryahndashPadbury and Yerrida Basins havebeen reported by Pirajno et al (1995ab 1996) andOcchipinti et al (1997) Pirajno (1996) and Pirajno et al(1995a 1998b) discussed possible models for the tectonicevolution of the BryahndashPadbury and Yerrida Basins Thestructure and metamorphism of the BryahndashPadbury Basinhave been described by Occhipinti et al (1998abc)whereas details of mineral potential production andore deposit geology can be found in Pirajno andOcchipinti (1995) and Pirajno and Preston (1998)Published 1100 000 geological maps and accompanyingExplanatory Notes that wholly or partly cover the BryahndashPadbury Basin comprise BRYAH (Pirajno and Occhipinti1998) GLENGARRY (Pirajno et al 1998a) MILGUN (Swagerand Myers 1999) PADBURY (Occhipinti et al 1998a)DOOLGUNNA (Adamides 1998) and MARYMIA (Bagas1998) The southern portion of the JAMINDI 1100 000 mapsheet containing rocks of the Bryah Group was alsomapped The layout of these map sheets in relation to theBryahndashPadbury Basin and adjacent tectonic units is shownin Figure 2 The geology of the Bryah and Padbury Basinsis presented in Plate 1
Regional tectonic settingThe Bryah and Padbury Basins are situated along thenorthern margin of the Archaean Yilgarn Craton and arepart of the Capricorn Orogen (Fig 2 inset of Plate 1)The Capricorn Orogen also includes the Ashburton Basin
and the Gascoyne Complex and can be traced for morethan 1000 km with northwesterly to westerly trendsforming a broad belt of deformed low-grade volcano-sedimentary high-grade metamorphic and granitoidrocks
The Capricorn Orogeny resulted from the collisionbetween the Pilbara and Yilgarn Cratons at c 1800 Maand involved the closure of an intervening oceanformation of a back-arc basin and the possible accretionof microcontinental fragments (Myers 1993 Myers et al1996 Tyler et al 1998) Prior to the Capricorn Orogenythe c 2000 Ma Glenburgh Orogeny (Occhipinti et al1999) resulted in the accretion of the Glenburgh terraneonto the Yilgarn Craton The convergence between thePilbara and Yilgarn Cratons was essentially oblique andresulted in the development of easterly trending strike-slipmovements which included regional sinistral faults TheCapricorn Orogeny also affected other tectonic units suchas the Archaean Narryer Terrane Marymia Inlier SylvaniaInlier and parts of the Hamersley Basin (Tyler andThorne 1990 Myers et al 1996 Tyler et al 1998)
The Palaeoproterozoic volcano-sedimentary andsedimentary successions of the Bryah and Padbury Basinsare unconformable on the northern margin of the YilgarnCraton whereas to the north they are either unconform-ably overlain by or in faulted contact with rocksof the Bangemall Basin and the Archaean graniticrocks of the Marymia Inlier The Marymia Inlier iseconomically important because it hosts a number of golddeposits including the Peak Hill deposit (AMG 672190E7163150N) on the southwestern tip of the inlier (seeMineralization)
Localities are specified by the Australian Map Grid (AMG) system AMGcoordinates (eastings and northings) of localities discussed in the text arelisted in Appendix 1
Table 1 Stratigraphy of the Bryah and Padbury Groups
Group Age Formation Rock type(Ma)
Padbury Group Millidie Creek sericitic siltstone chloritic siltstone banded iron-formation(peripheral foreland basin) dolomitic arenite
Robinson Range ferruginous shale banded iron-formation
ltc 2000 Wilthorpe quartz-pebble conglomerate(Beatty Park and (siltstonendashwacke and polymictic conglomerate respectively)Heines Members)
Labouchere turbidite sequence (quartz wacke siltstone)
unconformable contact mdash tectonized in many places
Bryah Group (rift basin) Horseshoe banded iron-formation wacke shale
ltc 2000 Ravelstone quartzndashlithic wacke
Narracoota maficndashultramafic volcanic rocks and intercalated sedimentary rocks
Karalundi conglomerate quartz wacke
faulted contact
Yerrida Group (sag and rift basin) c 2174
SOURCE Modified after Pirajno et al (1996)
4
Pirajno et al
Geology stratigraphy andgeochronology
The BryahndashPadbury Basin contains the Bryah andPadbury Groups and the Peak Hill Schist The stratigraphyfor the Bryah and Padbury Groups is summarized in
Figure 1 and Table 1 where a comparison with previousGSWA work is also provided The Peak Hill Schist is aseparate tectono-stratigraphic unit that is discussed herewith the Marymia Inlier as basement to the Bryah GroupDetailed descriptions of the various formations and theircontact relationships are presented in Occhipinti et al(1997) Martin (1998) Adamides (1998) Pirajno and
Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins showing 1100 000 map sheet boundariesInset shows the position of the basins in relation to the Capricorn Orogen
MARYMIAINLIER
GOODININLIER
Goodin
Fault
Fault
Killara
Narracoota
30 km
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
FMP375
117deg
30
118deg
30
26deg00
25deg00
Murchison
FaultMorris
Earaheedy Group
Padbury Group
Yerrida Group
Archaean granitendashgreenstonebasement
Bangemall Group
Bryah Group
Proterozoic granites
Fault
Moorarie Padbury
MilgunMarquis
FaultCooinbar
NarryerTerrane
Murchison
Terrane
Kerba Fault
119deg
30
Gabanintha Yanganoo
MooloogoolGlengarry
Bryah Doolgunna
Jamindi Three Rivers
010300
BRYAH-PADBURY
BASINS
PROTEROZOIC
5
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Occhipinti (1998) Pirajno et al (1998b) Occhipinti et al(1998c) and Swager and Myers (1999)
In this section the geology field relations stratigraphyand geochronological constraints of the Peak Hill SchistMarymia Inlier and the formations that make up the Bryahand Padbury Groups are discussed
Peak Hill Schist and MarymiaInlierThe Peak Hill Schist (formerly called the lsquoPeak HillMetamorphic Suitersquo Gee 1987) is exposed in the lsquoPeakHill Domersquo or anticline and constitutes a tectonic unitrepresenting the southwestern tip of the Marymia Inlier(Fig 2 Thornett 1995) The Peak Hill Schist iscontinuous with the Marymia Inlier and Thornett (1995)suggested that the lsquoPeak Hill Domersquo represents thedeformed southwestern end of the Marymia Inlier Fieldobservations and petrographic and aeromagnetic datasupport this view The boundary between the Peak HillSchist and granitic rocks of the Marymia Inlier is a zoneof intense deformation and metamorphism characterizedby tectonic interleaving and duplexing Towards thenortheast the intensity of the Capricorn Orogenydeformation in the Marymia Inlier granites decreases toareas where they are undeformed The contacts betweenthe Peak Hill Schist and rocks of the Bryah Group arefaulted (probably thrusted) and tectonically interleaved inplaces
Rocks of the Peak Hill Schist include phyllonitequartzndashmuscovite schist calc-silicate schist sericite(ndashquartz) schist and quartzndashmuscovitendashbiotitendashchloriteschist locally with rotated alkali feldspar porphyroblasts(Fig 3) and minor metabasite These units have beenvariously deformed and contain a range of mylonitictextures The mylonitic fabric of these rocks is revealedby SndashC surfaces and lines of lsquomica fishrsquo (Lister and Snoke1984) in a dominantly and variably recrystallized quartz-rich matrix (Figs 4 and 5) A few discrete mylonitic units
Figure 3 Orthoclase porphyroblast with curved inclusiontrails in quartzndashmuscovite schist of the Peak HillSchist crossed polars
Figure 4 Partially recrystallized mylonite (Crispin Mylonite)from the Peak Hill Schist This sample is from amylonitic quartzndashbiotitendashalbite schist from the MineSequence in which the biotite defines C planesThe S planes were obliterated by recrystallizationto a blastomylonite crossed polars
Figure 5 Peak Hill Schist mylonite The C surfaces havesurvived recrystallization and now form thin micatrails crossed polars
form arcuate zones interpreted as early possibly thrustfault zones (see Structure) One of these units is the PeakHill Mylonite (Pirajno and Occhipinti 1998) which is arefolded quartz blastomylonite and quartz mylonite lenswithin quartzndashmuscovite schist The Peak Hill Mylonite(Figs 6 and 7) is an important unit because it is spatiallyassociated with gold mineralization (Peak Hill and MountPleasant deposits) Other less conspicuous quartzmylonite lenses are common within the Peak Hill Schistand were previously mapped as cherts or banded cherts(Windh 1992) Another important unit is the CrispinMylonite (Pirajno and Occhipinti 1998) which lies in thesouthern part of the Peak Hill Schist between sericiteschist and quartzndashmuscovite schist The Crispin Mylonitereferred to by Gee (1987) as the lsquoCrispin Conglomeratersquois characterized by square to rounded quartz arenite clastsup to 60 cm long in a sericite-rich matrix On the basisof field and petrographic observations it is concluded
6
Pirajno et al
here that this unit is not a conglomerate but a mylonite(Pirajno and Occhipinti 1998) Mylonites that resembleconglomerates (pseudo- or tectonic conglomerates) havebeen reported by Peters (1993) and Raymond (1984ab)
The Marymia Inlier (Windh 1992 lsquoMarymia Domersquoof Gee 1987) represents a fragment of northeasterlytrending Archaean granitendashgreenstone basement Rocksof the Marymia Inlier are mainly granitic but also includesmall enclaves of calc-silicate rock orthoamphibolite andminor metamorphosed banded iron-formation (BIF) ThePeak Hill Schist is also tentatively placed within theMarymia Inlier The granitic rocks are locally stronglyfoliated to gneiss or display strong cataclastic fabricsGranitic rocks include both fine-grained (aplitic) andcoarse-grained porphyritic phases Some outcropspreviously mapped as granite by Gee (1987) have beenincluded in the Peak Hill Schist The granitic rocks of theMarymia Inlier are monzogranite in the east and showincreasing cataclastic deformation towards the southwest(Pirajno and Occhipinti 1998 Bagas 1998)
Bryah GroupThe Bryah Group is divided into four formations theKaralundi Narracoota Ravelstone and HorseshoeFormations (Figs 1 and 2 Table 1) The basal unit of theBryah Group is the Karalundi Formation which is infaulted contact with the Doolgunna Formation of theYerrida Group along the Goodin Fault The KaralundiFormation predominantly consists of quartz conglomeratequartz arenite lithic wacke and shale The NarracootaFormation (parts of which were previously known aslsquoNarracoota Volcanicsrsquo Gee and Grey 1993) is thedominant lithology in the Bryah Basin and consists oftholeiitic extrusive and intrusive rocks and subordinateultramafic units intercalated with minor jasperoidal chertunits and clastic sedimentary rocks The NarracootaFormation is disconformably overlain by and locallyinterfingers with the Ravelstone Formation TheRavelstone Formation comprises a succession of lithic andquartz wacke shale and siltstone that was deposited byturbidity currents This formation is in turn conformablyoverlain by the Horseshoe Formation comprising quartzwacke manganiferous shale and banded iron-formation
The age of the Bryah Group is poorly constrainedbetween c 2000 and 1800 Ma Detrital zircons ofuncertain provenance in the Ravelstone Formation (upperBryah Group) provide a maximum age of 2014 plusmn 22 Ma(Nelson 1997) The Bryah Group must be older than theunconformably overlying Mount Leake Formation (outlierof the Earaheedy Group) which has a UndashPb (detritalzircon) maximum age of 1785 plusmn 11 Ma (Nelson 1997)The PbndashPb isochron ages obtained from pyrite from themesothermal Mikhaburra gold deposit (174 Ga Pirajnoand Occhipinti 1998) and from inferred syngenetic pyritefrom the Narracoota Formation (1920 plusmn 35 Ma Windh1992) probably represent mineralizing events in the BryahBasin rather than the depositional age of the BryahGroup
Karalundi Formation
The Karalundi Formation forms the base of the BryahGroup outcropping in a northeasterly trending belt alongthe southeastern margin of the Bryah Basin (Plate 1)Rocks of the Karalundi Formation are estimated to reacha thickness of approximately 2500 m In the southeastalong the Great Northern Highway Karalundi Formationrocks are in faulted contact with the Doolgunna Formation(Yerrida Group) On the southeastern side of the Peak HillSchist and in faulted contact with it the KaralundiFormation outcrops 35 km east of the Wilgeena mine Inthe south the Karalundi Formation is intercalated withmafic volcaniclastic rocks of the Narracoota Formation
The Karalundi Formation is characterized by immatureclastic (mainly quartzndashlithic wacke and conglomerate)units containing angular quartz and lithic fragments setin a sericitendashclay-rich matrix Other rock types includesiltstone calcareous siltstone cross-bedded areniteferruginous arenite litharenite minor dolomite andpurple green and black shale The Karalundi Formationalso contains pods of hematitic jasperoidal chert (see
Figure 6 Outcrop of quartz mylonite Peak Hill Schist Notethe flaggy nature of this rock and its steep dip
Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating atypical mylonitic fabric and SndashC planes (C planesare horizontal S planes trend from upper right tolower left between the C planes) crossed polars
7
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
below) which were interpreted by Gee (1979 1987) asfumarolic pipes
On DOOLGUNNA quartz arenite and conglomerate unitsare present within a dominantly hematitic shaly successionthat was interpreted by Adamides (1998) as a deep-waterlateral facies of the Bryah rift succession This successionalso contains olistoliths (exotic blocks) whose origin isnot clear Adamides (1998) suggested that they might havebeen derived from units of the Juderina Formation as aresult of inversion of the adjacent Yerrida Basin and upliftof the Goodin Inlier
Narracoota Formation
Rocks of the Narracoota Formation constitute a majorlithotype of the Bryah Group They form the bulk of thegroup with a thickness estimated at about 6 km (Pirajnoand Occhipinti 1998) and extend for more than 180 kmeast to west across the Bryah Basin The NarracootaFormation conformably overlies and locally interfingerswith the Karalundi Formation and also interfingers withand is in disconformable contact with the base of theoverlying Ravelstone Formation Contacts between theNarracoota Formation and Padbury Group are tectonic Inthe north regional structural relationships suggest that theNarracoota Formation is also in tectonic contact with theHorseshoe Formation Gravity modelling indicates that theNarracoota Formation forms the floor of the central partsof the Bryah Basin (Pirajno and Occhipinti 1998)
Rocks of the Narracoota Formation are affected bysea-floor metasomatism and regional prograde andretrograde metamorphism (see Structure) On the basisof field observations texture geochemistry and petrologyrocks of the Narracoota Formation can be subdivided intometamorphosed peridotitic and high-Mg metabasaltbasaltic hyaloclastite pyroclastic rocks intrusive rocksand mafic and ultramafic schist Collectively thesesubdivisions are referred to as metabasites Mafic andultramafic schists are characterized by a pervasiveschistosity but the distinction between mafic andultramafic is subtle and most clearly demonstrated usinggeochemistry In the area 2 km northeast of the Ravelstonemanganese opencuts a texture described by Hynes andGee (1986) as polygonal jointing has been observed in themetabasalt and appears to be a well-developed pencilcleavage High-Mg basalts are associated with peridotiticunits Intrusive rocks cover a range of types frompyroxenite to gabbroic rocks and dykes Metabasaltichyaloclastites are lava flows that interacted with seawaterand have a distinct spilitic character Volcaniclastic rocksincluding vent breccias are commonly present in bothbasaltic hyaloclastite and mafic schist
Typically the metabasite rocks of the NarracootaFormation contain no or very few feldspar phenocrystsOther authors have suggested that the presence ofmedium-grained embayed quartz crystals indicates theproximity of felsic volcanic rocks (Hill and Cranney1990 Windh 1992) Felsic volcanic rocks are associatedwith the upper part of the Narracoota Formation at andaround the Horseshoe Lights copperndashgold mine onJAMINDI 29 km east of the Fortnum mine on MILGUN
Fine-grained grey to black metamorphosed shale andslate are present in places as lenses of interflowsedimentary rocks within the volcanic succession Wheremore deformed and metamorphosed these slates are finelylaminated biotitendashchlorite schists South of the RobinsonRange small lenses of sedimentary rock (lithic wacke andshale) are intercalated with the volcanic rocks of theNarracoota Formation In places pods and lenses ofjasperoidal chert are associated with the volcanic rocks
Peridotitic and high-Mg basalt association
Massive layered high-Mg basaltic rocks (possibly lavaflows shown on Plate 1 as Anu) are preserved inprominent hills between Top Dimble Well and DespairBore on MILGUN Hynes and Gee (1986) described thissequence as komatiitic basalt with up to 20 MgOUnequivocal pillow structures as mentioned by Hynes andGee (1986) were not observed The rocks are meta-morphosed but their protoliths include olivine cumulate(peridotite) high-Mg basalt with plumose and harrisitictextures and medium-grained basalt Layering is mainlydefined by massive olivine cumulate layers up to 20 mthick and plumose-textured basalt layers up to 5 m thickLocally large sheaves of skeletal amphibole (afterpyroxene) are arranged at approximately right angles tothe layering and resemble harrisitic textures (Fig 8a) Thehigh-Mg basalt units are characterized by well-developedlsquospinifexrsquo-like textures with acicular tremolitendashactinoliteafter pyroxene and up to 30 interstitial plagioclase(replaced by epidote or zoisite) The high-Mg basalt isinterlayered with medium-grained basalt of similarmineralogy and composition with 8ndash9 MgO Thewhole-rock geochemistry of these rocks is discussed inGeochemistry of the Narracoota Formation
Peridotite units commonly consist of 70ndash80 fine- tomedium-grained olivine replaced by tremolite(ndashtalc)skeletal amphiboles after pyroxene and 20ndash30 fine-grained matrix of plumose-textured amphibole High-Mgbasalt contains up to 30 locally glomeroporphyriticolivine (now tremolite) lesser amounts of acicularpyroxene in a 60ndash70 amphibole plumose-texturedmatrix and 15 MgO One particular example contains35 olivine (only partly altered to talc) skeletal(lsquoswallow-tailrsquo) fresh orthopyroxene and lesser amountsof acicular skeletal amphibole prisms possibly afterclinopyroxene (Fig 8b)
Intrusive rocks and layered intrusions
A metadolerite sheeted dyke complex (shown as And onPlate 1) outcrops north of the Robinson Syncline Theserocks are associated with deformed pillow metabasalt andtend to be internally undeformed but commonly formelongate bodies subparallel to the S2 foliation Theycontain diopside amphibole epidote and minor olivine
Lenses of cumulate-textured units represented bypyroxenite or peridotite and gabbroic rocks are locallyintercalated with the mafic and ultramafic schist Alensoidal outcrop of metapyroxenite is present nearDurack Well Gabbroic rocks are common betweenTrillbar Homestead and Friday Pool on MOORARIE
8
Pirajno et al
(Occhipinti and Myers 1999) These rocks have beenmetamorphosed and folded but are largely undeformedinternally The gabbroic rocks are surrounded by higherstrain zones consisting of tremolitendashactinolite schist
The Trillbar Complex (shown as Ant on Plate 1) is a30 km long by 25 km wide layered maficndashultramaficintrusion in the westernmost part of the Bryah Basin Thecomplex consists of rhythmically layered mafic andultramafic rocks with the layering oriented at a low angleto the regional foliation (Occhipinti and Myers 1999)Rock types include rhythmically layered gabbromelanogabbro leucogabbro pyroxenite and peridotiteThese rocks are metamorphosed to greenschist facies butthe original igneous textures are locally well preservedThe Trillbar Complex rocks contain assemblages ofserpentinendashtremolitendashtalc tremolitendashtalcndashmagnetitetremolitendashactinolite and actinolitendashfeldspar Cumulaterocks include olivinendashpyroxene pseudomorphed bytremolite and sphene West of the Trillbar Homestead arelayers of metamorphosed pyroxenite and peridotite inwhich the original mineral phases are totally replaced by
tremolite talc magnetite and chlorite The TrillbarComplex is interpreted here as representing a remnant ofLayer 3 (layered gabbroic rocks) of an oceanic crustsuccession (Burke et al 1981) If this is correct thenprogressively lower levels of the Narracoota Formation areexposed from east to west and this is supported by thewidespread occurrence of volcaniclastic units in thecentral and eastern parts of the Bryah Basin
Mafic and ultramafic schist
Maficndashultramafic schist consists of actinolite(ndashchloritendashclinozoisite) schist and chlorite schist (shown as Anu andAn on Plate 1) In the south-central part of BRYAH schistoutcrops form an arcuate band (possibly an antiformstructure Gee 1987) south of and following the trendsof the Robinson Syncline and the southern limbs of theFraser Synclinorium (see Structure) North of thesestructures sparse outcrops of mafic schist are present justsouth and north of the Peak Hill Schist Within the schistare pods of less deformed or internally undeformedmetabasites in which pillow structures are locally wellpreserved Overall this large band forms a majoranastomosing sheared domain (Pirajno et al 1995b) Thedominant schistosity strikes approximately easterly orwest-northwesterly and dips steeply to the north andsouth A number of quartz veins within this shear domainalso strike easterly Maficndashultramafic schist was formedas a result of deformation and metasomatism of metabasiterocks along D2 shear zones (see Structure) In most casesall original volcanic textures are obliterated although inplaces round or elongate chlorite aggregates areinterpreted as original amygdales or fine pyroclasts
To the northwest on MILGUN the mafic volcanicschist occurrences are in faulted or sheared contactwith rocks of the Labouchere Wilthorpe and RobinsonRange Formations Hill and Cranney (1990) documenteda sequence of ultramafic to mafic schists with orwithout jasperoidal chert lenses overlain by fragmentalvolcaniclastic rocks fine-grained siltstone and felsic(intermediate and dacitic) crystal tuffs These are in turnoverlain by the Ravelstone and Horseshoe Formations
Mineral constituents of the mafic schist are actinolitechlorite and clinozoisite with minor calcite pumpellyitesericite titanite quartz and relict albite Ultramafic schisthas a simpler and commonly almost monomineralicmineralogy consisting of actinolitendashtremolite withretrogressed patches of pale-green chlorite In zones ofmore intense deformation chlorite- or epidote-dominatedassemblages are present (chlorite schist and epidositerespectively) These minerals developed due to strongmagnesium and calcium metasomatism probably duringcirculation of H2OndashCO2 fluids (Pirajno et al 1995b) Fluidinfiltration caused the breakdown of tremolite andclinozoisite to produce chlorite calcite and silica Thesilica thus liberated was then channelled through shearzones resulting in silicification and quartz veins (Pirajnoet al 1995b) An example of this can be seen in abreakaway 13 km east of the Wembley gold mine wheremafic schist and deformed pillow lavas display chloritealteration and pervasive silicification near and along awest-northwesterly trending shear zone In high-strain
Figure 8 Maficndashultramafic volcanic rocks of the NarracootaFormation (Dimble Belt) a) Komatiitic pyroxenitewith skeletal amphibole prisms after a quench-textured pyroxene matrix b) Peridotite with olivinepartly altered to talc around the edges and pyroxenein a fine-grained tremolite matrix both in planepolarized light
9
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
zones a new fabric is defined by the alignment ofamphibole prisms elongate epidote and quartz Theseschists are commonly characterized by well-developedlsquopencil cleavagersquo as a result of two intersecting planarfabrics
Metabasite rocks commonly show relict igneoustextures of prismatic plagioclase and interstitial amphiboleand more abundant unoriented prisms or acicular grainsof fine- to medium-grained amphibole Massive sheaf-liketextures of acicular amphibole are interpreted as primaryigneous textures A few plagioclase phenocrysts (3ndash5 mm)are preserved The amphibole is colourless to pale-greenpleochroic actinolite (or actinolitendashtremolite) plagioclaseis albite and commonly pseudomorphed by clinozoisitendashepidote or sericitized in zones of alteration Minorconstituents include chlorite quartz and sphenendashleucoxene with local zones of massive epidote(ndashcarbonate)
A schistose metabasite 5 to 8 km northeast of the PeakHill opencut contains actinolite arfvedsonite calcitediopside epidote and quartz The alignment of actinoliteand arfvedsonite defines the S2 schistosity and thereforeboth these minerals were formed during prendashsyn-D2 (seeStructure) The presence of the arfvedsonite (sodicamphibole) suggests either an original sodium-rich rockor later sodic metasomatism during or prior to D2
Metabasaltic hyaloclastite
Metabasaltic hyaloclastites form a prominent outcrop areapartly covered by ferricrete and colluvium south of theMurchison River These rocks are separated from themafic and ultramafic schist by the Murchison Fault(Plate 1) and probably represent a substantial thicknessof mafic lavas and hypabyssal material Hynes and Gee(1986) and Gee (1987) estimated a total thickness rangingfrom 4 to 6 km On the northern part of the GLENGARRY
1100 000 sheet the metabasalts are intercalated withsedimentary rocks of the Karalundi Formation (Pirajnoet al 1998a) These metabasaltic rocks are interpreted ashyaloclastites mdash a term that denotes fragmentation dueto quenching (Fig 9) of lavas flowing in water or eruptingunder an ice sheet This results in non-explosive fracturingand disintegration of the quenched lavas (McPhie et al1993 Fischer and Schmincke 1984)
The metabasaltic hyaloclastites are undeformeddominantly of mafic composition and have a spiliticcharacter Spilites are basaltic rocks that become alteredthrough metasomatic exchange with seawater therebyincreasing their sodium content The hyaloclastites havenormative albite from 13 to 23 wt and Na2O contentsof up to 6 wt
The metabasaltic hyaloclastites are commonly aphyricand composed mainly of acicular crystals of actinolitearranged in sheaves together with epidote minorcarbonate prehnite quartz and titanite in a fine-grainedgroundmass of albite microlites chlorite and epidoteCoarse-grained equivalents (clinopyroxene and plagioclaselaths) display ophitic to subophitic textures North of theMikhaburra (Holdens Find) gold deposit a small shaft has
Figure 9 Basaltic hyaloclastite of the Narracoota Formationshowing cuneiform devitrified shards now replacedby silica and sericite plane polarized light
exposed a vesicular rock containing serpentinized olivinecrystals set in a very fine grained altered matrix ofactinolite probably replacing pyroxenes
These metabasalts are commonly unfoliated andmassive with a characteristic brecciated or jigsaw-fittexture outlined by epidote carbonate prehnite and quartzveining along cooling joints In places these cooling jointsmay form pseudo-pillow structures and may be mistakenfor pillow lavas (Hynes and Gee 1986) Microscalejigsaw-fit textures are also seen
Felsic schist
Felsic schists which host sulfide mineralization (seeMineralization) at the Horseshoe Lights copperndashgolddeposit are present in the northern part of the BryahBasin Stratigraphically the felsic schist are at the top ofmafic metavolcanic rocks of the Narracoota Formation andoverlain by rocks of the Ravelstone Formation (seebelow) which contain chert lenses and layers close to thiscontact The felsic rocks are offset by a northeasterlytrending fault near the mine area and extend for about75 km in a southeasterly direction where they are offsetagain by a northeasterly trending fault However they donot reappear on the other side of the fault where the maficmetavolcanic rocks are in contact with the clasticsedimentary rocks of the Ravelstone Formation
Felsic schist includes quartzndashsericite schist sericiteschist and chlorite schist all showing varying degrees ofdeformation and development of mylonite Examinationof drillcore from the Horseshoe Lights mine revealedstructures reminiscent of felsic volcaniclastic rocks suchas collapsed pumice fragments Quartzndashsericite andsericite schist are composed of quartz and feldsparporphyroclasts partially replaced by quartz and sericitecarbonate or chlorite and wrapped around by granoblasticaggregates of quartz and sericite these aggregates aretraversed by anastomosing bands of sericite Tourmalineis present in places In one example sericite schistcontains elliptical opaque fragments suggestive ofcollapsed pumice Chlorite schist is composed of chlorite
10
Pirajno et al
and granular quartz with the chlorite forming distinctmonomineralic laminae X-ray diffraction analyses ofaltered schist indicate the presence of quartz kaolinpyrite hematite goethite and dioctahedral sodianmuscovite or potassian paragonite
Based on petrographic and core examinations thefelsic schist precursor rocks may have been quartzndashfeldspar porphyry and felsic volcaniclastic rocks
Volcaniclastic rocks
Mafic volcaniclastic rocks have well-preserved eutaxiticor fragmental textures despite intensive foliation (Fig 10)In the Fortnum mine area mafic fragmental rocks andfine-grained mafic volcaniclastic rocks are spatiallyassociated with jasperoidal chert pods The fragmentalrocks are strongly schistose with flattened and stretched
fragments of chlorite schist quartzndashchlorite schist withplagioclase phenocrysts quartzndashfeldsparndashamphibole rock(metabasalt) medium-grained plagioclase grains andmore rarely quartz crystals in a fine-grained matrix Finelylayered mafic schists consist of an amphibolendashplagioclasematrix with scattered prismatic to ovoid plagioclasephenocrysts and quartz lsquoeyesrsquo Amphibole accessorybiotite and sericite lenses have a strong preferredorientation suggesting that recrystallization in these fine-grained rocks has destroyed any volcaniclastic texture
Volcanic breccia is present in at least three localitiesThe most important of these is 5 km north of the oldCashman mine in the southern part of BRYAH (seeMineralization) Outcrops of volcanic breccia are alsopresent at the Cashman mine and 3 km west of the PeakHill ndash Fortnum road junction The nature of these angularclast-supported poorly sorted blocks of mafic volcanicmaterial suggest that they are vent breccias Volcanicbreccia was intersected throughout 455 m of core indrillhole BD1 (BRYAH AMG 380380) drilled by NorthExploration Ltd in 1993 (McDonald 1994) This coreintersection is briefly described below
Drillhole BD1 was drilled to a depth of 520 m at aninclination of 70deg towards the south and intersected claysand gravels to a depth of 65 m followed by weatheredmafic volcanic breccias to 96 m Below this depth to theend of the hole at 520 m spectacular fresh proximal vent-facies material consisting of angular blocks and clasts ofbasaltic lava tuff and chert were intersected (Fig 11)Crude bedding is present locally as are thin layers oflaminated or cross-laminated cherty material The holebottomed in cross-laminated chert which is interpreted aspyroclastic surge and tuff deposits The basaltic rocksinclude fine-grained vesicular basalt and feldspar-phyricand augite-phyric basalts The porphyritic varieties arecharacterized by a microlite-rich feldspar matrixclinopyroxene granules interstitial glass and chlorite andopaque minerals (titanite or rutile) The feldspar
Figure 10 Mafic volcaniclastic rock of the NarracootaFormation showing relict glass shard (in centre)plane polarized light
Figure 11 Volcanic breccia of the Narracoota Formation intersected in diamond drillhole BD1 Clasts arepredominantly of basaltic rocks the matrix exhibits albitic alteration Width of the core trays is 040 m
11
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
phenocrysts are selectively altered to sericite whereas theaugite phenocrysts are fresh and exhibit distinct zoningVesicles are infilled (from rim to core) by albite epidotechlorite and calcite Minor sulfide specks mainlychalcopyrite may be present in the vesicular basalt Tuffscharacterized by fluidization (due to degassing) andeutaxitic textures consist of glass shards and crystal andlithic fragments set in a devitrified and variably alteredglassy matrix Alteration phases are mainly chloritecalcite quartz and albite Chalcopyrite blebs are presentin places Hydraulic fracturing and veins of calciteprehnite quartz and chlorite are abundant One sectionbetween 200 and 360 m is characterized by albiticalteration (sodium metasomatism) which imparts a pinkto reddish colouration to veinlets and patches where thealbite is present
The fragmental mafic volcanic rocks in drillhole BD1are interpreted to represent a proximal vent-facies volcanicbreccia This vent-facies material coincides withprominent magnetic and Bouguer gravity anomalies(Pirajno et al 1995a) The magnetic anomaly which isrelated to the presence of magnetite in pyroxene basalthas a well-defined northeasterly trending elliptical shapeand could conceivably indicate the remnants of a majorvolcanic edifice Magnetic modelling suggests thepresence of two tabular bodies dipping 25deg to the north(Bui Dung 1999 pers comm) The gravity anomaly isat the centre of a large regional gravity high whichunderlies most of the area occupied by the NarracootaFormation (Pirajno and Occhipinti 1998)
Carbonated and silicified metavolcanic rocks
Carbonated and silicified maficndashultramafic rocksinterpreted as part of the Narracoota Formation outcropin the Horseshoe anticlinal block (Plate 1) These rocksare compositionally heterogeneous and both underlie andare intercalated with rocks of the Horseshoe FormationThis suggests that the interleaving is tectonic becauseelsewhere in the Bryah Group the Horseshoe Formationis not observed to be in direct contact with the NarracootaFormation (Occhipinti et al 1999)
Jasperoidal chert
Jasperoidal chert pods are present locally within theNarracoota Formation (Gee 1987 Hill and Cranney1990 Pirajno and Occhipinti 1998) but are commonlytoo small to be represented individually on geologicalmaps One of the largest pods outcrops 15 km due southof Ruby Duffer Well in the southern part of BRYAH Windh(1992) investigated the chert pods in some detailgeochemically discriminated them on the basis of theirNiCr ratios and distinguished jasperoidal syngeneticexhalative chert silicified volcanic or sedimentary rockssilicified shear zone rocks and surface silicificationSeveral of these chert pods such as those in theNarracoota Formation south of the Peak Hill Schist innorthern BRYAH are quartz mylonites mdash probably Windhrsquos(1992) silicified shear zone rocks A few may be chemicalprecipitates deposited by hot springs whereas others mayrepresent silicified fault zones
The cherty material is reddish to grey colouredmassive to banded and extensively veined by quartzThe chert consists of very fine grained recrystallizedquartz with equant to elongate polygonalndashgranoblastictextures locally with a crystallographic preferredorientation Minute opaque minerals locally includingmagnetite or pyrite define trails parallel to the quartzfoliation In the Yarlarweelor opencut (Fortnum mine)pebbles of these cherts in overlying mafic fragmentalrocks suggest that the cherts formed as exhalative horizonsrelated to volcanism Alternatively the jasperoids mayrepresent iron-rich silicification along major shear zonesIn the Yarlarweelor opencut the chert pods host epigeneticgold mineralization in and around quartz(ndashpyrite) veinsystems (Hill and Cranney 1990)
Geochemistry of the Narracoota Formation
Major trace and rare earth element (REE) whole-rockanalyses of samples of metabasite rocks of the NarracootaFormation collected during this study are included in thedigital dataset in the back pocket These data were usedto characterize the geochemistry of the volcanic rocks ofthe Narracoota Formation in an attempt to better definethe rock types and gain an insight into the nature of theparent magma(s) and tectonic setting Representativeanalyses of Narracoota Formation rocks are presented inTable 2
The Narracoota metabasite rocks are commonly oftholeiitic composition with mixed mid-ocean ridge basalt(MORB) ndash oceanic island and continental geochemicalsignatures They span the range from high-Mg basalt tokomatiite and peridotitic komatiite or peridotite (possiblysubvolcanic cumulates) Common characteristics includehigh MgO high Ni and Cr moderate to low REEabundances and nearly flat chondrite-normalized REEpatterns with weak Eu anomalies possibly reflectingdepleted asthenospheric mantle sources (Pirajno and Davy1996 Pirajno et al 1996 Pirajno and Occhipinti 1998Occhipinti et al 1998ac) There are subtle chemicaldifferences between the hyaloclastites and maficndashultramafic schists (Tables 3 and 4 see below)
Hynes and Gee (1986) and Pirajno and Davy (1996)reported on the petrochemistry and tectonic setting ofthe Narracoota Formation metabasite rocks Hynesand Gee (1986) concluded that they have fairlyuniform chemistry and are of MORB affinity although theoriginal mafic volcanic rocks may have been emplacedthrough the rifting of continental crust Pirajno and Davy(1996) proposed that the Narracoota Formation meta-volcanic rocks might have formed in a setting analogousto that of the present-day Gulf of California (Lonsdaleand Becker 1985) The origin of the NarracootaFormation metabasites is discussed in Tectonic model andconclusions
Classification based on chemistry
The total alkali ndash silica (TAS) and high-Mg plot(Le Maitre 1989) indicates that the bulk of the rocks ofthe Narracoota Formation range in composition fromkomatiitendashpicrite through basalt to basaltic andesite
12
Pirajno et al
Table 2 Representative chemical analyses of the Narracoota Formation
Rock _________________ Mafic schist _________________ _______ Hyaloclastite _______ _______ Ultramafic _______ ____ Trillbar __type schist ComplexSample 132788 132789 132790 133033 133050 112643 116485 104256 132791 139138 139139 135482 143538
Percent
SiO2 5424 4945 5277 463 4907 5187 5139 5011 4923 4723 4789 5137 4961TiO2 028 113 031 019 026 073 063 053 019 016 017 037 141Al2O3 1422 1172 1466 948 794 138 1512 1503 1043 765 867 1481 1391Fe2O3 248 345 184 661 635 224 296 278 146 396 201 232 561FeO 598 824 705 741 101 848 662 529 834 548 708 561 717MnO 017 019 018 025 198 02 016 014 018 012 015 016 022MgO 929 1243 1036 1517 778 1036 83 936 2063 2877 2678 869 656CaO 1106 1107 962 1451 2262 974 1144 1514 86 641 704 1068 1136Na2O 218 212 274 003 009 216 32 145 092 018 019 306 204K2O 007 008 046 001 284 036 01 011 002 003 001 006 022P2O5 003 013 002 003 007 007 006 005 001 001 001 003 011Total 10000 10001 10001 9999 10001 10001 9998 9999 10001 10000 10000 9716 9822
Mg 6687 6615 6795 6692 6736 6377 6142 6816 792 85 843 ndash ndash
Parts per million
Ag ndash ndash ndash ndash ndash 1 ndash 1 ndash ndash ndash ndash ndashAs 155 157 052 22551 13032 ndash ndash ndash ndash 832 ndash ndash ndashAu ndash ndash ndash ndash ndash 104 ndash ndash ndash ndash ndash ndash ndash
Ba 55 140 79 27 2 846 341 127 92 74 37 102 39 322Cd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash
Co 55 86 58 223 51 ndash ndash ndash 99 113 111 ndash ndash
Cr 509 1 201 686 2 574 72 489 364 283 1 836 2 530 3 146 593 82Cu 168 124 63 327 20 108 101 39 55 9 11 59 172Ga 10 16 10 8 9 12 12 13 8 6 6 12 19Hf ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 07 14Mo ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 08 26Nb ndash 63 ndash ndash 52 ndash ndash ndash ndash ndash ndash 1 9Ni 203 548 241 1 274 91 258 143 164 866 1 531 1 230 124 98Pb ndash 2 ndash ndash 7 ndash ndash ndash ndash ndash ndash 1 4Pd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashPt ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashRb 1 ndash 6 ndash 85 6 ndash 2 ndash 1 ndash 1 4Sb ndash ndash ndash ndash ndash 415 ndash 511 ndash ndash ndash ndash ndashSc 50 41 51 31 10 ndash ndash ndash 40 34 38 51 48Sr 64 149 64 54 100 163 82 188 23 23 7 61 279Ta ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashTh ndash 104 ndash ndash 717 ndash ndash ndash ndash ndash ndash ndash ndashU ndash ndash ndash 064 13 ndash ndash ndash ndash ndash ndash 08 14V 196 277 202 138 78 250 249 217 144 115 143 235 362W ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashY 13 18 12 8 16 17 14 11 8 6 7 17 24Zn 65 94 68 45 50 85 73 55 62 51 45 61 91Zr 13 68 15 17 50 51 47 38 7 7 8 20 86
La 089 936 043 054 1819 36 35 35 093 017 056 2 6Ce 218 2264 129 084 4445 9 83 83 153 042 082 2 15Pr 037 29 02 02 418 12 11 13 02 009 019 0 2Nd 166 1193 108 102 1511 57 51 57 102 047 079 5 12Sm 08 328 065 056 306 15 14 15 065 03 034 ndash ndashEu 042 13 032 028 223 09 07 08 029 011 011 ndash ndashGd 166 409 141 085 305 23 17 2 129 065 071 ndash ndashTb 04 069 031 018 04 04 04 04 029 014 016 ndash ndashDy 268 408 233 12 202 27 24 24 214 108 116 ndash ndashHo 071 087 057 028 037 05 05 05 053 027 03 ndash ndashEr 222 231 173 094 115 18 15 16 162 083 091 ndash ndashTm 039 033 027 016 017 02 02 02 027 014 015 ndash ndashYb 229 196 182 115 125 15 14 15 166 086 09 ndash ndashLu ndash ndash ndash 019 02 02 02 02 ndash 013 014 ndash ndash
13
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(Fig 12) A small number of samples plot in the boniniteand andesite fields All metabasites of the NarracootaFormation (ultramafic and mafic schists and basaltichyaloclastite) are of subalkaline tholeiitic affinity (Fig 13)They commonly have restricted silica contents rangingfrom 45 to 55 wt (Fig 12)
The metabasites are all quartz albite anorthitediopside hypersthene and magnetite normative Themafic schists are hypersthene normative with lowerMgO contents (lt15 wt) and magnesium numbers (Mgmdash defined as MgO(FeO + MgO)) ranging from 43 to 74(Table 3) Some mafic schists have no quartz and areolivine normative (5ndash6 and up to 20 in some maficschists) The ultramafic schist is hypersthene and olivinenormative with MgO contents ranging from 153 to227 wt and Mg ranging from 75 to 86 (Table 3) Themetabasaltic hyaloclastites are albite and clinopyroxenenormative and have MgO contents of lt10 wt and Mgof between 47 to 68 (Table 3)
Ultramafic schist mafic schist and metabasaltichyaloclastite can be distinguished in terms of their Cr Niand Ti abundances FeOMgO ratios (Tables 3 and 4Figs 14a and 14b) and chondrite-normalized REEpatterns The hyaloclastite rocks are depleted in Cr andNi and enriched in TiO2 relative to the maficndashultramaficrocks (Fig 14c)
The Jensen (1976) cationic plot is based on theproportion of Fe2++Fe3++Ti versus Al and Mg cationsrecalculated to 100 and is particularly useful fordiscriminating subalkaline and Mg-rich metamorphosedvolcanic rocks in which the alkali content may havebeen modified during deformation and metamorphism(Rollinson 1993) In the Jensen plot (Fig 15a) the
Narracoota Formation rocks span the range of compo-sitions from high-Mg tholeiite through to komatiite andperidotitic komatiite in a trend of increasing MgO
Chondrite-normalized rare-earth element diagramscommonly regarded as the most useful of the traceelement plots in the petrogenesis of igneous rocks areused to determine the possible nature and source of themelts Particularly important are the overall patterns fromlight to heavy rare earth elements (LREE to HREE) thenormalized abundance of Eu controlled by feldspar andthat of Ce controlled by seawater or hydrothermal fluidsFor the Narracoota Formation rocks chondrite-normalizedREE abundances (Figs 15b and 15c) are commonly low(lt1 to lt40 times chondrite) The mafic schist ischaracterized by a spread in LREE from depleted toenriched (Fig 15b) with individual patterns almostidentical to those of mid-ocean ridges (OrsquoNions et al1976 Schilling 1982) and the recent basaltic lavas ofIceland (Schilling et al 1982) More specifically theLREE-depleted patterns (western Bryah Basin) arestrikingly similar to those of the Lau Basin spreadingcentre in Fiji (Pearce et al 1995) whereas slightlydepleted to slightly enriched LREE patterns (eastern Bryah
Table 3 Magnesium numbers for the Narracoota and Killara Formations
Rock Formation Range of Mg Average Mg Standard deviationof Mg
Metabasaltic hyaloclastite Narracoota 4677 ndash 6816 5716 525Mafic schist Narracoota 4337 ndash 7409 5957 669Ultramafic schist Narracoota 7516 ndash 8560 8105 254Tholeiitic basalt Killara 3504 ndash 6603 5035 739
NOTE Mg Magnesium number defined as MgO(FeO +MgO)
Table 4 Selected geochemical parameters for the NarracootaFormation
Parameters Hyaloclastite Mafic schist Ultramafic(mean values) schist
(LaYb)N 144 1702 037TiO2 (wt) 086 068 019NiCr 043 039 042Al2O3TiO2 162 205 4668MgO (wt) 731 780 2119
35 45 55 650
1
2
3
4
foidite andesite
basalt
boninite
basalticandesite
MgOgt18 picrite
basanite
tephrite
MgOgt18 amp TiO lt1 komatiite
picrobasalt
FMP365 021199
22
2
2
2
2
MgOgt18 amp TiO gt1 meimechiteMgOgt8 amp TiO lt05
SiO (wt)
Na
O +
K O
(w
t)
Figure 12 Total alkali versus silica diagram (Le Maitre1989) for rocks of the Narracoota FormationNote that a small number of samples fall withinthe boninite field this however may be due tohydrothermal alteration
14
Pirajno et al
Basin) are comparable to those of seamounts reflectinga more enriched source The nearly flat patterns havenegative Eu anomalies reflecting the primitive nature ofthe rocks presence of olivine clinopyroxene andorthopyroxene and fractionation of feldspar from themelt The patterns of the Iceland basalts that are nearlyidentical to those of the mafic schist of the Bryah Groupwere explained by Schilling et al (1982) as due toadvection of asthenospheric mantle at a mid-ocean ridgeConsidering field relations and petrological andgeochemical data it is conceivable that the NarracootaFormation metatholeiites may have had a similar originChondrite-normalized REE abundances for the meta-basaltic hyaloclastite are very low (9 to 14 timeschondrite) slightly LREE-enriched and with a distinctpositive Eu anomaly (Fig 15c) reflecting the addition ofalbite due to seawater metasomatism
The overall REE abundances and patterns of maficschist and hyaloclastite are strikingly similar to192 ndash 184 Ga mafic rocks of the Flin Flon belt in theTrans-Hudson Orogen in Canada (Lucas et al 1996)Some of the mafic rocks of the Flin Flon belt have beeninterpreted to belong to tectono-stratigraphic assemblagesof ocean floor and ocean island affinity Also the Flin Flonocean island tholeiites have REE patterns similar to
Figure 13 Total alkali versus silica diagram (Le Maitre 1989)defining limits of alkaline and subalkaline basaltsshowing the predominantly subalkaline nature ofthe Narracoota Formation
20
16
12
8
4
0
Na
O +
KO
(w
t)
22
857565554535
SiO (wt)2 11999FMP367
Hyaloclastite
Mafic schist
Ultramafic schist
Subalkaline
Alkaline
Figure 14 Geochemical characteristics of the NarracootaFormation a) TiO2 versus FeOMgO ratios notethe slight TiO2 enrichment of metabasaltichyaloclastite compared to maficndashultramafic schistb) Cr versus FeOMgO ratios note the Cr enrichmentof maficndashultramafic schist compared to meta-basaltic hyaloclastite c) TiO2ndashNindashCr triangular plotshowing Ni and Cr enrichment of maficndashultramaficschist compared to metabasaltic hyaloclastite
3
2
1
0
TiO
(wt
)2
1 2FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
4000
3000
2000
1000
0
Cr
(ppm
)
1 2 3FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
TiO 1002
Ni Cr91199FMP368a
Hyaloclastite
Mafic schist
Ultramafic schist
a)
b)
c)
15
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Hawaiian tholeiites (Stern et al 1995) The inference fromthese comparisons is that submarine volcanoes may havebeen a component of the Narracoota Formation
Tectonic discriminant diagrams do not provide reliableinformation on the palaeotectonic environment withinwhich igneous rocks were emplaced (Duncan 1987 Wangand Glover 1992) Nevertheless if there is petrologicalevidence that the rocks have not undergone extensivecrystal fractionation and the overall geological context is
taken into account selected discriminant diagrams can beused to estimate palaeotectonic settings With the aboveconsiderations in mind and remembering that the rocksin question have a subalkaline chemistry the FeO(tot)ndashMgOndashAl2O3 plot of Pearce et al (1977) is deemedappropriate (Fig 15d) The FeO(tot)ndashMgOndashAl2O3 plot hasbeen used successfully in geologically well constrainedareas (Breitkopf and Maiden 1988) The FeO(tot)ndashMgOndashAl2O3 plot suggests that the Narracoota Formationvolcanic rocks were formed in tectonic environments of
a)
c)
b)
d)
MgO
TA
TDTR
CR CDCA
HFTBK
PKCB
HMT
Sam
ple
chon
drite
100
10
2La Pr Eu Tb Ho Tm Lu
Ce Nd Sm Gd Dy Er Yb
La Pr Eu Tb Ho Tm LuCe Nd Sm Gd Dy Er Yb
Sam
ple
chon
drite
100
10
1
6
FeO
MgO
221199
Al O32
FeO + TiO2
Al O32
FMP154
Mafic and ultramafic schist
Metsabasltic hyaloclastite(tot)
Figure 15 Geochemical discriminant plots for Narracoota Formation rocks a) Jensen (1976) cationic plot showingrange of compositions from high-Mg tholeiite (HMT) through high-Fe tholeiite (HFT) basaltic komatiite(BK) peridotitic komatiite (PK) tholeiitic andesite (TA) tholeiitic dacite (TD) calc-alkaline basalt (CB)and calc-alkaline andesite (CA) b) Chondrite-normalized rare-earth element plot of mafic (HREE-enriched) and ultramafic (HREE-depleted) schist (normalizing factors after Sun 1982) c) Chondrite-normalized rare-earth element plot of metabasaltic hyaloclastite (normalizing factors after Sun 1982) d)Triangular discriminant plot (Pearce et al 1977) showing the tectonic environment of the NarracootaFormation Tectonic fields are as follows 1) spreading-centre island 2) orogenic 3) ocean ridge andfloor 4) ocean island and 5) continental
16
Pirajno et al
MORB ndash oceanic island to continental affinity (Fig 15d)This diagram however has limitations if the rocks havebeen subjected to ocean-floor metamorphism A moreuseful plot is the TiO2ndashFeO(tot)ndashMgO plot which was usedby Breitkopf and Maiden (1988) in their study of theNeoproterozoic Matchless Amphibolite Belt of theDamara Orogen in Namibia The TiO2ndash FeO(tot)ndashMgO plotsupports the gradation from MORB towards continentalflood basalt because the hyaloclastite rocks plot closer tothe continental field than do the mafic schist (Fig 16) Thisfeature together with other considerations such as Mgand geological and petrological constraints indicate thatthe hyaloclastite was erupted on a continental rift marginThis has important implications for the tectonic evolutionof the BryahndashPadbury Basin as explained in Tectonicmodel and conclusions
Ravelstone Formation
The Ravelstone Formation is poorly exposed in scatteredlow outcrops over a wide area in the northern and centralparts of the Bryah Basin Rocks of the RavelstoneFormation were previously considered by MacLeod(1970) and Gee (1979 1987) to belong to the lsquoThadunaGreywackersquo (now Thaduna Formation of the YerridaGroup) for which the type area is about 100 km to theeast-northeast on THADUNA (Pirajno and Adamides 1998)
The Ravelstone Formation comprises a succession oflithic and quartz wacke shale and siltstone that was
deposited from turbidity currents In the north theRavelstone Formation contains lenses of chert andis unconformably overlain by the MesoproterozoicBangemall Group West of the Peak Hill opencut thelower contact with the Narracoota Formation is dis-conformable whereas the upper contact with theHorseshoe Formation appears to be conformable In thecentral and northern parts of BRYAH the RavelstoneFormation although metamorphosed has no tectonitefabric On MILGUN (around Fortnum) however a well-developed foliation is present
Drillcore from the Harmony gold deposit shows thatthe contact between the base of the Ravelstone Formationand the top of the Narracoota Formation is interfingeredpossibly due to shearing The disconformable contactbetween the base of the Ravelstone Formation and the topof the Narracoota Formation is exposed in a river bedabout 1 km due east of the Fortnum ndash Peak Hill turn-offIn this area graded layers of immature subarkosicsandstone to siltstone contain fresh plagioclaseK-feldspar sericitized lithic fragments and angular quartzgrains in a matrix composed of sericite and biotite Inaddition the siltstone contains euhedral crystals oftourmaline Metamorphic brown biotite and muscovite areabundant and replace feldspars quartz and lithicfragments Lithic fragments include massive chlorite(ndashrutile) derived from mafic precursors chert hematitendashquartz shale as well as partly sericitized feldspar grainsQuartz grains include rounded to irregular shapes andbiotite is metamorphic in origin Quartz white micachlorite and variable amounts of carbonate are part of thefine-grained matrix Well-developed foliation wherepresent is defined by aligned sericite elongate quartzand to a lesser extent feldspar grains and by mica seamsNew muscovite flakes have grown along and across thefoliation
In the Fortnum mine area on MILGUN graded beddedlithic wacke and siltstone overlie the volcanic rocks of theNarracoota Formation The wacke contains medium tocoarse-grained crystals of feldspar (plagioclase minor K-feldspar) and quartz as well as fragments (fine metabasaltand chlorite) derived from mafic volcanic rocks Thefeldspar crystals which are strongly sericitized dominateover quartz The matrix consists of sericitendashchloritendashquartz with or without carbonate The reworked rocksinclude fragmental layers with fine metabasalt debris andgraded chloritic siltstone containing plagioclase laths Thederivation of the mafic component is easily explained butthe well-preserved feldspar crystals suggest nearbygranitic or felsic volcanic precursors
Horseshoe Formation
The Horseshoe Formation occupies areas west of thePeak Hill opencut and the northern parts of BRYAH
and MILGUN This formation includes finely laminatedferruginous (hematitic) shale and siltstone fine-grainedquartzndashfeldspar wacke with interleaved iron formation andchert graded quartz wacke manganiferous shalegarnetiferous biotitendashchlorite schist and garnetiferousiron-formation Relatively high manganese contents areinferred from the abundant manganese oxide staining in
CFB
MORB
20
18
15
13
10
08
05
03
000 1 2
TiO
2
FMP168 211099Ultramafic schist
Mafic schist
Hyaloclastite rocks
(tot)FeO MgO
Figure 16 TiO2 versus FeOMgO plot (Breitkopf and Maiden1988) for the Narracoota Formation showing themid-ocean ridge basalt (MORB) affinity of the maficand ultramafic schist and the transitional chemistryof the hyaloclastites towards continental floodbasalts (CFB)
17
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
weathered and lateritic rocks and lateritic manganese orehas been mined at the Horseshoe and Mount Padburymines The type area of the Horseshoe Formation is theHorseshoe Range (Occhipinti et al 1997) where athickness of approximately 1000 m was estimated by Gee(1979) The Horseshoe Formation overlies the NarracootaFormation however the contact is either conformable ortectonic Elsewhere on JAMINDI north of BRYAH theHorseshoe Formation overlies the Ravelstone Formationand the contact is gradational and conformable TheHorseshoe Formation underlies the Labouchere Formationof the Padbury Group The nature of this upper contactappears conformable however Martin (1994) suggestedthat there is a regional unconformity between these units
Structurally the Horseshoe Formation forms a broadsyncline with its axis trending approximately easterly Thesouthern limb of this syncline is in sheared contact withrocks of the Narracoota Formation In this area theHorseshoe Formation is complexly folded with axestrending 070deg parallel to the shear zone
In the Horseshoe Range Gee (1987) recognized threeunits 1) a lowermost part consisting of regularly beddedwacke and shale similar to the underlying Ravelstonesuccession but finer grained more calcareous andcontaining less chlorite and more feldspar and quartzindicative of a granitic rather than mafic volcanicprovenance 2) a middle iron-formation member withseveral BIF (chertndashmagnetitendashstilpnomelane white chert)horizons intercalated with chloritic shale and 3) anupper unit of calcareous manganiferous shale andwacke The lowermost unit is exposed on MILGUN in thelow hills east of Fortnum airstrip where fine-grainedcarbonate-cemented wacke and shale contain dis-harmonic-folded white-chert lenses (2ndash12 cm thick) andless common discontinuous quartzndashmagnetite layers(2ndash3 cm) The quartz wacke component of the HorseshoeFormation contains quartz plagioclase microclinebiotite and muscovite all as detrital minerals Nearthe Peak Hill opencut the iron formation is made upof biotite amphibole chlorite quartz magnetite andgarnet This unusually high grade assemblage may berelated to the metamorphism of the Peak Hill Schist (seeMetamorphism)
About 1 km north of the Ravelstone manganesedeposits a reasonably good exposure of the HorseshoeFormation was examined in detail A stratigraphic columnfor this locality is shown in Figure 17 This is a foldedupward-coarsening package approximately 350 m thickwhich from base to top consists of quartzndashlithic wackewith banded chert interbeds displaying a well-developedaxial planar cleavage quartz wacke with iron formationand shale interbeds massive beds of coarse-grainedquartzndashlithic wacke intercalated with thin granular iron-formation amphibole- and garnet-bearing granular iron-formation layers and massive quartzndashlithic wackeintercalated with thin iron-formation bands The quartzndashlithic wacke contains chert clasts detrital subangularquartz fresh plagioclase crystals and biotite in a matrixof sericite green chlorite and iron oxide grains Bandedcherty material is composed of granular quartz aggregatesbrown biotite actinolite and very fine carbonate-richlaminae (this rock is best classified as a quartzndashbiotitendash
actinolite schist) The granular iron-formation consists ofgranular aggregates of quartz and iron oxides withinterstitial biotite and chlorite Syntectonic garnetporphyroblasts are replaced in part by quartz andcarbonate Massive lithic wacke consists of a packedaggregate of angular quartz feldspar and chert grains thematrix is volumetrically small and made up of biotitequartz and sericite Garnetiferous iron-formation has darklaminae of quartz granules with interstitial actinolitendashchlorite iron oxides and light-coloured microbands (1 cmthick) of quartz with actinolitendashchlorite iron oxides anddisseminated synndashlate-tectonic garnet porphyroblastsGarnet is also present as porphyroblasts growing acrossmicroband boundaries
Padbury GroupThe Padbury Group locally unconformably overliesthe Horseshoe Formation of the Bryah Group but inplaces is in faulted contact with the Bryah Group andYarlarweelor gneiss complex (Narryer Terrane Yilgarn
FMP156 020300
0
100
200
300
intercalated with thin BIF and shale interbeds
Garnetiferous BIF
Massive beds of coarse-grained lithic wackewith interbeds of garnetiferous BIF and
Banded iron-formation interbedded with massive
Banded chertQuartzndashlithic wacke with carbonate cement
wacke and soft granular iron-formation
(m)
granular iron-formation
Massive quartzndashlithic wacke layers
Micaceous wacke
Figure 17 Schematic stratigraphy of the HorseshoeFormation from an area of outcrops about 12 kmwest-northwest of the Peak Hill mine (after Pirajnoand Occhipinti 1998 width of column reflectsrelative resistance to weathering)
18
Pirajno et al
Craton Fig 2) Considerable onlap of the Padburysuccession onto the various formations of the Bryah Groupcan be inferred these contacts were faulted possibly inseveral stages during basin closure The age of thePadbury Group is poorly constrained Nelson (1997)reported a maximum age of c 20 Ga from the upper partof the Wilthorpe Formation and Windh (1992) inferred aminimum age of c 18 Ga from a leucogranite dyke
Martin (1994 1998) proposed a formal stratigraphy forthe lower Padbury Group based on detailed sediment-ological studies in the area covering the southeastern andcentral parts of MILGUN This formal stratigraphy replacedprevious stratigraphic divisions (Barnett 1975 Gee1979 1987 Windh 1992) and has since beenexpanded to include two distinct lithostratigraphic unitsas members within the Wilthorpe Formation the Heinesand Beatty Park Members (Occhipinti et al 1997) Martin(1994 1998) interpreted the Labouchere and WilthorpeFormations as an upward-coarsening deep-water turbiditecomplex overlain by shales and iron formation of theRobinson Range Formation The turbidites were derivedby erosion from the granitendashgneiss basement (YilgarnCraton) and by reworking of underlying sedimentary andmafic volcanic rocks in the Bryah Basin
The Padbury Group contains quartz wacke siltstoneconglomerate iron formations hematitic shale and minorclastic rocks and dolomite (Martin 1994 Occhipintiet al 1997) and is subdivided into four formationsLabouchere Wilthorpe Robinson Range and MillidieCreek Formations Martin (1994) interpreted the PadburyGroup to have been deposited in a retroarc foreland basinthat developed on top of the Bryah Group
Labouchere Formation
The Labouchere Formation occupies areas in thenorthwestern part of the Bryah Basin where it isfaulted against the Yarlarweelor gneiss complex Martin(1994 1998) suggested that the Labouchere Formationunconformably overlies the Horseshoe Formation(Bryah Group) based on the regional geometry inthe Fortnum mine ndash Dandy Well area on MILGUN Theregional unconformity is inferred from the low-angletruncation of an iron-formation marker unit in theHorseshoe Formation against lowermost quartz areniteof the Labouchere Formation in the area south ofYarlarweelor Creek North of the Fortnum Fault ironformation within the Horseshoe Formation is nearlyparallel to bedding in the Labouchere FormationElsewhere in the region contacts between variousformations of the Bryah and Padbury Groupsare interpreted as unconformities (Windh 1992) oralternatively as faults or shear zones (Pirajno andOcchipinti 1998 Occhipinti et al 1998b) On BRYAH theLaboucherendashHorseshoe Formation contact is marked bya conglomeratic unit The Labouchere Formation isconformably overlain by and grades into the WilthorpeFormation (Martin 1994) although this contact waspreviously described as an unconformity (Gee 1979) Gee(1979) estimated the Labouchere Formation (including theWilthorpe Formation) to be 5000 m thick extending from
Mount Labouchere on MILGUN (type area Martin 1994)to the Horseshoe Range the southern continuation ofwhich is in northwestern BRYAH Martinrsquos (1994 1998)type section is a composite stratigraphy (up to 7000 mthick) based on four separate sections in southeasternMILGUN
The Labouchere Formation consists of quartz arenitemedium- to coarse-grained sericitic quartz wacke andsericitic siltstone minor conglomerate and banded iron-formation in an upward-coarsening succession Near theHorseshoe manganese mining area the LabouchereFormation consists of a thick succession of upward-finingcycles up to 700 m thick Each cycle consists ofconglomerate or a coarse lithicndashquartzndashsericite wacke unitat the base grading up through coarse- to fine-grainedquartzndashfeldsparndashlithic wacke and sericitic siltstone to iron-rich shale These cycles however become increasinglycoarser upwards so that there is regional upwardcoarsening The base of the topmost cycle begins with aquartz-pebble conglomerate Minor and thin bands of iron-formation are locally present as intercalations within thesedimentary units
Quartz arenite contains grain-supported well-roundedquartz in a sericitic matrix and is extensively silicified Aprominent quartz arenite marker forms the ridge includingMount Labouchere north of Fortnum mine on MILGUN andcan be traced for many tens of kilometres to the southeastwhere gradually more quartz wacke is interbedded withthe arenite A second quartz arenite marker approximatelyhalfway up the Labouchere Formation is present in thearea north of the Fortnum Fault In the same area an ironformation ndash chert layer is present about 250 m above thissecond quartz arenite Martin (1994) emphasized that thedeep-water environment of this iron formation indicatesa similar depositional environment for the clastic rocksQuartz wacke has a matrix-supported framework ofvariably rounded quartz grains minor lithic fragments andfeldspar in a sericitendashchlorite matrix whereas laminatedshale consists of sericitendashchlorite Wacke and siltstoneform numerous upward-fining cycles
Muscovitendashquartz schist or slate developed fromquartz wacke and siltstone in zones of high strain andhigher metamorphic grade adjacent to the Yarlarweelorgneiss complex Strongly foliated quartz wacke andmuscovitendashquartz schist occupy a 4 km-wide zone nearthe Labouchere mine on MILGUN Another belt of schistand slate is present between the Billara Fault and DespairGranite in southwestern MILGUN These strongly foliatedrocks can be traced northwards into recognizable thoughstrongly foliated pebbly quartz wacke The fine-grainedschist consists of elongate polygonalndashgranoblastic quartzwith spaced trails of aligned muscovite flakes Beddingndashcleavage relationships are found in less-deformed areaswhereas in high-strain zones differentiated layeringdeveloped from a pervasive crenulation cleavage
Sericite is abundant throughout most of the rocks ofthe Labouchere Formation The quartzndashsericite wacke iscomposed of subangular quartz grains embedded in asericitized matrix with occasional large muscovite lsquobooksrsquoand scattered small crystals of tourmaline and anatase
19
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Quartzndashfeldsparndashlithic wacke is made up of subangularquartz grains polycrystalline quartz K-feldspar andplagioclase in a matrix of quartz sericite biotite andminor detrital zircons
Wilthorpe Formation
The Wilthorpe Formation (formerly lsquoWilthorpeConglomeratersquo Gee 1987) including the Beatty Park andHeines Members comprises quartz- and chert-pebbleconglomerate quartz wacke sericitic siltstone chloritendashquartz shale quartzndashsericitendashhematite schist dolomiticsandstone and finely laminated chert lenses TheWilthorpe Formation is conformably overlain by theRobinson Range Formation
Martin (1994) measured the type section of theWilthorpe Formation (about 1300 m thick) along theTalbot Divide In this area the characteristic quartz-pebbleconglomerate forms a prominent ridge to the east of hillsunderlain by the Robinson Range Formation In theFortnumndashLabouchere area on MILGUN the exact locationof the LaboucherendashWilthorpe Formation transitionalboundary is less well defined (Swager and Myers 1999)Along the western wall of the Nathans Deep Southopencut (labelled Nathan Deep on Plate 1) severalupward-fining cycles of quartz-pebble conglomerategrading into quartz wacke and quartzndashmuscovite siltstonecan be observed These cycles are underlain by fine-grained chloritic shale interbedded with quartz wackeThis chloritic shale with detrital ilmenite is derived froma mafic precursor probably the Narracoota Formation(Windh 1992) Occhipinti et al (1998a) recognizedcomparable lsquomaficrsquo clastic rocks as a mappable unit(Beatty Park Member mdash see below) at the top of theWilthorpe Formation on PADBURY
The conglomerate contains well-rounded slightlyelongate or faceted vein-quartz clasts and less commonlychert quartzite quartz wacke and rare siltstonendashmudstoneclasts in a quartz wacke matrix Clasts range in size frompebbles to boulders Quartzite pebbles locally containfolded foliation fabrics Bunting et al (1977) suggestedthat large quartzite boulders in the southern part of thetype area were derived from the basal Finlayson Memberof the Juderina Formation (Yerrida Group) Martin (19941998) recognized two polymictic conglomerate intervalsin the type area which included silicified dolomite clastsThese intervals are similar to the polymictic conglomerateand sandstone of the Heines Member defined on BRYAH
(Pirajno and Occhipinti 1998) Siltstone forms a distinctmappable upper unit along the gradational contact withthe Robinson Range Formation
Beatty Park and Heines Members
The Beatty Park Member outcrops in the Mount Padburyarea on PADBURY and contains clastic rocks that werepossibly sourced at least in part from the mafic volcanicrocks of the underlying Narracoota Formation (BryahGroup) with sedimentary chert lenses towards its top Asensitive high-resolution ion microprobe (SHRIMP)UndashPb date obtained from detrital zircons in one of these
chert lenses suggests a maximum age of 1996 plusmn 35 Ma(Nelson 1997) The clastic rocks of the Beatty ParkMember are dominated by metamorphosed chloritendashquartzshale siltstone and wacke several conglomeratic orbreccia lenses and finely laminated chert layers in places(Occhipinti et al 1997) The contact between the BeattyPark Member and the overlying Robinson RangeFormation is gradational with chloritic siltstone and chertlayers and lenses grading into sericitendashquartz siltstone Thelower contact of the Beatty Park Member with theWilthorpe Formation appears to be gradational in the areawest of the Fraser Synclinorium (see Structure) whereferruginized kaolinitic siltstone and quartz wacke gradeinto chloritic siltstone In this area the minimum thicknessof 470 m is implied because the upper part of the BeattyPark Member is not exposed
The shalendashsiltstone layers are well bedded to finelylaminated and consist of quartz and chlorite with minorsericite epidote feldspar titanite and detrital hornblendeThese layers are accompanied by very fine grainedrecrystallized white chert beds in the upper part of theBeatty Park Member West of the Fraser Synclinoriumsedimentary structures such as bedding-parallel lamin-ations flame structures and contorted bedding can beobserved within chloritic siltstone Two types of wackeunits are present one containing quartz dolomite chloritefeldspar sericite epidote sphene and opaque minerals(either magnetite or pyrite) and the other containingquartz feldspar muscovite epidote chlorite carbonateand opaque minerals Lithic fragments in wacke layersinclude metabasalt and mafic schists in which leucoxenepseudomorphs of iron oxides can still be recognizedLenses of coarse-grained lithic wacke and conglomeratecomprise rock fragments of basalt mafic schist chertchloritendashquartz wacke and coarse detrital grains (quartzfeldspar) in a sericitendashchloritendashquartz matrix Coarseclastic rocks fill channels that cut into the fine-grainedrocks and contain numerous rip-up clasts This suggeststhat at least in part the Beatty Park Member wasdeposited distally from the source region Locally whitechert lenses crosscut erosional contacts indicating that thechert is diagenetic or epigenetic
Within all rocks of the Beatty Park Member sericiteand muscovite are of metamorphic origin They replacechlorite in the fine-grained chloritic shalendashsiltstone layersand feldspar clasts in the wacke units In several examplesfine-grained muscovite has grown along late cleavageplanes
A quartzndashchloritoidndashsericitendashchlorite(ndashsulfide) unitpreviously interpreted to be a carbonate intrusion (Lewis1971 Elias and Williams 1980) has been assigned to theBeatty Park Member The chloritoid is crystallized insprays and displays a lsquobow-tiersquo texture The presence ofabundant chloritoid indicates that this rock has a highalumina content implying either a pelitic precursor or thatthe protolith was extensively metasomatized
The Heines Member consists of an upward-finingsuccession of sedimentary rocks with a polymicticconglomerate at its base followed by clastic sedimentaryunits (sandstone to shale) The type area is near Durack
20
Pirajno et al
Well on BRYAH At this locality the Heines Memberis folded into a syncline and its southern limb is in faultedcontact with the underlying Narracoota Formation Thenorthern contact is obscured here by the Cainozoic coverThe Heines Member includes those outcrops south of theRobinson Syncline at the Heines Find prospect RandellBore and 35 km northwest of Durack Well which werepreviously mapped as lsquoWilthorpe Conglomeratersquo byGee (1987) The succession is approximately 600 mthick although basal units may have been shearedoff along the faulted contact The basal polymicticconglomerate contains clasts of mafic lithic wackelimestone quartz arenite and hematitic shale supportedby a carbonate matrix This is followed upward by a seriesof sandstonendashshale units with the shale componentbecoming volumetrically greater with stratigraphic heightThe basal conglomerate of the Heines Member containsno volcanic clasts of the underlying Narracoota Formationand this is taken as evidence that the contact with the latterformation is tectonic The provenance of the various clastsin the basal conglomerate is not known In the Heines Findprospect area the Heines Member is overlain by theRobinson Range Formation
Robinson Range Formation
The Robinson Range Formation forms elongate outcropsthat extend from east to west in the centre of the BryahndashPadbury Basin and in a northerly direction on the easternmargin of the Yarlarweelor gneiss complex on MILGUN andPADBURY (Plate 1) The Robinson Range Formation isdefined by the appearance of ferruginous or hematiticshale followed by two iron formations mdash a well-definedlower banded unit separated by 100 m of ferruginousshale from an upper unit with clastic textures as mappedby Gee (1987) which is in turn overlain by hematitendashchlorite siltstone The Robinson Range Formation isconformably overlain by the Millidie Creek Formation
The Robinson Range Formation consists of asuccession of BIF siltstone and iron-rich shale Granulariron formation is present as irregular lenses The BIFconsists of laminae up to 3 cm thick These laminationscomprise various amounts of quartz iron oxides (hematiteor magnetite) biotite and locally ferro-actinolite Theshale and siltstone consist of fine-grained sericite quartzchlorite iron oxides and in a few places minor spheneThe mesostructure microstructure and petrology ofthe BIF are relatively simple Microbands or laminae lessthan 1 to 2ndash3 mm thick are made up of alternatingmicrocrystalline quartz(ndash iron oxides) greenndashbrownbiotite(ndash iron oxides) quartz grains(ndash acicular crystals ndashiron oxides) quartz grains(ndash iron oxides ndash biotite ndashacicular crystals) Commonly the quartz grain(ndash acicularcrystal) assemblage displays a polygonized texturesuggestive of annealing due to metamorphism Theacicular crystals are weathered to iron oxides but onthe basis of their morphology they could be eitherstilpnomelane crystals or amphiboles The iron oxides areeither hematite or magnetite Incident light microscopyreveals that a primary titaniferous magnetite is replacedby hematite which in turn is replaced by goethite in thesupergene environment The biotite is porphyroblastic and
mostly grown under conditions of peak metamorphism(see Metamorphism)
Granular iron-formation is characterized by a granulartexture and the presence of elongate peloids 1 to 4 mmlong The peloids consist of microcrystalline chert outlinedby rims of iron oxides (hematite with inclusions ofilmenite) The chert peloids are enclosed in finemicrocrystalline cherty or chalcedonic material Thepeloids and chert make up bands approximately 1 to15 cm thick with occasional laminae of fine chert(ndash ironoxides)
The ferruginous shale is composed of silt-sized quartzgrains and iron oxides with abundant interstitial biotiteand minor disseminated euhedral tourmaline crystals Thetourmaline was formed either during metamorphism or ahydrothermal event
The iron formations of the Robinson Range Formationhave been correlated with the granular iron-formation ofthe Frere Formation (Earaheedy Basin) 150 to 450 km tothe east-southeast by Hall and Goode (1978) whocompared them to those of the Lake Superior region inNorth America
Millidie Creek Formation
The Millidie Creek Formation defined by Barnett (1975)and modified by Gee (1979) and Occhipinti et al (1997)forms comparatively small outcrops in the cores of theRobinson Syncline and Fraser Synclinorium (seeStructure)
Ferruginous shale and siltstone intercalated withirregularly banded manganiferous iron-formation formsthe basal unit of the formation This unit is locallylateritized and hosts many manganese deposits suchas the Millidie (or Elsa) mine (see Mineralization)The banded manganiferous iron-formation commonlyforms low ridges On PADBURY the Millidie CreekFormation consists of iron-rich shale and siltstoneirregularly banded manganiferous iron-formationdolomitic sandstone ferruginous quartz wacke andchloritic siltstone On BRYAH the Millidie Creek Formationconsists of ferruginous shales with a well-developed pencilcleavage sandstone and minor granular iron-formation
Dolomitic sandstone and quartz wacke are locallypresent within this formation The quartz wacke is wellbedded matrix supported and commonly containssubangular to subrounded quartz grains The matrix of thisrock is composed of randomly oriented fine-grainedbiotite and includes late sphene and minor sericite Thedolomitic sandstone comprises carbonate quartz andmuscovite
In low hills 3 km north of 5 Mile Well (Plate 1) finelybedded micaceous siltstonendashshale with interbeddedquartzndashdolomite siltstone layers previously assigned to theLabouchere Formation (Elias et al 1982) have beenassigned to the Millidie Creek Formation These rocks arefolded about northwesterly trending D4 fold axes andcontain S4 foliation They are unconformably overlain by
21
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
subhorizontal to shallowly dipping basal quartz arenite ofthe Bangemall Group
Chloritic siltstone at the top of the Millidie CreekFormation is compositionally similar to the Beatty ParkMember and comprises quartz feldspar lithic fragmentsof sericitendashquartz schist and detrital cordierite grains ina foliated matrix of chlorite
Unassigned units of the Padbury Group
Metasedimentary rocks and biotitendashsericite schist whichoutcrop within the Despair Granite near the Wilthorpegold mine (Plate 1) were previously referred to aschloritendashmuscovitendashquartz schist and not assigned to anygroup (Elias et al 1982) Occhipinti and Myers (1999)tentatively assigned these units to the Padbury GroupThere are two main outcrops one in the Wilthorpe mineand the other just outside the mine as a fault-boundedinclusion within the granite
Sedimentary rock found within the Despair Graniteis heterogeneously deformed and metamorphosedSedimentary structures such as cross-bedding andbedding-parallel laminations are present This rockconsists of alternating layers of very fine grained biotitequartz sericite and feldspar Accessory minerals includeopaque minerals In a few places this rock contains afoliation parallel to faults or fold-axial planes Opaqueminerals commonly crosscut the dominant (bedding)fabric The preservation of the primary sedimentarytextures suggests that strong deformation did notaccompany low-grade greenschist-facies metamorphism ofthese rocks
Within the Wilthorpe mine the metasedimentary rockscontain a slightly different mineralogy and are in faultedcontact with the sericitized Despair Granite For instancein one sample there are two distinct layers composed ofeither sericite quartz biotite and opaque minerals orbiotite sericite quartz and minor opaque minerals Thisvariation in bedding composition is consistent with thatobserved in the metasedimentary rocks outcroppingoutside the mine The rocks within the mine are coarsergrained and comprise quartz biotite sericite andandalusite Sericite and biotite overprint the foliation inthe rock
StructureThe Padbury and Bryah Basins are pervasively deformedThis deformation may have solely occurred duringthe c 18 Ga Capricorn Orogeny a period of obliquecollision between the Archaean Pilbara and YilgarnCratons (Tyler and Thorne 1990 Tyler et al 1998Fig 2) or in part during the earlier c 20 Ga GlenburghOrogeny (Occhipinti et al 1999) In addition to deformingthe Bryah and Padbury Groups this deform-ation also resulted in the reworking of parts of theArchaean Narryer Terrane and the Marymia Inlier of theYilgarn Craton (Fig 2) to form the Yarlarweelor gneisscomplex and Peak Hill Schist The rocks of the Bryah
and Padbury Groups are locally interleaved with theYarlarweelor gneiss complex in the western part of theregion (Fig 18) To the south the Bryah and PadburyGroups are tectonically juxtaposed against autochthonousrocks of the Archaean Murchison Terrane of the YilgarnCraton and the Palaeoproterozoic Yerrida Group (Fig 2)
The Yarlarweelor gneiss complex dominantly consistsof Archaean granitic gneisses that were intruded by felsicmagmas at c 1960 Ma (Sheppard and Swager 1999) and1820ndash1800 Ma (Occhipinti et al 1998b Sheppard andSwager 1999) Granite sheets and veins intruded into theArchaean gneisses were pervasively deformed into opento tight folds and metamorphosed at medium to highgrades during the Capricorn Orogeny Occhipinti andMyers (1999) suggested that these folds were originallynortherly trending however they are probably more likelyto have been northeasterly trending Dextral strike-slipshear movement involved a transition from early ductileto later brittle deformation (Occhipinti et al 1998b)coincident with uplift which probably progressed fromnortheast to southwest in the region This deformationproduced regional-scale fault-bend folds in both theYarlarweelor gneiss complex and overlying Palaeo-proterozoic Bryah and Padbury Group rocks
Deformation histories presented for the Yerrida Bryahand Padbury Groups by various authors (including Windh1992 and Gee 1990) have many elements in common(Table 5) This includes major northndashsouth compressionthat was responsible for the development of prominentregional easterly trending upright folds such as theRobinson Syncline (Fig 18) Northerly striking folds andfaults in the domain just east of the Yarlarweelor gneisscomplex have been recognized as a later deformation stage(Windh 1992 Martin 1994) Gee (1990) Windh (1992)and Martin (1994) proposed that eastward movement ofthe Narryer Terrane (here referred to as the Yarlarweelorgneiss complex) was responsible for the development ofthese northerly trending folds In their interpretation thenortherly striking folds formed in front of an advancingthrust sheet of Archaean gneiss and granite overriding theBryah and Padbury Groups Myers (1989 1990) andMyers et al (1996) on the other hand regarded the Bryahand Padbury Groups as allochthonous sheets that werethrust over Archaean granitendashgneiss
Contacts of the Bryah and Padbury Groups with theNarryer Terrane Yarlarweelor gneiss complex MarymiaInlier Murchison Terrane and the PalaeoproterozoicYerrida Group are zones of high strain and thereforeinferred to be faults Unconformable contacts between theBryah and Padbury Groups were reported by Martin(1994 1998) whereas sheared and faulted contacts werereported by Pirajno and Occhipinti (1998) Occhipintiet al (1998ac) and Occhipinti and Myers (1999) Forexample the Bryah Group is in faulted contact with theYarlarweelor gneiss complex north of Livingstones Findand the Murchison and Narryer Terranes are separatedfrom the Bryah and Padbury Groups by the steep easterlytrending Murchison Fault which has a sinistral strike-slipcomponent (Plate 1 Fig 2)
The Goodin Fault a high-angle reverse fault (Pirajnoand Occhipinti 1998) is the boundary between the
22
Pirajno et al
Yerrida and Bryah Groups (Fig 2 Plate 1) East of thisfault the Doolgunna Formation (Yerrida Group) is foldedinto isoclinal upright folds however much of thedeformation in the Yerrida Group dies out rapidly to theeast and southeast To the west the Goodin Fault mergeswith the Murchison Fault which has juxtaposed the Bryahand Padbury Groups against the Yilgarn Craton TheMurchison Fault has a sinistral strike-slip componentwhich offsets Archaean structures in the Murchison andNarryer Terranes
In this Report four distinct groups of structuresD1ndashD4 representing progressive compressional deform-ation are recognized (Table 5) This deformation historyalthough in broad agreement with the previously publishedstructural histories (eg Windh 1992) recognizes separateearly layer parallel structures The structures resultingfrom the four deformation events are not developedeverywhere or with the same intensity everywhere
The earliest deformation events are defined in the PeakHill Anticline area as D1 layer-parallel mylonitic thrustfaults and originally subhorizontal folds overprinted byD2 upright eastndashwest striking regional folds Both D1 andD2 structures developed by northndashsouth compression and
can be interpreted as successive stages of progressivedeformation Northerly trending regional D3 folds andupright foliations recording eastndashwest compression areweakly developed in the Peak Hill Anticline but betterdeveloped and largely restricted to a domain immediatelyeast of the Yarlarweelor gneiss complex However thesenortherly trending structures do not always overprint oldereasterly trending structures and in places these two setsof structures (D2 and D3) tend to be mutually exclusivesuggesting that they probably developed during the sameprogressive deformation event Late medium-scale D4structures include west-northwesterly to northwesterlytrending subvertical foliations shear zones zones ofsmall-scale folding and faults now outlined by quartzblows These locally developed structures suggest latenorth-northeast to south-southwest compression
Major fold structures in the Padbury and Bryah Basinsare the Peak Hill Anticline Robinson Syncline MillidieSyncline Fraser Synclinorium Horseshoe Anticline andPadbury Syncline (Plate 1 and Fig 18) The Peak HillAnticline Robinson Syncline Fraser Synclinorium andMillidie Syncline all represent refolded folds The easterlytrending doubly plunging Robinson Syncline andPeak Hill Anticline are D2 folds refolded during D3 D1
Figure 18 Major regional structures in the Bryah and Padbury Groups (after Occhipinti et al 1998a)
FMP371
MARYMIAINLIER
YILGARNCRATON
Goodin
Fault
GROUPBANGEMALL
Murchison Fault
118deg30 119deg30
30 km
020300
YERRIDAGROUPPeak Hill
Anticli
ne
Robinso
n
Synclin
e
Nathan Syncline
Zone of D folding3
Padbury
Horseshoe Anticline
Wilthorpe F
t
BRYAH ANDPADBURYGROUPS
GOODININLIER
EARAHEEDYGROUP
25deg30
26deg00
Syncline
Millidie Syncline
FaultD fold trace3
D fold trace2
1
D fault1
Anticline
SynclineD ndash D thrust fault2
Yarlarweelorgneiss
complex
FraserSynclinorium
23
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
folds are also present within these structures (see D1structures) The Horseshoe Anticline appears to be a D3fold contained within the fault-bounded Horseshoeanticlinal block This fault-bounded block also appears tobe cut by northwesterly trending (D4) faults
D1 structuresThe first Palaeoproterozoic deformation event (D1)produced layer-parallel folds a locally pervasive S1schistosity mylonites and faults However because thesestructures were pervasively overprinted by D2 structuresthey are rarely observed F1 folds are locally observed inthe Peak Hill Antiform Robinson Syncline FraserSynclinorium an area 5 km northeast of Mount Fraserand the Millidie Syncline These folds are also observednear the Peak Hill mine in F2 foldndashhinge zones of quartzblastomylonites of the Peak Hill Schist (Fig 6) Here theyare small-scale rootless isoclinal plunge shallowlytowards the east and strike eastndashwest In the FraserSynclinorium and Millidie Syncline the F1 folds are small-scale isoclinal folds that plunge gently towards the east-northeast or west-southwest and strike east-northeasterlyF1 folds are also inferred from aeromagnetic data to bepresent within the Fraser Synclinorium and MillidieSyncline (Figs 18 and 19)
The Goodin and Murchison Faults may be D1 faultsthat were reactivated during D2 (Occhipinti et al 1998c)The Murchison Fault (Figs 18 and 19 Plate 1) separateslargely undeformed basaltic hyaloclastite rocks in thesouth from foliated mafic schists to the north
Mesoscale F1 folds in the shale and banded iron-formation of the Robinson Range Formation are observednear Mount Padbury north-northwest of Beatty Park Bore
(Plate 1) in the hinge zone of the Robinson Synclinenorth of Tank Well and northeast of Randell Bore TheseF1 folds are tight to isoclinal with shallow plunges thattrend to the east or west The F1 folds in the area areinterpreted as originally recumbent D1 zones of highstrain and mylonite developed locally mainly in thePeak Hill Schist (Pirajno and Occhipinti 1998) andalong contacts between the Yarlarweelor gneiss complexand Palaeoproterozoic cover rocks These mylonite zonesare not observed at higher stratigraphic levels within thebasin suggesting that they are restricted to a deeper crustallevel represented by the Peak Hill Schist and basementndashcover contacts Quartz blastomylonites and the CrispinMylonite (Pirajno and Occhipinti 1998) form continuousunits within the Peak Hill Schist (Plate 1) The internalstructure of these units suggests that they may be D1shear zones which were refolded during the laterdeformation events The original nature and orientation ofthese shear zones is not known The Crispin Myloniteconsists of quartzite pebble-and boulder-sized clasts in asericitendashquartz-rich matrix and has the appearance of aconglomerate For that reason it was mapped by Gee(1987) as the lsquoCrispin Conglomeratersquo However meso-scopic and microscopic structures indicate that it is amylonite (Figs 4 and 7) Both the quartzite clasts andmatrix contain a mylonitic fabric The Crispin Myloniteis interpreted as a lsquopseudo-conglomeratersquo (Raymond1984ab) formed by shearing probably along or close toa fault plane that separated an arkosic or granitic unit froma quartz-rich unit
Like the Crispin Mylonite the quartz blastomylonitesform arcuate lenses within quartzndashmuscovite schist of thePeak Hill Schist and are refolded by F2 and F3 folds Thequartz blastomylonites contain isoclinal and sometimesrootless F1 folds and are interpreted to have beendeformed in a ductile high-strain zone (fault or shear zone)during D1 It is not possible to determine the sense ofmovement during D1 because no shear sense indicatorswere observed during mapping
D2 structuresThe D2 deformation produced large-scale uprightregional F2 folds with variably developed S2 foliationas well as faults and shear zones These structuresare easterly trending recording northndashsouth shorteningHowever more complex patterns in the Mount Fraserarea suggest complicated refolding patterns ProminentD2 folds include the doubly plunging Robinson Synclineand the Padbury Syncline which has the hinge zonelargely sheared out (Fig 18 Plate 1) Mesoscale F2folds show steeper plunges and the S2 foliation becomesmore intense to the north A pervasive S2 foliation isdeveloped over large areas in the mafic schists ofthe Narracoota Formation The Goodin Fault is a high-angle reverse fault that forms the boundary between theYerrida and Bryah Groups This fault may have developedduring D2 because south of the fault the DoolgunnaFormation is folded into tight to isoclinal upright folds(with fold-axial surfaces subparallel to the Goodin Fault)that are similar to D2 folds in the Bryah and PadburyBasins
Table 5 Sequence of deformation events in the Bryah and PadburyBasins
Deformation Compressionevent
D4 North-northeastndashsouth-southwest compressionSmall-scale folds subvertical foliation shearzones faults with quartz blows all trending
280degndash310deg
D3 Eastndashwest compressionnorthndashsouth trending folds subvertical foliationsubvertical faults or shear zones localized eastof Narryer Terrane increasingly disharmoniceast-northeasterly trending folds eastwards
D2 Northndashsouth compressionupright tightndashisoclinal eastndashwest folds andsubvertical foliation eastndashwest shear zonessouth-verging thrust faults
D1 Northndashsouth compressionsubhorizontal mylonites thrusts and foldsmesoscale recumbent folds tightndashisoclinalrootless
24
Pirajno et al
The Livingstone Synform a steep easterly plungingtight fold on MOORARIE may be part of a larger scale D2fold structure that is confined between the Kerba Fault inthe north and the Mount Seabrook Fault in the south(Occhipinti and Myers 1999)
Within the Yarlarweelor gneiss complex graniticgneisses form open to isoclinal easterly to northeasterlyand northerly trending shallowly to steeply plungingfolds These folds plunge either to the east and northeastor to the west and west-southwest indicating that on a
Figure 19 Simplified geological map of the Bryah and Padbury Groups (after Occhipinti et al 1998a) See Figures20 22 and 23 for cross sections
118deg 119deg
25deg45
10 km
MarymiaInlier
YilgarnCraton
BangemallBasin
Bill
ara
Fa
ult
Wilt
horp
eF
Fortnum
25deg30
Goo
din
Faul
t
Kinders FaultNathan
Peak Hill
B
AC
Mt Fraser
Yarlarweelor gneisscomplex
(reworked NarryerTerrane)
YerridaBasin
PADBURY GROUP
BRYAH GROUP
RAVELSTONE FORMATION lithic wacke
KARALUNDI FORMATION clastic rocks
quartzndashmuscovitendashbiotitendashstaurolite schist
HORSESHOE FORMATION shale banded iron-formation
YERRIDA GROUP
WILTHORPE FORMATION conglomerate siltstone
PA
LA
EO
PR
OT
ER
OZ
OIC
Greenstone
Peak Hill Schist
AR
CH
AE
AN
Fault
Anticline
Syncline
ME
TA
MO
RP
HO
SE
D
NARRACOOTA FORMATION maficndashultramafic volcanic rocks
LABOUCHERE FORMATION quartz wacke siltstone
Unconformity
Mine
Cross-section
Undifferentiated rocks
MILLIDIE CREEK FORMATION Lithic wacke dolomitic sandstone siltstone banded iron-formation
Granite and graniticgneiss
ROBINSON RANGE FORMATION shale granular iron-formation banded iron-formation
140300FMP373
25
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
regional scale they are doubly plunging possiblyrecording later refolding and eastndashwest shortening (D3)These folds deform both the Archaean gneiss and c 1960and c 1820 Ma granite sheets that intruded the gneiss(Sheppard and Swager 1999 Occhipinti et al 1998c)They refold tight to isoclinal subhorizontal to shallowlyplunging folds in the Archaean granitic gneisses whichmay have developed during the Archaean
The sense of shear of the steeply dipping D2 shearzones could not be determined South of the Robinson andFraser Synclines regional anastomosing D2 shear zonesdeveloped in the basaltic rocks of the NarracootaFormation To the northeast this regional structurebecomes the Jensen Fault (Pirajno and Adamides 2000)which can be shown to have displaced the Meso-proterozoic Bangemall Group suggesting that the faultwas reactivated after this time Along the southern limbof the Fraser Syncline another fault extends into the D2shear zones mentioned above A shear zone cuts thesouthern limb of the Heines Syncline which lies betweenthe Robinson and Fraser Synclines
D3 structures and theirrelationship to D2 structuresNortherly trending D3 folds faults and locally an uprightS3 foliation indicating an eastndashwest compression are welldeveloped in the area east of the Yarlarweelor gneisscomplex Further east F3 fold intensities decrease andfolds are locally more disharmonic The D3 event wasresponsible for the doubly plunging nature of theRobinson Syncline and the Peak Hill Anticline
The Kinders Fault (Fig 20 Elias and Williams 1980)is a northerly trending D3 fault separating a wedge ofmafic volcanic schists of the Narracoota Formation(Bryah Group) from the Robinson Range Wilthorpeand Labouchere Formation rocks (Padbury Group) Thisfault lies along the western limb of the sheared-out hingeof the F3 Nathan Syncline (Plate 1 and Fig 18) Thissyncline was previously correlated with the PadburySyncline to the south (Elias and Williams 1980 Martin1994 1998) Part of the southerly plunging fold hingeof the Nathan Syncline is preserved in the Nathan minearea and the closure of this syncline can be traced furthernorth The wedge of maficndashultramafic schists of theNarracoota Formation was interpreted by Occhipinti et al(1998c) and Martin (1994 1998) to represent an F3anticlinal fold-thrust wedge overlying pervasively foliatedand metamorphosed quartz wacke of the LabouchereFormation to the west (Figs 19 and 20)
West of the Kinders Fault along the Billara Faultsericitendashquartz schist locally with quartz-pebbleconglomerate layers contains a pervasive S3 fabricF3 folds however are difficult to trace East of theKinders Fault open to close and locally tight to isoclinalfolds are outlined by marker beds in the Labouchere andHorseshoe Formations S3 foliations and moderate tosteep southerly plunging small-scale F3 folds are welldeveloped in the area of the Horseshoe Syncline andfurther north
Several observations suggest that D2 and D3 structuresmay not reflect two separate events but may havedeveloped contemporaneously in different domainsIntense D3 folding is largely restricted to the area betweentwo basement highs represented by the Yarlarweelorgneiss complex in the west and the Peak Hill Schist in theeast (Figs 18 and 19) In the domain just east of andadjacent to the Yarlarweelor gneiss complex there is noevidence for D3 refolding D2 (ie upright northerlytrending D3 folds overprinting upright easterly trending D2folds) even though weak northerly trending D3 foldsdeform easterly trending F2 folds around and within thePeak Hill Anticline
In the Mount Fraser area complex fold and foliationpatterns show orientations different from and transitionalto both the regional D2 and D3 deformation Large-scaleeast-northeasterly trending F2 folds such as the RobinsonSyncline and Peak Hill Anticline die out in this area TheMillidie Syncline can be traced from a west-northwesterlystrike (subparallel to and en echelon with the RobinsonSyncline) to a west-southwesterly strike and is then cutoff to the south by D3 faults (Figs 18 and 19)
These observations suggest that the intensity and trendof the D2 and D3 structures were influenced by their spatialrelationship to the Yarlarweelor gneiss complex and PeakHill Schist
D4 structuresD4 structures include mesoscopic chevron folds kinksshear zones and faults and were locally accompanied bythe development of a foliation These D4 structuresdeveloped locally throughout the Bryah and PadburyBasins Yarlarweelor gneiss complex and the northern-most part of the Murchison Terrane In the PadburyndashBryahdomain most structures trend between west-northwest andnorthwest although in the Yarlarweelor gneiss complexa few late structures trend between north-northwest tonorth Brittle faults cutting the Yarlarweelor gneisscomplex often show dextral strike-slip shear movement
MetamorphismRegional metamorphic zones within the volcano-sedimentary succession are related to the geometry of thePeak Hill Anticline and Yarlarweelor gneiss complex Thehighest metamorphic grade assemblages are found in thecontact zones between the Yarlarweelor gneiss complexand overlying metasedimentary rocks Assemblages inthe Peak Hill Schist and within quartzndashmica schists(Labouchere Formation) along faulted contacts withthe Yarlarweelor gneiss complex record upper greenschist-to lower amphibolite-facies conditions Within theYarlarweelor gneiss complex upper amphibolite-faciesconditions were reached as incipient (minimum) meltpatches within granitic gneiss and amoeboid textures inPalaeoproterozoic coarse-grained granite probablydeveloped during D2 (Sheppard and Swager 1999) In theBryah and Padbury Groups however metamorphismtypically does not exceed greenschist facies and east of
26
Pirajno et al
0
2
4
6
Fault
Kilo
met
res
Southwest Northeast
FMP372
0
2
4
6
Kilo
met
res
West East
Billara
Fault
Kilo
met
res
0 Padbury
South North
SynclineDome
2
4
6
Yarlar-weelor
170300
Fault
Kinders
MIDDLE PROTEROZOIC
ARCHAEAN (reworked during Early Proterozoic)
Bangemall Group
Unconformity
Bedding or layering trend
Foliation
High-strain zone
Fault
Movement along fault
Movement away and towards observer
2
BRYAH GROUP
Geological boundary
Padbury Basin
Bryah Group
S N
d)
sediment fluxsediment flux
EARLY PROTEROZOICPADBURY GROUP
ARCHAEAN (in situ)
Peak Hill Schist quartzndashmuscovite schistquartz mylonite phyllonite
Granitendashgreenstone Murchison Terrane
Millidie Creek Formation sandstoneshale dolomitic siltstone
Robinson Range Formation ferruginous shalebanded iron-formation
Wilthorpe Formation quartz-pebbleconglomerate
Labouchere Formation quartz wackesiltstone quartz arenite
Horseshoe Formation ferruginous shaleiron formation
YERRIDA GROUP
Narracoota Formation metabasalt subordinatedolerite picrite and peridotite
Goodin
Normal fault reworked during D thrusting
Granite gneiss and granite with lenses of supracrustal rock Narryer Terrane
GranitendashgreenstoneMarymia Inlier ndash Murchison Terrane
Ravelstone Formation lithic wacke
Karalundi Formation clastic rocks
a) Cross section A
b) Cross section B c) Cross section C
Undifferentiated rocks
27
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
the Goodin Fault in the Yerrida Group metamorphic gradedecreases to subgreenschist facies (prehnitendashpumpellyite)The relationships between metamorphic mineral growthand deformation are summarized in Table 6
M1 was a prograde regional metamorphic event thattypically reached greenschist facies (Pirajno andOcchipinti 1998) and was probably coincident withD1 in the Bryah and Padbury Groups and Peak Hill SchistThornett (1995) suggested that some parts of the Peak HillSchist reached amphibolite-facies metamorphism withtemperatures between 500deg and 620degC and pressures of65 ndash 7 kbar Metamorphic mineral assemblages observedhowever commonly do not concur with these data Thesecond metamorphic episode M2 was commonly one ofretrogression throughout most of the Bryah and PadburyBasin and probably associated with metasomatismin high-strain zones during D2ndashD3 During M2 inthe western part of the Bryah and Padbury Basinsadjacent to the Billara Fault (Fig 18) staurolitendashandalusitendashbiotitendashmuscovitendashquartz schist developedfrom the metamorphism of Padbury Group sedimentaryrocks These rocks indicate metamorphism at amphibolitefacies Inclusion trails in staurolite and andalusiteporphyroblasts suggest that the porphyroblastic growthoccurred after D1 but before D2 The S2 foliation is definedby the alignment of muscovite and biotite which wrapsaround the porphyroblasts and probably developed in D2during M2 As staurolite is locally partially replaced byfine-grained muscovite this foliation may have developedin the greenschist facies This foliation is locallyoverprinted by chloritoid Further west at the contactbetween the Palaeoproterozoic Kerba Granite and theNarracoota Formation a quartzndashkyanitendashtremolitendashfeldspar schist indicates upper greenschist-faciesmetamorphism with the pressure of metamorphismestimated to have been between 3 and 4 kbar (Spear 1993Occhipinti and Myers 1999)
For the most part M2 involved retrogression meta-somatism and local hydrothermal alteration Mineralassemblages formed during M2 are commonly observedin high-strain zones where the S2 schistosity is welldeveloped These include a domain of well-developed D2shear zones south of the Robinson Syncline wherepervasive retrogression of metabasalts to actinolitendashchlorite schist is observed (Pirajno et al 1995a) In
addition in the Mount Pleasant opencut growth of albiteporphyroblasts and the development of chlorite at theexpense of biotite and epidote also occurred during M2
Banded iron-formation in the Robinson RangeFormation shows a change in metamorphic mineralassemblage from east to west across the trend of the D2Robinson Syncline To the west randomly oriented biotiteoverprinted quartz stilpnomelane and iron oxides Theappearance of this late-stage biotite coincides withregional geochemical trends (elevated Sb As and WDavy et al 1999) along the same structure suggesting alate- or post-D2 low-temperature metasomatic eventAlbite porphyroblasts in alteration zones associated withgold mineralization in the Peak Hill Schist also grew at alate stage because they overprint S2
South of the Murchison Fault little-deformed basaltichyaloclastites contain mineral assemblages characteristicof prehnitendashpumpellyite to lower greenschist facies Thissuggests that rocks south of the Murchison Fault were notexposed to the regional greenschist-facies metamorphismor moderate- to high-grade metamorphism that occurredelsewhere in the region
Structural synthesisA number of models have previously been presented toexplain the structural and metamorphic history of theBryahndashPadbury region For these models the driving forcewas assumed to be collisional tectonics related to theCapricorn Orogeny (eg Tyler et al 1998 Occhipintiet al 1998c Pirajno et al 1998b)
Gee (1990 p 207 Gee and Grey 1993) interpretedthe movement of the lsquoYarlarweelor Gneiss Beltrsquo andlsquoMarymia Domersquo in terms of rising lsquosolid-state crystalndashplasticrsquo domes They suggested that the resulting rise andsouthward movement of the lsquoYarlarweelor Gneiss Beltrsquoand lsquoMarymia Domersquo produced recumbent folds in theoverlying sedimentary rocks of the Bryah Basin Furtherrise and convergence of the domes following depositionof the Padbury Group caused complex refolding ThelsquoYarlarweelor Gneiss Beltrsquo was thrust to the east overthe Bryah and Padbury Groups at this time Martin(1994) interpreted the emplacement of the lsquoNarryer
Figure 20 Selected idealized cross sections through the Bryah and Padbury Groups (after Occhipinti et al 1998a) Locationsof a) to c) are shown on Figure 19 (note difference in scale)a) Northeastndashsouthwest section in the central-eastern part of the Bryah and Padbury Basins showing the fault-bendfold model for the Peak Hill Anticline and inferred suture between the Yilgarn Craton (Murchison Terrane) andreworked Archaean Marymia Inlier The extensional fault slice along the northern margin of the craton formed duringearly development of the Bryah Basin (lsquopassive marginrsquo) and was preserved in this idealized section after basinclosureb) Eastndashwest section across the zone of D3 fold and fault structures The section highlights the intense deformationacross the zone between the Billara and Kinders Faults and shows an inferred major detachment (within underlyingmafic volcanic rocks of the Narracoota Formation) zone of highly disharmonic F3 folding mapped at the surfacec) Northndashsouth section in the central-western part of the Bryah and Padbury Basins showing the Yarlarweelor Domethe sheared-out Padbury Syncline and the Murchison Fault as the suture between in situ and reworked ArchaeanNarryer Terrane Note the inferred detachment of the BryahndashPadbury succession along the contact with the NarryerTerraned) The development and onlap of the Padbury Basin onto the underlying Bryah Group
28
Pirajno et al
Gneiss Complexrsquo (lsquoYarlarweelor Gneiss Beltrsquo) as due tolsquolateral escape tectonicsrsquo resulting from the lsquotranscurrentsuturingrsquo of the Yilgarn and Pilbara Cratons during theCapricorn Orogeny Martin (1994) suggested that earlynorthndashsouth movements which changed to localized eastndashwest movements indicate the onset of lsquolateral escapetectonicsrsquo and the eastward expulsion of the northeasternpart of the lsquoYarlarweelor Gneiss Beltrsquo along the Wilthorpeand Kinders Faults In contrast Myers (1989 1990)regarded both the lsquoYarlarweelor Gneiss Beltrsquo and thevolcano-sedimentary rocks of the Bryah and PadburyGroups as allochthonous sheets that were thrust over the
Yilgarn Craton basement and subsequently folded abouteastndashwest axes
An alternative model was presented by Occhipintiet al (1998c Fig 21) who suggested that the Bryah Basindeveloped initially as a rift and the Padbury Basindeveloped over the Bryah Basin in a retroarc foreland-basin setting (see also Martin 1994) Formation of thePadbury Basin in a compressional regime was essentiallyconcommitant with the closure of the Bryah Basin and thedevelopment of D1 structures as subhorizontal shear zonesbetween the Archaean Narryer Terrane basement and the
Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group anddeformation fabrics
Formation Rock type Mineralogy Pre-S1 S1 Post-S1 S2ndashS3 Post-tectonicM1 M2
Peak Hill Schist pelite quartz biotite muscovite chlorite albite tourmaline
chemical sediment quartz spessartine magnetite
calc-silicate quartz epidote chlorite actinolite titanite magnetite
psammite quartz muscovite andesine opaques
Narracoota metabasite quartz actinolite epidote chlorite sericite arfvedsonite titanite calcite
volcanic breccia albite pumpellyite
Ravelstone pelitic tourmalinite quartz muscovite tourmaline garnet feldspar
subarkosic wacke quartz biotite albite sericite tourmaline
Horseshoe banded iron-formation quartz biotite grunerite spessartine chlorite
Robinson Range banded iron-formation quartz stilpnomelane biotite
NOTE No data are available for the Labouchere and Wilthorpe Formations
29
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
supracrustal rocks of the Bryah and Padbury Groups Theoverall movement direction was interpreted as being fromnorth to south but locally because of the possible effectof later dextral shear movement may actually have been
ram
p
Peak Hill Anticline
N S
eg Kinders Fault Peak HillAnticline
Thrust flatrsquo Lateral
ramp Obliq
ue
lateral ramp
Yarlarweelor
Basalthrustplane
2Dc)
d)
2D thrust flat
rsquo
eg Yarlarweelor gneiss complex
gneiss complex
Padbury Group
Bryah Group
Reworked Archaean granite
a)
Archaean granite
b)
2prospective D crustal thrustwith frontal ramp
1D tectonic interleaving zone(eg Peak Hill Schist)
1 2Post-D and pre-D
D tectonic interleaving between reworked Archaeancrust ( underplate) and BryahndashPadbury succession
rsquo1
Post-D D2 3
W E
Thrust ramp
Thrustfrontal
Later
al ra
mp
FMP374 011199
W E
N
Thrust flatrsquo
movement
Thrust
North to south
e)
ramprsquo
flatrsquorsquo
2D thrust flat ndash frontal ramp ndash lateral ramp geometry
Figure 21 Model of the structural development of the BryahndashPadbury Group succession (after Occhipinti et al1998a)a) Zone of D1 subhorizontal tectonic interleaving(by thrust duplexing) between reworked Archaeancrust and overlying rocks of the BryahndashPadburysuccession This zone includes high-strain ormylonitic rocks formed by lsquounderplatingrsquo of theArchaean rocks beneath the volcano-sedimentaryrocks during initial closure of the Bryah back-arcbasinb) Post-D1 geometry with trace of incipient D2crustal-scale thrust with frontal rampc) D2 geometry with fault-bend anticline developedabove the crustal D2 thrust ramp Upright folds inthe volcano-sedimentary succession (eg Padburyand Robinson Synclines) formed ahead of themain thrustd) Post-D2D3 geometry along schematic eastndashwestsection D2 fault-bend anticlines are not shownNorth-to-south movement ie movement towardsviewer leads to eastndashwest compression and hencenorthndashsouth folds and reverse or thrust faults in thedepression between (oblique) lateral ramps at thesame time as eastndashwest D2 folding occurredelsewheree) Schematic view looking north-northwest of thebasal thrust fault with frontal and lateral rampshighlighting the north-to-south movement directionof the thrust sheet
northwest to southeast Substantial movement and highstrains can be inferred from tectonic interleaving (egbetween the Billara and Wilthorpe Faults Fig 19) andfrom the development of the mylonitic zones in possiblethrust duplexes in the Peak Hill Schist Other possibleD1 structures in particular subhorizontal thrust faultsmay have locally developed along the contacts betweenthe Bryah and Padbury Groups Small-scale earlylayer-parallel folds in chert and BIF layers particularlyfrom within the Padbury Group suggest that subhorizontalD1 structures locally formed within the volcano-sedimentary succession (Pirajno and Occhipinti 1998Swager and Myers 1999) Deposition of the PadburyGroup in a retroarc foreland basin (Martin 1994)was probably contemporaneous with the early stagesof D1
The Yarlarweelor gneiss complex and Peak Hill Schistwere described by Occhipinti et al (1998c) as lsquobasement-cored anticlinesrsquo that developed above frontal thrust rampsThe overlying supracrustal rocks and their high-strain D1contact zones were folded by north to south movementover these ramps during D2 deformation In the Peak HillSchist subhorizontal D1 folds are refolded about anupright apparently easterly trending D2 antiformThe hinge of this fold may be sheared out along thecontact with the Marymia Inlier which is marked by aquartz blastomylonite previously mapped as deformedquartzite of the Juderina Formation (Adamides 1998) Theoriginal orientation of the D2 fold may have been east-northeasterly The Peak Hill Schist outcrops around adomal structure produced by refolding of the D2 fold aboutan approximately northerly trending D3 fold-axial surfaceIt was argued by Occhipinti et al (1998c) that the D3 foldsdeveloped in a structural lsquodepressionrsquo between the two
30
Pirajno et al
basement-cored anticlines which acted as lateral rampsin the thrust plane Northerly trending structures developedduring northndashsouth compression as the lateral ramps wereslightly oblique to the movement direction leading tospace problems between the basement-cored anticlinesThis resulted in either lateral shortening or verticalexpulsion (or both) of the Bryah and Padbury Groups
Occhipinti et al (1998c) assumed that the Yarlarweelorgneiss complex (referred to by them as the NarryerTerrane) was an Archaean crustal fragment that influencedthe structural deformation in the Palaeoproterozoic Bryahand Padbury Groups but was not itself largely deformedduring the Palaeoproterozoic Subsequently Sheppard andSwager (1999) and Occhipinti and Myers (1999)recognized Palaeoproterozoic deformation meta-morphism and felsic magmatism within the Yarlarweelorgneiss complex This indicates that the Yarlarweelor gneisscomplex was extensively reworked during the Palaeo-proterozoic and underwent the same D2ndashM2 metamorphicevent that has been recognized in the Bryah and PadburyGroups and Peak Hill Schist
Occhipinti et al (1998b) found that Palaeoproterozoiccoarse-grained granites and pegmatites with ages between1820 and 1780 Ma (Nelson 1998) intruded as sheetssynchronously with the D2 deformation event D McBMartin (1999 pers comm) interpreted granite exposedsouthwest of the Labouchere opencut as intruding thePadbury Group sedimentary rocks and suggested that thisgranite may also be of this age Intrusion of granitoiddykes and sheet-like plutons accompanied uplift of theYarlarweelor gneiss complex and is interpreted as beingconcomitant with dextral shearing in the region andpossibly D3 (Occhipinti et al 1998a Sheppard andSwager 1999) This movement was attributed to anoblique northndashsouth to northwestndashsoutheast collision ofthe Pilbara and Yilgarn Cratons during the CapricornOrogeny (Occhipinti et al 1998b 1999)
In the northwestern part of the Bryah and PadburyBasins the metamorphic grade increases from greenschistfacies in the east to amphibolite facies in the west Furtherwest in the Yarlarweelor gneiss complex the metamorphicgrade reached at least upper amphibolite facies (Sheppardand Swager 1999) Uplift of the Yarlarweelor gneisscomplex from 9ndash10 kbar to greenschist facies occurredbetween c 1812 and c 1800 Ma (Occhipinti et al 1998b)The c 1812 Ma granitoid sheets and dykes were meta-morphosed at high grade (see below) whereas c 1800 Magranites were only metamorphosed to greenschist facies(Occhipinti et al 1998b) Medium-grade metamorphismof the Padbury Group is solely preserved adjacent to theYarlarweelor gneiss complex between the Billara andWilthorpe Faults (see Metamorphism Fig 18 Plate 1)The drop in metamorphic grade to greenschist facies only15 ndash 25 km east of the contact suggests either a rapidincrease in temperature close to the Yarlarweelor gneisscomplex or that amphibolite-facies or upper greenschist-facies (or both) Bryah and Padbury Group rocks have beenfaulted out The latter explanation is preferred because theboundary between amphibolite-facies and lower to middlegreenschist-facies rocks of the Labouchere Formation issharp
In the Bryah and Padbury Groups and Peak Hill Schistmetasomatism accompanied retrogression of D1ndashM1assemblages to greenschist facies during M2 particularlyin D2 shear zones In the Yarlarweelor gneiss complexthere is no evidence for D1ndashM1 and M2 was initially ahigh-grade metamorphic event with the formation ofincipient minimum melt during the early stages of D2(Occhipinti et al 1998b) Post-M2 the metamorphic gradedropped significantly to greenschist facies
In the proposed model shown in Figure 22 the BryahGroup developed in a back-arc lsquorift-type settingrsquo (Pirajnoet al 1998b see Tectonic model and conclusions) If theBryah and Padbury Groups are c 20 Ga or older then D1structures could have developed during the c 20 GaGlenburgh Orogeny (Occhipinti et al 1999 Tyler 1999)as a result of west to east or northwest to southeastcompression Plutonism in the future Yarlarweelor gneisscomplex produced the 1960 Ma felsic granitoid rocksduring the late stages of D1 (Sheppard et al 1999Fig 22c) Alternatively if the Bryah and Padbury Groupswere deposited sometime between c 1945 and 1812 MaD1 could have developed during the c 18 Ga CapricornOrogeny due to north-northwest to south-southeastcompression (Figs 22 and 23) Further geochronologicalwork is required to establish the age of D1 and thedepositional age of the Bryah and Padbury Groups
In either case closure of the Bryah Basin took placeduring D1 with deposition of the Padbury Group in aretroarc foreland basin overlying the Bryah Group andpossibly the lsquofuturersquo Yarlarweelor gneiss complex(Fig 22b) D1 deacutecollements would have developedbetween the Bryah and Padbury Groups the futureYarlarweelor gneiss complex and the Peak Hill Schist(Figs 22b and 23a) Duplexes developed in the Peak HillSchist during D1 and it was detached from the MarymiaInlier (Fig 23b) In addition early D1 faults and foldsformed between and within the Bryah and PadburyGroups
The second deformation event D2 occurred during theCapricorn Orogeny Early in D2 approximately northwestto southeast compression caused further thickening of theBryah and Padbury Groups over the Yarlarweelor gneisscomplex destabilizing this piece of crust (Figs 22b and22c) The resulting increased pressure and temperaturemay have caused the underlying Archaean crust to startto melt This melt produced the c 1820 to c 1812 Mafelsic granitoid rocks (Occhipinti et al 1998a Sheppardand Swager 1999 Sheppard et al 1999) that intruded theupper parts of the Yarlarweelor gneiss complex as veinsand sheets (Sheppard and Swager 1999 Fig 22c) Asthese developed synchronously with the deformation (D2)they were commonly folded into upright steeply toshallowly plunging isoclinal to open folds These rockswere also metamorphosed at high grade during the D2deformation event Regionally this metamorphismcorresponds to M2
Padbury Group sedimentary rocks were meta-morphosed to medium grade along contact zones withthe Yarlarweelor gneiss complex during M2 This high- andmedium-grade metamorphism may have releasedfluid that moved through faults and shear zones and
31
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Figure 22 Schematic sections illustrating the proposed model of the structural development of the BryahndashPadburyGroup succession in the westa) Development of the Bryah Group pre-D1 over the Proto-Yarlarweelor gneiss complex and the northernmargin of the Yilgarn Craton in an extensional-rift settingb) Early- and syn-D1 deposition of the Padbury Group in a fold-and-thrust belt foreland-basin type settingover the Bryah Group Inversion of the Bryah rift-basin by possible reversal of D1 normal faultsDevelopment of D1 faults between the Bryah Group Padbury Group Yarlarweelor gneiss complex andYilgarn Cratonc) D2 to D3 local interleaving of the Bryah and Padbury Groups with the development of folds and faultsDeformation of the Bryah and Padbury Groups above basal detachments Early D1 faults refolded aboutD2 or D3 folds Formation of c 1810 Ma leucocratic granite locally associated with incipient minimum meltin the Archaean gneiss component of the Yarlarweelor gneiss complex Later at c 1800 Ma sheet-likeplutons developed particularly along the faulted boundaries between the Yarlarweelor gneiss complexand Bryah and Padbury Groups
Deposition of Padbury GroupEarly D
Development of fold and thrustbelt in D
1 1
Inversion of Bryah rift
1
Murchison Fault
Karalundi Formationequivalents Bryah Group
Hyaloclastites
Proto-Yarlarweelorgneiss complex
Post-rift phase
Thickening of supra-crustal succession over
Proto-Yarlarweelorgneiss complex
a)
b)
c)
v
SAO62 130300
Formation of c 1810 Ma leucocratic coarse-grained granitein Yarlarweelor gneiss complex (Sheppard et al 1999)
Deformation of the Yarlarweelor gneiss complex
NNW1
SSE
1
2 3
Early- and syn-D
Mafic and ultramaficvolcanic rocks
Early reversal of D normal faults some possible back thrustingof volcanic rocks below detachments cut by detachments
Folded c 1960 MaYamagee granite
Local plutonism into Proto-Yarlarweelor gneiss complex
at c 1960 Ma forming Yamageegranite of Sheppard and Swager (1999)
Pre-D extensionndashrift phase
D ndashD
Bryah Group
Proto-Yarlarweelorgneiss complex
Padbury Group
32
Pirajno et al
metasomatized M1 assemblages in the Bryah Group andPeak Hill Schist rocks during M2ndashD2 Elsewhere in theregion during D2 the Peak Hill Schist and Bryah andPadbury Group rocks were folded into tight to isoclinalupright folds with mainly easterly to northeasterly trends(Occhipinti et al 1998c) Post-D2 during D3 theYarlarweelor gneiss complex was uplifted and retrogressedto greenschist facies This uplift in a dextral strike-slipregime may have been accommodated by steeply dippingnormal faults between the Yarlarweelor gneiss complexand the Bryah and Padbury Groups (Figs 17 and 18) thathave now been inverted (Fig 24)
In the Peak Hill Schist subhorizontal D1 mylonitezones and rootless folds are refolded about an easterly oreast-northeasterly trending upright D2 antiform The domalshape of the Peak Hill Schist is an artefact of a northerlytrending upright D3 antiform refolding the D2 antiformThe Yarlarweelor gneiss complex apparently does notcontain D1 folds although shearing along basementndashcovercontacts between the Yarlarweelor gneiss complex and theBryah and Padbury Groups may have developed duringD1 (Fig 22b) The D2 fold-axial surfaces within the
Yarlarweelor gneiss complex parallel the arcuate faultedboundary with the Bryah and Padbury Group rocks Thischange in the trend of D2 may be explained in terms of afault-bend fold developed during dextral shearing(Occhipinti and Myers 1999) that may have accompanieduplift during D3
MineralizationThe mineral resources of the Peak Hill SchistBryah Group and Padbury Group are considerableconsidering the relatively small total area of thesebasins (about 6000 km2) These resources include goldmanganese iron ore talc and silver Pirajno andOcchipinti (1995) discussed the mineral potential of theBryah Basin and Pirajno and Preston (1998) described themineral deposits of the BryahndashPadbury region and PeakHill Schist Mineral production and defined resourceswithin these tectonic units as at 30 June 1999 arepresented in Tables 7 and 8 Known deposits andoccurrences are listed in Table 9
Figure 23 Schematic section illustrating the proposed model for the structural development of theBryahndashPadbury Group succession and the Peak Hill Schist a) Development of the BryahGroup in a rift setting pre-D1 over the Marymia Inlier (Yilgarn Craton) b) D1 closure of theBryah lsquoriftrsquo inversion of normal faults deposition of the Padbury Group and formation ofthe Peak Hill Schist
Future D fault
NNW SSE
Bryah Group
Basement
Proto-Peak Hill Schist
Pre-D extensionndashrift phase1
1Peak Hill Schist
D faults1
1
Rift closes Peak HillSchist develops as a
strongly duplexed packageof rock
Marymia Inlier
a)
b)
SAO63 150300
Padbury Group
Early- and syn-D
Mafic and ultramafic volcanic rocks
33
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The mineral deposits of the Peak Hill Schist andBryah and Padbury Groups include mesothermal-stylegold-only lodes volcanogenic massive sulfide (VMS)copperndashgold supergene-enriched manganese bandediron-formation iron ore and talc in metasomatizeddolomitic rocks The distribution of these mineral depositsis shown in Figures 25 and 26 and Plate 1
Gold depositsThe most important mineral deposits exploited to datehave been the mesothermal-style gold-only lodes all ofwhich are in the Peak Hill Schist and the Bryah andPadbury Groups If the area occupied by these groupsalone is taken into account (about 6000 km2) then theidentified contained gold per unit area is 125 kg goldkm2The mesothermal gold deposits including past and presentproducers include Peak Hill Jubilee and Mount Pleasantin the Peak Hill Schist Harmony Mikhaburra WembleyCashman and Ruby Well in the Bryah Group (Figs 25and 26) and Horseshoe Labouchere Nathans DeepSouth and Fortnum in the Padbury Group The Wilthorpedeposit is hosted in Upper Archaean granitic rocks whichare tectonically interleaved with rocks of the Bryah andPadbury Groups
The total gold produced is 595 t with total (producedplus remaining inferred indicated and measured)resources estimated at approximately 75 t of containedgold The Labouchere and Fortnum areas containthe regionrsquos largest pre-mining resource estimated as 333 tof contained gold at a grade of about 24 gt goldApproximately two-thirds (225 t) has been exploited
largely between 1989 and 1995 with the remainingresource (107 t) being in the Fortnum area Details of theLabouchere and Fortnum deposits can be found in Hannaand Ivey (1990) and Hill and Cranney (1990) respectivelyThe area around the Peak Hill opencut (includingRavelstone) has produced approximately 20 t of fine goldat an average grade of 4 gt gold more than half of whichhas been extracted in the last 13 years Remainingmeasured and indicated resources are estimated at about47 t of contained gold The Harmony deposit (NewBaxters Find) which was recently exhausted had totalpre-mining resources estimated at about 92 t with a gradeof 35 gt gold
The lode deposits are hosted in mylonitic schistmetasedimentary rocks metavolcanic rocks or along theircontact zones They are spatially associated with high-strain zones and hydrothermal alteration dominated bypyrite quartz muscovite biotite and alkali feldspars Themineralization is in ductile and brittlendashductile shears (egPeak Hill) and in discrete brittle fractures (eg Cashman)indicating a relationship of structural style with therheology of the host rocks The development of ductilebrittlendashductile and brittle structures (zones of highpermeability) was accompanied by infiltration ofhydrothermal fluids which produced alteration andmineralization The precise timing of the mineralizationis difficult to ascertain Windh (1992) suggested syn-D3but from field and petrological observations it is morelikely that circulation of mineralizing fluids occurredduring a continuum related to D1ndashD2 tectonism andmetamorphism under conditions of ductile or brittlendashductile regimes with perhaps some remobilization intobrittle structures occurring during D3 Lead isotope data
Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneisscomplex and then into the Bryah and Padbury Basins showing the possible present-day configuration of these units
Kerba FaultBangemall BasinFault boundary
YILGARNCRATON
vv
v
vv
v
vv
vv v
v
v
v vv v
vvv
vvv
vvv
vv
Errabiddy
Shear ZoneGascoyneComplex
Possible currenterosion level
SAO64 130300
NW SE
SeabrookndashMurchison Fault
v v
Bangemall Group
Yarlarweelor gneiss complex
Bryah and Padbury Group rocks
Cooinbar Fault
34
Pirajno et al
Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
_______________________ Production (P) _______________________ _______ Remaining resources (R) ________ TotalMining centre Ore Contained Alluvial Dollied Total Resource Ore Contained pre-miningor mine metal contained type metal resources
metal (P+R)(kt) (kg) (kg) (kg) (kg) (kt) (kg) (kg)
Pre-1986
Mount Fraser Mining Centre 09 24 27 13 288 ndash ndash ndash 288Mount Seabrook Mining Centre 17 383 ndash 02 385 ndash ndash ndash 385Ravelstone Mining Centre 49 1058 ndash 32 109 ndash ndash ndash 109Wilthorpe Mining Centre 01 15 ndash ndash 15 ndash ndash ndash 15Peak Hill sundry parcels 27 7706 889 139 8734 ndash ndash ndash 8734Peak Hill Mint deposits(a) ndash ndash 25 33 58 ndash ndash ndash 58Ruby Well Mining Centre 85 146 325 142 1927 ndash ndash ndash 1927Horseshoe Mining Centre 9049 2 9669 352 889 3 091 ndash ndash ndash 3 091Peak Hill Mining Centre 6217 8 200 367 628 8 2995 ndash ndash ndash 8 2995
1986 to 30 June 1999
Horseshoe Lights(b) mine 9059 3 7373 217 ndash 3 759 ndash ndash ndash 3 759Fortnum mine 5 832 15 6025 377 ndash 15 6402 MES + IND 2 221 7 542 23 1822
INF 991 3 194 3 194Labouchere mine 2 9108 6 9052 ndash ndash 6 9052 ndash ndash ndash 6 9052Mount Pleasant mine 1449 433 ndash ndash 433 ndash ndash ndash 433Peak Hill mine 6 5738 20 1266 908(c) ndash 20 2174 MES + IND 2 200 4 760 24 9774
Total 17 9128 59 0577 3487 1878 59 595 5 412 15 496 75 091
NOTES (a) Gold from the Peak Hill Mining Centre deposited at the Perth Mint(b) Horseshoe Lights also produced 261 675 t of copper concentrates containing 25803 kg of gold(c) Includes 625 kg of gold produced from retreated tailingsMES Measured resources IND Indicated resources INF Inferred resources
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
35
GSW
A R
eport 59G
eology and mineralization of the P
alaeoproterozoic Bryah and P
adbury Basins W
A
Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
_____ Production (P) to 300699 _____ __________________ Remaining resources (R) __________________ Total resource (P+R)Commodity Mine Ore or concentrate Contained metal Resource type Ore or concentrate Contained metal Contained metal
(t) (t) (t) (t) (t)
Copper and Cashman 7 11 ndash ndash ndash 11cupreous ore Peak Hill sundry 63 223 223
Horseshoe Lights 261 675 49 159 Indicated 2 080 000 22 897 72 056Inferred 3 340 000 22 879 22 879
Total 261 745 49 1824 5 420 000 45776 94 9584
Manganese Horseshoe 489 895 203 899 Measured + Indicated 80 000 21 000 224 899Inferred 205 000 100 000 100 000
Mount Fraser 228 108 Measured + Indicated 32 000 9 000 9 108Mount Padbury 7 319 3 498 Measured + Indicated 5 000 2 000 5 498Ravelstone (Peak Hill) 76 237 36 938 ndash ndash ndash 36 938Total 573 679 244 443 Measured + Indicated 117 000 32 000 276 443
Inferred 205 000 100 000 100 000
Iron Robinson Range ndash ndash Inferred 10 000 000 6 000 000 6 000 000
Talc Mount Seabrook ndash Livingstone ndash 540 416 Indicated ndash 1 470 000 2 010 416Inferred ndash 250 000 250 000
Total ndash 540 416 ndash 1 720 000 2 260 416
Silver Horseshoe Lights (post-1982) ndash 72 7194 kg ndash ndash ndash 72 7194 kg(by-product) Peak Hill general ndash 1182 kg ndash ndash ndash 1182 kg
(including Horseshoe pre-1983)Total ndash 72 8376 kg ndash ndash ndash 72 8376 kg
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
36
Pirajno et al
Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins (modified from Pirajnoand Preston 1998 see also Plate 1)
Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
Mine (M) AMG coordinates Principal Mineralization style Expression Ore minerals Relationshipprospect (P) or Easting Northing commodity to hostoccurrence (O)
Cashman (M) 662129 7126994 Gold Regolith enrichment Outcrop Gold Discordantand mesothermal lode
Durack (P) 670440 7150520 Gold Mesothermal lode Drill Gold pyrite Discordantintersections magnetite
Harmony (M) 664145 7161267 Gold Regolith enrichment Drill Gold chalcopyrite Discordantand primary intersections pyrrhotite scheelitemesothermal lode pentlandite pyrite
Heines Find (P) 682759 7145164 Gold Mesothermal lode Outcrop Gold Discordant
Horseshoe (P) 656994 7183734 Gold Eluvial Gold ndash
Horseshoe (P) 657579 7184413 Gold Eluvial Gold ndash
Horseshoe (P) 661219 7182977 Gold Eluvial Gold ndash
Horseshoe (P) Copperndashgold Multiple veins Outcrop Gold Discordant
Horseshoe 662648 7193894 Copperndashgold Supergene enrichment Gossan Chalcocite pyrite DiscordantLights (M) of VHMS chalcopyrite native
copper and gold
Jubilee (M) 671889 7165443 Gold Mesothermal lode Quartz vein Gold pyrite Discordant
Labouchere (M) 627730 7204710 Gold Mesothermal lode Not known Gold pyrite Discordant
Livingstone (M) 567540 7171032 Talc Replacement Outcrop Talc Discordant
Mikhaburra (P) 656252 7130396 Gold Multiple veins Outcrop Gold Discordant
Mount Pleasant (M) 674287 7162089 Gold Mesothermal lode Outcrop Gold pyrite Discordant
Mount Seabrook (M) 572631 7168338 Talc Replacement Outcrop Talc Discordant
Nathans Deep 631713 7198812 Gold Mesothermal lode Not known Gold pyrite DiscordantSouth (M)
Peak Hill (M) 672190 7163003 Gold Mesothermal lode Quartz vein Gold pyrite altaite Discordantchalcopyritebismuthotelluridemolybdenite magnetite
Ravelstone (M) 665734 7166777 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ravelstone (M) 669313 7166423 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ruby Well area (M) 674665 7129915 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 672600 7124378 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 674142 7127027 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677928 7129727 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677408 7130112 Gold Eluvial ndash Gold ndash
St Crispin (P) 691358 7158940 Gold Mesothermal lode Outcrop Gold Discordant
Trevs Starlight (M) 636412 7198887 Gold Mesothermal lode Not known Gold pyrite Discordant
Unnamed (O) 611598 7168985 Variscite Not known Not known Variscite Discordant
Unnamed (O) 611909 7167084 Variscite Not known Not known Variscite Discordant
Unnamed (P) 656664 7185310 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Wembley (P) 663983 7149044 Gold Mesothermal lode Outcrop Gold Discordant
Wilgeena (M) 685369 7155622 Gold Mesothermal lode Outcrop Gold Discordant
Wilthorpe (M) 630414 7176521 Gold Mesothermal lode Outcrop Gold pyrite galena Discordantarsenopyrite
Yarlarweelor (M) 636723 7196423 Gold Mesothermal lode Not known Gold pyrite Discordant
37
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
MARYMIAINLIER
MARYMIAINLIER
Jenkin
FaultGROUPBANGEMALL
Murchison Fault
NARRYERGNEISS
TERRANE
Padbury Bryahand
Yerrida Basins
FMP100b 181099
1000 km
5
67 16
8
9
17
23
4
11
10
15
1213 14
19
18
21
20
1
GOODININLIER
YILGARNCRATON
YILGARN
CRATON
Goodin
Fault
118deg30 119deg30
Killara
Narracoota
Mt Padbury
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
Yandil
119deg30
Milgun30 km
Jamindi Three Rivers Marymia
PEAK HILLROBINSON
RANGE
Padbury Bryah Doolgunna Thaduna
Glengarry Mooloogool Mount Bartle
MerewetherYanganooGabanintha
119deg00
25deg30
26deg30
26deg00
25deg30
GLENGARRY
Milgun
Mesothermal Au AundashCu
Shear zone-hosted Cu
Epigenetic Pb
Supergene Mn
2 Jubilee
5 Labouchere
7 Fortnum group8 Horseshoe Lights9 Horseshoe gold
10 Wilthorpe11 Wembley
12 Mikhaburra13 Cashman14 Ruby Well
group (including Elsa)
16 Horseshoe magnagese17 Ravelstone18 Robinson Range BIF
(no specific locality)19 Thaduna20 PGE-bearing gossan21 Magellan
3 Mount Pleasant4 Harmony
(New Baxters Find)Fault
Geological boundary
Bouguer gravity anomaly
Peak Hill Schist
Karalundi FormationGR
OU
PB
RY
AH
Padbury Group
Horseshoe and Ravelstone Formations
schistmetabasaltic hyaloclastiteNarracoota Formation mafic and ultramafic
Archaean basement
Earaheedy Group
WindplainSubgroup
MooloogoolSubgroup
YE
RR
IDA
GR
OU
P
Maraloou Formationintercalated Killara and Maraloou FormationsDoolgunna and Thaduna Formationswith intercalated Killara FormationJuderina and Johnson Cairn Formations
Homestead
Bangemall Group
Microgabbro dyke
BryahPEAK HILL
1100 000 map sheet 1250 000 map sheet
Aeromagnetic lineament
6 Nathans Deep South
15 Mount Padbury ndash Mount Fraser
Volcanogenic massive sulfide
Shale-hosted stratabound sulfides
MINERALIZATION STYLE
MINERAL DEPOSITS
38
Pirajno et al
Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet (after Pirajno and Occhipinti 1998)
Ravelstone Formation
Karalundi Formation
Horseshoe Formation
Granitoid rock and gneiss
Narracoota Formation
10 km
040400
Yerrida Group
Bangemall Group
Earaheedy Group
Padbury Group
Bry
ah G
roup
Prospect
Producer
JubileeGroup
Peak Hill
Harmony
Wilgeena
Wembley
DurackWell
HeinesFind
Mikhaburra
CashmanGroup
Ruby WellGroup
Goodin Find
Ravelstone Group
(Hit or Miss)
St CrispinWilsons Find
25deg30
118deg
30
119deg
00
26deg00
Mar
ymia
Inlie
r mylonite
Syncline
Anticline
Overturned syncline
Peak Hill Schist
Thrust fault
Fault
Strike-slip fault
FMP162a
Supergene manganese deposit
Alluvialndasheluvial gold deposit
Mesothermal gold lodes
Mount Pleasant
39
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(palaeo-isochrons) suggest that in the Bryah and PadburyBasins mineralization occurred between 192 and 17 Ga(Windh 1992 Thornett 1995) The results of lead isotopicstudies also indicate that the lead was derived from YilgarnCraton rocks (Dyer 1991 Windh 1992 Thornett 1995)although there is a suggestion that the lead from thePeak Hill deposit is similar to that from a galena in theMarymia gold deposit in the Marymia Inlier (McMillan1993)
The nature of the mineralizing fluids is poorlyconstrained Alteration assemblages at the Peak Hill andMount Pleasant deposits indicate that the ore fluids wereenriched in Fe K Na S B CO2 SiO2 and H2O (Thornett1995) Fluid inclusion studies of mineralized materialsfrom the Fortnum and Labouchere gold deposits (Dyer1991 Windh 1992) indicate that the ore fluids wererich in H2O and H2OndashCO2 with salinities of 7ndash12 wtand 5ndash17 wt NaCl equivalent respectively Micro-thermometric measurements (Dyer 1991 Windh 1992)indicate temperatures ranging from approximately 170degto 320degC
Peak Hill Jubilee and Mount Pleasantdeposits
Mine geologists subdivided the Peak Hill Jubilee andMount Pleasant lithologies into the Core sequence HoneyQuartzite Intermediate sequence Mine sequence MarkerQuartzite and Hangingwall sequence
The Core sequence is at the structural base and wellexposed in the Mount Pleasant opencut where it reachesa thickness of 55 m The contact with the Intermediatesequence is marked by the Honey Quartzite which is amylonite consisting of laminated or ribbon quartz TheCore sequence rocks have a mylonitic fabric and are madeup of quartzndashbiotitendashcarbonatendashmuscovite(ndashepidotendashhornblendendashgarnetndashmagnetitendashpyrite) locally withabundant very fine zircons and monazite in the biotite-richvarieties (Barrett 1989) At Mount Pleasant as mentionedabove graphitic schist is present near the top andassociated with a zone of chloritendashbiotite(ndashgarnet) schistwith albite porphyroblasts (Fig 27) containing inclusionsof monazite and zircon Geochemical discriminant plotsusing immobile elements suggest either a granitic (Nb SrLa and Ce) or maficndashintermediate (Ni Cr and Ti)protolith (Thornett 1995) Barrett (1989) on the otherhand proposed that much of the Core sequence could bederived from a sedimentary protolith The origin of thealbite porphyroblasts is uncertain Based on geochemistrypetrology and textural features Thornett (1995) advocateda combined hydrothermal ndash retrograde metamorphicorigin and compared the Peak Hill ndash Mount Pleasantalbites to those studied by Watkins (1983) in the Dalradianschists of Scotland Another possibility that could accountfor the presence of the albite porphyroblasts is lsquoreactionsofteningrsquo as proposed by Dixon and Williams (1983)These authors advanced the hypothesis supported bygeochemical and mineralogical data that mylonitizationof a quartzofeldspathic parent may be accompanied bymineralogical changes involving the breakdown ofplagioclase with release of Na2O and to a lesser extent
CaO and formation of muscovite This would result in theproduction of quartzndashmuscovite mylonites and sodium-rich fluids
The Intermediate sequence is discontinuous withlayers up to 2 m thick and is composed of a quartzndashmylonite-bearing white mica The Intermediate sequencelies above the Honey Quartzite has an estimated thicknessof between 200 and 400 m and forms the footwall to theMine sequence at Peak Hill and the hangingwall to theore zones at Mount Pleasant The Intermediate sequenceis dominantly quartzndashmuscovite schist with minorplagioclase biotite microcline carbonate and chloriteBarrett (1989) interpreted this rock as either a felsicporphyry or an arkose The lower part of the Intermediatesequence consists of mainly biotite schist with garnet andepidote Rocks of the Intermediate sequence exhibitmillimetre-scale metamorphic differentiation layeringwhich define a dominant S2 schistosity (Thornett 1995)This is interpreted by the present authors as a typicalmylonitic structure
The Mine sequence mostly found in drillholes ischaracterized by biotite ndash white mica(ndashchloritendashcarbonatendashamphibolendashgarnetndashalbite) schist and graphite schist(Fig 28) and may be 40 to 50 m thick Drillcore samplesof a hornblendendashplagioclasendashquartz rock (with garnetporphyroblasts) have been interpreted as an unalteredamphibolite (Barrett 1989 Thornett 1995)
The Marker Quartzite is a recrystallized quartzmylonite (lsquoMarker Chertrsquo of mine geologists)1 to 3 m thick at the top of the Mine sequenceOutcrops of Marker Quartzite exhibit radiating iron-oxidepseudomorphs after acicular crystals and iron-oxidepseudomorphs after porphyroblasts Windh (1992)identified these acicular crystals using the scanningelectron microscope as grunerite The porphyroblastpseudomorphs are possibly after garnet
The Hangingwall sequence can be up to 700 m thickand is made up of white mica ndash magnetite(ndashgarnetndashchlorite) mafic schist and metabasite The latter is locally
Figure 27 Albite porphyroblasts in mylonitic schist at theMount Pleasant deposit
40
Pirajno et al
garnetiferous and characterized by a metamorphic (andhydrothermal) assemblage containing variable amountsof hornblende plagioclase quartz garnet epidote andtitanite The metabasite is overlain by mylonitic schistcontaining mainly quartzndashplagioclasendashbiotite and locallyassociated with zones of albitendashmuscovite and garnetndashepidote (calc-silicate)
The Peak Hill Jubilee and Mount Pleasant depositswere studied by Barrett (1989) who based most of hiswork on drillcore samples and Thornett (1995) Theseauthors provided much of the information summarizedbelow augmented by data from this study The Peak HillJubilee and Mount Pleasant gold deposits are situated inthe west-northwestern portion of the Peak Hill Anticlineand hosted in the Peak Hill Schist (Figs 4ndash7 and 26) Inthe mine areas the rocks are intensely weathered to depthslocally exceeding 200 m Weathering products arepredominantly kaolinitic clays and iron oxyhydroxidesThis weathering is particularly well developed in zonesof hydrothermal alteration which in turn are related tohigh-strain zones the latter having facilitated percolationof meteoric waters Hydrothermal alteration is dominatedby sulfidation (pyrite) and alkali metasomatism (biotiteand albite) and contained within late-stage quartzndashcarbonate veins hosted in highly strained metabasites andquartz mylonites Other important alteration mineralsinclude iron-rich chlorite sericite garnet tourmalinedolomite and calcite In all about 20 t of gold has beenproduced
The Peak Hill mineralization was exploited in threeadjoining pits which from north to south are FivewaysPeak Hill Main and Mini In plan view (Fig 29) the entirePeak Hill mineralized system is contained within apackage of mylonitic schist (Mine sequence) at thefootwall of northerly trending and westerly dippingshear zones The mylonitic schist contains quartz podsveins lenses and stringers and locally graphitic quartzmylonite units (Marker Quartzite see below and Fig 30)The Mine sequence contains lenses of mafic rocks (egmetadolerite) The overall picture is one of a complex zoneof shearing and tectonic interleaving between rocks of the
FIVEWAYSPIT
MINIPIT
MAINPIT
100 m
sequence
Mine sequence
Intermediate sequence
Vein quartz
Marker Quartzite
Shear zone
Anticline
FMP160 271099
Hangingwall
Geology notmapped
Geology notmapped
N40
42
45
40
25
45
45 26
30
42
45
Fault42
Cleavage
Foliation
Figure 28 The Mine Sequence schist at the Peak Hill depositshowing biotite alteration the biotite is partlyretrogressed to chlorite plane polarized light
Figure 29 Schematic geological map of the Fiveways Mainand Mini opencuts Peak Hill deposit (after Thornett1995)
Figure 30 Peak Hill Mini opencut showing the ore-bearingmylonitic schist graphitic schist (dark bands) andMarker quartzite unit (above the upper graphiticschist)
41
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Narracoota Formation and Peak Hill Schist Kinematicindicators (CndashS surfaces) indicate a thrust movement fromwest to east (Thornett 1995)
The main orebody has a westerly dip ranging from20deg to 50deg (averaging 35deg) and is hosted in rocks of theMine sequence High-grade zones can contain up to30ndash40 gt gold The ore zones are characterized bypervasive alteration consisting of chloritendashbiotitendashquartzndashcarbonatendashgraphite The principal ore minerals arepyrite chalcopyrite and gold Other ore minerals includealtaite tetrahedrite bismuthotelluride molybdenite andvarious bismuthndashleadndashtellurium compounds The goldmineralization is thought to have been emplaced in at leasttwo stages In the first stage gold mineralization wasemplaced along the contact between the Marker Quartziteand the Mine sequence (see below) During the secondstage cross-faults were formed with the gold beingredistributed or rearranged along these cross-faults
The Jubilee deposit was at first mined underground in1892 from a number of workings but the production isunknown In 1992 a small pit was excavated based onprobable reserves of approximately 50 000 t at 4 gt goldIn this pit gold mineralization is hosted in rocks of theHangingwall sequence and is in a complex quartzstockwork system emplaced along the margins of a 250 m-thick undeformed metabasite The gold is on both thehangingwall and footwall sides of the metabasite bodyTourmaline is present in the ore-bearing material Near theJubilee pit a northerly striking westerly dipping quartzvein almost perpendicular to the dominant foliation trendextends for about 200 m This vein was mined in the pastand contained maximum grades of approximately 30 gtgold
Mining at Mount Pleasant began at the turn of thecentury with the production of 8000 t of ore with anaverage grade of 9 gt gold Mining resumed in the 1980swhen about 145 000 t of ore was extracted with anaverage grade of 3 gt gold and 04 t of gold wasproduced The ore zones are nearly flat lying and wereemplaced in subparallel fashion one above the other Thedeeper northern zone is hosted by the Core sequence Goldis in quartzndashcarbonate veins associated with zones ofalbite (Fig 27) iron-rich chlorite sericite carbonate andpyrite alteration as well as zones of nearly flat lyinggraphitic schist (dip is 10deg to the south) The veins areeither vertical or of saddle-reef type lodged in anticlinalfolds
Harmony deposit
The Harmony (also known as New Baxters Find orContact) gold deposit is located approximately 10 km westof Peak Hill in a featureless area of no outcrops andcovered by colluvium lateritic duricrust and hardpanmaterial Details of the geology of the Harmony depositcan be found in Harper et al (1998) from whom the briefreview that follows is taken
The Harmony gold deposit consists of a subhorizontalsupergene zone hosted in ferruginous lateritic materials
(transported and residual regolith) a northeasterlytrending subvertical primary vein system and carbonate-bearing breccias Most of the ore is contained within thevein system which is hosted in rocks of the NarracootaFormation and at the contact between the Narracoota andRavelstone Formation (Fig 31) with lesser low-grademineralization in laterite The Harmony mineralization ishosted in a northwesterly plunging antiform (Enigmastructural zone) of a southwesterly dipping succession ofaltered mafic rocks at the top of the Narracoota Formationand within a shear zone along the contact with overlyingmetasedimentary rocks of the Ravelstone Formation Themineralized array of quartz veins become locally closelyspaced forming a stockwork that is commonly associatedwith high-grade ore Primary ore minerals include pyritewith gold inclusions pyrrhotite pentlandite chalcopyriteand scheelite The primary mineralization was enrichedby supergene processes
Hydrothermal alteration is characterized mainly bysilicification carbonitization and locally chloritizationHarper et al (1998) reported that mafic rocks show aparagenetic sequence of early albite and quartz followedby muscovite and chlorite Alteration in the metasedi-mentary rocks in the hangingwall is characterized mainlyby sericite and chlorite This primary alteration grades intozones of supergene alteration containing limonitekaolinite smectite group minerals and hematite Theweathered bedrock extends to approximately 60 m depthRegolith studies from drillholes have revealed anomalousAu W As Sb and Se in the ferruginous materials
Labouchere Nathans and Fortnumdeposits
In the northwestern part of the BryahndashPadbury Basin (onMILGUN) three distinct zones of gold mineralization havebeen recognized in high-strain zones associated with themargin of the Yarlarweerlor gneiss complex (Fig 25 andPlate 1) The Labouchere group (Labouchere and CentralValley deposits) and Nathans group (Labouchere-NathansNathan Bitter and Nathans Deep South deposits) had early
Figure 31 Diagrammatic cross section of the Harmony orezones (modified from Harper et al 1998)
50 m
FMP159
Supergene ore
Primary ore
Pit outline
50
100
150
200
Met
res
Mafic rocks
Formation)
Ultramafic rocks
Formation)(Ravelstone
(Narracoota
(NarracootaFormation)
Pelitic rocks
SW NE
211099
42
Pirajno et al
mining activity recorded from 1939 to the early 1940swith additional discoveries in the mid-1980s (Hanna andIvey 1990) The Fortnum deposits (Trevs StarlightTwilight Ricks Toms Hill Alton Eldorado Callies D39and Yarlarweelor) were discovered in the early 1980s (Hilland Cranney 1990)
Gold mineralization is structurally controlled in hostrocks of both the Bryah and Padbury Groups (Hill andCranney 1990) Windh (1992) concluded from detailedstudies at the Labouchere Nathans Deep South andFortnum mines that aqueous fluids of high temperatureand moderate salinity were responsible for mineralizationConstraints on temperature are derived from the lowerto middle greenschist-facies alteration assemblages(muscovitendashchloritendashalbite(ndashbiotite)) and fluid inclusiontrapping temperatures of up to 320degC Based on leadisotope work (galena from Nathans Deep South) Windh(1992) suggested that the syn-D4 gold mineralizationoccurred between 19 and 18 Ga The main features ofthe ore deposits are described below from the availableliterature
At the Labouchere-Nathans mine gold mineralizationis hosted in pyritic chert lenses or pods that lie withinmaficndashultramafic schist and along the contact withoverlying quartz wacke of the Labouchere FormationWindh (1992) described volcanic breccia (with high Niand Cr) with fuchsitic ultramafic and chert clasts similarto the reworked clastic rocks immediately overlying themaficndashultramafic volcanic rocks in the NarracootaFormation at the Fortnum mine The maficndashultramaficschist lies in the core of a southerly plunging anticlineand is here interpreted as part of the NarracootaFormation The Narracoota Formation ndash LabouchereFormation contact is interpreted as an early (D1ndashD2) faultor shear zone that was tightly folded during D3 Thestructure is crosscut and slightly offset by D4 faultstrending 270degndash290deg including a shear that forms thesouthern limit to the mineralization (Hanna and Ivey1990) Gold is associated with quartz veining and pyritein the altered chert with sideritendashmuscovitendashpyritealteration around the veins (Windh 1992) Productionfigures are only known for the combined output of theLabouchere-Nathans and Nathans Deep South opencuts(nearly 7 t of gold over five years Table 7)
At the Nathans group of workings the Nathan Bittershafts within the upper Labouchere Formation or lowerWilthorpe Formation have a recorded production of about8 kg over the period 1943ndash1950 (Swager and Myers1999) About 500 m to the north-northwest shallow shaftslie along the Kinders Fault between coarse and pebblyquartz wacke to the east and ultramafic schist of theNarracoota Formation to the west The Nathans DeepSouth mineralization lies approximately 1 km south-southeast of Nathan Bitter and was discovered in 1986(Hanna and Ivey 1990) The mineralization is hosted byfinely laminated chloritic shale interbedded with coarsequartz wacke and overlain by coarse units grading fromquartz-pebble conglomerate to quartzndashsericite shale Theentire succession is here described as part of the WilthorpeFormation including the chloritic shale which is mostlikely derived from mafic volcanic precursors (Hanna and
Ivey 1990 Windh 1992) Occhipinti et al (1998a)mapped similar units in the Wilthorpe Formation as aseparate member the Beatty Park Member The westerlyyounging succession contains a northndashsouth S3 foliationaxial planar to a few small-scale parasitic D3 foldsplunging steeply south and is overprinted by F4microfolds and kinks trending 290deg Gold mineralizationis within pyrite which has replaced finely bedded chloriteshale near crosscutting D4 quartzndashankerite veins Highestgrades are found adjacent to D4 faults These and otherstructural observations led Windh (1992) to infer a syn-D4 timing of mineralization However small quartz-veinnetworks possibly related to low-grade mineralization inthe overlying coarsely graded units are deformed by D4microfolding
The Fortnum gold mineralization is hosted by theNarracoota Formation which is truncated to the northagainst the Fortnum Fault and wedges out to the southThe package contains maficndashultramafic schist withoverlying reworked fragmental and volcaniclastic rocksincluding rocks with a supposed felsic volcanic derivationoverlain by the Ravelstone Formation (Hill and Cranney1990)
Mineralization at Trevs (and closely associatedorebodies including a recent discovery named Starlight)is hosted by quartz-vein systems in a westerly dippingsuccession of graded sericitic siltstone and coarse wackewith medium- to coarse-grained feldspar quartz and lithicfragments at least partly derived from the underlyingmaficndashultramafic volcanic rocks The Yarlarweelormineralization is hosted by ovoid lenses of jasperoidalchert within variably schistose maficndashultramafic volcanicrocks including interleaved fine tuffaceous and coarsefragmental layers (Hill and Cranney 1990) The chertlenses are within a westerly dipping reverse D3 shear zonecharacterized by quartzndashchloritendashsericite alteration Gold-bearing quartz(ndashpyrite) veins within the chert pods andwithin magnetite-bearing chlorite schist trend at 120deg dipsteeply north and are parallel to small sinistral D4 faults(D3 in Windh 1992) Windh (1992) also reported a minorset of (dextral) faults trending 070deg and crosscutting theD3 shear zones This may suggest a conjugate fault setrecording eastndashwest compression possibly late during D3rather than during north-northeastndashwest-southwest D4compression
Mining at the Fortnum group of workings from 1990to 1998 yielded 11 928 kg of gold from 4685 Mt of orewith an average recovered grade of 254 gt gold (Swagerand Myers 1999) Remaining measured and indicatedresources at Fortnum including Trevs and Starlightcontain an additional 17 970 kg of gold with a further4340 kg of gold estimated within inferred resources(Perilya Mines NL 1998)
Wembley deposit
The Wembley deposit is located approximately 18 kmsouthwest of Peak Hill and 25 km southeast of MurphyWell (from the Peak Hill road) Although rewarding(average grade of 175 gt gold) ore production was verysmall (less than 1800 t)
43
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The Wembley mineralization is hosted in alteredmetabasite rocks within a major shear zone trending 120degThe mineralized zone strikes at 075deg and dips 63deg to thenorthwest A quartz vein near the old workings strikes at060deg and dips 54deg to the northwest Sedimentary units areintercalated with the volcanic rocks and consist ofturbiditic rocks (greywackendashshale) As at the Durackprospect (see below) quartz mylonite units trending120degndash140deg are within the metabasites
Wilgeena deposit
The Wilgeena (or Hit or Miss) gold mine area is located15 km southeast of the Peak Hill mine Production wasless than 15 000 t at an average grade of 26 gt gold
The deposit is within rocks of the Peak Hill Schist andmore specifically along the contact between the mylonitesand quartzndashsericite schist A northerly trending easterlydipping stoped-out ore lens was approximately 2 m thickThe mineralization is hosted in quartzndashmuscovitendashmagnetite schist Grab samples from the old excavationsreturned values ranging from 3 to 14 gt gold (Mountford1984) Whitfield (1987) estimated inferred resources asapproximately 600 000 t at 244 gt gold
Durack St Crispin and Heines Findprospects
The Durack prospect lies about 12 km south of Peak Hillalong and immediately west of the Old Peak Hill telegraphroad This gold deposit is blind being covered by soil andlateritic material and consists of primary mineralizationand a supergene mineralized zone The prospect wasidentified by a soil anomaly containing up to 100 ppb gold(Sabminco Annual Report 1994)
The prospect area is underlain by rocks ofthe Narracoota Formation which include metabasite(medium- to coarse-grained metabasalts) and maficpyroclastic rocks Thin magnetite-bearing chert bands(possibly chemical sediments) intercalated within themetabasites define a broad synclinal structure A numberof mylonite zones trending 120degndash125deg cut across theNarracoota Formation rocks and contain most of theprimary mineralization Grades intersected during drillingare in the order of 15 gt gold over widths of 4 to 6 m
The primary mineralization is contained within quartzndashsulfide veins and stockworks hosted by altered metabasiterocks The mineralized area is about 14 km long and200 m wide Hydrothermal alteration is pervasive andconsists of quartz chlorite biotite and iron-rich carbonate(ankerite) Pyrite is present as fine disseminations andveinlets Selvages of silicandashpyritendashcarbonate surround themineralized zones
The supergene mineralization at the Durack prospectis controlled by subhorizontal redox fronts within theregolith material Supergene enrichment shows grades ofup to 12 gt gold over an interval of about 5 m In somecases the redox-front-related mineralization developed upto 45 m on each side of the primary zone
The St Crispin prospect is situated 20 km east-southeast of Peak Hill The mineralization is along a north-northwesterly trending structure and hosted in sericite(ndashgraphite) schist of the Peak Hill Schist Quartz veins arepresent in the schists and may host the mineralization
The Heines Find prospect is located 20 km south-southeast of Peak Hill Mineralization can be traced forabout 6 km along the easterly trending contact betweenrocks of the Narracoota Formation and the HeinesMember of the Wilthorpe Formation This contact has adip of 80deg to the north and is sheared In this area theNarracoota Formation consists of strongly deformedpillow lavas and chlorite schist The sedimentary rocks ofthe overlying Heines Member include a basal polymicticconglomerate
Ruby Well group
The Ruby Well area includes a number of mineral leasesfrom which gold has been produced either from surfacematerials or from hard rock (02 t Table 7) The RubyWell leases lie on the northern side of the Great NorthernHighway about 80 km from Meekatharra and 4ndash5 km eastof the Peak Hill turn-off
The area is underlain by the Narracoota Doolgunnaand Karalundi Formations The Hard To Find Ruby Anneand Lucky Call deposits within mafic schist of theNarracoota Formation were exploited between 1912 and1917 Most of the current production (figures notavailable) is from a number of dry-blowing workingssurrounding these old mines
Mikhaburra deposit
The old Mikhaburra gold mine (also known as HoldensFind) is in Narracoota Formation volcanic rocks in thesouthwestern part of BRYAH (Fig 25) The recordedproduction of the Mikhaburra mine is about 226 kg ofgold (MacLeod 1970) The mineralization is associatedwith a system of auriferous quartz veins emplaced alonga shear zone trending about 130deg to 150deg and dipping 68degto the southwest The volcanic rocks include mainlychlorite schist A quartz vein with a strike of 120deg and dipof 58deg southwest lies to the west of the old workings Thisvein is about 1 m wide and locally displays a laminatedstructure
Wilthorpe deposit
The Wilthorpe deposit is hosted by granitic rocks of theDespair Granite (Fig 32) which contains xenoliths ofmafic material Gold mineralization is confined to a zonecontaining quartz veins and flanked by bleached andsilicified wallrocks The ore zone is hydrothermallyaltered with assemblages of chloritendashsericitendashbiotite andquartzndashmuscovitendashbiotitendashtourmaline flanked by near-pervasive silicification In addition to gold the mineralizedveins also contain pyrite galena arsenopyrite andchalcopyrite The wallrock granite has a cataclastic textureand consists of quartz and feldspar lsquoeyesrsquo surrounded bya network of granulated quartz and sericite
44
Pirajno et al
Cashman deposit
The Cashman area on BRYAH includes a number of smallmineral occurrences and deposits containing copperand copperndashgold The old Cashman copper mine isapproximately 250 m from the gold workings In 1917 thismine produced about 7 t of copper ore grading 165copper (Marston 1979) The copper mineralizationconsists of a metre-wide cupriferous limonite vein with astrike of 042deg and a shallow dip to the northwest Oreminerals are chrysocolla and malachite as disseminationsand veinlets (Marston 1979)
In 1937 there was a small production of gold ore fromquartz veins In 1986ndash87 the gold potential of theCashman area was reassessed and on the basis of thiswork a small opencut was excavated from which 8000 tof ore material was produced and stockpiled (Whitfield1987) Gold mineralization is hosted in quartz veins withinmetabasaltic hyaloclastite A 01 m-thick quartz vein in thepit has a strike of 115deg and dips 35deg to the northeast Atand near the surface supergene enrichment is present ina horizon about 30 m wide and dipping about 20deg to thenorth (Whitfield 1987)
Volcanogenic copperndashgolddepositsThe Horseshoe Lights copperndashgold deposit on JAMINDI hasproduced nearly 9 t of gold of which almost 26 t wasrecovered from the copper concentrate operation between1988 and 1993 (Table 7) The Horseshoe Lights depositis hosted in felsic schist of the Narracoota Formation(Bryah Group) The mineralization consists of massivesulfides overlying and flanked by disseminated andstringer sulfides Ore minerals are mainly chalcocitepyrite and chalcopyrite Native copper is also present(Parker and Brown 1990) The host rocks are mylonitizedchlorite schist kaolinitendashsericite schist and quartzndashsericiteschist The geometry of the ore zones (massive sulfidesand stringer zone) alteration patterns (silicificationsericitic and chloritic alteration) predominantly felsiccomposition of the host rocks and metal association (CundashAundashAgndashPbndashZn) suggest that the deposit was originally ofthe volcanogenic massive sulfide type but subsequentlyenriched by supergene processes Average grades havebeen about 8 gt gold about 10 copper and 300 ppmsilver The stringer mineralization is of low gradeaveraging between 02 and 03 gt gold Production ceasedin 1994 Remaining resources (Table 8) are of low-grademineralization
Supergene manganese depositsManganese mineralization is part of a historicallyimportant manganese field first recognized in 1905 withdeposits in the Mount Fraser Mount Padbury Ravelstone(Peak Hill) and Horseshoe areas The manganesemineralization is of supergene origin and related tomanganiferous and hematitic shale units and BIF of theHorseshoe Formation (Bryah Group) as well as units ofthe Padbury Group The chief ore minerals are pyrolusiteand cryptomelane The ore is lateritic locally pisolitic innature and in places forms caps overlying the primarymanganese-rich sedimentary material In places notablyat Horseshoe there is evidence to suggest that someenrichment may have taken place in a palaeodrainagechannel lake or swamp environment (MacLeod 1970)In the Ravelstone area just north of the Peak Hill golddeposit the manganese supergene enrichment appears tohave a structural control
The Horseshoe area has been the main producingregion with production from two deposits 2 and 3 kmnorth and northwest of the Horseshoe townsite (Plate 1)The main production period was from 1948 to 1971 when490 000 t was mined (Table 8) all but 5000 t of whichwas classified as metallurgical-grade ore The enrichedzone was 3 to 45 m thick and typically extended overlengths of 400 to 500 m The North deposit averaged 30 min width whereas the South deposit was fan shapedopening from 20 to 300 m wide at its maximum extentOre consisted of mixed manganese and iron oxides withhighly variable manganese and iron contents Gradesprogressively decreased from 42 to 35ndash38 after 1966
There are several small deposits in the Mount Fraserndash Mount Padbury area about 30 km west of Peak Hill
Figure 32 The west wall of the Wilthorpe opencut showingthe contact between biotitendashsericitendashquartz schistand deformed Despair Granite
45
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
They contain patches of high-grade ore within largedeposits of ferruginous manganese material Productionof high-grade ore occurred sporadically since 1949 andamounted to 7547 t at grades in excess of 46 manganeseA third mining operation commenced at the Millidie (orElsa) deposit in the early 1990s but this has notprogressed to a full-scale commercial operation High-grade mineralization in the area is estimated to containmeasured plus indicated resources of approximately11 000 t of manganese (Table 8)
In the Ravelstone area immediately north-northwestof Peak Hill mining occurred between 1956 and 1964producing 76 237 t of ore at 70ndash90 manganese oxide(Table 8) Remainng measured and indicated resources areestimated as 132 000 t of contained metal (Table 8)Manganese production at Ravelstone was from easterlystriking orebodies reaching lengths of up to 100 m andwidths of 30 m but commonly small and narrow Detailedexamination of one specimen of ore revealed that it wascomposed mainly of cryptomelane and accessorypyrolusite A partial geochemical analysis of the samesample provided the following results 064 wt SiO2465 wt Al2O3 0011 wt P 033 wt MgO 268 wtK2O 7038 wt MnO 119 wt Fe 005 ppm Au650 ppm Co 31 ppm Cu 53 ppm Ni 20 ppm Pb and98 ppm Zn
The manganese ore is characterized by high bariumabundances (3000 ppm to 30 at Mount Fraser3000 ppm to 1 at Horseshoe and 3943 to 9000 ppm atRavelstone)
Iron oreThe Robinson Range Formation (Padbury Group) containsunits of banded iron-formation (Fig 2) within which areareas of supergene enrichment of hematite and goethiteThese constitute demonstrated (pre-JORC code) iron-oreresources estimated at approximately 10 Mt with gradesin excess of 60 iron (Table 8) Enrichment is above twoBIF units approximately 100 m thick separated by ahematitic shale horizon Iron grades of the primary BIFvary between 20 and 50 Hematite and hematitendashgoethite surficial enrichment contains grades in excess of50 iron as determined from the sampling of one ofabout 200 small pods of potentially ore grade material(Sofoulis 1970)
TalcTalc in the Mount Seabrook ndash Livingstone ndash Trillbarregion is present within metasedimentary and meta-volcanic rocks and minor mafic and ultramafic rocks Talcis hosted in metasomatized dolomite orebodies (Plate 1)as a series of steeply plunging lenses (Lipple 1990) TheMount Seabrook deposit was discovered in 1965 and hasproduced over 540 000 t of talc mostly of cosmetic gradebetween 1973 and 1995 Indicated and inferred resourcesredefined at Mount Seabrook and Livingstone amount to172 Mt of ore with a significantly greater potentialbecause the orebodies are open along strike
DiscussionThe Horseshoe Lights VMS-type copperndashgold deposit issyn-volcanic and pre-orogenic All other deposits are ofepigenetic origin and syn- to post-orogenic
Figure 33 schematically depicts a simple regionalmodel of ore genesis for the epigenetic mineral depositsin the BryahndashPadbury ndash Peak Hill Schist (BPPS) tectono-metamorphic domain and the adjacent Yerrida Basin TheYerrida Basin and BPPS domain were tectonicallyjuxtaposed along the northeasterly trending Goodin FaultDeformation which affected the BPPS domain wastransmitted across the Goodin Fault for a few kilometresinto the Yerrida Basin This deformation becomes weakerfrom the Goodin Fault eastward The BPPS domain wassubjected to metamorphism (upper to lower greenschistfacies) At least two phases of metamorphism arerecognized a prograde phase overprinted by a retrogradephase Geothermometry and geobarometry studies inthe area around Peak Hill by Thornett (1995)indicated temperatures of around 500ndash620degC for peakprograde metamorphism and 65 to 7 kbar for minimumpressure of the prograde assemblages The timing ofthis metamorphism is probably linked to the collisionbetween the Pilbara and Yilgarn Cratons (see Tectonicmodel and conclusions) which is postulated to haveoccurred between 1820 and 1800 Ma (Occhipinti et al1999)
A genetic model proposed by Pirajno and Preston(1998) envisages that fluids were generated during phasesof dynamic and thermal metamorphism in the BPPSdomain and that these fluids were largely responsible forthe deposition of mesothermal gold-only and shear-zone-hosted deposits The paragenesis of the alterationassemblages associated with the mesothermal depositsand textural relationships suggest that metamorphism
Figure 33 Sketch illustrating a conceptual model for the originof precious and base metal epigenetic deposits inthe BryahndashPadbury and Yerrida Basins (after Pirajnoand Preston 1998)
FMP71a
Bryah and Padbury Groups
Mooloogool Subgroup
Windplain Subgroup
Direction of fluid movement
170300
Fault Cleavagedevelopment
ARCHAEANBASEMENT
NARRYERTERRANE
Area of Au deposition
Collisionzone
Cleavagelate epigeneticmineralisation
Metamorphism
Basin fluids
YERRIDA
and deformation
Goo
din
Faul
t
development
BRYAHndashPADBURYBASINS BASIN
NW SE
46
Pirajno et al
and mineralization were broadly contemporaneousalthough alteration was in most cases from peak toretrograde metamorphism Exceptions to this are localizedzones of sodium metasomatism (albite and arfvedsonite)which overprint the retrograde assemblages This sodiummetasomatism may be related to central zones ofhigher temperatures within the mineralized structuresOne possible explanation for the widespread sodiummetasomatism is granite magmatism however there is noevidence in either the Bryah or the Padbury Basin ofgranitic plutons intruding the volcano-sedimentarysuccessions Therefore a possible role of graniticmagmatism as one of the heat and metal sources for thehydrothermal solutions based on our present knowledgeis excluded
Hydrothermal solutions responsible for the emplace-ment of mesothermal lodes are considered to be generatedin tectonically active regions and are associated withcompressional and extensional tectonics (Kerrich andCassidy 1994) The mesothermal-style gold-only lodesof the BPPS domain were formed in a compressionalsetting characterized by thin-skinned thrusting associatedwith prograde and retrograde mineral assemblages(Pirajno 1996) Dyer (1991) concluded that the hydro-thermal mineralization in the LaboucherendashFortnumarea was generated by the mixing of two fluids ofdifferent density and salinity Deeply sourced hot salineCO2-bearing fluids were mixed with cooler less salinenear-surface aqueous fluids The available evidencepoints to the conclusion that the mineralizing fluids wereat first generated during compression and dehydrationand moved along ductile to brittle structures Duringsubsequent phases meteoric fluids would have infiltratedalong the same structures and mixed with the hottermetamorphic solutions The whole mechanism couldhave been repeated again in the next phase of compressionand extension leading to multiphase ore genesis processesin which the latest phase leaves the most detect-able imprint There is no obvious link with magmaticactivity
Other metal deposits in the BryahndashPadbury Basin aresupergene manganese and iron ore (Pirajno and Preston1998) The timing of the weathering event that led to thesupergene enrichment of the manganese and iron ores isnot known although it may be possible that the warm andhumid climate during the middle Tertiary (Cockbain andHocking 1990) played a major role in the genesis of thissupergene mineralization
Tectonic model andconclusions
Gee (1979) Hynes and Gee (1986) Windh (1992) andGee and Grey (1993) interpreted the geodynamicevolution of the lsquoGlengarry Basinrsquo as defined by Gee andGrey (1993) in terms of an ensialic or intracontinentalbasin Tyler and Thorne (1990) Myers (1993) Martin(1994) and Myers et al (1996) proposed models in whichthe former lsquoGlengarry Basinrsquo would have formed in aback-arc setting during the convergence of the Pilbara andYilgarn Cratons between 2000 and 1800 Ma
In the light of the re-interpretation of the formerlsquoGlengarry Basinrsquo into the Bryah Padbury and YerridaBasins some modification of the above tectonic schemesis necessary Lack of sufficient geochronological datahowever poses the problem of the precise timing ofevents This lack of information must be taken intoaccount when modelling basin tectonics Pirajno (1996)and Pirajno et al (1998b) suggested two models for thegeodynamic evolution of the BryahndashPadbury and YerridaBasins 1) the basins were formed during convergence andsubsequent collision in a back-arcndashforeland basin settingin which these basins were opened and infilled duringsouthward subduction of oceanic crust (extensional backarc) and subsequently overlain by sediments in a newlydeveloped foreland basin (syn-collisional) and 2) thebasins were formed at the time of the oblique collisionbetween the Pilbara and Yilgarn Cratons as pull-apartstructures in a strike-slip setting with transitions fromextensional (transtension) to compressional (transpression)regimes
In this study we propose a model whereby the BryahBasin was formed as a back-arc rift with a component ofrifting along the Yilgarn continental margin a kind ofproto-oceanic rift comparable to that of the present-day Guayamas Basin in the Gulf of California (Lonsdaleand Becker 1985) The Padbury Basin developed as aforeland basin on top of the Bryah Basin during theoblique collision of the Pilbara and Yilgarn Cratons Ourmodel is shown in Figure 34 in which two stages areschematically depicted and briefly discussed below
The Bryah Basin was formed by processes of back-arc opening during subduction of oceanic crust beneaththe northern margin of the Yilgarn Craton approximately
Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins withinthe context of the Capricorn Orogen (modified from Myers 1990 1993 and Myers et al 1996)a) At about 1960ndash1950 Ma development of Andean-type magmatic arc on a microcontinental active margin back-arcrifting and spreading with creation of oceanic crust (dominantly high-Mg and high-Fe tholeiite associated withsubvolcanic peridotitic cumulates representing future maficndashultramafic schist of the Narracoota Formation) anderuption of basaltic hyaloclastites probably from the same source as the maficndashultramafic material occurs on passivemargin of Yilgarn Craton Insets schematically show geochemical signatures of these volcanic rocks (see text fordetails)b) Capricorn Orogeny involved collision between the Pilbara and Yilgarn Cratons with formation of fold-and-thrustbelts on both northern and southern sides of orogen and thrusting of oceanic crust over hyaloclastite and margin ofYilgarn Craton The thrust separating oceanic crust material from hyaloclastite is represented by the Murchison Fault(see Plate 1) Chondrite-normalized REE patterns for metabasites and hyaloclastites of the Narracoota Formation areshown in the insets
47
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
N S
N S
Marymia In
lier
YILGARN
Backarc riftMicrocontinent
andvolcanic arc
Seafloor
Seafloor
Oceaniccrust
lt 1960ndash1950 Ma
PILBARA
PILBARAYILGARN
Fold-and-thrustbelt
PadburyBasin Bryah Basin
1820ndash1800 Ma
Present-dayBryahndashPadbury
area
Lithosphere
FMP376 170300
4000
3000
2000
1000
00 21 3
FeOMgO FeOMgO Ni Cr
1
2
0
3
0 1 2
La Eu Lu
Sam
ple
chon
drite
100
10
16
Sam
ple
chon
drite
100
10
2La Eu Lu
2
Cr
(ppm
)
TiO
(
)
TiO x1002
Mid-oc
ean r
idge
2
Clastic rocks
Padbury Group
Archaean basement
Metabasic rocksof Narracoota FormationHyaloclastites(Narracoota Formation)
Karalundi Formation
Oceanic crust
a)
b)
48
Pirajno et al
between 1960 and 1950 Ma (Occhipinti et al 1999Fig 34a) Myers (1993) speculated that a southwardoceanic subduction system with a south-facing Andean-type magmatic arc had developed off the northern passivemargin of the Yilgarn Craton Remnants of arc magmaticsuites have not been found but may be buried under theMesoproterozoic Bangemall Basin Back-arc rifting alsoaffected the northern margin of the Yilgarn Craton whererift propagation is postulated to have progressivelyadvanced from west to east through a succession ofcrustalndashlithospheric thinning rupture and grabenformation In this model the Marymia Inlier is a remnantof a rift shoulder (Fig 34a)
The closing of the ocean between the Pilbara andYilgarn Cratons was followed by the oblique collisionbetween the rifted passive margin on the Pilbara side aninferred active magmatic arc and the passive northernmargin of the Yilgarn Craton Closure of the interveningocean (1820ndash1800 Ma) resulted in inversion of the Bryahback-arc rift and thrusting of oceanic crust (nowNarracoota Formation) over the Yilgarn Cratonrsquos northernmargin (Fig 34b) During and following this collisionevent the southern side of the Pilbara was tectonicallysliced by major thrusts whereas most of the tectonictransport of the inferred magmatic and oceanic crust rockswas towards the south (Myers 1993)
High-Mg tholeiitic rocks with pillow structuressheeted dykes the Trillbar layered complex sea-floor metasomatism and trace and rare-earth elementgeochemistry support the oceanic crust model for theorigin of the mafic and ultramafic schist of the NarracootaFormation The hyaloclastites on the other hand wereerupted in shallow waters and locally characterized byexplosive activity and have mixed and overlappinggeochemical signatures with the mafic schist This featurecan be interpreted as suggesting a more continentalenvironment of emplacement and therefore were emplacedon Yilgarn crust (Fig 34a) In contrast to the maficndashultramafic schist the hyaloclastites are relativelytectonically undeformed Their contact with the maficndashultramafic schist is along the Murchison Fault (Plate 1)We conclude that the Murchison Fault represents atectonic boundary between these two components of theNarracoota Formation and that oceanic crust material(precursors of the maficndashultramafic schist) were thrustover the continental hyaloclastites during the CapricornOrogeny as shown in Figure 34b The suggested Gulf ofCalifornia-type palaeoenvironmental setting with thefuture Marymia Inlier as one of the rift shoulders(analogous to the California peninsula) is shown inFigure 34a
The absence of volcanic rocks of intermediate(andesitic) compositions suggests that the NarracootaFormation metabasites were not formed in a subduction-related volcanic-arc setting as proposed by Myers et al(1996) However we concur with Sun (1997) that theboninitic component in the chemistry of the metabasites(see inset of Fig 34 and Figs 12ndash15) needs explanationWe suggest that these boninitic characteristics of theNarracoota Formation can be compared to the boninitesof the Koh Ophiolite in New Caledonia (Meffre et al
1996) which are considered to have formed in a back-arc spreading centre
The overall high MgO and low TiO2 abundancesdepleted REE and low LaYb ratios of the NarracootaFormation are also consistent with the origin of theNarracoota Formation metabasites from a mantle plume(Pirajno et al 1998a)
The Padbury Basin was interpreted by Martin (1994)as a retroarc foreland basin recording the collision of theYilgarn and Pilbara Cratons During and followingcollision between 1820 and 1800 Ma (Occhipinti et al1999) back-arc volcanism ceased and a foreland basindeveloped on top of the back-arc succession (BryahGroup) This basin was filled by siliciclastic rocks only(Padbury Group) During continued regional compressionthe BryahndashPadbury Basin developed into a fold-and-thustbelt and was partly thrust over the Yerrida Basin alongthe Goodin Fault
In summary the convergence between the ArchaeanPilbara and Yilgarn Cratons resulted in progressivecompressional deformation that affected the Bryah andPadbury Groups as a coherent package At least fourgroups of structures are recognized in the regionaldeformation of the volcano-sedimentary succession andtheir reworked basement (ie Yarlarweelor GneissComplex) This same deformation and associatedmetamorphism was responsible for the mesothermal gold-only lodes of the Bryah and Padbury Basins
AcknowledgementsWe acknowledge the contribution of colleagues whoparticipated in the Glengarry mapping program JohnMyers N G Adamides and P G Le Blanc SmithRichard Davy first introduced the senior author to the areaWe are also grateful to the local pastoral community fortheir hospitality The geological staff of LabouchereFortnum Peak Hill and Harmony gold mines are thankedfor sharing their knowledge with us
49
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
References
ADAMIDES N G 1998 Geology of the Doolgunna 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BAGAS L B 1998 Geology of the Marymia 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BARNETT J C 1975 Some probable Lower Proterozoic sedimentsin the Mount Padbury area Western Australia Geological SurveyAnnual Report 1974 p 52ndash54
BARRETT F 1989 A study of wallrock alteration associated withgold mineralization mdash Peak Hill and Mt Pleasant area WesternAustralia Geological Survey M-series Item 7706 A41555(unpublished)
BRADLEY J J FAULKNER J A and SANDERS A J 1997Geochemical mapping of the Robinson Range 1250 000 sheetWestern Australia Geological Survey 1250 000 RegolithGeochemistry Series Explanatory Notes 57p
BREITKOPF J H and MAIDEN K J 1988 Tectonic setting of theMatchless Belt pyritic copper deposits Namibia EconomicGeology v 83 p 710ndash723
BUNTING J A COMMANDER D P and GEE R D 1977Preliminary synthesis of Lower Proterozoic stratigraphy andstructure adjacent to the northern margin of the Yilgarn BlockWestern Australia Geological Survey Annual Report 1976p 43ndash48
BURKE K C KIDD W S F TURCOTTE L DEWEY J FMOUGINIS-MARK P J PARMENTIER E M SENGORA M and TAPPONIER P E 1981 Tectonics of basalticvolcanism in Basaltic volcanism on the terrestrial planets HoustonLunar and Planetary Institute p 803ndash898
COCKBAIN A E and HOCKING R M 1990 Regolith in Geologyand mineral resources of Western Australia Western AustraliaGeological Survey Memoir 3 p 591ndash602
CRAWFORD R A FAULKNER J A SANDERS A J LEWISJ D and GOZZARD J R 1996 Geochemical mapping ofthe Glengarry 1250 000 sheet Western Australia GeologicalSurvey 1250 000 Regolith Geochemistry Series Explanatory Notes57p
DAVY R PIRAJNO F SANDERS A J and MORRIS P A1999 Regolith geochemical mapping as an adjunct to geologicalmapping and exploration examples from three contiguousProterozoic basins in Western Australia Journal of GeochemicalExploration v 66 p 37ndash53
DIXON J and WILLIAMS G 1983 Reaction softening in mylonitesfrom the Arnaboll thrust Sutherland Scottish Journal of Geologyv 19 p 157ndash168
DUNCAN A R 1987 The Karoo igneous province mdash a problemarea for inferring tectonic setting from basalt geochemistry Journalof Volcanology and Geothermal Research v 32 p 13ndash34
DYER F L 1991 The nature and origin of gold mineralization atthe Fortnum Nathans and Labouchere deposits Glengarry BasinWestern Australia University of Western Australia BSc Honoursthesis (unpublished)
ELIAS M 1982 Belele WA Western Australia Geological Survey1250 000 Geological Series Explanatory Notes 21p
ELIAS M BUNTING J A and WHARTON P H 1982 GlengarryWA Western Australia Geological Survey 1250 000 GeologicalSeries Explanatory Notes 27p
ELIAS M and WILLIAMS S J 1980 Robinson Range WAWestern Australia Geological Survey 1250 000 Geological SeriesExplanatory Notes 32p
FISHER R V and SCHMINCKE H-U 1984 Pyroclastic rocksBerlin Springer-Verlag 472p
GEE R D 1979 The geology of the Peak Hill area Western AustraliaGeological Survey Annual Report 1978 p 55ndash62
GEE R D 1987 Peak Hill WA (2nd edition) Western AustraliaGeological Survey 1250 000 Geological Series Explanatory Notes24p
GEE R D 1990 Nabberu Basin in Geology and mineral resourcesof Western Australia Western Australia Geological SurveyMemoir 3 p 202ndash210
GEE R D and GREY K 1993 Proterozoic rocks on the Glengarry1250 000 sheet mdash stratigraphy structure and stromatolitebiostratigraphy Western Australia Geological Survey Report 4130p
HALL W D M and GOODE A D T 1978 The Early ProterozoicNabberu Basin and associated iron formations of Western AustraliaPrecambrian Research v 7 p 129ndash184
HANNA J P and IVEY M E 1990 Labouchere and Deep Southgold deposits in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 667ndash670
HARPER M HILL M G RENTON J I and THORNETTS E 1998 Gold deposits of the Peak Hill area WesternAustralia in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 81ndash87
HILL A D and CRANNEY P J 1990 Fortnum golddeposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 665ndash666
HYNES A and GEE R D 1986 Geological setting andpetrochemistry of the Narracoota Volcanics Capricorn OrogenWestern Australia Precambrian Research v 31 p 107ndash132
JENSEN L S 1976 A new cation plot for classifying subalkalicvolcanic rocks Canada Ontario Division of Mines MP 66 22p
KERRICH R and CASSIDY K F 1994 Temporal relationships oflode gold mineralization to accretion magmatism metamorphismand deformation mdash Archaean to present a review Ore GeologyReviews v 9 p 263ndash310
LE MAITRE R W 1989 A classification of igneous rocksand glossary of terms Oxford Blackwell Scientific Publications193p
50
Pirajno et al
LEWIS J D 1971 The geology of some carbonate intrusions in theMount Fraser area Peak Hill Goldfield Western Australia WesternAustralia Geological Survey Annual Report 1970 p 50ndash56
LIPPLE S L 1990 Talc in Geology and mineral resources of WesternAustralia Western Australia Geological Survey Memoir 3p 678ndash679
LISTER G S and SNOKE A W 1984 SndashC mylonites Journal ofStructural Geology v 6 p 617ndash638
LONSDALE P and BECKER K 1985 Hydrothermal plumes hotsprings and conductive heat flow in the southern trough ofGuayamas Basin Earth and Planetary Science Letters v 73p 211ndash225
LUCAS S B STERN R A SYME E C REILLY B A andTHOMAS D J 1996 Intraoceanic tectonics and the developmentof continental crust 192 ndash 184 Ga evolution of the Flin Flon beltCanada Geological Society of America Bulletin 108 p 602ndash629
MacLEOD W N 1970 Peak Hill WA (1st edition) WesternAustralia Geological Survey 1250 000 Geological SeriesExplanatory Notes 21p
MARSHAK S TINKHAM D ALKMIN F BRUECKNER Hand BORNHORST T 1997 Dome-and-keel provinces formedduring Palaeoproterozoic orogenic collapse mdash core complexesdiapirs or neither examples from the Quadrilatero Ferrifero andthe Penkean orogen Geology v 25 p 415ndash418
MARSTON R J 1979 Copper mineralization in Western AustraliaWestern Australia Geological Survey Bulletin 13 208p
MARTIN D McB 1992 Turbidite facies and depositionalenvironment of the Precambrian Labouchere Formation PadburyGroup Western Australia Geological Society of AustraliaAbstracts 32 p 168ndash170
MARTIN D McB 1994 Sedimentology sequence stratigraphy andtectonic setting of a Palaeoproterozoic turbidite complex LowerPadbury Group Western Australia University of Western AustraliaPhD thesis (unpublished)
MARTIN D McB 1998 Lithostratigraphy and structure of thePalaeoproterozoic Padbury Group Milgun 1100 000 sheet WesternAustralia Western Australia Geological Survey Report 62 57p
McDONALD I R 1994 Final Report on the Glengarry nickel projectES502 and E51384 Western Australia Geological SurveyM-series Item 7706 A41555 (unpublished)
McMILLAN N M 1993 Structure metamorphism alteration andtiming of gold mineralisation at Marymia Gold Project in theMarymia Dome in An international conference on crustal evolutionmetallogeny and exploration of the Eastern Goldfields ExtendedAbstracts compiled by P R WILLIAMS and J A HALDANEAustralian Geological Survey Organisation Record 199354p 243ndash244
McPHIE J DOYLE M and ALLEN R 1993 Volcanic texturesHobart Tasmanian Government Printing Office 198p
MEFFRE S AITCHISON J C and CRAWFORD A J 1996Geochemical and tectonic significance of boninites and tholeiitesfrom the Koh Ophiolite New Caledonia Tectonics v 15p 67ndash83
MOUNTFORD B R 1984 Preliminary geological report onProspecting Licences 52104 and 52105 Mt Padbury area WesternAustralia Western Australia Geological Survey M-series Item3688 A16393 (unpublished)
MYERS J S 1989 Thrust sheets on the southern foreland of theCapricorn Orogen Robinson Range Western Australia WesternAustralia Geological Survey Report 26 Professional Papersp 127ndash130
MYERS J S 1990 Capricorn Orogen in Geology and mineralresources of Western Australia Western Australia GeologicalSurvey Memoir 3 p 197ndash198
MYERS J S 1993 Precambrian history of the West Australian cratonand adjacent orogens Annual Reviews of Earth and PlanetaryScience v 21 p 453ndash485
MYERS J S SHAW R D and TYLER I M 1996 Tectonicevolution of Proterozoic Australia Tectonics v 15 p 1431ndash1446
NELSON D R 1997 Compilation of SHRIMP UndashPb zircongeochronology data 1996 Western Australia Geological SurveyRecord 19972 189p
NELSON D R 1998 Compilation of SHRIMP UndashPb zircongeochronology data 1997 Western Australia Geological SurveyRecord 19982 242p
OrsquoNIONS R K PANKHURST R J and GRONVOLD K 1976Nature and development of basalt magma sources beneath Icelandand the Reykjanes ridge Journal of Petrology v 17 p 315ndash338
OCCHIPINTI S A GREY K PIRAJNO F ADAMIDES N GBAGAS L DAWES P and LE BLANC SMITH G 1997Stratigraphic revision of Palaeoproterozoic rocks of the YerridaBryah and Padbury Basins (former Glengarry Basin) WesternAustralia Geological Survey Record 19973 57p
OCCHIPINTI S A and MYERS J S 1999 Geology of the Moorarie1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 20p
OCCHIPINTI S A MYERS J S and SWAGER C P 1998aGeology of the Padbury 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes29p
OCCHIPINTI S A SHEPPARD S NELSON D R MYERS J Sand TYLER I M 1998b Syntectonic granite in the southernmargin of the Palaeoproterozoic Capricorn Orogen WesternAustralia Australian Journal of Earth Sciences v 45 p 509ndash512
OCCHIPINTI S A SHEPPARD S and TYLER I M 1999Palaeoproterozoic tectonic evolution of the southern margin of theCapricorn Orogen Western Australia Last Conference of theMillenium Halls Gap WA Abstract volume p 173ndash174
OCCHIPINTI S A SWAGER C P and PIRAJNO F 1998cStructuralndashmetamorphic evolution of the Palaeoproterozoic Bryahand Padbury Groups during the Capricorn Orogeny WesternAustralia Precambrian Research v 90 p 141ndash158
PARKER T W H and BROWN T 1990 Horseshoe goldndashcopperndashsilver deposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 671ndash675
PEARCE J A ERNEWEIN M BLOOMER S H PARSON L MMURTON B J and JOHNSON L E 1995 Geochemistry ofLau Basin volcanic rocks influence of ridge segmentation and arcproximity Geological Society Special Publication v 81p 53ndash75
PEARCE T H GORMAN B E and BIRKETT T C 1977 Therelationship between major element chemistry and tectonicenvironment of basic and intermediate volcanic rocks Earth andPlanetary Science Letters v 36 p 121ndash132
PERILYA MINES NL 1998 Annual report for the year ending30 June 1998 60p
PETERS S G 1993 Polygenetic meacutelange in the Hodgkinsongoldfield Northern Tasman Orogenic Zone Australian Journal ofEarth Sciences v 40 p 115ndash129
PIRAJNO F 1996 Models for the geodynamic evolution of thePalaeoproterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1995ndash96 p 96ndash103
PIRAJNO F and ADAMIDES N G 2000 Geology andmineralization of the Palaeoproterozoic Yerrida Basin WesternAustralia Western Australia Geological Survey Report 60 43p
51
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
PIRAJNO F and ADAMIDES N G 1998 Geology of the Thaduna1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 24p
PIRAJNO F ADAMIDES N G and FERDINANDO D D 1998aGeology of the Glengarry 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes16p
PIRAJNO F ADAMIDES N G OCCHIPINTI S A SWAGERC P and BAGAS L 1995a Geology and tectonic evolution ofthe early Proterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1994ndash95 p 71ndash80
PIRAJNO F BAGAS L SWAGER C P OCCHIPINTI S A andADAMIDES N G 1996 A reappraisal of the stratigraphy of theGlengarry Basin Western Australia Western Australia GeologicalSurvey Annual Review 1995ndash96 p 81ndash87
PIRAJNO F and DAVY R 1996 Mafic volcanism in thePalaeoproterozoic Glengarry Basin Western Australia andimplications for its tectonic evolution Geological Society ofAustralia Abstracts no 41 p 343
PIRAJNO F and OCCHIPINTI S A 1995 Base metal potential ofthe Palaeoproterozoic Glengarry and Bryah Basins WesternAustralia Recent developments in base metal geology andexploration Australian Institute of Geoscientists Bulletin 16p 51ndash56
PIRAJNO F and OCCHIPINTI S A 1998 Geology of the Bryah1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 41p
PIRAJNO F OCCHIPINTI S LE BLANC SMITH G andADAMIDES N G 1995b Pillow lavas in the Peak Hill terranesWestern Australia Geological Survey Annual Review 1993ndash94p 63ndash66
PIRAJNO F OCCHIPINTI S A and SWAGER C P 1998bGeology and tectonic evolution of the Palaeoproterozoic BryahPadbury and Yerrida Basins (formerly Glengarry Basin) WesternAustralia Precambrian Research v 90 p 119ndash140
PIRAJNO F and PRESTON W A 1998 Mineral deposits of thePadbury Bryah and Yerrida Basins in Geology of Australian andPapua New Guinean mineral deposits edited by D A BERKMANand D H MACKENZIE Australasian Institute of Mining andMetallurgy Monograph 22 p 63ndash69
RAYMOND L A 1984a Classification of meacutelanges GeologicalSociety of America Special Paper 198 p 7ndash20
RAYMOND L A 1984b Meacutelanges their nature origin andsignificance Geological Society of America Special Paper 198170p
ROLLINSON H R 1993 Using geochemical data evaluationpresentation interpretation Singapore Longman 352p
SABMINCO ANNUAL REPORT 1994 Annual report on miningleases M52202ndash203 vol 1 2 and 3 Western Australia GeologicalSurvey M-series Item 8967 A42856 (unpublished)
SCHILLING J-G 1982 Galapagos hot spot ndash spreading centersystem 1 Spatial petrological and geochemical variations (83degWndash101degW) Journal of Geophysical Research v 87p 5593ndash5610
SCHILLING J-G MEYER P S and KINGSLEY R H 1982Evolution of the Iceland hot spot Nature v 296 p 313ndash320
SHEPPARD S and SWAGER C P 1999 Geology of the Marquis1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 21p
SHEPPARD S OCCHIPINTI S A NELSON D and TYLERI M 1999 Granites of the southern Capricorn Orogen WesternAustralia Geological Society of Australia Abstracts no 56p44-46
SOFOULIS J 1970 Iron deposits of the Robinson Range Peak HillGoldfield WA Western Australia Geological Survey Record19706 10p
SPEAR F S 1993 Metamorphic phase equilibria and pressurendashtemperaturendashtime paths Mineralogical Society of AmericaMonograph p 799
STERN R A SYME E C and LUCAS S B 1995 Geochemistryof 19 Ga MORB and OIB-like basalts from the Amisk collageFlin Flon belt Canada evidence for an intra-oceanic originGeochimica et Cosmochimica Acta v 59 p 3131ndash3154
SUBRAMANYA A G FAULKNER J A SANDERS A J andGOZZARD J R 1995 Geochemical mapping of the Peak Hill1250 000 sheet Western Australia Geological Survey 1250 000Regolith Geochemistry Series Explanatory Notes 59p
SUN S-S 1982 Chemical composition and origin of the Earthrsquosprimitive mantle Geochimica et Cosmochimica Acta v 46p 179ndash192
SUN S-S 1997 Chemical and isotopic features of Palaeoproterozoicmafic igneous rocks of Australia implications for tectonic processesAustralian Geological Survey Organisation Record 19974p 119ndash122
SWAGER C P and MYERS J S 1999 Geology of the Milgun1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 27p
THORNETT S E 1995 The nature origin and timing of goldmineralization in Proterozoic rocks of the Peak Hill District WAUniversity of Western Australia MSc thesis (unpublished)
TYLER I M 1999 Palaeoproterozoic orogeny in Western AustraliaGeological Society of Australia Abstracts no 56 p 47ndash49
TYLER I M PIRAJNO F BAGAS L MYERS J S andPRESTON W A 1998 The geology and mineral deposits of theProterozoic in Western Australia Australian Geological SurveyOrganisation Journal of Geology and Geophysics v 17p 223ndash244
TYLER I M and THORNE A M 1990 The northern margin ofthe Capricorn Orogen Western Australia mdash an example of anEarly Proterozoic collision zone Journal of Structural Geologyv 12 p 685ndash701
WANG P and GLOVER L 1992 A tectonic test of the mostcommonly used geochemical discriminant diagrams and patternsEarth Science Reviews v 33 p 111ndash131
WATKINS K P 1983 Petrogenesis of Dalradian albite porphyroblastschists Journal of the Geological Society of London v 140p 601ndash618
WHITFIELD G B 1987 Wilgeena gold mine Progress report MS52111 and 112 Western Australia Geological Survey M-seriesItem 5862 A28194 (unpublished)
WINDH J 1992 Tectonic evolution and metallogenesis of the EarlyProterozoic Glengarry Basin Western Australia University ofWestern Australia PhD thesis (unpublished)
52
Pirajno et al
Appendix
Gazetteer of localities
Locality AMG coordinateEasting Northing
5 Mile Well 616500 7158100Beatty Park Bore 632200 7163500Cashman opencut 662129 7126994Dandy Well 646400 7188740Despair Bore 625300 7169600Durack prospect 670440 7150520Durack Well 671600 7143000Fortnum mine 636372 7197627Friday Pool 558620 7178625Harmony (New Baxters Find) opencut 664145 7161267Heines Find prospect 682759 7145164Horseshoe Lights opencut 662648 7193894Horseshoe Mn mine 656990 7186510Horseshoe Au prospect 661219 7182977Jubilee mine 671889 7165443Labouchere mine 627730 7204710Livingstone mine 567540 7171032Lucky Call prospect (Ruby Well group) 676747 7127188Mikhaburra (Holdens Find) opencut 656252 7130396Millidie (Elsa) deposit 643000 7160000Mount Fraser 639200 7163300Mount Labouchere 630360 7212620Mount Padbury 627400 7164100Mount Padbury mine 635100 7165100Mount Pleasant opencut 674287 7161900Mount Seabrook mine 572631 7168338Nathan Bitter mine 631100 7199820Nathans Deep South mine 631713 7198812Peak Hill opencut 672190 7163003Peak Hill townsite 673000 7163150Randell Bore 688000 7145200Ravelstone Group 669000 7167500Ravelstone opencut (Mn) 665734 7166777Ravelstone opencut (Mn) 669313 7166423Ruby Duffer Well 675290 7136000Ruby Well group 677900 7129700St Crispin prospect 691358 7158940Tank Well 675400 7147000Top Dimble Well 616600 7167600Trevs (and Starlight) opencut 636412 7198887Trillbar Homestead 576023 7170846Wembley mine 663983 7149044Wilgeena (Hit or Miss) mine 685369 7155622Wilthorpe mine 630414 7176521Yarlarweelor opencut 636723 7196423
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting
The Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collisionzone between the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains maficndashultramafic igneous rocks turbidites and chemical sedimentary rocks formed duringback-arc sea-floor spreading and rifting on the northern margin of the Yilgarn Cratonat or near a mid-oceanic ridge The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of theBryah Basin as a foreland structure resulting from either thec 1800 Ma oblique collision of the Pilbara and YilgarnCratons (Capricorn Orogeny) or the c 2000 Ma collisionof the Glenburgh Terrane and the Yilgarn Craton (GlenburghOrogeny) Important mineral deposits include orogenicgold-only lode deposits copperndashgold volcanogenic massivesulfides sedimentary and lateritic manganese and iron oreThe origin of the gold mineralization is related tometamorphism and deformation linked to the CapricornOrogeny at c 18 Ga The formation of other deposits isrelated to pre-orogenic syngenetic processes
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone (08) 9222 3459 Fax (08) 9222 3444wwwdmewagovau
Wandery
Creek
Wandery
Gum
Creek
Beda
burra
Easter
nCr
eek
Dim
ble
Dimble
Cree
k
Mt Fr
aser
Creek
Creek
Mt Fraser
Millidie CreekMURCHISONRIVER
MURCHISON
RIVER
GASCOYNE
RIVE
R
GASCOYNE
RIVER
Ck
Cree
k
Creek
Beatty Park B (abd)
Reefer W(abd)
YARLAR
WEELOR
MILGUN
ROAD
MEEKATHARRA
ROAD
ASHBURTON DOWNS
TrillbarYarlarweelor
ROADTRILLBAR
Mt Padbury
Yd
Yd
Yd
Yd
Yd Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd
MT CLARE
MEEKATHARRA
ROAD
Bryah
Narracoota
Old Peak Hill (ruin)
Mikhaburra
Yd
Yd
Yd
Yd
(ruin)Bilyuin Hotel
Yulga Jinna Community
Doolgunna
Yd
YdYd
Yd
THADUNACOPPER MINE ROAD
Yd
Karalundi
Yd
Yd
Yd
Yd
Bryah
Yd
Mikhaburra
Yarla
rwee
lor H
omes
tead
44
km
Milgun Homestead 4 km
Milgun Homestead 72 km
Meekatharra 108 km
Meekatharra 53 km
Mooloog
ool Ho
mestead
35 km
Diamond
Well
Homest
ead 68
km
Neds
Creek
Homest
ead 33
km
Kumerina Homestead 98 km
Three Rivers Homestead 42 km
MT LABOUCHERE
MT ARAPILES
CM 15
MT BEASLEY
MT SEABROOK
TALB
OT
DIVIDE
RED HILL
722 m
Yd
Yd
Yd
Yds
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd Yd
Yd
Yd
Yd
Yd
628 m
MT PADBURYMT FRASER
MT MAITLAND
R O B I N S O N
591 m
695 m
799 m
Yd
Yd
GREAT
NORTH
ERN
HIGH
WAY
HILL
THRE
E RIVER
S
ROAD
PEAK
MEEKATHARRA
ROAD
ROAD
PEAK HILL
R A N G E
Peak Hill
MC 14
NOONYEREENA HILL
MT LEAKE
MC 13
MC 12
MC 11
ASHBURTON DOWNS
core yard
602 m
605 m
640 m
Peak Hill
Yd
Earrie W Daulby W
Jilly Jilly W
Outcamp W (abd)
Watt W
Curly W
B
6 Mile B4 Corners W
Laurel W (abd)Bull W
Labouchere W
Sam W
Duffey W
Horseshoe W
Dandy W (PD)(abd)
Carlyon B (PD)
Kinder B (PD)
Vacation B
Garret W
Kylie B
Camel B
W (abd)Billarra W
Bull Paddock WAlarm B
Carlyon RH (PD)
Yaddyarra W
Mowara BGullgogo B
Horseshoe No 2 W (PD)Horseshoe No 1 W (PD)
Stink W (PD)
Crain B
Windalah B
Yandinhah W
Coomballey B
No 1 B
4 Corners W (abd)
Cement Tank W (abd)
Cork Tree B
Southern Cross W3 Corners B
Thompson B (abd)
W (abd)
Tommy B
Seabrook W17 Mile W (abd)
Midnight B
Gidgie WW (abd)
Snake W Dry W
Black Hill W
Minniarra W
Top Minniarra W
Doherty W
The Hut W
W
Red Hill W
Randall W
Dooley W
Walebie W
Mandora B
Babbawiri Pool
Winja B
WHWH
PBedaburra P
Friday P
Kerba P
S
Wandery P
W
Valley B
Quartz B
House WSouthern Cross W
P
Peak Hill B Shed W
Boundary B
No 3 W
McPherson B
Pinnacle B
WH
Mt Leake B
Hill B
Jack W
W
Mt Leake B
John B
No 2 B
Cow Hole B
WH
Red B
WH
No 6 W
Marck W
No 11 W
Limestone W
Dummy B
No 1 B
No 8 B
D
Government W
Central B
Gale W
W
West W
No 6 B
Ealgareengunna WH
Noonyereena P
Beefwood T
Narracoota B
WH
WH
Railway B
Meek W32 Mile W (Govt)
32 Mile W
Ruby W
Ruby South W
W (abd)
Scotty W
Ord W
Little Mill B
Killarney W
West WMillie W
D
Ord W (abd)
W(abd)
Eastern Stock W No 8(abd)
Gigbywabby W (PD)(abd)
No1 W
Paddy B (abd)
Kelly BRelief B
Top Dimble W
Despair B
Boundary B (PD)
B (abd)
Padbury W
Govt W (abd)
Bottom Dimble WHaystack W
Wandarrie W
Middle B
W
WW
W
No 3 B
Fish Pond B
Wooly Paddock B
5 Mile W
Knox W
Sleepy Hollow W (abd)
Old Homestead WB
Widespread W
W
Kennedy W
W
Deep W
Ross B
Gibbywabby WDandy W (PD)
Brunsden W
17 Mile WBrown Creek B (abd)
7 Mile BDavid W
17 Mile B (PD)
Lefeuvre W
Mick W
W (abd)
WH
WHWH
WH
WH
WH WH
S
Gum W (abd)
Wilthorpe W (PD)
1 Mile W
Bullgullan B
Wongawar B
Jinglegunna W
No 13 B
Orchard W
Fraser WW
Sorenson B
Central B
Tank W (abd)Bitter W (abd)
Murphy W
Trudgeon W
Moore W Spelling W
Randell B
Deadhorse W (abd) McLean W
Bore Hole BOHara W
Murchison W (abd)
McCarthy W2 Tank W (abd)
Hill W
Telegraph W
Cashman B (abd)
Ruby Centre W
White WW
McCann W (abd)
Holden W
Gum W
McDonald W
Don BNo 2 BNo 1 B
Bull W
D
D
DD
Gum Well P
Malleah P
Fremanga P
Yallaginda W (abd)
No 7 B (abd)
Stalley W (abd)
Durack W
No 26 W (abd)
Ruby Duffer W (abd)
WHs
WHs
WHWH
WH
WHWH
WH
P
PP
P
P
P
P
P
P
P
P
P
Ruby W (abd)
Narracoota W (abd)
WH S
P
B W
D T
(abd) (PD)
Cheroona W(abd)
Ti Tree B
56ocircocircocircocircYacute E 58 62 64 66 68 72
icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
56ocircocircocircocircYacute E 58 60 62 64 66 68 70 72 icirc40ocircocircocircocircYacute E
icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
74ocircocircocircocircYacute E7060
0frac34 0frac34 30Agrave
1frac34
Chalba Fault
CoolinbarFault
Fortnum Fault
BillaraFault
Wilthorpe
Fault
KindersFault
GoodinFault
Goodi
n
Fault
Murchison
Fault
Goodin
Fault
Padbury
Syncline
Millidie
Syncline
Peak HillAnticline
Robinso
n
Synclin
e
HorseshoeAnticline
3
33
3 3
3
3
3
3
30
85
8035
54
2
2
2
2
2
2
2
2
2
2
2
2
2
2
40
2
2
2
2
40
36
30
40
45
3
36
7081
62
51
6270
86
80
60
87
85
85 72
63
70
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55
3
4
3
3
3
3
3
8583
68
55
74
85
75
71
61
706260
3
3
3
3
3
3
87
66
70
60
7075
88
8081
4
4
4
4 44 4
4
4
3
3
81 83
80
7872
87
55
33
3
4
4
71
78
73
47
25
85
75
70
2
2
48
62
45
80 63
4785
75
60
60
70
85
15
72
80
60
32
85
60
6030
3565
4
4
4
2 2
4
4
3
3
3
4
3
3
2
42
2
4
4
86
86
73 75
8570 70
85
75
4
5264
58
45
60
80
70
60
78
65
46
80
5051
7050
60
38
80
84
50
70
60
74
56
48
42
70
8278
5058
35
70
80
55
46
58
70
77
85
53
80 52
2
2
2 2
1
1
11
1
2
2
2
2
2
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
65
50
55 85
80
60
30
70
40
5545 82
80
80
60
78
70
42
60
70
88
60
70
70
80
70
70
75
48
42
45
80
40
30
85
69
74
68
68
52
68
40
50
2
11
65
65
118958
118957
28
70
62
6884
10
72
75
4740
8878
60
74
80
1
2
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2
2
4
56
80
48
78
85
56
60
6470
80
60
8572
80
65
88
76 85
70
2
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3460
64
75
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7830
85
8488
75
50
4
60
66
75
48
64
66
10
45
35
80
48
75
58
66
60
72
70
35
80
36
2
88
70
78
25
70
58
45
86
2
80
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igraveYm
igraveYc
igraveYjigraveYm
igraveAk
igraveE
igraveE
igraveYjf
igraveYjf
igraveAk
igraveAk
igravePmi
igravePmc
igravePw
igraved
igraved
igravedigraveAhi
igraveAhi
igraved
igraveAn
igraved
igravePla
igravePwh
igraveAnd
igraved
igravePr
igravePr
igraveYj
igraved
igraveAnd
igraveAnd
igraveAr
igraved
igravePl
igravePl
igravePl
igravePla
igravePla
igravePla
igravePla
igravePla
igravePla igravePl
igraveArc
igraveArc
igraveArc
igravePla
igraveAk
ntildegde
ntildegMl
ntildegMl
igraveYjf
igraveYj
ntildegMlintildegMli
ntildegMla
ntildegMla
ntildeg
ntildeg
ntildeg
ntildegn
ntildeng
ntildeng
E
E
E
E
E
E
E 118961
118956
142851
88YacuteEcirc168
igraveAnd
TrevsYacuteYacuteYacuteStarlight
Yarlarweelor
Horseshoe
NathanDeep
Mt Seabrook
Labouchere
Wilthorpe
Wilgeena
Wembley
Livingstone
Harmony
Jubilee
Peak HillMt Pleasant
St Crispin
Durack
Heines Find
Mikhaburra
Cashman
Horseshoe Lights
Horseshoe
Yarlarweelor
Mn
T
MnMn
CuAu
Cu
Au
Mn
T
CuAu
HOLDENS
BAXTER
RAVELSTONE
PEAK HILL
HORSESHOE
HOLDENS
Ruby Well
Fortnum
Fortnum
M U R C H I S O N M I N E R A L F I E L D
M E E K A T H A R R A D I S T R I C T
P E A K H I L L M I N E R A L F I E L D
Goodin Fault Murchison Fault
Goodin Fault Murchison Fault
thrust
latera
l ramp
Billara Fault Kinders Fault
NARRYER
TERRANE
YILGARN
CRATON
Goodin F
ault
GOODIN
INLIER
Jenkin
Fault
Fault
Goodin
MARYMIA
INLIER
thrust ramp
Robinson Syncline
Peak Hill Anticline
Peak Hill Anticline
Horseshoe Anticline Millidie Syncline
Yarlarweelor gneiss belt
Marymia Inlier
40
MOUNT LEAKE FORMATION quartz arenite
DESPAIR GRANITE foliated to locally massive coarse-grained biotite granite late Archaean
30 km
Bangemall Group
Earaheedy Group
Padbury Group
Bryah Group
Mooloogool SubgroupDoolgunna_Thaduna Formations
Windplain Subgroup
Geological boundary
Fault
Finlayson Member quartz arenite
117frac34Yacute30Agrave
25frac34Yacute00Agrave
45Agrave118frac34Yacute00Agrave 15Agrave 30Agrave 45Agrave 119frac34Yacute00Agrave 15Agrave 119frac34Yacute30Agrave
25frac34Yacute00Agrave
15Agrave
30Agrave
45Agrave
26frac34Yacute00Agrave
26frac34Yacute10Agrave
119frac34Yacute30Agrave15Agrave119frac34Yacute00Agrave45Agrave15Agrave 30Agrave
118frac34Yacute00Agrave45Agrave117frac34Yacute30Agrave
26frac34Yacute10Agrave
26frac34Yacute00Agrave
45Agrave
30Agrave
15Agrave
Proterozoic granite
Q TR S
SEA LEVEL
5 km
11 km
F G
SEA LEVEL
5 km
11 km
L M O
SEA LEVEL
5 km
11 km
N
J K
SEA LEVEL
5 km
10 km
10 km
SEA LEVEL
5 km
H I
Archaean granitoid rock and greenstone
YerridaGroup
Maraloou_Killara Formations
SEA LEVEL
5 km
10 km
C D E
SEA LEVEL
5 km
10 km
A B
MILLIDIE CREEK FORMATION sandstone and shale minor granular iron-formation
ROBINSON RANGE FORMATION ferruginous shale and siltstone minor banded iron-formation
Beatty Park Member chloritic siltstone sandstone and breccia numerous mafic volcanic fragments
Heines Member quartz wacke siltstone and shale with minor polymictic conglomerate
LABOUCHERE FORMATION quartz wacke and siltstone local quartz pebble conglomerate layers turbiditic
KARALUNDI FORMATION sandstone with minor shale and conglomerate
JOHNSON CAIRN FORMATION siltstone and shale minor sandstone
JUDERINA FORMATION quartz wacke siltstone quartz arenite and quartz pebble conglomerate
PEAK HILL SCHIST quartz muscovite schist mylonitic schist and phyllonite
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS REPORT 59 PLATE 1
2
Trillbar Complexwith local magmatic layering well-preserved
interleaved foliated and metamorphosed basalt gabbro microgabbro pyroxenite and serpentinized peridotite
HORSESHOE FORMATION ferruginous chloritic shale and quartzEcircfeldspar wacke partly manganiferous andcalcareous minor iron-formation and chert
BANGEMALL
EARAHEEDY
PADBURYBASIN
BASINBRYAH
YERRIDABASIN
WILTHORPE FORMATION quartz pebble to boulder conglomerate predominant vein quartz clasts and some chert quartz wackeand granitoid rock clasts quartz wacke and finely bedded siltstone locally chloritic graded beds
1 2 3 4
C
58
78
75
20
15
SHEET INDEX
intruded by granite during the Capricorn Orogeny
High-grade gneissic granite and granite foliated derived predominantly from biotite monzogranite with numerouslenses of supracrustal rocks early middle and late Archaean components overprinted by structures and
NARRACOOTA FORMATION metabasalt and maficEcircultramafic schist locally pillowed with interflow sedimentary layers
Capr
icorn
Oro
geny
Mar
ymia
Inlie
r_re
work
ed d
uring
the
met
amor
phism
_Ca
prico
rn O
roge
nyup
per g
reen
schist to
lowe
r am
phib
olite
facie
s
gree
nsto
ne b
eltM
ount
Mai
tland
2672YacuteucircYacute3
lt1996YacuteucircYacute35
High-grade granitic gneiss derived predominantly from biotite monzogranite with numerous lenses ofsupracrustal rocks early middle and late Archaean components includes Palaeoproterozoicgranite sheets and dykes extensively deformed during Capricorn Orogeny
SCHEMATIC TECTONIC RELATIONSHIPS
BANGEMALL BASIN
1600 Ma and youngerc
EARAHEEDY BASIN
2000 Ma and youngercBRYAH BASIN
2000 Mac
YERRIDA BASIN
2200 Ma and youngerc
YILGARN CRATON
2600 Ma and olderc
PADBURY BASINyounger than 2000 Ma
BASIN
BASIN
igraveAn
igraveAndigraveAnhigraveAnuigraveAnxigraveAncigraveAnt
igraveAnf
ntildeg
ntildegn
ntildeng
igraveM
igraveE
igraved
igraveg
igraveP
igravePm
igravePmi
igravePmc
igravePr
igravePrg
igravePri
igravePw
igravePwb
igravePwh
igravePl
igravePli
igravePla
igraveAh
igraveAhi
igraveAr
igraveArc
igraveAnigraveAnd igraveAnh igraveAnu igraveAnx igraveAnc igraveAnt
igraveAk
igraveYm
igraveYc
igraveYj
igraveYjf
ntildegMl
ntilderMM
ntildegde
igraveAnf
igravePi
ethp
ethpm
ntildegMli
ntildegMla
igraveYjf
igraveYjf
igraveYj
igraved
igraved
igraveYm
igravePmigravePrg
igravePrigravePri
igravePwh
igraveAn
igraveAk ethp
igraveAnh igraveAnd
ntildegMl
igraveAnh
igraveAnxigraveYcigraveYj
igraveYjf
igraveAn
ethp
igraveAr igraveAr
igravePwh
ethpm igraveAn
igraveAn
igraveM
igravePrigravePri
igravePriigravePr
igraveAr
igraveAn
ethp
ethpm
igravePriigravePr igravePri
igravePw
igravePligravePla
igraveAh
igraveAn
igraveArc igraveAn
igraveArcigraveAnf
igraveAnd
igraveM
igraved
igraveAhiigravePm
igravePl
igraveAn
igraveAr
igravePr
igravePriigravePl
igravePla igraveAhigraveAnc
igraveAn igraveAhigraveM
ntildegMl
igraveArc
ntildegMl
ntildegMl
ntildegMl
igraveAnd
igravePrigravePri
igravePwb
igravePl
igraveAn
igraveAhigravePwb
igravePr
igravePri
igravePmi
igraveAr
igraved
igraveAn
igravePm
igravePwb
igravePr
igravePr
igravePri
igravePwigraveAnu
igravePm
igravePmc
igraveAr
igraveAk
igravePw
igraveM
ntildegMla
ntildegntildeg
ntildeg
ntildegntildeng
igraveM igraveM
igravePligraveAhi
igraveAhigraveAh
igraveAn
igraveAnigraveAr
ntildegMl
ethp
ntildeng
igraved igraved
igraved
WA
NT
SA
NSW
Vic
Qld
Tas
ACT
GEOLO
G IC A L SUR VEY
WE
ST
E R N A U S T R AL
IA
GEOLOGICAL SURVEY OF
WESTERN AUSTRALIA
DAVID BLIGHT DIRECTOR
DEPARTMENT OF MINERALS
AND ENERGY
L C RANFORD DIRECTOR GENERAL
GOVERNMENT OF WESTERN AUSTRALIA
HON NORMAN MOORE MLC
MINISTER FOR MINES
Bangemall Group undivided
Mafic dyke interpreted from aeromagnetic data + positive anomaly - negative anomaly
Granite includes muscovite-bearing leucogranite and pegmatite
Padbury Group undivided metamorphosed and variably foliated metasedimentary rocks
Iron-formation and chert
Banded iron-formation minor ferruginous sandstone and shale
Bedded dolomite and dolomitic siltstone
Granular iron-formation
Banded iron-formation
Banded iron-formation and ferruginous chert
Quartz arenite minor interleaved quartz wacke and siltstone
Iron-formation and quartzEcircmagnetite(Ecircstilpnomelane) schist garnetiferous white chert in lenses
lithic wacke and siltstone turbiditic
Chert
Felsic schist derived from felsic volcanic and volcaniclastic rockDolerite in sills and dykesBasaltic hyaloclastiteMetaperidotite and picrite ultramafic schistBasaltic vent brecciaJasperoidal chert
Quartz mylonite
Foliated to mylonitic and massive granitoid rock
Amphibolite
Banded iron-formation
Granite with minor greenstone locally overprinted by structures formed during Capricorn Orogeny
Basalt ultramafic rock dolerite felsic schist banded iron-formation and chert
RAVELSTONE FORMATION
MES
OPRO
TERO
ZOIC
PALA
EOPR
OTER
OZOI
CAR
CHAE
AN
Bang
emal
lGr
oup
Eara
heed
yGr
oup
Padb
ury G
roup
Brya
h Gr
oup
Yerri
da G
roup
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Yarla
rwee
lor g
neiss
belt
Narry
er T
erra
ne
lowe
r gre
ensc
hist to
upp
er a
mph
ibol
ite fa
cies
met
amor
phism
_Ca
prico
rn O
roge
ny
Mur
chiso
n Te
rrane
YILG
ARN
CRAT
ONYE
RRID
A BA
SIN
BRYA
H BA
SIN
preh
niteEcirc
pum
pelly
ite to
mid
-gre
ensc
hist fa
cies
met
amor
phism
_Ca
prico
rn O
roge
ny
PADB
URY
BASI
N
Undivided MARALOOU DOOLGUNNA THADUNA and KILLARA FORMATIONS
Contact Bryah Group_Padbury Group
Structural symbols are numbered according totheir age of formation where known
Middle Proterozoic
Early Proterozoic
interpreted movement
Fold showing direction of plunge
Small-scale fold axial surface showing strike and dip
Bedding showing strike and dip
Foliation showing strike and dip
Lineation showing direction of plunge
Single zircon UEcircPb SHRIMP geochronology data
Nutman A P Bennett V C Kinny P D and Price R 1993 Large scale crustalstructure of the northwestern Yilgarn Craton Western Australia evidence fromNd isotopic data and zircon geochronology Tectonics v12 p 971-981
Nelson D R 1997 Geological Survey of Western Australia Record 19972
Nelson D R in prep Geological Survey of Western Australia Record 19982Mineral occurrence
Edited by D Ferdinando and G Loan
Cartography by P Taylor and B Williams
Topography from the Department of Land Administration Sheets SG 50-7 -8 -11 -12with modifications from geological field survey
Published by the Geological Survey of Western Australia Copies available fromthe Information Centre Department of Minerals and Energy 100 Plain StreetEast Perth WA 6004 Phone (08) 9222 3459 Fax (08) 9222 3444
This map is also available in digital form
Printed by the Sands Print Group Western Australia
The recommended reference for this map isSWAGER C P OCCHIPINTI S A and PIRAJNO F 1998 Interpreted Geology of thePalaeoproterozoic Bryah and Padbury Basins Western Australia Geological Survey Report 59 Plate 1
Unconformity (section only)
unconformity with local major onlap reworked as a fault
Geological boundary
Edmund fold belt unspecified
Capricorn Orogeny unspecified
Capricorn Orogeny DOtilde DUcirc Dccedil Deacute
Fault
Reactivated normal fault
lateral (plan view) dip slip (section)
away from observer
Strongly foliated rock
anticline
syncline
overturned anticline
overturned syncline
towards observer
Minor fold showing direction of plunge
inclined
vertical
inclined
vertical
overturned
bedding or layering trend
inclined
vertical
trend (section only)
GSWA identification number
mineral lineation
intersection lineation
Nutman et al identification number
interpreted age of intrusion in Ma with reference number
youngest detrital zircon
Highway with national route marker
Formed road
Track
Landing ground
Townsite population less than 1000
Mineral field boundary
Homestead
Locality
Building yard
Microwave repeater station
Horizontal control major
Watercourse ephemeral pool
Waterhole spring
Bore well windpump
Dam tank
Abandoned position doubtful
Mining centre
Mining locality
Mine (gold unless otherwise indicated)
Major opencut
Opencut
Alluvial workings
Prospect
Copper
Gold
Manganese
Talc
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
0 5 10 15 20 255000
Metres Kilometres
VERTICAL DATUM AUSTRALIAN HEIGHT DATUM
SCALE 1Yacute250Yacute000
Grid lines indicate 20Yacute000 metre interval of the Map Grid Australia Zone 50
HORIZONTAL DATUM GEOCENTRIC DATUM OF AUSTRALIA 1994UNIVERSAL TRANSVERSE MERCATOR PROJECTION
The Map Grid Australia (MGA) is based on the Geocentric Datum of Australia 1994 (GDA94)
GEOCENTRIC DATUM OF AUSTRALIA
GDA94 positions are compatible within one metre of the datum WGS84 positions
Reference points to align maps based on the previous datum AGD84 have been placed near the map corners
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS
2344
2345
2346
2347
2444
2445
2446
2447
2544
2545
2546
2547
2644
2645
2646
2647
2744
2745
2746
2747
2844
2845
2846
2847
KALLI
MILEURA
GOULD
ERRABIDDY
MADOONGA
KOONMARRA
MOORARIE
MARQUIS
MEEKATHARRA
TIERACO
PADBURY
MILGUN
GABANINTHA
GLENGARRY
BRYAH
JAMINDI
YAGANOO
MOOLOOGOOL
DOOLGUNNA
MEREWETHER
THADUNA
MARYMIA
MOUNT BARTLE
THREE RIVERS
118958
88YacuteEcirc168
BELELE GLENGARRY
ROBINSON RANGE PEAK HILL
SG 50-7 SG 50-8
SG 50-11 SG 50-12
1100Yacute000 maps shown in black
Compiled by C P Swager S A Occhipinti and F Pirajno 1997
N
P
Geology from 1100Yacute000 GSWA maps (see sheet index)
See current GSWA map catalogue for the full range of published products
and by S A Occhipinti C P Swager 1995 1997 and J S Myers 1995
Published 1100Yacute000 maps used in compilation
1250Yacute000 maps shown in brown
+ means declination is east and correction must be
subtracted from compass bearing to give true bearing
Annual change is 1Agrave easterly
The lines indicate magnetic declination 1995
added to compass bearing to give true bearing
- means declination is west and correction must be
SEA LEVEL
5 km
11 km
brvbar Western Australia 1998
117frac34 30Agrave25frac3400Agrave
118frac3400Agrave 119frac3400Agrave 120frac3400Agrave
26frac3400Agrave
INTERPRETED GEOLOGY OF THE PALAEOPROTEROZOIC
AREA OF THIS MAP
GSWA
REPORT 60
PLATE 1
E
Version 11 _ May 2004
Q
R
S
T
F
G
L
M
O
P
N
J
K
C
D
E
A
B
H
I
1 2 3
1
2
3
cc 3300
1
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
2672YacuteucircYacute32
1808YacuteucircYacute6
3
cc 3300
1
3300
1
lt1996YacuteucircYacute352
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
lt1785YacuteucircYacute112
2672YacuteucircYacute32
2672YacuteucircYacute32
- Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
-
- Contents
- Abstract
- Introduction
- Regional tectonic setting
- Geology stratigraphy and geochronology
-
- Peak Hill Schist and Marymia Inlier
- Bryah Group
-
- Karalundi Formation
- Narracoota Formation
-
- Peridotitic and high-Mg basalt association
- Intrusive rocks and layered intrusions
- Mafic and ultramafic schist
- Metabasaltic hyaloclastite
- Felsic schist
- Volcaniclastic rocks
- Carbonated and silicified metavolcanic rocks
- Jasperoidal chert
- Geochemistry of the Narracoota Formation
-
- Ravelstone Formation
- Horseshoe Formation
-
- Padbury Group
-
- Labouchere Formation
- Wilthorpe Formation
-
- Beatty Park and Heines Members
-
- Robinson Range Formation
- Millidie Creek Formation
- Unassigned units of the Padbury Group
-
- Structure
-
- D1 structures
- D2 structures
- D3 structures and their relationship to D2 structures
- D4 structures
-
- Metamorphism
- Structural synthesis
- Mineralization
-
- Gold deposits
-
- Peak Hill Jubilee and Mount Pleasant deposits
- Harmony deposit
- Labouchere Nathans and Fortnum deposits
- Wembley deposit
- Wilgeena deposit
- Durack St Crispin and Heines Find prospects
- Ruby Well group
- Mikhaburra deposit
- Wilthorpe deposit
- Cashman deposit
-
- Volcanogenic copperndashgold deposits
- Supergene manganese deposits
- Iron ore
- Talc
- Discussion
-
- Tectonic model and conclusions
- Acknowledgements
- References
- Appendix Gazetteer of localities
- Plate 1 Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
- Figures
-
- Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
- Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins
- Figure 3 Rotated orthoclase porphyroblast Peak Hill Schist
- Figure 4 Partially recrystallized mylonite Peak Hill Schist
- Figure 5 Peak Hill Schist mylonite from the Hangingwall Sequence
- Figure 6 Outcrop of quartz mylonite Peak Hill Schist
- Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric
- Figure 8 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt)
- Figure 9 Basaltic hyaloclastite Narracoota Formation
- Figure 10 Mafic volcaniclastic rock Narracoota Formation
- Figure 11 Volcanic breccia intersected in diamond drillhole BD1
- Figure 12 Total alkali versus silica diagram for rocks the Narracoota Formation
- Figure 13 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the Narracoota Formation
- Figure 14 Geochemical characteristics of the Narracoota Formation rocks
- Figure 15 Geochemical discriminant plots for Narracoota Formation
- Figure 16 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation
- Figure 17 Schematic stratigraphy of the Horseshoe Formation
- Figure 18 Major regional structures in the Bryah and Padbury Groups
- Figure 19 Simplified geological map of the Bryah and Padbury Groups
- Figure 20 Selected hypothetical cross sections through the Bryah and Padbury Groups
- Figure 21 Model of the structural development of the BryahndashPadbury Group succession
- Figure 22 New model of the structural development of the BryahndashPadbury Group succession
- Figure 23 New model for the structural development of the BryahndashPadbury Group succession and the Peak Hill Schist
- Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins
- Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins
- Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH 1100 000 map sheet
- Figure 27 Albite porphyroblasts in mylonitic schist at Mount Pleasant
- Figure 28 The Mine Sequence schist
- Figure 29 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit
- Figure 30 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and Marker quartzite unit
- Figure 31 Diagrammatic cross section of the Harmony ore zones
- Figure 32 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and deformed Despair Granite
- Figure 33 Sketch illustrating a conceptual model for the origin of precious and base metal deposits in the BryahndashPadbury and Yerrida Basins
- Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins within the context of the Capricorn Orogen
-
- Tables
-
- Table 1 Stratigraphy of the Bryah and Padbury Groups
- Table 2 Representative chemical analyses of the Narracoota Formation
- Table 3 Magnesium numbers for the Narracoota and Killara Formations
- Table 4 Selected geochemical parameters for the Narracoota Formation
- Table 5 Sequence of deformation events in the Bryah and Padbury Basins
- Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group and deformation fabrics
- Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
- Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
- Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
-
GEOCHEMICAL ANALYSES OF ROCKS FROM THE NARRACOOTA FORMATION For details of analytical techniques see in text of Report 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
Sample | Easting | Northing | SiO2 | TiO2 | Al2O3 | Fe2O3 | FeO | MnO | MgO | CaO | Na2O | K2O | P2O5 | LOI | H2O- | H2O+ | TOTAL | CO2 | Ag | As | Au | Ba | Bi | Cd | Ce | Cr | Co | Cu | Ga | Ge | La | Li | Mo | Mn | Nb | Ni | Pb | Pd | Pt | Rb | Sb | Sc | Sn | Sr | Ta | Te | Th | Ti | U | V | Y | W | Zn | Zr | Hf | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm | Yb | Lu | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86342 | 746314 | 7198282 | 5151 | 032 | 1523 | 928 | 018 | 1049 | 1007 | 269 | 019 | 003 | 673 | 166 | 1 | 95 | 12 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86383 | 670171 | 7163822 | 5353 | 091 | 1468 | 115 | 019 | 744 | 863 | 299 | 005 | 008 | 253 | 100 | 1 | 85 | 21 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86384 | 670171 | 7163822 | 5048 | 062 | 1444 | 991 | 016 | 1135 | 933 | 362 | 004 | 005 | 640 | 209 | 1 | 157 | 16 | 33 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86397 | 799422 | 7201118 | 5529 | 026 | 1502 | 817 | 017 | 1136 | 416 | 549 | 005 | 002 | 1174 | 244 | 0 | 44 | 15 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104248 | 722651 | 7168587 | 4925 | 022 | 1137 | 963 | 017 | 1818 | 948 | 159 | 009 | 002 | 1 | 80 | 9 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104249 | 722651 | 7168587 | 4911 | 026 | 1065 | 973 | 017 | 2016 | 855 | 126 | 009 | 003 | 1 | 34 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104254 | 715830 | 7171470 | 4948 | 023 | 1121 | 95 | 016 | 2035 | 706 | 194 | 005 | 002 | 1877 | 647 | 1 | 49 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104255 | 715830 | 7171470 | 52 | 033 | 143 | 847 | 017 | 1071 | 1087 | 31 | 002 | 003 | 664 | 209 | 0 | 133 | 13 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256 | 715830 | 7171470 | 5244 | 067 | 1455 | 1007 | 019 | 834 | 983 | 376 | 007 | 007 | 0 | 140 | 17 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104257 | 713820 | 7171502 | 5144 | 092 | 1453 | 1078 | 02 | 689 | 1244 | 248 | 023 | 009 | 265 | 79 | 3 | 195 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104264 | 685287 | 7155494 | 5303 | 062 | 1391 | 94 | 017 | 768 | 1239 | 265 | 01 | 006 | 720 | 222 | 1 | 90 | 15 | 32 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104265 | 685287 | 7155494 | 5332 | 025 | 1592 | 97 | 017 | 658 | 1215 | 184 | 003 | 004 | 353 | 67 | 1 | 30 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104288 | 661877 | 7126843 | 5979 | 024 | 1346 | 798 | 016 | 522 | 1265 | 042 | 004 | 004 | 283 | 46 | 0 | 17 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104289 | 656054 | 7130760 | 5446 | 014 | 1559 | 955 | 017 | 826 | 957 | 204 | 019 | 003 | 358 | 116 | 4 | 43 | 8 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104292 | 657132 | 7123177 | 5103 | 09 | 1369 | 971 | 017 | 827 | 1334 | 272 | 009 | 008 | 0 | 165 | 18 | 51 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104294 | 664424 | 7119210 | 5108 | 095 | 1449 | 1021 | 018 | 879 | 1094 | 283 | 046 | 008 | 523 | 141 | 5 | 123 | 19 | 52 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104295 | 664424 | 7119210 | 5228 | 096 | 1446 | 1022 | 018 | 946 | 856 | 364 | 016 | 009 | 465 | 132 | 2 | 79 | 19 | 54 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104298 | 669014 | 7106533 | 5233 | 087 | 1367 | 939 | 017 | 778 | 1189 | 373 | 01 | 008 | 514 | 116 | 1 | 116 | 17 | 49 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104299 | 669014 | 7106533 | 5166 | 093 | 1404 | 982 | 018 | 823 | 1183 | 305 | 017 | 009 | 491 | 117 | 3 | 124 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104300 | 669014 | 7106533 | 477 | 05 | 173 | 984 | 019 | 747 | 1484 | 197 | 016 | 004 | 3 | 142 | 12 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104386 | 676392 | 7146500 | 5373 | 037 | 1501 | 846 | 016 | 864 | 977 | 373 | 009 | 004 | 557 | 152 | 0 | 106 | 18 | 18 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104391 | 687552 | 7144198 | 5002 | 023 | 845 | 934 | 016 | 2281 | 88 | 014 | 002 | 002 | 0 | 15 | 11 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104392 | 687552 | 7144198 | 5391 | 027 | 92 | 998 | 014 | 2087 | 515 | 017 | 027 | 003 | 2508 | 1103 | 12 | 16 | 22 | 10 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393 | 687539 | 7143275 | 508 | 023 | 965 | 1025 | 01 | 289 | 004 | 0 | 001 | 001 | 0 | 3 | 5 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104394 | 687539 | 7143275 | 5594 | 05 | 1494 | 867 | 019 | 73 | 697 | 537 | 006 | 006 | 363 | 88 | 0 | 90 | 19 | 24 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104397 | 670399 | 7142584 | 4687 | 019 | 1023 | 1015 | 017 | 2496 | 726 | 015 | 001 | 001 | 2786 | 971 | 0 | 7 | 8 | 4 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104398 | 669575 | 7143518 | 5329 | 035 | 1453 | 813 | 014 | 828 | 1207 | 315 | 002 | 004 | 574 | 124 | 0 | 78 | 13 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104399 | 670423 | 7144430 | 5183 | 036 | 1491 | 866 | 016 | 932 | 1147 | 323 | 002 | 003 | 682 | 173 | 0 | 42 | 14 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104400 | 670023 | 7145280 | 4958 | 037 | 1577 | 987 | 019 | 1044 | 1082 | 291 | 002 | 003 | 510 | 124 | 0 | 68 | 17 | 15 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109487 | 638809 | 7157725 | 5719 | 043 | 1423 | 73 | 013 | 868 | 626 | 569 | 004 | 004 | 442 | 116 | 0 | 18 | 11 | 19 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109492 | 663796 | 7149130 | 5231 | 011 | 617 | 72 | 015 | 24 | 1002 | 001 | 001 | 001 | 0 | 7 | 5 | 1 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109493 | 663796 | 7149130 | 5246 | 047 | 1508 | 881 | 019 | 766 | 1218 | 247 | 064 | 005 | 478 | 90 | 6 | 72 | 15 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109504 | 670124 | 7121353 | 5396 | 048 | 149 | 859 | 015 | 716 | 1237 | 231 | 003 | 005 | 445 | 96 | 0 | 61 | 17 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109513 | 732634 | 7164722 | 5396 | 197 | 1434 | 953 | 02 | 638 | 686 | 592 | 064 | 019 | 16 | 117 | 24 | 97 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601 | 668775 | 7146298 | 5332 | 179 | 1568 | 102 | 025 | 644 | 561 | 601 | 053 | 017 | 10 | 105 | 21 | 90 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112603 | 672130 | 7147178 | 108 | 034 | 2 | 1698 | lt10 | 462 | lt4 | lt5 | lt6 | 559 | 54 | 12 | lt3 | 6 | lt2 | lt7 | 115 | lt4 | 87 | 4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 167 | 19 | 92 | 203 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604 | 672238 | 7155486 | 202 | lt001 | 3 | lt4 | 40 | 34 | 8 | lt5 | 73 | 3639 | 69 | 16 | lt3 | 38 | lt2 | lt7 | 143 | 20 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | lt2 | lt2 | 453 | 29 | 20 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112620 | 626709 | 7204920 | 33 | 001 | 2 | lt4 | 220 | 35 | lt4 | lt5 | 19 | 1377 | 78 | 22 | lt3 | 25 | lt2 | 9 | 127 | 26 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | 10 | lt2 | 358 | 22 | 13 | 182 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112621 | 626709 | 7204920 | 116 | 011 | 1 | 144 | lt10 | lt11 | lt4 | lt5 | lt6 | 2354 | 82 | 8 | lt3 | lt5 | lt2 | lt7 | 1589 | lt4 | lt2 | 9 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 131 | 6 | 72 | 20 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112624 | 661284 | 7183319 | 507 | 074 | 139 | 274 | 769 | 018 | 791 | 104 | 244 | 025 | 007 | 358 | 1007 | 1 | lt4 | lt10 | 54 | lt4 | lt5 | lt6 | 186 | 92 | 13 | lt3 | lt5 | lt2 | lt7 | 96 | lt4 | 6 | lt4 | lt4 | 97 | lt5 | lt6 | lt2 | lt2 | 264 | 18 | 77 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112625 | 661284 | 7183319 | 498 | 074 | 143 | 244 | 747 | 016 | 831 | 116 | 237 | 03 | 007 | 324 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 354 | 90 | 12 | lt3 | lt5 | lt2 | lt7 | 111 | lt4 | 4 | lt4 | lt4 | 85 | lt5 | lt6 | lt2 | lt2 | 241 | 15 | 79 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112628 | 661284 | 7183319 | 49 | 08 | 138 | 357 | 726 | 018 | 738 | 14 | 143 | 008 | 007 | 277 | 1006 | 2 | lt4 | lt10 | 147 | lt4 | lt5 | 6 | 167 | 91 | 14 | lt3 | lt5 | lt2 | lt7 | 101 | lt4 | lt2 | lt4 | lt4 | 310 | lt5 | lt6 | lt2 | lt2 | 265 | 19 | 77 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112629 | 661284 | 7183319 | 642 | 049 | 103 | 271 | 402 | 012 | 438 | 113 | 051 | 013 | 005 | 18 | 1001 | lt1 | lt4 | lt10 | 109 | lt4 | lt5 | lt6 | 113 | 58 | 12 | lt3 | lt5 | lt2 | lt7 | 60 | lt4 | 2 | lt4 | lt4 | 86 | lt5 | lt6 | lt2 | lt2 | 166 | 11 | 50 | 39 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112640 | 675227 | 7128672 | 49 | 052 | 147 | 272 | 517 | 014 | 915 | 148 | 142 | 011 | 005 | 221 | 1002 | 1 | lt4 | lt10 | 90 | lt4 | lt5 | lt6 | 277 | 38 | 13 | lt3 | lt5 | lt2 | lt7 | 160 | lt4 | 2 | 5 | lt4 | 184 | lt5 | lt6 | lt2 | lt2 | 212 | 11 | 54 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112641 | 675215 | 7127749 | 508 | 079 | 142 | 308 | 703 | 017 | 744 | 118 | 207 | 012 | 008 | 299 | 1008 | 1 | lt4 | 90 | 26 | lt4 | lt5 | lt6 | 266 | 102 | 14 | lt3 | lt5 | lt2 | lt7 | 120 | lt4 | lt2 | lt4 | lt4 | 148 | lt5 | lt6 | lt2 | lt2 | 258 | 16 | 80 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643 | 675190 | 7125902 | 275 | 205 | lt1 | 10 | 40 | 767 | lt4 | lt5 | 175 | 994 | 257 | 12 | 3 | 12 | 2 | lt7 | lt3 | 34 | lt2 | lt4 | lt4 | 43 | lt5 | lt6 | lt2 | lt2 | 272 | 13 | 96 | 25 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112645 | 663956 | 7162053 | 23 | 059 | lt1 | 7 | lt10 | 227 | lt4 | lt5 | 34 | 2117 | 390 | 3 | 12 | lt2 | 8 | lt3 | 12 | lt2 | lt4 | 8 | 10 | lt5 | lt6 | 6 | lt2 | 467 | 14 | 81 | 132 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112646 | 663956 | 7162053 | 507 | 076 | 139 | 224 | 796 | 018 | 771 | 991 | 258 | 063 | 007 | 375 | 1005 | 1 | lt4 | lt10 | 164 | lt4 | lt5 | 6 | 207 | 79 | 13 | lt3 | lt5 | lt2 | lt7 | 123 | lt4 | 16 | lt4 | lt4 | 338 | lt5 | lt6 | lt2 | lt2 | 245 | 15 | 77 | 55 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112647 | 663956 | 7162053 | 356 | 002 | 1 | 133 | 1170 | lt11 | lt4 | lt5 | 13 | 489 | 846 | 6 | 4 | 6 | lt2 | lt7 | 533 | 1491 | lt2 | 4 | lt4 | lt2 | lt5 | 8 | lt2 | lt2 | 104 | 12 | 180 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112650 | 663956 | 7162053 | 573 | 424 | 959 | 166 | 036 | lt005 | 12 | 226 | 012 | 028 | 005 | 75 | 999 | 1 | lt4 | lt10 | 423 | lt4 | lt5 | 152 | 481 | 119 | 20 | lt3 | 90 | lt2 | 27 | 171 | 10 | 12 | lt4 | lt4 | 61 | lt5 | lt6 | 6 | lt2 | 365 | 37 | 54 | 296 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112652 | 663956 | 7162053 | 526 | 088 | 133 | 253 | 762 | 022 | 745 | 741 | 31 | 081 | 008 | 474 | 1009 | 1 | lt4 | lt10 | 242 | lt4 | lt5 | lt6 | 149 | 158 | 12 | lt3 | lt5 | lt2 | lt7 | 99 | 6 | 17 | 5 | lt4 | 87 | lt5 | lt6 | 2 | lt2 | 260 | 22 | 88 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112672 | 734725 | 7164593 | 628 | 07 | 136 | 355 | 364 | 034 | 337 | 494 | 286 | 093 | 009 | 313 | 1001 | 1 | lt4 | 20 | 258 | lt4 | lt5 | 76 | 122 | 16 | 17 | lt3 | 34 | lt2 | 17 | 75 | 13 | 19 | lt4 | 4 | 164 | lt5 | lt6 | 22 | 2 | 99 | 26 | 73 | 216 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 69 | 108 | 111 | 258 | 508 | 009 | 415 | 016 | 312 | 036 | 007 | 361 | 1006 | 1 | lt4 | lt10 | 386 | lt4 | lt5 | 30 | 56 | lt4 | 14 | lt3 | 18 | lt2 | 17 | 24 | lt4 | 17 | lt4 | lt4 | 79 | lt5 | lt6 | 8 | lt2 | 239 | 19 | 79 | 119 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 633 | 136 | 113 | 297 | 736 | 012 | 617 | 025 | 21 | 012 | 018 | 499 | 1004 | 1 | lt4 | 20 | 460 | lt4 | lt5 | 18 | 19 | 56 | 14 | lt3 | 10 | lt2 | 17 | 32 | 12 | 4 | lt4 | lt4 | 30 | lt5 | lt6 | 9 | 3 | 312 | 32 | 109 | 153 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 631 | 137 | 115 | 248 | 803 | 009 | 662 | 024 | 211 | lt005 | 016 | 496 | 1008 | 1 | lt4 | 20 | 28 | lt4 | lt5 | 37 | 21 | 203 | 17 | lt3 | 17 | 3 | 19 | 30 | 6 | lt2 | lt4 | lt4 | 27 | lt5 | lt6 | 9 | 3 | 336 | 24 | 107 | 158 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 129 | 697 | lt1 | 4 | 1250 | 1768 | lt4 | lt5 | 69 | 597 | 472 | 11 | lt3 | 53 | lt2 | lt7 | 327 | 22 | 90 | lt4 | lt4 | 226 | lt5 | lt6 | 8 | 2 | 181 | 19 | 118 | 101 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112675 | 734644 | 7166319 | 569 | 025 | 767 | 183 | 429 | 013 | 153 | 768 | 303 | 007 | lt005 | 396 | 1013 | 1 | lt4 | lt10 | 55 | lt4 | lt5 | lt6 | 541 | 26 | 4 | lt3 | lt5 | lt2 | lt7 | 262 | lt4 | 2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 117 | 9 | 46 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112678 | 734655 | 7166965 | 715 | 009 | 411 | 133 | 335 | 006 | 112 | 341 | 016 | lt005 | lt005 | 442 | 999 | 1 | lt4 | lt10 | 32 | lt4 | lt5 | lt6 | 1537 | 11 | 3 | lt3 | lt5 | lt2 | lt7 | 659 | lt4 | lt2 | lt4 | lt4 | 4 | lt5 | lt6 | lt2 | lt2 | 69 | 5 | 33 | 8 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112679 | 735684 | 7171472 | 518 | 034 | 135 | 289 | 531 | 014 | 945 | 12 | 267 | lt005 | lt005 | 277 | 1011 | 1 | lt4 | lt10 | 51 | lt4 | lt5 | lt6 | 670 | 56 | 12 | lt3 | lt5 | lt2 | lt7 | 272 | lt4 | lt2 | lt4 | lt4 | 60 | lt5 | lt6 | lt2 | lt2 | 198 | 16 | 55 | 21 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112680 | 735675 | 7172519 | 515 | 037 | 148 | 282 | 565 | 015 | 864 | 991 | 357 | lt005 | lt005 | 314 | 1008 | 1 | lt4 | lt10 | 83 | lt4 | lt5 | lt6 | 470 | 88 | 12 | lt3 | lt5 | lt2 | lt7 | 192 | lt4 | lt2 | 5 | lt4 | 88 | lt5 | lt6 | lt2 | lt2 | 216 | 17 | 62 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116407 | 603693 | 7169737 | 279 | lt001 | 1 | 4 | lt10 | 126 | lt4 | lt5 | 12 | 140 | 34 | lt3 | 3 | 7 | lt2 | 11 | 191 | 7 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | 3 | lt2 | 36 | 11 | 21 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116410 | 608442 | 7170499 | 211 | lt01 | lt1 | lt4 | lt10 | 726 | lt4 | lt5 | 6 | 696 | 17 | lt3 | lt3 | 5 | lt2 | lt7 | 82 | 4 | lt2 | lt4 | lt4 | 24 | lt5 | lt6 | 2 | lt2 | 40 | 5 | 10 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116415 | 611248 | 7168937 | 904 | lt005 | 265 | 094 | 095 | lt005 | 248 | 005 | 005 | lt005 | lt005 | 263 | 1005 | lt1 | 4 | lt10 | 947 | lt4 | lt5 | lt6 | 944 | 13 | lt3 | lt3 | 5 | lt2 | lt7 | 394 | lt4 | lt2 | lt4 | lt4 | 28 | lt5 | lt6 | lt2 | lt2 | 35 | 7 | 22 | lt5 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116428 | 614781 | 7170999 | 484 | 016 | 723 | 188 | 628 | 014 | 215 | 813 | 077 | lt005 | lt005 | 61 | 1011 | 1 | 4 | lt10 | 14 | lt4 | lt5 | lt6 | 2275 | 12 | 4 | lt3 | lt5 | lt2 | lt7 | 998 | lt4 | lt2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 126 | 8 | 60 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116429 | 614810 | 7171215 | 113 | 029 | 13 | 129 | 10 | 66 | lt4 | lt5 | lt6 | 2489 | 60 | 7 | lt5 | 15 | lt7 | 1344 | lt4 | 3 | 89 | 25 | lt4 | 75 | lt5 | 8 | lt2 | lt2 | 183 | 11 | 127 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116430 | 614807 | 7170845 | 217 | 002 | 10 | 12 | 2570 | 32 | lt4 | lt5 | 22 | 1581 | 463 | 4 | lt5 | lt6 | lt7 | 286 | 109 | lt2 | lt4 | 53 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 348 | 13 | 95 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116432 | 614348 | 7169311 | 101 | 009 | 6 | 5 | 80 | 44 | lt4 | lt5 | 15 | 1757 | 116 | lt3 | 7 | lt6 | 11 | 683 | lt4 | lt2 | lt4 | 37 | lt4 | 27 | lt5 | lt6 | lt2 | lt2 | 327 | 18 | 119 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116433 | 614232 | 7168820 | 211 | 029 | lt5 | 7 | 60 | 2075 | lt4 | lt5 | 35 | 254 | 126 | 5 | 26 | lt6 | 13 | 186 | 13 | 27 | 4 | 12 | lt4 | 56 | lt5 | lt6 | 4 | lt2 | 152 | 25 | 120 | 100 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116442 | 632664 | 7159418 | 414 | 022 | 21 | 7 | 10 | 710 | lt4 | lt5 | lt6 | 39 | 716 | lt3 | lt5 | lt6 | lt7 | 35 | 4 | lt2 | lt4 | 40 | lt4 | 28 | lt5 | 6 | lt2 | lt2 | 1073 | 16 | 137 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116443 | 634091 | 7159896 | 461 | 035 | 144 | 279 | 528 | 018 | 746 | 165 | 174 | 005 | lt005 | 545 | 1005 | 2 | lt4 | lt10 | 23 | lt4 | lt5 | lt6 | 443 | 62 | 15 | lt3 | lt5 | lt2 | lt7 | 164 | lt4 | lt2 | lt4 | lt4 | 63 | lt5 | lt6 | lt2 | lt2 | 233 | 17 | 56 | 22 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116444 | 633832 | 7161837 | 11 | 021 | lt1 | 13 | lt10 | 1185 | lt4 | lt5 | 42 | 173 | 66 | 13 | lt3 | 24 | lt2 | 14 | 67 | 10 | 23 | lt4 | lt4 | 28 | lt5 | lt6 | 4 | lt2 | 245 | 18 | 61 | 87 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116446 | 633910 | 7169621 | 458 | 014 | 847 | 147 | 74 | 016 | 22 | 765 | 02 | lt005 | lt005 | 71 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 2882 | 12 | 7 | lt3 | lt5 | lt2 | lt7 | 1306 | lt4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 142 | 8 | 67 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454 | 653363 | 7152948 | 174 | 01 | lt1 | 15 | 130 | 111 | lt4 | lt5 | lt6 | 389 | 106 | 21 | lt3 | lt5 | lt2 | lt7 | 204 | lt4 | 16 | lt4 | lt4 | 12 | lt5 | lt6 | lt2 | lt2 | 450 | 10 | 122 | 55 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477 | 645436 | 7177439 | 178 | 007 | lt1 | lt4 | 30 | 52 | lt4 | lt5 | lt6 | 689 | 88 | 21 | lt3 | 55 | lt2 | lt7 | 456 | 5 | 13 | lt4 | lt4 | 5 | lt5 | lt6 | lt2 | lt2 | 435 | 98 | 350 | 69 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485 | 655767 | 7129994 | 225 | 018 | lt1 | lt4 | lt10 | 78 | lt4 | lt5 | lt6 | 5612 | 129 | 8 | 3 | lt5 | 2 | 7 | 88 | 4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 119 | 7 | 39 | 38 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487 | 655561 | 7129043 | 168 | 013 | 1 | lt4 | lt10 | 191 | lt4 | lt5 | 11 | 4578 | 8 | 6 | lt3 | lt5 | lt2 | lt7 | 464 | 11 | 10 | lt4 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 87 | 7 | 70 | 35 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116488 | 655420 | 7128860 | 156 | 012 | lt1 | lt4 | 40 | 119 | lt4 | lt5 | 19 | 135 | 279 | 31 | lt3 | 7 | 2 | 7 | 313 | 21 | 23 | lt4 | lt4 | 15 | lt5 | lt6 | 3 | 3 | 585 | 10 | 97 | 149 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 128 | 007 | lt1 | lt4 | 170 | 169 | lt4 | lt5 | lt6 | 5588 | 63 | 4 | lt3 | lt5 | lt2 | lt7 | 687 | 14 | 12 | lt4 | lt4 | 6 | lt5 | 8 | 2 | 2 | 75 | 7 | 81 | 30 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 681 | 02 | 2 | 8 | lt10 | 34 | lt4 | lt5 | lt6 | 967 | 299 | 6 | lt3 | 9 | lt2 | lt7 | 348 | lt4 | lt2 | lt4 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 469 | 35 | 110 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116490 | 655978 | 7126699 | 491 | 078 | 147 | 315 | 779 | 017 | 816 | 994 | 274 | 065 | 008 | 371 | 1012 | 1 | lt4 | 20 | 228 | lt4 | lt5 | lt6 | 191 | 103 | 13 | lt3 | lt5 | lt2 | lt7 | 116 | lt4 | 9 | lt4 | lt4 | 300 | lt5 | lt6 | lt2 | lt2 | 267 | 17 | 87 | 56 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116491 | 656084 | 7126206 | 50 | 07 | 133 | 216 | 817 | 019 | 999 | 939 | 208 | 035 | 007 | 402 | 1007 | 1 | lt4 | 10 | 329 | lt4 | lt5 | lt6 | 471 | 104 | 12 | lt3 | lt5 | lt2 | lt7 | 249 | lt4 | 6 | 4 | lt4 | 157 | lt5 | lt6 | lt2 | lt2 | 241 | 16 | 82 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116492 | 656023 | 7125806 | 10 | 27 | 10 | 213 | lt4 | lt5 | lt6 | 17 | 170 | lt3 | lt5 | 7 | lt7 | 40 | lt4 | 49 | 4 | 49 | lt4 | 38 | 803 | lt6 | lt2 | lt2 | 434 | 28 | 45 | 58 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493 | 655992 | 7125530 | 13 | 25 | 60 | 150 | lt4 | lt5 | lt6 | 24 | 393 | lt3 | 6 | 10 | lt7 | 118 | 6 | 79 | lt4 | 55 | lt4 | 31 | 269 | lt6 | lt2 | lt2 | 464 | 37 | 239 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116498 | 709849 | 7162239 | 11 | 19 | 5000 | 269 | lt4 | lt5 | lt6 | 140 | 92 | lt3 | lt5 | 6 | lt7 | 83 | lt4 | 74 | lt4 | 47 | lt4 | 50 | 301 | lt6 | lt2 | lt2 | 316 | 25 | 123 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116500 | 709011 | 7162160 | 9 | 29 | 10 | 155 | lt4 | lt5 | lt6 | 27 | 121 | lt3 | lt5 | 6 | lt7 | 39 | 5 | 33 | lt4 | 66 | lt4 | 20 | 155 | lt6 | lt2 | lt2 | 535 | 34 | 28 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501 | 708508 | 7162137 | 11 | 6 | 20 | 23 | lt4 | lt5 | lt6 | 29 | 146 | lt3 | lt5 | 6 | lt7 | 102 | lt4 | 98 | lt4 | 57 | lt4 | 31 | 195 | 6 | lt2 | lt2 | 416 | 35 | 144 | 74 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116502 | 708368 | 7162139 | 756 | 052 | lt1 | 8 | lt10 | 368 | lt4 | lt5 | 11 | 25 | 398 | lt3 | lt3 | 12 | 2 | lt7 | 151 | 6 | lt2 | lt4 | 4 | 23 | lt5 | lt6 | lt2 | lt2 | 207 | 15 | 211 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116532 | 672308 | 7165117 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | 1009 | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | 117 | 13 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 5 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 275 | 21 | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120337 | 668950 | 7146475 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | nd | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | nd | 117 | 13 | lt5 | nd | lt2 | lt7 | 104 | lt4 | nd | nd | 5 | lt4 | nd | lt4 | 129 | lt2 | 44963 | lt2 | 275 | 21 | nd | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120340 | 669175 | 7145725 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | 1009 | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | 92 | 14 | lt3 | lt5 | lt2 | lt7 | 118 | lt4 | 4 | 4 | lt4 | 132 | lt5 | lt6 | 2 | lt2 | 259 | 18 | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369 | 665175 | 7156150 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | nd | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | nd | 92 | 14 | lt5 | nd | lt2 | lt7 | 118 | lt4 | nd | nd | 4 | 40 | nd | lt4 | 132 | 2 | 46162 | lt2 | 259 | 18 | nd | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373 | 675250 | 7167875 | 50 | 078 | 146 | 288 | 732 | 017 | 757 | 112 | 256 | lt005 | 008 | 328 | 328 | 1006 | nd | lt1 | lt4 | lt10 | 101 | lt4 | lt5 | lt6 | 224 | nd | 100 | 14 | lt3 | lt5 | nd | lt2 | lt7 | 125 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 120 | lt5 | lt6 | lt2 | 46761 | lt2 | 262 | 16 | nd | 84 | 57 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432 | 673950 | 7171700 | 52 | 077 | 146 | 219 | 763 | 015 | 753 | 793 | 429 | lt005 | 008 | 326 | 326 | 1006 | nd | 1 | 4 | lt10 | 126 | lt4 | lt5 | lt6 | 266 | nd | 109 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 123 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 97 | lt5 | lt6 | lt2 | 46162 | lt2 | 257 | 21 | nd | 84 | 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120549 | 709110 | 7163260 | 851 | 045 | 827 | 064 | 028 | lt005 | 066 | 02 | 025 | 252 | lt005 | 211 | 1007 | 1 | lt4 | lt10 | 516 | lt4 | lt5 | 49 | 56 | lt4 | 10 | lt3 | 18 | lt2 | 9 | 17 | 18 | 135 | 5 | lt4 | 13 | lt5 | lt6 | 13 | 5 | 139 | 21 | 8 | 114 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120550 | 709190 | 7162721 | 516 | 087 | 135 | 324 | 901 | 021 | 646 | 957 | 246 | 031 | 008 | 362 | 101 | 1 | 4 | lt10 | 145 | lt4 | lt5 | lt6 | 17 | 70 | 15 | lt3 | lt5 | lt2 | lt7 | 70 | lt4 | 7 | lt4 | lt4 | 93 | lt5 | lt6 | 2 | 52157 | lt2 | 267 | 20 | 85 | 62 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120566 | 734201 | 7165328 | 733 | 003 | 1 | lt4 | 10 | 261 | lt4 | lt5 | 8 | 257 | 24 | 24 | lt3 | lt5 | 2 | 8 | 97 | 12 | lt2 | lt4 | lt4 | 376 | lt5 | lt6 | lt2 | lt2 | 962 | 5 | 59 | 61 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120593 | 707343 | 7160447 | 48 | 046 | 116 | 248 | 735 | 017 | 14 | 101 | 148 | lt005 | 005 | 464 | 1007 | lt1 | lt4 | lt10 | 35 | lt4 | lt5 | lt6 | 1617 | 39 | 11 | lt3 | lt5 | lt2 | lt7 | 611 | lt4 | lt2 | lt4 | lt4 | 91 | lt5 | lt6 | lt2 | lt2 | 220 | 13 | 72 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120630 | 722750 | 7168750 | 38 | 014 | 733 | 088 | 695 | 014 | 207 | 725 | 095 | lt005 | lt005 | 18 | 1009 | 1 | lt4 | 10 | 41 | lt4 | lt5 | lt6 | 2746 | 46 | 6 | lt3 | lt5 | lt2 | lt7 | 1110 | lt4 | lt2 | lt4 | lt4 | 32 | lt5 | lt6 | lt2 | lt2 | 137 | 6 | 56 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120688 | 739099 | 7173927 | 521 | 084 | 139 | 322 | 775 | 017 | 658 | 104 | 288 | 017 | 008 | 277 | 101 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 160 | 35 | 13 | lt3 | lt5 | lt2 | lt7 | 133 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | lt2 | lt2 | 317 | 20 | 78 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120692 | 738903 | 7174351 | 496 | 032 | 134 | 271 | 658 | 015 | 115 | 101 | 223 | 009 | lt005 | 405 | 101 | lt1 | lt4 | lt10 | 149 | lt4 | lt5 | lt6 | 941 | 57 | 12 | lt3 | lt5 | lt2 | lt7 | 334 | lt4 | lt2 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 205 | 13 | 61 | 32 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120698 | 735588 | 7172781 | 546 | 059 | 136 | 26 | 576 | 014 | 727 | 101 | 346 | 006 | 006 | 246 | 1008 | lt1 | 15 | lt10 | 71 | lt4 | lt5 | lt6 | 315 | 60 | 11 | lt3 | lt5 | lt2 | lt7 | 100 | lt4 | lt2 | lt4 | lt4 | 67 | lt5 | lt6 | lt2 | lt2 | 228 | 16 | 65 | 44 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120727 | 456 | 015 | 815 | 227 | 694 | 016 | 225 | 686 | 045 | lt005 | lt005 | 726 | 1009 | lt1 | lt4 | lt10 | 27 | lt4 | lt5 | lt6 | 2788 | 31 | 6 | lt3 | lt5 | lt2 | lt7 | 1075 | lt4 | lt2 | lt4 | lt4 | 14 | lt5 | lt6 | lt2 | lt2 | 141 | 7 | 69 | 25 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120728 | 687200 | 7128470 | 545 | 04 | 141 | 225 | 609 | 015 | 916 | 624 | 5 | lt005 | 005 | 324 | 1014 | lt1 | 23 | lt10 | 61 | lt4 | lt5 | lt6 | 479 | 103 | 7 | lt3 | lt5 | lt2 | lt7 | 202 | lt4 | lt2 | lt4 | lt4 | 68 | lt5 | lt6 | lt2 | lt2 | 213 | 14 | 70 | 36 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120729 | 686100 | 7128750 | 833 | 027 | 1 | 814 | lt10 | 298 | lt4 | lt5 | lt6 | 2024 | 80 | 4 | lt3 | lt5 | lt2 | 9 | 796 | 4 | 46 | 17 | lt4 | 46 | lt5 | lt6 | lt2 | lt2 | 115 | 15 | 50 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120730 | 686300 | 7128650 | 383 | 003 | 1 | 9 | lt10 | 73 | lt4 | lt5 | lt6 | 3998 | 203 | 5 | lt3 | lt5 | lt2 | 15 | 1785 | lt4 | lt2 | 4 | lt4 | 8 | lt5 | lt6 | lt2 | lt2 | 270 | 19 | 108 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120770 | 675368 | 7143153 | 11 | 138 | lt1 | 246 | lt10 | 458 | lt4 | lt5 | lt6 | 1351 | 50 | 7 | lt3 | lt5 | lt2 | 12 | 259 | 4 | 57 | 5 | lt4 | 114 | lt5 | 6 | lt2 | lt2 | 155 | 9 | 45 | 31 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120801 | 686900 | 7143160 | 916 | 213 | 1 | 169 | 660 | 1736 | lt4 | lt5 | 66 | 1275 | 594 | 5 | lt3 | 26 | lt2 | 13 | 101 | 24 | 41 | lt4 | lt4 | 94 | lt5 | 11 | lt2 | lt2 | 147 | 35 | 98 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120802 | 686900 | 7143160 | 146 | 009 | lt1 | 17 | lt10 | 130 | lt4 | lt5 | 12 | 3035 | 213 | 19 | lt3 | 6 | lt2 | 19 | 1488 | 4 | 12 | lt4 | lt4 | 31 | lt5 | lt6 | 2 | lt2 | 432 | 22 | 148 | 116 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120873 | 697233 | 7155938 | 518 | 133 | 142 | 374 | 907 | 02 | 572 | 106 | 23 | 044 | 016 | 117 | 1009 | lt1 | lt4 | lt10 | 204 | lt4 | lt5 | 23 | 72 | 232 | 18 | lt3 | 8 | lt2 | lt7 | 58 | lt4 | 40 | lt4 | lt4 | 134 | lt5 | lt6 | 3 | lt2 | 239 | 33 | 95 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120874 | 699393 | 7156313 | 503 | 062 | 148 | 29 | 648 | 016 | 812 | 112 | 313 | 01 | 006 | 31 | 1012 | lt1 | lt4 | lt10 | 124 | lt4 | lt5 | lt6 | 356 | 99 | 12 | lt3 | lt5 | lt2 | lt7 | 140 | lt4 | lt2 | lt4 | lt4 | 80 | lt5 | lt6 | lt2 | lt2 | 244 | 14 | 71 | 46 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120876 | 694754 | 7155096 | 506 | 091 | 141 | 358 | 748 | 017 | 751 | 109 | 142 | 026 | 009 | 371 | 1009 | lt1 | lt4 | lt10 | 125 | lt4 | lt5 | lt6 | 176 | 141 | 15 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 3 | lt4 | lt4 | 178 | lt5 | lt6 | lt2 | lt2 | 262 | 20 | 103 | 71 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120877 | 694754 | 7155096 | 509 | 085 | 142 | 399 | 735 | 018 | 709 | 105 | 209 | 034 | 008 | 34 | 1011 | lt1 | lt4 | lt10 | 103 | lt4 | lt5 | lt6 | 119 | 158 | 15 | lt3 | lt5 | lt2 | lt7 | 107 | lt4 | 4 | lt4 | lt4 | 182 | lt5 | lt6 | 2 | lt2 | 269 | 19 | 95 | 70 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120878 | 694149 | 7154736 | 488 | 082 | 143 | 385 | 717 | 018 | 765 | 128 | 174 | 008 | 008 | 33 | 1009 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 137 | 107 | 15 | lt3 | lt5 | lt2 | lt7 | 105 | lt4 | lt2 | lt4 | lt4 | 142 | lt5 | lt6 | lt2 | lt2 | 257 | 24 | 83 | 60 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120891 | 677938 | 7168840 | 4880 | 082 | 1430 | 385 | 717 | 018 | 765 | 1280 | 174 | 008 | 008 | 330 | 10077 | 1 | 4 | 10 | 86 | 4 | 5 | 6 | 137 | 107 | 15 | 5 | 2 | 7 | 105 | 4 | 2 | 4 | 4 | 142 | 2 | 2 | 257 | 24 | 83 | 60 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124203 | 685884 | 7169152 | 496 | 089 | 14 | 329 | 852 | 02 | 733 | 981 | 233 | 009 | 008 | 36 | 998 | lt1 | lt4 | lt10 | 53 | lt4 | lt5 | lt6 | 65 | 122 | 14 | lt3 | lt5 | lt2 | lt7 | 91 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | 2 | lt2 | 280 | 19 | 104 | 66 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124204 | 685884 | 7168152 | 511 | 082 | 135 | 254 | 81 | 019 | 74 | 106 | 235 | 033 | 008 | 343 | 1006 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 130 | 85 | 12 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 4 | lt4 | lt4 | 47 | lt5 | lt6 | lt2 | lt2 | 261 | 18 | 88 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124208 | 685884 | 7169152 | 497 | 075 | 143 | 293 | 769 | 017 | 784 | 115 | 181 | 03 | 008 | 35 | 1007 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 129 | 132 | 14 | lt3 | lt5 | lt2 | lt7 | 94 | lt4 | 5 | lt4 | lt4 | 84 | lt5 | lt6 | lt2 | lt2 | 255 | 17 | 87 | 54 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132787 | 630625 | 7198600 | 492 | 07 | 142 | 265 | 735 | 017 | 857 | 126 | 176 | 009 | 006 | 335 | 1008 | 1 | lt4 | lt10 | 75 | lt4 | lt5 | lt6 | 136 | 105 | 16 | lt3 | lt5 | lt2 | lt7 | 158 | 5 | lt2 | lt4 | lt4 | 126 | lt5 | lt6 | lt2 | lt2 | 247 | 17 | 70 | 52 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132788 | 630625 | 7198600 | 218 | lt001 | lt1 | lt4 | lt10 | 864 | lt4 | lt5 | lt6 | 454 | 9 | lt3 | lt3 | lt5 | lt2 | lt7 | 67 | lt4 | lt2 | lt4 | lt4 | 9 | lt5 | lt6 | 2 | lt2 | 41 | 3 | 7 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132789 | 602460 | 7168288 | 556 | 021 | 138 | 329 | 587 | 016 | 612 | 111 | 131 | lt005 | lt005 | 303 | 303 | 1005 | nd | lt1 | lt4 | lt10 | 130 | lt4 | lt5 | lt6 | 158 | nd | 76 | 8 | lt3 | lt5 | nd | lt2 | lt7 | 98 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 16 | lt2 | 12590 | lt2 | 204 | 13 | nd | 72 | 17 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132790 | 613877 | 7170789 | 527 | 035 | 138 | 239 | 605 | 016 | 83 | 113 | 189 | lt005 | lt005 | 338 | 338 | 1006 | nd | lt1 | lt4 | lt10 | 81 | lt4 | lt5 | lt6 | 503 | nd | 81 | 10 | lt5 | nd | lt2 | lt7 | 190 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 27 | lt5 | 9 | lt2 | 20983 | lt2 | 211 | 14 | nd | 65 | 24 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132791 | 621561 | 7169810 | 499 | 057 | 133 | 308 | 649 | 015 | 96 | 121 | 204 | 005 | 006 | 316 | 316 | 1007 | nd | lt1 | 4 | lt10 | 71 | lt4 | lt5 | lt6 | 633 | nd | 80 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 281 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 75 | lt5 | lt6 | lt2 | 34172 | lt2 | 233 | 16 | nd | 74 | 40 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132792 | 616685 | 7171750 | 503 | 084 | 134 | 527 | 637 | 017 | 813 | 104 | 107 | 005 | 007 | 432 | 1006 | lt1 | lt4 | lt10 | 12 | lt4 | lt5 | lt6 | 314 | 144 | 13 | lt3 | 6 | lt2 | lt7 | 204 | 5 | lt2 | lt4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 285 | 28 | 95 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132793 | 622866 | 7161836 | 4860 | 031 | 1350 | 362 | 510 | 013 | 1040 | 1090 | 231 | 001 | 003 | 321 | 9812 | 2 | 4 | 3 | 29 | 4 | 5 | 6 | 872 | 45 | 61 | 11 | 3 | 97 | 7 | 379 | 4 | 3 | 2 | 2 | 4 | 4 | 72 | 2 | 2 | 216 | 14 | 4 | 60 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132794 | 622866 | 7161786 | 4840 | 014 | 576 | 203 | 615 | 015 | 2160 | 863 | 033 | 001 | 001 | 549 | 9870 | 2 | 4 | 4 | 11 | 6 | 5 | 6 | 2460 | 71 | 22 | 5 | 3 | 2 | 7 | 1020 | 4 | 4 | 3 | 2 | 4 | 4 | 11 | 2 | 2 | 155 | 7 | 4 | 63 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133033 | 638351 | 7157551 | 4450 | 156 | 1110 | 611 | 440 | 020 | 318 | 1330 | 468 | 034 | 021 | 906 | 9864 | 01 | 05 | 5 | 323 | 07 | 01 | 296 | 190 | 36 | 84 | 05 | 126 | 01 | 11 | 75 | 19 | 11 | 11 | 51 | 02 | 1 | 07 | 135 | 22 | 07 | 276 | 241 | 05 | 73 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133034 | 638351 | 7157551 | 4710 | 013 | 836 | 237 | 696 | 014 | 1980 | 764 | 012 | 001 | 003 | 596 | 9862 | 02 | 12 | 2 | 18 | 45 | 01 | 32 | 3448 | 69 | 22 | 16 | 16 | 23 | 32 | 1048 | 11 | 5 | 9 | 17 | 18 | 42 | 19 | 52 | 15 | 01 | 133 | 58 | 84 | 72 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133035 | 638300 | 7157750 | 4740 | 013 | 668 | 349 | 512 | 014 | 2200 | 801 | 022 | 003 | 001 | 521 | 9844 | 02 | 07 | 6 | 52 | 14 | 01 | 11 | 2608 | 73 | 34 | 22 | 12 | 03 | 33 | 1295 | 15 | 10 | 9 | 22 | 06 | 29 | 1 | 12 | 16 | 02 | 116 | 72 | 58 | 61 | 447 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133038 | 632615 | 7159390 | 5060 | 048 | 1600 | 316 | 443 | 012 | 572 | 1410 | 150 | 032 | 006 | 267 | 022 | 102 | lt05 | 70 | 110 | lt05 | lt01 | 216 | 392 | 29 | 93 | 57 | 147 | 10 | 12 | 28 | 138 | 29 | lt2 | 3 | 179 | 297 | 31 | 74 | 141 | 21 | 28776 | 02 | 181 | 14 | 139 | 59 | 709 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133039 | 632600 | 7159000 | 5160 | 034 | 1550 | 281 | 555 | 014 | 644 | 1090 | 252 | 026 | 002 | 309 | 026 | lt01 | lt05 | 30 | 80 | lt05 | lt01 | 06 | 422 | 36 | 88 | 47 | lt05 | 6 | 05 | 33 | 183 | lt05 | lt2 | lt2 | 46 | 115 | 32 | 29 | 139 | lt05 | 20383 | lt01 | 216 | 148 | 77 | 66 | 338 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133043 | 632906 | 7159832 | 4970 | 073 | 1490 | 272 | 790 | 018 | 626 | 1260 | 171 | 031 | 006 | 236 | 022 | 03 | 21 | 30 | 412 | 09 | 01 | 46 | 66 | 37 | 129 | 05 | 61 | 8 | 06 | 41 | 121 | 48 | lt2 | 9 | 99 | 44 | 11 | 27 | 119 | 13 | 43764 | 02 | 268 | 203 | 33 | 88 | 470 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133046 | 633939 | 7161905 | 4980 | 051 | 1280 | 263 | 708 | 016 | 1070 | 1060 | 163 | 014 | 005 | 309 | 016 | lt01 | lt05 | lt2 | 48 | lt05 | lt01 | 18 | 678 | 43 | 85 | 47 | 53 | 8 | 04 | 05 | 327 | lt05 | lt2 | lt2 | 06 | 68 | 34 | 15 | 123 | lt05 | 30575 | lt01 | 227 | 147 | 51 | 76 | 443 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133047 | 633939 | 7161905 | 5200 | 079 | 1400 | 280 | 738 | 017 | 548 | 1080 | 227 | 039 | 007 | 264 | 022 | 118 | lt05 | lt2 | 60 | lt05 | lt01 | 36 | 116 | 36 | 74 | 56 | 48 | 12 | 04 | 44 | 81 | lt05 | lt2 | lt2 | 95 | 46 | 38 | 09 | 101 | lt05 | 47361 | lt01 | 261 | 193 | 45 | 77 | 673 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133048 | 633939 | 7161905 | 4800 | 053 | 1050 | 391 | 746 | 018 | 972 | 1360 | 100 | 034 | 004 | 390 | 015 | lt01 | lt05 | 30 | 63 | lt05 | lt01 | 37 | 200 | 55 | 192 | 55 | 10 | 11 | 02 | 19 | 156 | 36 | lt2 | 3 | 55 | 08 | 43 | lt05 | 110 | lt05 | 31774 | lt01 | 276 | 126 | 12 | 76 | 410 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133049 | 634427 | 7166123 | 4900 | 059 | 1390 | 361 | 656 | 016 | 658 | 1300 | 190 | 019 | 005 | 328 | 015 | lt01 | lt05 | 30 | 45 | lt05 | lt01 | 25 | 120 | 42 | 164 | 66 | 12 | 10 | 07 | 32 | 143 | 24 | lt2 | lt2 | 20 | 33 | 24 | lt05 | 101 | lt05 | 35371 | lt01 | 220 | 145 | 82 | 67 | 442 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133050 | 635551 | 7169572 | 4890 | 060 | 1280 | 365 | 706 | 017 | 698 | 1370 | 137 | 023 | 005 | 348 | 011 | lt01 | lt05 | 30 | 36 | lt05 | lt01 | 22 | 165 | 49 | 108 | 64 | 08 | 11 | 04 | 24 | 152 | 22 | lt2 | 4 | 49 | 06 | 33 | lt05 | 108 | lt05 | 35970 | lt01 | 233 | 149 | 18 | 68 | 415 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133051 | 635603 | 7169579 | 0 | 74 | 0 | 02 | 15 | 12 | 114 | 114 | 24 | 91 | 13 | 05 | 84 | 73 | 27 | 12 | 11 | 24 | 0 | 40 | 15 | 158 | 173 | 043 | 256 | 18 | 05 | 74 | 62 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133052 | 635259 | 7169444 | 5160 | 086 | 1360 | 411 | 719 | 016 | 569 | 1030 | 155 | 048 | 008 | 344 | 9906 | 038 | 01 | 05 | 2 | 151 | 05 | 01 | 94 | 148 | 37 | 136 | 33 | 11 | 03 | 34 | 93 | 05 | 2 | 2 | 105 | 02 | 24 | 05 | 145 | 05 | 01 | 296 | 191 | 05 | 85 | 718 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133054 | 634952 | 7169267 | 0 | 62 | 05 | 0 | 38 | 5 | 105 | 44 | 18 | 25 | 41 | 12 | 13 | 57 | 48 | 5 | 6 | 12 | 0 | 26 | 18 | 411 | 6 | 166 | 182 | 18 | 08 | 38 | 104 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133060 | 648256 | 7160919 | 0 | 23 | 0 | 02 | 19 | 6 | 89 | 129 | 18 | 10 | 5 | 12 | 88 | 62 | 27 | 3 | 0 | 92 | 0 | 38 | 21 | 251 | 111 | 037 | 318 | 25 | 08 | 85 | 76 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133063 | 648467 | 7150024 | 4400 | 018 | 889 | 410 | 531 | 015 | 2270 | 702 | 037 | 003 | 002 | 705 | 9982 | 011 | 01 | 05 | 2 | 7 | 05 | 01 | 05 | 3170 | 83 | 19 | 53 | 05 | 03 | 18 | 1370 | 15 | 9 | 13 | 09 | 04 | 23 | 05 | 135 | 05 | 01 | 123 | 76 | 27 | 72 | 139 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133064 | 647573 | 7150076 | 5150 | 032 | 1450 | 307 | 514 | 015 | 634 | 1390 | 178 | 001 | 003 | 244 | 9918 | 015 | 01 | 05 | 3 | 50 | 05 | 01 | 05 | 456 | 29 | 40 | 65 | 14 | 04 | 09 | 191 | 05 | 11 | 11 | 05 | 04 | 36 | 05 | 577 | 05 | 01 | 222 | 144 | 21 | 61 | 26 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133073 | 626850 | 7161292 | 5150 | 033 | 1440 | 273 | 573 | 014 | 748 | 1250 | 232 | 001 | 003 | 264 | 9981 | 011 | 01 | 05 | 3 | 43 | 05 | 01 | 05 | 467 | 38 | 78 | 32 | 19 | 02 | 29 | 202 | 14 | 13 | 12 | 05 | 03 | 32 | 05 | 497 | 05 | 01 | 219 | 137 | 05 | 61 | 258 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133076 | 626850 | 7161292 | 4990 | 074 | 1490 | 410 | 612 | 015 | 546 | 1320 | 148 | 006 | 007 | 297 | 9915 | 022 | 01 | 05 | 3 | 42 | 05 | 01 | 85 | 154 | 33 | 55 | 65 | 34 | 03 | 34 | 93 | 05 | 7 | 11 | 05 | 02 | 33 | 05 | 151 | 05 | 01 | 263 | 169 | 16 | 84 | 678 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133096 | 645954 | 7171243 | 4500 | 013 | 916 | 192 | 711 | 014 | 2110 | 744 | 015 | 002 | 001 | 699 | 9917 | 022 | 01 | 05 | 2 | 75 | 05 | 01 | 23 | 3100 | 93 | 69 | 6 | 146 | 06 | 14 | 1620 | 17 | 7 | 7 | 07 | 17 | 26 | 05 | 27 | 05 | 01 | 132 | 212 | 21 | 69 | 103 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133098 | 636053 | 7155351 | 4950 | 057 | 1510 | 228 | 646 | 014 | 728 | 1380 | 135 | 010 | 006 | 307 | 9971 | 015 | 01 | 05 | 6 | 174 | 05 | 01 | 08 | 487 | 31 | 81 | 47 | 58 | 05 | 37 | 165 | 05 | 12 | 16 | 15 | 02 | 26 | 05 | 112 | 35 | 02 | 220 | 135 | 05 | 64 | 429 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136749 | 667073 | 7199167 | 5080 | 072 | 1420 | 410 | 567 | 015 | 601 | 1330 | 166 | 022 | 007 | 221 | 9911 | 011 | 01 | 05 | 4 | 222 | 05 | 01 | 42 | 331 | 37 | 82 | 57 | 59 | 04 | 29 | 131 | 1 | 12 | 11 | 32 | 07 | 31 | 05 | 237 | 05 | 01 | 257 | 175 | 15 | 75 | 665 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136751 | 659000 | 7122223 | 0 | 12 | 0 | 0 | 98 | 3 | 209 | 68 | 15 | 62 | 34 | 04 | 44 | 86 | 2 | 9 | 7 | 43 | 0 | 34 | 09 | 304 | 053 | 021 | 207 | 15 | 09 | 48 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139131 | 621200 | 7215100 | 4790 | 065 | 1470 | 301 | 746 | 019 | 682 | 1290 | 254 | 004 | 006 | 319 | 9946 | 026 | 01 | 05 | 3 | 211 | 05 | 01 | 43 | 358 | 43 | 103 | 07 | 4 | 02 | 46 | 154 | 05 | 8 | 14 | 05 | 02 | 29 | 05 | 616 | 05 | 02 | 281 | 19 | 05 | 77 | 484 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139132 | 621190 | 7215090 | 0 | 14 | 0 | 01 | 11 | 0 | 66 | 18 | 46 | 59 | 40 | 05 | 95 | 11 | 14 | 0 | 0 | 108 | 0 | 51 | 21 | 242 | 87 | 124 | 389 | 7 | 24 | 51 | 134 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139133 | 666700 | 7193500 | 0 | 09 | 0 | 02 | 56 | 0 | 0 | 18 | 37 | 39 | 92 | 05 | 63 | 4 | 62 | 0 | 0 | 63 | 0 | 53 | 19 | 33 | 21 | 24 | 29 | 18 | 08 | 25 | 290 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139134 | 621755 | 7169255 | 0 | 08 | 0 | 0 | 85 | 3 | 3 | 3 | 15 | 63 | 14 | 09 | 06 | 0 | 2 | 0 | 0 | 73 | 0 | 06 | 08 | 76 | 129 | 05 | 4 | 3 | 03 | 3 | 35 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139135 | 621000 | 7169500 | 5016 | 037 | 1406 | 241 | 647 | 017 | 918 | 1126 | 248 | 006 | 003 | 15 | 5812 | 222 | 438 | 53 | 65 | 10 | 438 | 077 | 1320 | 100E-07 | 171 | 100E-07 | 500E-08 | 54 | 2 | 53 | 500E-08 | 500E-08 | 212 | 15 | 72 | 19 | 036 | 194 | 094 | 048 | 190 | 038 | 289 | 071 | 222 | 034 | 232 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139136 | 621000 | 7169500 | 5236 | 027 | 1373 | 239 | 577 | 016 | 897 | 1068 | 21 | 007 | 003 | 15 | 5265 | 210 | 491 | 53 | 162 | 10 | 491 | 086 | 1290 | 100E-07 | 196 | 100E-07 | 1 | 48 | 200E-07 | 62 | 500E-08 | 500E-08 | 189 | 13 | 63 | 13 | 036 | 161 | 078 | 041 | 160 | 039 | 259 | 068 | 214 | 038 | 221 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139137 | 620904 | 7169533 | 4737 | 108 | 1123 | 33 | 789 | 018 | 1191 | 106 | 203 | 008 | 012 | 15 | 13407 | 2170 | 1150 | 82 | 119 | 15 | 1150 | 897 | 1380 | 6 | 525 | 2 | 500E-08 | 39 | 4 | 143 | 1 | 500E-08 | 265 | 17 | 90 | 65 | 278 | 1143 | 314 | 124 | 391 | 066 | 391 | 084 | 222 | 031 | 187 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139138 | 620992 | 7169508 | 5075 | 03 | 141 | 177 | 678 | 017 | 996 | 925 | 264 | 044 | 002 | 05 | 7628 | 124 | 660 | 56 | 61 | 10 | 660 | 042 | 1310 | 100E-07 | 232 | 100E-07 | 55 | 49 | 2 | 62 | 500E-08 | 500E-08 | 194 | 12 | 65 | 14 | 019 | 104 | 062 | 031 | 135 | 030 | 225 | 055 | 166 | 026 | 175 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139139 | 620992 | 7169508 | 4747 | 018 | 1006 | 141 | 804 | 017 | 1989 | 829 | 089 | 002 | 001 | 500E-08 | 7171 | 148 | 1770 | 95 | 53 | 75 | 1770 | 089 | 1320 | 100E-07 | 835 | 100E-07 | 500E-08 | 39 | 2 | 225 | 500E-08 | 500E-08 | 139 | 8 | 60 | 7 | 019 | 098 | 063 | 028 | 124 | 028 | 206 | 051 | 157 | 026 | 160 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139140 | 620992 | 7169508 | 5201 | 117 | 1269 | 224 | 762 | 016 | 761 | 1089 | 239 | 025 | 013 | 05 | 8447 | 2455 | 212 | 52 | 161 | 15 | 212 | 982 | 1210 | 5 | 135 | 100E-07 | 45 | 42 | 4 | 228 | 1 | 500E-08 | 270 | 17 | 87 | 80 | 308 | 1270 | 330 | 120 | 387 | 061 | 364 | 074 | 200 | 028 | 161 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139141 | 620992 | 7169488 | 6179 | 081 | 147 | 284 | 594 | 006 | 496 | 012 | 007 | 32 | 01 | 1 | 74341 | 6413 | 414 | 41 | 31 | 19 | 414 | 2988 | 410 | 12 | 163 | 3 | 161 | 29 | 4 | 11 | 155 | 3 | 90 | 19 | 132 | 198 | 677 | 2282 | 433 | 094 | 430 | 059 | 295 | 058 | 166 | 026 | 170 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256h | 715830 | 7171470 | 6528 | 068 | 1179 | 412 | 511 | 004 | 551 | 013 | 005 | 24 | 012 | 1 | 44782 | 7429 | 348 | 39 | 2 | 15 | 348 | 3419 | 300 | 10 | 176 | 3 | 121 | 21 | 4 | 9 | 19 | 3 | 73 | 27 | 83 | 266 | 834 | 2926 | 592 | 121 | 584 | 082 | 451 | 089 | 249 | 038 | 231 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393s | 687539 | 7143275 | 3634 | 015 | 744 | 519 | 582 | 02 | 1191 | 1139 | 002 | 001 | 002 | 177 | 2109 | 066 | 2020 | 175 | 257 | 6 | 043 | 1440 | 00000001 | 1000 | 00000001 | 000000005 | 24 | 2 | 42 | 000000005 | 05 | 108 | 6 | 35 | 13 | 016 | 080 | 044 | 022 | 067 | 014 | 094 | 022 | 074 | 012 | 090 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601s | 668775 | 7146298 | 1248 | 005 | 339 | 812 | 262 | 026 | 1592 | 217 | 005 | 001 | 0 | 156 | 1400 | 058 | 850 | 63 | 46 | 25 | 066 | 1990 | 00000001 | 1010 | 1 | 000000005 | 10 | 2 | 66 | 000000005 | 000000005 | 87 | 11 | 22 | 3 | 024 | 085 | 052 | 025 | 083 | 021 | 145 | 034 | 111 | 017 | 131 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
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120303 | 655250 | 7126000 | 2302 | 011 | 404 | 31 | 071 | 059 | 074 | 3572 | 004 | 141 | 004 | 53 | 20581 | 1117 | 285 | 7 | 4 | 45 | 720 | 4740 | 1 | 51 | 12 | 435 | 00000001 | 2 | 96 | 25 | 000000005 | 36 | 9 | 21 | 17 | 141 | 504 | 105 | 042 | 126 | 021 | 127 | 030 | 097 | 015 | 109 | 019 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
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120373s | 675250 | 7167875 | 5541 | 088 | 1306 | 795 | 346 | 014 | 199 | 144 | 005 | 004 | 009 | 1 | 7754 | 1109 | 26 | 29 | 74 | 225 | 521 | 1040 | 2 | 41 | 3 | 05 | 48 | 4 | 67 | 000000005 | 000000005 | 494 | 25 | 50 | 55 | 161 | 716 | 213 | 067 | 256 | 050 | 325 | 074 | 237 | 035 | 267 | 041 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432s | 673950 | 7171700 | 5469 | 078 | 1137 | 81 | 399 | 02 | 311 | 1468 | 016 | 005 | 006 | 2 | 11068 | 1433 | 62 | 44 | 22 | 20 | 634 | 1490 | 1 | 88 | 8 | 15 | 55 | 4 | 495 | 1 | 000000005 | 346 | 24 | 49 | 49 | 202 | 897 | 283 | 137 | 343 | 070 | 452 | 104 | 321 | 048 | 354 | 051 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137A | not available | 6241 | 067 | 991 | 186 | 893 | 019 | 924 | 011 | 0 | 005 | 01 | 15 | 2345 | 6927 | 595 | 43 | 123 | 12 | 3489 | 1470 | 10 | 235 | 4 | 25 | 21 | 4 | 55 | 175 | 2 | 77 | 16 | 112 | 288 | 734 | 2545 | 453 | 074 | 448 | 050 | 239 | 041 | 129 | 019 | 143 | 023 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137B | not available | 6118 | 074 | 1029 | 19 | 912 | 019 | 96 | 011 | 0 | 009 | 01 | 1 | 3042 | 6659 | 780 | 45 | 121 | 12 | 2999 | 1430 | 10 | 218 | 6 | 4 | 22 | 4 | 4 | 175 | 25 | 80 | 27 | 116 | 312 | 704 | 2493 | 499 | 095 | 542 | 075 | 415 | 083 | 249 | 037 | 262 | 039 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82144 | not available | 6901 | 044 | 1124 | 143 | 288 | 021 | 188 | 365 | 27 | 14 | 013 | 15 | 38750 | 6263 | 117 | 22 | 22 | 12 | 3381 | 1690 | 8 | 48 | 37 | 67 | 11 | 2 | 107 | 175 | 25 | 46 | 19 | 61 | 199 | 679 | 2348 | 436 | 093 | 441 | 056 | 304 | 052 | 157 | 022 | 154 | 022 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82148 | not available | 6314 | 07 | 124 | 312 | 581 | 017 | 717 | 01 | 005 | 197 | 01 | 1 | 41557 | 6431 | 505 | 53 | 22 | 15 | 3168 | 1310 | 10 | 211 | 4 | 99 | 23 | 4 | 8 | 165 | 25 | 72 | 18 | 121 | 227 | 689 | 2407 | 462 | 095 | 440 | 055 | 281 | 050 | 159 | 022 | 168 | 025 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82150 | not available | 9469 | 001 | 012 | 45 | 062 | 001 | 001 | 001 | 0 | 0 | 001 | 1150 | 13761 | 225 | 10 | 2 | 7 | 000000005 | 310 | 40 | 00000001 | 11 | 00000001 | 000000005 | 00000001 | 6 | 000000005 | 000000005 | 3800 | 00000001 | 700 | 300 | 044 | 122 | 021 | 012 | 021 | 002 | 013 | 002 | 004 | 000 | 005 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82153 | not available | 41767 | 296 | 256 | 047 | 214 | 049 | 031 | 072 | 013 | 090 | 023 | 077 | 010 | 072 | 010 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82155 | not available | 4977 | 081 | 1429 | 329 | 833 | 02 | 718 | 945 | 255 | 018 | 007 | 2 | 10432 | 1154 | 175 | 65 | 117 | 135 | 175 | 395 | 1540 | 2 | 135 | 100E-07 | 3 | 57 | 4 | 75 | 500E-08 | 500E-08 | 290 | 18 | 104 | 45 | 174 | 807 | 287 | 119 | 400 | 083 | 496 | 117 | 328 | 056 | 311 | 053 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82158 | not available | 5076 | 077 | 1356 | 336 | 794 | 019 | 714 | 996 | 197 | 035 | 006 | 15 | 16705 | 1081 | 163 | 55 | 128 | 135 | 163 | 373 | 1490 | 1 | 123 | 100E-07 | 55 | 54 | 2 | 166 | 500E-08 | 500E-08 | 268 | 17 | 98 | 43 | 159 | 772 | 261 | 108 | 365 | 070 | 470 | 107 | 304 | 046 | 279 | 042 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82160 | not available | 4799 | 033 | 127 | 192 | 57 | 017 | 1261 | 1352 | 09 | 004 | 002 | 115 | 5413 | 491 | 1360 | 52 | 50 | 105 | 1360 | 183 | 1370 | 100E-07 | 269 | 100E-07 | 05 | 46 | 4 | 87 | 500E-08 | 500E-08 | 159 | 8 | 50 | 18 | 074 | 333 | 108 | 052 | 167 | 030 | 198 | 045 | 131 | 019 | 116 | 016 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82179 | not available | 5338 | 053 | 1381 | 255 | 679 | 016 | 722 | 774 | 466 | 004 | 006 | 500E-08 | 3625 | 1347 | 326 | 50 | 48 | 115 | 326 | 523 | 1290 | 2 | 137 | 100E-07 | 500E-08 | 53 | 2 | 103 | 1 | 1 | 239 | 16 | 74 | 40 | 168 | 721 | 230 | 080 | 334 | 068 | 459 | 107 | 321 | 049 | 296 | 044 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82180 | not available | 462 | 02 | 998 | 154 | 752 | 017 | 1869 | 845 | 1 | 003 | 002 | 500E-08 | 749 | 081 | 2240 | 93 | 46 | 8 | 2240 | 029 | 1320 | 100E-07 | 795 | 100E-07 | 500E-08 | 40 | 200E-07 | 365 | 500E-08 | 500E-08 | 148 | 10 | 56 | 8 | 015 | 081 | 051 | 034 | 110 | 026 | 192 | 050 | 157 | 026 | 167 | 028 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82224 | not available | 5042 | 029 | 1394 | 187 | 675 | 015 | 976 | 1106 | 328 | 005 | 002 | 500E-08 | 1646 | 119 | 640 | 58 | 44 | 105 | 640 | 042 | 1140 | 100E-07 | 159 | 100E-07 | 500E-08 | 54 | 200E-07 | 109 | 500E-08 | 500E-08 | 204 | 12 | 41 | 14 | 022 | 124 | 075 | 041 | 160 | 036 | 265 | 063 | 195 | 031 | 206 | 032 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82225 | not available | 4701 | 022 | 1065 | 127 | 739 | 015 | 1732 | 727 | 233 | 002 | 001 | 500E-08 | 2735 | 106 | 1730 | 84 | 32 | 75 | 1730 | 062 | 1180 | 100E-07 | 690 | 100E-07 | 500E-08 | 43 | 2 | 415 | 500E-08 | 500E-08 | 159 | 11 | 58 | 9 | 023 | 128 | 063 | 031 | 125 | 028 | 204 | 050 | 161 | 026 | 162 | 025 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82226 | not available | 4256 | 014 | 689 | 357 | 494 | 011 | 2593 | 578 | 016 | 003 | 001 | 75 | 3377 | 038 | 2280 | 102 | 8 | 55 | 2280 | 015 | 835 | 100E-07 | 1380 | 100E-07 | 1 | 31 | 200E-07 | 205 | 500E-08 | 500E-08 | 104 | 5 | 46 | 6 | 008 | 042 | 027 | 010 | 058 | 013 | 097 | 025 | 075 | 012 | 078 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82228 | not available | 4399 | 016 | 796 | 185 | 65 | 014 | 246 | 647 | 017 | 001 | 001 | 500E-08 | 9402 | 076 | 2890 | 102 | 10 | 55 | 2890 | 052 | 1050 | 100E-07 | 1130 | 100E-07 | 500E-08 | 35 | 200E-07 | 65 | 500E-08 | 500E-08 | 131 | 6 | 41 | 7 | 017 | 072 | 032 | 010 | 065 | 014 | 106 | 027 | 084 | 013 | 082 | 013 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82229 | not available | 4897 | 024 | 1196 | 106 | 807 | 015 | 1448 | 71 | 298 | 003 | 002 | 500E-08 | 11033 | 081 | 1260 | 77 | 45 | 9 | 1260 | 024 | 1160 | 100E-07 | 459 | 100E-07 | 500E-08 | 46 | 200E-07 | 138 | 500E-08 | 500E-08 | 172 | 11 | 59 | 11 | 016 | 093 | 052 | 028 | 119 | 027 | 203 | 050 | 157 | 026 | 168 | 027 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82231 | not available | 509 | 027 | 1399 | 178 | 674 | 014 | 87 | 1152 | 329 | 005 | 002 | 500E-08 | 1186 | 092 | 510 | 52 | 58 | 10 | 510 | 038 | 1100 | 100E-07 | 136 | 100E-07 | 500E-08 | 57 | 2 | 144 | 500E-08 | 500E-08 | 202 | 13 | 41 | 12 | 018 | 101 | 057 | 030 | 135 | 030 | 220 | 058 | 177 | 029 | 191 | 029 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82234 | not available | 4847 | 087 | 1468 | 1174 | 022 | 874 | 1394 | 099 | 027 | 008 | 332 | 83 | 3 | 225 | 21 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82236 | not available | 5135 | 087 | 1461 | 1117 | 02 | 757 | 1032 | 274 | 109 | 008 | 228 | 70 | 15 | 329 | 19 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
135482 | Trillbar Complex | 5137 | 037 | 1481 | 232 | 561 | 016 | 869 | 1068 | 306 | 006 | 003 | 014 | 260 | 10014 | 39 | 2 | 593 | 59 | 61 | 00 | 08 | 08 | 1 | 124 | 1 | 1 | 51 | 00 | 08 | 235 | 17 | 61 | 20 | 0 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143538 | Trillbar Complex | 4961 | 141 | 1391 | 561 | 717 | 022 | 656 | 1136 | 204 | 022 | 011 | 014 | 163 | 10036 | 322 | 15 | 82 | 172 | 91 | 12 | 26 | 26 | 9 | 98 | 4 | 4 | 48 | 12 | 14 | 362 | 24 | 91 | 86 | 2 | 12 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143539 | Trillbar Complex | 4974 | 086 | 1196 | 128 | 734 | 016 | 1072 | 1395 | 237 | 009 | 006 | 013 | 150 | 10047 | 77 | 10 | 298 | 80 | 47 | 07 | 14 | 14 | 4 | 240 | 2 | 1 | 59 | 07 | 06 | 322 | 19 | 47 | 46 | 2 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
144310 | Trillbar Complex | 4711 | 115 | 1288 | 182 | 901 | 018 | 784 | 1161 | 250 | 008 | 012 | 013 | 240 | 10027 | 53 | 13 | 394 | 116 | 90 | 13 | 13 | 13 | 7 | 156 | 6 | 1 | 37 | 13 | 14 | 380 | 23 | 90 | 78 | 0 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
REPORT 59
GEOLOGY AND MINERALIZATIONOF THE PALAEOPROTEROZOICBRYAH AND PADBURY BASINSWESTERN AUSTRALIA
byF Pirajno S A Occhipinti and C P Swager
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
Perth 2000
MINISTER FOR MINESThe Hon Norman Moore MLC
DIRECTOR GENERALL C Ranford
DIRECTOR GEOLOGICAL SURVEY OF WESTERN AUSTRALIADavid Blight
Copy editor D P Reddy
REFERENCEThe recommended reference for this publication isPIRAJNO F OCCHIPINTI S A and SWAGER C P 2000 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury
Basins Western Australia Western Australia Geological Survey Report 59 52p
National Library of AustraliaCataloguing-in-publication entry
Pirajno Franco 1939ndashGeology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
BibliographyISBN 0 7309 6653 4
1 Geology Structural mdash Western Australia mdash Bryah Basin2 Geology Structural mdash Western Australia mdash Padbury Basin3 Mines and mineral resources mdash Western Australia mdash Bryah Basin4 Mines and mineral resources mdash Western Australia mdash Padbury Basin5 Bryah Region (WA)6 Padbury Region (WA)I Swager C PII Occhipinti S A (Sandra Anne)III Geological Survey of Western AustraliaIV Title (Series Report (Geological Survey of Western Australia) 59)
5531099413
ISSN 0508ndash4741
Grid references in this publication refer to the Australian Geodetic Datum (AGD84)
Printed by Optima Press Perth Western Australia
Copies available fromInformation CentreDepartment of Minerals and Energy100 Plain StreetEAST PERTH WESTERN AUSTRALIA 6004Telephone (08) 9222 3459 Facsimile (08) 9222 3444wwwdmewagovau
Cover photographFerruginous shale of the Millidie Creek Formation with a well-developed pencil cleavage 25 km northwest of Fraser Well(BRYAH AMG 651660)
iii
Contents
Abstract 1Introduction 1Regional tectonic setting 3Geology stratigraphy and geochronology 4
Peak Hill Schist and Marymia Inlier 5Bryah Group 6
Karalundi Formation 6Narracoota Formation 7
Peridotitic and high-Mg basalt association 7Intrusive rocks and layered intrusions 7Mafic and ultramafic schist 8Metabasaltic hyaloclastite 9Felsic schist 9Volcaniclastic rocks 10Carbonated and silicified metavolcanic rocks 11Jasperoidal chert 11Geochemistry of the Narracoota Formation 11
Ravelstone Formation 16Horseshoe Formation 16
Padbury Group 17Labouchere Formation 18Wilthorpe Formation 19
Beatty Park and Heines Members 19Robinson Range Formation 20Millidie Creek Formation 20Unassigned units of the Padbury Group 21
Structure 21D1 structures 23D2 structures 23D3 structures and their relationship to D2 structures 25D4 structures 25
Metamorphism 25Structural synthesis 27Mineralization 32
Gold deposits 33Peak Hill Jubilee and Mount Pleasant deposits 39Harmony deposit 41Labouchere Nathans and Fortnum deposits 41Wembley deposit 42Wilgeena deposit 43Durack St Crispin and Heines Find prospects 43Ruby Well group 43Mikhaburra deposit 43Wilthorpe deposit 43Cashman deposit 44
Volcanogenic copperndashgold deposits 44Supergene manganese deposits 44Iron ore 45Talc 45Discussion 45
Tectonic model and conclusions 46Acknowledgements 48References 49
Appendix
Gazetteer of localities 52
Plate
Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
iv
Figures
1 Stratigraphy of the former lsquoGlengarry Basinrsquo 22 Simplified geology of the Bryah Padbury and Yerrida Basins 43 Rotated orthoclase porphyroblast Peak Hill Schist 54 Partially recrystallized mylonite Peak Hill Schist 55 Peak Hill Schist mylonite from the Hangingwall Sequence 56 Outcrop of quartz mylonite Peak Hill Schist 67 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric 68 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt) 89 Basaltic hyaloclastite Narracoota Formation 9
10 Mafic volcaniclastic rock Narracoota Formation 1011 Volcanic breccia intersected in diamond drillhole BD1 1012 Total alkali versus silica diagram for rocks the Narracoota Formation 1313 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the
Narracoota Formation 1414 Geochemical characteristics of the Narracoota Formation rocks 1415 Geochemical discriminant plots for Narracoota Formation 1516 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation 1617 Schematic stratigraphy of the Horseshoe Formation 1718 Major regional structures in the Bryah and Padbury Groups 2219 Simplified geological map of the Bryah and Padbury Groups 2420 Selected hypothetical cross sections through the Bryah and Padbury Groups 2721 Model of the structural development of the BryahndashPadbury Group succession 2922 New model of the structural development of the BryahndashPadbury Group succession 3123 New model for the structural development of the BryahndashPadbury Group succession
and the Peak Hill Schist 3224 Schematic north-northwest to south-southeast cross section from the Bangemall Basin
into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins 3325 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins 3626 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet 3827 Albite porphyroblasts in mylonitic schist at Mount Pleasant 3928 The Mine Sequence schist 4029 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit 4030 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and
Marker quartzite unit 4031 Diagrammatic cross section of the Harmony ore zones 4132 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and
deformed Despair Granite 4433 Sketch illustrating a conceptual model for the origin of precious and base metal
deposits in the BryahndashPadbury and Yerrida Basins 4534 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and
Padbury Basins within the context of the Capricorn Orogen 46
Tables
1 Stratigraphy of the Bryah and Padbury Groups 32 Representative chemical analyses of the Narracoota Formation 123 Magnesium numbers for the Narracoota and Killara Formations 134 Selected geochemical parameters for the Narracoota Formation 135 Sequence of deformation events in the Bryah and Padbury Basins 236 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic
minerals of the Bryah Group and deformation fabrics 287 Gold production and remaining resources in the Bryah and Padbury Groups 348 Mineral production and remaining resources in the Bryah and Padbury Groups 359 Mineral deposits and occurrences in the Bryah and Padbury Basins 36
Digital dataset (in pocket)
Whole-rock geochemical analyses of Narracoota Formation rocks (narracootacsv)
1
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Geology and mineralization of thePalaeoproterozoic Bryah and Padbury
Basins Western Australia
by
F Pirajno S A Occhipinti and C P Swager
AbstractThe Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collision zonebetween the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains a succession of maficand ultramafic rocks of mid-oceanic ridge basalt to oceanic plateau affinity overlain by clastic andchemical sedimentary rocks The Bryah Basin was formed during back-arc sea-floor spreading andrifting on the northern margin of the Yilgarn Craton The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of the Bryah Basin as a forelandstructure resulting from either the c 1800 Ma oblique collision of the Pilbara and Yilgarn Cratons(Capricorn Orogeny) or the c 2000 Ma collision of the Glenburgh terrane and the Yilgarn Craton(Glenburgh Orogeny)
Important mineral deposits are contained in both basins and include mesothermal orogenic goldcopperndashgold volcanogenic massive sulfides manganese and iron ore The origin of the goldmineralization is related to metamorphism and deformation linked to the Capricorn Orogeny at c 18 GaThe formation of other deposits is related to pre-orogenic syngenetic processes
KEYWORDS Bryah Basin Padbury Basin Palaeoproterozoic stratigraphy geochemistry maficrocks ultramafic rocks mineralization mesothermal deposits gold
IntroductionIn early 1994 the Geological Survey of Western Australia(GSWA) commenced fieldwork to reassess the geologyand mineralization of the Palaeoproterozoic GlengarryBasin as part of a program of new mapping initiativesThe Glengarry Basin as defined by Gee and Grey (1993)constitutes the western part of the greater Palaeo-proterozoic Nabberu Province which in the east includesthe Earaheedy Basin (Bunting et al 1977 Hall andGoode 1978 Gee 1990)
The new mapping initiative resulted in the reappraisalof the geology tectonic evolution and mineralizationof the Glengarry Basin which is now recognized toconsist of three main geotectonic units the BryahPadbury and Yerrida Basins As a result the volcano-sedimentary rocks of the former lsquoGlengarry Grouprsquo arenow divided into the Bryah and Yerrida Groups (Fig 1 andTable 1) characterized not only by different lithologiesbut also by different regional structures metamorphismand mineral deposit types Some formations previouslyassigned to the lsquoGlengarry Grouprsquo have been reassigned
to the Padbury Group (Martin 1992) In additionthere is evidence to suggest that the economicallyimportant lsquoPeak Hill Metamorphic Suitersquo previouslyconsidered to be part of the lsquoGlengarry Grouprsquo (Gee1987) constitutes a separate unit the Peak Hill Schistderived from a protolith of probable Archaean ageConsequently the previous nomenclature (lsquoGlengarryGrouprsquo and lsquoGlengarry Basinrsquo) is no longer used Detailsof the old and new stratigraphy are presented in Figure 1and Table 1 and discussed in later sections The revisedstratigraphy of the former lsquoGlengarry Basinrsquo is presentedin Occhipinti et al (1997) Details of the stratigraphy andstructure of the lower Padbury Group are presented inMartin (1998)
The Bryah and Padbury Basins lie within the ROBINSON
RANGE and PEAK HILL 1250 000 sheets (MacLeod 1970Elias and Williams 1980 Gee 1987) and the north-western and northeastern corners of the BELELE andGLENGARRY 1250 000 sheets (Elias 1982 Elias et al
Capitalized names refer to standard 1100 000 map sheets unless otherwisespecified
2
Pirajno et al
1982) The Bryah and Padbury Groups (Fig 2) make upthe western part of the former lsquoGlengarry Basinrsquo andare now interpreted to have developed in rift and forelandbasins respectively (Martin 1994 Pirajno 1996 Pirajnoet al 1996 Pirajno et al 1998b) The Yerrida Group(Fig 2) makes up the eastern part of the former lsquoGlengarryBasinrsquo and includes two subgroups the Windplainand Mooloogool Subgroups (Fig 2 Table 1) whichdeveloped in sag and rift basins respectively (Pirajno et al1995ab 1996) The geology and mineralization ofthe Yerrida Basin are described in a separate Report(Pirajno and Adamides 2000) The Bryah Group isin faulted contact with the Yarlarweelor gneiss complexthe Marymia Inlier of the Archaean Yilgarn Cratonand the Palaeoproterozoic Yerrida Group The contactbetween the Bryah and the Yerrida Groups is along anortheasterly trending high-angle reverse fault (the GoodinFault)
Based on structural and metamorphic criteria the areaoccupied by the Bryah and Padbury Groups and thePeak Hill Schist can be regarded as a single domainIn this Report where appropriate this domain is referred
to as the BryahndashPadbury Basin The geology newstratigraphy geochronological constraints structureand metamorphism of the Bryah and Padbury Groups arediscussed The geochemistry of the volcanic componentof the Bryah Group and mineral deposits of the Bryahand Padbury Basins are also summarized A tectonicoverview and proposed model for the geodynamicevolution of the Bryah and Padbury Basins withinthe framework of the Capricorn Orogen conclude thereport
Work in the BryahndashPadbury area involved 125 000-scale mapping to produce 1100 000-scale geologicalmaps Geological mapping was carried out using125 000-scale colour aerial photography (availablefrom the Western Australian Department of LandAdministration) aeromagnetic images (400 m line-spacedcollected by GSWA in 1994) and Landsat TM imagesResults of geological mapping were integrated withpetrographic geochemical and geochronology studiesDuring this work a total of 1450 rock samples werecollected of which 776 were thin-sectioned and 136geochemically analysed In addition logging of diamond
Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
Gee (1987)P
AD
BU
RY
BA
SIN
GR
OU
PG
LEN
GA
RR
Y B
AS
ING
RO
UP
Millidie Creek Formation
Robinson Range Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Narracoota Volcanics
Karalundi Formation
Doolgunna Formation
Johnson Cairn Shale
Thaduna Greywacke
Juderina Formation
Maraloou Formation
Crispin Conglomerate
Finlayson Sandstone
Peak Hill Metamorphics
GLE
NG
AR
RY
BA
SIN
GR
OU
P
Maraloou Formation
Thaduna Greywacke
Narracoota Volcanics
Doolgunna Formation
Johnson Cairn Shale
Juderina Formation(Finlayson SandstoneMember)
YE
RR
IDA
BA
SIN
GR
OU
P
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Peak Hill Schist
BR
YA
H B
AS
ING
RO
UP
PA
DB
UR
Y B
AS
ING
RO
UP
TE
CT
ON
IC C
ON
TA
CT
Millidie Creek Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Karalundi Formation
Ravelstone Formation
Narracoota FormationMaraloou Formation
Killarra Formation(Bartle Member)
Doolgunna Formation
Thaduna Formation
Juderina Formation
170100
Gee and Grey (1993) Occhipinti et al (1997) Pirajno et al (1998b this study)
Robinson RangeFormation
Unconformity
Unconformity
Johnson CairnFormation
NOTE New or redefined units (Occhipinti et al 1997)
(Finlayson and BubbleWell Members)
ARCHAEAN BASEMENT
FMP409a
3
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
drillcore (1100 m) and several visits to prospects andoperating mines considerably enhanced our knowledge ofthe geology of the area Most of the mapped areas werealso included in a regional regolith geochemical samplingprogram covering the PEAK HILL ROBINSON RANGE andGLENGARRY 1250 000 sheets (Subramanya et al 1995Bradley et al 1997 Crawford et al 1996)
Interim accounts of the structural and stratigraphicrelations of the BryahndashPadbury and Yerrida Basins havebeen reported by Pirajno et al (1995ab 1996) andOcchipinti et al (1997) Pirajno (1996) and Pirajno et al(1995a 1998b) discussed possible models for the tectonicevolution of the BryahndashPadbury and Yerrida Basins Thestructure and metamorphism of the BryahndashPadbury Basinhave been described by Occhipinti et al (1998abc)whereas details of mineral potential production andore deposit geology can be found in Pirajno andOcchipinti (1995) and Pirajno and Preston (1998)Published 1100 000 geological maps and accompanyingExplanatory Notes that wholly or partly cover the BryahndashPadbury Basin comprise BRYAH (Pirajno and Occhipinti1998) GLENGARRY (Pirajno et al 1998a) MILGUN (Swagerand Myers 1999) PADBURY (Occhipinti et al 1998a)DOOLGUNNA (Adamides 1998) and MARYMIA (Bagas1998) The southern portion of the JAMINDI 1100 000 mapsheet containing rocks of the Bryah Group was alsomapped The layout of these map sheets in relation to theBryahndashPadbury Basin and adjacent tectonic units is shownin Figure 2 The geology of the Bryah and Padbury Basinsis presented in Plate 1
Regional tectonic settingThe Bryah and Padbury Basins are situated along thenorthern margin of the Archaean Yilgarn Craton and arepart of the Capricorn Orogen (Fig 2 inset of Plate 1)The Capricorn Orogen also includes the Ashburton Basin
and the Gascoyne Complex and can be traced for morethan 1000 km with northwesterly to westerly trendsforming a broad belt of deformed low-grade volcano-sedimentary high-grade metamorphic and granitoidrocks
The Capricorn Orogeny resulted from the collisionbetween the Pilbara and Yilgarn Cratons at c 1800 Maand involved the closure of an intervening oceanformation of a back-arc basin and the possible accretionof microcontinental fragments (Myers 1993 Myers et al1996 Tyler et al 1998) Prior to the Capricorn Orogenythe c 2000 Ma Glenburgh Orogeny (Occhipinti et al1999) resulted in the accretion of the Glenburgh terraneonto the Yilgarn Craton The convergence between thePilbara and Yilgarn Cratons was essentially oblique andresulted in the development of easterly trending strike-slipmovements which included regional sinistral faults TheCapricorn Orogeny also affected other tectonic units suchas the Archaean Narryer Terrane Marymia Inlier SylvaniaInlier and parts of the Hamersley Basin (Tyler andThorne 1990 Myers et al 1996 Tyler et al 1998)
The Palaeoproterozoic volcano-sedimentary andsedimentary successions of the Bryah and Padbury Basinsare unconformable on the northern margin of the YilgarnCraton whereas to the north they are either unconform-ably overlain by or in faulted contact with rocksof the Bangemall Basin and the Archaean graniticrocks of the Marymia Inlier The Marymia Inlier iseconomically important because it hosts a number of golddeposits including the Peak Hill deposit (AMG 672190E7163150N) on the southwestern tip of the inlier (seeMineralization)
Localities are specified by the Australian Map Grid (AMG) system AMGcoordinates (eastings and northings) of localities discussed in the text arelisted in Appendix 1
Table 1 Stratigraphy of the Bryah and Padbury Groups
Group Age Formation Rock type(Ma)
Padbury Group Millidie Creek sericitic siltstone chloritic siltstone banded iron-formation(peripheral foreland basin) dolomitic arenite
Robinson Range ferruginous shale banded iron-formation
ltc 2000 Wilthorpe quartz-pebble conglomerate(Beatty Park and (siltstonendashwacke and polymictic conglomerate respectively)Heines Members)
Labouchere turbidite sequence (quartz wacke siltstone)
unconformable contact mdash tectonized in many places
Bryah Group (rift basin) Horseshoe banded iron-formation wacke shale
ltc 2000 Ravelstone quartzndashlithic wacke
Narracoota maficndashultramafic volcanic rocks and intercalated sedimentary rocks
Karalundi conglomerate quartz wacke
faulted contact
Yerrida Group (sag and rift basin) c 2174
SOURCE Modified after Pirajno et al (1996)
4
Pirajno et al
Geology stratigraphy andgeochronology
The BryahndashPadbury Basin contains the Bryah andPadbury Groups and the Peak Hill Schist The stratigraphyfor the Bryah and Padbury Groups is summarized in
Figure 1 and Table 1 where a comparison with previousGSWA work is also provided The Peak Hill Schist is aseparate tectono-stratigraphic unit that is discussed herewith the Marymia Inlier as basement to the Bryah GroupDetailed descriptions of the various formations and theircontact relationships are presented in Occhipinti et al(1997) Martin (1998) Adamides (1998) Pirajno and
Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins showing 1100 000 map sheet boundariesInset shows the position of the basins in relation to the Capricorn Orogen
MARYMIAINLIER
GOODININLIER
Goodin
Fault
Fault
Killara
Narracoota
30 km
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
FMP375
117deg
30
118deg
30
26deg00
25deg00
Murchison
FaultMorris
Earaheedy Group
Padbury Group
Yerrida Group
Archaean granitendashgreenstonebasement
Bangemall Group
Bryah Group
Proterozoic granites
Fault
Moorarie Padbury
MilgunMarquis
FaultCooinbar
NarryerTerrane
Murchison
Terrane
Kerba Fault
119deg
30
Gabanintha Yanganoo
MooloogoolGlengarry
Bryah Doolgunna
Jamindi Three Rivers
010300
BRYAH-PADBURY
BASINS
PROTEROZOIC
5
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Occhipinti (1998) Pirajno et al (1998b) Occhipinti et al(1998c) and Swager and Myers (1999)
In this section the geology field relations stratigraphyand geochronological constraints of the Peak Hill SchistMarymia Inlier and the formations that make up the Bryahand Padbury Groups are discussed
Peak Hill Schist and MarymiaInlierThe Peak Hill Schist (formerly called the lsquoPeak HillMetamorphic Suitersquo Gee 1987) is exposed in the lsquoPeakHill Domersquo or anticline and constitutes a tectonic unitrepresenting the southwestern tip of the Marymia Inlier(Fig 2 Thornett 1995) The Peak Hill Schist iscontinuous with the Marymia Inlier and Thornett (1995)suggested that the lsquoPeak Hill Domersquo represents thedeformed southwestern end of the Marymia Inlier Fieldobservations and petrographic and aeromagnetic datasupport this view The boundary between the Peak HillSchist and granitic rocks of the Marymia Inlier is a zoneof intense deformation and metamorphism characterizedby tectonic interleaving and duplexing Towards thenortheast the intensity of the Capricorn Orogenydeformation in the Marymia Inlier granites decreases toareas where they are undeformed The contacts betweenthe Peak Hill Schist and rocks of the Bryah Group arefaulted (probably thrusted) and tectonically interleaved inplaces
Rocks of the Peak Hill Schist include phyllonitequartzndashmuscovite schist calc-silicate schist sericite(ndashquartz) schist and quartzndashmuscovitendashbiotitendashchloriteschist locally with rotated alkali feldspar porphyroblasts(Fig 3) and minor metabasite These units have beenvariously deformed and contain a range of mylonitictextures The mylonitic fabric of these rocks is revealedby SndashC surfaces and lines of lsquomica fishrsquo (Lister and Snoke1984) in a dominantly and variably recrystallized quartz-rich matrix (Figs 4 and 5) A few discrete mylonitic units
Figure 3 Orthoclase porphyroblast with curved inclusiontrails in quartzndashmuscovite schist of the Peak HillSchist crossed polars
Figure 4 Partially recrystallized mylonite (Crispin Mylonite)from the Peak Hill Schist This sample is from amylonitic quartzndashbiotitendashalbite schist from the MineSequence in which the biotite defines C planesThe S planes were obliterated by recrystallizationto a blastomylonite crossed polars
Figure 5 Peak Hill Schist mylonite The C surfaces havesurvived recrystallization and now form thin micatrails crossed polars
form arcuate zones interpreted as early possibly thrustfault zones (see Structure) One of these units is the PeakHill Mylonite (Pirajno and Occhipinti 1998) which is arefolded quartz blastomylonite and quartz mylonite lenswithin quartzndashmuscovite schist The Peak Hill Mylonite(Figs 6 and 7) is an important unit because it is spatiallyassociated with gold mineralization (Peak Hill and MountPleasant deposits) Other less conspicuous quartzmylonite lenses are common within the Peak Hill Schistand were previously mapped as cherts or banded cherts(Windh 1992) Another important unit is the CrispinMylonite (Pirajno and Occhipinti 1998) which lies in thesouthern part of the Peak Hill Schist between sericiteschist and quartzndashmuscovite schist The Crispin Mylonitereferred to by Gee (1987) as the lsquoCrispin Conglomeratersquois characterized by square to rounded quartz arenite clastsup to 60 cm long in a sericite-rich matrix On the basisof field and petrographic observations it is concluded
6
Pirajno et al
here that this unit is not a conglomerate but a mylonite(Pirajno and Occhipinti 1998) Mylonites that resembleconglomerates (pseudo- or tectonic conglomerates) havebeen reported by Peters (1993) and Raymond (1984ab)
The Marymia Inlier (Windh 1992 lsquoMarymia Domersquoof Gee 1987) represents a fragment of northeasterlytrending Archaean granitendashgreenstone basement Rocksof the Marymia Inlier are mainly granitic but also includesmall enclaves of calc-silicate rock orthoamphibolite andminor metamorphosed banded iron-formation (BIF) ThePeak Hill Schist is also tentatively placed within theMarymia Inlier The granitic rocks are locally stronglyfoliated to gneiss or display strong cataclastic fabricsGranitic rocks include both fine-grained (aplitic) andcoarse-grained porphyritic phases Some outcropspreviously mapped as granite by Gee (1987) have beenincluded in the Peak Hill Schist The granitic rocks of theMarymia Inlier are monzogranite in the east and showincreasing cataclastic deformation towards the southwest(Pirajno and Occhipinti 1998 Bagas 1998)
Bryah GroupThe Bryah Group is divided into four formations theKaralundi Narracoota Ravelstone and HorseshoeFormations (Figs 1 and 2 Table 1) The basal unit of theBryah Group is the Karalundi Formation which is infaulted contact with the Doolgunna Formation of theYerrida Group along the Goodin Fault The KaralundiFormation predominantly consists of quartz conglomeratequartz arenite lithic wacke and shale The NarracootaFormation (parts of which were previously known aslsquoNarracoota Volcanicsrsquo Gee and Grey 1993) is thedominant lithology in the Bryah Basin and consists oftholeiitic extrusive and intrusive rocks and subordinateultramafic units intercalated with minor jasperoidal chertunits and clastic sedimentary rocks The NarracootaFormation is disconformably overlain by and locallyinterfingers with the Ravelstone Formation TheRavelstone Formation comprises a succession of lithic andquartz wacke shale and siltstone that was deposited byturbidity currents This formation is in turn conformablyoverlain by the Horseshoe Formation comprising quartzwacke manganiferous shale and banded iron-formation
The age of the Bryah Group is poorly constrainedbetween c 2000 and 1800 Ma Detrital zircons ofuncertain provenance in the Ravelstone Formation (upperBryah Group) provide a maximum age of 2014 plusmn 22 Ma(Nelson 1997) The Bryah Group must be older than theunconformably overlying Mount Leake Formation (outlierof the Earaheedy Group) which has a UndashPb (detritalzircon) maximum age of 1785 plusmn 11 Ma (Nelson 1997)The PbndashPb isochron ages obtained from pyrite from themesothermal Mikhaburra gold deposit (174 Ga Pirajnoand Occhipinti 1998) and from inferred syngenetic pyritefrom the Narracoota Formation (1920 plusmn 35 Ma Windh1992) probably represent mineralizing events in the BryahBasin rather than the depositional age of the BryahGroup
Karalundi Formation
The Karalundi Formation forms the base of the BryahGroup outcropping in a northeasterly trending belt alongthe southeastern margin of the Bryah Basin (Plate 1)Rocks of the Karalundi Formation are estimated to reacha thickness of approximately 2500 m In the southeastalong the Great Northern Highway Karalundi Formationrocks are in faulted contact with the Doolgunna Formation(Yerrida Group) On the southeastern side of the Peak HillSchist and in faulted contact with it the KaralundiFormation outcrops 35 km east of the Wilgeena mine Inthe south the Karalundi Formation is intercalated withmafic volcaniclastic rocks of the Narracoota Formation
The Karalundi Formation is characterized by immatureclastic (mainly quartzndashlithic wacke and conglomerate)units containing angular quartz and lithic fragments setin a sericitendashclay-rich matrix Other rock types includesiltstone calcareous siltstone cross-bedded areniteferruginous arenite litharenite minor dolomite andpurple green and black shale The Karalundi Formationalso contains pods of hematitic jasperoidal chert (see
Figure 6 Outcrop of quartz mylonite Peak Hill Schist Notethe flaggy nature of this rock and its steep dip
Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating atypical mylonitic fabric and SndashC planes (C planesare horizontal S planes trend from upper right tolower left between the C planes) crossed polars
7
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
below) which were interpreted by Gee (1979 1987) asfumarolic pipes
On DOOLGUNNA quartz arenite and conglomerate unitsare present within a dominantly hematitic shaly successionthat was interpreted by Adamides (1998) as a deep-waterlateral facies of the Bryah rift succession This successionalso contains olistoliths (exotic blocks) whose origin isnot clear Adamides (1998) suggested that they might havebeen derived from units of the Juderina Formation as aresult of inversion of the adjacent Yerrida Basin and upliftof the Goodin Inlier
Narracoota Formation
Rocks of the Narracoota Formation constitute a majorlithotype of the Bryah Group They form the bulk of thegroup with a thickness estimated at about 6 km (Pirajnoand Occhipinti 1998) and extend for more than 180 kmeast to west across the Bryah Basin The NarracootaFormation conformably overlies and locally interfingerswith the Karalundi Formation and also interfingers withand is in disconformable contact with the base of theoverlying Ravelstone Formation Contacts between theNarracoota Formation and Padbury Group are tectonic Inthe north regional structural relationships suggest that theNarracoota Formation is also in tectonic contact with theHorseshoe Formation Gravity modelling indicates that theNarracoota Formation forms the floor of the central partsof the Bryah Basin (Pirajno and Occhipinti 1998)
Rocks of the Narracoota Formation are affected bysea-floor metasomatism and regional prograde andretrograde metamorphism (see Structure) On the basisof field observations texture geochemistry and petrologyrocks of the Narracoota Formation can be subdivided intometamorphosed peridotitic and high-Mg metabasaltbasaltic hyaloclastite pyroclastic rocks intrusive rocksand mafic and ultramafic schist Collectively thesesubdivisions are referred to as metabasites Mafic andultramafic schists are characterized by a pervasiveschistosity but the distinction between mafic andultramafic is subtle and most clearly demonstrated usinggeochemistry In the area 2 km northeast of the Ravelstonemanganese opencuts a texture described by Hynes andGee (1986) as polygonal jointing has been observed in themetabasalt and appears to be a well-developed pencilcleavage High-Mg basalts are associated with peridotiticunits Intrusive rocks cover a range of types frompyroxenite to gabbroic rocks and dykes Metabasaltichyaloclastites are lava flows that interacted with seawaterand have a distinct spilitic character Volcaniclastic rocksincluding vent breccias are commonly present in bothbasaltic hyaloclastite and mafic schist
Typically the metabasite rocks of the NarracootaFormation contain no or very few feldspar phenocrystsOther authors have suggested that the presence ofmedium-grained embayed quartz crystals indicates theproximity of felsic volcanic rocks (Hill and Cranney1990 Windh 1992) Felsic volcanic rocks are associatedwith the upper part of the Narracoota Formation at andaround the Horseshoe Lights copperndashgold mine onJAMINDI 29 km east of the Fortnum mine on MILGUN
Fine-grained grey to black metamorphosed shale andslate are present in places as lenses of interflowsedimentary rocks within the volcanic succession Wheremore deformed and metamorphosed these slates are finelylaminated biotitendashchlorite schists South of the RobinsonRange small lenses of sedimentary rock (lithic wacke andshale) are intercalated with the volcanic rocks of theNarracoota Formation In places pods and lenses ofjasperoidal chert are associated with the volcanic rocks
Peridotitic and high-Mg basalt association
Massive layered high-Mg basaltic rocks (possibly lavaflows shown on Plate 1 as Anu) are preserved inprominent hills between Top Dimble Well and DespairBore on MILGUN Hynes and Gee (1986) described thissequence as komatiitic basalt with up to 20 MgOUnequivocal pillow structures as mentioned by Hynes andGee (1986) were not observed The rocks are meta-morphosed but their protoliths include olivine cumulate(peridotite) high-Mg basalt with plumose and harrisitictextures and medium-grained basalt Layering is mainlydefined by massive olivine cumulate layers up to 20 mthick and plumose-textured basalt layers up to 5 m thickLocally large sheaves of skeletal amphibole (afterpyroxene) are arranged at approximately right angles tothe layering and resemble harrisitic textures (Fig 8a) Thehigh-Mg basalt units are characterized by well-developedlsquospinifexrsquo-like textures with acicular tremolitendashactinoliteafter pyroxene and up to 30 interstitial plagioclase(replaced by epidote or zoisite) The high-Mg basalt isinterlayered with medium-grained basalt of similarmineralogy and composition with 8ndash9 MgO Thewhole-rock geochemistry of these rocks is discussed inGeochemistry of the Narracoota Formation
Peridotite units commonly consist of 70ndash80 fine- tomedium-grained olivine replaced by tremolite(ndashtalc)skeletal amphiboles after pyroxene and 20ndash30 fine-grained matrix of plumose-textured amphibole High-Mgbasalt contains up to 30 locally glomeroporphyriticolivine (now tremolite) lesser amounts of acicularpyroxene in a 60ndash70 amphibole plumose-texturedmatrix and 15 MgO One particular example contains35 olivine (only partly altered to talc) skeletal(lsquoswallow-tailrsquo) fresh orthopyroxene and lesser amountsof acicular skeletal amphibole prisms possibly afterclinopyroxene (Fig 8b)
Intrusive rocks and layered intrusions
A metadolerite sheeted dyke complex (shown as And onPlate 1) outcrops north of the Robinson Syncline Theserocks are associated with deformed pillow metabasalt andtend to be internally undeformed but commonly formelongate bodies subparallel to the S2 foliation Theycontain diopside amphibole epidote and minor olivine
Lenses of cumulate-textured units represented bypyroxenite or peridotite and gabbroic rocks are locallyintercalated with the mafic and ultramafic schist Alensoidal outcrop of metapyroxenite is present nearDurack Well Gabbroic rocks are common betweenTrillbar Homestead and Friday Pool on MOORARIE
8
Pirajno et al
(Occhipinti and Myers 1999) These rocks have beenmetamorphosed and folded but are largely undeformedinternally The gabbroic rocks are surrounded by higherstrain zones consisting of tremolitendashactinolite schist
The Trillbar Complex (shown as Ant on Plate 1) is a30 km long by 25 km wide layered maficndashultramaficintrusion in the westernmost part of the Bryah Basin Thecomplex consists of rhythmically layered mafic andultramafic rocks with the layering oriented at a low angleto the regional foliation (Occhipinti and Myers 1999)Rock types include rhythmically layered gabbromelanogabbro leucogabbro pyroxenite and peridotiteThese rocks are metamorphosed to greenschist facies butthe original igneous textures are locally well preservedThe Trillbar Complex rocks contain assemblages ofserpentinendashtremolitendashtalc tremolitendashtalcndashmagnetitetremolitendashactinolite and actinolitendashfeldspar Cumulaterocks include olivinendashpyroxene pseudomorphed bytremolite and sphene West of the Trillbar Homestead arelayers of metamorphosed pyroxenite and peridotite inwhich the original mineral phases are totally replaced by
tremolite talc magnetite and chlorite The TrillbarComplex is interpreted here as representing a remnant ofLayer 3 (layered gabbroic rocks) of an oceanic crustsuccession (Burke et al 1981) If this is correct thenprogressively lower levels of the Narracoota Formation areexposed from east to west and this is supported by thewidespread occurrence of volcaniclastic units in thecentral and eastern parts of the Bryah Basin
Mafic and ultramafic schist
Maficndashultramafic schist consists of actinolite(ndashchloritendashclinozoisite) schist and chlorite schist (shown as Anu andAn on Plate 1) In the south-central part of BRYAH schistoutcrops form an arcuate band (possibly an antiformstructure Gee 1987) south of and following the trendsof the Robinson Syncline and the southern limbs of theFraser Synclinorium (see Structure) North of thesestructures sparse outcrops of mafic schist are present justsouth and north of the Peak Hill Schist Within the schistare pods of less deformed or internally undeformedmetabasites in which pillow structures are locally wellpreserved Overall this large band forms a majoranastomosing sheared domain (Pirajno et al 1995b) Thedominant schistosity strikes approximately easterly orwest-northwesterly and dips steeply to the north andsouth A number of quartz veins within this shear domainalso strike easterly Maficndashultramafic schist was formedas a result of deformation and metasomatism of metabasiterocks along D2 shear zones (see Structure) In most casesall original volcanic textures are obliterated although inplaces round or elongate chlorite aggregates areinterpreted as original amygdales or fine pyroclasts
To the northwest on MILGUN the mafic volcanicschist occurrences are in faulted or sheared contactwith rocks of the Labouchere Wilthorpe and RobinsonRange Formations Hill and Cranney (1990) documenteda sequence of ultramafic to mafic schists with orwithout jasperoidal chert lenses overlain by fragmentalvolcaniclastic rocks fine-grained siltstone and felsic(intermediate and dacitic) crystal tuffs These are in turnoverlain by the Ravelstone and Horseshoe Formations
Mineral constituents of the mafic schist are actinolitechlorite and clinozoisite with minor calcite pumpellyitesericite titanite quartz and relict albite Ultramafic schisthas a simpler and commonly almost monomineralicmineralogy consisting of actinolitendashtremolite withretrogressed patches of pale-green chlorite In zones ofmore intense deformation chlorite- or epidote-dominatedassemblages are present (chlorite schist and epidositerespectively) These minerals developed due to strongmagnesium and calcium metasomatism probably duringcirculation of H2OndashCO2 fluids (Pirajno et al 1995b) Fluidinfiltration caused the breakdown of tremolite andclinozoisite to produce chlorite calcite and silica Thesilica thus liberated was then channelled through shearzones resulting in silicification and quartz veins (Pirajnoet al 1995b) An example of this can be seen in abreakaway 13 km east of the Wembley gold mine wheremafic schist and deformed pillow lavas display chloritealteration and pervasive silicification near and along awest-northwesterly trending shear zone In high-strain
Figure 8 Maficndashultramafic volcanic rocks of the NarracootaFormation (Dimble Belt) a) Komatiitic pyroxenitewith skeletal amphibole prisms after a quench-textured pyroxene matrix b) Peridotite with olivinepartly altered to talc around the edges and pyroxenein a fine-grained tremolite matrix both in planepolarized light
9
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
zones a new fabric is defined by the alignment ofamphibole prisms elongate epidote and quartz Theseschists are commonly characterized by well-developedlsquopencil cleavagersquo as a result of two intersecting planarfabrics
Metabasite rocks commonly show relict igneoustextures of prismatic plagioclase and interstitial amphiboleand more abundant unoriented prisms or acicular grainsof fine- to medium-grained amphibole Massive sheaf-liketextures of acicular amphibole are interpreted as primaryigneous textures A few plagioclase phenocrysts (3ndash5 mm)are preserved The amphibole is colourless to pale-greenpleochroic actinolite (or actinolitendashtremolite) plagioclaseis albite and commonly pseudomorphed by clinozoisitendashepidote or sericitized in zones of alteration Minorconstituents include chlorite quartz and sphenendashleucoxene with local zones of massive epidote(ndashcarbonate)
A schistose metabasite 5 to 8 km northeast of the PeakHill opencut contains actinolite arfvedsonite calcitediopside epidote and quartz The alignment of actinoliteand arfvedsonite defines the S2 schistosity and thereforeboth these minerals were formed during prendashsyn-D2 (seeStructure) The presence of the arfvedsonite (sodicamphibole) suggests either an original sodium-rich rockor later sodic metasomatism during or prior to D2
Metabasaltic hyaloclastite
Metabasaltic hyaloclastites form a prominent outcrop areapartly covered by ferricrete and colluvium south of theMurchison River These rocks are separated from themafic and ultramafic schist by the Murchison Fault(Plate 1) and probably represent a substantial thicknessof mafic lavas and hypabyssal material Hynes and Gee(1986) and Gee (1987) estimated a total thickness rangingfrom 4 to 6 km On the northern part of the GLENGARRY
1100 000 sheet the metabasalts are intercalated withsedimentary rocks of the Karalundi Formation (Pirajnoet al 1998a) These metabasaltic rocks are interpreted ashyaloclastites mdash a term that denotes fragmentation dueto quenching (Fig 9) of lavas flowing in water or eruptingunder an ice sheet This results in non-explosive fracturingand disintegration of the quenched lavas (McPhie et al1993 Fischer and Schmincke 1984)
The metabasaltic hyaloclastites are undeformeddominantly of mafic composition and have a spiliticcharacter Spilites are basaltic rocks that become alteredthrough metasomatic exchange with seawater therebyincreasing their sodium content The hyaloclastites havenormative albite from 13 to 23 wt and Na2O contentsof up to 6 wt
The metabasaltic hyaloclastites are commonly aphyricand composed mainly of acicular crystals of actinolitearranged in sheaves together with epidote minorcarbonate prehnite quartz and titanite in a fine-grainedgroundmass of albite microlites chlorite and epidoteCoarse-grained equivalents (clinopyroxene and plagioclaselaths) display ophitic to subophitic textures North of theMikhaburra (Holdens Find) gold deposit a small shaft has
Figure 9 Basaltic hyaloclastite of the Narracoota Formationshowing cuneiform devitrified shards now replacedby silica and sericite plane polarized light
exposed a vesicular rock containing serpentinized olivinecrystals set in a very fine grained altered matrix ofactinolite probably replacing pyroxenes
These metabasalts are commonly unfoliated andmassive with a characteristic brecciated or jigsaw-fittexture outlined by epidote carbonate prehnite and quartzveining along cooling joints In places these cooling jointsmay form pseudo-pillow structures and may be mistakenfor pillow lavas (Hynes and Gee 1986) Microscalejigsaw-fit textures are also seen
Felsic schist
Felsic schists which host sulfide mineralization (seeMineralization) at the Horseshoe Lights copperndashgolddeposit are present in the northern part of the BryahBasin Stratigraphically the felsic schist are at the top ofmafic metavolcanic rocks of the Narracoota Formation andoverlain by rocks of the Ravelstone Formation (seebelow) which contain chert lenses and layers close to thiscontact The felsic rocks are offset by a northeasterlytrending fault near the mine area and extend for about75 km in a southeasterly direction where they are offsetagain by a northeasterly trending fault However they donot reappear on the other side of the fault where the maficmetavolcanic rocks are in contact with the clasticsedimentary rocks of the Ravelstone Formation
Felsic schist includes quartzndashsericite schist sericiteschist and chlorite schist all showing varying degrees ofdeformation and development of mylonite Examinationof drillcore from the Horseshoe Lights mine revealedstructures reminiscent of felsic volcaniclastic rocks suchas collapsed pumice fragments Quartzndashsericite andsericite schist are composed of quartz and feldsparporphyroclasts partially replaced by quartz and sericitecarbonate or chlorite and wrapped around by granoblasticaggregates of quartz and sericite these aggregates aretraversed by anastomosing bands of sericite Tourmalineis present in places In one example sericite schistcontains elliptical opaque fragments suggestive ofcollapsed pumice Chlorite schist is composed of chlorite
10
Pirajno et al
and granular quartz with the chlorite forming distinctmonomineralic laminae X-ray diffraction analyses ofaltered schist indicate the presence of quartz kaolinpyrite hematite goethite and dioctahedral sodianmuscovite or potassian paragonite
Based on petrographic and core examinations thefelsic schist precursor rocks may have been quartzndashfeldspar porphyry and felsic volcaniclastic rocks
Volcaniclastic rocks
Mafic volcaniclastic rocks have well-preserved eutaxiticor fragmental textures despite intensive foliation (Fig 10)In the Fortnum mine area mafic fragmental rocks andfine-grained mafic volcaniclastic rocks are spatiallyassociated with jasperoidal chert pods The fragmentalrocks are strongly schistose with flattened and stretched
fragments of chlorite schist quartzndashchlorite schist withplagioclase phenocrysts quartzndashfeldsparndashamphibole rock(metabasalt) medium-grained plagioclase grains andmore rarely quartz crystals in a fine-grained matrix Finelylayered mafic schists consist of an amphibolendashplagioclasematrix with scattered prismatic to ovoid plagioclasephenocrysts and quartz lsquoeyesrsquo Amphibole accessorybiotite and sericite lenses have a strong preferredorientation suggesting that recrystallization in these fine-grained rocks has destroyed any volcaniclastic texture
Volcanic breccia is present in at least three localitiesThe most important of these is 5 km north of the oldCashman mine in the southern part of BRYAH (seeMineralization) Outcrops of volcanic breccia are alsopresent at the Cashman mine and 3 km west of the PeakHill ndash Fortnum road junction The nature of these angularclast-supported poorly sorted blocks of mafic volcanicmaterial suggest that they are vent breccias Volcanicbreccia was intersected throughout 455 m of core indrillhole BD1 (BRYAH AMG 380380) drilled by NorthExploration Ltd in 1993 (McDonald 1994) This coreintersection is briefly described below
Drillhole BD1 was drilled to a depth of 520 m at aninclination of 70deg towards the south and intersected claysand gravels to a depth of 65 m followed by weatheredmafic volcanic breccias to 96 m Below this depth to theend of the hole at 520 m spectacular fresh proximal vent-facies material consisting of angular blocks and clasts ofbasaltic lava tuff and chert were intersected (Fig 11)Crude bedding is present locally as are thin layers oflaminated or cross-laminated cherty material The holebottomed in cross-laminated chert which is interpreted aspyroclastic surge and tuff deposits The basaltic rocksinclude fine-grained vesicular basalt and feldspar-phyricand augite-phyric basalts The porphyritic varieties arecharacterized by a microlite-rich feldspar matrixclinopyroxene granules interstitial glass and chlorite andopaque minerals (titanite or rutile) The feldspar
Figure 10 Mafic volcaniclastic rock of the NarracootaFormation showing relict glass shard (in centre)plane polarized light
Figure 11 Volcanic breccia of the Narracoota Formation intersected in diamond drillhole BD1 Clasts arepredominantly of basaltic rocks the matrix exhibits albitic alteration Width of the core trays is 040 m
11
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
phenocrysts are selectively altered to sericite whereas theaugite phenocrysts are fresh and exhibit distinct zoningVesicles are infilled (from rim to core) by albite epidotechlorite and calcite Minor sulfide specks mainlychalcopyrite may be present in the vesicular basalt Tuffscharacterized by fluidization (due to degassing) andeutaxitic textures consist of glass shards and crystal andlithic fragments set in a devitrified and variably alteredglassy matrix Alteration phases are mainly chloritecalcite quartz and albite Chalcopyrite blebs are presentin places Hydraulic fracturing and veins of calciteprehnite quartz and chlorite are abundant One sectionbetween 200 and 360 m is characterized by albiticalteration (sodium metasomatism) which imparts a pinkto reddish colouration to veinlets and patches where thealbite is present
The fragmental mafic volcanic rocks in drillhole BD1are interpreted to represent a proximal vent-facies volcanicbreccia This vent-facies material coincides withprominent magnetic and Bouguer gravity anomalies(Pirajno et al 1995a) The magnetic anomaly which isrelated to the presence of magnetite in pyroxene basalthas a well-defined northeasterly trending elliptical shapeand could conceivably indicate the remnants of a majorvolcanic edifice Magnetic modelling suggests thepresence of two tabular bodies dipping 25deg to the north(Bui Dung 1999 pers comm) The gravity anomaly isat the centre of a large regional gravity high whichunderlies most of the area occupied by the NarracootaFormation (Pirajno and Occhipinti 1998)
Carbonated and silicified metavolcanic rocks
Carbonated and silicified maficndashultramafic rocksinterpreted as part of the Narracoota Formation outcropin the Horseshoe anticlinal block (Plate 1) These rocksare compositionally heterogeneous and both underlie andare intercalated with rocks of the Horseshoe FormationThis suggests that the interleaving is tectonic becauseelsewhere in the Bryah Group the Horseshoe Formationis not observed to be in direct contact with the NarracootaFormation (Occhipinti et al 1999)
Jasperoidal chert
Jasperoidal chert pods are present locally within theNarracoota Formation (Gee 1987 Hill and Cranney1990 Pirajno and Occhipinti 1998) but are commonlytoo small to be represented individually on geologicalmaps One of the largest pods outcrops 15 km due southof Ruby Duffer Well in the southern part of BRYAH Windh(1992) investigated the chert pods in some detailgeochemically discriminated them on the basis of theirNiCr ratios and distinguished jasperoidal syngeneticexhalative chert silicified volcanic or sedimentary rockssilicified shear zone rocks and surface silicificationSeveral of these chert pods such as those in theNarracoota Formation south of the Peak Hill Schist innorthern BRYAH are quartz mylonites mdash probably Windhrsquos(1992) silicified shear zone rocks A few may be chemicalprecipitates deposited by hot springs whereas others mayrepresent silicified fault zones
The cherty material is reddish to grey colouredmassive to banded and extensively veined by quartzThe chert consists of very fine grained recrystallizedquartz with equant to elongate polygonalndashgranoblastictextures locally with a crystallographic preferredorientation Minute opaque minerals locally includingmagnetite or pyrite define trails parallel to the quartzfoliation In the Yarlarweelor opencut (Fortnum mine)pebbles of these cherts in overlying mafic fragmentalrocks suggest that the cherts formed as exhalative horizonsrelated to volcanism Alternatively the jasperoids mayrepresent iron-rich silicification along major shear zonesIn the Yarlarweelor opencut the chert pods host epigeneticgold mineralization in and around quartz(ndashpyrite) veinsystems (Hill and Cranney 1990)
Geochemistry of the Narracoota Formation
Major trace and rare earth element (REE) whole-rockanalyses of samples of metabasite rocks of the NarracootaFormation collected during this study are included in thedigital dataset in the back pocket These data were usedto characterize the geochemistry of the volcanic rocks ofthe Narracoota Formation in an attempt to better definethe rock types and gain an insight into the nature of theparent magma(s) and tectonic setting Representativeanalyses of Narracoota Formation rocks are presented inTable 2
The Narracoota metabasite rocks are commonly oftholeiitic composition with mixed mid-ocean ridge basalt(MORB) ndash oceanic island and continental geochemicalsignatures They span the range from high-Mg basalt tokomatiite and peridotitic komatiite or peridotite (possiblysubvolcanic cumulates) Common characteristics includehigh MgO high Ni and Cr moderate to low REEabundances and nearly flat chondrite-normalized REEpatterns with weak Eu anomalies possibly reflectingdepleted asthenospheric mantle sources (Pirajno and Davy1996 Pirajno et al 1996 Pirajno and Occhipinti 1998Occhipinti et al 1998ac) There are subtle chemicaldifferences between the hyaloclastites and maficndashultramafic schists (Tables 3 and 4 see below)
Hynes and Gee (1986) and Pirajno and Davy (1996)reported on the petrochemistry and tectonic setting ofthe Narracoota Formation metabasite rocks Hynesand Gee (1986) concluded that they have fairlyuniform chemistry and are of MORB affinity although theoriginal mafic volcanic rocks may have been emplacedthrough the rifting of continental crust Pirajno and Davy(1996) proposed that the Narracoota Formation meta-volcanic rocks might have formed in a setting analogousto that of the present-day Gulf of California (Lonsdaleand Becker 1985) The origin of the NarracootaFormation metabasites is discussed in Tectonic model andconclusions
Classification based on chemistry
The total alkali ndash silica (TAS) and high-Mg plot(Le Maitre 1989) indicates that the bulk of the rocks ofthe Narracoota Formation range in composition fromkomatiitendashpicrite through basalt to basaltic andesite
12
Pirajno et al
Table 2 Representative chemical analyses of the Narracoota Formation
Rock _________________ Mafic schist _________________ _______ Hyaloclastite _______ _______ Ultramafic _______ ____ Trillbar __type schist ComplexSample 132788 132789 132790 133033 133050 112643 116485 104256 132791 139138 139139 135482 143538
Percent
SiO2 5424 4945 5277 463 4907 5187 5139 5011 4923 4723 4789 5137 4961TiO2 028 113 031 019 026 073 063 053 019 016 017 037 141Al2O3 1422 1172 1466 948 794 138 1512 1503 1043 765 867 1481 1391Fe2O3 248 345 184 661 635 224 296 278 146 396 201 232 561FeO 598 824 705 741 101 848 662 529 834 548 708 561 717MnO 017 019 018 025 198 02 016 014 018 012 015 016 022MgO 929 1243 1036 1517 778 1036 83 936 2063 2877 2678 869 656CaO 1106 1107 962 1451 2262 974 1144 1514 86 641 704 1068 1136Na2O 218 212 274 003 009 216 32 145 092 018 019 306 204K2O 007 008 046 001 284 036 01 011 002 003 001 006 022P2O5 003 013 002 003 007 007 006 005 001 001 001 003 011Total 10000 10001 10001 9999 10001 10001 9998 9999 10001 10000 10000 9716 9822
Mg 6687 6615 6795 6692 6736 6377 6142 6816 792 85 843 ndash ndash
Parts per million
Ag ndash ndash ndash ndash ndash 1 ndash 1 ndash ndash ndash ndash ndashAs 155 157 052 22551 13032 ndash ndash ndash ndash 832 ndash ndash ndashAu ndash ndash ndash ndash ndash 104 ndash ndash ndash ndash ndash ndash ndash
Ba 55 140 79 27 2 846 341 127 92 74 37 102 39 322Cd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash
Co 55 86 58 223 51 ndash ndash ndash 99 113 111 ndash ndash
Cr 509 1 201 686 2 574 72 489 364 283 1 836 2 530 3 146 593 82Cu 168 124 63 327 20 108 101 39 55 9 11 59 172Ga 10 16 10 8 9 12 12 13 8 6 6 12 19Hf ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 07 14Mo ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 08 26Nb ndash 63 ndash ndash 52 ndash ndash ndash ndash ndash ndash 1 9Ni 203 548 241 1 274 91 258 143 164 866 1 531 1 230 124 98Pb ndash 2 ndash ndash 7 ndash ndash ndash ndash ndash ndash 1 4Pd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashPt ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashRb 1 ndash 6 ndash 85 6 ndash 2 ndash 1 ndash 1 4Sb ndash ndash ndash ndash ndash 415 ndash 511 ndash ndash ndash ndash ndashSc 50 41 51 31 10 ndash ndash ndash 40 34 38 51 48Sr 64 149 64 54 100 163 82 188 23 23 7 61 279Ta ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashTh ndash 104 ndash ndash 717 ndash ndash ndash ndash ndash ndash ndash ndashU ndash ndash ndash 064 13 ndash ndash ndash ndash ndash ndash 08 14V 196 277 202 138 78 250 249 217 144 115 143 235 362W ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashY 13 18 12 8 16 17 14 11 8 6 7 17 24Zn 65 94 68 45 50 85 73 55 62 51 45 61 91Zr 13 68 15 17 50 51 47 38 7 7 8 20 86
La 089 936 043 054 1819 36 35 35 093 017 056 2 6Ce 218 2264 129 084 4445 9 83 83 153 042 082 2 15Pr 037 29 02 02 418 12 11 13 02 009 019 0 2Nd 166 1193 108 102 1511 57 51 57 102 047 079 5 12Sm 08 328 065 056 306 15 14 15 065 03 034 ndash ndashEu 042 13 032 028 223 09 07 08 029 011 011 ndash ndashGd 166 409 141 085 305 23 17 2 129 065 071 ndash ndashTb 04 069 031 018 04 04 04 04 029 014 016 ndash ndashDy 268 408 233 12 202 27 24 24 214 108 116 ndash ndashHo 071 087 057 028 037 05 05 05 053 027 03 ndash ndashEr 222 231 173 094 115 18 15 16 162 083 091 ndash ndashTm 039 033 027 016 017 02 02 02 027 014 015 ndash ndashYb 229 196 182 115 125 15 14 15 166 086 09 ndash ndashLu ndash ndash ndash 019 02 02 02 02 ndash 013 014 ndash ndash
13
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(Fig 12) A small number of samples plot in the boniniteand andesite fields All metabasites of the NarracootaFormation (ultramafic and mafic schists and basaltichyaloclastite) are of subalkaline tholeiitic affinity (Fig 13)They commonly have restricted silica contents rangingfrom 45 to 55 wt (Fig 12)
The metabasites are all quartz albite anorthitediopside hypersthene and magnetite normative Themafic schists are hypersthene normative with lowerMgO contents (lt15 wt) and magnesium numbers (Mgmdash defined as MgO(FeO + MgO)) ranging from 43 to 74(Table 3) Some mafic schists have no quartz and areolivine normative (5ndash6 and up to 20 in some maficschists) The ultramafic schist is hypersthene and olivinenormative with MgO contents ranging from 153 to227 wt and Mg ranging from 75 to 86 (Table 3) Themetabasaltic hyaloclastites are albite and clinopyroxenenormative and have MgO contents of lt10 wt and Mgof between 47 to 68 (Table 3)
Ultramafic schist mafic schist and metabasaltichyaloclastite can be distinguished in terms of their Cr Niand Ti abundances FeOMgO ratios (Tables 3 and 4Figs 14a and 14b) and chondrite-normalized REEpatterns The hyaloclastite rocks are depleted in Cr andNi and enriched in TiO2 relative to the maficndashultramaficrocks (Fig 14c)
The Jensen (1976) cationic plot is based on theproportion of Fe2++Fe3++Ti versus Al and Mg cationsrecalculated to 100 and is particularly useful fordiscriminating subalkaline and Mg-rich metamorphosedvolcanic rocks in which the alkali content may havebeen modified during deformation and metamorphism(Rollinson 1993) In the Jensen plot (Fig 15a) the
Narracoota Formation rocks span the range of compo-sitions from high-Mg tholeiite through to komatiite andperidotitic komatiite in a trend of increasing MgO
Chondrite-normalized rare-earth element diagramscommonly regarded as the most useful of the traceelement plots in the petrogenesis of igneous rocks areused to determine the possible nature and source of themelts Particularly important are the overall patterns fromlight to heavy rare earth elements (LREE to HREE) thenormalized abundance of Eu controlled by feldspar andthat of Ce controlled by seawater or hydrothermal fluidsFor the Narracoota Formation rocks chondrite-normalizedREE abundances (Figs 15b and 15c) are commonly low(lt1 to lt40 times chondrite) The mafic schist ischaracterized by a spread in LREE from depleted toenriched (Fig 15b) with individual patterns almostidentical to those of mid-ocean ridges (OrsquoNions et al1976 Schilling 1982) and the recent basaltic lavas ofIceland (Schilling et al 1982) More specifically theLREE-depleted patterns (western Bryah Basin) arestrikingly similar to those of the Lau Basin spreadingcentre in Fiji (Pearce et al 1995) whereas slightlydepleted to slightly enriched LREE patterns (eastern Bryah
Table 3 Magnesium numbers for the Narracoota and Killara Formations
Rock Formation Range of Mg Average Mg Standard deviationof Mg
Metabasaltic hyaloclastite Narracoota 4677 ndash 6816 5716 525Mafic schist Narracoota 4337 ndash 7409 5957 669Ultramafic schist Narracoota 7516 ndash 8560 8105 254Tholeiitic basalt Killara 3504 ndash 6603 5035 739
NOTE Mg Magnesium number defined as MgO(FeO +MgO)
Table 4 Selected geochemical parameters for the NarracootaFormation
Parameters Hyaloclastite Mafic schist Ultramafic(mean values) schist
(LaYb)N 144 1702 037TiO2 (wt) 086 068 019NiCr 043 039 042Al2O3TiO2 162 205 4668MgO (wt) 731 780 2119
35 45 55 650
1
2
3
4
foidite andesite
basalt
boninite
basalticandesite
MgOgt18 picrite
basanite
tephrite
MgOgt18 amp TiO lt1 komatiite
picrobasalt
FMP365 021199
22
2
2
2
2
MgOgt18 amp TiO gt1 meimechiteMgOgt8 amp TiO lt05
SiO (wt)
Na
O +
K O
(w
t)
Figure 12 Total alkali versus silica diagram (Le Maitre1989) for rocks of the Narracoota FormationNote that a small number of samples fall withinthe boninite field this however may be due tohydrothermal alteration
14
Pirajno et al
Basin) are comparable to those of seamounts reflectinga more enriched source The nearly flat patterns havenegative Eu anomalies reflecting the primitive nature ofthe rocks presence of olivine clinopyroxene andorthopyroxene and fractionation of feldspar from themelt The patterns of the Iceland basalts that are nearlyidentical to those of the mafic schist of the Bryah Groupwere explained by Schilling et al (1982) as due toadvection of asthenospheric mantle at a mid-ocean ridgeConsidering field relations and petrological andgeochemical data it is conceivable that the NarracootaFormation metatholeiites may have had a similar originChondrite-normalized REE abundances for the meta-basaltic hyaloclastite are very low (9 to 14 timeschondrite) slightly LREE-enriched and with a distinctpositive Eu anomaly (Fig 15c) reflecting the addition ofalbite due to seawater metasomatism
The overall REE abundances and patterns of maficschist and hyaloclastite are strikingly similar to192 ndash 184 Ga mafic rocks of the Flin Flon belt in theTrans-Hudson Orogen in Canada (Lucas et al 1996)Some of the mafic rocks of the Flin Flon belt have beeninterpreted to belong to tectono-stratigraphic assemblagesof ocean floor and ocean island affinity Also the Flin Flonocean island tholeiites have REE patterns similar to
Figure 13 Total alkali versus silica diagram (Le Maitre 1989)defining limits of alkaline and subalkaline basaltsshowing the predominantly subalkaline nature ofthe Narracoota Formation
20
16
12
8
4
0
Na
O +
KO
(w
t)
22
857565554535
SiO (wt)2 11999FMP367
Hyaloclastite
Mafic schist
Ultramafic schist
Subalkaline
Alkaline
Figure 14 Geochemical characteristics of the NarracootaFormation a) TiO2 versus FeOMgO ratios notethe slight TiO2 enrichment of metabasaltichyaloclastite compared to maficndashultramafic schistb) Cr versus FeOMgO ratios note the Cr enrichmentof maficndashultramafic schist compared to meta-basaltic hyaloclastite c) TiO2ndashNindashCr triangular plotshowing Ni and Cr enrichment of maficndashultramaficschist compared to metabasaltic hyaloclastite
3
2
1
0
TiO
(wt
)2
1 2FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
4000
3000
2000
1000
0
Cr
(ppm
)
1 2 3FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
TiO 1002
Ni Cr91199FMP368a
Hyaloclastite
Mafic schist
Ultramafic schist
a)
b)
c)
15
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Hawaiian tholeiites (Stern et al 1995) The inference fromthese comparisons is that submarine volcanoes may havebeen a component of the Narracoota Formation
Tectonic discriminant diagrams do not provide reliableinformation on the palaeotectonic environment withinwhich igneous rocks were emplaced (Duncan 1987 Wangand Glover 1992) Nevertheless if there is petrologicalevidence that the rocks have not undergone extensivecrystal fractionation and the overall geological context is
taken into account selected discriminant diagrams can beused to estimate palaeotectonic settings With the aboveconsiderations in mind and remembering that the rocksin question have a subalkaline chemistry the FeO(tot)ndashMgOndashAl2O3 plot of Pearce et al (1977) is deemedappropriate (Fig 15d) The FeO(tot)ndashMgOndashAl2O3 plot hasbeen used successfully in geologically well constrainedareas (Breitkopf and Maiden 1988) The FeO(tot)ndashMgOndashAl2O3 plot suggests that the Narracoota Formationvolcanic rocks were formed in tectonic environments of
a)
c)
b)
d)
MgO
TA
TDTR
CR CDCA
HFTBK
PKCB
HMT
Sam
ple
chon
drite
100
10
2La Pr Eu Tb Ho Tm Lu
Ce Nd Sm Gd Dy Er Yb
La Pr Eu Tb Ho Tm LuCe Nd Sm Gd Dy Er Yb
Sam
ple
chon
drite
100
10
1
6
FeO
MgO
221199
Al O32
FeO + TiO2
Al O32
FMP154
Mafic and ultramafic schist
Metsabasltic hyaloclastite(tot)
Figure 15 Geochemical discriminant plots for Narracoota Formation rocks a) Jensen (1976) cationic plot showingrange of compositions from high-Mg tholeiite (HMT) through high-Fe tholeiite (HFT) basaltic komatiite(BK) peridotitic komatiite (PK) tholeiitic andesite (TA) tholeiitic dacite (TD) calc-alkaline basalt (CB)and calc-alkaline andesite (CA) b) Chondrite-normalized rare-earth element plot of mafic (HREE-enriched) and ultramafic (HREE-depleted) schist (normalizing factors after Sun 1982) c) Chondrite-normalized rare-earth element plot of metabasaltic hyaloclastite (normalizing factors after Sun 1982) d)Triangular discriminant plot (Pearce et al 1977) showing the tectonic environment of the NarracootaFormation Tectonic fields are as follows 1) spreading-centre island 2) orogenic 3) ocean ridge andfloor 4) ocean island and 5) continental
16
Pirajno et al
MORB ndash oceanic island to continental affinity (Fig 15d)This diagram however has limitations if the rocks havebeen subjected to ocean-floor metamorphism A moreuseful plot is the TiO2ndashFeO(tot)ndashMgO plot which was usedby Breitkopf and Maiden (1988) in their study of theNeoproterozoic Matchless Amphibolite Belt of theDamara Orogen in Namibia The TiO2ndash FeO(tot)ndashMgO plotsupports the gradation from MORB towards continentalflood basalt because the hyaloclastite rocks plot closer tothe continental field than do the mafic schist (Fig 16) Thisfeature together with other considerations such as Mgand geological and petrological constraints indicate thatthe hyaloclastite was erupted on a continental rift marginThis has important implications for the tectonic evolutionof the BryahndashPadbury Basin as explained in Tectonicmodel and conclusions
Ravelstone Formation
The Ravelstone Formation is poorly exposed in scatteredlow outcrops over a wide area in the northern and centralparts of the Bryah Basin Rocks of the RavelstoneFormation were previously considered by MacLeod(1970) and Gee (1979 1987) to belong to the lsquoThadunaGreywackersquo (now Thaduna Formation of the YerridaGroup) for which the type area is about 100 km to theeast-northeast on THADUNA (Pirajno and Adamides 1998)
The Ravelstone Formation comprises a succession oflithic and quartz wacke shale and siltstone that was
deposited from turbidity currents In the north theRavelstone Formation contains lenses of chert andis unconformably overlain by the MesoproterozoicBangemall Group West of the Peak Hill opencut thelower contact with the Narracoota Formation is dis-conformable whereas the upper contact with theHorseshoe Formation appears to be conformable In thecentral and northern parts of BRYAH the RavelstoneFormation although metamorphosed has no tectonitefabric On MILGUN (around Fortnum) however a well-developed foliation is present
Drillcore from the Harmony gold deposit shows thatthe contact between the base of the Ravelstone Formationand the top of the Narracoota Formation is interfingeredpossibly due to shearing The disconformable contactbetween the base of the Ravelstone Formation and the topof the Narracoota Formation is exposed in a river bedabout 1 km due east of the Fortnum ndash Peak Hill turn-offIn this area graded layers of immature subarkosicsandstone to siltstone contain fresh plagioclaseK-feldspar sericitized lithic fragments and angular quartzgrains in a matrix composed of sericite and biotite Inaddition the siltstone contains euhedral crystals oftourmaline Metamorphic brown biotite and muscovite areabundant and replace feldspars quartz and lithicfragments Lithic fragments include massive chlorite(ndashrutile) derived from mafic precursors chert hematitendashquartz shale as well as partly sericitized feldspar grainsQuartz grains include rounded to irregular shapes andbiotite is metamorphic in origin Quartz white micachlorite and variable amounts of carbonate are part of thefine-grained matrix Well-developed foliation wherepresent is defined by aligned sericite elongate quartzand to a lesser extent feldspar grains and by mica seamsNew muscovite flakes have grown along and across thefoliation
In the Fortnum mine area on MILGUN graded beddedlithic wacke and siltstone overlie the volcanic rocks of theNarracoota Formation The wacke contains medium tocoarse-grained crystals of feldspar (plagioclase minor K-feldspar) and quartz as well as fragments (fine metabasaltand chlorite) derived from mafic volcanic rocks Thefeldspar crystals which are strongly sericitized dominateover quartz The matrix consists of sericitendashchloritendashquartz with or without carbonate The reworked rocksinclude fragmental layers with fine metabasalt debris andgraded chloritic siltstone containing plagioclase laths Thederivation of the mafic component is easily explained butthe well-preserved feldspar crystals suggest nearbygranitic or felsic volcanic precursors
Horseshoe Formation
The Horseshoe Formation occupies areas west of thePeak Hill opencut and the northern parts of BRYAH
and MILGUN This formation includes finely laminatedferruginous (hematitic) shale and siltstone fine-grainedquartzndashfeldspar wacke with interleaved iron formation andchert graded quartz wacke manganiferous shalegarnetiferous biotitendashchlorite schist and garnetiferousiron-formation Relatively high manganese contents areinferred from the abundant manganese oxide staining in
CFB
MORB
20
18
15
13
10
08
05
03
000 1 2
TiO
2
FMP168 211099Ultramafic schist
Mafic schist
Hyaloclastite rocks
(tot)FeO MgO
Figure 16 TiO2 versus FeOMgO plot (Breitkopf and Maiden1988) for the Narracoota Formation showing themid-ocean ridge basalt (MORB) affinity of the maficand ultramafic schist and the transitional chemistryof the hyaloclastites towards continental floodbasalts (CFB)
17
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
weathered and lateritic rocks and lateritic manganese orehas been mined at the Horseshoe and Mount Padburymines The type area of the Horseshoe Formation is theHorseshoe Range (Occhipinti et al 1997) where athickness of approximately 1000 m was estimated by Gee(1979) The Horseshoe Formation overlies the NarracootaFormation however the contact is either conformable ortectonic Elsewhere on JAMINDI north of BRYAH theHorseshoe Formation overlies the Ravelstone Formationand the contact is gradational and conformable TheHorseshoe Formation underlies the Labouchere Formationof the Padbury Group The nature of this upper contactappears conformable however Martin (1994) suggestedthat there is a regional unconformity between these units
Structurally the Horseshoe Formation forms a broadsyncline with its axis trending approximately easterly Thesouthern limb of this syncline is in sheared contact withrocks of the Narracoota Formation In this area theHorseshoe Formation is complexly folded with axestrending 070deg parallel to the shear zone
In the Horseshoe Range Gee (1987) recognized threeunits 1) a lowermost part consisting of regularly beddedwacke and shale similar to the underlying Ravelstonesuccession but finer grained more calcareous andcontaining less chlorite and more feldspar and quartzindicative of a granitic rather than mafic volcanicprovenance 2) a middle iron-formation member withseveral BIF (chertndashmagnetitendashstilpnomelane white chert)horizons intercalated with chloritic shale and 3) anupper unit of calcareous manganiferous shale andwacke The lowermost unit is exposed on MILGUN in thelow hills east of Fortnum airstrip where fine-grainedcarbonate-cemented wacke and shale contain dis-harmonic-folded white-chert lenses (2ndash12 cm thick) andless common discontinuous quartzndashmagnetite layers(2ndash3 cm) The quartz wacke component of the HorseshoeFormation contains quartz plagioclase microclinebiotite and muscovite all as detrital minerals Nearthe Peak Hill opencut the iron formation is made upof biotite amphibole chlorite quartz magnetite andgarnet This unusually high grade assemblage may berelated to the metamorphism of the Peak Hill Schist (seeMetamorphism)
About 1 km north of the Ravelstone manganesedeposits a reasonably good exposure of the HorseshoeFormation was examined in detail A stratigraphic columnfor this locality is shown in Figure 17 This is a foldedupward-coarsening package approximately 350 m thickwhich from base to top consists of quartzndashlithic wackewith banded chert interbeds displaying a well-developedaxial planar cleavage quartz wacke with iron formationand shale interbeds massive beds of coarse-grainedquartzndashlithic wacke intercalated with thin granular iron-formation amphibole- and garnet-bearing granular iron-formation layers and massive quartzndashlithic wackeintercalated with thin iron-formation bands The quartzndashlithic wacke contains chert clasts detrital subangularquartz fresh plagioclase crystals and biotite in a matrixof sericite green chlorite and iron oxide grains Bandedcherty material is composed of granular quartz aggregatesbrown biotite actinolite and very fine carbonate-richlaminae (this rock is best classified as a quartzndashbiotitendash
actinolite schist) The granular iron-formation consists ofgranular aggregates of quartz and iron oxides withinterstitial biotite and chlorite Syntectonic garnetporphyroblasts are replaced in part by quartz andcarbonate Massive lithic wacke consists of a packedaggregate of angular quartz feldspar and chert grains thematrix is volumetrically small and made up of biotitequartz and sericite Garnetiferous iron-formation has darklaminae of quartz granules with interstitial actinolitendashchlorite iron oxides and light-coloured microbands (1 cmthick) of quartz with actinolitendashchlorite iron oxides anddisseminated synndashlate-tectonic garnet porphyroblastsGarnet is also present as porphyroblasts growing acrossmicroband boundaries
Padbury GroupThe Padbury Group locally unconformably overliesthe Horseshoe Formation of the Bryah Group but inplaces is in faulted contact with the Bryah Group andYarlarweelor gneiss complex (Narryer Terrane Yilgarn
FMP156 020300
0
100
200
300
intercalated with thin BIF and shale interbeds
Garnetiferous BIF
Massive beds of coarse-grained lithic wackewith interbeds of garnetiferous BIF and
Banded iron-formation interbedded with massive
Banded chertQuartzndashlithic wacke with carbonate cement
wacke and soft granular iron-formation
(m)
granular iron-formation
Massive quartzndashlithic wacke layers
Micaceous wacke
Figure 17 Schematic stratigraphy of the HorseshoeFormation from an area of outcrops about 12 kmwest-northwest of the Peak Hill mine (after Pirajnoand Occhipinti 1998 width of column reflectsrelative resistance to weathering)
18
Pirajno et al
Craton Fig 2) Considerable onlap of the Padburysuccession onto the various formations of the Bryah Groupcan be inferred these contacts were faulted possibly inseveral stages during basin closure The age of thePadbury Group is poorly constrained Nelson (1997)reported a maximum age of c 20 Ga from the upper partof the Wilthorpe Formation and Windh (1992) inferred aminimum age of c 18 Ga from a leucogranite dyke
Martin (1994 1998) proposed a formal stratigraphy forthe lower Padbury Group based on detailed sediment-ological studies in the area covering the southeastern andcentral parts of MILGUN This formal stratigraphy replacedprevious stratigraphic divisions (Barnett 1975 Gee1979 1987 Windh 1992) and has since beenexpanded to include two distinct lithostratigraphic unitsas members within the Wilthorpe Formation the Heinesand Beatty Park Members (Occhipinti et al 1997) Martin(1994 1998) interpreted the Labouchere and WilthorpeFormations as an upward-coarsening deep-water turbiditecomplex overlain by shales and iron formation of theRobinson Range Formation The turbidites were derivedby erosion from the granitendashgneiss basement (YilgarnCraton) and by reworking of underlying sedimentary andmafic volcanic rocks in the Bryah Basin
The Padbury Group contains quartz wacke siltstoneconglomerate iron formations hematitic shale and minorclastic rocks and dolomite (Martin 1994 Occhipintiet al 1997) and is subdivided into four formationsLabouchere Wilthorpe Robinson Range and MillidieCreek Formations Martin (1994) interpreted the PadburyGroup to have been deposited in a retroarc foreland basinthat developed on top of the Bryah Group
Labouchere Formation
The Labouchere Formation occupies areas in thenorthwestern part of the Bryah Basin where it isfaulted against the Yarlarweelor gneiss complex Martin(1994 1998) suggested that the Labouchere Formationunconformably overlies the Horseshoe Formation(Bryah Group) based on the regional geometry inthe Fortnum mine ndash Dandy Well area on MILGUN Theregional unconformity is inferred from the low-angletruncation of an iron-formation marker unit in theHorseshoe Formation against lowermost quartz areniteof the Labouchere Formation in the area south ofYarlarweelor Creek North of the Fortnum Fault ironformation within the Horseshoe Formation is nearlyparallel to bedding in the Labouchere FormationElsewhere in the region contacts between variousformations of the Bryah and Padbury Groupsare interpreted as unconformities (Windh 1992) oralternatively as faults or shear zones (Pirajno andOcchipinti 1998 Occhipinti et al 1998b) On BRYAH theLaboucherendashHorseshoe Formation contact is marked bya conglomeratic unit The Labouchere Formation isconformably overlain by and grades into the WilthorpeFormation (Martin 1994) although this contact waspreviously described as an unconformity (Gee 1979) Gee(1979) estimated the Labouchere Formation (including theWilthorpe Formation) to be 5000 m thick extending from
Mount Labouchere on MILGUN (type area Martin 1994)to the Horseshoe Range the southern continuation ofwhich is in northwestern BRYAH Martinrsquos (1994 1998)type section is a composite stratigraphy (up to 7000 mthick) based on four separate sections in southeasternMILGUN
The Labouchere Formation consists of quartz arenitemedium- to coarse-grained sericitic quartz wacke andsericitic siltstone minor conglomerate and banded iron-formation in an upward-coarsening succession Near theHorseshoe manganese mining area the LabouchereFormation consists of a thick succession of upward-finingcycles up to 700 m thick Each cycle consists ofconglomerate or a coarse lithicndashquartzndashsericite wacke unitat the base grading up through coarse- to fine-grainedquartzndashfeldsparndashlithic wacke and sericitic siltstone to iron-rich shale These cycles however become increasinglycoarser upwards so that there is regional upwardcoarsening The base of the topmost cycle begins with aquartz-pebble conglomerate Minor and thin bands of iron-formation are locally present as intercalations within thesedimentary units
Quartz arenite contains grain-supported well-roundedquartz in a sericitic matrix and is extensively silicified Aprominent quartz arenite marker forms the ridge includingMount Labouchere north of Fortnum mine on MILGUN andcan be traced for many tens of kilometres to the southeastwhere gradually more quartz wacke is interbedded withthe arenite A second quartz arenite marker approximatelyhalfway up the Labouchere Formation is present in thearea north of the Fortnum Fault In the same area an ironformation ndash chert layer is present about 250 m above thissecond quartz arenite Martin (1994) emphasized that thedeep-water environment of this iron formation indicatesa similar depositional environment for the clastic rocksQuartz wacke has a matrix-supported framework ofvariably rounded quartz grains minor lithic fragments andfeldspar in a sericitendashchlorite matrix whereas laminatedshale consists of sericitendashchlorite Wacke and siltstoneform numerous upward-fining cycles
Muscovitendashquartz schist or slate developed fromquartz wacke and siltstone in zones of high strain andhigher metamorphic grade adjacent to the Yarlarweelorgneiss complex Strongly foliated quartz wacke andmuscovitendashquartz schist occupy a 4 km-wide zone nearthe Labouchere mine on MILGUN Another belt of schistand slate is present between the Billara Fault and DespairGranite in southwestern MILGUN These strongly foliatedrocks can be traced northwards into recognizable thoughstrongly foliated pebbly quartz wacke The fine-grainedschist consists of elongate polygonalndashgranoblastic quartzwith spaced trails of aligned muscovite flakes Beddingndashcleavage relationships are found in less-deformed areaswhereas in high-strain zones differentiated layeringdeveloped from a pervasive crenulation cleavage
Sericite is abundant throughout most of the rocks ofthe Labouchere Formation The quartzndashsericite wacke iscomposed of subangular quartz grains embedded in asericitized matrix with occasional large muscovite lsquobooksrsquoand scattered small crystals of tourmaline and anatase
19
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Quartzndashfeldsparndashlithic wacke is made up of subangularquartz grains polycrystalline quartz K-feldspar andplagioclase in a matrix of quartz sericite biotite andminor detrital zircons
Wilthorpe Formation
The Wilthorpe Formation (formerly lsquoWilthorpeConglomeratersquo Gee 1987) including the Beatty Park andHeines Members comprises quartz- and chert-pebbleconglomerate quartz wacke sericitic siltstone chloritendashquartz shale quartzndashsericitendashhematite schist dolomiticsandstone and finely laminated chert lenses TheWilthorpe Formation is conformably overlain by theRobinson Range Formation
Martin (1994) measured the type section of theWilthorpe Formation (about 1300 m thick) along theTalbot Divide In this area the characteristic quartz-pebbleconglomerate forms a prominent ridge to the east of hillsunderlain by the Robinson Range Formation In theFortnumndashLabouchere area on MILGUN the exact locationof the LaboucherendashWilthorpe Formation transitionalboundary is less well defined (Swager and Myers 1999)Along the western wall of the Nathans Deep Southopencut (labelled Nathan Deep on Plate 1) severalupward-fining cycles of quartz-pebble conglomerategrading into quartz wacke and quartzndashmuscovite siltstonecan be observed These cycles are underlain by fine-grained chloritic shale interbedded with quartz wackeThis chloritic shale with detrital ilmenite is derived froma mafic precursor probably the Narracoota Formation(Windh 1992) Occhipinti et al (1998a) recognizedcomparable lsquomaficrsquo clastic rocks as a mappable unit(Beatty Park Member mdash see below) at the top of theWilthorpe Formation on PADBURY
The conglomerate contains well-rounded slightlyelongate or faceted vein-quartz clasts and less commonlychert quartzite quartz wacke and rare siltstonendashmudstoneclasts in a quartz wacke matrix Clasts range in size frompebbles to boulders Quartzite pebbles locally containfolded foliation fabrics Bunting et al (1977) suggestedthat large quartzite boulders in the southern part of thetype area were derived from the basal Finlayson Memberof the Juderina Formation (Yerrida Group) Martin (19941998) recognized two polymictic conglomerate intervalsin the type area which included silicified dolomite clastsThese intervals are similar to the polymictic conglomerateand sandstone of the Heines Member defined on BRYAH
(Pirajno and Occhipinti 1998) Siltstone forms a distinctmappable upper unit along the gradational contact withthe Robinson Range Formation
Beatty Park and Heines Members
The Beatty Park Member outcrops in the Mount Padburyarea on PADBURY and contains clastic rocks that werepossibly sourced at least in part from the mafic volcanicrocks of the underlying Narracoota Formation (BryahGroup) with sedimentary chert lenses towards its top Asensitive high-resolution ion microprobe (SHRIMP)UndashPb date obtained from detrital zircons in one of these
chert lenses suggests a maximum age of 1996 plusmn 35 Ma(Nelson 1997) The clastic rocks of the Beatty ParkMember are dominated by metamorphosed chloritendashquartzshale siltstone and wacke several conglomeratic orbreccia lenses and finely laminated chert layers in places(Occhipinti et al 1997) The contact between the BeattyPark Member and the overlying Robinson RangeFormation is gradational with chloritic siltstone and chertlayers and lenses grading into sericitendashquartz siltstone Thelower contact of the Beatty Park Member with theWilthorpe Formation appears to be gradational in the areawest of the Fraser Synclinorium (see Structure) whereferruginized kaolinitic siltstone and quartz wacke gradeinto chloritic siltstone In this area the minimum thicknessof 470 m is implied because the upper part of the BeattyPark Member is not exposed
The shalendashsiltstone layers are well bedded to finelylaminated and consist of quartz and chlorite with minorsericite epidote feldspar titanite and detrital hornblendeThese layers are accompanied by very fine grainedrecrystallized white chert beds in the upper part of theBeatty Park Member West of the Fraser Synclinoriumsedimentary structures such as bedding-parallel lamin-ations flame structures and contorted bedding can beobserved within chloritic siltstone Two types of wackeunits are present one containing quartz dolomite chloritefeldspar sericite epidote sphene and opaque minerals(either magnetite or pyrite) and the other containingquartz feldspar muscovite epidote chlorite carbonateand opaque minerals Lithic fragments in wacke layersinclude metabasalt and mafic schists in which leucoxenepseudomorphs of iron oxides can still be recognizedLenses of coarse-grained lithic wacke and conglomeratecomprise rock fragments of basalt mafic schist chertchloritendashquartz wacke and coarse detrital grains (quartzfeldspar) in a sericitendashchloritendashquartz matrix Coarseclastic rocks fill channels that cut into the fine-grainedrocks and contain numerous rip-up clasts This suggeststhat at least in part the Beatty Park Member wasdeposited distally from the source region Locally whitechert lenses crosscut erosional contacts indicating that thechert is diagenetic or epigenetic
Within all rocks of the Beatty Park Member sericiteand muscovite are of metamorphic origin They replacechlorite in the fine-grained chloritic shalendashsiltstone layersand feldspar clasts in the wacke units In several examplesfine-grained muscovite has grown along late cleavageplanes
A quartzndashchloritoidndashsericitendashchlorite(ndashsulfide) unitpreviously interpreted to be a carbonate intrusion (Lewis1971 Elias and Williams 1980) has been assigned to theBeatty Park Member The chloritoid is crystallized insprays and displays a lsquobow-tiersquo texture The presence ofabundant chloritoid indicates that this rock has a highalumina content implying either a pelitic precursor or thatthe protolith was extensively metasomatized
The Heines Member consists of an upward-finingsuccession of sedimentary rocks with a polymicticconglomerate at its base followed by clastic sedimentaryunits (sandstone to shale) The type area is near Durack
20
Pirajno et al
Well on BRYAH At this locality the Heines Memberis folded into a syncline and its southern limb is in faultedcontact with the underlying Narracoota Formation Thenorthern contact is obscured here by the Cainozoic coverThe Heines Member includes those outcrops south of theRobinson Syncline at the Heines Find prospect RandellBore and 35 km northwest of Durack Well which werepreviously mapped as lsquoWilthorpe Conglomeratersquo byGee (1987) The succession is approximately 600 mthick although basal units may have been shearedoff along the faulted contact The basal polymicticconglomerate contains clasts of mafic lithic wackelimestone quartz arenite and hematitic shale supportedby a carbonate matrix This is followed upward by a seriesof sandstonendashshale units with the shale componentbecoming volumetrically greater with stratigraphic heightThe basal conglomerate of the Heines Member containsno volcanic clasts of the underlying Narracoota Formationand this is taken as evidence that the contact with the latterformation is tectonic The provenance of the various clastsin the basal conglomerate is not known In the Heines Findprospect area the Heines Member is overlain by theRobinson Range Formation
Robinson Range Formation
The Robinson Range Formation forms elongate outcropsthat extend from east to west in the centre of the BryahndashPadbury Basin and in a northerly direction on the easternmargin of the Yarlarweelor gneiss complex on MILGUN andPADBURY (Plate 1) The Robinson Range Formation isdefined by the appearance of ferruginous or hematiticshale followed by two iron formations mdash a well-definedlower banded unit separated by 100 m of ferruginousshale from an upper unit with clastic textures as mappedby Gee (1987) which is in turn overlain by hematitendashchlorite siltstone The Robinson Range Formation isconformably overlain by the Millidie Creek Formation
The Robinson Range Formation consists of asuccession of BIF siltstone and iron-rich shale Granulariron formation is present as irregular lenses The BIFconsists of laminae up to 3 cm thick These laminationscomprise various amounts of quartz iron oxides (hematiteor magnetite) biotite and locally ferro-actinolite Theshale and siltstone consist of fine-grained sericite quartzchlorite iron oxides and in a few places minor spheneThe mesostructure microstructure and petrology ofthe BIF are relatively simple Microbands or laminae lessthan 1 to 2ndash3 mm thick are made up of alternatingmicrocrystalline quartz(ndash iron oxides) greenndashbrownbiotite(ndash iron oxides) quartz grains(ndash acicular crystals ndashiron oxides) quartz grains(ndash iron oxides ndash biotite ndashacicular crystals) Commonly the quartz grain(ndash acicularcrystal) assemblage displays a polygonized texturesuggestive of annealing due to metamorphism Theacicular crystals are weathered to iron oxides but onthe basis of their morphology they could be eitherstilpnomelane crystals or amphiboles The iron oxides areeither hematite or magnetite Incident light microscopyreveals that a primary titaniferous magnetite is replacedby hematite which in turn is replaced by goethite in thesupergene environment The biotite is porphyroblastic and
mostly grown under conditions of peak metamorphism(see Metamorphism)
Granular iron-formation is characterized by a granulartexture and the presence of elongate peloids 1 to 4 mmlong The peloids consist of microcrystalline chert outlinedby rims of iron oxides (hematite with inclusions ofilmenite) The chert peloids are enclosed in finemicrocrystalline cherty or chalcedonic material Thepeloids and chert make up bands approximately 1 to15 cm thick with occasional laminae of fine chert(ndash ironoxides)
The ferruginous shale is composed of silt-sized quartzgrains and iron oxides with abundant interstitial biotiteand minor disseminated euhedral tourmaline crystals Thetourmaline was formed either during metamorphism or ahydrothermal event
The iron formations of the Robinson Range Formationhave been correlated with the granular iron-formation ofthe Frere Formation (Earaheedy Basin) 150 to 450 km tothe east-southeast by Hall and Goode (1978) whocompared them to those of the Lake Superior region inNorth America
Millidie Creek Formation
The Millidie Creek Formation defined by Barnett (1975)and modified by Gee (1979) and Occhipinti et al (1997)forms comparatively small outcrops in the cores of theRobinson Syncline and Fraser Synclinorium (seeStructure)
Ferruginous shale and siltstone intercalated withirregularly banded manganiferous iron-formation formsthe basal unit of the formation This unit is locallylateritized and hosts many manganese deposits suchas the Millidie (or Elsa) mine (see Mineralization)The banded manganiferous iron-formation commonlyforms low ridges On PADBURY the Millidie CreekFormation consists of iron-rich shale and siltstoneirregularly banded manganiferous iron-formationdolomitic sandstone ferruginous quartz wacke andchloritic siltstone On BRYAH the Millidie Creek Formationconsists of ferruginous shales with a well-developed pencilcleavage sandstone and minor granular iron-formation
Dolomitic sandstone and quartz wacke are locallypresent within this formation The quartz wacke is wellbedded matrix supported and commonly containssubangular to subrounded quartz grains The matrix of thisrock is composed of randomly oriented fine-grainedbiotite and includes late sphene and minor sericite Thedolomitic sandstone comprises carbonate quartz andmuscovite
In low hills 3 km north of 5 Mile Well (Plate 1) finelybedded micaceous siltstonendashshale with interbeddedquartzndashdolomite siltstone layers previously assigned to theLabouchere Formation (Elias et al 1982) have beenassigned to the Millidie Creek Formation These rocks arefolded about northwesterly trending D4 fold axes andcontain S4 foliation They are unconformably overlain by
21
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
subhorizontal to shallowly dipping basal quartz arenite ofthe Bangemall Group
Chloritic siltstone at the top of the Millidie CreekFormation is compositionally similar to the Beatty ParkMember and comprises quartz feldspar lithic fragmentsof sericitendashquartz schist and detrital cordierite grains ina foliated matrix of chlorite
Unassigned units of the Padbury Group
Metasedimentary rocks and biotitendashsericite schist whichoutcrop within the Despair Granite near the Wilthorpegold mine (Plate 1) were previously referred to aschloritendashmuscovitendashquartz schist and not assigned to anygroup (Elias et al 1982) Occhipinti and Myers (1999)tentatively assigned these units to the Padbury GroupThere are two main outcrops one in the Wilthorpe mineand the other just outside the mine as a fault-boundedinclusion within the granite
Sedimentary rock found within the Despair Graniteis heterogeneously deformed and metamorphosedSedimentary structures such as cross-bedding andbedding-parallel laminations are present This rockconsists of alternating layers of very fine grained biotitequartz sericite and feldspar Accessory minerals includeopaque minerals In a few places this rock contains afoliation parallel to faults or fold-axial planes Opaqueminerals commonly crosscut the dominant (bedding)fabric The preservation of the primary sedimentarytextures suggests that strong deformation did notaccompany low-grade greenschist-facies metamorphism ofthese rocks
Within the Wilthorpe mine the metasedimentary rockscontain a slightly different mineralogy and are in faultedcontact with the sericitized Despair Granite For instancein one sample there are two distinct layers composed ofeither sericite quartz biotite and opaque minerals orbiotite sericite quartz and minor opaque minerals Thisvariation in bedding composition is consistent with thatobserved in the metasedimentary rocks outcroppingoutside the mine The rocks within the mine are coarsergrained and comprise quartz biotite sericite andandalusite Sericite and biotite overprint the foliation inthe rock
StructureThe Padbury and Bryah Basins are pervasively deformedThis deformation may have solely occurred duringthe c 18 Ga Capricorn Orogeny a period of obliquecollision between the Archaean Pilbara and YilgarnCratons (Tyler and Thorne 1990 Tyler et al 1998Fig 2) or in part during the earlier c 20 Ga GlenburghOrogeny (Occhipinti et al 1999) In addition to deformingthe Bryah and Padbury Groups this deform-ation also resulted in the reworking of parts of theArchaean Narryer Terrane and the Marymia Inlier of theYilgarn Craton (Fig 2) to form the Yarlarweelor gneisscomplex and Peak Hill Schist The rocks of the Bryah
and Padbury Groups are locally interleaved with theYarlarweelor gneiss complex in the western part of theregion (Fig 18) To the south the Bryah and PadburyGroups are tectonically juxtaposed against autochthonousrocks of the Archaean Murchison Terrane of the YilgarnCraton and the Palaeoproterozoic Yerrida Group (Fig 2)
The Yarlarweelor gneiss complex dominantly consistsof Archaean granitic gneisses that were intruded by felsicmagmas at c 1960 Ma (Sheppard and Swager 1999) and1820ndash1800 Ma (Occhipinti et al 1998b Sheppard andSwager 1999) Granite sheets and veins intruded into theArchaean gneisses were pervasively deformed into opento tight folds and metamorphosed at medium to highgrades during the Capricorn Orogeny Occhipinti andMyers (1999) suggested that these folds were originallynortherly trending however they are probably more likelyto have been northeasterly trending Dextral strike-slipshear movement involved a transition from early ductileto later brittle deformation (Occhipinti et al 1998b)coincident with uplift which probably progressed fromnortheast to southwest in the region This deformationproduced regional-scale fault-bend folds in both theYarlarweelor gneiss complex and overlying Palaeo-proterozoic Bryah and Padbury Group rocks
Deformation histories presented for the Yerrida Bryahand Padbury Groups by various authors (including Windh1992 and Gee 1990) have many elements in common(Table 5) This includes major northndashsouth compressionthat was responsible for the development of prominentregional easterly trending upright folds such as theRobinson Syncline (Fig 18) Northerly striking folds andfaults in the domain just east of the Yarlarweelor gneisscomplex have been recognized as a later deformation stage(Windh 1992 Martin 1994) Gee (1990) Windh (1992)and Martin (1994) proposed that eastward movement ofthe Narryer Terrane (here referred to as the Yarlarweelorgneiss complex) was responsible for the development ofthese northerly trending folds In their interpretation thenortherly striking folds formed in front of an advancingthrust sheet of Archaean gneiss and granite overriding theBryah and Padbury Groups Myers (1989 1990) andMyers et al (1996) on the other hand regarded the Bryahand Padbury Groups as allochthonous sheets that werethrust over Archaean granitendashgneiss
Contacts of the Bryah and Padbury Groups with theNarryer Terrane Yarlarweelor gneiss complex MarymiaInlier Murchison Terrane and the PalaeoproterozoicYerrida Group are zones of high strain and thereforeinferred to be faults Unconformable contacts between theBryah and Padbury Groups were reported by Martin(1994 1998) whereas sheared and faulted contacts werereported by Pirajno and Occhipinti (1998) Occhipintiet al (1998ac) and Occhipinti and Myers (1999) Forexample the Bryah Group is in faulted contact with theYarlarweelor gneiss complex north of Livingstones Findand the Murchison and Narryer Terranes are separatedfrom the Bryah and Padbury Groups by the steep easterlytrending Murchison Fault which has a sinistral strike-slipcomponent (Plate 1 Fig 2)
The Goodin Fault a high-angle reverse fault (Pirajnoand Occhipinti 1998) is the boundary between the
22
Pirajno et al
Yerrida and Bryah Groups (Fig 2 Plate 1) East of thisfault the Doolgunna Formation (Yerrida Group) is foldedinto isoclinal upright folds however much of thedeformation in the Yerrida Group dies out rapidly to theeast and southeast To the west the Goodin Fault mergeswith the Murchison Fault which has juxtaposed the Bryahand Padbury Groups against the Yilgarn Craton TheMurchison Fault has a sinistral strike-slip componentwhich offsets Archaean structures in the Murchison andNarryer Terranes
In this Report four distinct groups of structuresD1ndashD4 representing progressive compressional deform-ation are recognized (Table 5) This deformation historyalthough in broad agreement with the previously publishedstructural histories (eg Windh 1992) recognizes separateearly layer parallel structures The structures resultingfrom the four deformation events are not developedeverywhere or with the same intensity everywhere
The earliest deformation events are defined in the PeakHill Anticline area as D1 layer-parallel mylonitic thrustfaults and originally subhorizontal folds overprinted byD2 upright eastndashwest striking regional folds Both D1 andD2 structures developed by northndashsouth compression and
can be interpreted as successive stages of progressivedeformation Northerly trending regional D3 folds andupright foliations recording eastndashwest compression areweakly developed in the Peak Hill Anticline but betterdeveloped and largely restricted to a domain immediatelyeast of the Yarlarweelor gneiss complex However thesenortherly trending structures do not always overprint oldereasterly trending structures and in places these two setsof structures (D2 and D3) tend to be mutually exclusivesuggesting that they probably developed during the sameprogressive deformation event Late medium-scale D4structures include west-northwesterly to northwesterlytrending subvertical foliations shear zones zones ofsmall-scale folding and faults now outlined by quartzblows These locally developed structures suggest latenorth-northeast to south-southwest compression
Major fold structures in the Padbury and Bryah Basinsare the Peak Hill Anticline Robinson Syncline MillidieSyncline Fraser Synclinorium Horseshoe Anticline andPadbury Syncline (Plate 1 and Fig 18) The Peak HillAnticline Robinson Syncline Fraser Synclinorium andMillidie Syncline all represent refolded folds The easterlytrending doubly plunging Robinson Syncline andPeak Hill Anticline are D2 folds refolded during D3 D1
Figure 18 Major regional structures in the Bryah and Padbury Groups (after Occhipinti et al 1998a)
FMP371
MARYMIAINLIER
YILGARNCRATON
Goodin
Fault
GROUPBANGEMALL
Murchison Fault
118deg30 119deg30
30 km
020300
YERRIDAGROUPPeak Hill
Anticli
ne
Robinso
n
Synclin
e
Nathan Syncline
Zone of D folding3
Padbury
Horseshoe Anticline
Wilthorpe F
t
BRYAH ANDPADBURYGROUPS
GOODININLIER
EARAHEEDYGROUP
25deg30
26deg00
Syncline
Millidie Syncline
FaultD fold trace3
D fold trace2
1
D fault1
Anticline
SynclineD ndash D thrust fault2
Yarlarweelorgneiss
complex
FraserSynclinorium
23
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
folds are also present within these structures (see D1structures) The Horseshoe Anticline appears to be a D3fold contained within the fault-bounded Horseshoeanticlinal block This fault-bounded block also appears tobe cut by northwesterly trending (D4) faults
D1 structuresThe first Palaeoproterozoic deformation event (D1)produced layer-parallel folds a locally pervasive S1schistosity mylonites and faults However because thesestructures were pervasively overprinted by D2 structuresthey are rarely observed F1 folds are locally observed inthe Peak Hill Antiform Robinson Syncline FraserSynclinorium an area 5 km northeast of Mount Fraserand the Millidie Syncline These folds are also observednear the Peak Hill mine in F2 foldndashhinge zones of quartzblastomylonites of the Peak Hill Schist (Fig 6) Here theyare small-scale rootless isoclinal plunge shallowlytowards the east and strike eastndashwest In the FraserSynclinorium and Millidie Syncline the F1 folds are small-scale isoclinal folds that plunge gently towards the east-northeast or west-southwest and strike east-northeasterlyF1 folds are also inferred from aeromagnetic data to bepresent within the Fraser Synclinorium and MillidieSyncline (Figs 18 and 19)
The Goodin and Murchison Faults may be D1 faultsthat were reactivated during D2 (Occhipinti et al 1998c)The Murchison Fault (Figs 18 and 19 Plate 1) separateslargely undeformed basaltic hyaloclastite rocks in thesouth from foliated mafic schists to the north
Mesoscale F1 folds in the shale and banded iron-formation of the Robinson Range Formation are observednear Mount Padbury north-northwest of Beatty Park Bore
(Plate 1) in the hinge zone of the Robinson Synclinenorth of Tank Well and northeast of Randell Bore TheseF1 folds are tight to isoclinal with shallow plunges thattrend to the east or west The F1 folds in the area areinterpreted as originally recumbent D1 zones of highstrain and mylonite developed locally mainly in thePeak Hill Schist (Pirajno and Occhipinti 1998) andalong contacts between the Yarlarweelor gneiss complexand Palaeoproterozoic cover rocks These mylonite zonesare not observed at higher stratigraphic levels within thebasin suggesting that they are restricted to a deeper crustallevel represented by the Peak Hill Schist and basementndashcover contacts Quartz blastomylonites and the CrispinMylonite (Pirajno and Occhipinti 1998) form continuousunits within the Peak Hill Schist (Plate 1) The internalstructure of these units suggests that they may be D1shear zones which were refolded during the laterdeformation events The original nature and orientation ofthese shear zones is not known The Crispin Myloniteconsists of quartzite pebble-and boulder-sized clasts in asericitendashquartz-rich matrix and has the appearance of aconglomerate For that reason it was mapped by Gee(1987) as the lsquoCrispin Conglomeratersquo However meso-scopic and microscopic structures indicate that it is amylonite (Figs 4 and 7) Both the quartzite clasts andmatrix contain a mylonitic fabric The Crispin Myloniteis interpreted as a lsquopseudo-conglomeratersquo (Raymond1984ab) formed by shearing probably along or close toa fault plane that separated an arkosic or granitic unit froma quartz-rich unit
Like the Crispin Mylonite the quartz blastomylonitesform arcuate lenses within quartzndashmuscovite schist of thePeak Hill Schist and are refolded by F2 and F3 folds Thequartz blastomylonites contain isoclinal and sometimesrootless F1 folds and are interpreted to have beendeformed in a ductile high-strain zone (fault or shear zone)during D1 It is not possible to determine the sense ofmovement during D1 because no shear sense indicatorswere observed during mapping
D2 structuresThe D2 deformation produced large-scale uprightregional F2 folds with variably developed S2 foliationas well as faults and shear zones These structuresare easterly trending recording northndashsouth shorteningHowever more complex patterns in the Mount Fraserarea suggest complicated refolding patterns ProminentD2 folds include the doubly plunging Robinson Synclineand the Padbury Syncline which has the hinge zonelargely sheared out (Fig 18 Plate 1) Mesoscale F2folds show steeper plunges and the S2 foliation becomesmore intense to the north A pervasive S2 foliation isdeveloped over large areas in the mafic schists ofthe Narracoota Formation The Goodin Fault is a high-angle reverse fault that forms the boundary between theYerrida and Bryah Groups This fault may have developedduring D2 because south of the fault the DoolgunnaFormation is folded into tight to isoclinal upright folds(with fold-axial surfaces subparallel to the Goodin Fault)that are similar to D2 folds in the Bryah and PadburyBasins
Table 5 Sequence of deformation events in the Bryah and PadburyBasins
Deformation Compressionevent
D4 North-northeastndashsouth-southwest compressionSmall-scale folds subvertical foliation shearzones faults with quartz blows all trending
280degndash310deg
D3 Eastndashwest compressionnorthndashsouth trending folds subvertical foliationsubvertical faults or shear zones localized eastof Narryer Terrane increasingly disharmoniceast-northeasterly trending folds eastwards
D2 Northndashsouth compressionupright tightndashisoclinal eastndashwest folds andsubvertical foliation eastndashwest shear zonessouth-verging thrust faults
D1 Northndashsouth compressionsubhorizontal mylonites thrusts and foldsmesoscale recumbent folds tightndashisoclinalrootless
24
Pirajno et al
The Livingstone Synform a steep easterly plungingtight fold on MOORARIE may be part of a larger scale D2fold structure that is confined between the Kerba Fault inthe north and the Mount Seabrook Fault in the south(Occhipinti and Myers 1999)
Within the Yarlarweelor gneiss complex graniticgneisses form open to isoclinal easterly to northeasterlyand northerly trending shallowly to steeply plungingfolds These folds plunge either to the east and northeastor to the west and west-southwest indicating that on a
Figure 19 Simplified geological map of the Bryah and Padbury Groups (after Occhipinti et al 1998a) See Figures20 22 and 23 for cross sections
118deg 119deg
25deg45
10 km
MarymiaInlier
YilgarnCraton
BangemallBasin
Bill
ara
Fa
ult
Wilt
horp
eF
Fortnum
25deg30
Goo
din
Faul
t
Kinders FaultNathan
Peak Hill
B
AC
Mt Fraser
Yarlarweelor gneisscomplex
(reworked NarryerTerrane)
YerridaBasin
PADBURY GROUP
BRYAH GROUP
RAVELSTONE FORMATION lithic wacke
KARALUNDI FORMATION clastic rocks
quartzndashmuscovitendashbiotitendashstaurolite schist
HORSESHOE FORMATION shale banded iron-formation
YERRIDA GROUP
WILTHORPE FORMATION conglomerate siltstone
PA
LA
EO
PR
OT
ER
OZ
OIC
Greenstone
Peak Hill Schist
AR
CH
AE
AN
Fault
Anticline
Syncline
ME
TA
MO
RP
HO
SE
D
NARRACOOTA FORMATION maficndashultramafic volcanic rocks
LABOUCHERE FORMATION quartz wacke siltstone
Unconformity
Mine
Cross-section
Undifferentiated rocks
MILLIDIE CREEK FORMATION Lithic wacke dolomitic sandstone siltstone banded iron-formation
Granite and graniticgneiss
ROBINSON RANGE FORMATION shale granular iron-formation banded iron-formation
140300FMP373
25
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
regional scale they are doubly plunging possiblyrecording later refolding and eastndashwest shortening (D3)These folds deform both the Archaean gneiss and c 1960and c 1820 Ma granite sheets that intruded the gneiss(Sheppard and Swager 1999 Occhipinti et al 1998c)They refold tight to isoclinal subhorizontal to shallowlyplunging folds in the Archaean granitic gneisses whichmay have developed during the Archaean
The sense of shear of the steeply dipping D2 shearzones could not be determined South of the Robinson andFraser Synclines regional anastomosing D2 shear zonesdeveloped in the basaltic rocks of the NarracootaFormation To the northeast this regional structurebecomes the Jensen Fault (Pirajno and Adamides 2000)which can be shown to have displaced the Meso-proterozoic Bangemall Group suggesting that the faultwas reactivated after this time Along the southern limbof the Fraser Syncline another fault extends into the D2shear zones mentioned above A shear zone cuts thesouthern limb of the Heines Syncline which lies betweenthe Robinson and Fraser Synclines
D3 structures and theirrelationship to D2 structuresNortherly trending D3 folds faults and locally an uprightS3 foliation indicating an eastndashwest compression are welldeveloped in the area east of the Yarlarweelor gneisscomplex Further east F3 fold intensities decrease andfolds are locally more disharmonic The D3 event wasresponsible for the doubly plunging nature of theRobinson Syncline and the Peak Hill Anticline
The Kinders Fault (Fig 20 Elias and Williams 1980)is a northerly trending D3 fault separating a wedge ofmafic volcanic schists of the Narracoota Formation(Bryah Group) from the Robinson Range Wilthorpeand Labouchere Formation rocks (Padbury Group) Thisfault lies along the western limb of the sheared-out hingeof the F3 Nathan Syncline (Plate 1 and Fig 18) Thissyncline was previously correlated with the PadburySyncline to the south (Elias and Williams 1980 Martin1994 1998) Part of the southerly plunging fold hingeof the Nathan Syncline is preserved in the Nathan minearea and the closure of this syncline can be traced furthernorth The wedge of maficndashultramafic schists of theNarracoota Formation was interpreted by Occhipinti et al(1998c) and Martin (1994 1998) to represent an F3anticlinal fold-thrust wedge overlying pervasively foliatedand metamorphosed quartz wacke of the LabouchereFormation to the west (Figs 19 and 20)
West of the Kinders Fault along the Billara Faultsericitendashquartz schist locally with quartz-pebbleconglomerate layers contains a pervasive S3 fabricF3 folds however are difficult to trace East of theKinders Fault open to close and locally tight to isoclinalfolds are outlined by marker beds in the Labouchere andHorseshoe Formations S3 foliations and moderate tosteep southerly plunging small-scale F3 folds are welldeveloped in the area of the Horseshoe Syncline andfurther north
Several observations suggest that D2 and D3 structuresmay not reflect two separate events but may havedeveloped contemporaneously in different domainsIntense D3 folding is largely restricted to the area betweentwo basement highs represented by the Yarlarweelorgneiss complex in the west and the Peak Hill Schist in theeast (Figs 18 and 19) In the domain just east of andadjacent to the Yarlarweelor gneiss complex there is noevidence for D3 refolding D2 (ie upright northerlytrending D3 folds overprinting upright easterly trending D2folds) even though weak northerly trending D3 foldsdeform easterly trending F2 folds around and within thePeak Hill Anticline
In the Mount Fraser area complex fold and foliationpatterns show orientations different from and transitionalto both the regional D2 and D3 deformation Large-scaleeast-northeasterly trending F2 folds such as the RobinsonSyncline and Peak Hill Anticline die out in this area TheMillidie Syncline can be traced from a west-northwesterlystrike (subparallel to and en echelon with the RobinsonSyncline) to a west-southwesterly strike and is then cutoff to the south by D3 faults (Figs 18 and 19)
These observations suggest that the intensity and trendof the D2 and D3 structures were influenced by their spatialrelationship to the Yarlarweelor gneiss complex and PeakHill Schist
D4 structuresD4 structures include mesoscopic chevron folds kinksshear zones and faults and were locally accompanied bythe development of a foliation These D4 structuresdeveloped locally throughout the Bryah and PadburyBasins Yarlarweelor gneiss complex and the northern-most part of the Murchison Terrane In the PadburyndashBryahdomain most structures trend between west-northwest andnorthwest although in the Yarlarweelor gneiss complexa few late structures trend between north-northwest tonorth Brittle faults cutting the Yarlarweelor gneisscomplex often show dextral strike-slip shear movement
MetamorphismRegional metamorphic zones within the volcano-sedimentary succession are related to the geometry of thePeak Hill Anticline and Yarlarweelor gneiss complex Thehighest metamorphic grade assemblages are found in thecontact zones between the Yarlarweelor gneiss complexand overlying metasedimentary rocks Assemblages inthe Peak Hill Schist and within quartzndashmica schists(Labouchere Formation) along faulted contacts withthe Yarlarweelor gneiss complex record upper greenschist-to lower amphibolite-facies conditions Within theYarlarweelor gneiss complex upper amphibolite-faciesconditions were reached as incipient (minimum) meltpatches within granitic gneiss and amoeboid textures inPalaeoproterozoic coarse-grained granite probablydeveloped during D2 (Sheppard and Swager 1999) In theBryah and Padbury Groups however metamorphismtypically does not exceed greenschist facies and east of
26
Pirajno et al
0
2
4
6
Fault
Kilo
met
res
Southwest Northeast
FMP372
0
2
4
6
Kilo
met
res
West East
Billara
Fault
Kilo
met
res
0 Padbury
South North
SynclineDome
2
4
6
Yarlar-weelor
170300
Fault
Kinders
MIDDLE PROTEROZOIC
ARCHAEAN (reworked during Early Proterozoic)
Bangemall Group
Unconformity
Bedding or layering trend
Foliation
High-strain zone
Fault
Movement along fault
Movement away and towards observer
2
BRYAH GROUP
Geological boundary
Padbury Basin
Bryah Group
S N
d)
sediment fluxsediment flux
EARLY PROTEROZOICPADBURY GROUP
ARCHAEAN (in situ)
Peak Hill Schist quartzndashmuscovite schistquartz mylonite phyllonite
Granitendashgreenstone Murchison Terrane
Millidie Creek Formation sandstoneshale dolomitic siltstone
Robinson Range Formation ferruginous shalebanded iron-formation
Wilthorpe Formation quartz-pebbleconglomerate
Labouchere Formation quartz wackesiltstone quartz arenite
Horseshoe Formation ferruginous shaleiron formation
YERRIDA GROUP
Narracoota Formation metabasalt subordinatedolerite picrite and peridotite
Goodin
Normal fault reworked during D thrusting
Granite gneiss and granite with lenses of supracrustal rock Narryer Terrane
GranitendashgreenstoneMarymia Inlier ndash Murchison Terrane
Ravelstone Formation lithic wacke
Karalundi Formation clastic rocks
a) Cross section A
b) Cross section B c) Cross section C
Undifferentiated rocks
27
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
the Goodin Fault in the Yerrida Group metamorphic gradedecreases to subgreenschist facies (prehnitendashpumpellyite)The relationships between metamorphic mineral growthand deformation are summarized in Table 6
M1 was a prograde regional metamorphic event thattypically reached greenschist facies (Pirajno andOcchipinti 1998) and was probably coincident withD1 in the Bryah and Padbury Groups and Peak Hill SchistThornett (1995) suggested that some parts of the Peak HillSchist reached amphibolite-facies metamorphism withtemperatures between 500deg and 620degC and pressures of65 ndash 7 kbar Metamorphic mineral assemblages observedhowever commonly do not concur with these data Thesecond metamorphic episode M2 was commonly one ofretrogression throughout most of the Bryah and PadburyBasin and probably associated with metasomatismin high-strain zones during D2ndashD3 During M2 inthe western part of the Bryah and Padbury Basinsadjacent to the Billara Fault (Fig 18) staurolitendashandalusitendashbiotitendashmuscovitendashquartz schist developedfrom the metamorphism of Padbury Group sedimentaryrocks These rocks indicate metamorphism at amphibolitefacies Inclusion trails in staurolite and andalusiteporphyroblasts suggest that the porphyroblastic growthoccurred after D1 but before D2 The S2 foliation is definedby the alignment of muscovite and biotite which wrapsaround the porphyroblasts and probably developed in D2during M2 As staurolite is locally partially replaced byfine-grained muscovite this foliation may have developedin the greenschist facies This foliation is locallyoverprinted by chloritoid Further west at the contactbetween the Palaeoproterozoic Kerba Granite and theNarracoota Formation a quartzndashkyanitendashtremolitendashfeldspar schist indicates upper greenschist-faciesmetamorphism with the pressure of metamorphismestimated to have been between 3 and 4 kbar (Spear 1993Occhipinti and Myers 1999)
For the most part M2 involved retrogression meta-somatism and local hydrothermal alteration Mineralassemblages formed during M2 are commonly observedin high-strain zones where the S2 schistosity is welldeveloped These include a domain of well-developed D2shear zones south of the Robinson Syncline wherepervasive retrogression of metabasalts to actinolitendashchlorite schist is observed (Pirajno et al 1995a) In
addition in the Mount Pleasant opencut growth of albiteporphyroblasts and the development of chlorite at theexpense of biotite and epidote also occurred during M2
Banded iron-formation in the Robinson RangeFormation shows a change in metamorphic mineralassemblage from east to west across the trend of the D2Robinson Syncline To the west randomly oriented biotiteoverprinted quartz stilpnomelane and iron oxides Theappearance of this late-stage biotite coincides withregional geochemical trends (elevated Sb As and WDavy et al 1999) along the same structure suggesting alate- or post-D2 low-temperature metasomatic eventAlbite porphyroblasts in alteration zones associated withgold mineralization in the Peak Hill Schist also grew at alate stage because they overprint S2
South of the Murchison Fault little-deformed basaltichyaloclastites contain mineral assemblages characteristicof prehnitendashpumpellyite to lower greenschist facies Thissuggests that rocks south of the Murchison Fault were notexposed to the regional greenschist-facies metamorphismor moderate- to high-grade metamorphism that occurredelsewhere in the region
Structural synthesisA number of models have previously been presented toexplain the structural and metamorphic history of theBryahndashPadbury region For these models the driving forcewas assumed to be collisional tectonics related to theCapricorn Orogeny (eg Tyler et al 1998 Occhipintiet al 1998c Pirajno et al 1998b)
Gee (1990 p 207 Gee and Grey 1993) interpretedthe movement of the lsquoYarlarweelor Gneiss Beltrsquo andlsquoMarymia Domersquo in terms of rising lsquosolid-state crystalndashplasticrsquo domes They suggested that the resulting rise andsouthward movement of the lsquoYarlarweelor Gneiss Beltrsquoand lsquoMarymia Domersquo produced recumbent folds in theoverlying sedimentary rocks of the Bryah Basin Furtherrise and convergence of the domes following depositionof the Padbury Group caused complex refolding ThelsquoYarlarweelor Gneiss Beltrsquo was thrust to the east overthe Bryah and Padbury Groups at this time Martin(1994) interpreted the emplacement of the lsquoNarryer
Figure 20 Selected idealized cross sections through the Bryah and Padbury Groups (after Occhipinti et al 1998a) Locationsof a) to c) are shown on Figure 19 (note difference in scale)a) Northeastndashsouthwest section in the central-eastern part of the Bryah and Padbury Basins showing the fault-bendfold model for the Peak Hill Anticline and inferred suture between the Yilgarn Craton (Murchison Terrane) andreworked Archaean Marymia Inlier The extensional fault slice along the northern margin of the craton formed duringearly development of the Bryah Basin (lsquopassive marginrsquo) and was preserved in this idealized section after basinclosureb) Eastndashwest section across the zone of D3 fold and fault structures The section highlights the intense deformationacross the zone between the Billara and Kinders Faults and shows an inferred major detachment (within underlyingmafic volcanic rocks of the Narracoota Formation) zone of highly disharmonic F3 folding mapped at the surfacec) Northndashsouth section in the central-western part of the Bryah and Padbury Basins showing the Yarlarweelor Domethe sheared-out Padbury Syncline and the Murchison Fault as the suture between in situ and reworked ArchaeanNarryer Terrane Note the inferred detachment of the BryahndashPadbury succession along the contact with the NarryerTerraned) The development and onlap of the Padbury Basin onto the underlying Bryah Group
28
Pirajno et al
Gneiss Complexrsquo (lsquoYarlarweelor Gneiss Beltrsquo) as due tolsquolateral escape tectonicsrsquo resulting from the lsquotranscurrentsuturingrsquo of the Yilgarn and Pilbara Cratons during theCapricorn Orogeny Martin (1994) suggested that earlynorthndashsouth movements which changed to localized eastndashwest movements indicate the onset of lsquolateral escapetectonicsrsquo and the eastward expulsion of the northeasternpart of the lsquoYarlarweelor Gneiss Beltrsquo along the Wilthorpeand Kinders Faults In contrast Myers (1989 1990)regarded both the lsquoYarlarweelor Gneiss Beltrsquo and thevolcano-sedimentary rocks of the Bryah and PadburyGroups as allochthonous sheets that were thrust over the
Yilgarn Craton basement and subsequently folded abouteastndashwest axes
An alternative model was presented by Occhipintiet al (1998c Fig 21) who suggested that the Bryah Basindeveloped initially as a rift and the Padbury Basindeveloped over the Bryah Basin in a retroarc foreland-basin setting (see also Martin 1994) Formation of thePadbury Basin in a compressional regime was essentiallyconcommitant with the closure of the Bryah Basin and thedevelopment of D1 structures as subhorizontal shear zonesbetween the Archaean Narryer Terrane basement and the
Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group anddeformation fabrics
Formation Rock type Mineralogy Pre-S1 S1 Post-S1 S2ndashS3 Post-tectonicM1 M2
Peak Hill Schist pelite quartz biotite muscovite chlorite albite tourmaline
chemical sediment quartz spessartine magnetite
calc-silicate quartz epidote chlorite actinolite titanite magnetite
psammite quartz muscovite andesine opaques
Narracoota metabasite quartz actinolite epidote chlorite sericite arfvedsonite titanite calcite
volcanic breccia albite pumpellyite
Ravelstone pelitic tourmalinite quartz muscovite tourmaline garnet feldspar
subarkosic wacke quartz biotite albite sericite tourmaline
Horseshoe banded iron-formation quartz biotite grunerite spessartine chlorite
Robinson Range banded iron-formation quartz stilpnomelane biotite
NOTE No data are available for the Labouchere and Wilthorpe Formations
29
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
supracrustal rocks of the Bryah and Padbury Groups Theoverall movement direction was interpreted as being fromnorth to south but locally because of the possible effectof later dextral shear movement may actually have been
ram
p
Peak Hill Anticline
N S
eg Kinders Fault Peak HillAnticline
Thrust flatrsquo Lateral
ramp Obliq
ue
lateral ramp
Yarlarweelor
Basalthrustplane
2Dc)
d)
2D thrust flat
rsquo
eg Yarlarweelor gneiss complex
gneiss complex
Padbury Group
Bryah Group
Reworked Archaean granite
a)
Archaean granite
b)
2prospective D crustal thrustwith frontal ramp
1D tectonic interleaving zone(eg Peak Hill Schist)
1 2Post-D and pre-D
D tectonic interleaving between reworked Archaeancrust ( underplate) and BryahndashPadbury succession
rsquo1
Post-D D2 3
W E
Thrust ramp
Thrustfrontal
Later
al ra
mp
FMP374 011199
W E
N
Thrust flatrsquo
movement
Thrust
North to south
e)
ramprsquo
flatrsquorsquo
2D thrust flat ndash frontal ramp ndash lateral ramp geometry
Figure 21 Model of the structural development of the BryahndashPadbury Group succession (after Occhipinti et al1998a)a) Zone of D1 subhorizontal tectonic interleaving(by thrust duplexing) between reworked Archaeancrust and overlying rocks of the BryahndashPadburysuccession This zone includes high-strain ormylonitic rocks formed by lsquounderplatingrsquo of theArchaean rocks beneath the volcano-sedimentaryrocks during initial closure of the Bryah back-arcbasinb) Post-D1 geometry with trace of incipient D2crustal-scale thrust with frontal rampc) D2 geometry with fault-bend anticline developedabove the crustal D2 thrust ramp Upright folds inthe volcano-sedimentary succession (eg Padburyand Robinson Synclines) formed ahead of themain thrustd) Post-D2D3 geometry along schematic eastndashwestsection D2 fault-bend anticlines are not shownNorth-to-south movement ie movement towardsviewer leads to eastndashwest compression and hencenorthndashsouth folds and reverse or thrust faults in thedepression between (oblique) lateral ramps at thesame time as eastndashwest D2 folding occurredelsewheree) Schematic view looking north-northwest of thebasal thrust fault with frontal and lateral rampshighlighting the north-to-south movement directionof the thrust sheet
northwest to southeast Substantial movement and highstrains can be inferred from tectonic interleaving (egbetween the Billara and Wilthorpe Faults Fig 19) andfrom the development of the mylonitic zones in possiblethrust duplexes in the Peak Hill Schist Other possibleD1 structures in particular subhorizontal thrust faultsmay have locally developed along the contacts betweenthe Bryah and Padbury Groups Small-scale earlylayer-parallel folds in chert and BIF layers particularlyfrom within the Padbury Group suggest that subhorizontalD1 structures locally formed within the volcano-sedimentary succession (Pirajno and Occhipinti 1998Swager and Myers 1999) Deposition of the PadburyGroup in a retroarc foreland basin (Martin 1994)was probably contemporaneous with the early stagesof D1
The Yarlarweelor gneiss complex and Peak Hill Schistwere described by Occhipinti et al (1998c) as lsquobasement-cored anticlinesrsquo that developed above frontal thrust rampsThe overlying supracrustal rocks and their high-strain D1contact zones were folded by north to south movementover these ramps during D2 deformation In the Peak HillSchist subhorizontal D1 folds are refolded about anupright apparently easterly trending D2 antiformThe hinge of this fold may be sheared out along thecontact with the Marymia Inlier which is marked by aquartz blastomylonite previously mapped as deformedquartzite of the Juderina Formation (Adamides 1998) Theoriginal orientation of the D2 fold may have been east-northeasterly The Peak Hill Schist outcrops around adomal structure produced by refolding of the D2 fold aboutan approximately northerly trending D3 fold-axial surfaceIt was argued by Occhipinti et al (1998c) that the D3 foldsdeveloped in a structural lsquodepressionrsquo between the two
30
Pirajno et al
basement-cored anticlines which acted as lateral rampsin the thrust plane Northerly trending structures developedduring northndashsouth compression as the lateral ramps wereslightly oblique to the movement direction leading tospace problems between the basement-cored anticlinesThis resulted in either lateral shortening or verticalexpulsion (or both) of the Bryah and Padbury Groups
Occhipinti et al (1998c) assumed that the Yarlarweelorgneiss complex (referred to by them as the NarryerTerrane) was an Archaean crustal fragment that influencedthe structural deformation in the Palaeoproterozoic Bryahand Padbury Groups but was not itself largely deformedduring the Palaeoproterozoic Subsequently Sheppard andSwager (1999) and Occhipinti and Myers (1999)recognized Palaeoproterozoic deformation meta-morphism and felsic magmatism within the Yarlarweelorgneiss complex This indicates that the Yarlarweelor gneisscomplex was extensively reworked during the Palaeo-proterozoic and underwent the same D2ndashM2 metamorphicevent that has been recognized in the Bryah and PadburyGroups and Peak Hill Schist
Occhipinti et al (1998b) found that Palaeoproterozoiccoarse-grained granites and pegmatites with ages between1820 and 1780 Ma (Nelson 1998) intruded as sheetssynchronously with the D2 deformation event D McBMartin (1999 pers comm) interpreted granite exposedsouthwest of the Labouchere opencut as intruding thePadbury Group sedimentary rocks and suggested that thisgranite may also be of this age Intrusion of granitoiddykes and sheet-like plutons accompanied uplift of theYarlarweelor gneiss complex and is interpreted as beingconcomitant with dextral shearing in the region andpossibly D3 (Occhipinti et al 1998a Sheppard andSwager 1999) This movement was attributed to anoblique northndashsouth to northwestndashsoutheast collision ofthe Pilbara and Yilgarn Cratons during the CapricornOrogeny (Occhipinti et al 1998b 1999)
In the northwestern part of the Bryah and PadburyBasins the metamorphic grade increases from greenschistfacies in the east to amphibolite facies in the west Furtherwest in the Yarlarweelor gneiss complex the metamorphicgrade reached at least upper amphibolite facies (Sheppardand Swager 1999) Uplift of the Yarlarweelor gneisscomplex from 9ndash10 kbar to greenschist facies occurredbetween c 1812 and c 1800 Ma (Occhipinti et al 1998b)The c 1812 Ma granitoid sheets and dykes were meta-morphosed at high grade (see below) whereas c 1800 Magranites were only metamorphosed to greenschist facies(Occhipinti et al 1998b) Medium-grade metamorphismof the Padbury Group is solely preserved adjacent to theYarlarweelor gneiss complex between the Billara andWilthorpe Faults (see Metamorphism Fig 18 Plate 1)The drop in metamorphic grade to greenschist facies only15 ndash 25 km east of the contact suggests either a rapidincrease in temperature close to the Yarlarweelor gneisscomplex or that amphibolite-facies or upper greenschist-facies (or both) Bryah and Padbury Group rocks have beenfaulted out The latter explanation is preferred because theboundary between amphibolite-facies and lower to middlegreenschist-facies rocks of the Labouchere Formation issharp
In the Bryah and Padbury Groups and Peak Hill Schistmetasomatism accompanied retrogression of D1ndashM1assemblages to greenschist facies during M2 particularlyin D2 shear zones In the Yarlarweelor gneiss complexthere is no evidence for D1ndashM1 and M2 was initially ahigh-grade metamorphic event with the formation ofincipient minimum melt during the early stages of D2(Occhipinti et al 1998b) Post-M2 the metamorphic gradedropped significantly to greenschist facies
In the proposed model shown in Figure 22 the BryahGroup developed in a back-arc lsquorift-type settingrsquo (Pirajnoet al 1998b see Tectonic model and conclusions) If theBryah and Padbury Groups are c 20 Ga or older then D1structures could have developed during the c 20 GaGlenburgh Orogeny (Occhipinti et al 1999 Tyler 1999)as a result of west to east or northwest to southeastcompression Plutonism in the future Yarlarweelor gneisscomplex produced the 1960 Ma felsic granitoid rocksduring the late stages of D1 (Sheppard et al 1999Fig 22c) Alternatively if the Bryah and Padbury Groupswere deposited sometime between c 1945 and 1812 MaD1 could have developed during the c 18 Ga CapricornOrogeny due to north-northwest to south-southeastcompression (Figs 22 and 23) Further geochronologicalwork is required to establish the age of D1 and thedepositional age of the Bryah and Padbury Groups
In either case closure of the Bryah Basin took placeduring D1 with deposition of the Padbury Group in aretroarc foreland basin overlying the Bryah Group andpossibly the lsquofuturersquo Yarlarweelor gneiss complex(Fig 22b) D1 deacutecollements would have developedbetween the Bryah and Padbury Groups the futureYarlarweelor gneiss complex and the Peak Hill Schist(Figs 22b and 23a) Duplexes developed in the Peak HillSchist during D1 and it was detached from the MarymiaInlier (Fig 23b) In addition early D1 faults and foldsformed between and within the Bryah and PadburyGroups
The second deformation event D2 occurred during theCapricorn Orogeny Early in D2 approximately northwestto southeast compression caused further thickening of theBryah and Padbury Groups over the Yarlarweelor gneisscomplex destabilizing this piece of crust (Figs 22b and22c) The resulting increased pressure and temperaturemay have caused the underlying Archaean crust to startto melt This melt produced the c 1820 to c 1812 Mafelsic granitoid rocks (Occhipinti et al 1998a Sheppardand Swager 1999 Sheppard et al 1999) that intruded theupper parts of the Yarlarweelor gneiss complex as veinsand sheets (Sheppard and Swager 1999 Fig 22c) Asthese developed synchronously with the deformation (D2)they were commonly folded into upright steeply toshallowly plunging isoclinal to open folds These rockswere also metamorphosed at high grade during the D2deformation event Regionally this metamorphismcorresponds to M2
Padbury Group sedimentary rocks were meta-morphosed to medium grade along contact zones withthe Yarlarweelor gneiss complex during M2 This high- andmedium-grade metamorphism may have releasedfluid that moved through faults and shear zones and
31
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Figure 22 Schematic sections illustrating the proposed model of the structural development of the BryahndashPadburyGroup succession in the westa) Development of the Bryah Group pre-D1 over the Proto-Yarlarweelor gneiss complex and the northernmargin of the Yilgarn Craton in an extensional-rift settingb) Early- and syn-D1 deposition of the Padbury Group in a fold-and-thrust belt foreland-basin type settingover the Bryah Group Inversion of the Bryah rift-basin by possible reversal of D1 normal faultsDevelopment of D1 faults between the Bryah Group Padbury Group Yarlarweelor gneiss complex andYilgarn Cratonc) D2 to D3 local interleaving of the Bryah and Padbury Groups with the development of folds and faultsDeformation of the Bryah and Padbury Groups above basal detachments Early D1 faults refolded aboutD2 or D3 folds Formation of c 1810 Ma leucocratic granite locally associated with incipient minimum meltin the Archaean gneiss component of the Yarlarweelor gneiss complex Later at c 1800 Ma sheet-likeplutons developed particularly along the faulted boundaries between the Yarlarweelor gneiss complexand Bryah and Padbury Groups
Deposition of Padbury GroupEarly D
Development of fold and thrustbelt in D
1 1
Inversion of Bryah rift
1
Murchison Fault
Karalundi Formationequivalents Bryah Group
Hyaloclastites
Proto-Yarlarweelorgneiss complex
Post-rift phase
Thickening of supra-crustal succession over
Proto-Yarlarweelorgneiss complex
a)
b)
c)
v
SAO62 130300
Formation of c 1810 Ma leucocratic coarse-grained granitein Yarlarweelor gneiss complex (Sheppard et al 1999)
Deformation of the Yarlarweelor gneiss complex
NNW1
SSE
1
2 3
Early- and syn-D
Mafic and ultramaficvolcanic rocks
Early reversal of D normal faults some possible back thrustingof volcanic rocks below detachments cut by detachments
Folded c 1960 MaYamagee granite
Local plutonism into Proto-Yarlarweelor gneiss complex
at c 1960 Ma forming Yamageegranite of Sheppard and Swager (1999)
Pre-D extensionndashrift phase
D ndashD
Bryah Group
Proto-Yarlarweelorgneiss complex
Padbury Group
32
Pirajno et al
metasomatized M1 assemblages in the Bryah Group andPeak Hill Schist rocks during M2ndashD2 Elsewhere in theregion during D2 the Peak Hill Schist and Bryah andPadbury Group rocks were folded into tight to isoclinalupright folds with mainly easterly to northeasterly trends(Occhipinti et al 1998c) Post-D2 during D3 theYarlarweelor gneiss complex was uplifted and retrogressedto greenschist facies This uplift in a dextral strike-slipregime may have been accommodated by steeply dippingnormal faults between the Yarlarweelor gneiss complexand the Bryah and Padbury Groups (Figs 17 and 18) thathave now been inverted (Fig 24)
In the Peak Hill Schist subhorizontal D1 mylonitezones and rootless folds are refolded about an easterly oreast-northeasterly trending upright D2 antiform The domalshape of the Peak Hill Schist is an artefact of a northerlytrending upright D3 antiform refolding the D2 antiformThe Yarlarweelor gneiss complex apparently does notcontain D1 folds although shearing along basementndashcovercontacts between the Yarlarweelor gneiss complex and theBryah and Padbury Groups may have developed duringD1 (Fig 22b) The D2 fold-axial surfaces within the
Yarlarweelor gneiss complex parallel the arcuate faultedboundary with the Bryah and Padbury Group rocks Thischange in the trend of D2 may be explained in terms of afault-bend fold developed during dextral shearing(Occhipinti and Myers 1999) that may have accompanieduplift during D3
MineralizationThe mineral resources of the Peak Hill SchistBryah Group and Padbury Group are considerableconsidering the relatively small total area of thesebasins (about 6000 km2) These resources include goldmanganese iron ore talc and silver Pirajno andOcchipinti (1995) discussed the mineral potential of theBryah Basin and Pirajno and Preston (1998) described themineral deposits of the BryahndashPadbury region and PeakHill Schist Mineral production and defined resourceswithin these tectonic units as at 30 June 1999 arepresented in Tables 7 and 8 Known deposits andoccurrences are listed in Table 9
Figure 23 Schematic section illustrating the proposed model for the structural development of theBryahndashPadbury Group succession and the Peak Hill Schist a) Development of the BryahGroup in a rift setting pre-D1 over the Marymia Inlier (Yilgarn Craton) b) D1 closure of theBryah lsquoriftrsquo inversion of normal faults deposition of the Padbury Group and formation ofthe Peak Hill Schist
Future D fault
NNW SSE
Bryah Group
Basement
Proto-Peak Hill Schist
Pre-D extensionndashrift phase1
1Peak Hill Schist
D faults1
1
Rift closes Peak HillSchist develops as a
strongly duplexed packageof rock
Marymia Inlier
a)
b)
SAO63 150300
Padbury Group
Early- and syn-D
Mafic and ultramafic volcanic rocks
33
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The mineral deposits of the Peak Hill Schist andBryah and Padbury Groups include mesothermal-stylegold-only lodes volcanogenic massive sulfide (VMS)copperndashgold supergene-enriched manganese bandediron-formation iron ore and talc in metasomatizeddolomitic rocks The distribution of these mineral depositsis shown in Figures 25 and 26 and Plate 1
Gold depositsThe most important mineral deposits exploited to datehave been the mesothermal-style gold-only lodes all ofwhich are in the Peak Hill Schist and the Bryah andPadbury Groups If the area occupied by these groupsalone is taken into account (about 6000 km2) then theidentified contained gold per unit area is 125 kg goldkm2The mesothermal gold deposits including past and presentproducers include Peak Hill Jubilee and Mount Pleasantin the Peak Hill Schist Harmony Mikhaburra WembleyCashman and Ruby Well in the Bryah Group (Figs 25and 26) and Horseshoe Labouchere Nathans DeepSouth and Fortnum in the Padbury Group The Wilthorpedeposit is hosted in Upper Archaean granitic rocks whichare tectonically interleaved with rocks of the Bryah andPadbury Groups
The total gold produced is 595 t with total (producedplus remaining inferred indicated and measured)resources estimated at approximately 75 t of containedgold The Labouchere and Fortnum areas containthe regionrsquos largest pre-mining resource estimated as 333 tof contained gold at a grade of about 24 gt goldApproximately two-thirds (225 t) has been exploited
largely between 1989 and 1995 with the remainingresource (107 t) being in the Fortnum area Details of theLabouchere and Fortnum deposits can be found in Hannaand Ivey (1990) and Hill and Cranney (1990) respectivelyThe area around the Peak Hill opencut (includingRavelstone) has produced approximately 20 t of fine goldat an average grade of 4 gt gold more than half of whichhas been extracted in the last 13 years Remainingmeasured and indicated resources are estimated at about47 t of contained gold The Harmony deposit (NewBaxters Find) which was recently exhausted had totalpre-mining resources estimated at about 92 t with a gradeof 35 gt gold
The lode deposits are hosted in mylonitic schistmetasedimentary rocks metavolcanic rocks or along theircontact zones They are spatially associated with high-strain zones and hydrothermal alteration dominated bypyrite quartz muscovite biotite and alkali feldspars Themineralization is in ductile and brittlendashductile shears (egPeak Hill) and in discrete brittle fractures (eg Cashman)indicating a relationship of structural style with therheology of the host rocks The development of ductilebrittlendashductile and brittle structures (zones of highpermeability) was accompanied by infiltration ofhydrothermal fluids which produced alteration andmineralization The precise timing of the mineralizationis difficult to ascertain Windh (1992) suggested syn-D3but from field and petrological observations it is morelikely that circulation of mineralizing fluids occurredduring a continuum related to D1ndashD2 tectonism andmetamorphism under conditions of ductile or brittlendashductile regimes with perhaps some remobilization intobrittle structures occurring during D3 Lead isotope data
Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneisscomplex and then into the Bryah and Padbury Basins showing the possible present-day configuration of these units
Kerba FaultBangemall BasinFault boundary
YILGARNCRATON
vv
v
vv
v
vv
vv v
v
v
v vv v
vvv
vvv
vvv
vv
Errabiddy
Shear ZoneGascoyneComplex
Possible currenterosion level
SAO64 130300
NW SE
SeabrookndashMurchison Fault
v v
Bangemall Group
Yarlarweelor gneiss complex
Bryah and Padbury Group rocks
Cooinbar Fault
34
Pirajno et al
Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
_______________________ Production (P) _______________________ _______ Remaining resources (R) ________ TotalMining centre Ore Contained Alluvial Dollied Total Resource Ore Contained pre-miningor mine metal contained type metal resources
metal (P+R)(kt) (kg) (kg) (kg) (kg) (kt) (kg) (kg)
Pre-1986
Mount Fraser Mining Centre 09 24 27 13 288 ndash ndash ndash 288Mount Seabrook Mining Centre 17 383 ndash 02 385 ndash ndash ndash 385Ravelstone Mining Centre 49 1058 ndash 32 109 ndash ndash ndash 109Wilthorpe Mining Centre 01 15 ndash ndash 15 ndash ndash ndash 15Peak Hill sundry parcels 27 7706 889 139 8734 ndash ndash ndash 8734Peak Hill Mint deposits(a) ndash ndash 25 33 58 ndash ndash ndash 58Ruby Well Mining Centre 85 146 325 142 1927 ndash ndash ndash 1927Horseshoe Mining Centre 9049 2 9669 352 889 3 091 ndash ndash ndash 3 091Peak Hill Mining Centre 6217 8 200 367 628 8 2995 ndash ndash ndash 8 2995
1986 to 30 June 1999
Horseshoe Lights(b) mine 9059 3 7373 217 ndash 3 759 ndash ndash ndash 3 759Fortnum mine 5 832 15 6025 377 ndash 15 6402 MES + IND 2 221 7 542 23 1822
INF 991 3 194 3 194Labouchere mine 2 9108 6 9052 ndash ndash 6 9052 ndash ndash ndash 6 9052Mount Pleasant mine 1449 433 ndash ndash 433 ndash ndash ndash 433Peak Hill mine 6 5738 20 1266 908(c) ndash 20 2174 MES + IND 2 200 4 760 24 9774
Total 17 9128 59 0577 3487 1878 59 595 5 412 15 496 75 091
NOTES (a) Gold from the Peak Hill Mining Centre deposited at the Perth Mint(b) Horseshoe Lights also produced 261 675 t of copper concentrates containing 25803 kg of gold(c) Includes 625 kg of gold produced from retreated tailingsMES Measured resources IND Indicated resources INF Inferred resources
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
35
GSW
A R
eport 59G
eology and mineralization of the P
alaeoproterozoic Bryah and P
adbury Basins W
A
Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
_____ Production (P) to 300699 _____ __________________ Remaining resources (R) __________________ Total resource (P+R)Commodity Mine Ore or concentrate Contained metal Resource type Ore or concentrate Contained metal Contained metal
(t) (t) (t) (t) (t)
Copper and Cashman 7 11 ndash ndash ndash 11cupreous ore Peak Hill sundry 63 223 223
Horseshoe Lights 261 675 49 159 Indicated 2 080 000 22 897 72 056Inferred 3 340 000 22 879 22 879
Total 261 745 49 1824 5 420 000 45776 94 9584
Manganese Horseshoe 489 895 203 899 Measured + Indicated 80 000 21 000 224 899Inferred 205 000 100 000 100 000
Mount Fraser 228 108 Measured + Indicated 32 000 9 000 9 108Mount Padbury 7 319 3 498 Measured + Indicated 5 000 2 000 5 498Ravelstone (Peak Hill) 76 237 36 938 ndash ndash ndash 36 938Total 573 679 244 443 Measured + Indicated 117 000 32 000 276 443
Inferred 205 000 100 000 100 000
Iron Robinson Range ndash ndash Inferred 10 000 000 6 000 000 6 000 000
Talc Mount Seabrook ndash Livingstone ndash 540 416 Indicated ndash 1 470 000 2 010 416Inferred ndash 250 000 250 000
Total ndash 540 416 ndash 1 720 000 2 260 416
Silver Horseshoe Lights (post-1982) ndash 72 7194 kg ndash ndash ndash 72 7194 kg(by-product) Peak Hill general ndash 1182 kg ndash ndash ndash 1182 kg
(including Horseshoe pre-1983)Total ndash 72 8376 kg ndash ndash ndash 72 8376 kg
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
36
Pirajno et al
Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins (modified from Pirajnoand Preston 1998 see also Plate 1)
Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
Mine (M) AMG coordinates Principal Mineralization style Expression Ore minerals Relationshipprospect (P) or Easting Northing commodity to hostoccurrence (O)
Cashman (M) 662129 7126994 Gold Regolith enrichment Outcrop Gold Discordantand mesothermal lode
Durack (P) 670440 7150520 Gold Mesothermal lode Drill Gold pyrite Discordantintersections magnetite
Harmony (M) 664145 7161267 Gold Regolith enrichment Drill Gold chalcopyrite Discordantand primary intersections pyrrhotite scheelitemesothermal lode pentlandite pyrite
Heines Find (P) 682759 7145164 Gold Mesothermal lode Outcrop Gold Discordant
Horseshoe (P) 656994 7183734 Gold Eluvial Gold ndash
Horseshoe (P) 657579 7184413 Gold Eluvial Gold ndash
Horseshoe (P) 661219 7182977 Gold Eluvial Gold ndash
Horseshoe (P) Copperndashgold Multiple veins Outcrop Gold Discordant
Horseshoe 662648 7193894 Copperndashgold Supergene enrichment Gossan Chalcocite pyrite DiscordantLights (M) of VHMS chalcopyrite native
copper and gold
Jubilee (M) 671889 7165443 Gold Mesothermal lode Quartz vein Gold pyrite Discordant
Labouchere (M) 627730 7204710 Gold Mesothermal lode Not known Gold pyrite Discordant
Livingstone (M) 567540 7171032 Talc Replacement Outcrop Talc Discordant
Mikhaburra (P) 656252 7130396 Gold Multiple veins Outcrop Gold Discordant
Mount Pleasant (M) 674287 7162089 Gold Mesothermal lode Outcrop Gold pyrite Discordant
Mount Seabrook (M) 572631 7168338 Talc Replacement Outcrop Talc Discordant
Nathans Deep 631713 7198812 Gold Mesothermal lode Not known Gold pyrite DiscordantSouth (M)
Peak Hill (M) 672190 7163003 Gold Mesothermal lode Quartz vein Gold pyrite altaite Discordantchalcopyritebismuthotelluridemolybdenite magnetite
Ravelstone (M) 665734 7166777 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ravelstone (M) 669313 7166423 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ruby Well area (M) 674665 7129915 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 672600 7124378 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 674142 7127027 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677928 7129727 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677408 7130112 Gold Eluvial ndash Gold ndash
St Crispin (P) 691358 7158940 Gold Mesothermal lode Outcrop Gold Discordant
Trevs Starlight (M) 636412 7198887 Gold Mesothermal lode Not known Gold pyrite Discordant
Unnamed (O) 611598 7168985 Variscite Not known Not known Variscite Discordant
Unnamed (O) 611909 7167084 Variscite Not known Not known Variscite Discordant
Unnamed (P) 656664 7185310 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Wembley (P) 663983 7149044 Gold Mesothermal lode Outcrop Gold Discordant
Wilgeena (M) 685369 7155622 Gold Mesothermal lode Outcrop Gold Discordant
Wilthorpe (M) 630414 7176521 Gold Mesothermal lode Outcrop Gold pyrite galena Discordantarsenopyrite
Yarlarweelor (M) 636723 7196423 Gold Mesothermal lode Not known Gold pyrite Discordant
37
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
MARYMIAINLIER
MARYMIAINLIER
Jenkin
FaultGROUPBANGEMALL
Murchison Fault
NARRYERGNEISS
TERRANE
Padbury Bryahand
Yerrida Basins
FMP100b 181099
1000 km
5
67 16
8
9
17
23
4
11
10
15
1213 14
19
18
21
20
1
GOODININLIER
YILGARNCRATON
YILGARN
CRATON
Goodin
Fault
118deg30 119deg30
Killara
Narracoota
Mt Padbury
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
Yandil
119deg30
Milgun30 km
Jamindi Three Rivers Marymia
PEAK HILLROBINSON
RANGE
Padbury Bryah Doolgunna Thaduna
Glengarry Mooloogool Mount Bartle
MerewetherYanganooGabanintha
119deg00
25deg30
26deg30
26deg00
25deg30
GLENGARRY
Milgun
Mesothermal Au AundashCu
Shear zone-hosted Cu
Epigenetic Pb
Supergene Mn
2 Jubilee
5 Labouchere
7 Fortnum group8 Horseshoe Lights9 Horseshoe gold
10 Wilthorpe11 Wembley
12 Mikhaburra13 Cashman14 Ruby Well
group (including Elsa)
16 Horseshoe magnagese17 Ravelstone18 Robinson Range BIF
(no specific locality)19 Thaduna20 PGE-bearing gossan21 Magellan
3 Mount Pleasant4 Harmony
(New Baxters Find)Fault
Geological boundary
Bouguer gravity anomaly
Peak Hill Schist
Karalundi FormationGR
OU
PB
RY
AH
Padbury Group
Horseshoe and Ravelstone Formations
schistmetabasaltic hyaloclastiteNarracoota Formation mafic and ultramafic
Archaean basement
Earaheedy Group
WindplainSubgroup
MooloogoolSubgroup
YE
RR
IDA
GR
OU
P
Maraloou Formationintercalated Killara and Maraloou FormationsDoolgunna and Thaduna Formationswith intercalated Killara FormationJuderina and Johnson Cairn Formations
Homestead
Bangemall Group
Microgabbro dyke
BryahPEAK HILL
1100 000 map sheet 1250 000 map sheet
Aeromagnetic lineament
6 Nathans Deep South
15 Mount Padbury ndash Mount Fraser
Volcanogenic massive sulfide
Shale-hosted stratabound sulfides
MINERALIZATION STYLE
MINERAL DEPOSITS
38
Pirajno et al
Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet (after Pirajno and Occhipinti 1998)
Ravelstone Formation
Karalundi Formation
Horseshoe Formation
Granitoid rock and gneiss
Narracoota Formation
10 km
040400
Yerrida Group
Bangemall Group
Earaheedy Group
Padbury Group
Bry
ah G
roup
Prospect
Producer
JubileeGroup
Peak Hill
Harmony
Wilgeena
Wembley
DurackWell
HeinesFind
Mikhaburra
CashmanGroup
Ruby WellGroup
Goodin Find
Ravelstone Group
(Hit or Miss)
St CrispinWilsons Find
25deg30
118deg
30
119deg
00
26deg00
Mar
ymia
Inlie
r mylonite
Syncline
Anticline
Overturned syncline
Peak Hill Schist
Thrust fault
Fault
Strike-slip fault
FMP162a
Supergene manganese deposit
Alluvialndasheluvial gold deposit
Mesothermal gold lodes
Mount Pleasant
39
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(palaeo-isochrons) suggest that in the Bryah and PadburyBasins mineralization occurred between 192 and 17 Ga(Windh 1992 Thornett 1995) The results of lead isotopicstudies also indicate that the lead was derived from YilgarnCraton rocks (Dyer 1991 Windh 1992 Thornett 1995)although there is a suggestion that the lead from thePeak Hill deposit is similar to that from a galena in theMarymia gold deposit in the Marymia Inlier (McMillan1993)
The nature of the mineralizing fluids is poorlyconstrained Alteration assemblages at the Peak Hill andMount Pleasant deposits indicate that the ore fluids wereenriched in Fe K Na S B CO2 SiO2 and H2O (Thornett1995) Fluid inclusion studies of mineralized materialsfrom the Fortnum and Labouchere gold deposits (Dyer1991 Windh 1992) indicate that the ore fluids wererich in H2O and H2OndashCO2 with salinities of 7ndash12 wtand 5ndash17 wt NaCl equivalent respectively Micro-thermometric measurements (Dyer 1991 Windh 1992)indicate temperatures ranging from approximately 170degto 320degC
Peak Hill Jubilee and Mount Pleasantdeposits
Mine geologists subdivided the Peak Hill Jubilee andMount Pleasant lithologies into the Core sequence HoneyQuartzite Intermediate sequence Mine sequence MarkerQuartzite and Hangingwall sequence
The Core sequence is at the structural base and wellexposed in the Mount Pleasant opencut where it reachesa thickness of 55 m The contact with the Intermediatesequence is marked by the Honey Quartzite which is amylonite consisting of laminated or ribbon quartz TheCore sequence rocks have a mylonitic fabric and are madeup of quartzndashbiotitendashcarbonatendashmuscovite(ndashepidotendashhornblendendashgarnetndashmagnetitendashpyrite) locally withabundant very fine zircons and monazite in the biotite-richvarieties (Barrett 1989) At Mount Pleasant as mentionedabove graphitic schist is present near the top andassociated with a zone of chloritendashbiotite(ndashgarnet) schistwith albite porphyroblasts (Fig 27) containing inclusionsof monazite and zircon Geochemical discriminant plotsusing immobile elements suggest either a granitic (Nb SrLa and Ce) or maficndashintermediate (Ni Cr and Ti)protolith (Thornett 1995) Barrett (1989) on the otherhand proposed that much of the Core sequence could bederived from a sedimentary protolith The origin of thealbite porphyroblasts is uncertain Based on geochemistrypetrology and textural features Thornett (1995) advocateda combined hydrothermal ndash retrograde metamorphicorigin and compared the Peak Hill ndash Mount Pleasantalbites to those studied by Watkins (1983) in the Dalradianschists of Scotland Another possibility that could accountfor the presence of the albite porphyroblasts is lsquoreactionsofteningrsquo as proposed by Dixon and Williams (1983)These authors advanced the hypothesis supported bygeochemical and mineralogical data that mylonitizationof a quartzofeldspathic parent may be accompanied bymineralogical changes involving the breakdown ofplagioclase with release of Na2O and to a lesser extent
CaO and formation of muscovite This would result in theproduction of quartzndashmuscovite mylonites and sodium-rich fluids
The Intermediate sequence is discontinuous withlayers up to 2 m thick and is composed of a quartzndashmylonite-bearing white mica The Intermediate sequencelies above the Honey Quartzite has an estimated thicknessof between 200 and 400 m and forms the footwall to theMine sequence at Peak Hill and the hangingwall to theore zones at Mount Pleasant The Intermediate sequenceis dominantly quartzndashmuscovite schist with minorplagioclase biotite microcline carbonate and chloriteBarrett (1989) interpreted this rock as either a felsicporphyry or an arkose The lower part of the Intermediatesequence consists of mainly biotite schist with garnet andepidote Rocks of the Intermediate sequence exhibitmillimetre-scale metamorphic differentiation layeringwhich define a dominant S2 schistosity (Thornett 1995)This is interpreted by the present authors as a typicalmylonitic structure
The Mine sequence mostly found in drillholes ischaracterized by biotite ndash white mica(ndashchloritendashcarbonatendashamphibolendashgarnetndashalbite) schist and graphite schist(Fig 28) and may be 40 to 50 m thick Drillcore samplesof a hornblendendashplagioclasendashquartz rock (with garnetporphyroblasts) have been interpreted as an unalteredamphibolite (Barrett 1989 Thornett 1995)
The Marker Quartzite is a recrystallized quartzmylonite (lsquoMarker Chertrsquo of mine geologists)1 to 3 m thick at the top of the Mine sequenceOutcrops of Marker Quartzite exhibit radiating iron-oxidepseudomorphs after acicular crystals and iron-oxidepseudomorphs after porphyroblasts Windh (1992)identified these acicular crystals using the scanningelectron microscope as grunerite The porphyroblastpseudomorphs are possibly after garnet
The Hangingwall sequence can be up to 700 m thickand is made up of white mica ndash magnetite(ndashgarnetndashchlorite) mafic schist and metabasite The latter is locally
Figure 27 Albite porphyroblasts in mylonitic schist at theMount Pleasant deposit
40
Pirajno et al
garnetiferous and characterized by a metamorphic (andhydrothermal) assemblage containing variable amountsof hornblende plagioclase quartz garnet epidote andtitanite The metabasite is overlain by mylonitic schistcontaining mainly quartzndashplagioclasendashbiotite and locallyassociated with zones of albitendashmuscovite and garnetndashepidote (calc-silicate)
The Peak Hill Jubilee and Mount Pleasant depositswere studied by Barrett (1989) who based most of hiswork on drillcore samples and Thornett (1995) Theseauthors provided much of the information summarizedbelow augmented by data from this study The Peak HillJubilee and Mount Pleasant gold deposits are situated inthe west-northwestern portion of the Peak Hill Anticlineand hosted in the Peak Hill Schist (Figs 4ndash7 and 26) Inthe mine areas the rocks are intensely weathered to depthslocally exceeding 200 m Weathering products arepredominantly kaolinitic clays and iron oxyhydroxidesThis weathering is particularly well developed in zonesof hydrothermal alteration which in turn are related tohigh-strain zones the latter having facilitated percolationof meteoric waters Hydrothermal alteration is dominatedby sulfidation (pyrite) and alkali metasomatism (biotiteand albite) and contained within late-stage quartzndashcarbonate veins hosted in highly strained metabasites andquartz mylonites Other important alteration mineralsinclude iron-rich chlorite sericite garnet tourmalinedolomite and calcite In all about 20 t of gold has beenproduced
The Peak Hill mineralization was exploited in threeadjoining pits which from north to south are FivewaysPeak Hill Main and Mini In plan view (Fig 29) the entirePeak Hill mineralized system is contained within apackage of mylonitic schist (Mine sequence) at thefootwall of northerly trending and westerly dippingshear zones The mylonitic schist contains quartz podsveins lenses and stringers and locally graphitic quartzmylonite units (Marker Quartzite see below and Fig 30)The Mine sequence contains lenses of mafic rocks (egmetadolerite) The overall picture is one of a complex zoneof shearing and tectonic interleaving between rocks of the
FIVEWAYSPIT
MINIPIT
MAINPIT
100 m
sequence
Mine sequence
Intermediate sequence
Vein quartz
Marker Quartzite
Shear zone
Anticline
FMP160 271099
Hangingwall
Geology notmapped
Geology notmapped
N40
42
45
40
25
45
45 26
30
42
45
Fault42
Cleavage
Foliation
Figure 28 The Mine Sequence schist at the Peak Hill depositshowing biotite alteration the biotite is partlyretrogressed to chlorite plane polarized light
Figure 29 Schematic geological map of the Fiveways Mainand Mini opencuts Peak Hill deposit (after Thornett1995)
Figure 30 Peak Hill Mini opencut showing the ore-bearingmylonitic schist graphitic schist (dark bands) andMarker quartzite unit (above the upper graphiticschist)
41
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Narracoota Formation and Peak Hill Schist Kinematicindicators (CndashS surfaces) indicate a thrust movement fromwest to east (Thornett 1995)
The main orebody has a westerly dip ranging from20deg to 50deg (averaging 35deg) and is hosted in rocks of theMine sequence High-grade zones can contain up to30ndash40 gt gold The ore zones are characterized bypervasive alteration consisting of chloritendashbiotitendashquartzndashcarbonatendashgraphite The principal ore minerals arepyrite chalcopyrite and gold Other ore minerals includealtaite tetrahedrite bismuthotelluride molybdenite andvarious bismuthndashleadndashtellurium compounds The goldmineralization is thought to have been emplaced in at leasttwo stages In the first stage gold mineralization wasemplaced along the contact between the Marker Quartziteand the Mine sequence (see below) During the secondstage cross-faults were formed with the gold beingredistributed or rearranged along these cross-faults
The Jubilee deposit was at first mined underground in1892 from a number of workings but the production isunknown In 1992 a small pit was excavated based onprobable reserves of approximately 50 000 t at 4 gt goldIn this pit gold mineralization is hosted in rocks of theHangingwall sequence and is in a complex quartzstockwork system emplaced along the margins of a 250 m-thick undeformed metabasite The gold is on both thehangingwall and footwall sides of the metabasite bodyTourmaline is present in the ore-bearing material Near theJubilee pit a northerly striking westerly dipping quartzvein almost perpendicular to the dominant foliation trendextends for about 200 m This vein was mined in the pastand contained maximum grades of approximately 30 gtgold
Mining at Mount Pleasant began at the turn of thecentury with the production of 8000 t of ore with anaverage grade of 9 gt gold Mining resumed in the 1980swhen about 145 000 t of ore was extracted with anaverage grade of 3 gt gold and 04 t of gold wasproduced The ore zones are nearly flat lying and wereemplaced in subparallel fashion one above the other Thedeeper northern zone is hosted by the Core sequence Goldis in quartzndashcarbonate veins associated with zones ofalbite (Fig 27) iron-rich chlorite sericite carbonate andpyrite alteration as well as zones of nearly flat lyinggraphitic schist (dip is 10deg to the south) The veins areeither vertical or of saddle-reef type lodged in anticlinalfolds
Harmony deposit
The Harmony (also known as New Baxters Find orContact) gold deposit is located approximately 10 km westof Peak Hill in a featureless area of no outcrops andcovered by colluvium lateritic duricrust and hardpanmaterial Details of the geology of the Harmony depositcan be found in Harper et al (1998) from whom the briefreview that follows is taken
The Harmony gold deposit consists of a subhorizontalsupergene zone hosted in ferruginous lateritic materials
(transported and residual regolith) a northeasterlytrending subvertical primary vein system and carbonate-bearing breccias Most of the ore is contained within thevein system which is hosted in rocks of the NarracootaFormation and at the contact between the Narracoota andRavelstone Formation (Fig 31) with lesser low-grademineralization in laterite The Harmony mineralization ishosted in a northwesterly plunging antiform (Enigmastructural zone) of a southwesterly dipping succession ofaltered mafic rocks at the top of the Narracoota Formationand within a shear zone along the contact with overlyingmetasedimentary rocks of the Ravelstone Formation Themineralized array of quartz veins become locally closelyspaced forming a stockwork that is commonly associatedwith high-grade ore Primary ore minerals include pyritewith gold inclusions pyrrhotite pentlandite chalcopyriteand scheelite The primary mineralization was enrichedby supergene processes
Hydrothermal alteration is characterized mainly bysilicification carbonitization and locally chloritizationHarper et al (1998) reported that mafic rocks show aparagenetic sequence of early albite and quartz followedby muscovite and chlorite Alteration in the metasedi-mentary rocks in the hangingwall is characterized mainlyby sericite and chlorite This primary alteration grades intozones of supergene alteration containing limonitekaolinite smectite group minerals and hematite Theweathered bedrock extends to approximately 60 m depthRegolith studies from drillholes have revealed anomalousAu W As Sb and Se in the ferruginous materials
Labouchere Nathans and Fortnumdeposits
In the northwestern part of the BryahndashPadbury Basin (onMILGUN) three distinct zones of gold mineralization havebeen recognized in high-strain zones associated with themargin of the Yarlarweerlor gneiss complex (Fig 25 andPlate 1) The Labouchere group (Labouchere and CentralValley deposits) and Nathans group (Labouchere-NathansNathan Bitter and Nathans Deep South deposits) had early
Figure 31 Diagrammatic cross section of the Harmony orezones (modified from Harper et al 1998)
50 m
FMP159
Supergene ore
Primary ore
Pit outline
50
100
150
200
Met
res
Mafic rocks
Formation)
Ultramafic rocks
Formation)(Ravelstone
(Narracoota
(NarracootaFormation)
Pelitic rocks
SW NE
211099
42
Pirajno et al
mining activity recorded from 1939 to the early 1940swith additional discoveries in the mid-1980s (Hanna andIvey 1990) The Fortnum deposits (Trevs StarlightTwilight Ricks Toms Hill Alton Eldorado Callies D39and Yarlarweelor) were discovered in the early 1980s (Hilland Cranney 1990)
Gold mineralization is structurally controlled in hostrocks of both the Bryah and Padbury Groups (Hill andCranney 1990) Windh (1992) concluded from detailedstudies at the Labouchere Nathans Deep South andFortnum mines that aqueous fluids of high temperatureand moderate salinity were responsible for mineralizationConstraints on temperature are derived from the lowerto middle greenschist-facies alteration assemblages(muscovitendashchloritendashalbite(ndashbiotite)) and fluid inclusiontrapping temperatures of up to 320degC Based on leadisotope work (galena from Nathans Deep South) Windh(1992) suggested that the syn-D4 gold mineralizationoccurred between 19 and 18 Ga The main features ofthe ore deposits are described below from the availableliterature
At the Labouchere-Nathans mine gold mineralizationis hosted in pyritic chert lenses or pods that lie withinmaficndashultramafic schist and along the contact withoverlying quartz wacke of the Labouchere FormationWindh (1992) described volcanic breccia (with high Niand Cr) with fuchsitic ultramafic and chert clasts similarto the reworked clastic rocks immediately overlying themaficndashultramafic volcanic rocks in the NarracootaFormation at the Fortnum mine The maficndashultramaficschist lies in the core of a southerly plunging anticlineand is here interpreted as part of the NarracootaFormation The Narracoota Formation ndash LabouchereFormation contact is interpreted as an early (D1ndashD2) faultor shear zone that was tightly folded during D3 Thestructure is crosscut and slightly offset by D4 faultstrending 270degndash290deg including a shear that forms thesouthern limit to the mineralization (Hanna and Ivey1990) Gold is associated with quartz veining and pyritein the altered chert with sideritendashmuscovitendashpyritealteration around the veins (Windh 1992) Productionfigures are only known for the combined output of theLabouchere-Nathans and Nathans Deep South opencuts(nearly 7 t of gold over five years Table 7)
At the Nathans group of workings the Nathan Bittershafts within the upper Labouchere Formation or lowerWilthorpe Formation have a recorded production of about8 kg over the period 1943ndash1950 (Swager and Myers1999) About 500 m to the north-northwest shallow shaftslie along the Kinders Fault between coarse and pebblyquartz wacke to the east and ultramafic schist of theNarracoota Formation to the west The Nathans DeepSouth mineralization lies approximately 1 km south-southeast of Nathan Bitter and was discovered in 1986(Hanna and Ivey 1990) The mineralization is hosted byfinely laminated chloritic shale interbedded with coarsequartz wacke and overlain by coarse units grading fromquartz-pebble conglomerate to quartzndashsericite shale Theentire succession is here described as part of the WilthorpeFormation including the chloritic shale which is mostlikely derived from mafic volcanic precursors (Hanna and
Ivey 1990 Windh 1992) Occhipinti et al (1998a)mapped similar units in the Wilthorpe Formation as aseparate member the Beatty Park Member The westerlyyounging succession contains a northndashsouth S3 foliationaxial planar to a few small-scale parasitic D3 foldsplunging steeply south and is overprinted by F4microfolds and kinks trending 290deg Gold mineralizationis within pyrite which has replaced finely bedded chloriteshale near crosscutting D4 quartzndashankerite veins Highestgrades are found adjacent to D4 faults These and otherstructural observations led Windh (1992) to infer a syn-D4 timing of mineralization However small quartz-veinnetworks possibly related to low-grade mineralization inthe overlying coarsely graded units are deformed by D4microfolding
The Fortnum gold mineralization is hosted by theNarracoota Formation which is truncated to the northagainst the Fortnum Fault and wedges out to the southThe package contains maficndashultramafic schist withoverlying reworked fragmental and volcaniclastic rocksincluding rocks with a supposed felsic volcanic derivationoverlain by the Ravelstone Formation (Hill and Cranney1990)
Mineralization at Trevs (and closely associatedorebodies including a recent discovery named Starlight)is hosted by quartz-vein systems in a westerly dippingsuccession of graded sericitic siltstone and coarse wackewith medium- to coarse-grained feldspar quartz and lithicfragments at least partly derived from the underlyingmaficndashultramafic volcanic rocks The Yarlarweelormineralization is hosted by ovoid lenses of jasperoidalchert within variably schistose maficndashultramafic volcanicrocks including interleaved fine tuffaceous and coarsefragmental layers (Hill and Cranney 1990) The chertlenses are within a westerly dipping reverse D3 shear zonecharacterized by quartzndashchloritendashsericite alteration Gold-bearing quartz(ndashpyrite) veins within the chert pods andwithin magnetite-bearing chlorite schist trend at 120deg dipsteeply north and are parallel to small sinistral D4 faults(D3 in Windh 1992) Windh (1992) also reported a minorset of (dextral) faults trending 070deg and crosscutting theD3 shear zones This may suggest a conjugate fault setrecording eastndashwest compression possibly late during D3rather than during north-northeastndashwest-southwest D4compression
Mining at the Fortnum group of workings from 1990to 1998 yielded 11 928 kg of gold from 4685 Mt of orewith an average recovered grade of 254 gt gold (Swagerand Myers 1999) Remaining measured and indicatedresources at Fortnum including Trevs and Starlightcontain an additional 17 970 kg of gold with a further4340 kg of gold estimated within inferred resources(Perilya Mines NL 1998)
Wembley deposit
The Wembley deposit is located approximately 18 kmsouthwest of Peak Hill and 25 km southeast of MurphyWell (from the Peak Hill road) Although rewarding(average grade of 175 gt gold) ore production was verysmall (less than 1800 t)
43
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The Wembley mineralization is hosted in alteredmetabasite rocks within a major shear zone trending 120degThe mineralized zone strikes at 075deg and dips 63deg to thenorthwest A quartz vein near the old workings strikes at060deg and dips 54deg to the northwest Sedimentary units areintercalated with the volcanic rocks and consist ofturbiditic rocks (greywackendashshale) As at the Durackprospect (see below) quartz mylonite units trending120degndash140deg are within the metabasites
Wilgeena deposit
The Wilgeena (or Hit or Miss) gold mine area is located15 km southeast of the Peak Hill mine Production wasless than 15 000 t at an average grade of 26 gt gold
The deposit is within rocks of the Peak Hill Schist andmore specifically along the contact between the mylonitesand quartzndashsericite schist A northerly trending easterlydipping stoped-out ore lens was approximately 2 m thickThe mineralization is hosted in quartzndashmuscovitendashmagnetite schist Grab samples from the old excavationsreturned values ranging from 3 to 14 gt gold (Mountford1984) Whitfield (1987) estimated inferred resources asapproximately 600 000 t at 244 gt gold
Durack St Crispin and Heines Findprospects
The Durack prospect lies about 12 km south of Peak Hillalong and immediately west of the Old Peak Hill telegraphroad This gold deposit is blind being covered by soil andlateritic material and consists of primary mineralizationand a supergene mineralized zone The prospect wasidentified by a soil anomaly containing up to 100 ppb gold(Sabminco Annual Report 1994)
The prospect area is underlain by rocks ofthe Narracoota Formation which include metabasite(medium- to coarse-grained metabasalts) and maficpyroclastic rocks Thin magnetite-bearing chert bands(possibly chemical sediments) intercalated within themetabasites define a broad synclinal structure A numberof mylonite zones trending 120degndash125deg cut across theNarracoota Formation rocks and contain most of theprimary mineralization Grades intersected during drillingare in the order of 15 gt gold over widths of 4 to 6 m
The primary mineralization is contained within quartzndashsulfide veins and stockworks hosted by altered metabasiterocks The mineralized area is about 14 km long and200 m wide Hydrothermal alteration is pervasive andconsists of quartz chlorite biotite and iron-rich carbonate(ankerite) Pyrite is present as fine disseminations andveinlets Selvages of silicandashpyritendashcarbonate surround themineralized zones
The supergene mineralization at the Durack prospectis controlled by subhorizontal redox fronts within theregolith material Supergene enrichment shows grades ofup to 12 gt gold over an interval of about 5 m In somecases the redox-front-related mineralization developed upto 45 m on each side of the primary zone
The St Crispin prospect is situated 20 km east-southeast of Peak Hill The mineralization is along a north-northwesterly trending structure and hosted in sericite(ndashgraphite) schist of the Peak Hill Schist Quartz veins arepresent in the schists and may host the mineralization
The Heines Find prospect is located 20 km south-southeast of Peak Hill Mineralization can be traced forabout 6 km along the easterly trending contact betweenrocks of the Narracoota Formation and the HeinesMember of the Wilthorpe Formation This contact has adip of 80deg to the north and is sheared In this area theNarracoota Formation consists of strongly deformedpillow lavas and chlorite schist The sedimentary rocks ofthe overlying Heines Member include a basal polymicticconglomerate
Ruby Well group
The Ruby Well area includes a number of mineral leasesfrom which gold has been produced either from surfacematerials or from hard rock (02 t Table 7) The RubyWell leases lie on the northern side of the Great NorthernHighway about 80 km from Meekatharra and 4ndash5 km eastof the Peak Hill turn-off
The area is underlain by the Narracoota Doolgunnaand Karalundi Formations The Hard To Find Ruby Anneand Lucky Call deposits within mafic schist of theNarracoota Formation were exploited between 1912 and1917 Most of the current production (figures notavailable) is from a number of dry-blowing workingssurrounding these old mines
Mikhaburra deposit
The old Mikhaburra gold mine (also known as HoldensFind) is in Narracoota Formation volcanic rocks in thesouthwestern part of BRYAH (Fig 25) The recordedproduction of the Mikhaburra mine is about 226 kg ofgold (MacLeod 1970) The mineralization is associatedwith a system of auriferous quartz veins emplaced alonga shear zone trending about 130deg to 150deg and dipping 68degto the southwest The volcanic rocks include mainlychlorite schist A quartz vein with a strike of 120deg and dipof 58deg southwest lies to the west of the old workings Thisvein is about 1 m wide and locally displays a laminatedstructure
Wilthorpe deposit
The Wilthorpe deposit is hosted by granitic rocks of theDespair Granite (Fig 32) which contains xenoliths ofmafic material Gold mineralization is confined to a zonecontaining quartz veins and flanked by bleached andsilicified wallrocks The ore zone is hydrothermallyaltered with assemblages of chloritendashsericitendashbiotite andquartzndashmuscovitendashbiotitendashtourmaline flanked by near-pervasive silicification In addition to gold the mineralizedveins also contain pyrite galena arsenopyrite andchalcopyrite The wallrock granite has a cataclastic textureand consists of quartz and feldspar lsquoeyesrsquo surrounded bya network of granulated quartz and sericite
44
Pirajno et al
Cashman deposit
The Cashman area on BRYAH includes a number of smallmineral occurrences and deposits containing copperand copperndashgold The old Cashman copper mine isapproximately 250 m from the gold workings In 1917 thismine produced about 7 t of copper ore grading 165copper (Marston 1979) The copper mineralizationconsists of a metre-wide cupriferous limonite vein with astrike of 042deg and a shallow dip to the northwest Oreminerals are chrysocolla and malachite as disseminationsand veinlets (Marston 1979)
In 1937 there was a small production of gold ore fromquartz veins In 1986ndash87 the gold potential of theCashman area was reassessed and on the basis of thiswork a small opencut was excavated from which 8000 tof ore material was produced and stockpiled (Whitfield1987) Gold mineralization is hosted in quartz veins withinmetabasaltic hyaloclastite A 01 m-thick quartz vein in thepit has a strike of 115deg and dips 35deg to the northeast Atand near the surface supergene enrichment is present ina horizon about 30 m wide and dipping about 20deg to thenorth (Whitfield 1987)
Volcanogenic copperndashgolddepositsThe Horseshoe Lights copperndashgold deposit on JAMINDI hasproduced nearly 9 t of gold of which almost 26 t wasrecovered from the copper concentrate operation between1988 and 1993 (Table 7) The Horseshoe Lights depositis hosted in felsic schist of the Narracoota Formation(Bryah Group) The mineralization consists of massivesulfides overlying and flanked by disseminated andstringer sulfides Ore minerals are mainly chalcocitepyrite and chalcopyrite Native copper is also present(Parker and Brown 1990) The host rocks are mylonitizedchlorite schist kaolinitendashsericite schist and quartzndashsericiteschist The geometry of the ore zones (massive sulfidesand stringer zone) alteration patterns (silicificationsericitic and chloritic alteration) predominantly felsiccomposition of the host rocks and metal association (CundashAundashAgndashPbndashZn) suggest that the deposit was originally ofthe volcanogenic massive sulfide type but subsequentlyenriched by supergene processes Average grades havebeen about 8 gt gold about 10 copper and 300 ppmsilver The stringer mineralization is of low gradeaveraging between 02 and 03 gt gold Production ceasedin 1994 Remaining resources (Table 8) are of low-grademineralization
Supergene manganese depositsManganese mineralization is part of a historicallyimportant manganese field first recognized in 1905 withdeposits in the Mount Fraser Mount Padbury Ravelstone(Peak Hill) and Horseshoe areas The manganesemineralization is of supergene origin and related tomanganiferous and hematitic shale units and BIF of theHorseshoe Formation (Bryah Group) as well as units ofthe Padbury Group The chief ore minerals are pyrolusiteand cryptomelane The ore is lateritic locally pisolitic innature and in places forms caps overlying the primarymanganese-rich sedimentary material In places notablyat Horseshoe there is evidence to suggest that someenrichment may have taken place in a palaeodrainagechannel lake or swamp environment (MacLeod 1970)In the Ravelstone area just north of the Peak Hill golddeposit the manganese supergene enrichment appears tohave a structural control
The Horseshoe area has been the main producingregion with production from two deposits 2 and 3 kmnorth and northwest of the Horseshoe townsite (Plate 1)The main production period was from 1948 to 1971 when490 000 t was mined (Table 8) all but 5000 t of whichwas classified as metallurgical-grade ore The enrichedzone was 3 to 45 m thick and typically extended overlengths of 400 to 500 m The North deposit averaged 30 min width whereas the South deposit was fan shapedopening from 20 to 300 m wide at its maximum extentOre consisted of mixed manganese and iron oxides withhighly variable manganese and iron contents Gradesprogressively decreased from 42 to 35ndash38 after 1966
There are several small deposits in the Mount Fraserndash Mount Padbury area about 30 km west of Peak Hill
Figure 32 The west wall of the Wilthorpe opencut showingthe contact between biotitendashsericitendashquartz schistand deformed Despair Granite
45
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
They contain patches of high-grade ore within largedeposits of ferruginous manganese material Productionof high-grade ore occurred sporadically since 1949 andamounted to 7547 t at grades in excess of 46 manganeseA third mining operation commenced at the Millidie (orElsa) deposit in the early 1990s but this has notprogressed to a full-scale commercial operation High-grade mineralization in the area is estimated to containmeasured plus indicated resources of approximately11 000 t of manganese (Table 8)
In the Ravelstone area immediately north-northwestof Peak Hill mining occurred between 1956 and 1964producing 76 237 t of ore at 70ndash90 manganese oxide(Table 8) Remainng measured and indicated resources areestimated as 132 000 t of contained metal (Table 8)Manganese production at Ravelstone was from easterlystriking orebodies reaching lengths of up to 100 m andwidths of 30 m but commonly small and narrow Detailedexamination of one specimen of ore revealed that it wascomposed mainly of cryptomelane and accessorypyrolusite A partial geochemical analysis of the samesample provided the following results 064 wt SiO2465 wt Al2O3 0011 wt P 033 wt MgO 268 wtK2O 7038 wt MnO 119 wt Fe 005 ppm Au650 ppm Co 31 ppm Cu 53 ppm Ni 20 ppm Pb and98 ppm Zn
The manganese ore is characterized by high bariumabundances (3000 ppm to 30 at Mount Fraser3000 ppm to 1 at Horseshoe and 3943 to 9000 ppm atRavelstone)
Iron oreThe Robinson Range Formation (Padbury Group) containsunits of banded iron-formation (Fig 2) within which areareas of supergene enrichment of hematite and goethiteThese constitute demonstrated (pre-JORC code) iron-oreresources estimated at approximately 10 Mt with gradesin excess of 60 iron (Table 8) Enrichment is above twoBIF units approximately 100 m thick separated by ahematitic shale horizon Iron grades of the primary BIFvary between 20 and 50 Hematite and hematitendashgoethite surficial enrichment contains grades in excess of50 iron as determined from the sampling of one ofabout 200 small pods of potentially ore grade material(Sofoulis 1970)
TalcTalc in the Mount Seabrook ndash Livingstone ndash Trillbarregion is present within metasedimentary and meta-volcanic rocks and minor mafic and ultramafic rocks Talcis hosted in metasomatized dolomite orebodies (Plate 1)as a series of steeply plunging lenses (Lipple 1990) TheMount Seabrook deposit was discovered in 1965 and hasproduced over 540 000 t of talc mostly of cosmetic gradebetween 1973 and 1995 Indicated and inferred resourcesredefined at Mount Seabrook and Livingstone amount to172 Mt of ore with a significantly greater potentialbecause the orebodies are open along strike
DiscussionThe Horseshoe Lights VMS-type copperndashgold deposit issyn-volcanic and pre-orogenic All other deposits are ofepigenetic origin and syn- to post-orogenic
Figure 33 schematically depicts a simple regionalmodel of ore genesis for the epigenetic mineral depositsin the BryahndashPadbury ndash Peak Hill Schist (BPPS) tectono-metamorphic domain and the adjacent Yerrida Basin TheYerrida Basin and BPPS domain were tectonicallyjuxtaposed along the northeasterly trending Goodin FaultDeformation which affected the BPPS domain wastransmitted across the Goodin Fault for a few kilometresinto the Yerrida Basin This deformation becomes weakerfrom the Goodin Fault eastward The BPPS domain wassubjected to metamorphism (upper to lower greenschistfacies) At least two phases of metamorphism arerecognized a prograde phase overprinted by a retrogradephase Geothermometry and geobarometry studies inthe area around Peak Hill by Thornett (1995)indicated temperatures of around 500ndash620degC for peakprograde metamorphism and 65 to 7 kbar for minimumpressure of the prograde assemblages The timing ofthis metamorphism is probably linked to the collisionbetween the Pilbara and Yilgarn Cratons (see Tectonicmodel and conclusions) which is postulated to haveoccurred between 1820 and 1800 Ma (Occhipinti et al1999)
A genetic model proposed by Pirajno and Preston(1998) envisages that fluids were generated during phasesof dynamic and thermal metamorphism in the BPPSdomain and that these fluids were largely responsible forthe deposition of mesothermal gold-only and shear-zone-hosted deposits The paragenesis of the alterationassemblages associated with the mesothermal depositsand textural relationships suggest that metamorphism
Figure 33 Sketch illustrating a conceptual model for the originof precious and base metal epigenetic deposits inthe BryahndashPadbury and Yerrida Basins (after Pirajnoand Preston 1998)
FMP71a
Bryah and Padbury Groups
Mooloogool Subgroup
Windplain Subgroup
Direction of fluid movement
170300
Fault Cleavagedevelopment
ARCHAEANBASEMENT
NARRYERTERRANE
Area of Au deposition
Collisionzone
Cleavagelate epigeneticmineralisation
Metamorphism
Basin fluids
YERRIDA
and deformation
Goo
din
Faul
t
development
BRYAHndashPADBURYBASINS BASIN
NW SE
46
Pirajno et al
and mineralization were broadly contemporaneousalthough alteration was in most cases from peak toretrograde metamorphism Exceptions to this are localizedzones of sodium metasomatism (albite and arfvedsonite)which overprint the retrograde assemblages This sodiummetasomatism may be related to central zones ofhigher temperatures within the mineralized structuresOne possible explanation for the widespread sodiummetasomatism is granite magmatism however there is noevidence in either the Bryah or the Padbury Basin ofgranitic plutons intruding the volcano-sedimentarysuccessions Therefore a possible role of graniticmagmatism as one of the heat and metal sources for thehydrothermal solutions based on our present knowledgeis excluded
Hydrothermal solutions responsible for the emplace-ment of mesothermal lodes are considered to be generatedin tectonically active regions and are associated withcompressional and extensional tectonics (Kerrich andCassidy 1994) The mesothermal-style gold-only lodesof the BPPS domain were formed in a compressionalsetting characterized by thin-skinned thrusting associatedwith prograde and retrograde mineral assemblages(Pirajno 1996) Dyer (1991) concluded that the hydro-thermal mineralization in the LaboucherendashFortnumarea was generated by the mixing of two fluids ofdifferent density and salinity Deeply sourced hot salineCO2-bearing fluids were mixed with cooler less salinenear-surface aqueous fluids The available evidencepoints to the conclusion that the mineralizing fluids wereat first generated during compression and dehydrationand moved along ductile to brittle structures Duringsubsequent phases meteoric fluids would have infiltratedalong the same structures and mixed with the hottermetamorphic solutions The whole mechanism couldhave been repeated again in the next phase of compressionand extension leading to multiphase ore genesis processesin which the latest phase leaves the most detect-able imprint There is no obvious link with magmaticactivity
Other metal deposits in the BryahndashPadbury Basin aresupergene manganese and iron ore (Pirajno and Preston1998) The timing of the weathering event that led to thesupergene enrichment of the manganese and iron ores isnot known although it may be possible that the warm andhumid climate during the middle Tertiary (Cockbain andHocking 1990) played a major role in the genesis of thissupergene mineralization
Tectonic model andconclusions
Gee (1979) Hynes and Gee (1986) Windh (1992) andGee and Grey (1993) interpreted the geodynamicevolution of the lsquoGlengarry Basinrsquo as defined by Gee andGrey (1993) in terms of an ensialic or intracontinentalbasin Tyler and Thorne (1990) Myers (1993) Martin(1994) and Myers et al (1996) proposed models in whichthe former lsquoGlengarry Basinrsquo would have formed in aback-arc setting during the convergence of the Pilbara andYilgarn Cratons between 2000 and 1800 Ma
In the light of the re-interpretation of the formerlsquoGlengarry Basinrsquo into the Bryah Padbury and YerridaBasins some modification of the above tectonic schemesis necessary Lack of sufficient geochronological datahowever poses the problem of the precise timing ofevents This lack of information must be taken intoaccount when modelling basin tectonics Pirajno (1996)and Pirajno et al (1998b) suggested two models for thegeodynamic evolution of the BryahndashPadbury and YerridaBasins 1) the basins were formed during convergence andsubsequent collision in a back-arcndashforeland basin settingin which these basins were opened and infilled duringsouthward subduction of oceanic crust (extensional backarc) and subsequently overlain by sediments in a newlydeveloped foreland basin (syn-collisional) and 2) thebasins were formed at the time of the oblique collisionbetween the Pilbara and Yilgarn Cratons as pull-apartstructures in a strike-slip setting with transitions fromextensional (transtension) to compressional (transpression)regimes
In this study we propose a model whereby the BryahBasin was formed as a back-arc rift with a component ofrifting along the Yilgarn continental margin a kind ofproto-oceanic rift comparable to that of the present-day Guayamas Basin in the Gulf of California (Lonsdaleand Becker 1985) The Padbury Basin developed as aforeland basin on top of the Bryah Basin during theoblique collision of the Pilbara and Yilgarn Cratons Ourmodel is shown in Figure 34 in which two stages areschematically depicted and briefly discussed below
The Bryah Basin was formed by processes of back-arc opening during subduction of oceanic crust beneaththe northern margin of the Yilgarn Craton approximately
Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins withinthe context of the Capricorn Orogen (modified from Myers 1990 1993 and Myers et al 1996)a) At about 1960ndash1950 Ma development of Andean-type magmatic arc on a microcontinental active margin back-arcrifting and spreading with creation of oceanic crust (dominantly high-Mg and high-Fe tholeiite associated withsubvolcanic peridotitic cumulates representing future maficndashultramafic schist of the Narracoota Formation) anderuption of basaltic hyaloclastites probably from the same source as the maficndashultramafic material occurs on passivemargin of Yilgarn Craton Insets schematically show geochemical signatures of these volcanic rocks (see text fordetails)b) Capricorn Orogeny involved collision between the Pilbara and Yilgarn Cratons with formation of fold-and-thrustbelts on both northern and southern sides of orogen and thrusting of oceanic crust over hyaloclastite and margin ofYilgarn Craton The thrust separating oceanic crust material from hyaloclastite is represented by the Murchison Fault(see Plate 1) Chondrite-normalized REE patterns for metabasites and hyaloclastites of the Narracoota Formation areshown in the insets
47
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
N S
N S
Marymia In
lier
YILGARN
Backarc riftMicrocontinent
andvolcanic arc
Seafloor
Seafloor
Oceaniccrust
lt 1960ndash1950 Ma
PILBARA
PILBARAYILGARN
Fold-and-thrustbelt
PadburyBasin Bryah Basin
1820ndash1800 Ma
Present-dayBryahndashPadbury
area
Lithosphere
FMP376 170300
4000
3000
2000
1000
00 21 3
FeOMgO FeOMgO Ni Cr
1
2
0
3
0 1 2
La Eu Lu
Sam
ple
chon
drite
100
10
16
Sam
ple
chon
drite
100
10
2La Eu Lu
2
Cr
(ppm
)
TiO
(
)
TiO x1002
Mid-oc
ean r
idge
2
Clastic rocks
Padbury Group
Archaean basement
Metabasic rocksof Narracoota FormationHyaloclastites(Narracoota Formation)
Karalundi Formation
Oceanic crust
a)
b)
48
Pirajno et al
between 1960 and 1950 Ma (Occhipinti et al 1999Fig 34a) Myers (1993) speculated that a southwardoceanic subduction system with a south-facing Andean-type magmatic arc had developed off the northern passivemargin of the Yilgarn Craton Remnants of arc magmaticsuites have not been found but may be buried under theMesoproterozoic Bangemall Basin Back-arc rifting alsoaffected the northern margin of the Yilgarn Craton whererift propagation is postulated to have progressivelyadvanced from west to east through a succession ofcrustalndashlithospheric thinning rupture and grabenformation In this model the Marymia Inlier is a remnantof a rift shoulder (Fig 34a)
The closing of the ocean between the Pilbara andYilgarn Cratons was followed by the oblique collisionbetween the rifted passive margin on the Pilbara side aninferred active magmatic arc and the passive northernmargin of the Yilgarn Craton Closure of the interveningocean (1820ndash1800 Ma) resulted in inversion of the Bryahback-arc rift and thrusting of oceanic crust (nowNarracoota Formation) over the Yilgarn Cratonrsquos northernmargin (Fig 34b) During and following this collisionevent the southern side of the Pilbara was tectonicallysliced by major thrusts whereas most of the tectonictransport of the inferred magmatic and oceanic crust rockswas towards the south (Myers 1993)
High-Mg tholeiitic rocks with pillow structuressheeted dykes the Trillbar layered complex sea-floor metasomatism and trace and rare-earth elementgeochemistry support the oceanic crust model for theorigin of the mafic and ultramafic schist of the NarracootaFormation The hyaloclastites on the other hand wereerupted in shallow waters and locally characterized byexplosive activity and have mixed and overlappinggeochemical signatures with the mafic schist This featurecan be interpreted as suggesting a more continentalenvironment of emplacement and therefore were emplacedon Yilgarn crust (Fig 34a) In contrast to the maficndashultramafic schist the hyaloclastites are relativelytectonically undeformed Their contact with the maficndashultramafic schist is along the Murchison Fault (Plate 1)We conclude that the Murchison Fault represents atectonic boundary between these two components of theNarracoota Formation and that oceanic crust material(precursors of the maficndashultramafic schist) were thrustover the continental hyaloclastites during the CapricornOrogeny as shown in Figure 34b The suggested Gulf ofCalifornia-type palaeoenvironmental setting with thefuture Marymia Inlier as one of the rift shoulders(analogous to the California peninsula) is shown inFigure 34a
The absence of volcanic rocks of intermediate(andesitic) compositions suggests that the NarracootaFormation metabasites were not formed in a subduction-related volcanic-arc setting as proposed by Myers et al(1996) However we concur with Sun (1997) that theboninitic component in the chemistry of the metabasites(see inset of Fig 34 and Figs 12ndash15) needs explanationWe suggest that these boninitic characteristics of theNarracoota Formation can be compared to the boninitesof the Koh Ophiolite in New Caledonia (Meffre et al
1996) which are considered to have formed in a back-arc spreading centre
The overall high MgO and low TiO2 abundancesdepleted REE and low LaYb ratios of the NarracootaFormation are also consistent with the origin of theNarracoota Formation metabasites from a mantle plume(Pirajno et al 1998a)
The Padbury Basin was interpreted by Martin (1994)as a retroarc foreland basin recording the collision of theYilgarn and Pilbara Cratons During and followingcollision between 1820 and 1800 Ma (Occhipinti et al1999) back-arc volcanism ceased and a foreland basindeveloped on top of the back-arc succession (BryahGroup) This basin was filled by siliciclastic rocks only(Padbury Group) During continued regional compressionthe BryahndashPadbury Basin developed into a fold-and-thustbelt and was partly thrust over the Yerrida Basin alongthe Goodin Fault
In summary the convergence between the ArchaeanPilbara and Yilgarn Cratons resulted in progressivecompressional deformation that affected the Bryah andPadbury Groups as a coherent package At least fourgroups of structures are recognized in the regionaldeformation of the volcano-sedimentary succession andtheir reworked basement (ie Yarlarweelor GneissComplex) This same deformation and associatedmetamorphism was responsible for the mesothermal gold-only lodes of the Bryah and Padbury Basins
AcknowledgementsWe acknowledge the contribution of colleagues whoparticipated in the Glengarry mapping program JohnMyers N G Adamides and P G Le Blanc SmithRichard Davy first introduced the senior author to the areaWe are also grateful to the local pastoral community fortheir hospitality The geological staff of LabouchereFortnum Peak Hill and Harmony gold mines are thankedfor sharing their knowledge with us
49
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
References
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BAGAS L B 1998 Geology of the Marymia 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BARNETT J C 1975 Some probable Lower Proterozoic sedimentsin the Mount Padbury area Western Australia Geological SurveyAnnual Report 1974 p 52ndash54
BARRETT F 1989 A study of wallrock alteration associated withgold mineralization mdash Peak Hill and Mt Pleasant area WesternAustralia Geological Survey M-series Item 7706 A41555(unpublished)
BRADLEY J J FAULKNER J A and SANDERS A J 1997Geochemical mapping of the Robinson Range 1250 000 sheetWestern Australia Geological Survey 1250 000 RegolithGeochemistry Series Explanatory Notes 57p
BREITKOPF J H and MAIDEN K J 1988 Tectonic setting of theMatchless Belt pyritic copper deposits Namibia EconomicGeology v 83 p 710ndash723
BUNTING J A COMMANDER D P and GEE R D 1977Preliminary synthesis of Lower Proterozoic stratigraphy andstructure adjacent to the northern margin of the Yilgarn BlockWestern Australia Geological Survey Annual Report 1976p 43ndash48
BURKE K C KIDD W S F TURCOTTE L DEWEY J FMOUGINIS-MARK P J PARMENTIER E M SENGORA M and TAPPONIER P E 1981 Tectonics of basalticvolcanism in Basaltic volcanism on the terrestrial planets HoustonLunar and Planetary Institute p 803ndash898
COCKBAIN A E and HOCKING R M 1990 Regolith in Geologyand mineral resources of Western Australia Western AustraliaGeological Survey Memoir 3 p 591ndash602
CRAWFORD R A FAULKNER J A SANDERS A J LEWISJ D and GOZZARD J R 1996 Geochemical mapping ofthe Glengarry 1250 000 sheet Western Australia GeologicalSurvey 1250 000 Regolith Geochemistry Series Explanatory Notes57p
DAVY R PIRAJNO F SANDERS A J and MORRIS P A1999 Regolith geochemical mapping as an adjunct to geologicalmapping and exploration examples from three contiguousProterozoic basins in Western Australia Journal of GeochemicalExploration v 66 p 37ndash53
DIXON J and WILLIAMS G 1983 Reaction softening in mylonitesfrom the Arnaboll thrust Sutherland Scottish Journal of Geologyv 19 p 157ndash168
DUNCAN A R 1987 The Karoo igneous province mdash a problemarea for inferring tectonic setting from basalt geochemistry Journalof Volcanology and Geothermal Research v 32 p 13ndash34
DYER F L 1991 The nature and origin of gold mineralization atthe Fortnum Nathans and Labouchere deposits Glengarry BasinWestern Australia University of Western Australia BSc Honoursthesis (unpublished)
ELIAS M 1982 Belele WA Western Australia Geological Survey1250 000 Geological Series Explanatory Notes 21p
ELIAS M BUNTING J A and WHARTON P H 1982 GlengarryWA Western Australia Geological Survey 1250 000 GeologicalSeries Explanatory Notes 27p
ELIAS M and WILLIAMS S J 1980 Robinson Range WAWestern Australia Geological Survey 1250 000 Geological SeriesExplanatory Notes 32p
FISHER R V and SCHMINCKE H-U 1984 Pyroclastic rocksBerlin Springer-Verlag 472p
GEE R D 1979 The geology of the Peak Hill area Western AustraliaGeological Survey Annual Report 1978 p 55ndash62
GEE R D 1987 Peak Hill WA (2nd edition) Western AustraliaGeological Survey 1250 000 Geological Series Explanatory Notes24p
GEE R D 1990 Nabberu Basin in Geology and mineral resourcesof Western Australia Western Australia Geological SurveyMemoir 3 p 202ndash210
GEE R D and GREY K 1993 Proterozoic rocks on the Glengarry1250 000 sheet mdash stratigraphy structure and stromatolitebiostratigraphy Western Australia Geological Survey Report 4130p
HALL W D M and GOODE A D T 1978 The Early ProterozoicNabberu Basin and associated iron formations of Western AustraliaPrecambrian Research v 7 p 129ndash184
HANNA J P and IVEY M E 1990 Labouchere and Deep Southgold deposits in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 667ndash670
HARPER M HILL M G RENTON J I and THORNETTS E 1998 Gold deposits of the Peak Hill area WesternAustralia in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 81ndash87
HILL A D and CRANNEY P J 1990 Fortnum golddeposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 665ndash666
HYNES A and GEE R D 1986 Geological setting andpetrochemistry of the Narracoota Volcanics Capricorn OrogenWestern Australia Precambrian Research v 31 p 107ndash132
JENSEN L S 1976 A new cation plot for classifying subalkalicvolcanic rocks Canada Ontario Division of Mines MP 66 22p
KERRICH R and CASSIDY K F 1994 Temporal relationships oflode gold mineralization to accretion magmatism metamorphismand deformation mdash Archaean to present a review Ore GeologyReviews v 9 p 263ndash310
LE MAITRE R W 1989 A classification of igneous rocksand glossary of terms Oxford Blackwell Scientific Publications193p
50
Pirajno et al
LEWIS J D 1971 The geology of some carbonate intrusions in theMount Fraser area Peak Hill Goldfield Western Australia WesternAustralia Geological Survey Annual Report 1970 p 50ndash56
LIPPLE S L 1990 Talc in Geology and mineral resources of WesternAustralia Western Australia Geological Survey Memoir 3p 678ndash679
LISTER G S and SNOKE A W 1984 SndashC mylonites Journal ofStructural Geology v 6 p 617ndash638
LONSDALE P and BECKER K 1985 Hydrothermal plumes hotsprings and conductive heat flow in the southern trough ofGuayamas Basin Earth and Planetary Science Letters v 73p 211ndash225
LUCAS S B STERN R A SYME E C REILLY B A andTHOMAS D J 1996 Intraoceanic tectonics and the developmentof continental crust 192 ndash 184 Ga evolution of the Flin Flon beltCanada Geological Society of America Bulletin 108 p 602ndash629
MacLEOD W N 1970 Peak Hill WA (1st edition) WesternAustralia Geological Survey 1250 000 Geological SeriesExplanatory Notes 21p
MARSHAK S TINKHAM D ALKMIN F BRUECKNER Hand BORNHORST T 1997 Dome-and-keel provinces formedduring Palaeoproterozoic orogenic collapse mdash core complexesdiapirs or neither examples from the Quadrilatero Ferrifero andthe Penkean orogen Geology v 25 p 415ndash418
MARSTON R J 1979 Copper mineralization in Western AustraliaWestern Australia Geological Survey Bulletin 13 208p
MARTIN D McB 1992 Turbidite facies and depositionalenvironment of the Precambrian Labouchere Formation PadburyGroup Western Australia Geological Society of AustraliaAbstracts 32 p 168ndash170
MARTIN D McB 1994 Sedimentology sequence stratigraphy andtectonic setting of a Palaeoproterozoic turbidite complex LowerPadbury Group Western Australia University of Western AustraliaPhD thesis (unpublished)
MARTIN D McB 1998 Lithostratigraphy and structure of thePalaeoproterozoic Padbury Group Milgun 1100 000 sheet WesternAustralia Western Australia Geological Survey Report 62 57p
McDONALD I R 1994 Final Report on the Glengarry nickel projectES502 and E51384 Western Australia Geological SurveyM-series Item 7706 A41555 (unpublished)
McMILLAN N M 1993 Structure metamorphism alteration andtiming of gold mineralisation at Marymia Gold Project in theMarymia Dome in An international conference on crustal evolutionmetallogeny and exploration of the Eastern Goldfields ExtendedAbstracts compiled by P R WILLIAMS and J A HALDANEAustralian Geological Survey Organisation Record 199354p 243ndash244
McPHIE J DOYLE M and ALLEN R 1993 Volcanic texturesHobart Tasmanian Government Printing Office 198p
MEFFRE S AITCHISON J C and CRAWFORD A J 1996Geochemical and tectonic significance of boninites and tholeiitesfrom the Koh Ophiolite New Caledonia Tectonics v 15p 67ndash83
MOUNTFORD B R 1984 Preliminary geological report onProspecting Licences 52104 and 52105 Mt Padbury area WesternAustralia Western Australia Geological Survey M-series Item3688 A16393 (unpublished)
MYERS J S 1989 Thrust sheets on the southern foreland of theCapricorn Orogen Robinson Range Western Australia WesternAustralia Geological Survey Report 26 Professional Papersp 127ndash130
MYERS J S 1990 Capricorn Orogen in Geology and mineralresources of Western Australia Western Australia GeologicalSurvey Memoir 3 p 197ndash198
MYERS J S 1993 Precambrian history of the West Australian cratonand adjacent orogens Annual Reviews of Earth and PlanetaryScience v 21 p 453ndash485
MYERS J S SHAW R D and TYLER I M 1996 Tectonicevolution of Proterozoic Australia Tectonics v 15 p 1431ndash1446
NELSON D R 1997 Compilation of SHRIMP UndashPb zircongeochronology data 1996 Western Australia Geological SurveyRecord 19972 189p
NELSON D R 1998 Compilation of SHRIMP UndashPb zircongeochronology data 1997 Western Australia Geological SurveyRecord 19982 242p
OrsquoNIONS R K PANKHURST R J and GRONVOLD K 1976Nature and development of basalt magma sources beneath Icelandand the Reykjanes ridge Journal of Petrology v 17 p 315ndash338
OCCHIPINTI S A GREY K PIRAJNO F ADAMIDES N GBAGAS L DAWES P and LE BLANC SMITH G 1997Stratigraphic revision of Palaeoproterozoic rocks of the YerridaBryah and Padbury Basins (former Glengarry Basin) WesternAustralia Geological Survey Record 19973 57p
OCCHIPINTI S A and MYERS J S 1999 Geology of the Moorarie1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 20p
OCCHIPINTI S A MYERS J S and SWAGER C P 1998aGeology of the Padbury 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes29p
OCCHIPINTI S A SHEPPARD S NELSON D R MYERS J Sand TYLER I M 1998b Syntectonic granite in the southernmargin of the Palaeoproterozoic Capricorn Orogen WesternAustralia Australian Journal of Earth Sciences v 45 p 509ndash512
OCCHIPINTI S A SHEPPARD S and TYLER I M 1999Palaeoproterozoic tectonic evolution of the southern margin of theCapricorn Orogen Western Australia Last Conference of theMillenium Halls Gap WA Abstract volume p 173ndash174
OCCHIPINTI S A SWAGER C P and PIRAJNO F 1998cStructuralndashmetamorphic evolution of the Palaeoproterozoic Bryahand Padbury Groups during the Capricorn Orogeny WesternAustralia Precambrian Research v 90 p 141ndash158
PARKER T W H and BROWN T 1990 Horseshoe goldndashcopperndashsilver deposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 671ndash675
PEARCE J A ERNEWEIN M BLOOMER S H PARSON L MMURTON B J and JOHNSON L E 1995 Geochemistry ofLau Basin volcanic rocks influence of ridge segmentation and arcproximity Geological Society Special Publication v 81p 53ndash75
PEARCE T H GORMAN B E and BIRKETT T C 1977 Therelationship between major element chemistry and tectonicenvironment of basic and intermediate volcanic rocks Earth andPlanetary Science Letters v 36 p 121ndash132
PERILYA MINES NL 1998 Annual report for the year ending30 June 1998 60p
PETERS S G 1993 Polygenetic meacutelange in the Hodgkinsongoldfield Northern Tasman Orogenic Zone Australian Journal ofEarth Sciences v 40 p 115ndash129
PIRAJNO F 1996 Models for the geodynamic evolution of thePalaeoproterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1995ndash96 p 96ndash103
PIRAJNO F and ADAMIDES N G 2000 Geology andmineralization of the Palaeoproterozoic Yerrida Basin WesternAustralia Western Australia Geological Survey Report 60 43p
51
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
PIRAJNO F and ADAMIDES N G 1998 Geology of the Thaduna1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 24p
PIRAJNO F ADAMIDES N G and FERDINANDO D D 1998aGeology of the Glengarry 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes16p
PIRAJNO F ADAMIDES N G OCCHIPINTI S A SWAGERC P and BAGAS L 1995a Geology and tectonic evolution ofthe early Proterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1994ndash95 p 71ndash80
PIRAJNO F BAGAS L SWAGER C P OCCHIPINTI S A andADAMIDES N G 1996 A reappraisal of the stratigraphy of theGlengarry Basin Western Australia Western Australia GeologicalSurvey Annual Review 1995ndash96 p 81ndash87
PIRAJNO F and DAVY R 1996 Mafic volcanism in thePalaeoproterozoic Glengarry Basin Western Australia andimplications for its tectonic evolution Geological Society ofAustralia Abstracts no 41 p 343
PIRAJNO F and OCCHIPINTI S A 1995 Base metal potential ofthe Palaeoproterozoic Glengarry and Bryah Basins WesternAustralia Recent developments in base metal geology andexploration Australian Institute of Geoscientists Bulletin 16p 51ndash56
PIRAJNO F and OCCHIPINTI S A 1998 Geology of the Bryah1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 41p
PIRAJNO F OCCHIPINTI S LE BLANC SMITH G andADAMIDES N G 1995b Pillow lavas in the Peak Hill terranesWestern Australia Geological Survey Annual Review 1993ndash94p 63ndash66
PIRAJNO F OCCHIPINTI S A and SWAGER C P 1998bGeology and tectonic evolution of the Palaeoproterozoic BryahPadbury and Yerrida Basins (formerly Glengarry Basin) WesternAustralia Precambrian Research v 90 p 119ndash140
PIRAJNO F and PRESTON W A 1998 Mineral deposits of thePadbury Bryah and Yerrida Basins in Geology of Australian andPapua New Guinean mineral deposits edited by D A BERKMANand D H MACKENZIE Australasian Institute of Mining andMetallurgy Monograph 22 p 63ndash69
RAYMOND L A 1984a Classification of meacutelanges GeologicalSociety of America Special Paper 198 p 7ndash20
RAYMOND L A 1984b Meacutelanges their nature origin andsignificance Geological Society of America Special Paper 198170p
ROLLINSON H R 1993 Using geochemical data evaluationpresentation interpretation Singapore Longman 352p
SABMINCO ANNUAL REPORT 1994 Annual report on miningleases M52202ndash203 vol 1 2 and 3 Western Australia GeologicalSurvey M-series Item 8967 A42856 (unpublished)
SCHILLING J-G 1982 Galapagos hot spot ndash spreading centersystem 1 Spatial petrological and geochemical variations (83degWndash101degW) Journal of Geophysical Research v 87p 5593ndash5610
SCHILLING J-G MEYER P S and KINGSLEY R H 1982Evolution of the Iceland hot spot Nature v 296 p 313ndash320
SHEPPARD S and SWAGER C P 1999 Geology of the Marquis1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 21p
SHEPPARD S OCCHIPINTI S A NELSON D and TYLERI M 1999 Granites of the southern Capricorn Orogen WesternAustralia Geological Society of Australia Abstracts no 56p44-46
SOFOULIS J 1970 Iron deposits of the Robinson Range Peak HillGoldfield WA Western Australia Geological Survey Record19706 10p
SPEAR F S 1993 Metamorphic phase equilibria and pressurendashtemperaturendashtime paths Mineralogical Society of AmericaMonograph p 799
STERN R A SYME E C and LUCAS S B 1995 Geochemistryof 19 Ga MORB and OIB-like basalts from the Amisk collageFlin Flon belt Canada evidence for an intra-oceanic originGeochimica et Cosmochimica Acta v 59 p 3131ndash3154
SUBRAMANYA A G FAULKNER J A SANDERS A J andGOZZARD J R 1995 Geochemical mapping of the Peak Hill1250 000 sheet Western Australia Geological Survey 1250 000Regolith Geochemistry Series Explanatory Notes 59p
SUN S-S 1982 Chemical composition and origin of the Earthrsquosprimitive mantle Geochimica et Cosmochimica Acta v 46p 179ndash192
SUN S-S 1997 Chemical and isotopic features of Palaeoproterozoicmafic igneous rocks of Australia implications for tectonic processesAustralian Geological Survey Organisation Record 19974p 119ndash122
SWAGER C P and MYERS J S 1999 Geology of the Milgun1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 27p
THORNETT S E 1995 The nature origin and timing of goldmineralization in Proterozoic rocks of the Peak Hill District WAUniversity of Western Australia MSc thesis (unpublished)
TYLER I M 1999 Palaeoproterozoic orogeny in Western AustraliaGeological Society of Australia Abstracts no 56 p 47ndash49
TYLER I M PIRAJNO F BAGAS L MYERS J S andPRESTON W A 1998 The geology and mineral deposits of theProterozoic in Western Australia Australian Geological SurveyOrganisation Journal of Geology and Geophysics v 17p 223ndash244
TYLER I M and THORNE A M 1990 The northern margin ofthe Capricorn Orogen Western Australia mdash an example of anEarly Proterozoic collision zone Journal of Structural Geologyv 12 p 685ndash701
WANG P and GLOVER L 1992 A tectonic test of the mostcommonly used geochemical discriminant diagrams and patternsEarth Science Reviews v 33 p 111ndash131
WATKINS K P 1983 Petrogenesis of Dalradian albite porphyroblastschists Journal of the Geological Society of London v 140p 601ndash618
WHITFIELD G B 1987 Wilgeena gold mine Progress report MS52111 and 112 Western Australia Geological Survey M-seriesItem 5862 A28194 (unpublished)
WINDH J 1992 Tectonic evolution and metallogenesis of the EarlyProterozoic Glengarry Basin Western Australia University ofWestern Australia PhD thesis (unpublished)
52
Pirajno et al
Appendix
Gazetteer of localities
Locality AMG coordinateEasting Northing
5 Mile Well 616500 7158100Beatty Park Bore 632200 7163500Cashman opencut 662129 7126994Dandy Well 646400 7188740Despair Bore 625300 7169600Durack prospect 670440 7150520Durack Well 671600 7143000Fortnum mine 636372 7197627Friday Pool 558620 7178625Harmony (New Baxters Find) opencut 664145 7161267Heines Find prospect 682759 7145164Horseshoe Lights opencut 662648 7193894Horseshoe Mn mine 656990 7186510Horseshoe Au prospect 661219 7182977Jubilee mine 671889 7165443Labouchere mine 627730 7204710Livingstone mine 567540 7171032Lucky Call prospect (Ruby Well group) 676747 7127188Mikhaburra (Holdens Find) opencut 656252 7130396Millidie (Elsa) deposit 643000 7160000Mount Fraser 639200 7163300Mount Labouchere 630360 7212620Mount Padbury 627400 7164100Mount Padbury mine 635100 7165100Mount Pleasant opencut 674287 7161900Mount Seabrook mine 572631 7168338Nathan Bitter mine 631100 7199820Nathans Deep South mine 631713 7198812Peak Hill opencut 672190 7163003Peak Hill townsite 673000 7163150Randell Bore 688000 7145200Ravelstone Group 669000 7167500Ravelstone opencut (Mn) 665734 7166777Ravelstone opencut (Mn) 669313 7166423Ruby Duffer Well 675290 7136000Ruby Well group 677900 7129700St Crispin prospect 691358 7158940Tank Well 675400 7147000Top Dimble Well 616600 7167600Trevs (and Starlight) opencut 636412 7198887Trillbar Homestead 576023 7170846Wembley mine 663983 7149044Wilgeena (Hit or Miss) mine 685369 7155622Wilthorpe mine 630414 7176521Yarlarweelor opencut 636723 7196423
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting
The Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collisionzone between the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains maficndashultramafic igneous rocks turbidites and chemical sedimentary rocks formed duringback-arc sea-floor spreading and rifting on the northern margin of the Yilgarn Cratonat or near a mid-oceanic ridge The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of theBryah Basin as a foreland structure resulting from either thec 1800 Ma oblique collision of the Pilbara and YilgarnCratons (Capricorn Orogeny) or the c 2000 Ma collisionof the Glenburgh Terrane and the Yilgarn Craton (GlenburghOrogeny) Important mineral deposits include orogenicgold-only lode deposits copperndashgold volcanogenic massivesulfides sedimentary and lateritic manganese and iron oreThe origin of the gold mineralization is related tometamorphism and deformation linked to the CapricornOrogeny at c 18 Ga The formation of other deposits isrelated to pre-orogenic syngenetic processes
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone (08) 9222 3459 Fax (08) 9222 3444wwwdmewagovau
Wandery
Creek
Wandery
Gum
Creek
Beda
burra
Easter
nCr
eek
Dim
ble
Dimble
Cree
k
Mt Fr
aser
Creek
Creek
Mt Fraser
Millidie CreekMURCHISONRIVER
MURCHISON
RIVER
GASCOYNE
RIVE
R
GASCOYNE
RIVER
Ck
Cree
k
Creek
Beatty Park B (abd)
Reefer W(abd)
YARLAR
WEELOR
MILGUN
ROAD
MEEKATHARRA
ROAD
ASHBURTON DOWNS
TrillbarYarlarweelor
ROADTRILLBAR
Mt Padbury
Yd
Yd
Yd
Yd
Yd Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd
MT CLARE
MEEKATHARRA
ROAD
Bryah
Narracoota
Old Peak Hill (ruin)
Mikhaburra
Yd
Yd
Yd
Yd
(ruin)Bilyuin Hotel
Yulga Jinna Community
Doolgunna
Yd
YdYd
Yd
THADUNACOPPER MINE ROAD
Yd
Karalundi
Yd
Yd
Yd
Yd
Bryah
Yd
Mikhaburra
Yarla
rwee
lor H
omes
tead
44
km
Milgun Homestead 4 km
Milgun Homestead 72 km
Meekatharra 108 km
Meekatharra 53 km
Mooloog
ool Ho
mestead
35 km
Diamond
Well
Homest
ead 68
km
Neds
Creek
Homest
ead 33
km
Kumerina Homestead 98 km
Three Rivers Homestead 42 km
MT LABOUCHERE
MT ARAPILES
CM 15
MT BEASLEY
MT SEABROOK
TALB
OT
DIVIDE
RED HILL
722 m
Yd
Yd
Yd
Yds
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd Yd
Yd
Yd
Yd
Yd
628 m
MT PADBURYMT FRASER
MT MAITLAND
R O B I N S O N
591 m
695 m
799 m
Yd
Yd
GREAT
NORTH
ERN
HIGH
WAY
HILL
THRE
E RIVER
S
ROAD
PEAK
MEEKATHARRA
ROAD
ROAD
PEAK HILL
R A N G E
Peak Hill
MC 14
NOONYEREENA HILL
MT LEAKE
MC 13
MC 12
MC 11
ASHBURTON DOWNS
core yard
602 m
605 m
640 m
Peak Hill
Yd
Earrie W Daulby W
Jilly Jilly W
Outcamp W (abd)
Watt W
Curly W
B
6 Mile B4 Corners W
Laurel W (abd)Bull W
Labouchere W
Sam W
Duffey W
Horseshoe W
Dandy W (PD)(abd)
Carlyon B (PD)
Kinder B (PD)
Vacation B
Garret W
Kylie B
Camel B
W (abd)Billarra W
Bull Paddock WAlarm B
Carlyon RH (PD)
Yaddyarra W
Mowara BGullgogo B
Horseshoe No 2 W (PD)Horseshoe No 1 W (PD)
Stink W (PD)
Crain B
Windalah B
Yandinhah W
Coomballey B
No 1 B
4 Corners W (abd)
Cement Tank W (abd)
Cork Tree B
Southern Cross W3 Corners B
Thompson B (abd)
W (abd)
Tommy B
Seabrook W17 Mile W (abd)
Midnight B
Gidgie WW (abd)
Snake W Dry W
Black Hill W
Minniarra W
Top Minniarra W
Doherty W
The Hut W
W
Red Hill W
Randall W
Dooley W
Walebie W
Mandora B
Babbawiri Pool
Winja B
WHWH
PBedaburra P
Friday P
Kerba P
S
Wandery P
W
Valley B
Quartz B
House WSouthern Cross W
P
Peak Hill B Shed W
Boundary B
No 3 W
McPherson B
Pinnacle B
WH
Mt Leake B
Hill B
Jack W
W
Mt Leake B
John B
No 2 B
Cow Hole B
WH
Red B
WH
No 6 W
Marck W
No 11 W
Limestone W
Dummy B
No 1 B
No 8 B
D
Government W
Central B
Gale W
W
West W
No 6 B
Ealgareengunna WH
Noonyereena P
Beefwood T
Narracoota B
WH
WH
Railway B
Meek W32 Mile W (Govt)
32 Mile W
Ruby W
Ruby South W
W (abd)
Scotty W
Ord W
Little Mill B
Killarney W
West WMillie W
D
Ord W (abd)
W(abd)
Eastern Stock W No 8(abd)
Gigbywabby W (PD)(abd)
No1 W
Paddy B (abd)
Kelly BRelief B
Top Dimble W
Despair B
Boundary B (PD)
B (abd)
Padbury W
Govt W (abd)
Bottom Dimble WHaystack W
Wandarrie W
Middle B
W
WW
W
No 3 B
Fish Pond B
Wooly Paddock B
5 Mile W
Knox W
Sleepy Hollow W (abd)
Old Homestead WB
Widespread W
W
Kennedy W
W
Deep W
Ross B
Gibbywabby WDandy W (PD)
Brunsden W
17 Mile WBrown Creek B (abd)
7 Mile BDavid W
17 Mile B (PD)
Lefeuvre W
Mick W
W (abd)
WH
WHWH
WH
WH
WH WH
S
Gum W (abd)
Wilthorpe W (PD)
1 Mile W
Bullgullan B
Wongawar B
Jinglegunna W
No 13 B
Orchard W
Fraser WW
Sorenson B
Central B
Tank W (abd)Bitter W (abd)
Murphy W
Trudgeon W
Moore W Spelling W
Randell B
Deadhorse W (abd) McLean W
Bore Hole BOHara W
Murchison W (abd)
McCarthy W2 Tank W (abd)
Hill W
Telegraph W
Cashman B (abd)
Ruby Centre W
White WW
McCann W (abd)
Holden W
Gum W
McDonald W
Don BNo 2 BNo 1 B
Bull W
D
D
DD
Gum Well P
Malleah P
Fremanga P
Yallaginda W (abd)
No 7 B (abd)
Stalley W (abd)
Durack W
No 26 W (abd)
Ruby Duffer W (abd)
WHs
WHs
WHWH
WH
WHWH
WH
P
PP
P
P
P
P
P
P
P
P
P
Ruby W (abd)
Narracoota W (abd)
WH S
P
B W
D T
(abd) (PD)
Cheroona W(abd)
Ti Tree B
56ocircocircocircocircYacute E 58 62 64 66 68 72
icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
56ocircocircocircocircYacute E 58 60 62 64 66 68 70 72 icirc40ocircocircocircocircYacute E
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14
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Yarlarweelor
Horseshoe
NathanDeep
Mt Seabrook
Labouchere
Wilthorpe
Wilgeena
Wembley
Livingstone
Harmony
Jubilee
Peak HillMt Pleasant
St Crispin
Durack
Heines Find
Mikhaburra
Cashman
Horseshoe Lights
Horseshoe
Yarlarweelor
Mn
T
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HOLDENS
BAXTER
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PEAK HILL
HORSESHOE
HOLDENS
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Fortnum
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M U R C H I S O N M I N E R A L F I E L D
M E E K A T H A R R A D I S T R I C T
P E A K H I L L M I N E R A L F I E L D
Goodin Fault Murchison Fault
Goodin Fault Murchison Fault
thrust
latera
l ramp
Billara Fault Kinders Fault
NARRYER
TERRANE
YILGARN
CRATON
Goodin F
ault
GOODIN
INLIER
Jenkin
Fault
Fault
Goodin
MARYMIA
INLIER
thrust ramp
Robinson Syncline
Peak Hill Anticline
Peak Hill Anticline
Horseshoe Anticline Millidie Syncline
Yarlarweelor gneiss belt
Marymia Inlier
40
MOUNT LEAKE FORMATION quartz arenite
DESPAIR GRANITE foliated to locally massive coarse-grained biotite granite late Archaean
30 km
Bangemall Group
Earaheedy Group
Padbury Group
Bryah Group
Mooloogool SubgroupDoolgunna_Thaduna Formations
Windplain Subgroup
Geological boundary
Fault
Finlayson Member quartz arenite
117frac34Yacute30Agrave
25frac34Yacute00Agrave
45Agrave118frac34Yacute00Agrave 15Agrave 30Agrave 45Agrave 119frac34Yacute00Agrave 15Agrave 119frac34Yacute30Agrave
25frac34Yacute00Agrave
15Agrave
30Agrave
45Agrave
26frac34Yacute00Agrave
26frac34Yacute10Agrave
119frac34Yacute30Agrave15Agrave119frac34Yacute00Agrave45Agrave15Agrave 30Agrave
118frac34Yacute00Agrave45Agrave117frac34Yacute30Agrave
26frac34Yacute10Agrave
26frac34Yacute00Agrave
45Agrave
30Agrave
15Agrave
Proterozoic granite
Q TR S
SEA LEVEL
5 km
11 km
F G
SEA LEVEL
5 km
11 km
L M O
SEA LEVEL
5 km
11 km
N
J K
SEA LEVEL
5 km
10 km
10 km
SEA LEVEL
5 km
H I
Archaean granitoid rock and greenstone
YerridaGroup
Maraloou_Killara Formations
SEA LEVEL
5 km
10 km
C D E
SEA LEVEL
5 km
10 km
A B
MILLIDIE CREEK FORMATION sandstone and shale minor granular iron-formation
ROBINSON RANGE FORMATION ferruginous shale and siltstone minor banded iron-formation
Beatty Park Member chloritic siltstone sandstone and breccia numerous mafic volcanic fragments
Heines Member quartz wacke siltstone and shale with minor polymictic conglomerate
LABOUCHERE FORMATION quartz wacke and siltstone local quartz pebble conglomerate layers turbiditic
KARALUNDI FORMATION sandstone with minor shale and conglomerate
JOHNSON CAIRN FORMATION siltstone and shale minor sandstone
JUDERINA FORMATION quartz wacke siltstone quartz arenite and quartz pebble conglomerate
PEAK HILL SCHIST quartz muscovite schist mylonitic schist and phyllonite
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS REPORT 59 PLATE 1
2
Trillbar Complexwith local magmatic layering well-preserved
interleaved foliated and metamorphosed basalt gabbro microgabbro pyroxenite and serpentinized peridotite
HORSESHOE FORMATION ferruginous chloritic shale and quartzEcircfeldspar wacke partly manganiferous andcalcareous minor iron-formation and chert
BANGEMALL
EARAHEEDY
PADBURYBASIN
BASINBRYAH
YERRIDABASIN
WILTHORPE FORMATION quartz pebble to boulder conglomerate predominant vein quartz clasts and some chert quartz wackeand granitoid rock clasts quartz wacke and finely bedded siltstone locally chloritic graded beds
1 2 3 4
C
58
78
75
20
15
SHEET INDEX
intruded by granite during the Capricorn Orogeny
High-grade gneissic granite and granite foliated derived predominantly from biotite monzogranite with numerouslenses of supracrustal rocks early middle and late Archaean components overprinted by structures and
NARRACOOTA FORMATION metabasalt and maficEcircultramafic schist locally pillowed with interflow sedimentary layers
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ne b
eltM
ount
Mai
tland
2672YacuteucircYacute3
lt1996YacuteucircYacute35
High-grade granitic gneiss derived predominantly from biotite monzogranite with numerous lenses ofsupracrustal rocks early middle and late Archaean components includes Palaeoproterozoicgranite sheets and dykes extensively deformed during Capricorn Orogeny
SCHEMATIC TECTONIC RELATIONSHIPS
BANGEMALL BASIN
1600 Ma and youngerc
EARAHEEDY BASIN
2000 Ma and youngercBRYAH BASIN
2000 Mac
YERRIDA BASIN
2200 Ma and youngerc
YILGARN CRATON
2600 Ma and olderc
PADBURY BASINyounger than 2000 Ma
BASIN
BASIN
igraveAn
igraveAndigraveAnhigraveAnuigraveAnxigraveAncigraveAnt
igraveAnf
ntildeg
ntildegn
ntildeng
igraveM
igraveE
igraved
igraveg
igraveP
igravePm
igravePmi
igravePmc
igravePr
igravePrg
igravePri
igravePw
igravePwb
igravePwh
igravePl
igravePli
igravePla
igraveAh
igraveAhi
igraveAr
igraveArc
igraveAnigraveAnd igraveAnh igraveAnu igraveAnx igraveAnc igraveAnt
igraveAk
igraveYm
igraveYc
igraveYj
igraveYjf
ntildegMl
ntilderMM
ntildegde
igraveAnf
igravePi
ethp
ethpm
ntildegMli
ntildegMla
igraveYjf
igraveYjf
igraveYj
igraved
igraved
igraveYm
igravePmigravePrg
igravePrigravePri
igravePwh
igraveAn
igraveAk ethp
igraveAnh igraveAnd
ntildegMl
igraveAnh
igraveAnxigraveYcigraveYj
igraveYjf
igraveAn
ethp
igraveAr igraveAr
igravePwh
ethpm igraveAn
igraveAn
igraveM
igravePrigravePri
igravePriigravePr
igraveAr
igraveAn
ethp
ethpm
igravePriigravePr igravePri
igravePw
igravePligravePla
igraveAh
igraveAn
igraveArc igraveAn
igraveArcigraveAnf
igraveAnd
igraveM
igraved
igraveAhiigravePm
igravePl
igraveAn
igraveAr
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igravePla igraveAhigraveAnc
igraveAn igraveAhigraveM
ntildegMl
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ntildegMl
ntildegMl
igraveAnd
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igravePwb
igravePl
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igravePr
igravePri
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igraveAr
igraved
igraveAn
igravePm
igravePwb
igravePr
igravePr
igravePri
igravePwigraveAnu
igravePm
igravePmc
igraveAr
igraveAk
igravePw
igraveM
ntildegMla
ntildegntildeg
ntildeg
ntildegntildeng
igraveM igraveM
igravePligraveAhi
igraveAhigraveAh
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ethp
ntildeng
igraved igraved
igraved
WA
NT
SA
NSW
Vic
Qld
Tas
ACT
GEOLO
G IC A L SUR VEY
WE
ST
E R N A U S T R AL
IA
GEOLOGICAL SURVEY OF
WESTERN AUSTRALIA
DAVID BLIGHT DIRECTOR
DEPARTMENT OF MINERALS
AND ENERGY
L C RANFORD DIRECTOR GENERAL
GOVERNMENT OF WESTERN AUSTRALIA
HON NORMAN MOORE MLC
MINISTER FOR MINES
Bangemall Group undivided
Mafic dyke interpreted from aeromagnetic data + positive anomaly - negative anomaly
Granite includes muscovite-bearing leucogranite and pegmatite
Padbury Group undivided metamorphosed and variably foliated metasedimentary rocks
Iron-formation and chert
Banded iron-formation minor ferruginous sandstone and shale
Bedded dolomite and dolomitic siltstone
Granular iron-formation
Banded iron-formation
Banded iron-formation and ferruginous chert
Quartz arenite minor interleaved quartz wacke and siltstone
Iron-formation and quartzEcircmagnetite(Ecircstilpnomelane) schist garnetiferous white chert in lenses
lithic wacke and siltstone turbiditic
Chert
Felsic schist derived from felsic volcanic and volcaniclastic rockDolerite in sills and dykesBasaltic hyaloclastiteMetaperidotite and picrite ultramafic schistBasaltic vent brecciaJasperoidal chert
Quartz mylonite
Foliated to mylonitic and massive granitoid rock
Amphibolite
Banded iron-formation
Granite with minor greenstone locally overprinted by structures formed during Capricorn Orogeny
Basalt ultramafic rock dolerite felsic schist banded iron-formation and chert
RAVELSTONE FORMATION
MES
OPRO
TERO
ZOIC
PALA
EOPR
OTER
OZOI
CAR
CHAE
AN
Bang
emal
lGr
oup
Eara
heed
yGr
oup
Padb
ury G
roup
Brya
h Gr
oup
Yerri
da G
roup
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Yarla
rwee
lor g
neiss
belt
Narry
er T
erra
ne
lowe
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hist to
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er a
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ibol
ite fa
cies
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phism
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prico
rn O
roge
ny
Mur
chiso
n Te
rrane
YILG
ARN
CRAT
ONYE
RRID
A BA
SIN
BRYA
H BA
SIN
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rn O
roge
ny
PADB
URY
BASI
N
Undivided MARALOOU DOOLGUNNA THADUNA and KILLARA FORMATIONS
Contact Bryah Group_Padbury Group
Structural symbols are numbered according totheir age of formation where known
Middle Proterozoic
Early Proterozoic
interpreted movement
Fold showing direction of plunge
Small-scale fold axial surface showing strike and dip
Bedding showing strike and dip
Foliation showing strike and dip
Lineation showing direction of plunge
Single zircon UEcircPb SHRIMP geochronology data
Nutman A P Bennett V C Kinny P D and Price R 1993 Large scale crustalstructure of the northwestern Yilgarn Craton Western Australia evidence fromNd isotopic data and zircon geochronology Tectonics v12 p 971-981
Nelson D R 1997 Geological Survey of Western Australia Record 19972
Nelson D R in prep Geological Survey of Western Australia Record 19982Mineral occurrence
Edited by D Ferdinando and G Loan
Cartography by P Taylor and B Williams
Topography from the Department of Land Administration Sheets SG 50-7 -8 -11 -12with modifications from geological field survey
Published by the Geological Survey of Western Australia Copies available fromthe Information Centre Department of Minerals and Energy 100 Plain StreetEast Perth WA 6004 Phone (08) 9222 3459 Fax (08) 9222 3444
This map is also available in digital form
Printed by the Sands Print Group Western Australia
The recommended reference for this map isSWAGER C P OCCHIPINTI S A and PIRAJNO F 1998 Interpreted Geology of thePalaeoproterozoic Bryah and Padbury Basins Western Australia Geological Survey Report 59 Plate 1
Unconformity (section only)
unconformity with local major onlap reworked as a fault
Geological boundary
Edmund fold belt unspecified
Capricorn Orogeny unspecified
Capricorn Orogeny DOtilde DUcirc Dccedil Deacute
Fault
Reactivated normal fault
lateral (plan view) dip slip (section)
away from observer
Strongly foliated rock
anticline
syncline
overturned anticline
overturned syncline
towards observer
Minor fold showing direction of plunge
inclined
vertical
inclined
vertical
overturned
bedding or layering trend
inclined
vertical
trend (section only)
GSWA identification number
mineral lineation
intersection lineation
Nutman et al identification number
interpreted age of intrusion in Ma with reference number
youngest detrital zircon
Highway with national route marker
Formed road
Track
Landing ground
Townsite population less than 1000
Mineral field boundary
Homestead
Locality
Building yard
Microwave repeater station
Horizontal control major
Watercourse ephemeral pool
Waterhole spring
Bore well windpump
Dam tank
Abandoned position doubtful
Mining centre
Mining locality
Mine (gold unless otherwise indicated)
Major opencut
Opencut
Alluvial workings
Prospect
Copper
Gold
Manganese
Talc
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
0 5 10 15 20 255000
Metres Kilometres
VERTICAL DATUM AUSTRALIAN HEIGHT DATUM
SCALE 1Yacute250Yacute000
Grid lines indicate 20Yacute000 metre interval of the Map Grid Australia Zone 50
HORIZONTAL DATUM GEOCENTRIC DATUM OF AUSTRALIA 1994UNIVERSAL TRANSVERSE MERCATOR PROJECTION
The Map Grid Australia (MGA) is based on the Geocentric Datum of Australia 1994 (GDA94)
GEOCENTRIC DATUM OF AUSTRALIA
GDA94 positions are compatible within one metre of the datum WGS84 positions
Reference points to align maps based on the previous datum AGD84 have been placed near the map corners
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS
2344
2345
2346
2347
2444
2445
2446
2447
2544
2545
2546
2547
2644
2645
2646
2647
2744
2745
2746
2747
2844
2845
2846
2847
KALLI
MILEURA
GOULD
ERRABIDDY
MADOONGA
KOONMARRA
MOORARIE
MARQUIS
MEEKATHARRA
TIERACO
PADBURY
MILGUN
GABANINTHA
GLENGARRY
BRYAH
JAMINDI
YAGANOO
MOOLOOGOOL
DOOLGUNNA
MEREWETHER
THADUNA
MARYMIA
MOUNT BARTLE
THREE RIVERS
118958
88YacuteEcirc168
BELELE GLENGARRY
ROBINSON RANGE PEAK HILL
SG 50-7 SG 50-8
SG 50-11 SG 50-12
1100Yacute000 maps shown in black
Compiled by C P Swager S A Occhipinti and F Pirajno 1997
N
P
Geology from 1100Yacute000 GSWA maps (see sheet index)
See current GSWA map catalogue for the full range of published products
and by S A Occhipinti C P Swager 1995 1997 and J S Myers 1995
Published 1100Yacute000 maps used in compilation
1250Yacute000 maps shown in brown
+ means declination is east and correction must be
subtracted from compass bearing to give true bearing
Annual change is 1Agrave easterly
The lines indicate magnetic declination 1995
added to compass bearing to give true bearing
- means declination is west and correction must be
SEA LEVEL
5 km
11 km
brvbar Western Australia 1998
117frac34 30Agrave25frac3400Agrave
118frac3400Agrave 119frac3400Agrave 120frac3400Agrave
26frac3400Agrave
INTERPRETED GEOLOGY OF THE PALAEOPROTEROZOIC
AREA OF THIS MAP
GSWA
REPORT 60
PLATE 1
E
Version 11 _ May 2004
Q
R
S
T
F
G
L
M
O
P
N
J
K
C
D
E
A
B
H
I
1 2 3
1
2
3
cc 3300
1
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
2672YacuteucircYacute32
1808YacuteucircYacute6
3
cc 3300
1
3300
1
lt1996YacuteucircYacute352
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
lt1785YacuteucircYacute112
2672YacuteucircYacute32
2672YacuteucircYacute32
- Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
-
- Contents
- Abstract
- Introduction
- Regional tectonic setting
- Geology stratigraphy and geochronology
-
- Peak Hill Schist and Marymia Inlier
- Bryah Group
-
- Karalundi Formation
- Narracoota Formation
-
- Peridotitic and high-Mg basalt association
- Intrusive rocks and layered intrusions
- Mafic and ultramafic schist
- Metabasaltic hyaloclastite
- Felsic schist
- Volcaniclastic rocks
- Carbonated and silicified metavolcanic rocks
- Jasperoidal chert
- Geochemistry of the Narracoota Formation
-
- Ravelstone Formation
- Horseshoe Formation
-
- Padbury Group
-
- Labouchere Formation
- Wilthorpe Formation
-
- Beatty Park and Heines Members
-
- Robinson Range Formation
- Millidie Creek Formation
- Unassigned units of the Padbury Group
-
- Structure
-
- D1 structures
- D2 structures
- D3 structures and their relationship to D2 structures
- D4 structures
-
- Metamorphism
- Structural synthesis
- Mineralization
-
- Gold deposits
-
- Peak Hill Jubilee and Mount Pleasant deposits
- Harmony deposit
- Labouchere Nathans and Fortnum deposits
- Wembley deposit
- Wilgeena deposit
- Durack St Crispin and Heines Find prospects
- Ruby Well group
- Mikhaburra deposit
- Wilthorpe deposit
- Cashman deposit
-
- Volcanogenic copperndashgold deposits
- Supergene manganese deposits
- Iron ore
- Talc
- Discussion
-
- Tectonic model and conclusions
- Acknowledgements
- References
- Appendix Gazetteer of localities
- Plate 1 Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
- Figures
-
- Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
- Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins
- Figure 3 Rotated orthoclase porphyroblast Peak Hill Schist
- Figure 4 Partially recrystallized mylonite Peak Hill Schist
- Figure 5 Peak Hill Schist mylonite from the Hangingwall Sequence
- Figure 6 Outcrop of quartz mylonite Peak Hill Schist
- Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric
- Figure 8 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt)
- Figure 9 Basaltic hyaloclastite Narracoota Formation
- Figure 10 Mafic volcaniclastic rock Narracoota Formation
- Figure 11 Volcanic breccia intersected in diamond drillhole BD1
- Figure 12 Total alkali versus silica diagram for rocks the Narracoota Formation
- Figure 13 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the Narracoota Formation
- Figure 14 Geochemical characteristics of the Narracoota Formation rocks
- Figure 15 Geochemical discriminant plots for Narracoota Formation
- Figure 16 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation
- Figure 17 Schematic stratigraphy of the Horseshoe Formation
- Figure 18 Major regional structures in the Bryah and Padbury Groups
- Figure 19 Simplified geological map of the Bryah and Padbury Groups
- Figure 20 Selected hypothetical cross sections through the Bryah and Padbury Groups
- Figure 21 Model of the structural development of the BryahndashPadbury Group succession
- Figure 22 New model of the structural development of the BryahndashPadbury Group succession
- Figure 23 New model for the structural development of the BryahndashPadbury Group succession and the Peak Hill Schist
- Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins
- Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins
- Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH 1100 000 map sheet
- Figure 27 Albite porphyroblasts in mylonitic schist at Mount Pleasant
- Figure 28 The Mine Sequence schist
- Figure 29 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit
- Figure 30 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and Marker quartzite unit
- Figure 31 Diagrammatic cross section of the Harmony ore zones
- Figure 32 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and deformed Despair Granite
- Figure 33 Sketch illustrating a conceptual model for the origin of precious and base metal deposits in the BryahndashPadbury and Yerrida Basins
- Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins within the context of the Capricorn Orogen
-
- Tables
-
- Table 1 Stratigraphy of the Bryah and Padbury Groups
- Table 2 Representative chemical analyses of the Narracoota Formation
- Table 3 Magnesium numbers for the Narracoota and Killara Formations
- Table 4 Selected geochemical parameters for the Narracoota Formation
- Table 5 Sequence of deformation events in the Bryah and Padbury Basins
- Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group and deformation fabrics
- Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
- Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
- Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
-
GEOCHEMICAL ANALYSES OF ROCKS FROM THE NARRACOOTA FORMATION For details of analytical techniques see in text of Report 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
Sample | Easting | Northing | SiO2 | TiO2 | Al2O3 | Fe2O3 | FeO | MnO | MgO | CaO | Na2O | K2O | P2O5 | LOI | H2O- | H2O+ | TOTAL | CO2 | Ag | As | Au | Ba | Bi | Cd | Ce | Cr | Co | Cu | Ga | Ge | La | Li | Mo | Mn | Nb | Ni | Pb | Pd | Pt | Rb | Sb | Sc | Sn | Sr | Ta | Te | Th | Ti | U | V | Y | W | Zn | Zr | Hf | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm | Yb | Lu | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86342 | 746314 | 7198282 | 5151 | 032 | 1523 | 928 | 018 | 1049 | 1007 | 269 | 019 | 003 | 673 | 166 | 1 | 95 | 12 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86383 | 670171 | 7163822 | 5353 | 091 | 1468 | 115 | 019 | 744 | 863 | 299 | 005 | 008 | 253 | 100 | 1 | 85 | 21 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86384 | 670171 | 7163822 | 5048 | 062 | 1444 | 991 | 016 | 1135 | 933 | 362 | 004 | 005 | 640 | 209 | 1 | 157 | 16 | 33 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86397 | 799422 | 7201118 | 5529 | 026 | 1502 | 817 | 017 | 1136 | 416 | 549 | 005 | 002 | 1174 | 244 | 0 | 44 | 15 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104248 | 722651 | 7168587 | 4925 | 022 | 1137 | 963 | 017 | 1818 | 948 | 159 | 009 | 002 | 1 | 80 | 9 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104249 | 722651 | 7168587 | 4911 | 026 | 1065 | 973 | 017 | 2016 | 855 | 126 | 009 | 003 | 1 | 34 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104254 | 715830 | 7171470 | 4948 | 023 | 1121 | 95 | 016 | 2035 | 706 | 194 | 005 | 002 | 1877 | 647 | 1 | 49 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104255 | 715830 | 7171470 | 52 | 033 | 143 | 847 | 017 | 1071 | 1087 | 31 | 002 | 003 | 664 | 209 | 0 | 133 | 13 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256 | 715830 | 7171470 | 5244 | 067 | 1455 | 1007 | 019 | 834 | 983 | 376 | 007 | 007 | 0 | 140 | 17 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104257 | 713820 | 7171502 | 5144 | 092 | 1453 | 1078 | 02 | 689 | 1244 | 248 | 023 | 009 | 265 | 79 | 3 | 195 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104264 | 685287 | 7155494 | 5303 | 062 | 1391 | 94 | 017 | 768 | 1239 | 265 | 01 | 006 | 720 | 222 | 1 | 90 | 15 | 32 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104265 | 685287 | 7155494 | 5332 | 025 | 1592 | 97 | 017 | 658 | 1215 | 184 | 003 | 004 | 353 | 67 | 1 | 30 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104288 | 661877 | 7126843 | 5979 | 024 | 1346 | 798 | 016 | 522 | 1265 | 042 | 004 | 004 | 283 | 46 | 0 | 17 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104289 | 656054 | 7130760 | 5446 | 014 | 1559 | 955 | 017 | 826 | 957 | 204 | 019 | 003 | 358 | 116 | 4 | 43 | 8 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104292 | 657132 | 7123177 | 5103 | 09 | 1369 | 971 | 017 | 827 | 1334 | 272 | 009 | 008 | 0 | 165 | 18 | 51 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104294 | 664424 | 7119210 | 5108 | 095 | 1449 | 1021 | 018 | 879 | 1094 | 283 | 046 | 008 | 523 | 141 | 5 | 123 | 19 | 52 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104295 | 664424 | 7119210 | 5228 | 096 | 1446 | 1022 | 018 | 946 | 856 | 364 | 016 | 009 | 465 | 132 | 2 | 79 | 19 | 54 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104298 | 669014 | 7106533 | 5233 | 087 | 1367 | 939 | 017 | 778 | 1189 | 373 | 01 | 008 | 514 | 116 | 1 | 116 | 17 | 49 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104299 | 669014 | 7106533 | 5166 | 093 | 1404 | 982 | 018 | 823 | 1183 | 305 | 017 | 009 | 491 | 117 | 3 | 124 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104300 | 669014 | 7106533 | 477 | 05 | 173 | 984 | 019 | 747 | 1484 | 197 | 016 | 004 | 3 | 142 | 12 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104386 | 676392 | 7146500 | 5373 | 037 | 1501 | 846 | 016 | 864 | 977 | 373 | 009 | 004 | 557 | 152 | 0 | 106 | 18 | 18 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104391 | 687552 | 7144198 | 5002 | 023 | 845 | 934 | 016 | 2281 | 88 | 014 | 002 | 002 | 0 | 15 | 11 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104392 | 687552 | 7144198 | 5391 | 027 | 92 | 998 | 014 | 2087 | 515 | 017 | 027 | 003 | 2508 | 1103 | 12 | 16 | 22 | 10 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393 | 687539 | 7143275 | 508 | 023 | 965 | 1025 | 01 | 289 | 004 | 0 | 001 | 001 | 0 | 3 | 5 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104394 | 687539 | 7143275 | 5594 | 05 | 1494 | 867 | 019 | 73 | 697 | 537 | 006 | 006 | 363 | 88 | 0 | 90 | 19 | 24 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104397 | 670399 | 7142584 | 4687 | 019 | 1023 | 1015 | 017 | 2496 | 726 | 015 | 001 | 001 | 2786 | 971 | 0 | 7 | 8 | 4 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104398 | 669575 | 7143518 | 5329 | 035 | 1453 | 813 | 014 | 828 | 1207 | 315 | 002 | 004 | 574 | 124 | 0 | 78 | 13 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104399 | 670423 | 7144430 | 5183 | 036 | 1491 | 866 | 016 | 932 | 1147 | 323 | 002 | 003 | 682 | 173 | 0 | 42 | 14 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104400 | 670023 | 7145280 | 4958 | 037 | 1577 | 987 | 019 | 1044 | 1082 | 291 | 002 | 003 | 510 | 124 | 0 | 68 | 17 | 15 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109487 | 638809 | 7157725 | 5719 | 043 | 1423 | 73 | 013 | 868 | 626 | 569 | 004 | 004 | 442 | 116 | 0 | 18 | 11 | 19 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109492 | 663796 | 7149130 | 5231 | 011 | 617 | 72 | 015 | 24 | 1002 | 001 | 001 | 001 | 0 | 7 | 5 | 1 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109493 | 663796 | 7149130 | 5246 | 047 | 1508 | 881 | 019 | 766 | 1218 | 247 | 064 | 005 | 478 | 90 | 6 | 72 | 15 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109504 | 670124 | 7121353 | 5396 | 048 | 149 | 859 | 015 | 716 | 1237 | 231 | 003 | 005 | 445 | 96 | 0 | 61 | 17 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109513 | 732634 | 7164722 | 5396 | 197 | 1434 | 953 | 02 | 638 | 686 | 592 | 064 | 019 | 16 | 117 | 24 | 97 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601 | 668775 | 7146298 | 5332 | 179 | 1568 | 102 | 025 | 644 | 561 | 601 | 053 | 017 | 10 | 105 | 21 | 90 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112603 | 672130 | 7147178 | 108 | 034 | 2 | 1698 | lt10 | 462 | lt4 | lt5 | lt6 | 559 | 54 | 12 | lt3 | 6 | lt2 | lt7 | 115 | lt4 | 87 | 4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 167 | 19 | 92 | 203 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604 | 672238 | 7155486 | 202 | lt001 | 3 | lt4 | 40 | 34 | 8 | lt5 | 73 | 3639 | 69 | 16 | lt3 | 38 | lt2 | lt7 | 143 | 20 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | lt2 | lt2 | 453 | 29 | 20 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112620 | 626709 | 7204920 | 33 | 001 | 2 | lt4 | 220 | 35 | lt4 | lt5 | 19 | 1377 | 78 | 22 | lt3 | 25 | lt2 | 9 | 127 | 26 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | 10 | lt2 | 358 | 22 | 13 | 182 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112621 | 626709 | 7204920 | 116 | 011 | 1 | 144 | lt10 | lt11 | lt4 | lt5 | lt6 | 2354 | 82 | 8 | lt3 | lt5 | lt2 | lt7 | 1589 | lt4 | lt2 | 9 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 131 | 6 | 72 | 20 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112624 | 661284 | 7183319 | 507 | 074 | 139 | 274 | 769 | 018 | 791 | 104 | 244 | 025 | 007 | 358 | 1007 | 1 | lt4 | lt10 | 54 | lt4 | lt5 | lt6 | 186 | 92 | 13 | lt3 | lt5 | lt2 | lt7 | 96 | lt4 | 6 | lt4 | lt4 | 97 | lt5 | lt6 | lt2 | lt2 | 264 | 18 | 77 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112625 | 661284 | 7183319 | 498 | 074 | 143 | 244 | 747 | 016 | 831 | 116 | 237 | 03 | 007 | 324 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 354 | 90 | 12 | lt3 | lt5 | lt2 | lt7 | 111 | lt4 | 4 | lt4 | lt4 | 85 | lt5 | lt6 | lt2 | lt2 | 241 | 15 | 79 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112628 | 661284 | 7183319 | 49 | 08 | 138 | 357 | 726 | 018 | 738 | 14 | 143 | 008 | 007 | 277 | 1006 | 2 | lt4 | lt10 | 147 | lt4 | lt5 | 6 | 167 | 91 | 14 | lt3 | lt5 | lt2 | lt7 | 101 | lt4 | lt2 | lt4 | lt4 | 310 | lt5 | lt6 | lt2 | lt2 | 265 | 19 | 77 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112629 | 661284 | 7183319 | 642 | 049 | 103 | 271 | 402 | 012 | 438 | 113 | 051 | 013 | 005 | 18 | 1001 | lt1 | lt4 | lt10 | 109 | lt4 | lt5 | lt6 | 113 | 58 | 12 | lt3 | lt5 | lt2 | lt7 | 60 | lt4 | 2 | lt4 | lt4 | 86 | lt5 | lt6 | lt2 | lt2 | 166 | 11 | 50 | 39 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112640 | 675227 | 7128672 | 49 | 052 | 147 | 272 | 517 | 014 | 915 | 148 | 142 | 011 | 005 | 221 | 1002 | 1 | lt4 | lt10 | 90 | lt4 | lt5 | lt6 | 277 | 38 | 13 | lt3 | lt5 | lt2 | lt7 | 160 | lt4 | 2 | 5 | lt4 | 184 | lt5 | lt6 | lt2 | lt2 | 212 | 11 | 54 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112641 | 675215 | 7127749 | 508 | 079 | 142 | 308 | 703 | 017 | 744 | 118 | 207 | 012 | 008 | 299 | 1008 | 1 | lt4 | 90 | 26 | lt4 | lt5 | lt6 | 266 | 102 | 14 | lt3 | lt5 | lt2 | lt7 | 120 | lt4 | lt2 | lt4 | lt4 | 148 | lt5 | lt6 | lt2 | lt2 | 258 | 16 | 80 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643 | 675190 | 7125902 | 275 | 205 | lt1 | 10 | 40 | 767 | lt4 | lt5 | 175 | 994 | 257 | 12 | 3 | 12 | 2 | lt7 | lt3 | 34 | lt2 | lt4 | lt4 | 43 | lt5 | lt6 | lt2 | lt2 | 272 | 13 | 96 | 25 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112645 | 663956 | 7162053 | 23 | 059 | lt1 | 7 | lt10 | 227 | lt4 | lt5 | 34 | 2117 | 390 | 3 | 12 | lt2 | 8 | lt3 | 12 | lt2 | lt4 | 8 | 10 | lt5 | lt6 | 6 | lt2 | 467 | 14 | 81 | 132 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112646 | 663956 | 7162053 | 507 | 076 | 139 | 224 | 796 | 018 | 771 | 991 | 258 | 063 | 007 | 375 | 1005 | 1 | lt4 | lt10 | 164 | lt4 | lt5 | 6 | 207 | 79 | 13 | lt3 | lt5 | lt2 | lt7 | 123 | lt4 | 16 | lt4 | lt4 | 338 | lt5 | lt6 | lt2 | lt2 | 245 | 15 | 77 | 55 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112647 | 663956 | 7162053 | 356 | 002 | 1 | 133 | 1170 | lt11 | lt4 | lt5 | 13 | 489 | 846 | 6 | 4 | 6 | lt2 | lt7 | 533 | 1491 | lt2 | 4 | lt4 | lt2 | lt5 | 8 | lt2 | lt2 | 104 | 12 | 180 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112650 | 663956 | 7162053 | 573 | 424 | 959 | 166 | 036 | lt005 | 12 | 226 | 012 | 028 | 005 | 75 | 999 | 1 | lt4 | lt10 | 423 | lt4 | lt5 | 152 | 481 | 119 | 20 | lt3 | 90 | lt2 | 27 | 171 | 10 | 12 | lt4 | lt4 | 61 | lt5 | lt6 | 6 | lt2 | 365 | 37 | 54 | 296 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112652 | 663956 | 7162053 | 526 | 088 | 133 | 253 | 762 | 022 | 745 | 741 | 31 | 081 | 008 | 474 | 1009 | 1 | lt4 | lt10 | 242 | lt4 | lt5 | lt6 | 149 | 158 | 12 | lt3 | lt5 | lt2 | lt7 | 99 | 6 | 17 | 5 | lt4 | 87 | lt5 | lt6 | 2 | lt2 | 260 | 22 | 88 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112672 | 734725 | 7164593 | 628 | 07 | 136 | 355 | 364 | 034 | 337 | 494 | 286 | 093 | 009 | 313 | 1001 | 1 | lt4 | 20 | 258 | lt4 | lt5 | 76 | 122 | 16 | 17 | lt3 | 34 | lt2 | 17 | 75 | 13 | 19 | lt4 | 4 | 164 | lt5 | lt6 | 22 | 2 | 99 | 26 | 73 | 216 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 69 | 108 | 111 | 258 | 508 | 009 | 415 | 016 | 312 | 036 | 007 | 361 | 1006 | 1 | lt4 | lt10 | 386 | lt4 | lt5 | 30 | 56 | lt4 | 14 | lt3 | 18 | lt2 | 17 | 24 | lt4 | 17 | lt4 | lt4 | 79 | lt5 | lt6 | 8 | lt2 | 239 | 19 | 79 | 119 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 633 | 136 | 113 | 297 | 736 | 012 | 617 | 025 | 21 | 012 | 018 | 499 | 1004 | 1 | lt4 | 20 | 460 | lt4 | lt5 | 18 | 19 | 56 | 14 | lt3 | 10 | lt2 | 17 | 32 | 12 | 4 | lt4 | lt4 | 30 | lt5 | lt6 | 9 | 3 | 312 | 32 | 109 | 153 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 631 | 137 | 115 | 248 | 803 | 009 | 662 | 024 | 211 | lt005 | 016 | 496 | 1008 | 1 | lt4 | 20 | 28 | lt4 | lt5 | 37 | 21 | 203 | 17 | lt3 | 17 | 3 | 19 | 30 | 6 | lt2 | lt4 | lt4 | 27 | lt5 | lt6 | 9 | 3 | 336 | 24 | 107 | 158 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 129 | 697 | lt1 | 4 | 1250 | 1768 | lt4 | lt5 | 69 | 597 | 472 | 11 | lt3 | 53 | lt2 | lt7 | 327 | 22 | 90 | lt4 | lt4 | 226 | lt5 | lt6 | 8 | 2 | 181 | 19 | 118 | 101 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112675 | 734644 | 7166319 | 569 | 025 | 767 | 183 | 429 | 013 | 153 | 768 | 303 | 007 | lt005 | 396 | 1013 | 1 | lt4 | lt10 | 55 | lt4 | lt5 | lt6 | 541 | 26 | 4 | lt3 | lt5 | lt2 | lt7 | 262 | lt4 | 2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 117 | 9 | 46 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112678 | 734655 | 7166965 | 715 | 009 | 411 | 133 | 335 | 006 | 112 | 341 | 016 | lt005 | lt005 | 442 | 999 | 1 | lt4 | lt10 | 32 | lt4 | lt5 | lt6 | 1537 | 11 | 3 | lt3 | lt5 | lt2 | lt7 | 659 | lt4 | lt2 | lt4 | lt4 | 4 | lt5 | lt6 | lt2 | lt2 | 69 | 5 | 33 | 8 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112679 | 735684 | 7171472 | 518 | 034 | 135 | 289 | 531 | 014 | 945 | 12 | 267 | lt005 | lt005 | 277 | 1011 | 1 | lt4 | lt10 | 51 | lt4 | lt5 | lt6 | 670 | 56 | 12 | lt3 | lt5 | lt2 | lt7 | 272 | lt4 | lt2 | lt4 | lt4 | 60 | lt5 | lt6 | lt2 | lt2 | 198 | 16 | 55 | 21 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112680 | 735675 | 7172519 | 515 | 037 | 148 | 282 | 565 | 015 | 864 | 991 | 357 | lt005 | lt005 | 314 | 1008 | 1 | lt4 | lt10 | 83 | lt4 | lt5 | lt6 | 470 | 88 | 12 | lt3 | lt5 | lt2 | lt7 | 192 | lt4 | lt2 | 5 | lt4 | 88 | lt5 | lt6 | lt2 | lt2 | 216 | 17 | 62 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116407 | 603693 | 7169737 | 279 | lt001 | 1 | 4 | lt10 | 126 | lt4 | lt5 | 12 | 140 | 34 | lt3 | 3 | 7 | lt2 | 11 | 191 | 7 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | 3 | lt2 | 36 | 11 | 21 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116410 | 608442 | 7170499 | 211 | lt01 | lt1 | lt4 | lt10 | 726 | lt4 | lt5 | 6 | 696 | 17 | lt3 | lt3 | 5 | lt2 | lt7 | 82 | 4 | lt2 | lt4 | lt4 | 24 | lt5 | lt6 | 2 | lt2 | 40 | 5 | 10 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116415 | 611248 | 7168937 | 904 | lt005 | 265 | 094 | 095 | lt005 | 248 | 005 | 005 | lt005 | lt005 | 263 | 1005 | lt1 | 4 | lt10 | 947 | lt4 | lt5 | lt6 | 944 | 13 | lt3 | lt3 | 5 | lt2 | lt7 | 394 | lt4 | lt2 | lt4 | lt4 | 28 | lt5 | lt6 | lt2 | lt2 | 35 | 7 | 22 | lt5 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116428 | 614781 | 7170999 | 484 | 016 | 723 | 188 | 628 | 014 | 215 | 813 | 077 | lt005 | lt005 | 61 | 1011 | 1 | 4 | lt10 | 14 | lt4 | lt5 | lt6 | 2275 | 12 | 4 | lt3 | lt5 | lt2 | lt7 | 998 | lt4 | lt2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 126 | 8 | 60 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116429 | 614810 | 7171215 | 113 | 029 | 13 | 129 | 10 | 66 | lt4 | lt5 | lt6 | 2489 | 60 | 7 | lt5 | 15 | lt7 | 1344 | lt4 | 3 | 89 | 25 | lt4 | 75 | lt5 | 8 | lt2 | lt2 | 183 | 11 | 127 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116430 | 614807 | 7170845 | 217 | 002 | 10 | 12 | 2570 | 32 | lt4 | lt5 | 22 | 1581 | 463 | 4 | lt5 | lt6 | lt7 | 286 | 109 | lt2 | lt4 | 53 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 348 | 13 | 95 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116432 | 614348 | 7169311 | 101 | 009 | 6 | 5 | 80 | 44 | lt4 | lt5 | 15 | 1757 | 116 | lt3 | 7 | lt6 | 11 | 683 | lt4 | lt2 | lt4 | 37 | lt4 | 27 | lt5 | lt6 | lt2 | lt2 | 327 | 18 | 119 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116433 | 614232 | 7168820 | 211 | 029 | lt5 | 7 | 60 | 2075 | lt4 | lt5 | 35 | 254 | 126 | 5 | 26 | lt6 | 13 | 186 | 13 | 27 | 4 | 12 | lt4 | 56 | lt5 | lt6 | 4 | lt2 | 152 | 25 | 120 | 100 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116442 | 632664 | 7159418 | 414 | 022 | 21 | 7 | 10 | 710 | lt4 | lt5 | lt6 | 39 | 716 | lt3 | lt5 | lt6 | lt7 | 35 | 4 | lt2 | lt4 | 40 | lt4 | 28 | lt5 | 6 | lt2 | lt2 | 1073 | 16 | 137 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116443 | 634091 | 7159896 | 461 | 035 | 144 | 279 | 528 | 018 | 746 | 165 | 174 | 005 | lt005 | 545 | 1005 | 2 | lt4 | lt10 | 23 | lt4 | lt5 | lt6 | 443 | 62 | 15 | lt3 | lt5 | lt2 | lt7 | 164 | lt4 | lt2 | lt4 | lt4 | 63 | lt5 | lt6 | lt2 | lt2 | 233 | 17 | 56 | 22 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116444 | 633832 | 7161837 | 11 | 021 | lt1 | 13 | lt10 | 1185 | lt4 | lt5 | 42 | 173 | 66 | 13 | lt3 | 24 | lt2 | 14 | 67 | 10 | 23 | lt4 | lt4 | 28 | lt5 | lt6 | 4 | lt2 | 245 | 18 | 61 | 87 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116446 | 633910 | 7169621 | 458 | 014 | 847 | 147 | 74 | 016 | 22 | 765 | 02 | lt005 | lt005 | 71 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 2882 | 12 | 7 | lt3 | lt5 | lt2 | lt7 | 1306 | lt4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 142 | 8 | 67 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454 | 653363 | 7152948 | 174 | 01 | lt1 | 15 | 130 | 111 | lt4 | lt5 | lt6 | 389 | 106 | 21 | lt3 | lt5 | lt2 | lt7 | 204 | lt4 | 16 | lt4 | lt4 | 12 | lt5 | lt6 | lt2 | lt2 | 450 | 10 | 122 | 55 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477 | 645436 | 7177439 | 178 | 007 | lt1 | lt4 | 30 | 52 | lt4 | lt5 | lt6 | 689 | 88 | 21 | lt3 | 55 | lt2 | lt7 | 456 | 5 | 13 | lt4 | lt4 | 5 | lt5 | lt6 | lt2 | lt2 | 435 | 98 | 350 | 69 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485 | 655767 | 7129994 | 225 | 018 | lt1 | lt4 | lt10 | 78 | lt4 | lt5 | lt6 | 5612 | 129 | 8 | 3 | lt5 | 2 | 7 | 88 | 4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 119 | 7 | 39 | 38 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487 | 655561 | 7129043 | 168 | 013 | 1 | lt4 | lt10 | 191 | lt4 | lt5 | 11 | 4578 | 8 | 6 | lt3 | lt5 | lt2 | lt7 | 464 | 11 | 10 | lt4 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 87 | 7 | 70 | 35 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116488 | 655420 | 7128860 | 156 | 012 | lt1 | lt4 | 40 | 119 | lt4 | lt5 | 19 | 135 | 279 | 31 | lt3 | 7 | 2 | 7 | 313 | 21 | 23 | lt4 | lt4 | 15 | lt5 | lt6 | 3 | 3 | 585 | 10 | 97 | 149 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 128 | 007 | lt1 | lt4 | 170 | 169 | lt4 | lt5 | lt6 | 5588 | 63 | 4 | lt3 | lt5 | lt2 | lt7 | 687 | 14 | 12 | lt4 | lt4 | 6 | lt5 | 8 | 2 | 2 | 75 | 7 | 81 | 30 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 681 | 02 | 2 | 8 | lt10 | 34 | lt4 | lt5 | lt6 | 967 | 299 | 6 | lt3 | 9 | lt2 | lt7 | 348 | lt4 | lt2 | lt4 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 469 | 35 | 110 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116490 | 655978 | 7126699 | 491 | 078 | 147 | 315 | 779 | 017 | 816 | 994 | 274 | 065 | 008 | 371 | 1012 | 1 | lt4 | 20 | 228 | lt4 | lt5 | lt6 | 191 | 103 | 13 | lt3 | lt5 | lt2 | lt7 | 116 | lt4 | 9 | lt4 | lt4 | 300 | lt5 | lt6 | lt2 | lt2 | 267 | 17 | 87 | 56 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116491 | 656084 | 7126206 | 50 | 07 | 133 | 216 | 817 | 019 | 999 | 939 | 208 | 035 | 007 | 402 | 1007 | 1 | lt4 | 10 | 329 | lt4 | lt5 | lt6 | 471 | 104 | 12 | lt3 | lt5 | lt2 | lt7 | 249 | lt4 | 6 | 4 | lt4 | 157 | lt5 | lt6 | lt2 | lt2 | 241 | 16 | 82 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116492 | 656023 | 7125806 | 10 | 27 | 10 | 213 | lt4 | lt5 | lt6 | 17 | 170 | lt3 | lt5 | 7 | lt7 | 40 | lt4 | 49 | 4 | 49 | lt4 | 38 | 803 | lt6 | lt2 | lt2 | 434 | 28 | 45 | 58 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493 | 655992 | 7125530 | 13 | 25 | 60 | 150 | lt4 | lt5 | lt6 | 24 | 393 | lt3 | 6 | 10 | lt7 | 118 | 6 | 79 | lt4 | 55 | lt4 | 31 | 269 | lt6 | lt2 | lt2 | 464 | 37 | 239 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116498 | 709849 | 7162239 | 11 | 19 | 5000 | 269 | lt4 | lt5 | lt6 | 140 | 92 | lt3 | lt5 | 6 | lt7 | 83 | lt4 | 74 | lt4 | 47 | lt4 | 50 | 301 | lt6 | lt2 | lt2 | 316 | 25 | 123 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116500 | 709011 | 7162160 | 9 | 29 | 10 | 155 | lt4 | lt5 | lt6 | 27 | 121 | lt3 | lt5 | 6 | lt7 | 39 | 5 | 33 | lt4 | 66 | lt4 | 20 | 155 | lt6 | lt2 | lt2 | 535 | 34 | 28 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501 | 708508 | 7162137 | 11 | 6 | 20 | 23 | lt4 | lt5 | lt6 | 29 | 146 | lt3 | lt5 | 6 | lt7 | 102 | lt4 | 98 | lt4 | 57 | lt4 | 31 | 195 | 6 | lt2 | lt2 | 416 | 35 | 144 | 74 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116502 | 708368 | 7162139 | 756 | 052 | lt1 | 8 | lt10 | 368 | lt4 | lt5 | 11 | 25 | 398 | lt3 | lt3 | 12 | 2 | lt7 | 151 | 6 | lt2 | lt4 | 4 | 23 | lt5 | lt6 | lt2 | lt2 | 207 | 15 | 211 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116532 | 672308 | 7165117 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | 1009 | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | 117 | 13 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 5 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 275 | 21 | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120337 | 668950 | 7146475 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | nd | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | nd | 117 | 13 | lt5 | nd | lt2 | lt7 | 104 | lt4 | nd | nd | 5 | lt4 | nd | lt4 | 129 | lt2 | 44963 | lt2 | 275 | 21 | nd | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120340 | 669175 | 7145725 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | 1009 | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | 92 | 14 | lt3 | lt5 | lt2 | lt7 | 118 | lt4 | 4 | 4 | lt4 | 132 | lt5 | lt6 | 2 | lt2 | 259 | 18 | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369 | 665175 | 7156150 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | nd | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | nd | 92 | 14 | lt5 | nd | lt2 | lt7 | 118 | lt4 | nd | nd | 4 | 40 | nd | lt4 | 132 | 2 | 46162 | lt2 | 259 | 18 | nd | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373 | 675250 | 7167875 | 50 | 078 | 146 | 288 | 732 | 017 | 757 | 112 | 256 | lt005 | 008 | 328 | 328 | 1006 | nd | lt1 | lt4 | lt10 | 101 | lt4 | lt5 | lt6 | 224 | nd | 100 | 14 | lt3 | lt5 | nd | lt2 | lt7 | 125 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 120 | lt5 | lt6 | lt2 | 46761 | lt2 | 262 | 16 | nd | 84 | 57 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432 | 673950 | 7171700 | 52 | 077 | 146 | 219 | 763 | 015 | 753 | 793 | 429 | lt005 | 008 | 326 | 326 | 1006 | nd | 1 | 4 | lt10 | 126 | lt4 | lt5 | lt6 | 266 | nd | 109 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 123 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 97 | lt5 | lt6 | lt2 | 46162 | lt2 | 257 | 21 | nd | 84 | 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120549 | 709110 | 7163260 | 851 | 045 | 827 | 064 | 028 | lt005 | 066 | 02 | 025 | 252 | lt005 | 211 | 1007 | 1 | lt4 | lt10 | 516 | lt4 | lt5 | 49 | 56 | lt4 | 10 | lt3 | 18 | lt2 | 9 | 17 | 18 | 135 | 5 | lt4 | 13 | lt5 | lt6 | 13 | 5 | 139 | 21 | 8 | 114 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120550 | 709190 | 7162721 | 516 | 087 | 135 | 324 | 901 | 021 | 646 | 957 | 246 | 031 | 008 | 362 | 101 | 1 | 4 | lt10 | 145 | lt4 | lt5 | lt6 | 17 | 70 | 15 | lt3 | lt5 | lt2 | lt7 | 70 | lt4 | 7 | lt4 | lt4 | 93 | lt5 | lt6 | 2 | 52157 | lt2 | 267 | 20 | 85 | 62 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120566 | 734201 | 7165328 | 733 | 003 | 1 | lt4 | 10 | 261 | lt4 | lt5 | 8 | 257 | 24 | 24 | lt3 | lt5 | 2 | 8 | 97 | 12 | lt2 | lt4 | lt4 | 376 | lt5 | lt6 | lt2 | lt2 | 962 | 5 | 59 | 61 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120593 | 707343 | 7160447 | 48 | 046 | 116 | 248 | 735 | 017 | 14 | 101 | 148 | lt005 | 005 | 464 | 1007 | lt1 | lt4 | lt10 | 35 | lt4 | lt5 | lt6 | 1617 | 39 | 11 | lt3 | lt5 | lt2 | lt7 | 611 | lt4 | lt2 | lt4 | lt4 | 91 | lt5 | lt6 | lt2 | lt2 | 220 | 13 | 72 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120630 | 722750 | 7168750 | 38 | 014 | 733 | 088 | 695 | 014 | 207 | 725 | 095 | lt005 | lt005 | 18 | 1009 | 1 | lt4 | 10 | 41 | lt4 | lt5 | lt6 | 2746 | 46 | 6 | lt3 | lt5 | lt2 | lt7 | 1110 | lt4 | lt2 | lt4 | lt4 | 32 | lt5 | lt6 | lt2 | lt2 | 137 | 6 | 56 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120688 | 739099 | 7173927 | 521 | 084 | 139 | 322 | 775 | 017 | 658 | 104 | 288 | 017 | 008 | 277 | 101 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 160 | 35 | 13 | lt3 | lt5 | lt2 | lt7 | 133 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | lt2 | lt2 | 317 | 20 | 78 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120692 | 738903 | 7174351 | 496 | 032 | 134 | 271 | 658 | 015 | 115 | 101 | 223 | 009 | lt005 | 405 | 101 | lt1 | lt4 | lt10 | 149 | lt4 | lt5 | lt6 | 941 | 57 | 12 | lt3 | lt5 | lt2 | lt7 | 334 | lt4 | lt2 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 205 | 13 | 61 | 32 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120698 | 735588 | 7172781 | 546 | 059 | 136 | 26 | 576 | 014 | 727 | 101 | 346 | 006 | 006 | 246 | 1008 | lt1 | 15 | lt10 | 71 | lt4 | lt5 | lt6 | 315 | 60 | 11 | lt3 | lt5 | lt2 | lt7 | 100 | lt4 | lt2 | lt4 | lt4 | 67 | lt5 | lt6 | lt2 | lt2 | 228 | 16 | 65 | 44 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120727 | 456 | 015 | 815 | 227 | 694 | 016 | 225 | 686 | 045 | lt005 | lt005 | 726 | 1009 | lt1 | lt4 | lt10 | 27 | lt4 | lt5 | lt6 | 2788 | 31 | 6 | lt3 | lt5 | lt2 | lt7 | 1075 | lt4 | lt2 | lt4 | lt4 | 14 | lt5 | lt6 | lt2 | lt2 | 141 | 7 | 69 | 25 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120728 | 687200 | 7128470 | 545 | 04 | 141 | 225 | 609 | 015 | 916 | 624 | 5 | lt005 | 005 | 324 | 1014 | lt1 | 23 | lt10 | 61 | lt4 | lt5 | lt6 | 479 | 103 | 7 | lt3 | lt5 | lt2 | lt7 | 202 | lt4 | lt2 | lt4 | lt4 | 68 | lt5 | lt6 | lt2 | lt2 | 213 | 14 | 70 | 36 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120729 | 686100 | 7128750 | 833 | 027 | 1 | 814 | lt10 | 298 | lt4 | lt5 | lt6 | 2024 | 80 | 4 | lt3 | lt5 | lt2 | 9 | 796 | 4 | 46 | 17 | lt4 | 46 | lt5 | lt6 | lt2 | lt2 | 115 | 15 | 50 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120730 | 686300 | 7128650 | 383 | 003 | 1 | 9 | lt10 | 73 | lt4 | lt5 | lt6 | 3998 | 203 | 5 | lt3 | lt5 | lt2 | 15 | 1785 | lt4 | lt2 | 4 | lt4 | 8 | lt5 | lt6 | lt2 | lt2 | 270 | 19 | 108 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120770 | 675368 | 7143153 | 11 | 138 | lt1 | 246 | lt10 | 458 | lt4 | lt5 | lt6 | 1351 | 50 | 7 | lt3 | lt5 | lt2 | 12 | 259 | 4 | 57 | 5 | lt4 | 114 | lt5 | 6 | lt2 | lt2 | 155 | 9 | 45 | 31 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120801 | 686900 | 7143160 | 916 | 213 | 1 | 169 | 660 | 1736 | lt4 | lt5 | 66 | 1275 | 594 | 5 | lt3 | 26 | lt2 | 13 | 101 | 24 | 41 | lt4 | lt4 | 94 | lt5 | 11 | lt2 | lt2 | 147 | 35 | 98 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120802 | 686900 | 7143160 | 146 | 009 | lt1 | 17 | lt10 | 130 | lt4 | lt5 | 12 | 3035 | 213 | 19 | lt3 | 6 | lt2 | 19 | 1488 | 4 | 12 | lt4 | lt4 | 31 | lt5 | lt6 | 2 | lt2 | 432 | 22 | 148 | 116 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120873 | 697233 | 7155938 | 518 | 133 | 142 | 374 | 907 | 02 | 572 | 106 | 23 | 044 | 016 | 117 | 1009 | lt1 | lt4 | lt10 | 204 | lt4 | lt5 | 23 | 72 | 232 | 18 | lt3 | 8 | lt2 | lt7 | 58 | lt4 | 40 | lt4 | lt4 | 134 | lt5 | lt6 | 3 | lt2 | 239 | 33 | 95 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120874 | 699393 | 7156313 | 503 | 062 | 148 | 29 | 648 | 016 | 812 | 112 | 313 | 01 | 006 | 31 | 1012 | lt1 | lt4 | lt10 | 124 | lt4 | lt5 | lt6 | 356 | 99 | 12 | lt3 | lt5 | lt2 | lt7 | 140 | lt4 | lt2 | lt4 | lt4 | 80 | lt5 | lt6 | lt2 | lt2 | 244 | 14 | 71 | 46 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120876 | 694754 | 7155096 | 506 | 091 | 141 | 358 | 748 | 017 | 751 | 109 | 142 | 026 | 009 | 371 | 1009 | lt1 | lt4 | lt10 | 125 | lt4 | lt5 | lt6 | 176 | 141 | 15 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 3 | lt4 | lt4 | 178 | lt5 | lt6 | lt2 | lt2 | 262 | 20 | 103 | 71 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120877 | 694754 | 7155096 | 509 | 085 | 142 | 399 | 735 | 018 | 709 | 105 | 209 | 034 | 008 | 34 | 1011 | lt1 | lt4 | lt10 | 103 | lt4 | lt5 | lt6 | 119 | 158 | 15 | lt3 | lt5 | lt2 | lt7 | 107 | lt4 | 4 | lt4 | lt4 | 182 | lt5 | lt6 | 2 | lt2 | 269 | 19 | 95 | 70 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120878 | 694149 | 7154736 | 488 | 082 | 143 | 385 | 717 | 018 | 765 | 128 | 174 | 008 | 008 | 33 | 1009 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 137 | 107 | 15 | lt3 | lt5 | lt2 | lt7 | 105 | lt4 | lt2 | lt4 | lt4 | 142 | lt5 | lt6 | lt2 | lt2 | 257 | 24 | 83 | 60 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120891 | 677938 | 7168840 | 4880 | 082 | 1430 | 385 | 717 | 018 | 765 | 1280 | 174 | 008 | 008 | 330 | 10077 | 1 | 4 | 10 | 86 | 4 | 5 | 6 | 137 | 107 | 15 | 5 | 2 | 7 | 105 | 4 | 2 | 4 | 4 | 142 | 2 | 2 | 257 | 24 | 83 | 60 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124203 | 685884 | 7169152 | 496 | 089 | 14 | 329 | 852 | 02 | 733 | 981 | 233 | 009 | 008 | 36 | 998 | lt1 | lt4 | lt10 | 53 | lt4 | lt5 | lt6 | 65 | 122 | 14 | lt3 | lt5 | lt2 | lt7 | 91 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | 2 | lt2 | 280 | 19 | 104 | 66 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124204 | 685884 | 7168152 | 511 | 082 | 135 | 254 | 81 | 019 | 74 | 106 | 235 | 033 | 008 | 343 | 1006 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 130 | 85 | 12 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 4 | lt4 | lt4 | 47 | lt5 | lt6 | lt2 | lt2 | 261 | 18 | 88 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124208 | 685884 | 7169152 | 497 | 075 | 143 | 293 | 769 | 017 | 784 | 115 | 181 | 03 | 008 | 35 | 1007 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 129 | 132 | 14 | lt3 | lt5 | lt2 | lt7 | 94 | lt4 | 5 | lt4 | lt4 | 84 | lt5 | lt6 | lt2 | lt2 | 255 | 17 | 87 | 54 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132787 | 630625 | 7198600 | 492 | 07 | 142 | 265 | 735 | 017 | 857 | 126 | 176 | 009 | 006 | 335 | 1008 | 1 | lt4 | lt10 | 75 | lt4 | lt5 | lt6 | 136 | 105 | 16 | lt3 | lt5 | lt2 | lt7 | 158 | 5 | lt2 | lt4 | lt4 | 126 | lt5 | lt6 | lt2 | lt2 | 247 | 17 | 70 | 52 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132788 | 630625 | 7198600 | 218 | lt001 | lt1 | lt4 | lt10 | 864 | lt4 | lt5 | lt6 | 454 | 9 | lt3 | lt3 | lt5 | lt2 | lt7 | 67 | lt4 | lt2 | lt4 | lt4 | 9 | lt5 | lt6 | 2 | lt2 | 41 | 3 | 7 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132789 | 602460 | 7168288 | 556 | 021 | 138 | 329 | 587 | 016 | 612 | 111 | 131 | lt005 | lt005 | 303 | 303 | 1005 | nd | lt1 | lt4 | lt10 | 130 | lt4 | lt5 | lt6 | 158 | nd | 76 | 8 | lt3 | lt5 | nd | lt2 | lt7 | 98 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 16 | lt2 | 12590 | lt2 | 204 | 13 | nd | 72 | 17 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132790 | 613877 | 7170789 | 527 | 035 | 138 | 239 | 605 | 016 | 83 | 113 | 189 | lt005 | lt005 | 338 | 338 | 1006 | nd | lt1 | lt4 | lt10 | 81 | lt4 | lt5 | lt6 | 503 | nd | 81 | 10 | lt5 | nd | lt2 | lt7 | 190 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 27 | lt5 | 9 | lt2 | 20983 | lt2 | 211 | 14 | nd | 65 | 24 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132791 | 621561 | 7169810 | 499 | 057 | 133 | 308 | 649 | 015 | 96 | 121 | 204 | 005 | 006 | 316 | 316 | 1007 | nd | lt1 | 4 | lt10 | 71 | lt4 | lt5 | lt6 | 633 | nd | 80 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 281 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 75 | lt5 | lt6 | lt2 | 34172 | lt2 | 233 | 16 | nd | 74 | 40 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132792 | 616685 | 7171750 | 503 | 084 | 134 | 527 | 637 | 017 | 813 | 104 | 107 | 005 | 007 | 432 | 1006 | lt1 | lt4 | lt10 | 12 | lt4 | lt5 | lt6 | 314 | 144 | 13 | lt3 | 6 | lt2 | lt7 | 204 | 5 | lt2 | lt4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 285 | 28 | 95 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132793 | 622866 | 7161836 | 4860 | 031 | 1350 | 362 | 510 | 013 | 1040 | 1090 | 231 | 001 | 003 | 321 | 9812 | 2 | 4 | 3 | 29 | 4 | 5 | 6 | 872 | 45 | 61 | 11 | 3 | 97 | 7 | 379 | 4 | 3 | 2 | 2 | 4 | 4 | 72 | 2 | 2 | 216 | 14 | 4 | 60 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132794 | 622866 | 7161786 | 4840 | 014 | 576 | 203 | 615 | 015 | 2160 | 863 | 033 | 001 | 001 | 549 | 9870 | 2 | 4 | 4 | 11 | 6 | 5 | 6 | 2460 | 71 | 22 | 5 | 3 | 2 | 7 | 1020 | 4 | 4 | 3 | 2 | 4 | 4 | 11 | 2 | 2 | 155 | 7 | 4 | 63 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133033 | 638351 | 7157551 | 4450 | 156 | 1110 | 611 | 440 | 020 | 318 | 1330 | 468 | 034 | 021 | 906 | 9864 | 01 | 05 | 5 | 323 | 07 | 01 | 296 | 190 | 36 | 84 | 05 | 126 | 01 | 11 | 75 | 19 | 11 | 11 | 51 | 02 | 1 | 07 | 135 | 22 | 07 | 276 | 241 | 05 | 73 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133034 | 638351 | 7157551 | 4710 | 013 | 836 | 237 | 696 | 014 | 1980 | 764 | 012 | 001 | 003 | 596 | 9862 | 02 | 12 | 2 | 18 | 45 | 01 | 32 | 3448 | 69 | 22 | 16 | 16 | 23 | 32 | 1048 | 11 | 5 | 9 | 17 | 18 | 42 | 19 | 52 | 15 | 01 | 133 | 58 | 84 | 72 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133035 | 638300 | 7157750 | 4740 | 013 | 668 | 349 | 512 | 014 | 2200 | 801 | 022 | 003 | 001 | 521 | 9844 | 02 | 07 | 6 | 52 | 14 | 01 | 11 | 2608 | 73 | 34 | 22 | 12 | 03 | 33 | 1295 | 15 | 10 | 9 | 22 | 06 | 29 | 1 | 12 | 16 | 02 | 116 | 72 | 58 | 61 | 447 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133038 | 632615 | 7159390 | 5060 | 048 | 1600 | 316 | 443 | 012 | 572 | 1410 | 150 | 032 | 006 | 267 | 022 | 102 | lt05 | 70 | 110 | lt05 | lt01 | 216 | 392 | 29 | 93 | 57 | 147 | 10 | 12 | 28 | 138 | 29 | lt2 | 3 | 179 | 297 | 31 | 74 | 141 | 21 | 28776 | 02 | 181 | 14 | 139 | 59 | 709 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133039 | 632600 | 7159000 | 5160 | 034 | 1550 | 281 | 555 | 014 | 644 | 1090 | 252 | 026 | 002 | 309 | 026 | lt01 | lt05 | 30 | 80 | lt05 | lt01 | 06 | 422 | 36 | 88 | 47 | lt05 | 6 | 05 | 33 | 183 | lt05 | lt2 | lt2 | 46 | 115 | 32 | 29 | 139 | lt05 | 20383 | lt01 | 216 | 148 | 77 | 66 | 338 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133043 | 632906 | 7159832 | 4970 | 073 | 1490 | 272 | 790 | 018 | 626 | 1260 | 171 | 031 | 006 | 236 | 022 | 03 | 21 | 30 | 412 | 09 | 01 | 46 | 66 | 37 | 129 | 05 | 61 | 8 | 06 | 41 | 121 | 48 | lt2 | 9 | 99 | 44 | 11 | 27 | 119 | 13 | 43764 | 02 | 268 | 203 | 33 | 88 | 470 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133046 | 633939 | 7161905 | 4980 | 051 | 1280 | 263 | 708 | 016 | 1070 | 1060 | 163 | 014 | 005 | 309 | 016 | lt01 | lt05 | lt2 | 48 | lt05 | lt01 | 18 | 678 | 43 | 85 | 47 | 53 | 8 | 04 | 05 | 327 | lt05 | lt2 | lt2 | 06 | 68 | 34 | 15 | 123 | lt05 | 30575 | lt01 | 227 | 147 | 51 | 76 | 443 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133047 | 633939 | 7161905 | 5200 | 079 | 1400 | 280 | 738 | 017 | 548 | 1080 | 227 | 039 | 007 | 264 | 022 | 118 | lt05 | lt2 | 60 | lt05 | lt01 | 36 | 116 | 36 | 74 | 56 | 48 | 12 | 04 | 44 | 81 | lt05 | lt2 | lt2 | 95 | 46 | 38 | 09 | 101 | lt05 | 47361 | lt01 | 261 | 193 | 45 | 77 | 673 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133048 | 633939 | 7161905 | 4800 | 053 | 1050 | 391 | 746 | 018 | 972 | 1360 | 100 | 034 | 004 | 390 | 015 | lt01 | lt05 | 30 | 63 | lt05 | lt01 | 37 | 200 | 55 | 192 | 55 | 10 | 11 | 02 | 19 | 156 | 36 | lt2 | 3 | 55 | 08 | 43 | lt05 | 110 | lt05 | 31774 | lt01 | 276 | 126 | 12 | 76 | 410 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133049 | 634427 | 7166123 | 4900 | 059 | 1390 | 361 | 656 | 016 | 658 | 1300 | 190 | 019 | 005 | 328 | 015 | lt01 | lt05 | 30 | 45 | lt05 | lt01 | 25 | 120 | 42 | 164 | 66 | 12 | 10 | 07 | 32 | 143 | 24 | lt2 | lt2 | 20 | 33 | 24 | lt05 | 101 | lt05 | 35371 | lt01 | 220 | 145 | 82 | 67 | 442 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133050 | 635551 | 7169572 | 4890 | 060 | 1280 | 365 | 706 | 017 | 698 | 1370 | 137 | 023 | 005 | 348 | 011 | lt01 | lt05 | 30 | 36 | lt05 | lt01 | 22 | 165 | 49 | 108 | 64 | 08 | 11 | 04 | 24 | 152 | 22 | lt2 | 4 | 49 | 06 | 33 | lt05 | 108 | lt05 | 35970 | lt01 | 233 | 149 | 18 | 68 | 415 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133051 | 635603 | 7169579 | 0 | 74 | 0 | 02 | 15 | 12 | 114 | 114 | 24 | 91 | 13 | 05 | 84 | 73 | 27 | 12 | 11 | 24 | 0 | 40 | 15 | 158 | 173 | 043 | 256 | 18 | 05 | 74 | 62 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133052 | 635259 | 7169444 | 5160 | 086 | 1360 | 411 | 719 | 016 | 569 | 1030 | 155 | 048 | 008 | 344 | 9906 | 038 | 01 | 05 | 2 | 151 | 05 | 01 | 94 | 148 | 37 | 136 | 33 | 11 | 03 | 34 | 93 | 05 | 2 | 2 | 105 | 02 | 24 | 05 | 145 | 05 | 01 | 296 | 191 | 05 | 85 | 718 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133054 | 634952 | 7169267 | 0 | 62 | 05 | 0 | 38 | 5 | 105 | 44 | 18 | 25 | 41 | 12 | 13 | 57 | 48 | 5 | 6 | 12 | 0 | 26 | 18 | 411 | 6 | 166 | 182 | 18 | 08 | 38 | 104 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133060 | 648256 | 7160919 | 0 | 23 | 0 | 02 | 19 | 6 | 89 | 129 | 18 | 10 | 5 | 12 | 88 | 62 | 27 | 3 | 0 | 92 | 0 | 38 | 21 | 251 | 111 | 037 | 318 | 25 | 08 | 85 | 76 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133063 | 648467 | 7150024 | 4400 | 018 | 889 | 410 | 531 | 015 | 2270 | 702 | 037 | 003 | 002 | 705 | 9982 | 011 | 01 | 05 | 2 | 7 | 05 | 01 | 05 | 3170 | 83 | 19 | 53 | 05 | 03 | 18 | 1370 | 15 | 9 | 13 | 09 | 04 | 23 | 05 | 135 | 05 | 01 | 123 | 76 | 27 | 72 | 139 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133064 | 647573 | 7150076 | 5150 | 032 | 1450 | 307 | 514 | 015 | 634 | 1390 | 178 | 001 | 003 | 244 | 9918 | 015 | 01 | 05 | 3 | 50 | 05 | 01 | 05 | 456 | 29 | 40 | 65 | 14 | 04 | 09 | 191 | 05 | 11 | 11 | 05 | 04 | 36 | 05 | 577 | 05 | 01 | 222 | 144 | 21 | 61 | 26 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133073 | 626850 | 7161292 | 5150 | 033 | 1440 | 273 | 573 | 014 | 748 | 1250 | 232 | 001 | 003 | 264 | 9981 | 011 | 01 | 05 | 3 | 43 | 05 | 01 | 05 | 467 | 38 | 78 | 32 | 19 | 02 | 29 | 202 | 14 | 13 | 12 | 05 | 03 | 32 | 05 | 497 | 05 | 01 | 219 | 137 | 05 | 61 | 258 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133076 | 626850 | 7161292 | 4990 | 074 | 1490 | 410 | 612 | 015 | 546 | 1320 | 148 | 006 | 007 | 297 | 9915 | 022 | 01 | 05 | 3 | 42 | 05 | 01 | 85 | 154 | 33 | 55 | 65 | 34 | 03 | 34 | 93 | 05 | 7 | 11 | 05 | 02 | 33 | 05 | 151 | 05 | 01 | 263 | 169 | 16 | 84 | 678 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133096 | 645954 | 7171243 | 4500 | 013 | 916 | 192 | 711 | 014 | 2110 | 744 | 015 | 002 | 001 | 699 | 9917 | 022 | 01 | 05 | 2 | 75 | 05 | 01 | 23 | 3100 | 93 | 69 | 6 | 146 | 06 | 14 | 1620 | 17 | 7 | 7 | 07 | 17 | 26 | 05 | 27 | 05 | 01 | 132 | 212 | 21 | 69 | 103 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133098 | 636053 | 7155351 | 4950 | 057 | 1510 | 228 | 646 | 014 | 728 | 1380 | 135 | 010 | 006 | 307 | 9971 | 015 | 01 | 05 | 6 | 174 | 05 | 01 | 08 | 487 | 31 | 81 | 47 | 58 | 05 | 37 | 165 | 05 | 12 | 16 | 15 | 02 | 26 | 05 | 112 | 35 | 02 | 220 | 135 | 05 | 64 | 429 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136749 | 667073 | 7199167 | 5080 | 072 | 1420 | 410 | 567 | 015 | 601 | 1330 | 166 | 022 | 007 | 221 | 9911 | 011 | 01 | 05 | 4 | 222 | 05 | 01 | 42 | 331 | 37 | 82 | 57 | 59 | 04 | 29 | 131 | 1 | 12 | 11 | 32 | 07 | 31 | 05 | 237 | 05 | 01 | 257 | 175 | 15 | 75 | 665 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136751 | 659000 | 7122223 | 0 | 12 | 0 | 0 | 98 | 3 | 209 | 68 | 15 | 62 | 34 | 04 | 44 | 86 | 2 | 9 | 7 | 43 | 0 | 34 | 09 | 304 | 053 | 021 | 207 | 15 | 09 | 48 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139131 | 621200 | 7215100 | 4790 | 065 | 1470 | 301 | 746 | 019 | 682 | 1290 | 254 | 004 | 006 | 319 | 9946 | 026 | 01 | 05 | 3 | 211 | 05 | 01 | 43 | 358 | 43 | 103 | 07 | 4 | 02 | 46 | 154 | 05 | 8 | 14 | 05 | 02 | 29 | 05 | 616 | 05 | 02 | 281 | 19 | 05 | 77 | 484 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139132 | 621190 | 7215090 | 0 | 14 | 0 | 01 | 11 | 0 | 66 | 18 | 46 | 59 | 40 | 05 | 95 | 11 | 14 | 0 | 0 | 108 | 0 | 51 | 21 | 242 | 87 | 124 | 389 | 7 | 24 | 51 | 134 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139133 | 666700 | 7193500 | 0 | 09 | 0 | 02 | 56 | 0 | 0 | 18 | 37 | 39 | 92 | 05 | 63 | 4 | 62 | 0 | 0 | 63 | 0 | 53 | 19 | 33 | 21 | 24 | 29 | 18 | 08 | 25 | 290 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139134 | 621755 | 7169255 | 0 | 08 | 0 | 0 | 85 | 3 | 3 | 3 | 15 | 63 | 14 | 09 | 06 | 0 | 2 | 0 | 0 | 73 | 0 | 06 | 08 | 76 | 129 | 05 | 4 | 3 | 03 | 3 | 35 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139135 | 621000 | 7169500 | 5016 | 037 | 1406 | 241 | 647 | 017 | 918 | 1126 | 248 | 006 | 003 | 15 | 5812 | 222 | 438 | 53 | 65 | 10 | 438 | 077 | 1320 | 100E-07 | 171 | 100E-07 | 500E-08 | 54 | 2 | 53 | 500E-08 | 500E-08 | 212 | 15 | 72 | 19 | 036 | 194 | 094 | 048 | 190 | 038 | 289 | 071 | 222 | 034 | 232 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139136 | 621000 | 7169500 | 5236 | 027 | 1373 | 239 | 577 | 016 | 897 | 1068 | 21 | 007 | 003 | 15 | 5265 | 210 | 491 | 53 | 162 | 10 | 491 | 086 | 1290 | 100E-07 | 196 | 100E-07 | 1 | 48 | 200E-07 | 62 | 500E-08 | 500E-08 | 189 | 13 | 63 | 13 | 036 | 161 | 078 | 041 | 160 | 039 | 259 | 068 | 214 | 038 | 221 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139137 | 620904 | 7169533 | 4737 | 108 | 1123 | 33 | 789 | 018 | 1191 | 106 | 203 | 008 | 012 | 15 | 13407 | 2170 | 1150 | 82 | 119 | 15 | 1150 | 897 | 1380 | 6 | 525 | 2 | 500E-08 | 39 | 4 | 143 | 1 | 500E-08 | 265 | 17 | 90 | 65 | 278 | 1143 | 314 | 124 | 391 | 066 | 391 | 084 | 222 | 031 | 187 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139138 | 620992 | 7169508 | 5075 | 03 | 141 | 177 | 678 | 017 | 996 | 925 | 264 | 044 | 002 | 05 | 7628 | 124 | 660 | 56 | 61 | 10 | 660 | 042 | 1310 | 100E-07 | 232 | 100E-07 | 55 | 49 | 2 | 62 | 500E-08 | 500E-08 | 194 | 12 | 65 | 14 | 019 | 104 | 062 | 031 | 135 | 030 | 225 | 055 | 166 | 026 | 175 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139139 | 620992 | 7169508 | 4747 | 018 | 1006 | 141 | 804 | 017 | 1989 | 829 | 089 | 002 | 001 | 500E-08 | 7171 | 148 | 1770 | 95 | 53 | 75 | 1770 | 089 | 1320 | 100E-07 | 835 | 100E-07 | 500E-08 | 39 | 2 | 225 | 500E-08 | 500E-08 | 139 | 8 | 60 | 7 | 019 | 098 | 063 | 028 | 124 | 028 | 206 | 051 | 157 | 026 | 160 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139140 | 620992 | 7169508 | 5201 | 117 | 1269 | 224 | 762 | 016 | 761 | 1089 | 239 | 025 | 013 | 05 | 8447 | 2455 | 212 | 52 | 161 | 15 | 212 | 982 | 1210 | 5 | 135 | 100E-07 | 45 | 42 | 4 | 228 | 1 | 500E-08 | 270 | 17 | 87 | 80 | 308 | 1270 | 330 | 120 | 387 | 061 | 364 | 074 | 200 | 028 | 161 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139141 | 620992 | 7169488 | 6179 | 081 | 147 | 284 | 594 | 006 | 496 | 012 | 007 | 32 | 01 | 1 | 74341 | 6413 | 414 | 41 | 31 | 19 | 414 | 2988 | 410 | 12 | 163 | 3 | 161 | 29 | 4 | 11 | 155 | 3 | 90 | 19 | 132 | 198 | 677 | 2282 | 433 | 094 | 430 | 059 | 295 | 058 | 166 | 026 | 170 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256h | 715830 | 7171470 | 6528 | 068 | 1179 | 412 | 511 | 004 | 551 | 013 | 005 | 24 | 012 | 1 | 44782 | 7429 | 348 | 39 | 2 | 15 | 348 | 3419 | 300 | 10 | 176 | 3 | 121 | 21 | 4 | 9 | 19 | 3 | 73 | 27 | 83 | 266 | 834 | 2926 | 592 | 121 | 584 | 082 | 451 | 089 | 249 | 038 | 231 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393s | 687539 | 7143275 | 3634 | 015 | 744 | 519 | 582 | 02 | 1191 | 1139 | 002 | 001 | 002 | 177 | 2109 | 066 | 2020 | 175 | 257 | 6 | 043 | 1440 | 00000001 | 1000 | 00000001 | 000000005 | 24 | 2 | 42 | 000000005 | 05 | 108 | 6 | 35 | 13 | 016 | 080 | 044 | 022 | 067 | 014 | 094 | 022 | 074 | 012 | 090 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601s | 668775 | 7146298 | 1248 | 005 | 339 | 812 | 262 | 026 | 1592 | 217 | 005 | 001 | 0 | 156 | 1400 | 058 | 850 | 63 | 46 | 25 | 066 | 1990 | 00000001 | 1010 | 1 | 000000005 | 10 | 2 | 66 | 000000005 | 000000005 | 87 | 11 | 22 | 3 | 024 | 085 | 052 | 025 | 083 | 021 | 145 | 034 | 111 | 017 | 131 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604s | 672238 | 7155486 | 7639 | 017 | 1136 | 256 | 551 | 022 | 087 | 002 | 002 | 01 | 001 | 457 | 15133 | 087 | 2260 | 9 | 10 | 8 | 031 | 1590 | 00000001 | 228 | 1 | 45 | 21 | 00000002 | 17 | 000000005 | 05 | 149 | 2 | 17 | 9 | 009 | 043 | 014 | 012 | 017 | 004 | 028 | 006 | 023 | 004 | 035 | 005 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643h | 675190 | 7125902 | 5583 | 097 | 1236 | 543 | 726 | 045 | 595 | 128 | 308 | 005 | 015 | 195 | 2804 | 1728 | 46 | 41 | 13 | 145 | 738 | 3010 | 2 | 63 | 1 | 2 | 58 | 2 | 38 | 000000005 | 000000005 | 278 | 24 | 111 | 58 | 201 | 930 | 276 | 073 | 275 | 049 | 297 | 064 | 202 | 031 | 236 | 038 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454s | 653363 | 7152948 | 2576 | 011 | 467 | 59 | 024 | 018 | 1282 | 1816 | 172 | 064 | 003 | 695 | 7663 | 012 | 1570 | 58 | 23 | 35 | 042 | 1370 | 00000001 | 620 | 2 | 34 | 15 | 00000002 | 385 | 000000005 | 000000005 | 76 | 5 | 30 | 4 | 013 | 027 | 019 | 018 | 037 | 010 | 069 | 017 | 060 | 009 | 070 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477s | 645436 | 7177439 | 2009 | 0 | 084 | 152 | 0 | 038 | 1639 | 2363 | 022 | 04 | 003 | 6 | 6838 | 126 | 31 | 10 | 19 | 000000005 | 107 | 2940 | 00000001 | 93 | 1 | 75 | 00000001 | 00000002 | 103 | 000000005 | 000000005 | 9 | 10 | 4 | 00000001 | 034 | 113 | 036 | 118 | 051 | 012 | 084 | 027 | 105 | 017 | 142 | 020 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485h | 655767 | 7129994 | 5901 | 078 | 1092 | 14 | 102 | 013 | 1024 | 016 | 003 | 0 | 008 | 65 | 744 | 774 | 86 | 47 | 39 | 125 | 276 | 965 | 2 | 136 | 00000001 | 000000005 | 62 | 2 | 15 | 000000005 | 000000005 | 304 | 15 | 85 | 45 | 099 | 490 | 138 | 035 | 148 | 026 | 164 | 036 | 114 | 018 | 143 | 023 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487h | 655561 | 7129043 | 2488 | 011 | 535 | 29 | 312 | 04 | 1401 | 2084 | 003 | 004 | 005 | 110 | 4392 | 265 | 1410 | 69 | 15 | 5 | 175 | 3200 | 00000001 | 685 | 1 | 15 | 19 | 2 | 140 | 000000005 | 05 | 99 | 5 | 42 | 14 | 048 | 147 | 045 | 021 | 054 | 010 | 063 | 013 | 045 | 007 | 052 | 008 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493h | 655992 | 7125530 | 5148 | 073 | 1516 | 172 | 1092 | 013 | 932 | 024 | 26 | 03 | 009 | 15 | 10919 | 1023 | 98 | 58 | 72 | 155 | 430 | 935 | 2 | 98 | 00000001 | 45 | 69 | 2 | 75 | 000000005 | 1 | 357 | 18 | 113 | 42 | 127 | 601 | 174 | 057 | 201 | 036 | 234 | 054 | 176 | 028 | 217 | 036 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501h | 708508 | 7162137 | 4773 | 039 | 1372 | 423 | 456 | 016 | 666 | 527 | 438 | 098 | 006 | 1 | 120917 | 449 | 56 | 49 | 35 | 13 | 1277 | 1170 | 1 | 192 | 2 | 31 | 67 | 00000002 | 51 | 000000005 | 000000005 | 284 | 29 | 114 | 20 | 154 | 703 | 155 | 116 | 228 | 033 | 198 | 048 | 147 | 020 | 136 | 024 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116518s | 685232 | 7155526 | 3765 | 02 | 609 | 573 | 0 | 152 | 597 | 1736 | 007 | 218 | 005 | 100 | 218361 | 3411 | 55 | 39 | 15 | 7 | 1396 | 11070 | 4 | 70 | 5 | 65 | 8 | 00000002 | 77 | 55 | 1 | 60 | 12 | 38 | 38 | 321 | 1160 | 235 | 171 | 234 | 031 | 155 | 028 | 088 | 013 | 096 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120303 | 655250 | 7126000 | 2302 | 011 | 404 | 31 | 071 | 059 | 074 | 3572 | 004 | 141 | 004 | 53 | 20581 | 1117 | 285 | 7 | 4 | 45 | 720 | 4740 | 1 | 51 | 12 | 435 | 00000001 | 2 | 96 | 25 | 000000005 | 36 | 9 | 21 | 17 | 141 | 504 | 105 | 042 | 126 | 021 | 127 | 030 | 097 | 015 | 109 | 019 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339A | 669650 | 7146425 | 9409 | 001 | 03 | 425 | 065 | 002 | 003 | 005 | 0 | 006 | 003 | 155 | 1042 | 267 | 29 | 6 | 65 | 05 | 117 | 110 | 00000001 | 15 | 10 | 85 | 1 | 00000002 | 5 | 05 | 05 | 55 | 1 | 10 | 4 | 023 | 092 | 016 | 004 | 021 | 003 | 014 | 003 | 009 | 001 | 012 | 002 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339B | 669650 | 7146425 | 9632 | 0 | 002 | 319 | 053 | 001 | 0 | 001 | 0 | 0 | 001 | 5 | 2442 | 083 | 6 | 3 | 9 | 000000005 | 039 | 40 | 00000001 | 3 | 1 | 000000005 | 00000001 | 00000002 | 1 | 000000005 | 000000005 | 10 | 00000001 | 3 | 2 | 008 | 030 | 006 | 004 | 009 | 001 | 005 | 002 | 006 | 001 | 008 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369s | 665175 | 7156150 | 6131 | 098 | 1297 | 175 | 906 | 025 | 457 | 058 | 144 | 134 | 007 | 285 | 27950 | 3230 | 284 | 43 | 121 | 15 | 1406 | 1690 | 6 | 128 | 13 | 54 | 41 | 4 | 305 | 65 | 1 | 178 | 16 | 119 | 106 | 355 | 1340 | 286 | 087 | 269 | 039 | 202 | 036 | 119 | 017 | 130 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373s | 675250 | 7167875 | 5541 | 088 | 1306 | 795 | 346 | 014 | 199 | 144 | 005 | 004 | 009 | 1 | 7754 | 1109 | 26 | 29 | 74 | 225 | 521 | 1040 | 2 | 41 | 3 | 05 | 48 | 4 | 67 | 000000005 | 000000005 | 494 | 25 | 50 | 55 | 161 | 716 | 213 | 067 | 256 | 050 | 325 | 074 | 237 | 035 | 267 | 041 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432s | 673950 | 7171700 | 5469 | 078 | 1137 | 81 | 399 | 02 | 311 | 1468 | 016 | 005 | 006 | 2 | 11068 | 1433 | 62 | 44 | 22 | 20 | 634 | 1490 | 1 | 88 | 8 | 15 | 55 | 4 | 495 | 1 | 000000005 | 346 | 24 | 49 | 49 | 202 | 897 | 283 | 137 | 343 | 070 | 452 | 104 | 321 | 048 | 354 | 051 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137A | not available | 6241 | 067 | 991 | 186 | 893 | 019 | 924 | 011 | 0 | 005 | 01 | 15 | 2345 | 6927 | 595 | 43 | 123 | 12 | 3489 | 1470 | 10 | 235 | 4 | 25 | 21 | 4 | 55 | 175 | 2 | 77 | 16 | 112 | 288 | 734 | 2545 | 453 | 074 | 448 | 050 | 239 | 041 | 129 | 019 | 143 | 023 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137B | not available | 6118 | 074 | 1029 | 19 | 912 | 019 | 96 | 011 | 0 | 009 | 01 | 1 | 3042 | 6659 | 780 | 45 | 121 | 12 | 2999 | 1430 | 10 | 218 | 6 | 4 | 22 | 4 | 4 | 175 | 25 | 80 | 27 | 116 | 312 | 704 | 2493 | 499 | 095 | 542 | 075 | 415 | 083 | 249 | 037 | 262 | 039 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82144 | not available | 6901 | 044 | 1124 | 143 | 288 | 021 | 188 | 365 | 27 | 14 | 013 | 15 | 38750 | 6263 | 117 | 22 | 22 | 12 | 3381 | 1690 | 8 | 48 | 37 | 67 | 11 | 2 | 107 | 175 | 25 | 46 | 19 | 61 | 199 | 679 | 2348 | 436 | 093 | 441 | 056 | 304 | 052 | 157 | 022 | 154 | 022 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82148 | not available | 6314 | 07 | 124 | 312 | 581 | 017 | 717 | 01 | 005 | 197 | 01 | 1 | 41557 | 6431 | 505 | 53 | 22 | 15 | 3168 | 1310 | 10 | 211 | 4 | 99 | 23 | 4 | 8 | 165 | 25 | 72 | 18 | 121 | 227 | 689 | 2407 | 462 | 095 | 440 | 055 | 281 | 050 | 159 | 022 | 168 | 025 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82150 | not available | 9469 | 001 | 012 | 45 | 062 | 001 | 001 | 001 | 0 | 0 | 001 | 1150 | 13761 | 225 | 10 | 2 | 7 | 000000005 | 310 | 40 | 00000001 | 11 | 00000001 | 000000005 | 00000001 | 6 | 000000005 | 000000005 | 3800 | 00000001 | 700 | 300 | 044 | 122 | 021 | 012 | 021 | 002 | 013 | 002 | 004 | 000 | 005 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82153 | not available | 41767 | 296 | 256 | 047 | 214 | 049 | 031 | 072 | 013 | 090 | 023 | 077 | 010 | 072 | 010 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82155 | not available | 4977 | 081 | 1429 | 329 | 833 | 02 | 718 | 945 | 255 | 018 | 007 | 2 | 10432 | 1154 | 175 | 65 | 117 | 135 | 175 | 395 | 1540 | 2 | 135 | 100E-07 | 3 | 57 | 4 | 75 | 500E-08 | 500E-08 | 290 | 18 | 104 | 45 | 174 | 807 | 287 | 119 | 400 | 083 | 496 | 117 | 328 | 056 | 311 | 053 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82158 | not available | 5076 | 077 | 1356 | 336 | 794 | 019 | 714 | 996 | 197 | 035 | 006 | 15 | 16705 | 1081 | 163 | 55 | 128 | 135 | 163 | 373 | 1490 | 1 | 123 | 100E-07 | 55 | 54 | 2 | 166 | 500E-08 | 500E-08 | 268 | 17 | 98 | 43 | 159 | 772 | 261 | 108 | 365 | 070 | 470 | 107 | 304 | 046 | 279 | 042 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82160 | not available | 4799 | 033 | 127 | 192 | 57 | 017 | 1261 | 1352 | 09 | 004 | 002 | 115 | 5413 | 491 | 1360 | 52 | 50 | 105 | 1360 | 183 | 1370 | 100E-07 | 269 | 100E-07 | 05 | 46 | 4 | 87 | 500E-08 | 500E-08 | 159 | 8 | 50 | 18 | 074 | 333 | 108 | 052 | 167 | 030 | 198 | 045 | 131 | 019 | 116 | 016 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82179 | not available | 5338 | 053 | 1381 | 255 | 679 | 016 | 722 | 774 | 466 | 004 | 006 | 500E-08 | 3625 | 1347 | 326 | 50 | 48 | 115 | 326 | 523 | 1290 | 2 | 137 | 100E-07 | 500E-08 | 53 | 2 | 103 | 1 | 1 | 239 | 16 | 74 | 40 | 168 | 721 | 230 | 080 | 334 | 068 | 459 | 107 | 321 | 049 | 296 | 044 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82180 | not available | 462 | 02 | 998 | 154 | 752 | 017 | 1869 | 845 | 1 | 003 | 002 | 500E-08 | 749 | 081 | 2240 | 93 | 46 | 8 | 2240 | 029 | 1320 | 100E-07 | 795 | 100E-07 | 500E-08 | 40 | 200E-07 | 365 | 500E-08 | 500E-08 | 148 | 10 | 56 | 8 | 015 | 081 | 051 | 034 | 110 | 026 | 192 | 050 | 157 | 026 | 167 | 028 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82224 | not available | 5042 | 029 | 1394 | 187 | 675 | 015 | 976 | 1106 | 328 | 005 | 002 | 500E-08 | 1646 | 119 | 640 | 58 | 44 | 105 | 640 | 042 | 1140 | 100E-07 | 159 | 100E-07 | 500E-08 | 54 | 200E-07 | 109 | 500E-08 | 500E-08 | 204 | 12 | 41 | 14 | 022 | 124 | 075 | 041 | 160 | 036 | 265 | 063 | 195 | 031 | 206 | 032 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82225 | not available | 4701 | 022 | 1065 | 127 | 739 | 015 | 1732 | 727 | 233 | 002 | 001 | 500E-08 | 2735 | 106 | 1730 | 84 | 32 | 75 | 1730 | 062 | 1180 | 100E-07 | 690 | 100E-07 | 500E-08 | 43 | 2 | 415 | 500E-08 | 500E-08 | 159 | 11 | 58 | 9 | 023 | 128 | 063 | 031 | 125 | 028 | 204 | 050 | 161 | 026 | 162 | 025 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82226 | not available | 4256 | 014 | 689 | 357 | 494 | 011 | 2593 | 578 | 016 | 003 | 001 | 75 | 3377 | 038 | 2280 | 102 | 8 | 55 | 2280 | 015 | 835 | 100E-07 | 1380 | 100E-07 | 1 | 31 | 200E-07 | 205 | 500E-08 | 500E-08 | 104 | 5 | 46 | 6 | 008 | 042 | 027 | 010 | 058 | 013 | 097 | 025 | 075 | 012 | 078 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82228 | not available | 4399 | 016 | 796 | 185 | 65 | 014 | 246 | 647 | 017 | 001 | 001 | 500E-08 | 9402 | 076 | 2890 | 102 | 10 | 55 | 2890 | 052 | 1050 | 100E-07 | 1130 | 100E-07 | 500E-08 | 35 | 200E-07 | 65 | 500E-08 | 500E-08 | 131 | 6 | 41 | 7 | 017 | 072 | 032 | 010 | 065 | 014 | 106 | 027 | 084 | 013 | 082 | 013 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82229 | not available | 4897 | 024 | 1196 | 106 | 807 | 015 | 1448 | 71 | 298 | 003 | 002 | 500E-08 | 11033 | 081 | 1260 | 77 | 45 | 9 | 1260 | 024 | 1160 | 100E-07 | 459 | 100E-07 | 500E-08 | 46 | 200E-07 | 138 | 500E-08 | 500E-08 | 172 | 11 | 59 | 11 | 016 | 093 | 052 | 028 | 119 | 027 | 203 | 050 | 157 | 026 | 168 | 027 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82231 | not available | 509 | 027 | 1399 | 178 | 674 | 014 | 87 | 1152 | 329 | 005 | 002 | 500E-08 | 1186 | 092 | 510 | 52 | 58 | 10 | 510 | 038 | 1100 | 100E-07 | 136 | 100E-07 | 500E-08 | 57 | 2 | 144 | 500E-08 | 500E-08 | 202 | 13 | 41 | 12 | 018 | 101 | 057 | 030 | 135 | 030 | 220 | 058 | 177 | 029 | 191 | 029 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82234 | not available | 4847 | 087 | 1468 | 1174 | 022 | 874 | 1394 | 099 | 027 | 008 | 332 | 83 | 3 | 225 | 21 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82236 | not available | 5135 | 087 | 1461 | 1117 | 02 | 757 | 1032 | 274 | 109 | 008 | 228 | 70 | 15 | 329 | 19 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
135482 | Trillbar Complex | 5137 | 037 | 1481 | 232 | 561 | 016 | 869 | 1068 | 306 | 006 | 003 | 014 | 260 | 10014 | 39 | 2 | 593 | 59 | 61 | 00 | 08 | 08 | 1 | 124 | 1 | 1 | 51 | 00 | 08 | 235 | 17 | 61 | 20 | 0 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143538 | Trillbar Complex | 4961 | 141 | 1391 | 561 | 717 | 022 | 656 | 1136 | 204 | 022 | 011 | 014 | 163 | 10036 | 322 | 15 | 82 | 172 | 91 | 12 | 26 | 26 | 9 | 98 | 4 | 4 | 48 | 12 | 14 | 362 | 24 | 91 | 86 | 2 | 12 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143539 | Trillbar Complex | 4974 | 086 | 1196 | 128 | 734 | 016 | 1072 | 1395 | 237 | 009 | 006 | 013 | 150 | 10047 | 77 | 10 | 298 | 80 | 47 | 07 | 14 | 14 | 4 | 240 | 2 | 1 | 59 | 07 | 06 | 322 | 19 | 47 | 46 | 2 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
144310 | Trillbar Complex | 4711 | 115 | 1288 | 182 | 901 | 018 | 784 | 1161 | 250 | 008 | 012 | 013 | 240 | 10027 | 53 | 13 | 394 | 116 | 90 | 13 | 13 | 13 | 7 | 156 | 6 | 1 | 37 | 13 | 14 | 380 | 23 | 90 | 78 | 0 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
MINISTER FOR MINESThe Hon Norman Moore MLC
DIRECTOR GENERALL C Ranford
DIRECTOR GEOLOGICAL SURVEY OF WESTERN AUSTRALIADavid Blight
Copy editor D P Reddy
REFERENCEThe recommended reference for this publication isPIRAJNO F OCCHIPINTI S A and SWAGER C P 2000 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury
Basins Western Australia Western Australia Geological Survey Report 59 52p
National Library of AustraliaCataloguing-in-publication entry
Pirajno Franco 1939ndashGeology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
BibliographyISBN 0 7309 6653 4
1 Geology Structural mdash Western Australia mdash Bryah Basin2 Geology Structural mdash Western Australia mdash Padbury Basin3 Mines and mineral resources mdash Western Australia mdash Bryah Basin4 Mines and mineral resources mdash Western Australia mdash Padbury Basin5 Bryah Region (WA)6 Padbury Region (WA)I Swager C PII Occhipinti S A (Sandra Anne)III Geological Survey of Western AustraliaIV Title (Series Report (Geological Survey of Western Australia) 59)
5531099413
ISSN 0508ndash4741
Grid references in this publication refer to the Australian Geodetic Datum (AGD84)
Printed by Optima Press Perth Western Australia
Copies available fromInformation CentreDepartment of Minerals and Energy100 Plain StreetEAST PERTH WESTERN AUSTRALIA 6004Telephone (08) 9222 3459 Facsimile (08) 9222 3444wwwdmewagovau
Cover photographFerruginous shale of the Millidie Creek Formation with a well-developed pencil cleavage 25 km northwest of Fraser Well(BRYAH AMG 651660)
iii
Contents
Abstract 1Introduction 1Regional tectonic setting 3Geology stratigraphy and geochronology 4
Peak Hill Schist and Marymia Inlier 5Bryah Group 6
Karalundi Formation 6Narracoota Formation 7
Peridotitic and high-Mg basalt association 7Intrusive rocks and layered intrusions 7Mafic and ultramafic schist 8Metabasaltic hyaloclastite 9Felsic schist 9Volcaniclastic rocks 10Carbonated and silicified metavolcanic rocks 11Jasperoidal chert 11Geochemistry of the Narracoota Formation 11
Ravelstone Formation 16Horseshoe Formation 16
Padbury Group 17Labouchere Formation 18Wilthorpe Formation 19
Beatty Park and Heines Members 19Robinson Range Formation 20Millidie Creek Formation 20Unassigned units of the Padbury Group 21
Structure 21D1 structures 23D2 structures 23D3 structures and their relationship to D2 structures 25D4 structures 25
Metamorphism 25Structural synthesis 27Mineralization 32
Gold deposits 33Peak Hill Jubilee and Mount Pleasant deposits 39Harmony deposit 41Labouchere Nathans and Fortnum deposits 41Wembley deposit 42Wilgeena deposit 43Durack St Crispin and Heines Find prospects 43Ruby Well group 43Mikhaburra deposit 43Wilthorpe deposit 43Cashman deposit 44
Volcanogenic copperndashgold deposits 44Supergene manganese deposits 44Iron ore 45Talc 45Discussion 45
Tectonic model and conclusions 46Acknowledgements 48References 49
Appendix
Gazetteer of localities 52
Plate
Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
iv
Figures
1 Stratigraphy of the former lsquoGlengarry Basinrsquo 22 Simplified geology of the Bryah Padbury and Yerrida Basins 43 Rotated orthoclase porphyroblast Peak Hill Schist 54 Partially recrystallized mylonite Peak Hill Schist 55 Peak Hill Schist mylonite from the Hangingwall Sequence 56 Outcrop of quartz mylonite Peak Hill Schist 67 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric 68 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt) 89 Basaltic hyaloclastite Narracoota Formation 9
10 Mafic volcaniclastic rock Narracoota Formation 1011 Volcanic breccia intersected in diamond drillhole BD1 1012 Total alkali versus silica diagram for rocks the Narracoota Formation 1313 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the
Narracoota Formation 1414 Geochemical characteristics of the Narracoota Formation rocks 1415 Geochemical discriminant plots for Narracoota Formation 1516 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation 1617 Schematic stratigraphy of the Horseshoe Formation 1718 Major regional structures in the Bryah and Padbury Groups 2219 Simplified geological map of the Bryah and Padbury Groups 2420 Selected hypothetical cross sections through the Bryah and Padbury Groups 2721 Model of the structural development of the BryahndashPadbury Group succession 2922 New model of the structural development of the BryahndashPadbury Group succession 3123 New model for the structural development of the BryahndashPadbury Group succession
and the Peak Hill Schist 3224 Schematic north-northwest to south-southeast cross section from the Bangemall Basin
into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins 3325 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins 3626 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet 3827 Albite porphyroblasts in mylonitic schist at Mount Pleasant 3928 The Mine Sequence schist 4029 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit 4030 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and
Marker quartzite unit 4031 Diagrammatic cross section of the Harmony ore zones 4132 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and
deformed Despair Granite 4433 Sketch illustrating a conceptual model for the origin of precious and base metal
deposits in the BryahndashPadbury and Yerrida Basins 4534 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and
Padbury Basins within the context of the Capricorn Orogen 46
Tables
1 Stratigraphy of the Bryah and Padbury Groups 32 Representative chemical analyses of the Narracoota Formation 123 Magnesium numbers for the Narracoota and Killara Formations 134 Selected geochemical parameters for the Narracoota Formation 135 Sequence of deformation events in the Bryah and Padbury Basins 236 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic
minerals of the Bryah Group and deformation fabrics 287 Gold production and remaining resources in the Bryah and Padbury Groups 348 Mineral production and remaining resources in the Bryah and Padbury Groups 359 Mineral deposits and occurrences in the Bryah and Padbury Basins 36
Digital dataset (in pocket)
Whole-rock geochemical analyses of Narracoota Formation rocks (narracootacsv)
1
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Geology and mineralization of thePalaeoproterozoic Bryah and Padbury
Basins Western Australia
by
F Pirajno S A Occhipinti and C P Swager
AbstractThe Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collision zonebetween the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains a succession of maficand ultramafic rocks of mid-oceanic ridge basalt to oceanic plateau affinity overlain by clastic andchemical sedimentary rocks The Bryah Basin was formed during back-arc sea-floor spreading andrifting on the northern margin of the Yilgarn Craton The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of the Bryah Basin as a forelandstructure resulting from either the c 1800 Ma oblique collision of the Pilbara and Yilgarn Cratons(Capricorn Orogeny) or the c 2000 Ma collision of the Glenburgh terrane and the Yilgarn Craton(Glenburgh Orogeny)
Important mineral deposits are contained in both basins and include mesothermal orogenic goldcopperndashgold volcanogenic massive sulfides manganese and iron ore The origin of the goldmineralization is related to metamorphism and deformation linked to the Capricorn Orogeny at c 18 GaThe formation of other deposits is related to pre-orogenic syngenetic processes
KEYWORDS Bryah Basin Padbury Basin Palaeoproterozoic stratigraphy geochemistry maficrocks ultramafic rocks mineralization mesothermal deposits gold
IntroductionIn early 1994 the Geological Survey of Western Australia(GSWA) commenced fieldwork to reassess the geologyand mineralization of the Palaeoproterozoic GlengarryBasin as part of a program of new mapping initiativesThe Glengarry Basin as defined by Gee and Grey (1993)constitutes the western part of the greater Palaeo-proterozoic Nabberu Province which in the east includesthe Earaheedy Basin (Bunting et al 1977 Hall andGoode 1978 Gee 1990)
The new mapping initiative resulted in the reappraisalof the geology tectonic evolution and mineralizationof the Glengarry Basin which is now recognized toconsist of three main geotectonic units the BryahPadbury and Yerrida Basins As a result the volcano-sedimentary rocks of the former lsquoGlengarry Grouprsquo arenow divided into the Bryah and Yerrida Groups (Fig 1 andTable 1) characterized not only by different lithologiesbut also by different regional structures metamorphismand mineral deposit types Some formations previouslyassigned to the lsquoGlengarry Grouprsquo have been reassigned
to the Padbury Group (Martin 1992) In additionthere is evidence to suggest that the economicallyimportant lsquoPeak Hill Metamorphic Suitersquo previouslyconsidered to be part of the lsquoGlengarry Grouprsquo (Gee1987) constitutes a separate unit the Peak Hill Schistderived from a protolith of probable Archaean ageConsequently the previous nomenclature (lsquoGlengarryGrouprsquo and lsquoGlengarry Basinrsquo) is no longer used Detailsof the old and new stratigraphy are presented in Figure 1and Table 1 and discussed in later sections The revisedstratigraphy of the former lsquoGlengarry Basinrsquo is presentedin Occhipinti et al (1997) Details of the stratigraphy andstructure of the lower Padbury Group are presented inMartin (1998)
The Bryah and Padbury Basins lie within the ROBINSON
RANGE and PEAK HILL 1250 000 sheets (MacLeod 1970Elias and Williams 1980 Gee 1987) and the north-western and northeastern corners of the BELELE andGLENGARRY 1250 000 sheets (Elias 1982 Elias et al
Capitalized names refer to standard 1100 000 map sheets unless otherwisespecified
2
Pirajno et al
1982) The Bryah and Padbury Groups (Fig 2) make upthe western part of the former lsquoGlengarry Basinrsquo andare now interpreted to have developed in rift and forelandbasins respectively (Martin 1994 Pirajno 1996 Pirajnoet al 1996 Pirajno et al 1998b) The Yerrida Group(Fig 2) makes up the eastern part of the former lsquoGlengarryBasinrsquo and includes two subgroups the Windplainand Mooloogool Subgroups (Fig 2 Table 1) whichdeveloped in sag and rift basins respectively (Pirajno et al1995ab 1996) The geology and mineralization ofthe Yerrida Basin are described in a separate Report(Pirajno and Adamides 2000) The Bryah Group isin faulted contact with the Yarlarweelor gneiss complexthe Marymia Inlier of the Archaean Yilgarn Cratonand the Palaeoproterozoic Yerrida Group The contactbetween the Bryah and the Yerrida Groups is along anortheasterly trending high-angle reverse fault (the GoodinFault)
Based on structural and metamorphic criteria the areaoccupied by the Bryah and Padbury Groups and thePeak Hill Schist can be regarded as a single domainIn this Report where appropriate this domain is referred
to as the BryahndashPadbury Basin The geology newstratigraphy geochronological constraints structureand metamorphism of the Bryah and Padbury Groups arediscussed The geochemistry of the volcanic componentof the Bryah Group and mineral deposits of the Bryahand Padbury Basins are also summarized A tectonicoverview and proposed model for the geodynamicevolution of the Bryah and Padbury Basins withinthe framework of the Capricorn Orogen conclude thereport
Work in the BryahndashPadbury area involved 125 000-scale mapping to produce 1100 000-scale geologicalmaps Geological mapping was carried out using125 000-scale colour aerial photography (availablefrom the Western Australian Department of LandAdministration) aeromagnetic images (400 m line-spacedcollected by GSWA in 1994) and Landsat TM imagesResults of geological mapping were integrated withpetrographic geochemical and geochronology studiesDuring this work a total of 1450 rock samples werecollected of which 776 were thin-sectioned and 136geochemically analysed In addition logging of diamond
Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
Gee (1987)P
AD
BU
RY
BA
SIN
GR
OU
PG
LEN
GA
RR
Y B
AS
ING
RO
UP
Millidie Creek Formation
Robinson Range Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Narracoota Volcanics
Karalundi Formation
Doolgunna Formation
Johnson Cairn Shale
Thaduna Greywacke
Juderina Formation
Maraloou Formation
Crispin Conglomerate
Finlayson Sandstone
Peak Hill Metamorphics
GLE
NG
AR
RY
BA
SIN
GR
OU
P
Maraloou Formation
Thaduna Greywacke
Narracoota Volcanics
Doolgunna Formation
Johnson Cairn Shale
Juderina Formation(Finlayson SandstoneMember)
YE
RR
IDA
BA
SIN
GR
OU
P
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Peak Hill Schist
BR
YA
H B
AS
ING
RO
UP
PA
DB
UR
Y B
AS
ING
RO
UP
TE
CT
ON
IC C
ON
TA
CT
Millidie Creek Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Karalundi Formation
Ravelstone Formation
Narracoota FormationMaraloou Formation
Killarra Formation(Bartle Member)
Doolgunna Formation
Thaduna Formation
Juderina Formation
170100
Gee and Grey (1993) Occhipinti et al (1997) Pirajno et al (1998b this study)
Robinson RangeFormation
Unconformity
Unconformity
Johnson CairnFormation
NOTE New or redefined units (Occhipinti et al 1997)
(Finlayson and BubbleWell Members)
ARCHAEAN BASEMENT
FMP409a
3
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
drillcore (1100 m) and several visits to prospects andoperating mines considerably enhanced our knowledge ofthe geology of the area Most of the mapped areas werealso included in a regional regolith geochemical samplingprogram covering the PEAK HILL ROBINSON RANGE andGLENGARRY 1250 000 sheets (Subramanya et al 1995Bradley et al 1997 Crawford et al 1996)
Interim accounts of the structural and stratigraphicrelations of the BryahndashPadbury and Yerrida Basins havebeen reported by Pirajno et al (1995ab 1996) andOcchipinti et al (1997) Pirajno (1996) and Pirajno et al(1995a 1998b) discussed possible models for the tectonicevolution of the BryahndashPadbury and Yerrida Basins Thestructure and metamorphism of the BryahndashPadbury Basinhave been described by Occhipinti et al (1998abc)whereas details of mineral potential production andore deposit geology can be found in Pirajno andOcchipinti (1995) and Pirajno and Preston (1998)Published 1100 000 geological maps and accompanyingExplanatory Notes that wholly or partly cover the BryahndashPadbury Basin comprise BRYAH (Pirajno and Occhipinti1998) GLENGARRY (Pirajno et al 1998a) MILGUN (Swagerand Myers 1999) PADBURY (Occhipinti et al 1998a)DOOLGUNNA (Adamides 1998) and MARYMIA (Bagas1998) The southern portion of the JAMINDI 1100 000 mapsheet containing rocks of the Bryah Group was alsomapped The layout of these map sheets in relation to theBryahndashPadbury Basin and adjacent tectonic units is shownin Figure 2 The geology of the Bryah and Padbury Basinsis presented in Plate 1
Regional tectonic settingThe Bryah and Padbury Basins are situated along thenorthern margin of the Archaean Yilgarn Craton and arepart of the Capricorn Orogen (Fig 2 inset of Plate 1)The Capricorn Orogen also includes the Ashburton Basin
and the Gascoyne Complex and can be traced for morethan 1000 km with northwesterly to westerly trendsforming a broad belt of deformed low-grade volcano-sedimentary high-grade metamorphic and granitoidrocks
The Capricorn Orogeny resulted from the collisionbetween the Pilbara and Yilgarn Cratons at c 1800 Maand involved the closure of an intervening oceanformation of a back-arc basin and the possible accretionof microcontinental fragments (Myers 1993 Myers et al1996 Tyler et al 1998) Prior to the Capricorn Orogenythe c 2000 Ma Glenburgh Orogeny (Occhipinti et al1999) resulted in the accretion of the Glenburgh terraneonto the Yilgarn Craton The convergence between thePilbara and Yilgarn Cratons was essentially oblique andresulted in the development of easterly trending strike-slipmovements which included regional sinistral faults TheCapricorn Orogeny also affected other tectonic units suchas the Archaean Narryer Terrane Marymia Inlier SylvaniaInlier and parts of the Hamersley Basin (Tyler andThorne 1990 Myers et al 1996 Tyler et al 1998)
The Palaeoproterozoic volcano-sedimentary andsedimentary successions of the Bryah and Padbury Basinsare unconformable on the northern margin of the YilgarnCraton whereas to the north they are either unconform-ably overlain by or in faulted contact with rocksof the Bangemall Basin and the Archaean graniticrocks of the Marymia Inlier The Marymia Inlier iseconomically important because it hosts a number of golddeposits including the Peak Hill deposit (AMG 672190E7163150N) on the southwestern tip of the inlier (seeMineralization)
Localities are specified by the Australian Map Grid (AMG) system AMGcoordinates (eastings and northings) of localities discussed in the text arelisted in Appendix 1
Table 1 Stratigraphy of the Bryah and Padbury Groups
Group Age Formation Rock type(Ma)
Padbury Group Millidie Creek sericitic siltstone chloritic siltstone banded iron-formation(peripheral foreland basin) dolomitic arenite
Robinson Range ferruginous shale banded iron-formation
ltc 2000 Wilthorpe quartz-pebble conglomerate(Beatty Park and (siltstonendashwacke and polymictic conglomerate respectively)Heines Members)
Labouchere turbidite sequence (quartz wacke siltstone)
unconformable contact mdash tectonized in many places
Bryah Group (rift basin) Horseshoe banded iron-formation wacke shale
ltc 2000 Ravelstone quartzndashlithic wacke
Narracoota maficndashultramafic volcanic rocks and intercalated sedimentary rocks
Karalundi conglomerate quartz wacke
faulted contact
Yerrida Group (sag and rift basin) c 2174
SOURCE Modified after Pirajno et al (1996)
4
Pirajno et al
Geology stratigraphy andgeochronology
The BryahndashPadbury Basin contains the Bryah andPadbury Groups and the Peak Hill Schist The stratigraphyfor the Bryah and Padbury Groups is summarized in
Figure 1 and Table 1 where a comparison with previousGSWA work is also provided The Peak Hill Schist is aseparate tectono-stratigraphic unit that is discussed herewith the Marymia Inlier as basement to the Bryah GroupDetailed descriptions of the various formations and theircontact relationships are presented in Occhipinti et al(1997) Martin (1998) Adamides (1998) Pirajno and
Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins showing 1100 000 map sheet boundariesInset shows the position of the basins in relation to the Capricorn Orogen
MARYMIAINLIER
GOODININLIER
Goodin
Fault
Fault
Killara
Narracoota
30 km
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
FMP375
117deg
30
118deg
30
26deg00
25deg00
Murchison
FaultMorris
Earaheedy Group
Padbury Group
Yerrida Group
Archaean granitendashgreenstonebasement
Bangemall Group
Bryah Group
Proterozoic granites
Fault
Moorarie Padbury
MilgunMarquis
FaultCooinbar
NarryerTerrane
Murchison
Terrane
Kerba Fault
119deg
30
Gabanintha Yanganoo
MooloogoolGlengarry
Bryah Doolgunna
Jamindi Three Rivers
010300
BRYAH-PADBURY
BASINS
PROTEROZOIC
5
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Occhipinti (1998) Pirajno et al (1998b) Occhipinti et al(1998c) and Swager and Myers (1999)
In this section the geology field relations stratigraphyand geochronological constraints of the Peak Hill SchistMarymia Inlier and the formations that make up the Bryahand Padbury Groups are discussed
Peak Hill Schist and MarymiaInlierThe Peak Hill Schist (formerly called the lsquoPeak HillMetamorphic Suitersquo Gee 1987) is exposed in the lsquoPeakHill Domersquo or anticline and constitutes a tectonic unitrepresenting the southwestern tip of the Marymia Inlier(Fig 2 Thornett 1995) The Peak Hill Schist iscontinuous with the Marymia Inlier and Thornett (1995)suggested that the lsquoPeak Hill Domersquo represents thedeformed southwestern end of the Marymia Inlier Fieldobservations and petrographic and aeromagnetic datasupport this view The boundary between the Peak HillSchist and granitic rocks of the Marymia Inlier is a zoneof intense deformation and metamorphism characterizedby tectonic interleaving and duplexing Towards thenortheast the intensity of the Capricorn Orogenydeformation in the Marymia Inlier granites decreases toareas where they are undeformed The contacts betweenthe Peak Hill Schist and rocks of the Bryah Group arefaulted (probably thrusted) and tectonically interleaved inplaces
Rocks of the Peak Hill Schist include phyllonitequartzndashmuscovite schist calc-silicate schist sericite(ndashquartz) schist and quartzndashmuscovitendashbiotitendashchloriteschist locally with rotated alkali feldspar porphyroblasts(Fig 3) and minor metabasite These units have beenvariously deformed and contain a range of mylonitictextures The mylonitic fabric of these rocks is revealedby SndashC surfaces and lines of lsquomica fishrsquo (Lister and Snoke1984) in a dominantly and variably recrystallized quartz-rich matrix (Figs 4 and 5) A few discrete mylonitic units
Figure 3 Orthoclase porphyroblast with curved inclusiontrails in quartzndashmuscovite schist of the Peak HillSchist crossed polars
Figure 4 Partially recrystallized mylonite (Crispin Mylonite)from the Peak Hill Schist This sample is from amylonitic quartzndashbiotitendashalbite schist from the MineSequence in which the biotite defines C planesThe S planes were obliterated by recrystallizationto a blastomylonite crossed polars
Figure 5 Peak Hill Schist mylonite The C surfaces havesurvived recrystallization and now form thin micatrails crossed polars
form arcuate zones interpreted as early possibly thrustfault zones (see Structure) One of these units is the PeakHill Mylonite (Pirajno and Occhipinti 1998) which is arefolded quartz blastomylonite and quartz mylonite lenswithin quartzndashmuscovite schist The Peak Hill Mylonite(Figs 6 and 7) is an important unit because it is spatiallyassociated with gold mineralization (Peak Hill and MountPleasant deposits) Other less conspicuous quartzmylonite lenses are common within the Peak Hill Schistand were previously mapped as cherts or banded cherts(Windh 1992) Another important unit is the CrispinMylonite (Pirajno and Occhipinti 1998) which lies in thesouthern part of the Peak Hill Schist between sericiteschist and quartzndashmuscovite schist The Crispin Mylonitereferred to by Gee (1987) as the lsquoCrispin Conglomeratersquois characterized by square to rounded quartz arenite clastsup to 60 cm long in a sericite-rich matrix On the basisof field and petrographic observations it is concluded
6
Pirajno et al
here that this unit is not a conglomerate but a mylonite(Pirajno and Occhipinti 1998) Mylonites that resembleconglomerates (pseudo- or tectonic conglomerates) havebeen reported by Peters (1993) and Raymond (1984ab)
The Marymia Inlier (Windh 1992 lsquoMarymia Domersquoof Gee 1987) represents a fragment of northeasterlytrending Archaean granitendashgreenstone basement Rocksof the Marymia Inlier are mainly granitic but also includesmall enclaves of calc-silicate rock orthoamphibolite andminor metamorphosed banded iron-formation (BIF) ThePeak Hill Schist is also tentatively placed within theMarymia Inlier The granitic rocks are locally stronglyfoliated to gneiss or display strong cataclastic fabricsGranitic rocks include both fine-grained (aplitic) andcoarse-grained porphyritic phases Some outcropspreviously mapped as granite by Gee (1987) have beenincluded in the Peak Hill Schist The granitic rocks of theMarymia Inlier are monzogranite in the east and showincreasing cataclastic deformation towards the southwest(Pirajno and Occhipinti 1998 Bagas 1998)
Bryah GroupThe Bryah Group is divided into four formations theKaralundi Narracoota Ravelstone and HorseshoeFormations (Figs 1 and 2 Table 1) The basal unit of theBryah Group is the Karalundi Formation which is infaulted contact with the Doolgunna Formation of theYerrida Group along the Goodin Fault The KaralundiFormation predominantly consists of quartz conglomeratequartz arenite lithic wacke and shale The NarracootaFormation (parts of which were previously known aslsquoNarracoota Volcanicsrsquo Gee and Grey 1993) is thedominant lithology in the Bryah Basin and consists oftholeiitic extrusive and intrusive rocks and subordinateultramafic units intercalated with minor jasperoidal chertunits and clastic sedimentary rocks The NarracootaFormation is disconformably overlain by and locallyinterfingers with the Ravelstone Formation TheRavelstone Formation comprises a succession of lithic andquartz wacke shale and siltstone that was deposited byturbidity currents This formation is in turn conformablyoverlain by the Horseshoe Formation comprising quartzwacke manganiferous shale and banded iron-formation
The age of the Bryah Group is poorly constrainedbetween c 2000 and 1800 Ma Detrital zircons ofuncertain provenance in the Ravelstone Formation (upperBryah Group) provide a maximum age of 2014 plusmn 22 Ma(Nelson 1997) The Bryah Group must be older than theunconformably overlying Mount Leake Formation (outlierof the Earaheedy Group) which has a UndashPb (detritalzircon) maximum age of 1785 plusmn 11 Ma (Nelson 1997)The PbndashPb isochron ages obtained from pyrite from themesothermal Mikhaburra gold deposit (174 Ga Pirajnoand Occhipinti 1998) and from inferred syngenetic pyritefrom the Narracoota Formation (1920 plusmn 35 Ma Windh1992) probably represent mineralizing events in the BryahBasin rather than the depositional age of the BryahGroup
Karalundi Formation
The Karalundi Formation forms the base of the BryahGroup outcropping in a northeasterly trending belt alongthe southeastern margin of the Bryah Basin (Plate 1)Rocks of the Karalundi Formation are estimated to reacha thickness of approximately 2500 m In the southeastalong the Great Northern Highway Karalundi Formationrocks are in faulted contact with the Doolgunna Formation(Yerrida Group) On the southeastern side of the Peak HillSchist and in faulted contact with it the KaralundiFormation outcrops 35 km east of the Wilgeena mine Inthe south the Karalundi Formation is intercalated withmafic volcaniclastic rocks of the Narracoota Formation
The Karalundi Formation is characterized by immatureclastic (mainly quartzndashlithic wacke and conglomerate)units containing angular quartz and lithic fragments setin a sericitendashclay-rich matrix Other rock types includesiltstone calcareous siltstone cross-bedded areniteferruginous arenite litharenite minor dolomite andpurple green and black shale The Karalundi Formationalso contains pods of hematitic jasperoidal chert (see
Figure 6 Outcrop of quartz mylonite Peak Hill Schist Notethe flaggy nature of this rock and its steep dip
Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating atypical mylonitic fabric and SndashC planes (C planesare horizontal S planes trend from upper right tolower left between the C planes) crossed polars
7
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
below) which were interpreted by Gee (1979 1987) asfumarolic pipes
On DOOLGUNNA quartz arenite and conglomerate unitsare present within a dominantly hematitic shaly successionthat was interpreted by Adamides (1998) as a deep-waterlateral facies of the Bryah rift succession This successionalso contains olistoliths (exotic blocks) whose origin isnot clear Adamides (1998) suggested that they might havebeen derived from units of the Juderina Formation as aresult of inversion of the adjacent Yerrida Basin and upliftof the Goodin Inlier
Narracoota Formation
Rocks of the Narracoota Formation constitute a majorlithotype of the Bryah Group They form the bulk of thegroup with a thickness estimated at about 6 km (Pirajnoand Occhipinti 1998) and extend for more than 180 kmeast to west across the Bryah Basin The NarracootaFormation conformably overlies and locally interfingerswith the Karalundi Formation and also interfingers withand is in disconformable contact with the base of theoverlying Ravelstone Formation Contacts between theNarracoota Formation and Padbury Group are tectonic Inthe north regional structural relationships suggest that theNarracoota Formation is also in tectonic contact with theHorseshoe Formation Gravity modelling indicates that theNarracoota Formation forms the floor of the central partsof the Bryah Basin (Pirajno and Occhipinti 1998)
Rocks of the Narracoota Formation are affected bysea-floor metasomatism and regional prograde andretrograde metamorphism (see Structure) On the basisof field observations texture geochemistry and petrologyrocks of the Narracoota Formation can be subdivided intometamorphosed peridotitic and high-Mg metabasaltbasaltic hyaloclastite pyroclastic rocks intrusive rocksand mafic and ultramafic schist Collectively thesesubdivisions are referred to as metabasites Mafic andultramafic schists are characterized by a pervasiveschistosity but the distinction between mafic andultramafic is subtle and most clearly demonstrated usinggeochemistry In the area 2 km northeast of the Ravelstonemanganese opencuts a texture described by Hynes andGee (1986) as polygonal jointing has been observed in themetabasalt and appears to be a well-developed pencilcleavage High-Mg basalts are associated with peridotiticunits Intrusive rocks cover a range of types frompyroxenite to gabbroic rocks and dykes Metabasaltichyaloclastites are lava flows that interacted with seawaterand have a distinct spilitic character Volcaniclastic rocksincluding vent breccias are commonly present in bothbasaltic hyaloclastite and mafic schist
Typically the metabasite rocks of the NarracootaFormation contain no or very few feldspar phenocrystsOther authors have suggested that the presence ofmedium-grained embayed quartz crystals indicates theproximity of felsic volcanic rocks (Hill and Cranney1990 Windh 1992) Felsic volcanic rocks are associatedwith the upper part of the Narracoota Formation at andaround the Horseshoe Lights copperndashgold mine onJAMINDI 29 km east of the Fortnum mine on MILGUN
Fine-grained grey to black metamorphosed shale andslate are present in places as lenses of interflowsedimentary rocks within the volcanic succession Wheremore deformed and metamorphosed these slates are finelylaminated biotitendashchlorite schists South of the RobinsonRange small lenses of sedimentary rock (lithic wacke andshale) are intercalated with the volcanic rocks of theNarracoota Formation In places pods and lenses ofjasperoidal chert are associated with the volcanic rocks
Peridotitic and high-Mg basalt association
Massive layered high-Mg basaltic rocks (possibly lavaflows shown on Plate 1 as Anu) are preserved inprominent hills between Top Dimble Well and DespairBore on MILGUN Hynes and Gee (1986) described thissequence as komatiitic basalt with up to 20 MgOUnequivocal pillow structures as mentioned by Hynes andGee (1986) were not observed The rocks are meta-morphosed but their protoliths include olivine cumulate(peridotite) high-Mg basalt with plumose and harrisitictextures and medium-grained basalt Layering is mainlydefined by massive olivine cumulate layers up to 20 mthick and plumose-textured basalt layers up to 5 m thickLocally large sheaves of skeletal amphibole (afterpyroxene) are arranged at approximately right angles tothe layering and resemble harrisitic textures (Fig 8a) Thehigh-Mg basalt units are characterized by well-developedlsquospinifexrsquo-like textures with acicular tremolitendashactinoliteafter pyroxene and up to 30 interstitial plagioclase(replaced by epidote or zoisite) The high-Mg basalt isinterlayered with medium-grained basalt of similarmineralogy and composition with 8ndash9 MgO Thewhole-rock geochemistry of these rocks is discussed inGeochemistry of the Narracoota Formation
Peridotite units commonly consist of 70ndash80 fine- tomedium-grained olivine replaced by tremolite(ndashtalc)skeletal amphiboles after pyroxene and 20ndash30 fine-grained matrix of plumose-textured amphibole High-Mgbasalt contains up to 30 locally glomeroporphyriticolivine (now tremolite) lesser amounts of acicularpyroxene in a 60ndash70 amphibole plumose-texturedmatrix and 15 MgO One particular example contains35 olivine (only partly altered to talc) skeletal(lsquoswallow-tailrsquo) fresh orthopyroxene and lesser amountsof acicular skeletal amphibole prisms possibly afterclinopyroxene (Fig 8b)
Intrusive rocks and layered intrusions
A metadolerite sheeted dyke complex (shown as And onPlate 1) outcrops north of the Robinson Syncline Theserocks are associated with deformed pillow metabasalt andtend to be internally undeformed but commonly formelongate bodies subparallel to the S2 foliation Theycontain diopside amphibole epidote and minor olivine
Lenses of cumulate-textured units represented bypyroxenite or peridotite and gabbroic rocks are locallyintercalated with the mafic and ultramafic schist Alensoidal outcrop of metapyroxenite is present nearDurack Well Gabbroic rocks are common betweenTrillbar Homestead and Friday Pool on MOORARIE
8
Pirajno et al
(Occhipinti and Myers 1999) These rocks have beenmetamorphosed and folded but are largely undeformedinternally The gabbroic rocks are surrounded by higherstrain zones consisting of tremolitendashactinolite schist
The Trillbar Complex (shown as Ant on Plate 1) is a30 km long by 25 km wide layered maficndashultramaficintrusion in the westernmost part of the Bryah Basin Thecomplex consists of rhythmically layered mafic andultramafic rocks with the layering oriented at a low angleto the regional foliation (Occhipinti and Myers 1999)Rock types include rhythmically layered gabbromelanogabbro leucogabbro pyroxenite and peridotiteThese rocks are metamorphosed to greenschist facies butthe original igneous textures are locally well preservedThe Trillbar Complex rocks contain assemblages ofserpentinendashtremolitendashtalc tremolitendashtalcndashmagnetitetremolitendashactinolite and actinolitendashfeldspar Cumulaterocks include olivinendashpyroxene pseudomorphed bytremolite and sphene West of the Trillbar Homestead arelayers of metamorphosed pyroxenite and peridotite inwhich the original mineral phases are totally replaced by
tremolite talc magnetite and chlorite The TrillbarComplex is interpreted here as representing a remnant ofLayer 3 (layered gabbroic rocks) of an oceanic crustsuccession (Burke et al 1981) If this is correct thenprogressively lower levels of the Narracoota Formation areexposed from east to west and this is supported by thewidespread occurrence of volcaniclastic units in thecentral and eastern parts of the Bryah Basin
Mafic and ultramafic schist
Maficndashultramafic schist consists of actinolite(ndashchloritendashclinozoisite) schist and chlorite schist (shown as Anu andAn on Plate 1) In the south-central part of BRYAH schistoutcrops form an arcuate band (possibly an antiformstructure Gee 1987) south of and following the trendsof the Robinson Syncline and the southern limbs of theFraser Synclinorium (see Structure) North of thesestructures sparse outcrops of mafic schist are present justsouth and north of the Peak Hill Schist Within the schistare pods of less deformed or internally undeformedmetabasites in which pillow structures are locally wellpreserved Overall this large band forms a majoranastomosing sheared domain (Pirajno et al 1995b) Thedominant schistosity strikes approximately easterly orwest-northwesterly and dips steeply to the north andsouth A number of quartz veins within this shear domainalso strike easterly Maficndashultramafic schist was formedas a result of deformation and metasomatism of metabasiterocks along D2 shear zones (see Structure) In most casesall original volcanic textures are obliterated although inplaces round or elongate chlorite aggregates areinterpreted as original amygdales or fine pyroclasts
To the northwest on MILGUN the mafic volcanicschist occurrences are in faulted or sheared contactwith rocks of the Labouchere Wilthorpe and RobinsonRange Formations Hill and Cranney (1990) documenteda sequence of ultramafic to mafic schists with orwithout jasperoidal chert lenses overlain by fragmentalvolcaniclastic rocks fine-grained siltstone and felsic(intermediate and dacitic) crystal tuffs These are in turnoverlain by the Ravelstone and Horseshoe Formations
Mineral constituents of the mafic schist are actinolitechlorite and clinozoisite with minor calcite pumpellyitesericite titanite quartz and relict albite Ultramafic schisthas a simpler and commonly almost monomineralicmineralogy consisting of actinolitendashtremolite withretrogressed patches of pale-green chlorite In zones ofmore intense deformation chlorite- or epidote-dominatedassemblages are present (chlorite schist and epidositerespectively) These minerals developed due to strongmagnesium and calcium metasomatism probably duringcirculation of H2OndashCO2 fluids (Pirajno et al 1995b) Fluidinfiltration caused the breakdown of tremolite andclinozoisite to produce chlorite calcite and silica Thesilica thus liberated was then channelled through shearzones resulting in silicification and quartz veins (Pirajnoet al 1995b) An example of this can be seen in abreakaway 13 km east of the Wembley gold mine wheremafic schist and deformed pillow lavas display chloritealteration and pervasive silicification near and along awest-northwesterly trending shear zone In high-strain
Figure 8 Maficndashultramafic volcanic rocks of the NarracootaFormation (Dimble Belt) a) Komatiitic pyroxenitewith skeletal amphibole prisms after a quench-textured pyroxene matrix b) Peridotite with olivinepartly altered to talc around the edges and pyroxenein a fine-grained tremolite matrix both in planepolarized light
9
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
zones a new fabric is defined by the alignment ofamphibole prisms elongate epidote and quartz Theseschists are commonly characterized by well-developedlsquopencil cleavagersquo as a result of two intersecting planarfabrics
Metabasite rocks commonly show relict igneoustextures of prismatic plagioclase and interstitial amphiboleand more abundant unoriented prisms or acicular grainsof fine- to medium-grained amphibole Massive sheaf-liketextures of acicular amphibole are interpreted as primaryigneous textures A few plagioclase phenocrysts (3ndash5 mm)are preserved The amphibole is colourless to pale-greenpleochroic actinolite (or actinolitendashtremolite) plagioclaseis albite and commonly pseudomorphed by clinozoisitendashepidote or sericitized in zones of alteration Minorconstituents include chlorite quartz and sphenendashleucoxene with local zones of massive epidote(ndashcarbonate)
A schistose metabasite 5 to 8 km northeast of the PeakHill opencut contains actinolite arfvedsonite calcitediopside epidote and quartz The alignment of actinoliteand arfvedsonite defines the S2 schistosity and thereforeboth these minerals were formed during prendashsyn-D2 (seeStructure) The presence of the arfvedsonite (sodicamphibole) suggests either an original sodium-rich rockor later sodic metasomatism during or prior to D2
Metabasaltic hyaloclastite
Metabasaltic hyaloclastites form a prominent outcrop areapartly covered by ferricrete and colluvium south of theMurchison River These rocks are separated from themafic and ultramafic schist by the Murchison Fault(Plate 1) and probably represent a substantial thicknessof mafic lavas and hypabyssal material Hynes and Gee(1986) and Gee (1987) estimated a total thickness rangingfrom 4 to 6 km On the northern part of the GLENGARRY
1100 000 sheet the metabasalts are intercalated withsedimentary rocks of the Karalundi Formation (Pirajnoet al 1998a) These metabasaltic rocks are interpreted ashyaloclastites mdash a term that denotes fragmentation dueto quenching (Fig 9) of lavas flowing in water or eruptingunder an ice sheet This results in non-explosive fracturingand disintegration of the quenched lavas (McPhie et al1993 Fischer and Schmincke 1984)
The metabasaltic hyaloclastites are undeformeddominantly of mafic composition and have a spiliticcharacter Spilites are basaltic rocks that become alteredthrough metasomatic exchange with seawater therebyincreasing their sodium content The hyaloclastites havenormative albite from 13 to 23 wt and Na2O contentsof up to 6 wt
The metabasaltic hyaloclastites are commonly aphyricand composed mainly of acicular crystals of actinolitearranged in sheaves together with epidote minorcarbonate prehnite quartz and titanite in a fine-grainedgroundmass of albite microlites chlorite and epidoteCoarse-grained equivalents (clinopyroxene and plagioclaselaths) display ophitic to subophitic textures North of theMikhaburra (Holdens Find) gold deposit a small shaft has
Figure 9 Basaltic hyaloclastite of the Narracoota Formationshowing cuneiform devitrified shards now replacedby silica and sericite plane polarized light
exposed a vesicular rock containing serpentinized olivinecrystals set in a very fine grained altered matrix ofactinolite probably replacing pyroxenes
These metabasalts are commonly unfoliated andmassive with a characteristic brecciated or jigsaw-fittexture outlined by epidote carbonate prehnite and quartzveining along cooling joints In places these cooling jointsmay form pseudo-pillow structures and may be mistakenfor pillow lavas (Hynes and Gee 1986) Microscalejigsaw-fit textures are also seen
Felsic schist
Felsic schists which host sulfide mineralization (seeMineralization) at the Horseshoe Lights copperndashgolddeposit are present in the northern part of the BryahBasin Stratigraphically the felsic schist are at the top ofmafic metavolcanic rocks of the Narracoota Formation andoverlain by rocks of the Ravelstone Formation (seebelow) which contain chert lenses and layers close to thiscontact The felsic rocks are offset by a northeasterlytrending fault near the mine area and extend for about75 km in a southeasterly direction where they are offsetagain by a northeasterly trending fault However they donot reappear on the other side of the fault where the maficmetavolcanic rocks are in contact with the clasticsedimentary rocks of the Ravelstone Formation
Felsic schist includes quartzndashsericite schist sericiteschist and chlorite schist all showing varying degrees ofdeformation and development of mylonite Examinationof drillcore from the Horseshoe Lights mine revealedstructures reminiscent of felsic volcaniclastic rocks suchas collapsed pumice fragments Quartzndashsericite andsericite schist are composed of quartz and feldsparporphyroclasts partially replaced by quartz and sericitecarbonate or chlorite and wrapped around by granoblasticaggregates of quartz and sericite these aggregates aretraversed by anastomosing bands of sericite Tourmalineis present in places In one example sericite schistcontains elliptical opaque fragments suggestive ofcollapsed pumice Chlorite schist is composed of chlorite
10
Pirajno et al
and granular quartz with the chlorite forming distinctmonomineralic laminae X-ray diffraction analyses ofaltered schist indicate the presence of quartz kaolinpyrite hematite goethite and dioctahedral sodianmuscovite or potassian paragonite
Based on petrographic and core examinations thefelsic schist precursor rocks may have been quartzndashfeldspar porphyry and felsic volcaniclastic rocks
Volcaniclastic rocks
Mafic volcaniclastic rocks have well-preserved eutaxiticor fragmental textures despite intensive foliation (Fig 10)In the Fortnum mine area mafic fragmental rocks andfine-grained mafic volcaniclastic rocks are spatiallyassociated with jasperoidal chert pods The fragmentalrocks are strongly schistose with flattened and stretched
fragments of chlorite schist quartzndashchlorite schist withplagioclase phenocrysts quartzndashfeldsparndashamphibole rock(metabasalt) medium-grained plagioclase grains andmore rarely quartz crystals in a fine-grained matrix Finelylayered mafic schists consist of an amphibolendashplagioclasematrix with scattered prismatic to ovoid plagioclasephenocrysts and quartz lsquoeyesrsquo Amphibole accessorybiotite and sericite lenses have a strong preferredorientation suggesting that recrystallization in these fine-grained rocks has destroyed any volcaniclastic texture
Volcanic breccia is present in at least three localitiesThe most important of these is 5 km north of the oldCashman mine in the southern part of BRYAH (seeMineralization) Outcrops of volcanic breccia are alsopresent at the Cashman mine and 3 km west of the PeakHill ndash Fortnum road junction The nature of these angularclast-supported poorly sorted blocks of mafic volcanicmaterial suggest that they are vent breccias Volcanicbreccia was intersected throughout 455 m of core indrillhole BD1 (BRYAH AMG 380380) drilled by NorthExploration Ltd in 1993 (McDonald 1994) This coreintersection is briefly described below
Drillhole BD1 was drilled to a depth of 520 m at aninclination of 70deg towards the south and intersected claysand gravels to a depth of 65 m followed by weatheredmafic volcanic breccias to 96 m Below this depth to theend of the hole at 520 m spectacular fresh proximal vent-facies material consisting of angular blocks and clasts ofbasaltic lava tuff and chert were intersected (Fig 11)Crude bedding is present locally as are thin layers oflaminated or cross-laminated cherty material The holebottomed in cross-laminated chert which is interpreted aspyroclastic surge and tuff deposits The basaltic rocksinclude fine-grained vesicular basalt and feldspar-phyricand augite-phyric basalts The porphyritic varieties arecharacterized by a microlite-rich feldspar matrixclinopyroxene granules interstitial glass and chlorite andopaque minerals (titanite or rutile) The feldspar
Figure 10 Mafic volcaniclastic rock of the NarracootaFormation showing relict glass shard (in centre)plane polarized light
Figure 11 Volcanic breccia of the Narracoota Formation intersected in diamond drillhole BD1 Clasts arepredominantly of basaltic rocks the matrix exhibits albitic alteration Width of the core trays is 040 m
11
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
phenocrysts are selectively altered to sericite whereas theaugite phenocrysts are fresh and exhibit distinct zoningVesicles are infilled (from rim to core) by albite epidotechlorite and calcite Minor sulfide specks mainlychalcopyrite may be present in the vesicular basalt Tuffscharacterized by fluidization (due to degassing) andeutaxitic textures consist of glass shards and crystal andlithic fragments set in a devitrified and variably alteredglassy matrix Alteration phases are mainly chloritecalcite quartz and albite Chalcopyrite blebs are presentin places Hydraulic fracturing and veins of calciteprehnite quartz and chlorite are abundant One sectionbetween 200 and 360 m is characterized by albiticalteration (sodium metasomatism) which imparts a pinkto reddish colouration to veinlets and patches where thealbite is present
The fragmental mafic volcanic rocks in drillhole BD1are interpreted to represent a proximal vent-facies volcanicbreccia This vent-facies material coincides withprominent magnetic and Bouguer gravity anomalies(Pirajno et al 1995a) The magnetic anomaly which isrelated to the presence of magnetite in pyroxene basalthas a well-defined northeasterly trending elliptical shapeand could conceivably indicate the remnants of a majorvolcanic edifice Magnetic modelling suggests thepresence of two tabular bodies dipping 25deg to the north(Bui Dung 1999 pers comm) The gravity anomaly isat the centre of a large regional gravity high whichunderlies most of the area occupied by the NarracootaFormation (Pirajno and Occhipinti 1998)
Carbonated and silicified metavolcanic rocks
Carbonated and silicified maficndashultramafic rocksinterpreted as part of the Narracoota Formation outcropin the Horseshoe anticlinal block (Plate 1) These rocksare compositionally heterogeneous and both underlie andare intercalated with rocks of the Horseshoe FormationThis suggests that the interleaving is tectonic becauseelsewhere in the Bryah Group the Horseshoe Formationis not observed to be in direct contact with the NarracootaFormation (Occhipinti et al 1999)
Jasperoidal chert
Jasperoidal chert pods are present locally within theNarracoota Formation (Gee 1987 Hill and Cranney1990 Pirajno and Occhipinti 1998) but are commonlytoo small to be represented individually on geologicalmaps One of the largest pods outcrops 15 km due southof Ruby Duffer Well in the southern part of BRYAH Windh(1992) investigated the chert pods in some detailgeochemically discriminated them on the basis of theirNiCr ratios and distinguished jasperoidal syngeneticexhalative chert silicified volcanic or sedimentary rockssilicified shear zone rocks and surface silicificationSeveral of these chert pods such as those in theNarracoota Formation south of the Peak Hill Schist innorthern BRYAH are quartz mylonites mdash probably Windhrsquos(1992) silicified shear zone rocks A few may be chemicalprecipitates deposited by hot springs whereas others mayrepresent silicified fault zones
The cherty material is reddish to grey colouredmassive to banded and extensively veined by quartzThe chert consists of very fine grained recrystallizedquartz with equant to elongate polygonalndashgranoblastictextures locally with a crystallographic preferredorientation Minute opaque minerals locally includingmagnetite or pyrite define trails parallel to the quartzfoliation In the Yarlarweelor opencut (Fortnum mine)pebbles of these cherts in overlying mafic fragmentalrocks suggest that the cherts formed as exhalative horizonsrelated to volcanism Alternatively the jasperoids mayrepresent iron-rich silicification along major shear zonesIn the Yarlarweelor opencut the chert pods host epigeneticgold mineralization in and around quartz(ndashpyrite) veinsystems (Hill and Cranney 1990)
Geochemistry of the Narracoota Formation
Major trace and rare earth element (REE) whole-rockanalyses of samples of metabasite rocks of the NarracootaFormation collected during this study are included in thedigital dataset in the back pocket These data were usedto characterize the geochemistry of the volcanic rocks ofthe Narracoota Formation in an attempt to better definethe rock types and gain an insight into the nature of theparent magma(s) and tectonic setting Representativeanalyses of Narracoota Formation rocks are presented inTable 2
The Narracoota metabasite rocks are commonly oftholeiitic composition with mixed mid-ocean ridge basalt(MORB) ndash oceanic island and continental geochemicalsignatures They span the range from high-Mg basalt tokomatiite and peridotitic komatiite or peridotite (possiblysubvolcanic cumulates) Common characteristics includehigh MgO high Ni and Cr moderate to low REEabundances and nearly flat chondrite-normalized REEpatterns with weak Eu anomalies possibly reflectingdepleted asthenospheric mantle sources (Pirajno and Davy1996 Pirajno et al 1996 Pirajno and Occhipinti 1998Occhipinti et al 1998ac) There are subtle chemicaldifferences between the hyaloclastites and maficndashultramafic schists (Tables 3 and 4 see below)
Hynes and Gee (1986) and Pirajno and Davy (1996)reported on the petrochemistry and tectonic setting ofthe Narracoota Formation metabasite rocks Hynesand Gee (1986) concluded that they have fairlyuniform chemistry and are of MORB affinity although theoriginal mafic volcanic rocks may have been emplacedthrough the rifting of continental crust Pirajno and Davy(1996) proposed that the Narracoota Formation meta-volcanic rocks might have formed in a setting analogousto that of the present-day Gulf of California (Lonsdaleand Becker 1985) The origin of the NarracootaFormation metabasites is discussed in Tectonic model andconclusions
Classification based on chemistry
The total alkali ndash silica (TAS) and high-Mg plot(Le Maitre 1989) indicates that the bulk of the rocks ofthe Narracoota Formation range in composition fromkomatiitendashpicrite through basalt to basaltic andesite
12
Pirajno et al
Table 2 Representative chemical analyses of the Narracoota Formation
Rock _________________ Mafic schist _________________ _______ Hyaloclastite _______ _______ Ultramafic _______ ____ Trillbar __type schist ComplexSample 132788 132789 132790 133033 133050 112643 116485 104256 132791 139138 139139 135482 143538
Percent
SiO2 5424 4945 5277 463 4907 5187 5139 5011 4923 4723 4789 5137 4961TiO2 028 113 031 019 026 073 063 053 019 016 017 037 141Al2O3 1422 1172 1466 948 794 138 1512 1503 1043 765 867 1481 1391Fe2O3 248 345 184 661 635 224 296 278 146 396 201 232 561FeO 598 824 705 741 101 848 662 529 834 548 708 561 717MnO 017 019 018 025 198 02 016 014 018 012 015 016 022MgO 929 1243 1036 1517 778 1036 83 936 2063 2877 2678 869 656CaO 1106 1107 962 1451 2262 974 1144 1514 86 641 704 1068 1136Na2O 218 212 274 003 009 216 32 145 092 018 019 306 204K2O 007 008 046 001 284 036 01 011 002 003 001 006 022P2O5 003 013 002 003 007 007 006 005 001 001 001 003 011Total 10000 10001 10001 9999 10001 10001 9998 9999 10001 10000 10000 9716 9822
Mg 6687 6615 6795 6692 6736 6377 6142 6816 792 85 843 ndash ndash
Parts per million
Ag ndash ndash ndash ndash ndash 1 ndash 1 ndash ndash ndash ndash ndashAs 155 157 052 22551 13032 ndash ndash ndash ndash 832 ndash ndash ndashAu ndash ndash ndash ndash ndash 104 ndash ndash ndash ndash ndash ndash ndash
Ba 55 140 79 27 2 846 341 127 92 74 37 102 39 322Cd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash
Co 55 86 58 223 51 ndash ndash ndash 99 113 111 ndash ndash
Cr 509 1 201 686 2 574 72 489 364 283 1 836 2 530 3 146 593 82Cu 168 124 63 327 20 108 101 39 55 9 11 59 172Ga 10 16 10 8 9 12 12 13 8 6 6 12 19Hf ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 07 14Mo ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 08 26Nb ndash 63 ndash ndash 52 ndash ndash ndash ndash ndash ndash 1 9Ni 203 548 241 1 274 91 258 143 164 866 1 531 1 230 124 98Pb ndash 2 ndash ndash 7 ndash ndash ndash ndash ndash ndash 1 4Pd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashPt ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashRb 1 ndash 6 ndash 85 6 ndash 2 ndash 1 ndash 1 4Sb ndash ndash ndash ndash ndash 415 ndash 511 ndash ndash ndash ndash ndashSc 50 41 51 31 10 ndash ndash ndash 40 34 38 51 48Sr 64 149 64 54 100 163 82 188 23 23 7 61 279Ta ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashTh ndash 104 ndash ndash 717 ndash ndash ndash ndash ndash ndash ndash ndashU ndash ndash ndash 064 13 ndash ndash ndash ndash ndash ndash 08 14V 196 277 202 138 78 250 249 217 144 115 143 235 362W ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashY 13 18 12 8 16 17 14 11 8 6 7 17 24Zn 65 94 68 45 50 85 73 55 62 51 45 61 91Zr 13 68 15 17 50 51 47 38 7 7 8 20 86
La 089 936 043 054 1819 36 35 35 093 017 056 2 6Ce 218 2264 129 084 4445 9 83 83 153 042 082 2 15Pr 037 29 02 02 418 12 11 13 02 009 019 0 2Nd 166 1193 108 102 1511 57 51 57 102 047 079 5 12Sm 08 328 065 056 306 15 14 15 065 03 034 ndash ndashEu 042 13 032 028 223 09 07 08 029 011 011 ndash ndashGd 166 409 141 085 305 23 17 2 129 065 071 ndash ndashTb 04 069 031 018 04 04 04 04 029 014 016 ndash ndashDy 268 408 233 12 202 27 24 24 214 108 116 ndash ndashHo 071 087 057 028 037 05 05 05 053 027 03 ndash ndashEr 222 231 173 094 115 18 15 16 162 083 091 ndash ndashTm 039 033 027 016 017 02 02 02 027 014 015 ndash ndashYb 229 196 182 115 125 15 14 15 166 086 09 ndash ndashLu ndash ndash ndash 019 02 02 02 02 ndash 013 014 ndash ndash
13
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(Fig 12) A small number of samples plot in the boniniteand andesite fields All metabasites of the NarracootaFormation (ultramafic and mafic schists and basaltichyaloclastite) are of subalkaline tholeiitic affinity (Fig 13)They commonly have restricted silica contents rangingfrom 45 to 55 wt (Fig 12)
The metabasites are all quartz albite anorthitediopside hypersthene and magnetite normative Themafic schists are hypersthene normative with lowerMgO contents (lt15 wt) and magnesium numbers (Mgmdash defined as MgO(FeO + MgO)) ranging from 43 to 74(Table 3) Some mafic schists have no quartz and areolivine normative (5ndash6 and up to 20 in some maficschists) The ultramafic schist is hypersthene and olivinenormative with MgO contents ranging from 153 to227 wt and Mg ranging from 75 to 86 (Table 3) Themetabasaltic hyaloclastites are albite and clinopyroxenenormative and have MgO contents of lt10 wt and Mgof between 47 to 68 (Table 3)
Ultramafic schist mafic schist and metabasaltichyaloclastite can be distinguished in terms of their Cr Niand Ti abundances FeOMgO ratios (Tables 3 and 4Figs 14a and 14b) and chondrite-normalized REEpatterns The hyaloclastite rocks are depleted in Cr andNi and enriched in TiO2 relative to the maficndashultramaficrocks (Fig 14c)
The Jensen (1976) cationic plot is based on theproportion of Fe2++Fe3++Ti versus Al and Mg cationsrecalculated to 100 and is particularly useful fordiscriminating subalkaline and Mg-rich metamorphosedvolcanic rocks in which the alkali content may havebeen modified during deformation and metamorphism(Rollinson 1993) In the Jensen plot (Fig 15a) the
Narracoota Formation rocks span the range of compo-sitions from high-Mg tholeiite through to komatiite andperidotitic komatiite in a trend of increasing MgO
Chondrite-normalized rare-earth element diagramscommonly regarded as the most useful of the traceelement plots in the petrogenesis of igneous rocks areused to determine the possible nature and source of themelts Particularly important are the overall patterns fromlight to heavy rare earth elements (LREE to HREE) thenormalized abundance of Eu controlled by feldspar andthat of Ce controlled by seawater or hydrothermal fluidsFor the Narracoota Formation rocks chondrite-normalizedREE abundances (Figs 15b and 15c) are commonly low(lt1 to lt40 times chondrite) The mafic schist ischaracterized by a spread in LREE from depleted toenriched (Fig 15b) with individual patterns almostidentical to those of mid-ocean ridges (OrsquoNions et al1976 Schilling 1982) and the recent basaltic lavas ofIceland (Schilling et al 1982) More specifically theLREE-depleted patterns (western Bryah Basin) arestrikingly similar to those of the Lau Basin spreadingcentre in Fiji (Pearce et al 1995) whereas slightlydepleted to slightly enriched LREE patterns (eastern Bryah
Table 3 Magnesium numbers for the Narracoota and Killara Formations
Rock Formation Range of Mg Average Mg Standard deviationof Mg
Metabasaltic hyaloclastite Narracoota 4677 ndash 6816 5716 525Mafic schist Narracoota 4337 ndash 7409 5957 669Ultramafic schist Narracoota 7516 ndash 8560 8105 254Tholeiitic basalt Killara 3504 ndash 6603 5035 739
NOTE Mg Magnesium number defined as MgO(FeO +MgO)
Table 4 Selected geochemical parameters for the NarracootaFormation
Parameters Hyaloclastite Mafic schist Ultramafic(mean values) schist
(LaYb)N 144 1702 037TiO2 (wt) 086 068 019NiCr 043 039 042Al2O3TiO2 162 205 4668MgO (wt) 731 780 2119
35 45 55 650
1
2
3
4
foidite andesite
basalt
boninite
basalticandesite
MgOgt18 picrite
basanite
tephrite
MgOgt18 amp TiO lt1 komatiite
picrobasalt
FMP365 021199
22
2
2
2
2
MgOgt18 amp TiO gt1 meimechiteMgOgt8 amp TiO lt05
SiO (wt)
Na
O +
K O
(w
t)
Figure 12 Total alkali versus silica diagram (Le Maitre1989) for rocks of the Narracoota FormationNote that a small number of samples fall withinthe boninite field this however may be due tohydrothermal alteration
14
Pirajno et al
Basin) are comparable to those of seamounts reflectinga more enriched source The nearly flat patterns havenegative Eu anomalies reflecting the primitive nature ofthe rocks presence of olivine clinopyroxene andorthopyroxene and fractionation of feldspar from themelt The patterns of the Iceland basalts that are nearlyidentical to those of the mafic schist of the Bryah Groupwere explained by Schilling et al (1982) as due toadvection of asthenospheric mantle at a mid-ocean ridgeConsidering field relations and petrological andgeochemical data it is conceivable that the NarracootaFormation metatholeiites may have had a similar originChondrite-normalized REE abundances for the meta-basaltic hyaloclastite are very low (9 to 14 timeschondrite) slightly LREE-enriched and with a distinctpositive Eu anomaly (Fig 15c) reflecting the addition ofalbite due to seawater metasomatism
The overall REE abundances and patterns of maficschist and hyaloclastite are strikingly similar to192 ndash 184 Ga mafic rocks of the Flin Flon belt in theTrans-Hudson Orogen in Canada (Lucas et al 1996)Some of the mafic rocks of the Flin Flon belt have beeninterpreted to belong to tectono-stratigraphic assemblagesof ocean floor and ocean island affinity Also the Flin Flonocean island tholeiites have REE patterns similar to
Figure 13 Total alkali versus silica diagram (Le Maitre 1989)defining limits of alkaline and subalkaline basaltsshowing the predominantly subalkaline nature ofthe Narracoota Formation
20
16
12
8
4
0
Na
O +
KO
(w
t)
22
857565554535
SiO (wt)2 11999FMP367
Hyaloclastite
Mafic schist
Ultramafic schist
Subalkaline
Alkaline
Figure 14 Geochemical characteristics of the NarracootaFormation a) TiO2 versus FeOMgO ratios notethe slight TiO2 enrichment of metabasaltichyaloclastite compared to maficndashultramafic schistb) Cr versus FeOMgO ratios note the Cr enrichmentof maficndashultramafic schist compared to meta-basaltic hyaloclastite c) TiO2ndashNindashCr triangular plotshowing Ni and Cr enrichment of maficndashultramaficschist compared to metabasaltic hyaloclastite
3
2
1
0
TiO
(wt
)2
1 2FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
4000
3000
2000
1000
0
Cr
(ppm
)
1 2 3FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
TiO 1002
Ni Cr91199FMP368a
Hyaloclastite
Mafic schist
Ultramafic schist
a)
b)
c)
15
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Hawaiian tholeiites (Stern et al 1995) The inference fromthese comparisons is that submarine volcanoes may havebeen a component of the Narracoota Formation
Tectonic discriminant diagrams do not provide reliableinformation on the palaeotectonic environment withinwhich igneous rocks were emplaced (Duncan 1987 Wangand Glover 1992) Nevertheless if there is petrologicalevidence that the rocks have not undergone extensivecrystal fractionation and the overall geological context is
taken into account selected discriminant diagrams can beused to estimate palaeotectonic settings With the aboveconsiderations in mind and remembering that the rocksin question have a subalkaline chemistry the FeO(tot)ndashMgOndashAl2O3 plot of Pearce et al (1977) is deemedappropriate (Fig 15d) The FeO(tot)ndashMgOndashAl2O3 plot hasbeen used successfully in geologically well constrainedareas (Breitkopf and Maiden 1988) The FeO(tot)ndashMgOndashAl2O3 plot suggests that the Narracoota Formationvolcanic rocks were formed in tectonic environments of
a)
c)
b)
d)
MgO
TA
TDTR
CR CDCA
HFTBK
PKCB
HMT
Sam
ple
chon
drite
100
10
2La Pr Eu Tb Ho Tm Lu
Ce Nd Sm Gd Dy Er Yb
La Pr Eu Tb Ho Tm LuCe Nd Sm Gd Dy Er Yb
Sam
ple
chon
drite
100
10
1
6
FeO
MgO
221199
Al O32
FeO + TiO2
Al O32
FMP154
Mafic and ultramafic schist
Metsabasltic hyaloclastite(tot)
Figure 15 Geochemical discriminant plots for Narracoota Formation rocks a) Jensen (1976) cationic plot showingrange of compositions from high-Mg tholeiite (HMT) through high-Fe tholeiite (HFT) basaltic komatiite(BK) peridotitic komatiite (PK) tholeiitic andesite (TA) tholeiitic dacite (TD) calc-alkaline basalt (CB)and calc-alkaline andesite (CA) b) Chondrite-normalized rare-earth element plot of mafic (HREE-enriched) and ultramafic (HREE-depleted) schist (normalizing factors after Sun 1982) c) Chondrite-normalized rare-earth element plot of metabasaltic hyaloclastite (normalizing factors after Sun 1982) d)Triangular discriminant plot (Pearce et al 1977) showing the tectonic environment of the NarracootaFormation Tectonic fields are as follows 1) spreading-centre island 2) orogenic 3) ocean ridge andfloor 4) ocean island and 5) continental
16
Pirajno et al
MORB ndash oceanic island to continental affinity (Fig 15d)This diagram however has limitations if the rocks havebeen subjected to ocean-floor metamorphism A moreuseful plot is the TiO2ndashFeO(tot)ndashMgO plot which was usedby Breitkopf and Maiden (1988) in their study of theNeoproterozoic Matchless Amphibolite Belt of theDamara Orogen in Namibia The TiO2ndash FeO(tot)ndashMgO plotsupports the gradation from MORB towards continentalflood basalt because the hyaloclastite rocks plot closer tothe continental field than do the mafic schist (Fig 16) Thisfeature together with other considerations such as Mgand geological and petrological constraints indicate thatthe hyaloclastite was erupted on a continental rift marginThis has important implications for the tectonic evolutionof the BryahndashPadbury Basin as explained in Tectonicmodel and conclusions
Ravelstone Formation
The Ravelstone Formation is poorly exposed in scatteredlow outcrops over a wide area in the northern and centralparts of the Bryah Basin Rocks of the RavelstoneFormation were previously considered by MacLeod(1970) and Gee (1979 1987) to belong to the lsquoThadunaGreywackersquo (now Thaduna Formation of the YerridaGroup) for which the type area is about 100 km to theeast-northeast on THADUNA (Pirajno and Adamides 1998)
The Ravelstone Formation comprises a succession oflithic and quartz wacke shale and siltstone that was
deposited from turbidity currents In the north theRavelstone Formation contains lenses of chert andis unconformably overlain by the MesoproterozoicBangemall Group West of the Peak Hill opencut thelower contact with the Narracoota Formation is dis-conformable whereas the upper contact with theHorseshoe Formation appears to be conformable In thecentral and northern parts of BRYAH the RavelstoneFormation although metamorphosed has no tectonitefabric On MILGUN (around Fortnum) however a well-developed foliation is present
Drillcore from the Harmony gold deposit shows thatthe contact between the base of the Ravelstone Formationand the top of the Narracoota Formation is interfingeredpossibly due to shearing The disconformable contactbetween the base of the Ravelstone Formation and the topof the Narracoota Formation is exposed in a river bedabout 1 km due east of the Fortnum ndash Peak Hill turn-offIn this area graded layers of immature subarkosicsandstone to siltstone contain fresh plagioclaseK-feldspar sericitized lithic fragments and angular quartzgrains in a matrix composed of sericite and biotite Inaddition the siltstone contains euhedral crystals oftourmaline Metamorphic brown biotite and muscovite areabundant and replace feldspars quartz and lithicfragments Lithic fragments include massive chlorite(ndashrutile) derived from mafic precursors chert hematitendashquartz shale as well as partly sericitized feldspar grainsQuartz grains include rounded to irregular shapes andbiotite is metamorphic in origin Quartz white micachlorite and variable amounts of carbonate are part of thefine-grained matrix Well-developed foliation wherepresent is defined by aligned sericite elongate quartzand to a lesser extent feldspar grains and by mica seamsNew muscovite flakes have grown along and across thefoliation
In the Fortnum mine area on MILGUN graded beddedlithic wacke and siltstone overlie the volcanic rocks of theNarracoota Formation The wacke contains medium tocoarse-grained crystals of feldspar (plagioclase minor K-feldspar) and quartz as well as fragments (fine metabasaltand chlorite) derived from mafic volcanic rocks Thefeldspar crystals which are strongly sericitized dominateover quartz The matrix consists of sericitendashchloritendashquartz with or without carbonate The reworked rocksinclude fragmental layers with fine metabasalt debris andgraded chloritic siltstone containing plagioclase laths Thederivation of the mafic component is easily explained butthe well-preserved feldspar crystals suggest nearbygranitic or felsic volcanic precursors
Horseshoe Formation
The Horseshoe Formation occupies areas west of thePeak Hill opencut and the northern parts of BRYAH
and MILGUN This formation includes finely laminatedferruginous (hematitic) shale and siltstone fine-grainedquartzndashfeldspar wacke with interleaved iron formation andchert graded quartz wacke manganiferous shalegarnetiferous biotitendashchlorite schist and garnetiferousiron-formation Relatively high manganese contents areinferred from the abundant manganese oxide staining in
CFB
MORB
20
18
15
13
10
08
05
03
000 1 2
TiO
2
FMP168 211099Ultramafic schist
Mafic schist
Hyaloclastite rocks
(tot)FeO MgO
Figure 16 TiO2 versus FeOMgO plot (Breitkopf and Maiden1988) for the Narracoota Formation showing themid-ocean ridge basalt (MORB) affinity of the maficand ultramafic schist and the transitional chemistryof the hyaloclastites towards continental floodbasalts (CFB)
17
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
weathered and lateritic rocks and lateritic manganese orehas been mined at the Horseshoe and Mount Padburymines The type area of the Horseshoe Formation is theHorseshoe Range (Occhipinti et al 1997) where athickness of approximately 1000 m was estimated by Gee(1979) The Horseshoe Formation overlies the NarracootaFormation however the contact is either conformable ortectonic Elsewhere on JAMINDI north of BRYAH theHorseshoe Formation overlies the Ravelstone Formationand the contact is gradational and conformable TheHorseshoe Formation underlies the Labouchere Formationof the Padbury Group The nature of this upper contactappears conformable however Martin (1994) suggestedthat there is a regional unconformity between these units
Structurally the Horseshoe Formation forms a broadsyncline with its axis trending approximately easterly Thesouthern limb of this syncline is in sheared contact withrocks of the Narracoota Formation In this area theHorseshoe Formation is complexly folded with axestrending 070deg parallel to the shear zone
In the Horseshoe Range Gee (1987) recognized threeunits 1) a lowermost part consisting of regularly beddedwacke and shale similar to the underlying Ravelstonesuccession but finer grained more calcareous andcontaining less chlorite and more feldspar and quartzindicative of a granitic rather than mafic volcanicprovenance 2) a middle iron-formation member withseveral BIF (chertndashmagnetitendashstilpnomelane white chert)horizons intercalated with chloritic shale and 3) anupper unit of calcareous manganiferous shale andwacke The lowermost unit is exposed on MILGUN in thelow hills east of Fortnum airstrip where fine-grainedcarbonate-cemented wacke and shale contain dis-harmonic-folded white-chert lenses (2ndash12 cm thick) andless common discontinuous quartzndashmagnetite layers(2ndash3 cm) The quartz wacke component of the HorseshoeFormation contains quartz plagioclase microclinebiotite and muscovite all as detrital minerals Nearthe Peak Hill opencut the iron formation is made upof biotite amphibole chlorite quartz magnetite andgarnet This unusually high grade assemblage may berelated to the metamorphism of the Peak Hill Schist (seeMetamorphism)
About 1 km north of the Ravelstone manganesedeposits a reasonably good exposure of the HorseshoeFormation was examined in detail A stratigraphic columnfor this locality is shown in Figure 17 This is a foldedupward-coarsening package approximately 350 m thickwhich from base to top consists of quartzndashlithic wackewith banded chert interbeds displaying a well-developedaxial planar cleavage quartz wacke with iron formationand shale interbeds massive beds of coarse-grainedquartzndashlithic wacke intercalated with thin granular iron-formation amphibole- and garnet-bearing granular iron-formation layers and massive quartzndashlithic wackeintercalated with thin iron-formation bands The quartzndashlithic wacke contains chert clasts detrital subangularquartz fresh plagioclase crystals and biotite in a matrixof sericite green chlorite and iron oxide grains Bandedcherty material is composed of granular quartz aggregatesbrown biotite actinolite and very fine carbonate-richlaminae (this rock is best classified as a quartzndashbiotitendash
actinolite schist) The granular iron-formation consists ofgranular aggregates of quartz and iron oxides withinterstitial biotite and chlorite Syntectonic garnetporphyroblasts are replaced in part by quartz andcarbonate Massive lithic wacke consists of a packedaggregate of angular quartz feldspar and chert grains thematrix is volumetrically small and made up of biotitequartz and sericite Garnetiferous iron-formation has darklaminae of quartz granules with interstitial actinolitendashchlorite iron oxides and light-coloured microbands (1 cmthick) of quartz with actinolitendashchlorite iron oxides anddisseminated synndashlate-tectonic garnet porphyroblastsGarnet is also present as porphyroblasts growing acrossmicroband boundaries
Padbury GroupThe Padbury Group locally unconformably overliesthe Horseshoe Formation of the Bryah Group but inplaces is in faulted contact with the Bryah Group andYarlarweelor gneiss complex (Narryer Terrane Yilgarn
FMP156 020300
0
100
200
300
intercalated with thin BIF and shale interbeds
Garnetiferous BIF
Massive beds of coarse-grained lithic wackewith interbeds of garnetiferous BIF and
Banded iron-formation interbedded with massive
Banded chertQuartzndashlithic wacke with carbonate cement
wacke and soft granular iron-formation
(m)
granular iron-formation
Massive quartzndashlithic wacke layers
Micaceous wacke
Figure 17 Schematic stratigraphy of the HorseshoeFormation from an area of outcrops about 12 kmwest-northwest of the Peak Hill mine (after Pirajnoand Occhipinti 1998 width of column reflectsrelative resistance to weathering)
18
Pirajno et al
Craton Fig 2) Considerable onlap of the Padburysuccession onto the various formations of the Bryah Groupcan be inferred these contacts were faulted possibly inseveral stages during basin closure The age of thePadbury Group is poorly constrained Nelson (1997)reported a maximum age of c 20 Ga from the upper partof the Wilthorpe Formation and Windh (1992) inferred aminimum age of c 18 Ga from a leucogranite dyke
Martin (1994 1998) proposed a formal stratigraphy forthe lower Padbury Group based on detailed sediment-ological studies in the area covering the southeastern andcentral parts of MILGUN This formal stratigraphy replacedprevious stratigraphic divisions (Barnett 1975 Gee1979 1987 Windh 1992) and has since beenexpanded to include two distinct lithostratigraphic unitsas members within the Wilthorpe Formation the Heinesand Beatty Park Members (Occhipinti et al 1997) Martin(1994 1998) interpreted the Labouchere and WilthorpeFormations as an upward-coarsening deep-water turbiditecomplex overlain by shales and iron formation of theRobinson Range Formation The turbidites were derivedby erosion from the granitendashgneiss basement (YilgarnCraton) and by reworking of underlying sedimentary andmafic volcanic rocks in the Bryah Basin
The Padbury Group contains quartz wacke siltstoneconglomerate iron formations hematitic shale and minorclastic rocks and dolomite (Martin 1994 Occhipintiet al 1997) and is subdivided into four formationsLabouchere Wilthorpe Robinson Range and MillidieCreek Formations Martin (1994) interpreted the PadburyGroup to have been deposited in a retroarc foreland basinthat developed on top of the Bryah Group
Labouchere Formation
The Labouchere Formation occupies areas in thenorthwestern part of the Bryah Basin where it isfaulted against the Yarlarweelor gneiss complex Martin(1994 1998) suggested that the Labouchere Formationunconformably overlies the Horseshoe Formation(Bryah Group) based on the regional geometry inthe Fortnum mine ndash Dandy Well area on MILGUN Theregional unconformity is inferred from the low-angletruncation of an iron-formation marker unit in theHorseshoe Formation against lowermost quartz areniteof the Labouchere Formation in the area south ofYarlarweelor Creek North of the Fortnum Fault ironformation within the Horseshoe Formation is nearlyparallel to bedding in the Labouchere FormationElsewhere in the region contacts between variousformations of the Bryah and Padbury Groupsare interpreted as unconformities (Windh 1992) oralternatively as faults or shear zones (Pirajno andOcchipinti 1998 Occhipinti et al 1998b) On BRYAH theLaboucherendashHorseshoe Formation contact is marked bya conglomeratic unit The Labouchere Formation isconformably overlain by and grades into the WilthorpeFormation (Martin 1994) although this contact waspreviously described as an unconformity (Gee 1979) Gee(1979) estimated the Labouchere Formation (including theWilthorpe Formation) to be 5000 m thick extending from
Mount Labouchere on MILGUN (type area Martin 1994)to the Horseshoe Range the southern continuation ofwhich is in northwestern BRYAH Martinrsquos (1994 1998)type section is a composite stratigraphy (up to 7000 mthick) based on four separate sections in southeasternMILGUN
The Labouchere Formation consists of quartz arenitemedium- to coarse-grained sericitic quartz wacke andsericitic siltstone minor conglomerate and banded iron-formation in an upward-coarsening succession Near theHorseshoe manganese mining area the LabouchereFormation consists of a thick succession of upward-finingcycles up to 700 m thick Each cycle consists ofconglomerate or a coarse lithicndashquartzndashsericite wacke unitat the base grading up through coarse- to fine-grainedquartzndashfeldsparndashlithic wacke and sericitic siltstone to iron-rich shale These cycles however become increasinglycoarser upwards so that there is regional upwardcoarsening The base of the topmost cycle begins with aquartz-pebble conglomerate Minor and thin bands of iron-formation are locally present as intercalations within thesedimentary units
Quartz arenite contains grain-supported well-roundedquartz in a sericitic matrix and is extensively silicified Aprominent quartz arenite marker forms the ridge includingMount Labouchere north of Fortnum mine on MILGUN andcan be traced for many tens of kilometres to the southeastwhere gradually more quartz wacke is interbedded withthe arenite A second quartz arenite marker approximatelyhalfway up the Labouchere Formation is present in thearea north of the Fortnum Fault In the same area an ironformation ndash chert layer is present about 250 m above thissecond quartz arenite Martin (1994) emphasized that thedeep-water environment of this iron formation indicatesa similar depositional environment for the clastic rocksQuartz wacke has a matrix-supported framework ofvariably rounded quartz grains minor lithic fragments andfeldspar in a sericitendashchlorite matrix whereas laminatedshale consists of sericitendashchlorite Wacke and siltstoneform numerous upward-fining cycles
Muscovitendashquartz schist or slate developed fromquartz wacke and siltstone in zones of high strain andhigher metamorphic grade adjacent to the Yarlarweelorgneiss complex Strongly foliated quartz wacke andmuscovitendashquartz schist occupy a 4 km-wide zone nearthe Labouchere mine on MILGUN Another belt of schistand slate is present between the Billara Fault and DespairGranite in southwestern MILGUN These strongly foliatedrocks can be traced northwards into recognizable thoughstrongly foliated pebbly quartz wacke The fine-grainedschist consists of elongate polygonalndashgranoblastic quartzwith spaced trails of aligned muscovite flakes Beddingndashcleavage relationships are found in less-deformed areaswhereas in high-strain zones differentiated layeringdeveloped from a pervasive crenulation cleavage
Sericite is abundant throughout most of the rocks ofthe Labouchere Formation The quartzndashsericite wacke iscomposed of subangular quartz grains embedded in asericitized matrix with occasional large muscovite lsquobooksrsquoand scattered small crystals of tourmaline and anatase
19
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Quartzndashfeldsparndashlithic wacke is made up of subangularquartz grains polycrystalline quartz K-feldspar andplagioclase in a matrix of quartz sericite biotite andminor detrital zircons
Wilthorpe Formation
The Wilthorpe Formation (formerly lsquoWilthorpeConglomeratersquo Gee 1987) including the Beatty Park andHeines Members comprises quartz- and chert-pebbleconglomerate quartz wacke sericitic siltstone chloritendashquartz shale quartzndashsericitendashhematite schist dolomiticsandstone and finely laminated chert lenses TheWilthorpe Formation is conformably overlain by theRobinson Range Formation
Martin (1994) measured the type section of theWilthorpe Formation (about 1300 m thick) along theTalbot Divide In this area the characteristic quartz-pebbleconglomerate forms a prominent ridge to the east of hillsunderlain by the Robinson Range Formation In theFortnumndashLabouchere area on MILGUN the exact locationof the LaboucherendashWilthorpe Formation transitionalboundary is less well defined (Swager and Myers 1999)Along the western wall of the Nathans Deep Southopencut (labelled Nathan Deep on Plate 1) severalupward-fining cycles of quartz-pebble conglomerategrading into quartz wacke and quartzndashmuscovite siltstonecan be observed These cycles are underlain by fine-grained chloritic shale interbedded with quartz wackeThis chloritic shale with detrital ilmenite is derived froma mafic precursor probably the Narracoota Formation(Windh 1992) Occhipinti et al (1998a) recognizedcomparable lsquomaficrsquo clastic rocks as a mappable unit(Beatty Park Member mdash see below) at the top of theWilthorpe Formation on PADBURY
The conglomerate contains well-rounded slightlyelongate or faceted vein-quartz clasts and less commonlychert quartzite quartz wacke and rare siltstonendashmudstoneclasts in a quartz wacke matrix Clasts range in size frompebbles to boulders Quartzite pebbles locally containfolded foliation fabrics Bunting et al (1977) suggestedthat large quartzite boulders in the southern part of thetype area were derived from the basal Finlayson Memberof the Juderina Formation (Yerrida Group) Martin (19941998) recognized two polymictic conglomerate intervalsin the type area which included silicified dolomite clastsThese intervals are similar to the polymictic conglomerateand sandstone of the Heines Member defined on BRYAH
(Pirajno and Occhipinti 1998) Siltstone forms a distinctmappable upper unit along the gradational contact withthe Robinson Range Formation
Beatty Park and Heines Members
The Beatty Park Member outcrops in the Mount Padburyarea on PADBURY and contains clastic rocks that werepossibly sourced at least in part from the mafic volcanicrocks of the underlying Narracoota Formation (BryahGroup) with sedimentary chert lenses towards its top Asensitive high-resolution ion microprobe (SHRIMP)UndashPb date obtained from detrital zircons in one of these
chert lenses suggests a maximum age of 1996 plusmn 35 Ma(Nelson 1997) The clastic rocks of the Beatty ParkMember are dominated by metamorphosed chloritendashquartzshale siltstone and wacke several conglomeratic orbreccia lenses and finely laminated chert layers in places(Occhipinti et al 1997) The contact between the BeattyPark Member and the overlying Robinson RangeFormation is gradational with chloritic siltstone and chertlayers and lenses grading into sericitendashquartz siltstone Thelower contact of the Beatty Park Member with theWilthorpe Formation appears to be gradational in the areawest of the Fraser Synclinorium (see Structure) whereferruginized kaolinitic siltstone and quartz wacke gradeinto chloritic siltstone In this area the minimum thicknessof 470 m is implied because the upper part of the BeattyPark Member is not exposed
The shalendashsiltstone layers are well bedded to finelylaminated and consist of quartz and chlorite with minorsericite epidote feldspar titanite and detrital hornblendeThese layers are accompanied by very fine grainedrecrystallized white chert beds in the upper part of theBeatty Park Member West of the Fraser Synclinoriumsedimentary structures such as bedding-parallel lamin-ations flame structures and contorted bedding can beobserved within chloritic siltstone Two types of wackeunits are present one containing quartz dolomite chloritefeldspar sericite epidote sphene and opaque minerals(either magnetite or pyrite) and the other containingquartz feldspar muscovite epidote chlorite carbonateand opaque minerals Lithic fragments in wacke layersinclude metabasalt and mafic schists in which leucoxenepseudomorphs of iron oxides can still be recognizedLenses of coarse-grained lithic wacke and conglomeratecomprise rock fragments of basalt mafic schist chertchloritendashquartz wacke and coarse detrital grains (quartzfeldspar) in a sericitendashchloritendashquartz matrix Coarseclastic rocks fill channels that cut into the fine-grainedrocks and contain numerous rip-up clasts This suggeststhat at least in part the Beatty Park Member wasdeposited distally from the source region Locally whitechert lenses crosscut erosional contacts indicating that thechert is diagenetic or epigenetic
Within all rocks of the Beatty Park Member sericiteand muscovite are of metamorphic origin They replacechlorite in the fine-grained chloritic shalendashsiltstone layersand feldspar clasts in the wacke units In several examplesfine-grained muscovite has grown along late cleavageplanes
A quartzndashchloritoidndashsericitendashchlorite(ndashsulfide) unitpreviously interpreted to be a carbonate intrusion (Lewis1971 Elias and Williams 1980) has been assigned to theBeatty Park Member The chloritoid is crystallized insprays and displays a lsquobow-tiersquo texture The presence ofabundant chloritoid indicates that this rock has a highalumina content implying either a pelitic precursor or thatthe protolith was extensively metasomatized
The Heines Member consists of an upward-finingsuccession of sedimentary rocks with a polymicticconglomerate at its base followed by clastic sedimentaryunits (sandstone to shale) The type area is near Durack
20
Pirajno et al
Well on BRYAH At this locality the Heines Memberis folded into a syncline and its southern limb is in faultedcontact with the underlying Narracoota Formation Thenorthern contact is obscured here by the Cainozoic coverThe Heines Member includes those outcrops south of theRobinson Syncline at the Heines Find prospect RandellBore and 35 km northwest of Durack Well which werepreviously mapped as lsquoWilthorpe Conglomeratersquo byGee (1987) The succession is approximately 600 mthick although basal units may have been shearedoff along the faulted contact The basal polymicticconglomerate contains clasts of mafic lithic wackelimestone quartz arenite and hematitic shale supportedby a carbonate matrix This is followed upward by a seriesof sandstonendashshale units with the shale componentbecoming volumetrically greater with stratigraphic heightThe basal conglomerate of the Heines Member containsno volcanic clasts of the underlying Narracoota Formationand this is taken as evidence that the contact with the latterformation is tectonic The provenance of the various clastsin the basal conglomerate is not known In the Heines Findprospect area the Heines Member is overlain by theRobinson Range Formation
Robinson Range Formation
The Robinson Range Formation forms elongate outcropsthat extend from east to west in the centre of the BryahndashPadbury Basin and in a northerly direction on the easternmargin of the Yarlarweelor gneiss complex on MILGUN andPADBURY (Plate 1) The Robinson Range Formation isdefined by the appearance of ferruginous or hematiticshale followed by two iron formations mdash a well-definedlower banded unit separated by 100 m of ferruginousshale from an upper unit with clastic textures as mappedby Gee (1987) which is in turn overlain by hematitendashchlorite siltstone The Robinson Range Formation isconformably overlain by the Millidie Creek Formation
The Robinson Range Formation consists of asuccession of BIF siltstone and iron-rich shale Granulariron formation is present as irregular lenses The BIFconsists of laminae up to 3 cm thick These laminationscomprise various amounts of quartz iron oxides (hematiteor magnetite) biotite and locally ferro-actinolite Theshale and siltstone consist of fine-grained sericite quartzchlorite iron oxides and in a few places minor spheneThe mesostructure microstructure and petrology ofthe BIF are relatively simple Microbands or laminae lessthan 1 to 2ndash3 mm thick are made up of alternatingmicrocrystalline quartz(ndash iron oxides) greenndashbrownbiotite(ndash iron oxides) quartz grains(ndash acicular crystals ndashiron oxides) quartz grains(ndash iron oxides ndash biotite ndashacicular crystals) Commonly the quartz grain(ndash acicularcrystal) assemblage displays a polygonized texturesuggestive of annealing due to metamorphism Theacicular crystals are weathered to iron oxides but onthe basis of their morphology they could be eitherstilpnomelane crystals or amphiboles The iron oxides areeither hematite or magnetite Incident light microscopyreveals that a primary titaniferous magnetite is replacedby hematite which in turn is replaced by goethite in thesupergene environment The biotite is porphyroblastic and
mostly grown under conditions of peak metamorphism(see Metamorphism)
Granular iron-formation is characterized by a granulartexture and the presence of elongate peloids 1 to 4 mmlong The peloids consist of microcrystalline chert outlinedby rims of iron oxides (hematite with inclusions ofilmenite) The chert peloids are enclosed in finemicrocrystalline cherty or chalcedonic material Thepeloids and chert make up bands approximately 1 to15 cm thick with occasional laminae of fine chert(ndash ironoxides)
The ferruginous shale is composed of silt-sized quartzgrains and iron oxides with abundant interstitial biotiteand minor disseminated euhedral tourmaline crystals Thetourmaline was formed either during metamorphism or ahydrothermal event
The iron formations of the Robinson Range Formationhave been correlated with the granular iron-formation ofthe Frere Formation (Earaheedy Basin) 150 to 450 km tothe east-southeast by Hall and Goode (1978) whocompared them to those of the Lake Superior region inNorth America
Millidie Creek Formation
The Millidie Creek Formation defined by Barnett (1975)and modified by Gee (1979) and Occhipinti et al (1997)forms comparatively small outcrops in the cores of theRobinson Syncline and Fraser Synclinorium (seeStructure)
Ferruginous shale and siltstone intercalated withirregularly banded manganiferous iron-formation formsthe basal unit of the formation This unit is locallylateritized and hosts many manganese deposits suchas the Millidie (or Elsa) mine (see Mineralization)The banded manganiferous iron-formation commonlyforms low ridges On PADBURY the Millidie CreekFormation consists of iron-rich shale and siltstoneirregularly banded manganiferous iron-formationdolomitic sandstone ferruginous quartz wacke andchloritic siltstone On BRYAH the Millidie Creek Formationconsists of ferruginous shales with a well-developed pencilcleavage sandstone and minor granular iron-formation
Dolomitic sandstone and quartz wacke are locallypresent within this formation The quartz wacke is wellbedded matrix supported and commonly containssubangular to subrounded quartz grains The matrix of thisrock is composed of randomly oriented fine-grainedbiotite and includes late sphene and minor sericite Thedolomitic sandstone comprises carbonate quartz andmuscovite
In low hills 3 km north of 5 Mile Well (Plate 1) finelybedded micaceous siltstonendashshale with interbeddedquartzndashdolomite siltstone layers previously assigned to theLabouchere Formation (Elias et al 1982) have beenassigned to the Millidie Creek Formation These rocks arefolded about northwesterly trending D4 fold axes andcontain S4 foliation They are unconformably overlain by
21
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
subhorizontal to shallowly dipping basal quartz arenite ofthe Bangemall Group
Chloritic siltstone at the top of the Millidie CreekFormation is compositionally similar to the Beatty ParkMember and comprises quartz feldspar lithic fragmentsof sericitendashquartz schist and detrital cordierite grains ina foliated matrix of chlorite
Unassigned units of the Padbury Group
Metasedimentary rocks and biotitendashsericite schist whichoutcrop within the Despair Granite near the Wilthorpegold mine (Plate 1) were previously referred to aschloritendashmuscovitendashquartz schist and not assigned to anygroup (Elias et al 1982) Occhipinti and Myers (1999)tentatively assigned these units to the Padbury GroupThere are two main outcrops one in the Wilthorpe mineand the other just outside the mine as a fault-boundedinclusion within the granite
Sedimentary rock found within the Despair Graniteis heterogeneously deformed and metamorphosedSedimentary structures such as cross-bedding andbedding-parallel laminations are present This rockconsists of alternating layers of very fine grained biotitequartz sericite and feldspar Accessory minerals includeopaque minerals In a few places this rock contains afoliation parallel to faults or fold-axial planes Opaqueminerals commonly crosscut the dominant (bedding)fabric The preservation of the primary sedimentarytextures suggests that strong deformation did notaccompany low-grade greenschist-facies metamorphism ofthese rocks
Within the Wilthorpe mine the metasedimentary rockscontain a slightly different mineralogy and are in faultedcontact with the sericitized Despair Granite For instancein one sample there are two distinct layers composed ofeither sericite quartz biotite and opaque minerals orbiotite sericite quartz and minor opaque minerals Thisvariation in bedding composition is consistent with thatobserved in the metasedimentary rocks outcroppingoutside the mine The rocks within the mine are coarsergrained and comprise quartz biotite sericite andandalusite Sericite and biotite overprint the foliation inthe rock
StructureThe Padbury and Bryah Basins are pervasively deformedThis deformation may have solely occurred duringthe c 18 Ga Capricorn Orogeny a period of obliquecollision between the Archaean Pilbara and YilgarnCratons (Tyler and Thorne 1990 Tyler et al 1998Fig 2) or in part during the earlier c 20 Ga GlenburghOrogeny (Occhipinti et al 1999) In addition to deformingthe Bryah and Padbury Groups this deform-ation also resulted in the reworking of parts of theArchaean Narryer Terrane and the Marymia Inlier of theYilgarn Craton (Fig 2) to form the Yarlarweelor gneisscomplex and Peak Hill Schist The rocks of the Bryah
and Padbury Groups are locally interleaved with theYarlarweelor gneiss complex in the western part of theregion (Fig 18) To the south the Bryah and PadburyGroups are tectonically juxtaposed against autochthonousrocks of the Archaean Murchison Terrane of the YilgarnCraton and the Palaeoproterozoic Yerrida Group (Fig 2)
The Yarlarweelor gneiss complex dominantly consistsof Archaean granitic gneisses that were intruded by felsicmagmas at c 1960 Ma (Sheppard and Swager 1999) and1820ndash1800 Ma (Occhipinti et al 1998b Sheppard andSwager 1999) Granite sheets and veins intruded into theArchaean gneisses were pervasively deformed into opento tight folds and metamorphosed at medium to highgrades during the Capricorn Orogeny Occhipinti andMyers (1999) suggested that these folds were originallynortherly trending however they are probably more likelyto have been northeasterly trending Dextral strike-slipshear movement involved a transition from early ductileto later brittle deformation (Occhipinti et al 1998b)coincident with uplift which probably progressed fromnortheast to southwest in the region This deformationproduced regional-scale fault-bend folds in both theYarlarweelor gneiss complex and overlying Palaeo-proterozoic Bryah and Padbury Group rocks
Deformation histories presented for the Yerrida Bryahand Padbury Groups by various authors (including Windh1992 and Gee 1990) have many elements in common(Table 5) This includes major northndashsouth compressionthat was responsible for the development of prominentregional easterly trending upright folds such as theRobinson Syncline (Fig 18) Northerly striking folds andfaults in the domain just east of the Yarlarweelor gneisscomplex have been recognized as a later deformation stage(Windh 1992 Martin 1994) Gee (1990) Windh (1992)and Martin (1994) proposed that eastward movement ofthe Narryer Terrane (here referred to as the Yarlarweelorgneiss complex) was responsible for the development ofthese northerly trending folds In their interpretation thenortherly striking folds formed in front of an advancingthrust sheet of Archaean gneiss and granite overriding theBryah and Padbury Groups Myers (1989 1990) andMyers et al (1996) on the other hand regarded the Bryahand Padbury Groups as allochthonous sheets that werethrust over Archaean granitendashgneiss
Contacts of the Bryah and Padbury Groups with theNarryer Terrane Yarlarweelor gneiss complex MarymiaInlier Murchison Terrane and the PalaeoproterozoicYerrida Group are zones of high strain and thereforeinferred to be faults Unconformable contacts between theBryah and Padbury Groups were reported by Martin(1994 1998) whereas sheared and faulted contacts werereported by Pirajno and Occhipinti (1998) Occhipintiet al (1998ac) and Occhipinti and Myers (1999) Forexample the Bryah Group is in faulted contact with theYarlarweelor gneiss complex north of Livingstones Findand the Murchison and Narryer Terranes are separatedfrom the Bryah and Padbury Groups by the steep easterlytrending Murchison Fault which has a sinistral strike-slipcomponent (Plate 1 Fig 2)
The Goodin Fault a high-angle reverse fault (Pirajnoand Occhipinti 1998) is the boundary between the
22
Pirajno et al
Yerrida and Bryah Groups (Fig 2 Plate 1) East of thisfault the Doolgunna Formation (Yerrida Group) is foldedinto isoclinal upright folds however much of thedeformation in the Yerrida Group dies out rapidly to theeast and southeast To the west the Goodin Fault mergeswith the Murchison Fault which has juxtaposed the Bryahand Padbury Groups against the Yilgarn Craton TheMurchison Fault has a sinistral strike-slip componentwhich offsets Archaean structures in the Murchison andNarryer Terranes
In this Report four distinct groups of structuresD1ndashD4 representing progressive compressional deform-ation are recognized (Table 5) This deformation historyalthough in broad agreement with the previously publishedstructural histories (eg Windh 1992) recognizes separateearly layer parallel structures The structures resultingfrom the four deformation events are not developedeverywhere or with the same intensity everywhere
The earliest deformation events are defined in the PeakHill Anticline area as D1 layer-parallel mylonitic thrustfaults and originally subhorizontal folds overprinted byD2 upright eastndashwest striking regional folds Both D1 andD2 structures developed by northndashsouth compression and
can be interpreted as successive stages of progressivedeformation Northerly trending regional D3 folds andupright foliations recording eastndashwest compression areweakly developed in the Peak Hill Anticline but betterdeveloped and largely restricted to a domain immediatelyeast of the Yarlarweelor gneiss complex However thesenortherly trending structures do not always overprint oldereasterly trending structures and in places these two setsof structures (D2 and D3) tend to be mutually exclusivesuggesting that they probably developed during the sameprogressive deformation event Late medium-scale D4structures include west-northwesterly to northwesterlytrending subvertical foliations shear zones zones ofsmall-scale folding and faults now outlined by quartzblows These locally developed structures suggest latenorth-northeast to south-southwest compression
Major fold structures in the Padbury and Bryah Basinsare the Peak Hill Anticline Robinson Syncline MillidieSyncline Fraser Synclinorium Horseshoe Anticline andPadbury Syncline (Plate 1 and Fig 18) The Peak HillAnticline Robinson Syncline Fraser Synclinorium andMillidie Syncline all represent refolded folds The easterlytrending doubly plunging Robinson Syncline andPeak Hill Anticline are D2 folds refolded during D3 D1
Figure 18 Major regional structures in the Bryah and Padbury Groups (after Occhipinti et al 1998a)
FMP371
MARYMIAINLIER
YILGARNCRATON
Goodin
Fault
GROUPBANGEMALL
Murchison Fault
118deg30 119deg30
30 km
020300
YERRIDAGROUPPeak Hill
Anticli
ne
Robinso
n
Synclin
e
Nathan Syncline
Zone of D folding3
Padbury
Horseshoe Anticline
Wilthorpe F
t
BRYAH ANDPADBURYGROUPS
GOODININLIER
EARAHEEDYGROUP
25deg30
26deg00
Syncline
Millidie Syncline
FaultD fold trace3
D fold trace2
1
D fault1
Anticline
SynclineD ndash D thrust fault2
Yarlarweelorgneiss
complex
FraserSynclinorium
23
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
folds are also present within these structures (see D1structures) The Horseshoe Anticline appears to be a D3fold contained within the fault-bounded Horseshoeanticlinal block This fault-bounded block also appears tobe cut by northwesterly trending (D4) faults
D1 structuresThe first Palaeoproterozoic deformation event (D1)produced layer-parallel folds a locally pervasive S1schistosity mylonites and faults However because thesestructures were pervasively overprinted by D2 structuresthey are rarely observed F1 folds are locally observed inthe Peak Hill Antiform Robinson Syncline FraserSynclinorium an area 5 km northeast of Mount Fraserand the Millidie Syncline These folds are also observednear the Peak Hill mine in F2 foldndashhinge zones of quartzblastomylonites of the Peak Hill Schist (Fig 6) Here theyare small-scale rootless isoclinal plunge shallowlytowards the east and strike eastndashwest In the FraserSynclinorium and Millidie Syncline the F1 folds are small-scale isoclinal folds that plunge gently towards the east-northeast or west-southwest and strike east-northeasterlyF1 folds are also inferred from aeromagnetic data to bepresent within the Fraser Synclinorium and MillidieSyncline (Figs 18 and 19)
The Goodin and Murchison Faults may be D1 faultsthat were reactivated during D2 (Occhipinti et al 1998c)The Murchison Fault (Figs 18 and 19 Plate 1) separateslargely undeformed basaltic hyaloclastite rocks in thesouth from foliated mafic schists to the north
Mesoscale F1 folds in the shale and banded iron-formation of the Robinson Range Formation are observednear Mount Padbury north-northwest of Beatty Park Bore
(Plate 1) in the hinge zone of the Robinson Synclinenorth of Tank Well and northeast of Randell Bore TheseF1 folds are tight to isoclinal with shallow plunges thattrend to the east or west The F1 folds in the area areinterpreted as originally recumbent D1 zones of highstrain and mylonite developed locally mainly in thePeak Hill Schist (Pirajno and Occhipinti 1998) andalong contacts between the Yarlarweelor gneiss complexand Palaeoproterozoic cover rocks These mylonite zonesare not observed at higher stratigraphic levels within thebasin suggesting that they are restricted to a deeper crustallevel represented by the Peak Hill Schist and basementndashcover contacts Quartz blastomylonites and the CrispinMylonite (Pirajno and Occhipinti 1998) form continuousunits within the Peak Hill Schist (Plate 1) The internalstructure of these units suggests that they may be D1shear zones which were refolded during the laterdeformation events The original nature and orientation ofthese shear zones is not known The Crispin Myloniteconsists of quartzite pebble-and boulder-sized clasts in asericitendashquartz-rich matrix and has the appearance of aconglomerate For that reason it was mapped by Gee(1987) as the lsquoCrispin Conglomeratersquo However meso-scopic and microscopic structures indicate that it is amylonite (Figs 4 and 7) Both the quartzite clasts andmatrix contain a mylonitic fabric The Crispin Myloniteis interpreted as a lsquopseudo-conglomeratersquo (Raymond1984ab) formed by shearing probably along or close toa fault plane that separated an arkosic or granitic unit froma quartz-rich unit
Like the Crispin Mylonite the quartz blastomylonitesform arcuate lenses within quartzndashmuscovite schist of thePeak Hill Schist and are refolded by F2 and F3 folds Thequartz blastomylonites contain isoclinal and sometimesrootless F1 folds and are interpreted to have beendeformed in a ductile high-strain zone (fault or shear zone)during D1 It is not possible to determine the sense ofmovement during D1 because no shear sense indicatorswere observed during mapping
D2 structuresThe D2 deformation produced large-scale uprightregional F2 folds with variably developed S2 foliationas well as faults and shear zones These structuresare easterly trending recording northndashsouth shorteningHowever more complex patterns in the Mount Fraserarea suggest complicated refolding patterns ProminentD2 folds include the doubly plunging Robinson Synclineand the Padbury Syncline which has the hinge zonelargely sheared out (Fig 18 Plate 1) Mesoscale F2folds show steeper plunges and the S2 foliation becomesmore intense to the north A pervasive S2 foliation isdeveloped over large areas in the mafic schists ofthe Narracoota Formation The Goodin Fault is a high-angle reverse fault that forms the boundary between theYerrida and Bryah Groups This fault may have developedduring D2 because south of the fault the DoolgunnaFormation is folded into tight to isoclinal upright folds(with fold-axial surfaces subparallel to the Goodin Fault)that are similar to D2 folds in the Bryah and PadburyBasins
Table 5 Sequence of deformation events in the Bryah and PadburyBasins
Deformation Compressionevent
D4 North-northeastndashsouth-southwest compressionSmall-scale folds subvertical foliation shearzones faults with quartz blows all trending
280degndash310deg
D3 Eastndashwest compressionnorthndashsouth trending folds subvertical foliationsubvertical faults or shear zones localized eastof Narryer Terrane increasingly disharmoniceast-northeasterly trending folds eastwards
D2 Northndashsouth compressionupright tightndashisoclinal eastndashwest folds andsubvertical foliation eastndashwest shear zonessouth-verging thrust faults
D1 Northndashsouth compressionsubhorizontal mylonites thrusts and foldsmesoscale recumbent folds tightndashisoclinalrootless
24
Pirajno et al
The Livingstone Synform a steep easterly plungingtight fold on MOORARIE may be part of a larger scale D2fold structure that is confined between the Kerba Fault inthe north and the Mount Seabrook Fault in the south(Occhipinti and Myers 1999)
Within the Yarlarweelor gneiss complex graniticgneisses form open to isoclinal easterly to northeasterlyand northerly trending shallowly to steeply plungingfolds These folds plunge either to the east and northeastor to the west and west-southwest indicating that on a
Figure 19 Simplified geological map of the Bryah and Padbury Groups (after Occhipinti et al 1998a) See Figures20 22 and 23 for cross sections
118deg 119deg
25deg45
10 km
MarymiaInlier
YilgarnCraton
BangemallBasin
Bill
ara
Fa
ult
Wilt
horp
eF
Fortnum
25deg30
Goo
din
Faul
t
Kinders FaultNathan
Peak Hill
B
AC
Mt Fraser
Yarlarweelor gneisscomplex
(reworked NarryerTerrane)
YerridaBasin
PADBURY GROUP
BRYAH GROUP
RAVELSTONE FORMATION lithic wacke
KARALUNDI FORMATION clastic rocks
quartzndashmuscovitendashbiotitendashstaurolite schist
HORSESHOE FORMATION shale banded iron-formation
YERRIDA GROUP
WILTHORPE FORMATION conglomerate siltstone
PA
LA
EO
PR
OT
ER
OZ
OIC
Greenstone
Peak Hill Schist
AR
CH
AE
AN
Fault
Anticline
Syncline
ME
TA
MO
RP
HO
SE
D
NARRACOOTA FORMATION maficndashultramafic volcanic rocks
LABOUCHERE FORMATION quartz wacke siltstone
Unconformity
Mine
Cross-section
Undifferentiated rocks
MILLIDIE CREEK FORMATION Lithic wacke dolomitic sandstone siltstone banded iron-formation
Granite and graniticgneiss
ROBINSON RANGE FORMATION shale granular iron-formation banded iron-formation
140300FMP373
25
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
regional scale they are doubly plunging possiblyrecording later refolding and eastndashwest shortening (D3)These folds deform both the Archaean gneiss and c 1960and c 1820 Ma granite sheets that intruded the gneiss(Sheppard and Swager 1999 Occhipinti et al 1998c)They refold tight to isoclinal subhorizontal to shallowlyplunging folds in the Archaean granitic gneisses whichmay have developed during the Archaean
The sense of shear of the steeply dipping D2 shearzones could not be determined South of the Robinson andFraser Synclines regional anastomosing D2 shear zonesdeveloped in the basaltic rocks of the NarracootaFormation To the northeast this regional structurebecomes the Jensen Fault (Pirajno and Adamides 2000)which can be shown to have displaced the Meso-proterozoic Bangemall Group suggesting that the faultwas reactivated after this time Along the southern limbof the Fraser Syncline another fault extends into the D2shear zones mentioned above A shear zone cuts thesouthern limb of the Heines Syncline which lies betweenthe Robinson and Fraser Synclines
D3 structures and theirrelationship to D2 structuresNortherly trending D3 folds faults and locally an uprightS3 foliation indicating an eastndashwest compression are welldeveloped in the area east of the Yarlarweelor gneisscomplex Further east F3 fold intensities decrease andfolds are locally more disharmonic The D3 event wasresponsible for the doubly plunging nature of theRobinson Syncline and the Peak Hill Anticline
The Kinders Fault (Fig 20 Elias and Williams 1980)is a northerly trending D3 fault separating a wedge ofmafic volcanic schists of the Narracoota Formation(Bryah Group) from the Robinson Range Wilthorpeand Labouchere Formation rocks (Padbury Group) Thisfault lies along the western limb of the sheared-out hingeof the F3 Nathan Syncline (Plate 1 and Fig 18) Thissyncline was previously correlated with the PadburySyncline to the south (Elias and Williams 1980 Martin1994 1998) Part of the southerly plunging fold hingeof the Nathan Syncline is preserved in the Nathan minearea and the closure of this syncline can be traced furthernorth The wedge of maficndashultramafic schists of theNarracoota Formation was interpreted by Occhipinti et al(1998c) and Martin (1994 1998) to represent an F3anticlinal fold-thrust wedge overlying pervasively foliatedand metamorphosed quartz wacke of the LabouchereFormation to the west (Figs 19 and 20)
West of the Kinders Fault along the Billara Faultsericitendashquartz schist locally with quartz-pebbleconglomerate layers contains a pervasive S3 fabricF3 folds however are difficult to trace East of theKinders Fault open to close and locally tight to isoclinalfolds are outlined by marker beds in the Labouchere andHorseshoe Formations S3 foliations and moderate tosteep southerly plunging small-scale F3 folds are welldeveloped in the area of the Horseshoe Syncline andfurther north
Several observations suggest that D2 and D3 structuresmay not reflect two separate events but may havedeveloped contemporaneously in different domainsIntense D3 folding is largely restricted to the area betweentwo basement highs represented by the Yarlarweelorgneiss complex in the west and the Peak Hill Schist in theeast (Figs 18 and 19) In the domain just east of andadjacent to the Yarlarweelor gneiss complex there is noevidence for D3 refolding D2 (ie upright northerlytrending D3 folds overprinting upright easterly trending D2folds) even though weak northerly trending D3 foldsdeform easterly trending F2 folds around and within thePeak Hill Anticline
In the Mount Fraser area complex fold and foliationpatterns show orientations different from and transitionalto both the regional D2 and D3 deformation Large-scaleeast-northeasterly trending F2 folds such as the RobinsonSyncline and Peak Hill Anticline die out in this area TheMillidie Syncline can be traced from a west-northwesterlystrike (subparallel to and en echelon with the RobinsonSyncline) to a west-southwesterly strike and is then cutoff to the south by D3 faults (Figs 18 and 19)
These observations suggest that the intensity and trendof the D2 and D3 structures were influenced by their spatialrelationship to the Yarlarweelor gneiss complex and PeakHill Schist
D4 structuresD4 structures include mesoscopic chevron folds kinksshear zones and faults and were locally accompanied bythe development of a foliation These D4 structuresdeveloped locally throughout the Bryah and PadburyBasins Yarlarweelor gneiss complex and the northern-most part of the Murchison Terrane In the PadburyndashBryahdomain most structures trend between west-northwest andnorthwest although in the Yarlarweelor gneiss complexa few late structures trend between north-northwest tonorth Brittle faults cutting the Yarlarweelor gneisscomplex often show dextral strike-slip shear movement
MetamorphismRegional metamorphic zones within the volcano-sedimentary succession are related to the geometry of thePeak Hill Anticline and Yarlarweelor gneiss complex Thehighest metamorphic grade assemblages are found in thecontact zones between the Yarlarweelor gneiss complexand overlying metasedimentary rocks Assemblages inthe Peak Hill Schist and within quartzndashmica schists(Labouchere Formation) along faulted contacts withthe Yarlarweelor gneiss complex record upper greenschist-to lower amphibolite-facies conditions Within theYarlarweelor gneiss complex upper amphibolite-faciesconditions were reached as incipient (minimum) meltpatches within granitic gneiss and amoeboid textures inPalaeoproterozoic coarse-grained granite probablydeveloped during D2 (Sheppard and Swager 1999) In theBryah and Padbury Groups however metamorphismtypically does not exceed greenschist facies and east of
26
Pirajno et al
0
2
4
6
Fault
Kilo
met
res
Southwest Northeast
FMP372
0
2
4
6
Kilo
met
res
West East
Billara
Fault
Kilo
met
res
0 Padbury
South North
SynclineDome
2
4
6
Yarlar-weelor
170300
Fault
Kinders
MIDDLE PROTEROZOIC
ARCHAEAN (reworked during Early Proterozoic)
Bangemall Group
Unconformity
Bedding or layering trend
Foliation
High-strain zone
Fault
Movement along fault
Movement away and towards observer
2
BRYAH GROUP
Geological boundary
Padbury Basin
Bryah Group
S N
d)
sediment fluxsediment flux
EARLY PROTEROZOICPADBURY GROUP
ARCHAEAN (in situ)
Peak Hill Schist quartzndashmuscovite schistquartz mylonite phyllonite
Granitendashgreenstone Murchison Terrane
Millidie Creek Formation sandstoneshale dolomitic siltstone
Robinson Range Formation ferruginous shalebanded iron-formation
Wilthorpe Formation quartz-pebbleconglomerate
Labouchere Formation quartz wackesiltstone quartz arenite
Horseshoe Formation ferruginous shaleiron formation
YERRIDA GROUP
Narracoota Formation metabasalt subordinatedolerite picrite and peridotite
Goodin
Normal fault reworked during D thrusting
Granite gneiss and granite with lenses of supracrustal rock Narryer Terrane
GranitendashgreenstoneMarymia Inlier ndash Murchison Terrane
Ravelstone Formation lithic wacke
Karalundi Formation clastic rocks
a) Cross section A
b) Cross section B c) Cross section C
Undifferentiated rocks
27
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
the Goodin Fault in the Yerrida Group metamorphic gradedecreases to subgreenschist facies (prehnitendashpumpellyite)The relationships between metamorphic mineral growthand deformation are summarized in Table 6
M1 was a prograde regional metamorphic event thattypically reached greenschist facies (Pirajno andOcchipinti 1998) and was probably coincident withD1 in the Bryah and Padbury Groups and Peak Hill SchistThornett (1995) suggested that some parts of the Peak HillSchist reached amphibolite-facies metamorphism withtemperatures between 500deg and 620degC and pressures of65 ndash 7 kbar Metamorphic mineral assemblages observedhowever commonly do not concur with these data Thesecond metamorphic episode M2 was commonly one ofretrogression throughout most of the Bryah and PadburyBasin and probably associated with metasomatismin high-strain zones during D2ndashD3 During M2 inthe western part of the Bryah and Padbury Basinsadjacent to the Billara Fault (Fig 18) staurolitendashandalusitendashbiotitendashmuscovitendashquartz schist developedfrom the metamorphism of Padbury Group sedimentaryrocks These rocks indicate metamorphism at amphibolitefacies Inclusion trails in staurolite and andalusiteporphyroblasts suggest that the porphyroblastic growthoccurred after D1 but before D2 The S2 foliation is definedby the alignment of muscovite and biotite which wrapsaround the porphyroblasts and probably developed in D2during M2 As staurolite is locally partially replaced byfine-grained muscovite this foliation may have developedin the greenschist facies This foliation is locallyoverprinted by chloritoid Further west at the contactbetween the Palaeoproterozoic Kerba Granite and theNarracoota Formation a quartzndashkyanitendashtremolitendashfeldspar schist indicates upper greenschist-faciesmetamorphism with the pressure of metamorphismestimated to have been between 3 and 4 kbar (Spear 1993Occhipinti and Myers 1999)
For the most part M2 involved retrogression meta-somatism and local hydrothermal alteration Mineralassemblages formed during M2 are commonly observedin high-strain zones where the S2 schistosity is welldeveloped These include a domain of well-developed D2shear zones south of the Robinson Syncline wherepervasive retrogression of metabasalts to actinolitendashchlorite schist is observed (Pirajno et al 1995a) In
addition in the Mount Pleasant opencut growth of albiteporphyroblasts and the development of chlorite at theexpense of biotite and epidote also occurred during M2
Banded iron-formation in the Robinson RangeFormation shows a change in metamorphic mineralassemblage from east to west across the trend of the D2Robinson Syncline To the west randomly oriented biotiteoverprinted quartz stilpnomelane and iron oxides Theappearance of this late-stage biotite coincides withregional geochemical trends (elevated Sb As and WDavy et al 1999) along the same structure suggesting alate- or post-D2 low-temperature metasomatic eventAlbite porphyroblasts in alteration zones associated withgold mineralization in the Peak Hill Schist also grew at alate stage because they overprint S2
South of the Murchison Fault little-deformed basaltichyaloclastites contain mineral assemblages characteristicof prehnitendashpumpellyite to lower greenschist facies Thissuggests that rocks south of the Murchison Fault were notexposed to the regional greenschist-facies metamorphismor moderate- to high-grade metamorphism that occurredelsewhere in the region
Structural synthesisA number of models have previously been presented toexplain the structural and metamorphic history of theBryahndashPadbury region For these models the driving forcewas assumed to be collisional tectonics related to theCapricorn Orogeny (eg Tyler et al 1998 Occhipintiet al 1998c Pirajno et al 1998b)
Gee (1990 p 207 Gee and Grey 1993) interpretedthe movement of the lsquoYarlarweelor Gneiss Beltrsquo andlsquoMarymia Domersquo in terms of rising lsquosolid-state crystalndashplasticrsquo domes They suggested that the resulting rise andsouthward movement of the lsquoYarlarweelor Gneiss Beltrsquoand lsquoMarymia Domersquo produced recumbent folds in theoverlying sedimentary rocks of the Bryah Basin Furtherrise and convergence of the domes following depositionof the Padbury Group caused complex refolding ThelsquoYarlarweelor Gneiss Beltrsquo was thrust to the east overthe Bryah and Padbury Groups at this time Martin(1994) interpreted the emplacement of the lsquoNarryer
Figure 20 Selected idealized cross sections through the Bryah and Padbury Groups (after Occhipinti et al 1998a) Locationsof a) to c) are shown on Figure 19 (note difference in scale)a) Northeastndashsouthwest section in the central-eastern part of the Bryah and Padbury Basins showing the fault-bendfold model for the Peak Hill Anticline and inferred suture between the Yilgarn Craton (Murchison Terrane) andreworked Archaean Marymia Inlier The extensional fault slice along the northern margin of the craton formed duringearly development of the Bryah Basin (lsquopassive marginrsquo) and was preserved in this idealized section after basinclosureb) Eastndashwest section across the zone of D3 fold and fault structures The section highlights the intense deformationacross the zone between the Billara and Kinders Faults and shows an inferred major detachment (within underlyingmafic volcanic rocks of the Narracoota Formation) zone of highly disharmonic F3 folding mapped at the surfacec) Northndashsouth section in the central-western part of the Bryah and Padbury Basins showing the Yarlarweelor Domethe sheared-out Padbury Syncline and the Murchison Fault as the suture between in situ and reworked ArchaeanNarryer Terrane Note the inferred detachment of the BryahndashPadbury succession along the contact with the NarryerTerraned) The development and onlap of the Padbury Basin onto the underlying Bryah Group
28
Pirajno et al
Gneiss Complexrsquo (lsquoYarlarweelor Gneiss Beltrsquo) as due tolsquolateral escape tectonicsrsquo resulting from the lsquotranscurrentsuturingrsquo of the Yilgarn and Pilbara Cratons during theCapricorn Orogeny Martin (1994) suggested that earlynorthndashsouth movements which changed to localized eastndashwest movements indicate the onset of lsquolateral escapetectonicsrsquo and the eastward expulsion of the northeasternpart of the lsquoYarlarweelor Gneiss Beltrsquo along the Wilthorpeand Kinders Faults In contrast Myers (1989 1990)regarded both the lsquoYarlarweelor Gneiss Beltrsquo and thevolcano-sedimentary rocks of the Bryah and PadburyGroups as allochthonous sheets that were thrust over the
Yilgarn Craton basement and subsequently folded abouteastndashwest axes
An alternative model was presented by Occhipintiet al (1998c Fig 21) who suggested that the Bryah Basindeveloped initially as a rift and the Padbury Basindeveloped over the Bryah Basin in a retroarc foreland-basin setting (see also Martin 1994) Formation of thePadbury Basin in a compressional regime was essentiallyconcommitant with the closure of the Bryah Basin and thedevelopment of D1 structures as subhorizontal shear zonesbetween the Archaean Narryer Terrane basement and the
Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group anddeformation fabrics
Formation Rock type Mineralogy Pre-S1 S1 Post-S1 S2ndashS3 Post-tectonicM1 M2
Peak Hill Schist pelite quartz biotite muscovite chlorite albite tourmaline
chemical sediment quartz spessartine magnetite
calc-silicate quartz epidote chlorite actinolite titanite magnetite
psammite quartz muscovite andesine opaques
Narracoota metabasite quartz actinolite epidote chlorite sericite arfvedsonite titanite calcite
volcanic breccia albite pumpellyite
Ravelstone pelitic tourmalinite quartz muscovite tourmaline garnet feldspar
subarkosic wacke quartz biotite albite sericite tourmaline
Horseshoe banded iron-formation quartz biotite grunerite spessartine chlorite
Robinson Range banded iron-formation quartz stilpnomelane biotite
NOTE No data are available for the Labouchere and Wilthorpe Formations
29
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
supracrustal rocks of the Bryah and Padbury Groups Theoverall movement direction was interpreted as being fromnorth to south but locally because of the possible effectof later dextral shear movement may actually have been
ram
p
Peak Hill Anticline
N S
eg Kinders Fault Peak HillAnticline
Thrust flatrsquo Lateral
ramp Obliq
ue
lateral ramp
Yarlarweelor
Basalthrustplane
2Dc)
d)
2D thrust flat
rsquo
eg Yarlarweelor gneiss complex
gneiss complex
Padbury Group
Bryah Group
Reworked Archaean granite
a)
Archaean granite
b)
2prospective D crustal thrustwith frontal ramp
1D tectonic interleaving zone(eg Peak Hill Schist)
1 2Post-D and pre-D
D tectonic interleaving between reworked Archaeancrust ( underplate) and BryahndashPadbury succession
rsquo1
Post-D D2 3
W E
Thrust ramp
Thrustfrontal
Later
al ra
mp
FMP374 011199
W E
N
Thrust flatrsquo
movement
Thrust
North to south
e)
ramprsquo
flatrsquorsquo
2D thrust flat ndash frontal ramp ndash lateral ramp geometry
Figure 21 Model of the structural development of the BryahndashPadbury Group succession (after Occhipinti et al1998a)a) Zone of D1 subhorizontal tectonic interleaving(by thrust duplexing) between reworked Archaeancrust and overlying rocks of the BryahndashPadburysuccession This zone includes high-strain ormylonitic rocks formed by lsquounderplatingrsquo of theArchaean rocks beneath the volcano-sedimentaryrocks during initial closure of the Bryah back-arcbasinb) Post-D1 geometry with trace of incipient D2crustal-scale thrust with frontal rampc) D2 geometry with fault-bend anticline developedabove the crustal D2 thrust ramp Upright folds inthe volcano-sedimentary succession (eg Padburyand Robinson Synclines) formed ahead of themain thrustd) Post-D2D3 geometry along schematic eastndashwestsection D2 fault-bend anticlines are not shownNorth-to-south movement ie movement towardsviewer leads to eastndashwest compression and hencenorthndashsouth folds and reverse or thrust faults in thedepression between (oblique) lateral ramps at thesame time as eastndashwest D2 folding occurredelsewheree) Schematic view looking north-northwest of thebasal thrust fault with frontal and lateral rampshighlighting the north-to-south movement directionof the thrust sheet
northwest to southeast Substantial movement and highstrains can be inferred from tectonic interleaving (egbetween the Billara and Wilthorpe Faults Fig 19) andfrom the development of the mylonitic zones in possiblethrust duplexes in the Peak Hill Schist Other possibleD1 structures in particular subhorizontal thrust faultsmay have locally developed along the contacts betweenthe Bryah and Padbury Groups Small-scale earlylayer-parallel folds in chert and BIF layers particularlyfrom within the Padbury Group suggest that subhorizontalD1 structures locally formed within the volcano-sedimentary succession (Pirajno and Occhipinti 1998Swager and Myers 1999) Deposition of the PadburyGroup in a retroarc foreland basin (Martin 1994)was probably contemporaneous with the early stagesof D1
The Yarlarweelor gneiss complex and Peak Hill Schistwere described by Occhipinti et al (1998c) as lsquobasement-cored anticlinesrsquo that developed above frontal thrust rampsThe overlying supracrustal rocks and their high-strain D1contact zones were folded by north to south movementover these ramps during D2 deformation In the Peak HillSchist subhorizontal D1 folds are refolded about anupright apparently easterly trending D2 antiformThe hinge of this fold may be sheared out along thecontact with the Marymia Inlier which is marked by aquartz blastomylonite previously mapped as deformedquartzite of the Juderina Formation (Adamides 1998) Theoriginal orientation of the D2 fold may have been east-northeasterly The Peak Hill Schist outcrops around adomal structure produced by refolding of the D2 fold aboutan approximately northerly trending D3 fold-axial surfaceIt was argued by Occhipinti et al (1998c) that the D3 foldsdeveloped in a structural lsquodepressionrsquo between the two
30
Pirajno et al
basement-cored anticlines which acted as lateral rampsin the thrust plane Northerly trending structures developedduring northndashsouth compression as the lateral ramps wereslightly oblique to the movement direction leading tospace problems between the basement-cored anticlinesThis resulted in either lateral shortening or verticalexpulsion (or both) of the Bryah and Padbury Groups
Occhipinti et al (1998c) assumed that the Yarlarweelorgneiss complex (referred to by them as the NarryerTerrane) was an Archaean crustal fragment that influencedthe structural deformation in the Palaeoproterozoic Bryahand Padbury Groups but was not itself largely deformedduring the Palaeoproterozoic Subsequently Sheppard andSwager (1999) and Occhipinti and Myers (1999)recognized Palaeoproterozoic deformation meta-morphism and felsic magmatism within the Yarlarweelorgneiss complex This indicates that the Yarlarweelor gneisscomplex was extensively reworked during the Palaeo-proterozoic and underwent the same D2ndashM2 metamorphicevent that has been recognized in the Bryah and PadburyGroups and Peak Hill Schist
Occhipinti et al (1998b) found that Palaeoproterozoiccoarse-grained granites and pegmatites with ages between1820 and 1780 Ma (Nelson 1998) intruded as sheetssynchronously with the D2 deformation event D McBMartin (1999 pers comm) interpreted granite exposedsouthwest of the Labouchere opencut as intruding thePadbury Group sedimentary rocks and suggested that thisgranite may also be of this age Intrusion of granitoiddykes and sheet-like plutons accompanied uplift of theYarlarweelor gneiss complex and is interpreted as beingconcomitant with dextral shearing in the region andpossibly D3 (Occhipinti et al 1998a Sheppard andSwager 1999) This movement was attributed to anoblique northndashsouth to northwestndashsoutheast collision ofthe Pilbara and Yilgarn Cratons during the CapricornOrogeny (Occhipinti et al 1998b 1999)
In the northwestern part of the Bryah and PadburyBasins the metamorphic grade increases from greenschistfacies in the east to amphibolite facies in the west Furtherwest in the Yarlarweelor gneiss complex the metamorphicgrade reached at least upper amphibolite facies (Sheppardand Swager 1999) Uplift of the Yarlarweelor gneisscomplex from 9ndash10 kbar to greenschist facies occurredbetween c 1812 and c 1800 Ma (Occhipinti et al 1998b)The c 1812 Ma granitoid sheets and dykes were meta-morphosed at high grade (see below) whereas c 1800 Magranites were only metamorphosed to greenschist facies(Occhipinti et al 1998b) Medium-grade metamorphismof the Padbury Group is solely preserved adjacent to theYarlarweelor gneiss complex between the Billara andWilthorpe Faults (see Metamorphism Fig 18 Plate 1)The drop in metamorphic grade to greenschist facies only15 ndash 25 km east of the contact suggests either a rapidincrease in temperature close to the Yarlarweelor gneisscomplex or that amphibolite-facies or upper greenschist-facies (or both) Bryah and Padbury Group rocks have beenfaulted out The latter explanation is preferred because theboundary between amphibolite-facies and lower to middlegreenschist-facies rocks of the Labouchere Formation issharp
In the Bryah and Padbury Groups and Peak Hill Schistmetasomatism accompanied retrogression of D1ndashM1assemblages to greenschist facies during M2 particularlyin D2 shear zones In the Yarlarweelor gneiss complexthere is no evidence for D1ndashM1 and M2 was initially ahigh-grade metamorphic event with the formation ofincipient minimum melt during the early stages of D2(Occhipinti et al 1998b) Post-M2 the metamorphic gradedropped significantly to greenschist facies
In the proposed model shown in Figure 22 the BryahGroup developed in a back-arc lsquorift-type settingrsquo (Pirajnoet al 1998b see Tectonic model and conclusions) If theBryah and Padbury Groups are c 20 Ga or older then D1structures could have developed during the c 20 GaGlenburgh Orogeny (Occhipinti et al 1999 Tyler 1999)as a result of west to east or northwest to southeastcompression Plutonism in the future Yarlarweelor gneisscomplex produced the 1960 Ma felsic granitoid rocksduring the late stages of D1 (Sheppard et al 1999Fig 22c) Alternatively if the Bryah and Padbury Groupswere deposited sometime between c 1945 and 1812 MaD1 could have developed during the c 18 Ga CapricornOrogeny due to north-northwest to south-southeastcompression (Figs 22 and 23) Further geochronologicalwork is required to establish the age of D1 and thedepositional age of the Bryah and Padbury Groups
In either case closure of the Bryah Basin took placeduring D1 with deposition of the Padbury Group in aretroarc foreland basin overlying the Bryah Group andpossibly the lsquofuturersquo Yarlarweelor gneiss complex(Fig 22b) D1 deacutecollements would have developedbetween the Bryah and Padbury Groups the futureYarlarweelor gneiss complex and the Peak Hill Schist(Figs 22b and 23a) Duplexes developed in the Peak HillSchist during D1 and it was detached from the MarymiaInlier (Fig 23b) In addition early D1 faults and foldsformed between and within the Bryah and PadburyGroups
The second deformation event D2 occurred during theCapricorn Orogeny Early in D2 approximately northwestto southeast compression caused further thickening of theBryah and Padbury Groups over the Yarlarweelor gneisscomplex destabilizing this piece of crust (Figs 22b and22c) The resulting increased pressure and temperaturemay have caused the underlying Archaean crust to startto melt This melt produced the c 1820 to c 1812 Mafelsic granitoid rocks (Occhipinti et al 1998a Sheppardand Swager 1999 Sheppard et al 1999) that intruded theupper parts of the Yarlarweelor gneiss complex as veinsand sheets (Sheppard and Swager 1999 Fig 22c) Asthese developed synchronously with the deformation (D2)they were commonly folded into upright steeply toshallowly plunging isoclinal to open folds These rockswere also metamorphosed at high grade during the D2deformation event Regionally this metamorphismcorresponds to M2
Padbury Group sedimentary rocks were meta-morphosed to medium grade along contact zones withthe Yarlarweelor gneiss complex during M2 This high- andmedium-grade metamorphism may have releasedfluid that moved through faults and shear zones and
31
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Figure 22 Schematic sections illustrating the proposed model of the structural development of the BryahndashPadburyGroup succession in the westa) Development of the Bryah Group pre-D1 over the Proto-Yarlarweelor gneiss complex and the northernmargin of the Yilgarn Craton in an extensional-rift settingb) Early- and syn-D1 deposition of the Padbury Group in a fold-and-thrust belt foreland-basin type settingover the Bryah Group Inversion of the Bryah rift-basin by possible reversal of D1 normal faultsDevelopment of D1 faults between the Bryah Group Padbury Group Yarlarweelor gneiss complex andYilgarn Cratonc) D2 to D3 local interleaving of the Bryah and Padbury Groups with the development of folds and faultsDeformation of the Bryah and Padbury Groups above basal detachments Early D1 faults refolded aboutD2 or D3 folds Formation of c 1810 Ma leucocratic granite locally associated with incipient minimum meltin the Archaean gneiss component of the Yarlarweelor gneiss complex Later at c 1800 Ma sheet-likeplutons developed particularly along the faulted boundaries between the Yarlarweelor gneiss complexand Bryah and Padbury Groups
Deposition of Padbury GroupEarly D
Development of fold and thrustbelt in D
1 1
Inversion of Bryah rift
1
Murchison Fault
Karalundi Formationequivalents Bryah Group
Hyaloclastites
Proto-Yarlarweelorgneiss complex
Post-rift phase
Thickening of supra-crustal succession over
Proto-Yarlarweelorgneiss complex
a)
b)
c)
v
SAO62 130300
Formation of c 1810 Ma leucocratic coarse-grained granitein Yarlarweelor gneiss complex (Sheppard et al 1999)
Deformation of the Yarlarweelor gneiss complex
NNW1
SSE
1
2 3
Early- and syn-D
Mafic and ultramaficvolcanic rocks
Early reversal of D normal faults some possible back thrustingof volcanic rocks below detachments cut by detachments
Folded c 1960 MaYamagee granite
Local plutonism into Proto-Yarlarweelor gneiss complex
at c 1960 Ma forming Yamageegranite of Sheppard and Swager (1999)
Pre-D extensionndashrift phase
D ndashD
Bryah Group
Proto-Yarlarweelorgneiss complex
Padbury Group
32
Pirajno et al
metasomatized M1 assemblages in the Bryah Group andPeak Hill Schist rocks during M2ndashD2 Elsewhere in theregion during D2 the Peak Hill Schist and Bryah andPadbury Group rocks were folded into tight to isoclinalupright folds with mainly easterly to northeasterly trends(Occhipinti et al 1998c) Post-D2 during D3 theYarlarweelor gneiss complex was uplifted and retrogressedto greenschist facies This uplift in a dextral strike-slipregime may have been accommodated by steeply dippingnormal faults between the Yarlarweelor gneiss complexand the Bryah and Padbury Groups (Figs 17 and 18) thathave now been inverted (Fig 24)
In the Peak Hill Schist subhorizontal D1 mylonitezones and rootless folds are refolded about an easterly oreast-northeasterly trending upright D2 antiform The domalshape of the Peak Hill Schist is an artefact of a northerlytrending upright D3 antiform refolding the D2 antiformThe Yarlarweelor gneiss complex apparently does notcontain D1 folds although shearing along basementndashcovercontacts between the Yarlarweelor gneiss complex and theBryah and Padbury Groups may have developed duringD1 (Fig 22b) The D2 fold-axial surfaces within the
Yarlarweelor gneiss complex parallel the arcuate faultedboundary with the Bryah and Padbury Group rocks Thischange in the trend of D2 may be explained in terms of afault-bend fold developed during dextral shearing(Occhipinti and Myers 1999) that may have accompanieduplift during D3
MineralizationThe mineral resources of the Peak Hill SchistBryah Group and Padbury Group are considerableconsidering the relatively small total area of thesebasins (about 6000 km2) These resources include goldmanganese iron ore talc and silver Pirajno andOcchipinti (1995) discussed the mineral potential of theBryah Basin and Pirajno and Preston (1998) described themineral deposits of the BryahndashPadbury region and PeakHill Schist Mineral production and defined resourceswithin these tectonic units as at 30 June 1999 arepresented in Tables 7 and 8 Known deposits andoccurrences are listed in Table 9
Figure 23 Schematic section illustrating the proposed model for the structural development of theBryahndashPadbury Group succession and the Peak Hill Schist a) Development of the BryahGroup in a rift setting pre-D1 over the Marymia Inlier (Yilgarn Craton) b) D1 closure of theBryah lsquoriftrsquo inversion of normal faults deposition of the Padbury Group and formation ofthe Peak Hill Schist
Future D fault
NNW SSE
Bryah Group
Basement
Proto-Peak Hill Schist
Pre-D extensionndashrift phase1
1Peak Hill Schist
D faults1
1
Rift closes Peak HillSchist develops as a
strongly duplexed packageof rock
Marymia Inlier
a)
b)
SAO63 150300
Padbury Group
Early- and syn-D
Mafic and ultramafic volcanic rocks
33
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The mineral deposits of the Peak Hill Schist andBryah and Padbury Groups include mesothermal-stylegold-only lodes volcanogenic massive sulfide (VMS)copperndashgold supergene-enriched manganese bandediron-formation iron ore and talc in metasomatizeddolomitic rocks The distribution of these mineral depositsis shown in Figures 25 and 26 and Plate 1
Gold depositsThe most important mineral deposits exploited to datehave been the mesothermal-style gold-only lodes all ofwhich are in the Peak Hill Schist and the Bryah andPadbury Groups If the area occupied by these groupsalone is taken into account (about 6000 km2) then theidentified contained gold per unit area is 125 kg goldkm2The mesothermal gold deposits including past and presentproducers include Peak Hill Jubilee and Mount Pleasantin the Peak Hill Schist Harmony Mikhaburra WembleyCashman and Ruby Well in the Bryah Group (Figs 25and 26) and Horseshoe Labouchere Nathans DeepSouth and Fortnum in the Padbury Group The Wilthorpedeposit is hosted in Upper Archaean granitic rocks whichare tectonically interleaved with rocks of the Bryah andPadbury Groups
The total gold produced is 595 t with total (producedplus remaining inferred indicated and measured)resources estimated at approximately 75 t of containedgold The Labouchere and Fortnum areas containthe regionrsquos largest pre-mining resource estimated as 333 tof contained gold at a grade of about 24 gt goldApproximately two-thirds (225 t) has been exploited
largely between 1989 and 1995 with the remainingresource (107 t) being in the Fortnum area Details of theLabouchere and Fortnum deposits can be found in Hannaand Ivey (1990) and Hill and Cranney (1990) respectivelyThe area around the Peak Hill opencut (includingRavelstone) has produced approximately 20 t of fine goldat an average grade of 4 gt gold more than half of whichhas been extracted in the last 13 years Remainingmeasured and indicated resources are estimated at about47 t of contained gold The Harmony deposit (NewBaxters Find) which was recently exhausted had totalpre-mining resources estimated at about 92 t with a gradeof 35 gt gold
The lode deposits are hosted in mylonitic schistmetasedimentary rocks metavolcanic rocks or along theircontact zones They are spatially associated with high-strain zones and hydrothermal alteration dominated bypyrite quartz muscovite biotite and alkali feldspars Themineralization is in ductile and brittlendashductile shears (egPeak Hill) and in discrete brittle fractures (eg Cashman)indicating a relationship of structural style with therheology of the host rocks The development of ductilebrittlendashductile and brittle structures (zones of highpermeability) was accompanied by infiltration ofhydrothermal fluids which produced alteration andmineralization The precise timing of the mineralizationis difficult to ascertain Windh (1992) suggested syn-D3but from field and petrological observations it is morelikely that circulation of mineralizing fluids occurredduring a continuum related to D1ndashD2 tectonism andmetamorphism under conditions of ductile or brittlendashductile regimes with perhaps some remobilization intobrittle structures occurring during D3 Lead isotope data
Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneisscomplex and then into the Bryah and Padbury Basins showing the possible present-day configuration of these units
Kerba FaultBangemall BasinFault boundary
YILGARNCRATON
vv
v
vv
v
vv
vv v
v
v
v vv v
vvv
vvv
vvv
vv
Errabiddy
Shear ZoneGascoyneComplex
Possible currenterosion level
SAO64 130300
NW SE
SeabrookndashMurchison Fault
v v
Bangemall Group
Yarlarweelor gneiss complex
Bryah and Padbury Group rocks
Cooinbar Fault
34
Pirajno et al
Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
_______________________ Production (P) _______________________ _______ Remaining resources (R) ________ TotalMining centre Ore Contained Alluvial Dollied Total Resource Ore Contained pre-miningor mine metal contained type metal resources
metal (P+R)(kt) (kg) (kg) (kg) (kg) (kt) (kg) (kg)
Pre-1986
Mount Fraser Mining Centre 09 24 27 13 288 ndash ndash ndash 288Mount Seabrook Mining Centre 17 383 ndash 02 385 ndash ndash ndash 385Ravelstone Mining Centre 49 1058 ndash 32 109 ndash ndash ndash 109Wilthorpe Mining Centre 01 15 ndash ndash 15 ndash ndash ndash 15Peak Hill sundry parcels 27 7706 889 139 8734 ndash ndash ndash 8734Peak Hill Mint deposits(a) ndash ndash 25 33 58 ndash ndash ndash 58Ruby Well Mining Centre 85 146 325 142 1927 ndash ndash ndash 1927Horseshoe Mining Centre 9049 2 9669 352 889 3 091 ndash ndash ndash 3 091Peak Hill Mining Centre 6217 8 200 367 628 8 2995 ndash ndash ndash 8 2995
1986 to 30 June 1999
Horseshoe Lights(b) mine 9059 3 7373 217 ndash 3 759 ndash ndash ndash 3 759Fortnum mine 5 832 15 6025 377 ndash 15 6402 MES + IND 2 221 7 542 23 1822
INF 991 3 194 3 194Labouchere mine 2 9108 6 9052 ndash ndash 6 9052 ndash ndash ndash 6 9052Mount Pleasant mine 1449 433 ndash ndash 433 ndash ndash ndash 433Peak Hill mine 6 5738 20 1266 908(c) ndash 20 2174 MES + IND 2 200 4 760 24 9774
Total 17 9128 59 0577 3487 1878 59 595 5 412 15 496 75 091
NOTES (a) Gold from the Peak Hill Mining Centre deposited at the Perth Mint(b) Horseshoe Lights also produced 261 675 t of copper concentrates containing 25803 kg of gold(c) Includes 625 kg of gold produced from retreated tailingsMES Measured resources IND Indicated resources INF Inferred resources
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
35
GSW
A R
eport 59G
eology and mineralization of the P
alaeoproterozoic Bryah and P
adbury Basins W
A
Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
_____ Production (P) to 300699 _____ __________________ Remaining resources (R) __________________ Total resource (P+R)Commodity Mine Ore or concentrate Contained metal Resource type Ore or concentrate Contained metal Contained metal
(t) (t) (t) (t) (t)
Copper and Cashman 7 11 ndash ndash ndash 11cupreous ore Peak Hill sundry 63 223 223
Horseshoe Lights 261 675 49 159 Indicated 2 080 000 22 897 72 056Inferred 3 340 000 22 879 22 879
Total 261 745 49 1824 5 420 000 45776 94 9584
Manganese Horseshoe 489 895 203 899 Measured + Indicated 80 000 21 000 224 899Inferred 205 000 100 000 100 000
Mount Fraser 228 108 Measured + Indicated 32 000 9 000 9 108Mount Padbury 7 319 3 498 Measured + Indicated 5 000 2 000 5 498Ravelstone (Peak Hill) 76 237 36 938 ndash ndash ndash 36 938Total 573 679 244 443 Measured + Indicated 117 000 32 000 276 443
Inferred 205 000 100 000 100 000
Iron Robinson Range ndash ndash Inferred 10 000 000 6 000 000 6 000 000
Talc Mount Seabrook ndash Livingstone ndash 540 416 Indicated ndash 1 470 000 2 010 416Inferred ndash 250 000 250 000
Total ndash 540 416 ndash 1 720 000 2 260 416
Silver Horseshoe Lights (post-1982) ndash 72 7194 kg ndash ndash ndash 72 7194 kg(by-product) Peak Hill general ndash 1182 kg ndash ndash ndash 1182 kg
(including Horseshoe pre-1983)Total ndash 72 8376 kg ndash ndash ndash 72 8376 kg
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
36
Pirajno et al
Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins (modified from Pirajnoand Preston 1998 see also Plate 1)
Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
Mine (M) AMG coordinates Principal Mineralization style Expression Ore minerals Relationshipprospect (P) or Easting Northing commodity to hostoccurrence (O)
Cashman (M) 662129 7126994 Gold Regolith enrichment Outcrop Gold Discordantand mesothermal lode
Durack (P) 670440 7150520 Gold Mesothermal lode Drill Gold pyrite Discordantintersections magnetite
Harmony (M) 664145 7161267 Gold Regolith enrichment Drill Gold chalcopyrite Discordantand primary intersections pyrrhotite scheelitemesothermal lode pentlandite pyrite
Heines Find (P) 682759 7145164 Gold Mesothermal lode Outcrop Gold Discordant
Horseshoe (P) 656994 7183734 Gold Eluvial Gold ndash
Horseshoe (P) 657579 7184413 Gold Eluvial Gold ndash
Horseshoe (P) 661219 7182977 Gold Eluvial Gold ndash
Horseshoe (P) Copperndashgold Multiple veins Outcrop Gold Discordant
Horseshoe 662648 7193894 Copperndashgold Supergene enrichment Gossan Chalcocite pyrite DiscordantLights (M) of VHMS chalcopyrite native
copper and gold
Jubilee (M) 671889 7165443 Gold Mesothermal lode Quartz vein Gold pyrite Discordant
Labouchere (M) 627730 7204710 Gold Mesothermal lode Not known Gold pyrite Discordant
Livingstone (M) 567540 7171032 Talc Replacement Outcrop Talc Discordant
Mikhaburra (P) 656252 7130396 Gold Multiple veins Outcrop Gold Discordant
Mount Pleasant (M) 674287 7162089 Gold Mesothermal lode Outcrop Gold pyrite Discordant
Mount Seabrook (M) 572631 7168338 Talc Replacement Outcrop Talc Discordant
Nathans Deep 631713 7198812 Gold Mesothermal lode Not known Gold pyrite DiscordantSouth (M)
Peak Hill (M) 672190 7163003 Gold Mesothermal lode Quartz vein Gold pyrite altaite Discordantchalcopyritebismuthotelluridemolybdenite magnetite
Ravelstone (M) 665734 7166777 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ravelstone (M) 669313 7166423 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ruby Well area (M) 674665 7129915 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 672600 7124378 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 674142 7127027 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677928 7129727 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677408 7130112 Gold Eluvial ndash Gold ndash
St Crispin (P) 691358 7158940 Gold Mesothermal lode Outcrop Gold Discordant
Trevs Starlight (M) 636412 7198887 Gold Mesothermal lode Not known Gold pyrite Discordant
Unnamed (O) 611598 7168985 Variscite Not known Not known Variscite Discordant
Unnamed (O) 611909 7167084 Variscite Not known Not known Variscite Discordant
Unnamed (P) 656664 7185310 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Wembley (P) 663983 7149044 Gold Mesothermal lode Outcrop Gold Discordant
Wilgeena (M) 685369 7155622 Gold Mesothermal lode Outcrop Gold Discordant
Wilthorpe (M) 630414 7176521 Gold Mesothermal lode Outcrop Gold pyrite galena Discordantarsenopyrite
Yarlarweelor (M) 636723 7196423 Gold Mesothermal lode Not known Gold pyrite Discordant
37
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
MARYMIAINLIER
MARYMIAINLIER
Jenkin
FaultGROUPBANGEMALL
Murchison Fault
NARRYERGNEISS
TERRANE
Padbury Bryahand
Yerrida Basins
FMP100b 181099
1000 km
5
67 16
8
9
17
23
4
11
10
15
1213 14
19
18
21
20
1
GOODININLIER
YILGARNCRATON
YILGARN
CRATON
Goodin
Fault
118deg30 119deg30
Killara
Narracoota
Mt Padbury
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
Yandil
119deg30
Milgun30 km
Jamindi Three Rivers Marymia
PEAK HILLROBINSON
RANGE
Padbury Bryah Doolgunna Thaduna
Glengarry Mooloogool Mount Bartle
MerewetherYanganooGabanintha
119deg00
25deg30
26deg30
26deg00
25deg30
GLENGARRY
Milgun
Mesothermal Au AundashCu
Shear zone-hosted Cu
Epigenetic Pb
Supergene Mn
2 Jubilee
5 Labouchere
7 Fortnum group8 Horseshoe Lights9 Horseshoe gold
10 Wilthorpe11 Wembley
12 Mikhaburra13 Cashman14 Ruby Well
group (including Elsa)
16 Horseshoe magnagese17 Ravelstone18 Robinson Range BIF
(no specific locality)19 Thaduna20 PGE-bearing gossan21 Magellan
3 Mount Pleasant4 Harmony
(New Baxters Find)Fault
Geological boundary
Bouguer gravity anomaly
Peak Hill Schist
Karalundi FormationGR
OU
PB
RY
AH
Padbury Group
Horseshoe and Ravelstone Formations
schistmetabasaltic hyaloclastiteNarracoota Formation mafic and ultramafic
Archaean basement
Earaheedy Group
WindplainSubgroup
MooloogoolSubgroup
YE
RR
IDA
GR
OU
P
Maraloou Formationintercalated Killara and Maraloou FormationsDoolgunna and Thaduna Formationswith intercalated Killara FormationJuderina and Johnson Cairn Formations
Homestead
Bangemall Group
Microgabbro dyke
BryahPEAK HILL
1100 000 map sheet 1250 000 map sheet
Aeromagnetic lineament
6 Nathans Deep South
15 Mount Padbury ndash Mount Fraser
Volcanogenic massive sulfide
Shale-hosted stratabound sulfides
MINERALIZATION STYLE
MINERAL DEPOSITS
38
Pirajno et al
Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet (after Pirajno and Occhipinti 1998)
Ravelstone Formation
Karalundi Formation
Horseshoe Formation
Granitoid rock and gneiss
Narracoota Formation
10 km
040400
Yerrida Group
Bangemall Group
Earaheedy Group
Padbury Group
Bry
ah G
roup
Prospect
Producer
JubileeGroup
Peak Hill
Harmony
Wilgeena
Wembley
DurackWell
HeinesFind
Mikhaburra
CashmanGroup
Ruby WellGroup
Goodin Find
Ravelstone Group
(Hit or Miss)
St CrispinWilsons Find
25deg30
118deg
30
119deg
00
26deg00
Mar
ymia
Inlie
r mylonite
Syncline
Anticline
Overturned syncline
Peak Hill Schist
Thrust fault
Fault
Strike-slip fault
FMP162a
Supergene manganese deposit
Alluvialndasheluvial gold deposit
Mesothermal gold lodes
Mount Pleasant
39
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(palaeo-isochrons) suggest that in the Bryah and PadburyBasins mineralization occurred between 192 and 17 Ga(Windh 1992 Thornett 1995) The results of lead isotopicstudies also indicate that the lead was derived from YilgarnCraton rocks (Dyer 1991 Windh 1992 Thornett 1995)although there is a suggestion that the lead from thePeak Hill deposit is similar to that from a galena in theMarymia gold deposit in the Marymia Inlier (McMillan1993)
The nature of the mineralizing fluids is poorlyconstrained Alteration assemblages at the Peak Hill andMount Pleasant deposits indicate that the ore fluids wereenriched in Fe K Na S B CO2 SiO2 and H2O (Thornett1995) Fluid inclusion studies of mineralized materialsfrom the Fortnum and Labouchere gold deposits (Dyer1991 Windh 1992) indicate that the ore fluids wererich in H2O and H2OndashCO2 with salinities of 7ndash12 wtand 5ndash17 wt NaCl equivalent respectively Micro-thermometric measurements (Dyer 1991 Windh 1992)indicate temperatures ranging from approximately 170degto 320degC
Peak Hill Jubilee and Mount Pleasantdeposits
Mine geologists subdivided the Peak Hill Jubilee andMount Pleasant lithologies into the Core sequence HoneyQuartzite Intermediate sequence Mine sequence MarkerQuartzite and Hangingwall sequence
The Core sequence is at the structural base and wellexposed in the Mount Pleasant opencut where it reachesa thickness of 55 m The contact with the Intermediatesequence is marked by the Honey Quartzite which is amylonite consisting of laminated or ribbon quartz TheCore sequence rocks have a mylonitic fabric and are madeup of quartzndashbiotitendashcarbonatendashmuscovite(ndashepidotendashhornblendendashgarnetndashmagnetitendashpyrite) locally withabundant very fine zircons and monazite in the biotite-richvarieties (Barrett 1989) At Mount Pleasant as mentionedabove graphitic schist is present near the top andassociated with a zone of chloritendashbiotite(ndashgarnet) schistwith albite porphyroblasts (Fig 27) containing inclusionsof monazite and zircon Geochemical discriminant plotsusing immobile elements suggest either a granitic (Nb SrLa and Ce) or maficndashintermediate (Ni Cr and Ti)protolith (Thornett 1995) Barrett (1989) on the otherhand proposed that much of the Core sequence could bederived from a sedimentary protolith The origin of thealbite porphyroblasts is uncertain Based on geochemistrypetrology and textural features Thornett (1995) advocateda combined hydrothermal ndash retrograde metamorphicorigin and compared the Peak Hill ndash Mount Pleasantalbites to those studied by Watkins (1983) in the Dalradianschists of Scotland Another possibility that could accountfor the presence of the albite porphyroblasts is lsquoreactionsofteningrsquo as proposed by Dixon and Williams (1983)These authors advanced the hypothesis supported bygeochemical and mineralogical data that mylonitizationof a quartzofeldspathic parent may be accompanied bymineralogical changes involving the breakdown ofplagioclase with release of Na2O and to a lesser extent
CaO and formation of muscovite This would result in theproduction of quartzndashmuscovite mylonites and sodium-rich fluids
The Intermediate sequence is discontinuous withlayers up to 2 m thick and is composed of a quartzndashmylonite-bearing white mica The Intermediate sequencelies above the Honey Quartzite has an estimated thicknessof between 200 and 400 m and forms the footwall to theMine sequence at Peak Hill and the hangingwall to theore zones at Mount Pleasant The Intermediate sequenceis dominantly quartzndashmuscovite schist with minorplagioclase biotite microcline carbonate and chloriteBarrett (1989) interpreted this rock as either a felsicporphyry or an arkose The lower part of the Intermediatesequence consists of mainly biotite schist with garnet andepidote Rocks of the Intermediate sequence exhibitmillimetre-scale metamorphic differentiation layeringwhich define a dominant S2 schistosity (Thornett 1995)This is interpreted by the present authors as a typicalmylonitic structure
The Mine sequence mostly found in drillholes ischaracterized by biotite ndash white mica(ndashchloritendashcarbonatendashamphibolendashgarnetndashalbite) schist and graphite schist(Fig 28) and may be 40 to 50 m thick Drillcore samplesof a hornblendendashplagioclasendashquartz rock (with garnetporphyroblasts) have been interpreted as an unalteredamphibolite (Barrett 1989 Thornett 1995)
The Marker Quartzite is a recrystallized quartzmylonite (lsquoMarker Chertrsquo of mine geologists)1 to 3 m thick at the top of the Mine sequenceOutcrops of Marker Quartzite exhibit radiating iron-oxidepseudomorphs after acicular crystals and iron-oxidepseudomorphs after porphyroblasts Windh (1992)identified these acicular crystals using the scanningelectron microscope as grunerite The porphyroblastpseudomorphs are possibly after garnet
The Hangingwall sequence can be up to 700 m thickand is made up of white mica ndash magnetite(ndashgarnetndashchlorite) mafic schist and metabasite The latter is locally
Figure 27 Albite porphyroblasts in mylonitic schist at theMount Pleasant deposit
40
Pirajno et al
garnetiferous and characterized by a metamorphic (andhydrothermal) assemblage containing variable amountsof hornblende plagioclase quartz garnet epidote andtitanite The metabasite is overlain by mylonitic schistcontaining mainly quartzndashplagioclasendashbiotite and locallyassociated with zones of albitendashmuscovite and garnetndashepidote (calc-silicate)
The Peak Hill Jubilee and Mount Pleasant depositswere studied by Barrett (1989) who based most of hiswork on drillcore samples and Thornett (1995) Theseauthors provided much of the information summarizedbelow augmented by data from this study The Peak HillJubilee and Mount Pleasant gold deposits are situated inthe west-northwestern portion of the Peak Hill Anticlineand hosted in the Peak Hill Schist (Figs 4ndash7 and 26) Inthe mine areas the rocks are intensely weathered to depthslocally exceeding 200 m Weathering products arepredominantly kaolinitic clays and iron oxyhydroxidesThis weathering is particularly well developed in zonesof hydrothermal alteration which in turn are related tohigh-strain zones the latter having facilitated percolationof meteoric waters Hydrothermal alteration is dominatedby sulfidation (pyrite) and alkali metasomatism (biotiteand albite) and contained within late-stage quartzndashcarbonate veins hosted in highly strained metabasites andquartz mylonites Other important alteration mineralsinclude iron-rich chlorite sericite garnet tourmalinedolomite and calcite In all about 20 t of gold has beenproduced
The Peak Hill mineralization was exploited in threeadjoining pits which from north to south are FivewaysPeak Hill Main and Mini In plan view (Fig 29) the entirePeak Hill mineralized system is contained within apackage of mylonitic schist (Mine sequence) at thefootwall of northerly trending and westerly dippingshear zones The mylonitic schist contains quartz podsveins lenses and stringers and locally graphitic quartzmylonite units (Marker Quartzite see below and Fig 30)The Mine sequence contains lenses of mafic rocks (egmetadolerite) The overall picture is one of a complex zoneof shearing and tectonic interleaving between rocks of the
FIVEWAYSPIT
MINIPIT
MAINPIT
100 m
sequence
Mine sequence
Intermediate sequence
Vein quartz
Marker Quartzite
Shear zone
Anticline
FMP160 271099
Hangingwall
Geology notmapped
Geology notmapped
N40
42
45
40
25
45
45 26
30
42
45
Fault42
Cleavage
Foliation
Figure 28 The Mine Sequence schist at the Peak Hill depositshowing biotite alteration the biotite is partlyretrogressed to chlorite plane polarized light
Figure 29 Schematic geological map of the Fiveways Mainand Mini opencuts Peak Hill deposit (after Thornett1995)
Figure 30 Peak Hill Mini opencut showing the ore-bearingmylonitic schist graphitic schist (dark bands) andMarker quartzite unit (above the upper graphiticschist)
41
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Narracoota Formation and Peak Hill Schist Kinematicindicators (CndashS surfaces) indicate a thrust movement fromwest to east (Thornett 1995)
The main orebody has a westerly dip ranging from20deg to 50deg (averaging 35deg) and is hosted in rocks of theMine sequence High-grade zones can contain up to30ndash40 gt gold The ore zones are characterized bypervasive alteration consisting of chloritendashbiotitendashquartzndashcarbonatendashgraphite The principal ore minerals arepyrite chalcopyrite and gold Other ore minerals includealtaite tetrahedrite bismuthotelluride molybdenite andvarious bismuthndashleadndashtellurium compounds The goldmineralization is thought to have been emplaced in at leasttwo stages In the first stage gold mineralization wasemplaced along the contact between the Marker Quartziteand the Mine sequence (see below) During the secondstage cross-faults were formed with the gold beingredistributed or rearranged along these cross-faults
The Jubilee deposit was at first mined underground in1892 from a number of workings but the production isunknown In 1992 a small pit was excavated based onprobable reserves of approximately 50 000 t at 4 gt goldIn this pit gold mineralization is hosted in rocks of theHangingwall sequence and is in a complex quartzstockwork system emplaced along the margins of a 250 m-thick undeformed metabasite The gold is on both thehangingwall and footwall sides of the metabasite bodyTourmaline is present in the ore-bearing material Near theJubilee pit a northerly striking westerly dipping quartzvein almost perpendicular to the dominant foliation trendextends for about 200 m This vein was mined in the pastand contained maximum grades of approximately 30 gtgold
Mining at Mount Pleasant began at the turn of thecentury with the production of 8000 t of ore with anaverage grade of 9 gt gold Mining resumed in the 1980swhen about 145 000 t of ore was extracted with anaverage grade of 3 gt gold and 04 t of gold wasproduced The ore zones are nearly flat lying and wereemplaced in subparallel fashion one above the other Thedeeper northern zone is hosted by the Core sequence Goldis in quartzndashcarbonate veins associated with zones ofalbite (Fig 27) iron-rich chlorite sericite carbonate andpyrite alteration as well as zones of nearly flat lyinggraphitic schist (dip is 10deg to the south) The veins areeither vertical or of saddle-reef type lodged in anticlinalfolds
Harmony deposit
The Harmony (also known as New Baxters Find orContact) gold deposit is located approximately 10 km westof Peak Hill in a featureless area of no outcrops andcovered by colluvium lateritic duricrust and hardpanmaterial Details of the geology of the Harmony depositcan be found in Harper et al (1998) from whom the briefreview that follows is taken
The Harmony gold deposit consists of a subhorizontalsupergene zone hosted in ferruginous lateritic materials
(transported and residual regolith) a northeasterlytrending subvertical primary vein system and carbonate-bearing breccias Most of the ore is contained within thevein system which is hosted in rocks of the NarracootaFormation and at the contact between the Narracoota andRavelstone Formation (Fig 31) with lesser low-grademineralization in laterite The Harmony mineralization ishosted in a northwesterly plunging antiform (Enigmastructural zone) of a southwesterly dipping succession ofaltered mafic rocks at the top of the Narracoota Formationand within a shear zone along the contact with overlyingmetasedimentary rocks of the Ravelstone Formation Themineralized array of quartz veins become locally closelyspaced forming a stockwork that is commonly associatedwith high-grade ore Primary ore minerals include pyritewith gold inclusions pyrrhotite pentlandite chalcopyriteand scheelite The primary mineralization was enrichedby supergene processes
Hydrothermal alteration is characterized mainly bysilicification carbonitization and locally chloritizationHarper et al (1998) reported that mafic rocks show aparagenetic sequence of early albite and quartz followedby muscovite and chlorite Alteration in the metasedi-mentary rocks in the hangingwall is characterized mainlyby sericite and chlorite This primary alteration grades intozones of supergene alteration containing limonitekaolinite smectite group minerals and hematite Theweathered bedrock extends to approximately 60 m depthRegolith studies from drillholes have revealed anomalousAu W As Sb and Se in the ferruginous materials
Labouchere Nathans and Fortnumdeposits
In the northwestern part of the BryahndashPadbury Basin (onMILGUN) three distinct zones of gold mineralization havebeen recognized in high-strain zones associated with themargin of the Yarlarweerlor gneiss complex (Fig 25 andPlate 1) The Labouchere group (Labouchere and CentralValley deposits) and Nathans group (Labouchere-NathansNathan Bitter and Nathans Deep South deposits) had early
Figure 31 Diagrammatic cross section of the Harmony orezones (modified from Harper et al 1998)
50 m
FMP159
Supergene ore
Primary ore
Pit outline
50
100
150
200
Met
res
Mafic rocks
Formation)
Ultramafic rocks
Formation)(Ravelstone
(Narracoota
(NarracootaFormation)
Pelitic rocks
SW NE
211099
42
Pirajno et al
mining activity recorded from 1939 to the early 1940swith additional discoveries in the mid-1980s (Hanna andIvey 1990) The Fortnum deposits (Trevs StarlightTwilight Ricks Toms Hill Alton Eldorado Callies D39and Yarlarweelor) were discovered in the early 1980s (Hilland Cranney 1990)
Gold mineralization is structurally controlled in hostrocks of both the Bryah and Padbury Groups (Hill andCranney 1990) Windh (1992) concluded from detailedstudies at the Labouchere Nathans Deep South andFortnum mines that aqueous fluids of high temperatureand moderate salinity were responsible for mineralizationConstraints on temperature are derived from the lowerto middle greenschist-facies alteration assemblages(muscovitendashchloritendashalbite(ndashbiotite)) and fluid inclusiontrapping temperatures of up to 320degC Based on leadisotope work (galena from Nathans Deep South) Windh(1992) suggested that the syn-D4 gold mineralizationoccurred between 19 and 18 Ga The main features ofthe ore deposits are described below from the availableliterature
At the Labouchere-Nathans mine gold mineralizationis hosted in pyritic chert lenses or pods that lie withinmaficndashultramafic schist and along the contact withoverlying quartz wacke of the Labouchere FormationWindh (1992) described volcanic breccia (with high Niand Cr) with fuchsitic ultramafic and chert clasts similarto the reworked clastic rocks immediately overlying themaficndashultramafic volcanic rocks in the NarracootaFormation at the Fortnum mine The maficndashultramaficschist lies in the core of a southerly plunging anticlineand is here interpreted as part of the NarracootaFormation The Narracoota Formation ndash LabouchereFormation contact is interpreted as an early (D1ndashD2) faultor shear zone that was tightly folded during D3 Thestructure is crosscut and slightly offset by D4 faultstrending 270degndash290deg including a shear that forms thesouthern limit to the mineralization (Hanna and Ivey1990) Gold is associated with quartz veining and pyritein the altered chert with sideritendashmuscovitendashpyritealteration around the veins (Windh 1992) Productionfigures are only known for the combined output of theLabouchere-Nathans and Nathans Deep South opencuts(nearly 7 t of gold over five years Table 7)
At the Nathans group of workings the Nathan Bittershafts within the upper Labouchere Formation or lowerWilthorpe Formation have a recorded production of about8 kg over the period 1943ndash1950 (Swager and Myers1999) About 500 m to the north-northwest shallow shaftslie along the Kinders Fault between coarse and pebblyquartz wacke to the east and ultramafic schist of theNarracoota Formation to the west The Nathans DeepSouth mineralization lies approximately 1 km south-southeast of Nathan Bitter and was discovered in 1986(Hanna and Ivey 1990) The mineralization is hosted byfinely laminated chloritic shale interbedded with coarsequartz wacke and overlain by coarse units grading fromquartz-pebble conglomerate to quartzndashsericite shale Theentire succession is here described as part of the WilthorpeFormation including the chloritic shale which is mostlikely derived from mafic volcanic precursors (Hanna and
Ivey 1990 Windh 1992) Occhipinti et al (1998a)mapped similar units in the Wilthorpe Formation as aseparate member the Beatty Park Member The westerlyyounging succession contains a northndashsouth S3 foliationaxial planar to a few small-scale parasitic D3 foldsplunging steeply south and is overprinted by F4microfolds and kinks trending 290deg Gold mineralizationis within pyrite which has replaced finely bedded chloriteshale near crosscutting D4 quartzndashankerite veins Highestgrades are found adjacent to D4 faults These and otherstructural observations led Windh (1992) to infer a syn-D4 timing of mineralization However small quartz-veinnetworks possibly related to low-grade mineralization inthe overlying coarsely graded units are deformed by D4microfolding
The Fortnum gold mineralization is hosted by theNarracoota Formation which is truncated to the northagainst the Fortnum Fault and wedges out to the southThe package contains maficndashultramafic schist withoverlying reworked fragmental and volcaniclastic rocksincluding rocks with a supposed felsic volcanic derivationoverlain by the Ravelstone Formation (Hill and Cranney1990)
Mineralization at Trevs (and closely associatedorebodies including a recent discovery named Starlight)is hosted by quartz-vein systems in a westerly dippingsuccession of graded sericitic siltstone and coarse wackewith medium- to coarse-grained feldspar quartz and lithicfragments at least partly derived from the underlyingmaficndashultramafic volcanic rocks The Yarlarweelormineralization is hosted by ovoid lenses of jasperoidalchert within variably schistose maficndashultramafic volcanicrocks including interleaved fine tuffaceous and coarsefragmental layers (Hill and Cranney 1990) The chertlenses are within a westerly dipping reverse D3 shear zonecharacterized by quartzndashchloritendashsericite alteration Gold-bearing quartz(ndashpyrite) veins within the chert pods andwithin magnetite-bearing chlorite schist trend at 120deg dipsteeply north and are parallel to small sinistral D4 faults(D3 in Windh 1992) Windh (1992) also reported a minorset of (dextral) faults trending 070deg and crosscutting theD3 shear zones This may suggest a conjugate fault setrecording eastndashwest compression possibly late during D3rather than during north-northeastndashwest-southwest D4compression
Mining at the Fortnum group of workings from 1990to 1998 yielded 11 928 kg of gold from 4685 Mt of orewith an average recovered grade of 254 gt gold (Swagerand Myers 1999) Remaining measured and indicatedresources at Fortnum including Trevs and Starlightcontain an additional 17 970 kg of gold with a further4340 kg of gold estimated within inferred resources(Perilya Mines NL 1998)
Wembley deposit
The Wembley deposit is located approximately 18 kmsouthwest of Peak Hill and 25 km southeast of MurphyWell (from the Peak Hill road) Although rewarding(average grade of 175 gt gold) ore production was verysmall (less than 1800 t)
43
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The Wembley mineralization is hosted in alteredmetabasite rocks within a major shear zone trending 120degThe mineralized zone strikes at 075deg and dips 63deg to thenorthwest A quartz vein near the old workings strikes at060deg and dips 54deg to the northwest Sedimentary units areintercalated with the volcanic rocks and consist ofturbiditic rocks (greywackendashshale) As at the Durackprospect (see below) quartz mylonite units trending120degndash140deg are within the metabasites
Wilgeena deposit
The Wilgeena (or Hit or Miss) gold mine area is located15 km southeast of the Peak Hill mine Production wasless than 15 000 t at an average grade of 26 gt gold
The deposit is within rocks of the Peak Hill Schist andmore specifically along the contact between the mylonitesand quartzndashsericite schist A northerly trending easterlydipping stoped-out ore lens was approximately 2 m thickThe mineralization is hosted in quartzndashmuscovitendashmagnetite schist Grab samples from the old excavationsreturned values ranging from 3 to 14 gt gold (Mountford1984) Whitfield (1987) estimated inferred resources asapproximately 600 000 t at 244 gt gold
Durack St Crispin and Heines Findprospects
The Durack prospect lies about 12 km south of Peak Hillalong and immediately west of the Old Peak Hill telegraphroad This gold deposit is blind being covered by soil andlateritic material and consists of primary mineralizationand a supergene mineralized zone The prospect wasidentified by a soil anomaly containing up to 100 ppb gold(Sabminco Annual Report 1994)
The prospect area is underlain by rocks ofthe Narracoota Formation which include metabasite(medium- to coarse-grained metabasalts) and maficpyroclastic rocks Thin magnetite-bearing chert bands(possibly chemical sediments) intercalated within themetabasites define a broad synclinal structure A numberof mylonite zones trending 120degndash125deg cut across theNarracoota Formation rocks and contain most of theprimary mineralization Grades intersected during drillingare in the order of 15 gt gold over widths of 4 to 6 m
The primary mineralization is contained within quartzndashsulfide veins and stockworks hosted by altered metabasiterocks The mineralized area is about 14 km long and200 m wide Hydrothermal alteration is pervasive andconsists of quartz chlorite biotite and iron-rich carbonate(ankerite) Pyrite is present as fine disseminations andveinlets Selvages of silicandashpyritendashcarbonate surround themineralized zones
The supergene mineralization at the Durack prospectis controlled by subhorizontal redox fronts within theregolith material Supergene enrichment shows grades ofup to 12 gt gold over an interval of about 5 m In somecases the redox-front-related mineralization developed upto 45 m on each side of the primary zone
The St Crispin prospect is situated 20 km east-southeast of Peak Hill The mineralization is along a north-northwesterly trending structure and hosted in sericite(ndashgraphite) schist of the Peak Hill Schist Quartz veins arepresent in the schists and may host the mineralization
The Heines Find prospect is located 20 km south-southeast of Peak Hill Mineralization can be traced forabout 6 km along the easterly trending contact betweenrocks of the Narracoota Formation and the HeinesMember of the Wilthorpe Formation This contact has adip of 80deg to the north and is sheared In this area theNarracoota Formation consists of strongly deformedpillow lavas and chlorite schist The sedimentary rocks ofthe overlying Heines Member include a basal polymicticconglomerate
Ruby Well group
The Ruby Well area includes a number of mineral leasesfrom which gold has been produced either from surfacematerials or from hard rock (02 t Table 7) The RubyWell leases lie on the northern side of the Great NorthernHighway about 80 km from Meekatharra and 4ndash5 km eastof the Peak Hill turn-off
The area is underlain by the Narracoota Doolgunnaand Karalundi Formations The Hard To Find Ruby Anneand Lucky Call deposits within mafic schist of theNarracoota Formation were exploited between 1912 and1917 Most of the current production (figures notavailable) is from a number of dry-blowing workingssurrounding these old mines
Mikhaburra deposit
The old Mikhaburra gold mine (also known as HoldensFind) is in Narracoota Formation volcanic rocks in thesouthwestern part of BRYAH (Fig 25) The recordedproduction of the Mikhaburra mine is about 226 kg ofgold (MacLeod 1970) The mineralization is associatedwith a system of auriferous quartz veins emplaced alonga shear zone trending about 130deg to 150deg and dipping 68degto the southwest The volcanic rocks include mainlychlorite schist A quartz vein with a strike of 120deg and dipof 58deg southwest lies to the west of the old workings Thisvein is about 1 m wide and locally displays a laminatedstructure
Wilthorpe deposit
The Wilthorpe deposit is hosted by granitic rocks of theDespair Granite (Fig 32) which contains xenoliths ofmafic material Gold mineralization is confined to a zonecontaining quartz veins and flanked by bleached andsilicified wallrocks The ore zone is hydrothermallyaltered with assemblages of chloritendashsericitendashbiotite andquartzndashmuscovitendashbiotitendashtourmaline flanked by near-pervasive silicification In addition to gold the mineralizedveins also contain pyrite galena arsenopyrite andchalcopyrite The wallrock granite has a cataclastic textureand consists of quartz and feldspar lsquoeyesrsquo surrounded bya network of granulated quartz and sericite
44
Pirajno et al
Cashman deposit
The Cashman area on BRYAH includes a number of smallmineral occurrences and deposits containing copperand copperndashgold The old Cashman copper mine isapproximately 250 m from the gold workings In 1917 thismine produced about 7 t of copper ore grading 165copper (Marston 1979) The copper mineralizationconsists of a metre-wide cupriferous limonite vein with astrike of 042deg and a shallow dip to the northwest Oreminerals are chrysocolla and malachite as disseminationsand veinlets (Marston 1979)
In 1937 there was a small production of gold ore fromquartz veins In 1986ndash87 the gold potential of theCashman area was reassessed and on the basis of thiswork a small opencut was excavated from which 8000 tof ore material was produced and stockpiled (Whitfield1987) Gold mineralization is hosted in quartz veins withinmetabasaltic hyaloclastite A 01 m-thick quartz vein in thepit has a strike of 115deg and dips 35deg to the northeast Atand near the surface supergene enrichment is present ina horizon about 30 m wide and dipping about 20deg to thenorth (Whitfield 1987)
Volcanogenic copperndashgolddepositsThe Horseshoe Lights copperndashgold deposit on JAMINDI hasproduced nearly 9 t of gold of which almost 26 t wasrecovered from the copper concentrate operation between1988 and 1993 (Table 7) The Horseshoe Lights depositis hosted in felsic schist of the Narracoota Formation(Bryah Group) The mineralization consists of massivesulfides overlying and flanked by disseminated andstringer sulfides Ore minerals are mainly chalcocitepyrite and chalcopyrite Native copper is also present(Parker and Brown 1990) The host rocks are mylonitizedchlorite schist kaolinitendashsericite schist and quartzndashsericiteschist The geometry of the ore zones (massive sulfidesand stringer zone) alteration patterns (silicificationsericitic and chloritic alteration) predominantly felsiccomposition of the host rocks and metal association (CundashAundashAgndashPbndashZn) suggest that the deposit was originally ofthe volcanogenic massive sulfide type but subsequentlyenriched by supergene processes Average grades havebeen about 8 gt gold about 10 copper and 300 ppmsilver The stringer mineralization is of low gradeaveraging between 02 and 03 gt gold Production ceasedin 1994 Remaining resources (Table 8) are of low-grademineralization
Supergene manganese depositsManganese mineralization is part of a historicallyimportant manganese field first recognized in 1905 withdeposits in the Mount Fraser Mount Padbury Ravelstone(Peak Hill) and Horseshoe areas The manganesemineralization is of supergene origin and related tomanganiferous and hematitic shale units and BIF of theHorseshoe Formation (Bryah Group) as well as units ofthe Padbury Group The chief ore minerals are pyrolusiteand cryptomelane The ore is lateritic locally pisolitic innature and in places forms caps overlying the primarymanganese-rich sedimentary material In places notablyat Horseshoe there is evidence to suggest that someenrichment may have taken place in a palaeodrainagechannel lake or swamp environment (MacLeod 1970)In the Ravelstone area just north of the Peak Hill golddeposit the manganese supergene enrichment appears tohave a structural control
The Horseshoe area has been the main producingregion with production from two deposits 2 and 3 kmnorth and northwest of the Horseshoe townsite (Plate 1)The main production period was from 1948 to 1971 when490 000 t was mined (Table 8) all but 5000 t of whichwas classified as metallurgical-grade ore The enrichedzone was 3 to 45 m thick and typically extended overlengths of 400 to 500 m The North deposit averaged 30 min width whereas the South deposit was fan shapedopening from 20 to 300 m wide at its maximum extentOre consisted of mixed manganese and iron oxides withhighly variable manganese and iron contents Gradesprogressively decreased from 42 to 35ndash38 after 1966
There are several small deposits in the Mount Fraserndash Mount Padbury area about 30 km west of Peak Hill
Figure 32 The west wall of the Wilthorpe opencut showingthe contact between biotitendashsericitendashquartz schistand deformed Despair Granite
45
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
They contain patches of high-grade ore within largedeposits of ferruginous manganese material Productionof high-grade ore occurred sporadically since 1949 andamounted to 7547 t at grades in excess of 46 manganeseA third mining operation commenced at the Millidie (orElsa) deposit in the early 1990s but this has notprogressed to a full-scale commercial operation High-grade mineralization in the area is estimated to containmeasured plus indicated resources of approximately11 000 t of manganese (Table 8)
In the Ravelstone area immediately north-northwestof Peak Hill mining occurred between 1956 and 1964producing 76 237 t of ore at 70ndash90 manganese oxide(Table 8) Remainng measured and indicated resources areestimated as 132 000 t of contained metal (Table 8)Manganese production at Ravelstone was from easterlystriking orebodies reaching lengths of up to 100 m andwidths of 30 m but commonly small and narrow Detailedexamination of one specimen of ore revealed that it wascomposed mainly of cryptomelane and accessorypyrolusite A partial geochemical analysis of the samesample provided the following results 064 wt SiO2465 wt Al2O3 0011 wt P 033 wt MgO 268 wtK2O 7038 wt MnO 119 wt Fe 005 ppm Au650 ppm Co 31 ppm Cu 53 ppm Ni 20 ppm Pb and98 ppm Zn
The manganese ore is characterized by high bariumabundances (3000 ppm to 30 at Mount Fraser3000 ppm to 1 at Horseshoe and 3943 to 9000 ppm atRavelstone)
Iron oreThe Robinson Range Formation (Padbury Group) containsunits of banded iron-formation (Fig 2) within which areareas of supergene enrichment of hematite and goethiteThese constitute demonstrated (pre-JORC code) iron-oreresources estimated at approximately 10 Mt with gradesin excess of 60 iron (Table 8) Enrichment is above twoBIF units approximately 100 m thick separated by ahematitic shale horizon Iron grades of the primary BIFvary between 20 and 50 Hematite and hematitendashgoethite surficial enrichment contains grades in excess of50 iron as determined from the sampling of one ofabout 200 small pods of potentially ore grade material(Sofoulis 1970)
TalcTalc in the Mount Seabrook ndash Livingstone ndash Trillbarregion is present within metasedimentary and meta-volcanic rocks and minor mafic and ultramafic rocks Talcis hosted in metasomatized dolomite orebodies (Plate 1)as a series of steeply plunging lenses (Lipple 1990) TheMount Seabrook deposit was discovered in 1965 and hasproduced over 540 000 t of talc mostly of cosmetic gradebetween 1973 and 1995 Indicated and inferred resourcesredefined at Mount Seabrook and Livingstone amount to172 Mt of ore with a significantly greater potentialbecause the orebodies are open along strike
DiscussionThe Horseshoe Lights VMS-type copperndashgold deposit issyn-volcanic and pre-orogenic All other deposits are ofepigenetic origin and syn- to post-orogenic
Figure 33 schematically depicts a simple regionalmodel of ore genesis for the epigenetic mineral depositsin the BryahndashPadbury ndash Peak Hill Schist (BPPS) tectono-metamorphic domain and the adjacent Yerrida Basin TheYerrida Basin and BPPS domain were tectonicallyjuxtaposed along the northeasterly trending Goodin FaultDeformation which affected the BPPS domain wastransmitted across the Goodin Fault for a few kilometresinto the Yerrida Basin This deformation becomes weakerfrom the Goodin Fault eastward The BPPS domain wassubjected to metamorphism (upper to lower greenschistfacies) At least two phases of metamorphism arerecognized a prograde phase overprinted by a retrogradephase Geothermometry and geobarometry studies inthe area around Peak Hill by Thornett (1995)indicated temperatures of around 500ndash620degC for peakprograde metamorphism and 65 to 7 kbar for minimumpressure of the prograde assemblages The timing ofthis metamorphism is probably linked to the collisionbetween the Pilbara and Yilgarn Cratons (see Tectonicmodel and conclusions) which is postulated to haveoccurred between 1820 and 1800 Ma (Occhipinti et al1999)
A genetic model proposed by Pirajno and Preston(1998) envisages that fluids were generated during phasesof dynamic and thermal metamorphism in the BPPSdomain and that these fluids were largely responsible forthe deposition of mesothermal gold-only and shear-zone-hosted deposits The paragenesis of the alterationassemblages associated with the mesothermal depositsand textural relationships suggest that metamorphism
Figure 33 Sketch illustrating a conceptual model for the originof precious and base metal epigenetic deposits inthe BryahndashPadbury and Yerrida Basins (after Pirajnoand Preston 1998)
FMP71a
Bryah and Padbury Groups
Mooloogool Subgroup
Windplain Subgroup
Direction of fluid movement
170300
Fault Cleavagedevelopment
ARCHAEANBASEMENT
NARRYERTERRANE
Area of Au deposition
Collisionzone
Cleavagelate epigeneticmineralisation
Metamorphism
Basin fluids
YERRIDA
and deformation
Goo
din
Faul
t
development
BRYAHndashPADBURYBASINS BASIN
NW SE
46
Pirajno et al
and mineralization were broadly contemporaneousalthough alteration was in most cases from peak toretrograde metamorphism Exceptions to this are localizedzones of sodium metasomatism (albite and arfvedsonite)which overprint the retrograde assemblages This sodiummetasomatism may be related to central zones ofhigher temperatures within the mineralized structuresOne possible explanation for the widespread sodiummetasomatism is granite magmatism however there is noevidence in either the Bryah or the Padbury Basin ofgranitic plutons intruding the volcano-sedimentarysuccessions Therefore a possible role of graniticmagmatism as one of the heat and metal sources for thehydrothermal solutions based on our present knowledgeis excluded
Hydrothermal solutions responsible for the emplace-ment of mesothermal lodes are considered to be generatedin tectonically active regions and are associated withcompressional and extensional tectonics (Kerrich andCassidy 1994) The mesothermal-style gold-only lodesof the BPPS domain were formed in a compressionalsetting characterized by thin-skinned thrusting associatedwith prograde and retrograde mineral assemblages(Pirajno 1996) Dyer (1991) concluded that the hydro-thermal mineralization in the LaboucherendashFortnumarea was generated by the mixing of two fluids ofdifferent density and salinity Deeply sourced hot salineCO2-bearing fluids were mixed with cooler less salinenear-surface aqueous fluids The available evidencepoints to the conclusion that the mineralizing fluids wereat first generated during compression and dehydrationand moved along ductile to brittle structures Duringsubsequent phases meteoric fluids would have infiltratedalong the same structures and mixed with the hottermetamorphic solutions The whole mechanism couldhave been repeated again in the next phase of compressionand extension leading to multiphase ore genesis processesin which the latest phase leaves the most detect-able imprint There is no obvious link with magmaticactivity
Other metal deposits in the BryahndashPadbury Basin aresupergene manganese and iron ore (Pirajno and Preston1998) The timing of the weathering event that led to thesupergene enrichment of the manganese and iron ores isnot known although it may be possible that the warm andhumid climate during the middle Tertiary (Cockbain andHocking 1990) played a major role in the genesis of thissupergene mineralization
Tectonic model andconclusions
Gee (1979) Hynes and Gee (1986) Windh (1992) andGee and Grey (1993) interpreted the geodynamicevolution of the lsquoGlengarry Basinrsquo as defined by Gee andGrey (1993) in terms of an ensialic or intracontinentalbasin Tyler and Thorne (1990) Myers (1993) Martin(1994) and Myers et al (1996) proposed models in whichthe former lsquoGlengarry Basinrsquo would have formed in aback-arc setting during the convergence of the Pilbara andYilgarn Cratons between 2000 and 1800 Ma
In the light of the re-interpretation of the formerlsquoGlengarry Basinrsquo into the Bryah Padbury and YerridaBasins some modification of the above tectonic schemesis necessary Lack of sufficient geochronological datahowever poses the problem of the precise timing ofevents This lack of information must be taken intoaccount when modelling basin tectonics Pirajno (1996)and Pirajno et al (1998b) suggested two models for thegeodynamic evolution of the BryahndashPadbury and YerridaBasins 1) the basins were formed during convergence andsubsequent collision in a back-arcndashforeland basin settingin which these basins were opened and infilled duringsouthward subduction of oceanic crust (extensional backarc) and subsequently overlain by sediments in a newlydeveloped foreland basin (syn-collisional) and 2) thebasins were formed at the time of the oblique collisionbetween the Pilbara and Yilgarn Cratons as pull-apartstructures in a strike-slip setting with transitions fromextensional (transtension) to compressional (transpression)regimes
In this study we propose a model whereby the BryahBasin was formed as a back-arc rift with a component ofrifting along the Yilgarn continental margin a kind ofproto-oceanic rift comparable to that of the present-day Guayamas Basin in the Gulf of California (Lonsdaleand Becker 1985) The Padbury Basin developed as aforeland basin on top of the Bryah Basin during theoblique collision of the Pilbara and Yilgarn Cratons Ourmodel is shown in Figure 34 in which two stages areschematically depicted and briefly discussed below
The Bryah Basin was formed by processes of back-arc opening during subduction of oceanic crust beneaththe northern margin of the Yilgarn Craton approximately
Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins withinthe context of the Capricorn Orogen (modified from Myers 1990 1993 and Myers et al 1996)a) At about 1960ndash1950 Ma development of Andean-type magmatic arc on a microcontinental active margin back-arcrifting and spreading with creation of oceanic crust (dominantly high-Mg and high-Fe tholeiite associated withsubvolcanic peridotitic cumulates representing future maficndashultramafic schist of the Narracoota Formation) anderuption of basaltic hyaloclastites probably from the same source as the maficndashultramafic material occurs on passivemargin of Yilgarn Craton Insets schematically show geochemical signatures of these volcanic rocks (see text fordetails)b) Capricorn Orogeny involved collision between the Pilbara and Yilgarn Cratons with formation of fold-and-thrustbelts on both northern and southern sides of orogen and thrusting of oceanic crust over hyaloclastite and margin ofYilgarn Craton The thrust separating oceanic crust material from hyaloclastite is represented by the Murchison Fault(see Plate 1) Chondrite-normalized REE patterns for metabasites and hyaloclastites of the Narracoota Formation areshown in the insets
47
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
N S
N S
Marymia In
lier
YILGARN
Backarc riftMicrocontinent
andvolcanic arc
Seafloor
Seafloor
Oceaniccrust
lt 1960ndash1950 Ma
PILBARA
PILBARAYILGARN
Fold-and-thrustbelt
PadburyBasin Bryah Basin
1820ndash1800 Ma
Present-dayBryahndashPadbury
area
Lithosphere
FMP376 170300
4000
3000
2000
1000
00 21 3
FeOMgO FeOMgO Ni Cr
1
2
0
3
0 1 2
La Eu Lu
Sam
ple
chon
drite
100
10
16
Sam
ple
chon
drite
100
10
2La Eu Lu
2
Cr
(ppm
)
TiO
(
)
TiO x1002
Mid-oc
ean r
idge
2
Clastic rocks
Padbury Group
Archaean basement
Metabasic rocksof Narracoota FormationHyaloclastites(Narracoota Formation)
Karalundi Formation
Oceanic crust
a)
b)
48
Pirajno et al
between 1960 and 1950 Ma (Occhipinti et al 1999Fig 34a) Myers (1993) speculated that a southwardoceanic subduction system with a south-facing Andean-type magmatic arc had developed off the northern passivemargin of the Yilgarn Craton Remnants of arc magmaticsuites have not been found but may be buried under theMesoproterozoic Bangemall Basin Back-arc rifting alsoaffected the northern margin of the Yilgarn Craton whererift propagation is postulated to have progressivelyadvanced from west to east through a succession ofcrustalndashlithospheric thinning rupture and grabenformation In this model the Marymia Inlier is a remnantof a rift shoulder (Fig 34a)
The closing of the ocean between the Pilbara andYilgarn Cratons was followed by the oblique collisionbetween the rifted passive margin on the Pilbara side aninferred active magmatic arc and the passive northernmargin of the Yilgarn Craton Closure of the interveningocean (1820ndash1800 Ma) resulted in inversion of the Bryahback-arc rift and thrusting of oceanic crust (nowNarracoota Formation) over the Yilgarn Cratonrsquos northernmargin (Fig 34b) During and following this collisionevent the southern side of the Pilbara was tectonicallysliced by major thrusts whereas most of the tectonictransport of the inferred magmatic and oceanic crust rockswas towards the south (Myers 1993)
High-Mg tholeiitic rocks with pillow structuressheeted dykes the Trillbar layered complex sea-floor metasomatism and trace and rare-earth elementgeochemistry support the oceanic crust model for theorigin of the mafic and ultramafic schist of the NarracootaFormation The hyaloclastites on the other hand wereerupted in shallow waters and locally characterized byexplosive activity and have mixed and overlappinggeochemical signatures with the mafic schist This featurecan be interpreted as suggesting a more continentalenvironment of emplacement and therefore were emplacedon Yilgarn crust (Fig 34a) In contrast to the maficndashultramafic schist the hyaloclastites are relativelytectonically undeformed Their contact with the maficndashultramafic schist is along the Murchison Fault (Plate 1)We conclude that the Murchison Fault represents atectonic boundary between these two components of theNarracoota Formation and that oceanic crust material(precursors of the maficndashultramafic schist) were thrustover the continental hyaloclastites during the CapricornOrogeny as shown in Figure 34b The suggested Gulf ofCalifornia-type palaeoenvironmental setting with thefuture Marymia Inlier as one of the rift shoulders(analogous to the California peninsula) is shown inFigure 34a
The absence of volcanic rocks of intermediate(andesitic) compositions suggests that the NarracootaFormation metabasites were not formed in a subduction-related volcanic-arc setting as proposed by Myers et al(1996) However we concur with Sun (1997) that theboninitic component in the chemistry of the metabasites(see inset of Fig 34 and Figs 12ndash15) needs explanationWe suggest that these boninitic characteristics of theNarracoota Formation can be compared to the boninitesof the Koh Ophiolite in New Caledonia (Meffre et al
1996) which are considered to have formed in a back-arc spreading centre
The overall high MgO and low TiO2 abundancesdepleted REE and low LaYb ratios of the NarracootaFormation are also consistent with the origin of theNarracoota Formation metabasites from a mantle plume(Pirajno et al 1998a)
The Padbury Basin was interpreted by Martin (1994)as a retroarc foreland basin recording the collision of theYilgarn and Pilbara Cratons During and followingcollision between 1820 and 1800 Ma (Occhipinti et al1999) back-arc volcanism ceased and a foreland basindeveloped on top of the back-arc succession (BryahGroup) This basin was filled by siliciclastic rocks only(Padbury Group) During continued regional compressionthe BryahndashPadbury Basin developed into a fold-and-thustbelt and was partly thrust over the Yerrida Basin alongthe Goodin Fault
In summary the convergence between the ArchaeanPilbara and Yilgarn Cratons resulted in progressivecompressional deformation that affected the Bryah andPadbury Groups as a coherent package At least fourgroups of structures are recognized in the regionaldeformation of the volcano-sedimentary succession andtheir reworked basement (ie Yarlarweelor GneissComplex) This same deformation and associatedmetamorphism was responsible for the mesothermal gold-only lodes of the Bryah and Padbury Basins
AcknowledgementsWe acknowledge the contribution of colleagues whoparticipated in the Glengarry mapping program JohnMyers N G Adamides and P G Le Blanc SmithRichard Davy first introduced the senior author to the areaWe are also grateful to the local pastoral community fortheir hospitality The geological staff of LabouchereFortnum Peak Hill and Harmony gold mines are thankedfor sharing their knowledge with us
49
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
References
ADAMIDES N G 1998 Geology of the Doolgunna 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BAGAS L B 1998 Geology of the Marymia 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BARNETT J C 1975 Some probable Lower Proterozoic sedimentsin the Mount Padbury area Western Australia Geological SurveyAnnual Report 1974 p 52ndash54
BARRETT F 1989 A study of wallrock alteration associated withgold mineralization mdash Peak Hill and Mt Pleasant area WesternAustralia Geological Survey M-series Item 7706 A41555(unpublished)
BRADLEY J J FAULKNER J A and SANDERS A J 1997Geochemical mapping of the Robinson Range 1250 000 sheetWestern Australia Geological Survey 1250 000 RegolithGeochemistry Series Explanatory Notes 57p
BREITKOPF J H and MAIDEN K J 1988 Tectonic setting of theMatchless Belt pyritic copper deposits Namibia EconomicGeology v 83 p 710ndash723
BUNTING J A COMMANDER D P and GEE R D 1977Preliminary synthesis of Lower Proterozoic stratigraphy andstructure adjacent to the northern margin of the Yilgarn BlockWestern Australia Geological Survey Annual Report 1976p 43ndash48
BURKE K C KIDD W S F TURCOTTE L DEWEY J FMOUGINIS-MARK P J PARMENTIER E M SENGORA M and TAPPONIER P E 1981 Tectonics of basalticvolcanism in Basaltic volcanism on the terrestrial planets HoustonLunar and Planetary Institute p 803ndash898
COCKBAIN A E and HOCKING R M 1990 Regolith in Geologyand mineral resources of Western Australia Western AustraliaGeological Survey Memoir 3 p 591ndash602
CRAWFORD R A FAULKNER J A SANDERS A J LEWISJ D and GOZZARD J R 1996 Geochemical mapping ofthe Glengarry 1250 000 sheet Western Australia GeologicalSurvey 1250 000 Regolith Geochemistry Series Explanatory Notes57p
DAVY R PIRAJNO F SANDERS A J and MORRIS P A1999 Regolith geochemical mapping as an adjunct to geologicalmapping and exploration examples from three contiguousProterozoic basins in Western Australia Journal of GeochemicalExploration v 66 p 37ndash53
DIXON J and WILLIAMS G 1983 Reaction softening in mylonitesfrom the Arnaboll thrust Sutherland Scottish Journal of Geologyv 19 p 157ndash168
DUNCAN A R 1987 The Karoo igneous province mdash a problemarea for inferring tectonic setting from basalt geochemistry Journalof Volcanology and Geothermal Research v 32 p 13ndash34
DYER F L 1991 The nature and origin of gold mineralization atthe Fortnum Nathans and Labouchere deposits Glengarry BasinWestern Australia University of Western Australia BSc Honoursthesis (unpublished)
ELIAS M 1982 Belele WA Western Australia Geological Survey1250 000 Geological Series Explanatory Notes 21p
ELIAS M BUNTING J A and WHARTON P H 1982 GlengarryWA Western Australia Geological Survey 1250 000 GeologicalSeries Explanatory Notes 27p
ELIAS M and WILLIAMS S J 1980 Robinson Range WAWestern Australia Geological Survey 1250 000 Geological SeriesExplanatory Notes 32p
FISHER R V and SCHMINCKE H-U 1984 Pyroclastic rocksBerlin Springer-Verlag 472p
GEE R D 1979 The geology of the Peak Hill area Western AustraliaGeological Survey Annual Report 1978 p 55ndash62
GEE R D 1987 Peak Hill WA (2nd edition) Western AustraliaGeological Survey 1250 000 Geological Series Explanatory Notes24p
GEE R D 1990 Nabberu Basin in Geology and mineral resourcesof Western Australia Western Australia Geological SurveyMemoir 3 p 202ndash210
GEE R D and GREY K 1993 Proterozoic rocks on the Glengarry1250 000 sheet mdash stratigraphy structure and stromatolitebiostratigraphy Western Australia Geological Survey Report 4130p
HALL W D M and GOODE A D T 1978 The Early ProterozoicNabberu Basin and associated iron formations of Western AustraliaPrecambrian Research v 7 p 129ndash184
HANNA J P and IVEY M E 1990 Labouchere and Deep Southgold deposits in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 667ndash670
HARPER M HILL M G RENTON J I and THORNETTS E 1998 Gold deposits of the Peak Hill area WesternAustralia in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 81ndash87
HILL A D and CRANNEY P J 1990 Fortnum golddeposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 665ndash666
HYNES A and GEE R D 1986 Geological setting andpetrochemistry of the Narracoota Volcanics Capricorn OrogenWestern Australia Precambrian Research v 31 p 107ndash132
JENSEN L S 1976 A new cation plot for classifying subalkalicvolcanic rocks Canada Ontario Division of Mines MP 66 22p
KERRICH R and CASSIDY K F 1994 Temporal relationships oflode gold mineralization to accretion magmatism metamorphismand deformation mdash Archaean to present a review Ore GeologyReviews v 9 p 263ndash310
LE MAITRE R W 1989 A classification of igneous rocksand glossary of terms Oxford Blackwell Scientific Publications193p
50
Pirajno et al
LEWIS J D 1971 The geology of some carbonate intrusions in theMount Fraser area Peak Hill Goldfield Western Australia WesternAustralia Geological Survey Annual Report 1970 p 50ndash56
LIPPLE S L 1990 Talc in Geology and mineral resources of WesternAustralia Western Australia Geological Survey Memoir 3p 678ndash679
LISTER G S and SNOKE A W 1984 SndashC mylonites Journal ofStructural Geology v 6 p 617ndash638
LONSDALE P and BECKER K 1985 Hydrothermal plumes hotsprings and conductive heat flow in the southern trough ofGuayamas Basin Earth and Planetary Science Letters v 73p 211ndash225
LUCAS S B STERN R A SYME E C REILLY B A andTHOMAS D J 1996 Intraoceanic tectonics and the developmentof continental crust 192 ndash 184 Ga evolution of the Flin Flon beltCanada Geological Society of America Bulletin 108 p 602ndash629
MacLEOD W N 1970 Peak Hill WA (1st edition) WesternAustralia Geological Survey 1250 000 Geological SeriesExplanatory Notes 21p
MARSHAK S TINKHAM D ALKMIN F BRUECKNER Hand BORNHORST T 1997 Dome-and-keel provinces formedduring Palaeoproterozoic orogenic collapse mdash core complexesdiapirs or neither examples from the Quadrilatero Ferrifero andthe Penkean orogen Geology v 25 p 415ndash418
MARSTON R J 1979 Copper mineralization in Western AustraliaWestern Australia Geological Survey Bulletin 13 208p
MARTIN D McB 1992 Turbidite facies and depositionalenvironment of the Precambrian Labouchere Formation PadburyGroup Western Australia Geological Society of AustraliaAbstracts 32 p 168ndash170
MARTIN D McB 1994 Sedimentology sequence stratigraphy andtectonic setting of a Palaeoproterozoic turbidite complex LowerPadbury Group Western Australia University of Western AustraliaPhD thesis (unpublished)
MARTIN D McB 1998 Lithostratigraphy and structure of thePalaeoproterozoic Padbury Group Milgun 1100 000 sheet WesternAustralia Western Australia Geological Survey Report 62 57p
McDONALD I R 1994 Final Report on the Glengarry nickel projectES502 and E51384 Western Australia Geological SurveyM-series Item 7706 A41555 (unpublished)
McMILLAN N M 1993 Structure metamorphism alteration andtiming of gold mineralisation at Marymia Gold Project in theMarymia Dome in An international conference on crustal evolutionmetallogeny and exploration of the Eastern Goldfields ExtendedAbstracts compiled by P R WILLIAMS and J A HALDANEAustralian Geological Survey Organisation Record 199354p 243ndash244
McPHIE J DOYLE M and ALLEN R 1993 Volcanic texturesHobart Tasmanian Government Printing Office 198p
MEFFRE S AITCHISON J C and CRAWFORD A J 1996Geochemical and tectonic significance of boninites and tholeiitesfrom the Koh Ophiolite New Caledonia Tectonics v 15p 67ndash83
MOUNTFORD B R 1984 Preliminary geological report onProspecting Licences 52104 and 52105 Mt Padbury area WesternAustralia Western Australia Geological Survey M-series Item3688 A16393 (unpublished)
MYERS J S 1989 Thrust sheets on the southern foreland of theCapricorn Orogen Robinson Range Western Australia WesternAustralia Geological Survey Report 26 Professional Papersp 127ndash130
MYERS J S 1990 Capricorn Orogen in Geology and mineralresources of Western Australia Western Australia GeologicalSurvey Memoir 3 p 197ndash198
MYERS J S 1993 Precambrian history of the West Australian cratonand adjacent orogens Annual Reviews of Earth and PlanetaryScience v 21 p 453ndash485
MYERS J S SHAW R D and TYLER I M 1996 Tectonicevolution of Proterozoic Australia Tectonics v 15 p 1431ndash1446
NELSON D R 1997 Compilation of SHRIMP UndashPb zircongeochronology data 1996 Western Australia Geological SurveyRecord 19972 189p
NELSON D R 1998 Compilation of SHRIMP UndashPb zircongeochronology data 1997 Western Australia Geological SurveyRecord 19982 242p
OrsquoNIONS R K PANKHURST R J and GRONVOLD K 1976Nature and development of basalt magma sources beneath Icelandand the Reykjanes ridge Journal of Petrology v 17 p 315ndash338
OCCHIPINTI S A GREY K PIRAJNO F ADAMIDES N GBAGAS L DAWES P and LE BLANC SMITH G 1997Stratigraphic revision of Palaeoproterozoic rocks of the YerridaBryah and Padbury Basins (former Glengarry Basin) WesternAustralia Geological Survey Record 19973 57p
OCCHIPINTI S A and MYERS J S 1999 Geology of the Moorarie1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 20p
OCCHIPINTI S A MYERS J S and SWAGER C P 1998aGeology of the Padbury 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes29p
OCCHIPINTI S A SHEPPARD S NELSON D R MYERS J Sand TYLER I M 1998b Syntectonic granite in the southernmargin of the Palaeoproterozoic Capricorn Orogen WesternAustralia Australian Journal of Earth Sciences v 45 p 509ndash512
OCCHIPINTI S A SHEPPARD S and TYLER I M 1999Palaeoproterozoic tectonic evolution of the southern margin of theCapricorn Orogen Western Australia Last Conference of theMillenium Halls Gap WA Abstract volume p 173ndash174
OCCHIPINTI S A SWAGER C P and PIRAJNO F 1998cStructuralndashmetamorphic evolution of the Palaeoproterozoic Bryahand Padbury Groups during the Capricorn Orogeny WesternAustralia Precambrian Research v 90 p 141ndash158
PARKER T W H and BROWN T 1990 Horseshoe goldndashcopperndashsilver deposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 671ndash675
PEARCE J A ERNEWEIN M BLOOMER S H PARSON L MMURTON B J and JOHNSON L E 1995 Geochemistry ofLau Basin volcanic rocks influence of ridge segmentation and arcproximity Geological Society Special Publication v 81p 53ndash75
PEARCE T H GORMAN B E and BIRKETT T C 1977 Therelationship between major element chemistry and tectonicenvironment of basic and intermediate volcanic rocks Earth andPlanetary Science Letters v 36 p 121ndash132
PERILYA MINES NL 1998 Annual report for the year ending30 June 1998 60p
PETERS S G 1993 Polygenetic meacutelange in the Hodgkinsongoldfield Northern Tasman Orogenic Zone Australian Journal ofEarth Sciences v 40 p 115ndash129
PIRAJNO F 1996 Models for the geodynamic evolution of thePalaeoproterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1995ndash96 p 96ndash103
PIRAJNO F and ADAMIDES N G 2000 Geology andmineralization of the Palaeoproterozoic Yerrida Basin WesternAustralia Western Australia Geological Survey Report 60 43p
51
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
PIRAJNO F and ADAMIDES N G 1998 Geology of the Thaduna1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 24p
PIRAJNO F ADAMIDES N G and FERDINANDO D D 1998aGeology of the Glengarry 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes16p
PIRAJNO F ADAMIDES N G OCCHIPINTI S A SWAGERC P and BAGAS L 1995a Geology and tectonic evolution ofthe early Proterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1994ndash95 p 71ndash80
PIRAJNO F BAGAS L SWAGER C P OCCHIPINTI S A andADAMIDES N G 1996 A reappraisal of the stratigraphy of theGlengarry Basin Western Australia Western Australia GeologicalSurvey Annual Review 1995ndash96 p 81ndash87
PIRAJNO F and DAVY R 1996 Mafic volcanism in thePalaeoproterozoic Glengarry Basin Western Australia andimplications for its tectonic evolution Geological Society ofAustralia Abstracts no 41 p 343
PIRAJNO F and OCCHIPINTI S A 1995 Base metal potential ofthe Palaeoproterozoic Glengarry and Bryah Basins WesternAustralia Recent developments in base metal geology andexploration Australian Institute of Geoscientists Bulletin 16p 51ndash56
PIRAJNO F and OCCHIPINTI S A 1998 Geology of the Bryah1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 41p
PIRAJNO F OCCHIPINTI S LE BLANC SMITH G andADAMIDES N G 1995b Pillow lavas in the Peak Hill terranesWestern Australia Geological Survey Annual Review 1993ndash94p 63ndash66
PIRAJNO F OCCHIPINTI S A and SWAGER C P 1998bGeology and tectonic evolution of the Palaeoproterozoic BryahPadbury and Yerrida Basins (formerly Glengarry Basin) WesternAustralia Precambrian Research v 90 p 119ndash140
PIRAJNO F and PRESTON W A 1998 Mineral deposits of thePadbury Bryah and Yerrida Basins in Geology of Australian andPapua New Guinean mineral deposits edited by D A BERKMANand D H MACKENZIE Australasian Institute of Mining andMetallurgy Monograph 22 p 63ndash69
RAYMOND L A 1984a Classification of meacutelanges GeologicalSociety of America Special Paper 198 p 7ndash20
RAYMOND L A 1984b Meacutelanges their nature origin andsignificance Geological Society of America Special Paper 198170p
ROLLINSON H R 1993 Using geochemical data evaluationpresentation interpretation Singapore Longman 352p
SABMINCO ANNUAL REPORT 1994 Annual report on miningleases M52202ndash203 vol 1 2 and 3 Western Australia GeologicalSurvey M-series Item 8967 A42856 (unpublished)
SCHILLING J-G 1982 Galapagos hot spot ndash spreading centersystem 1 Spatial petrological and geochemical variations (83degWndash101degW) Journal of Geophysical Research v 87p 5593ndash5610
SCHILLING J-G MEYER P S and KINGSLEY R H 1982Evolution of the Iceland hot spot Nature v 296 p 313ndash320
SHEPPARD S and SWAGER C P 1999 Geology of the Marquis1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 21p
SHEPPARD S OCCHIPINTI S A NELSON D and TYLERI M 1999 Granites of the southern Capricorn Orogen WesternAustralia Geological Society of Australia Abstracts no 56p44-46
SOFOULIS J 1970 Iron deposits of the Robinson Range Peak HillGoldfield WA Western Australia Geological Survey Record19706 10p
SPEAR F S 1993 Metamorphic phase equilibria and pressurendashtemperaturendashtime paths Mineralogical Society of AmericaMonograph p 799
STERN R A SYME E C and LUCAS S B 1995 Geochemistryof 19 Ga MORB and OIB-like basalts from the Amisk collageFlin Flon belt Canada evidence for an intra-oceanic originGeochimica et Cosmochimica Acta v 59 p 3131ndash3154
SUBRAMANYA A G FAULKNER J A SANDERS A J andGOZZARD J R 1995 Geochemical mapping of the Peak Hill1250 000 sheet Western Australia Geological Survey 1250 000Regolith Geochemistry Series Explanatory Notes 59p
SUN S-S 1982 Chemical composition and origin of the Earthrsquosprimitive mantle Geochimica et Cosmochimica Acta v 46p 179ndash192
SUN S-S 1997 Chemical and isotopic features of Palaeoproterozoicmafic igneous rocks of Australia implications for tectonic processesAustralian Geological Survey Organisation Record 19974p 119ndash122
SWAGER C P and MYERS J S 1999 Geology of the Milgun1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 27p
THORNETT S E 1995 The nature origin and timing of goldmineralization in Proterozoic rocks of the Peak Hill District WAUniversity of Western Australia MSc thesis (unpublished)
TYLER I M 1999 Palaeoproterozoic orogeny in Western AustraliaGeological Society of Australia Abstracts no 56 p 47ndash49
TYLER I M PIRAJNO F BAGAS L MYERS J S andPRESTON W A 1998 The geology and mineral deposits of theProterozoic in Western Australia Australian Geological SurveyOrganisation Journal of Geology and Geophysics v 17p 223ndash244
TYLER I M and THORNE A M 1990 The northern margin ofthe Capricorn Orogen Western Australia mdash an example of anEarly Proterozoic collision zone Journal of Structural Geologyv 12 p 685ndash701
WANG P and GLOVER L 1992 A tectonic test of the mostcommonly used geochemical discriminant diagrams and patternsEarth Science Reviews v 33 p 111ndash131
WATKINS K P 1983 Petrogenesis of Dalradian albite porphyroblastschists Journal of the Geological Society of London v 140p 601ndash618
WHITFIELD G B 1987 Wilgeena gold mine Progress report MS52111 and 112 Western Australia Geological Survey M-seriesItem 5862 A28194 (unpublished)
WINDH J 1992 Tectonic evolution and metallogenesis of the EarlyProterozoic Glengarry Basin Western Australia University ofWestern Australia PhD thesis (unpublished)
52
Pirajno et al
Appendix
Gazetteer of localities
Locality AMG coordinateEasting Northing
5 Mile Well 616500 7158100Beatty Park Bore 632200 7163500Cashman opencut 662129 7126994Dandy Well 646400 7188740Despair Bore 625300 7169600Durack prospect 670440 7150520Durack Well 671600 7143000Fortnum mine 636372 7197627Friday Pool 558620 7178625Harmony (New Baxters Find) opencut 664145 7161267Heines Find prospect 682759 7145164Horseshoe Lights opencut 662648 7193894Horseshoe Mn mine 656990 7186510Horseshoe Au prospect 661219 7182977Jubilee mine 671889 7165443Labouchere mine 627730 7204710Livingstone mine 567540 7171032Lucky Call prospect (Ruby Well group) 676747 7127188Mikhaburra (Holdens Find) opencut 656252 7130396Millidie (Elsa) deposit 643000 7160000Mount Fraser 639200 7163300Mount Labouchere 630360 7212620Mount Padbury 627400 7164100Mount Padbury mine 635100 7165100Mount Pleasant opencut 674287 7161900Mount Seabrook mine 572631 7168338Nathan Bitter mine 631100 7199820Nathans Deep South mine 631713 7198812Peak Hill opencut 672190 7163003Peak Hill townsite 673000 7163150Randell Bore 688000 7145200Ravelstone Group 669000 7167500Ravelstone opencut (Mn) 665734 7166777Ravelstone opencut (Mn) 669313 7166423Ruby Duffer Well 675290 7136000Ruby Well group 677900 7129700St Crispin prospect 691358 7158940Tank Well 675400 7147000Top Dimble Well 616600 7167600Trevs (and Starlight) opencut 636412 7198887Trillbar Homestead 576023 7170846Wembley mine 663983 7149044Wilgeena (Hit or Miss) mine 685369 7155622Wilthorpe mine 630414 7176521Yarlarweelor opencut 636723 7196423
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting
The Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collisionzone between the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains maficndashultramafic igneous rocks turbidites and chemical sedimentary rocks formed duringback-arc sea-floor spreading and rifting on the northern margin of the Yilgarn Cratonat or near a mid-oceanic ridge The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of theBryah Basin as a foreland structure resulting from either thec 1800 Ma oblique collision of the Pilbara and YilgarnCratons (Capricorn Orogeny) or the c 2000 Ma collisionof the Glenburgh Terrane and the Yilgarn Craton (GlenburghOrogeny) Important mineral deposits include orogenicgold-only lode deposits copperndashgold volcanogenic massivesulfides sedimentary and lateritic manganese and iron oreThe origin of the gold mineralization is related tometamorphism and deformation linked to the CapricornOrogeny at c 18 Ga The formation of other deposits isrelated to pre-orogenic syngenetic processes
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone (08) 9222 3459 Fax (08) 9222 3444wwwdmewagovau
Wandery
Creek
Wandery
Gum
Creek
Beda
burra
Easter
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eek
Dim
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Dimble
Cree
k
Mt Fr
aser
Creek
Creek
Mt Fraser
Millidie CreekMURCHISONRIVER
MURCHISON
RIVER
GASCOYNE
RIVE
R
GASCOYNE
RIVER
Ck
Cree
k
Creek
Beatty Park B (abd)
Reefer W(abd)
YARLAR
WEELOR
MILGUN
ROAD
MEEKATHARRA
ROAD
ASHBURTON DOWNS
TrillbarYarlarweelor
ROADTRILLBAR
Mt Padbury
Yd
Yd
Yd
Yd
Yd Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd
MT CLARE
MEEKATHARRA
ROAD
Bryah
Narracoota
Old Peak Hill (ruin)
Mikhaburra
Yd
Yd
Yd
Yd
(ruin)Bilyuin Hotel
Yulga Jinna Community
Doolgunna
Yd
YdYd
Yd
THADUNACOPPER MINE ROAD
Yd
Karalundi
Yd
Yd
Yd
Yd
Bryah
Yd
Mikhaburra
Yarla
rwee
lor H
omes
tead
44
km
Milgun Homestead 4 km
Milgun Homestead 72 km
Meekatharra 108 km
Meekatharra 53 km
Mooloog
ool Ho
mestead
35 km
Diamond
Well
Homest
ead 68
km
Neds
Creek
Homest
ead 33
km
Kumerina Homestead 98 km
Three Rivers Homestead 42 km
MT LABOUCHERE
MT ARAPILES
CM 15
MT BEASLEY
MT SEABROOK
TALB
OT
DIVIDE
RED HILL
722 m
Yd
Yd
Yd
Yds
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd Yd
Yd
Yd
Yd
Yd
628 m
MT PADBURYMT FRASER
MT MAITLAND
R O B I N S O N
591 m
695 m
799 m
Yd
Yd
GREAT
NORTH
ERN
HIGH
WAY
HILL
THRE
E RIVER
S
ROAD
PEAK
MEEKATHARRA
ROAD
ROAD
PEAK HILL
R A N G E
Peak Hill
MC 14
NOONYEREENA HILL
MT LEAKE
MC 13
MC 12
MC 11
ASHBURTON DOWNS
core yard
602 m
605 m
640 m
Peak Hill
Yd
Earrie W Daulby W
Jilly Jilly W
Outcamp W (abd)
Watt W
Curly W
B
6 Mile B4 Corners W
Laurel W (abd)Bull W
Labouchere W
Sam W
Duffey W
Horseshoe W
Dandy W (PD)(abd)
Carlyon B (PD)
Kinder B (PD)
Vacation B
Garret W
Kylie B
Camel B
W (abd)Billarra W
Bull Paddock WAlarm B
Carlyon RH (PD)
Yaddyarra W
Mowara BGullgogo B
Horseshoe No 2 W (PD)Horseshoe No 1 W (PD)
Stink W (PD)
Crain B
Windalah B
Yandinhah W
Coomballey B
No 1 B
4 Corners W (abd)
Cement Tank W (abd)
Cork Tree B
Southern Cross W3 Corners B
Thompson B (abd)
W (abd)
Tommy B
Seabrook W17 Mile W (abd)
Midnight B
Gidgie WW (abd)
Snake W Dry W
Black Hill W
Minniarra W
Top Minniarra W
Doherty W
The Hut W
W
Red Hill W
Randall W
Dooley W
Walebie W
Mandora B
Babbawiri Pool
Winja B
WHWH
PBedaburra P
Friday P
Kerba P
S
Wandery P
W
Valley B
Quartz B
House WSouthern Cross W
P
Peak Hill B Shed W
Boundary B
No 3 W
McPherson B
Pinnacle B
WH
Mt Leake B
Hill B
Jack W
W
Mt Leake B
John B
No 2 B
Cow Hole B
WH
Red B
WH
No 6 W
Marck W
No 11 W
Limestone W
Dummy B
No 1 B
No 8 B
D
Government W
Central B
Gale W
W
West W
No 6 B
Ealgareengunna WH
Noonyereena P
Beefwood T
Narracoota B
WH
WH
Railway B
Meek W32 Mile W (Govt)
32 Mile W
Ruby W
Ruby South W
W (abd)
Scotty W
Ord W
Little Mill B
Killarney W
West WMillie W
D
Ord W (abd)
W(abd)
Eastern Stock W No 8(abd)
Gigbywabby W (PD)(abd)
No1 W
Paddy B (abd)
Kelly BRelief B
Top Dimble W
Despair B
Boundary B (PD)
B (abd)
Padbury W
Govt W (abd)
Bottom Dimble WHaystack W
Wandarrie W
Middle B
W
WW
W
No 3 B
Fish Pond B
Wooly Paddock B
5 Mile W
Knox W
Sleepy Hollow W (abd)
Old Homestead WB
Widespread W
W
Kennedy W
W
Deep W
Ross B
Gibbywabby WDandy W (PD)
Brunsden W
17 Mile WBrown Creek B (abd)
7 Mile BDavid W
17 Mile B (PD)
Lefeuvre W
Mick W
W (abd)
WH
WHWH
WH
WH
WH WH
S
Gum W (abd)
Wilthorpe W (PD)
1 Mile W
Bullgullan B
Wongawar B
Jinglegunna W
No 13 B
Orchard W
Fraser WW
Sorenson B
Central B
Tank W (abd)Bitter W (abd)
Murphy W
Trudgeon W
Moore W Spelling W
Randell B
Deadhorse W (abd) McLean W
Bore Hole BOHara W
Murchison W (abd)
McCarthy W2 Tank W (abd)
Hill W
Telegraph W
Cashman B (abd)
Ruby Centre W
White WW
McCann W (abd)
Holden W
Gum W
McDonald W
Don BNo 2 BNo 1 B
Bull W
D
D
DD
Gum Well P
Malleah P
Fremanga P
Yallaginda W (abd)
No 7 B (abd)
Stalley W (abd)
Durack W
No 26 W (abd)
Ruby Duffer W (abd)
WHs
WHs
WHWH
WH
WHWH
WH
P
PP
P
P
P
P
P
P
P
P
P
Ruby W (abd)
Narracoota W (abd)
WH S
P
B W
D T
(abd) (PD)
Cheroona W(abd)
Ti Tree B
56ocircocircocircocircYacute E 58 62 64 66 68 72
icirc12ocircocircocircocircYacute N
14
16
18
20
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icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
74ocircocircocircocircYacute E7060
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3
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3 3
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3
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30
85
8035
54
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63
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87
66
70
60
7075
88
8081
4
4
4
4 44 4
4
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3
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81 83
80
7872
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33
3
4
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71
78
73
47
25
85
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70
2
2
48
62
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4785
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60
60
70
85
15
72
80
60
32
85
60
6030
3565
4
4
4
2 2
4
4
3
3
3
4
3
3
2
42
2
4
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86
86
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8570 70
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E
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118956
142851
88YacuteEcirc168
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Yarlarweelor
Horseshoe
NathanDeep
Mt Seabrook
Labouchere
Wilthorpe
Wilgeena
Wembley
Livingstone
Harmony
Jubilee
Peak HillMt Pleasant
St Crispin
Durack
Heines Find
Mikhaburra
Cashman
Horseshoe Lights
Horseshoe
Yarlarweelor
Mn
T
MnMn
CuAu
Cu
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Mn
T
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HOLDENS
BAXTER
RAVELSTONE
PEAK HILL
HORSESHOE
HOLDENS
Ruby Well
Fortnum
Fortnum
M U R C H I S O N M I N E R A L F I E L D
M E E K A T H A R R A D I S T R I C T
P E A K H I L L M I N E R A L F I E L D
Goodin Fault Murchison Fault
Goodin Fault Murchison Fault
thrust
latera
l ramp
Billara Fault Kinders Fault
NARRYER
TERRANE
YILGARN
CRATON
Goodin F
ault
GOODIN
INLIER
Jenkin
Fault
Fault
Goodin
MARYMIA
INLIER
thrust ramp
Robinson Syncline
Peak Hill Anticline
Peak Hill Anticline
Horseshoe Anticline Millidie Syncline
Yarlarweelor gneiss belt
Marymia Inlier
40
MOUNT LEAKE FORMATION quartz arenite
DESPAIR GRANITE foliated to locally massive coarse-grained biotite granite late Archaean
30 km
Bangemall Group
Earaheedy Group
Padbury Group
Bryah Group
Mooloogool SubgroupDoolgunna_Thaduna Formations
Windplain Subgroup
Geological boundary
Fault
Finlayson Member quartz arenite
117frac34Yacute30Agrave
25frac34Yacute00Agrave
45Agrave118frac34Yacute00Agrave 15Agrave 30Agrave 45Agrave 119frac34Yacute00Agrave 15Agrave 119frac34Yacute30Agrave
25frac34Yacute00Agrave
15Agrave
30Agrave
45Agrave
26frac34Yacute00Agrave
26frac34Yacute10Agrave
119frac34Yacute30Agrave15Agrave119frac34Yacute00Agrave45Agrave15Agrave 30Agrave
118frac34Yacute00Agrave45Agrave117frac34Yacute30Agrave
26frac34Yacute10Agrave
26frac34Yacute00Agrave
45Agrave
30Agrave
15Agrave
Proterozoic granite
Q TR S
SEA LEVEL
5 km
11 km
F G
SEA LEVEL
5 km
11 km
L M O
SEA LEVEL
5 km
11 km
N
J K
SEA LEVEL
5 km
10 km
10 km
SEA LEVEL
5 km
H I
Archaean granitoid rock and greenstone
YerridaGroup
Maraloou_Killara Formations
SEA LEVEL
5 km
10 km
C D E
SEA LEVEL
5 km
10 km
A B
MILLIDIE CREEK FORMATION sandstone and shale minor granular iron-formation
ROBINSON RANGE FORMATION ferruginous shale and siltstone minor banded iron-formation
Beatty Park Member chloritic siltstone sandstone and breccia numerous mafic volcanic fragments
Heines Member quartz wacke siltstone and shale with minor polymictic conglomerate
LABOUCHERE FORMATION quartz wacke and siltstone local quartz pebble conglomerate layers turbiditic
KARALUNDI FORMATION sandstone with minor shale and conglomerate
JOHNSON CAIRN FORMATION siltstone and shale minor sandstone
JUDERINA FORMATION quartz wacke siltstone quartz arenite and quartz pebble conglomerate
PEAK HILL SCHIST quartz muscovite schist mylonitic schist and phyllonite
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS REPORT 59 PLATE 1
2
Trillbar Complexwith local magmatic layering well-preserved
interleaved foliated and metamorphosed basalt gabbro microgabbro pyroxenite and serpentinized peridotite
HORSESHOE FORMATION ferruginous chloritic shale and quartzEcircfeldspar wacke partly manganiferous andcalcareous minor iron-formation and chert
BANGEMALL
EARAHEEDY
PADBURYBASIN
BASINBRYAH
YERRIDABASIN
WILTHORPE FORMATION quartz pebble to boulder conglomerate predominant vein quartz clasts and some chert quartz wackeand granitoid rock clasts quartz wacke and finely bedded siltstone locally chloritic graded beds
1 2 3 4
C
58
78
75
20
15
SHEET INDEX
intruded by granite during the Capricorn Orogeny
High-grade gneissic granite and granite foliated derived predominantly from biotite monzogranite with numerouslenses of supracrustal rocks early middle and late Archaean components overprinted by structures and
NARRACOOTA FORMATION metabasalt and maficEcircultramafic schist locally pillowed with interflow sedimentary layers
Capr
icorn
Oro
geny
Mar
ymia
Inlie
r_re
work
ed d
uring
the
met
amor
phism
_Ca
prico
rn O
roge
nyup
per g
reen
schist to
lowe
r am
phib
olite
facie
s
gree
nsto
ne b
eltM
ount
Mai
tland
2672YacuteucircYacute3
lt1996YacuteucircYacute35
High-grade granitic gneiss derived predominantly from biotite monzogranite with numerous lenses ofsupracrustal rocks early middle and late Archaean components includes Palaeoproterozoicgranite sheets and dykes extensively deformed during Capricorn Orogeny
SCHEMATIC TECTONIC RELATIONSHIPS
BANGEMALL BASIN
1600 Ma and youngerc
EARAHEEDY BASIN
2000 Ma and youngercBRYAH BASIN
2000 Mac
YERRIDA BASIN
2200 Ma and youngerc
YILGARN CRATON
2600 Ma and olderc
PADBURY BASINyounger than 2000 Ma
BASIN
BASIN
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WA
NT
SA
NSW
Vic
Qld
Tas
ACT
GEOLO
G IC A L SUR VEY
WE
ST
E R N A U S T R AL
IA
GEOLOGICAL SURVEY OF
WESTERN AUSTRALIA
DAVID BLIGHT DIRECTOR
DEPARTMENT OF MINERALS
AND ENERGY
L C RANFORD DIRECTOR GENERAL
GOVERNMENT OF WESTERN AUSTRALIA
HON NORMAN MOORE MLC
MINISTER FOR MINES
Bangemall Group undivided
Mafic dyke interpreted from aeromagnetic data + positive anomaly - negative anomaly
Granite includes muscovite-bearing leucogranite and pegmatite
Padbury Group undivided metamorphosed and variably foliated metasedimentary rocks
Iron-formation and chert
Banded iron-formation minor ferruginous sandstone and shale
Bedded dolomite and dolomitic siltstone
Granular iron-formation
Banded iron-formation
Banded iron-formation and ferruginous chert
Quartz arenite minor interleaved quartz wacke and siltstone
Iron-formation and quartzEcircmagnetite(Ecircstilpnomelane) schist garnetiferous white chert in lenses
lithic wacke and siltstone turbiditic
Chert
Felsic schist derived from felsic volcanic and volcaniclastic rockDolerite in sills and dykesBasaltic hyaloclastiteMetaperidotite and picrite ultramafic schistBasaltic vent brecciaJasperoidal chert
Quartz mylonite
Foliated to mylonitic and massive granitoid rock
Amphibolite
Banded iron-formation
Granite with minor greenstone locally overprinted by structures formed during Capricorn Orogeny
Basalt ultramafic rock dolerite felsic schist banded iron-formation and chert
RAVELSTONE FORMATION
MES
OPRO
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ZOIC
PALA
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CAR
CHAE
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Bang
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PADB
URY
BASI
N
Undivided MARALOOU DOOLGUNNA THADUNA and KILLARA FORMATIONS
Contact Bryah Group_Padbury Group
Structural symbols are numbered according totheir age of formation where known
Middle Proterozoic
Early Proterozoic
interpreted movement
Fold showing direction of plunge
Small-scale fold axial surface showing strike and dip
Bedding showing strike and dip
Foliation showing strike and dip
Lineation showing direction of plunge
Single zircon UEcircPb SHRIMP geochronology data
Nutman A P Bennett V C Kinny P D and Price R 1993 Large scale crustalstructure of the northwestern Yilgarn Craton Western Australia evidence fromNd isotopic data and zircon geochronology Tectonics v12 p 971-981
Nelson D R 1997 Geological Survey of Western Australia Record 19972
Nelson D R in prep Geological Survey of Western Australia Record 19982Mineral occurrence
Edited by D Ferdinando and G Loan
Cartography by P Taylor and B Williams
Topography from the Department of Land Administration Sheets SG 50-7 -8 -11 -12with modifications from geological field survey
Published by the Geological Survey of Western Australia Copies available fromthe Information Centre Department of Minerals and Energy 100 Plain StreetEast Perth WA 6004 Phone (08) 9222 3459 Fax (08) 9222 3444
This map is also available in digital form
Printed by the Sands Print Group Western Australia
The recommended reference for this map isSWAGER C P OCCHIPINTI S A and PIRAJNO F 1998 Interpreted Geology of thePalaeoproterozoic Bryah and Padbury Basins Western Australia Geological Survey Report 59 Plate 1
Unconformity (section only)
unconformity with local major onlap reworked as a fault
Geological boundary
Edmund fold belt unspecified
Capricorn Orogeny unspecified
Capricorn Orogeny DOtilde DUcirc Dccedil Deacute
Fault
Reactivated normal fault
lateral (plan view) dip slip (section)
away from observer
Strongly foliated rock
anticline
syncline
overturned anticline
overturned syncline
towards observer
Minor fold showing direction of plunge
inclined
vertical
inclined
vertical
overturned
bedding or layering trend
inclined
vertical
trend (section only)
GSWA identification number
mineral lineation
intersection lineation
Nutman et al identification number
interpreted age of intrusion in Ma with reference number
youngest detrital zircon
Highway with national route marker
Formed road
Track
Landing ground
Townsite population less than 1000
Mineral field boundary
Homestead
Locality
Building yard
Microwave repeater station
Horizontal control major
Watercourse ephemeral pool
Waterhole spring
Bore well windpump
Dam tank
Abandoned position doubtful
Mining centre
Mining locality
Mine (gold unless otherwise indicated)
Major opencut
Opencut
Alluvial workings
Prospect
Copper
Gold
Manganese
Talc
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
0 5 10 15 20 255000
Metres Kilometres
VERTICAL DATUM AUSTRALIAN HEIGHT DATUM
SCALE 1Yacute250Yacute000
Grid lines indicate 20Yacute000 metre interval of the Map Grid Australia Zone 50
HORIZONTAL DATUM GEOCENTRIC DATUM OF AUSTRALIA 1994UNIVERSAL TRANSVERSE MERCATOR PROJECTION
The Map Grid Australia (MGA) is based on the Geocentric Datum of Australia 1994 (GDA94)
GEOCENTRIC DATUM OF AUSTRALIA
GDA94 positions are compatible within one metre of the datum WGS84 positions
Reference points to align maps based on the previous datum AGD84 have been placed near the map corners
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS
2344
2345
2346
2347
2444
2445
2446
2447
2544
2545
2546
2547
2644
2645
2646
2647
2744
2745
2746
2747
2844
2845
2846
2847
KALLI
MILEURA
GOULD
ERRABIDDY
MADOONGA
KOONMARRA
MOORARIE
MARQUIS
MEEKATHARRA
TIERACO
PADBURY
MILGUN
GABANINTHA
GLENGARRY
BRYAH
JAMINDI
YAGANOO
MOOLOOGOOL
DOOLGUNNA
MEREWETHER
THADUNA
MARYMIA
MOUNT BARTLE
THREE RIVERS
118958
88YacuteEcirc168
BELELE GLENGARRY
ROBINSON RANGE PEAK HILL
SG 50-7 SG 50-8
SG 50-11 SG 50-12
1100Yacute000 maps shown in black
Compiled by C P Swager S A Occhipinti and F Pirajno 1997
N
P
Geology from 1100Yacute000 GSWA maps (see sheet index)
See current GSWA map catalogue for the full range of published products
and by S A Occhipinti C P Swager 1995 1997 and J S Myers 1995
Published 1100Yacute000 maps used in compilation
1250Yacute000 maps shown in brown
+ means declination is east and correction must be
subtracted from compass bearing to give true bearing
Annual change is 1Agrave easterly
The lines indicate magnetic declination 1995
added to compass bearing to give true bearing
- means declination is west and correction must be
SEA LEVEL
5 km
11 km
brvbar Western Australia 1998
117frac34 30Agrave25frac3400Agrave
118frac3400Agrave 119frac3400Agrave 120frac3400Agrave
26frac3400Agrave
INTERPRETED GEOLOGY OF THE PALAEOPROTEROZOIC
AREA OF THIS MAP
GSWA
REPORT 60
PLATE 1
E
Version 11 _ May 2004
Q
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lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
2672YacuteucircYacute32
1808YacuteucircYacute6
3
cc 3300
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lt1996YacuteucircYacute352
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
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2672YacuteucircYacute32
- Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
-
- Contents
- Abstract
- Introduction
- Regional tectonic setting
- Geology stratigraphy and geochronology
-
- Peak Hill Schist and Marymia Inlier
- Bryah Group
-
- Karalundi Formation
- Narracoota Formation
-
- Peridotitic and high-Mg basalt association
- Intrusive rocks and layered intrusions
- Mafic and ultramafic schist
- Metabasaltic hyaloclastite
- Felsic schist
- Volcaniclastic rocks
- Carbonated and silicified metavolcanic rocks
- Jasperoidal chert
- Geochemistry of the Narracoota Formation
-
- Ravelstone Formation
- Horseshoe Formation
-
- Padbury Group
-
- Labouchere Formation
- Wilthorpe Formation
-
- Beatty Park and Heines Members
-
- Robinson Range Formation
- Millidie Creek Formation
- Unassigned units of the Padbury Group
-
- Structure
-
- D1 structures
- D2 structures
- D3 structures and their relationship to D2 structures
- D4 structures
-
- Metamorphism
- Structural synthesis
- Mineralization
-
- Gold deposits
-
- Peak Hill Jubilee and Mount Pleasant deposits
- Harmony deposit
- Labouchere Nathans and Fortnum deposits
- Wembley deposit
- Wilgeena deposit
- Durack St Crispin and Heines Find prospects
- Ruby Well group
- Mikhaburra deposit
- Wilthorpe deposit
- Cashman deposit
-
- Volcanogenic copperndashgold deposits
- Supergene manganese deposits
- Iron ore
- Talc
- Discussion
-
- Tectonic model and conclusions
- Acknowledgements
- References
- Appendix Gazetteer of localities
- Plate 1 Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
- Figures
-
- Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
- Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins
- Figure 3 Rotated orthoclase porphyroblast Peak Hill Schist
- Figure 4 Partially recrystallized mylonite Peak Hill Schist
- Figure 5 Peak Hill Schist mylonite from the Hangingwall Sequence
- Figure 6 Outcrop of quartz mylonite Peak Hill Schist
- Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric
- Figure 8 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt)
- Figure 9 Basaltic hyaloclastite Narracoota Formation
- Figure 10 Mafic volcaniclastic rock Narracoota Formation
- Figure 11 Volcanic breccia intersected in diamond drillhole BD1
- Figure 12 Total alkali versus silica diagram for rocks the Narracoota Formation
- Figure 13 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the Narracoota Formation
- Figure 14 Geochemical characteristics of the Narracoota Formation rocks
- Figure 15 Geochemical discriminant plots for Narracoota Formation
- Figure 16 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation
- Figure 17 Schematic stratigraphy of the Horseshoe Formation
- Figure 18 Major regional structures in the Bryah and Padbury Groups
- Figure 19 Simplified geological map of the Bryah and Padbury Groups
- Figure 20 Selected hypothetical cross sections through the Bryah and Padbury Groups
- Figure 21 Model of the structural development of the BryahndashPadbury Group succession
- Figure 22 New model of the structural development of the BryahndashPadbury Group succession
- Figure 23 New model for the structural development of the BryahndashPadbury Group succession and the Peak Hill Schist
- Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins
- Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins
- Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH 1100 000 map sheet
- Figure 27 Albite porphyroblasts in mylonitic schist at Mount Pleasant
- Figure 28 The Mine Sequence schist
- Figure 29 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit
- Figure 30 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and Marker quartzite unit
- Figure 31 Diagrammatic cross section of the Harmony ore zones
- Figure 32 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and deformed Despair Granite
- Figure 33 Sketch illustrating a conceptual model for the origin of precious and base metal deposits in the BryahndashPadbury and Yerrida Basins
- Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins within the context of the Capricorn Orogen
-
- Tables
-
- Table 1 Stratigraphy of the Bryah and Padbury Groups
- Table 2 Representative chemical analyses of the Narracoota Formation
- Table 3 Magnesium numbers for the Narracoota and Killara Formations
- Table 4 Selected geochemical parameters for the Narracoota Formation
- Table 5 Sequence of deformation events in the Bryah and Padbury Basins
- Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group and deformation fabrics
- Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
- Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
- Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
-
GEOCHEMICAL ANALYSES OF ROCKS FROM THE NARRACOOTA FORMATION For details of analytical techniques see in text of Report 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
Sample | Easting | Northing | SiO2 | TiO2 | Al2O3 | Fe2O3 | FeO | MnO | MgO | CaO | Na2O | K2O | P2O5 | LOI | H2O- | H2O+ | TOTAL | CO2 | Ag | As | Au | Ba | Bi | Cd | Ce | Cr | Co | Cu | Ga | Ge | La | Li | Mo | Mn | Nb | Ni | Pb | Pd | Pt | Rb | Sb | Sc | Sn | Sr | Ta | Te | Th | Ti | U | V | Y | W | Zn | Zr | Hf | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm | Yb | Lu | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86342 | 746314 | 7198282 | 5151 | 032 | 1523 | 928 | 018 | 1049 | 1007 | 269 | 019 | 003 | 673 | 166 | 1 | 95 | 12 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86383 | 670171 | 7163822 | 5353 | 091 | 1468 | 115 | 019 | 744 | 863 | 299 | 005 | 008 | 253 | 100 | 1 | 85 | 21 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86384 | 670171 | 7163822 | 5048 | 062 | 1444 | 991 | 016 | 1135 | 933 | 362 | 004 | 005 | 640 | 209 | 1 | 157 | 16 | 33 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86397 | 799422 | 7201118 | 5529 | 026 | 1502 | 817 | 017 | 1136 | 416 | 549 | 005 | 002 | 1174 | 244 | 0 | 44 | 15 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104248 | 722651 | 7168587 | 4925 | 022 | 1137 | 963 | 017 | 1818 | 948 | 159 | 009 | 002 | 1 | 80 | 9 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104249 | 722651 | 7168587 | 4911 | 026 | 1065 | 973 | 017 | 2016 | 855 | 126 | 009 | 003 | 1 | 34 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104254 | 715830 | 7171470 | 4948 | 023 | 1121 | 95 | 016 | 2035 | 706 | 194 | 005 | 002 | 1877 | 647 | 1 | 49 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104255 | 715830 | 7171470 | 52 | 033 | 143 | 847 | 017 | 1071 | 1087 | 31 | 002 | 003 | 664 | 209 | 0 | 133 | 13 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256 | 715830 | 7171470 | 5244 | 067 | 1455 | 1007 | 019 | 834 | 983 | 376 | 007 | 007 | 0 | 140 | 17 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104257 | 713820 | 7171502 | 5144 | 092 | 1453 | 1078 | 02 | 689 | 1244 | 248 | 023 | 009 | 265 | 79 | 3 | 195 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104264 | 685287 | 7155494 | 5303 | 062 | 1391 | 94 | 017 | 768 | 1239 | 265 | 01 | 006 | 720 | 222 | 1 | 90 | 15 | 32 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104265 | 685287 | 7155494 | 5332 | 025 | 1592 | 97 | 017 | 658 | 1215 | 184 | 003 | 004 | 353 | 67 | 1 | 30 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104288 | 661877 | 7126843 | 5979 | 024 | 1346 | 798 | 016 | 522 | 1265 | 042 | 004 | 004 | 283 | 46 | 0 | 17 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104289 | 656054 | 7130760 | 5446 | 014 | 1559 | 955 | 017 | 826 | 957 | 204 | 019 | 003 | 358 | 116 | 4 | 43 | 8 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104292 | 657132 | 7123177 | 5103 | 09 | 1369 | 971 | 017 | 827 | 1334 | 272 | 009 | 008 | 0 | 165 | 18 | 51 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104294 | 664424 | 7119210 | 5108 | 095 | 1449 | 1021 | 018 | 879 | 1094 | 283 | 046 | 008 | 523 | 141 | 5 | 123 | 19 | 52 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104295 | 664424 | 7119210 | 5228 | 096 | 1446 | 1022 | 018 | 946 | 856 | 364 | 016 | 009 | 465 | 132 | 2 | 79 | 19 | 54 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104298 | 669014 | 7106533 | 5233 | 087 | 1367 | 939 | 017 | 778 | 1189 | 373 | 01 | 008 | 514 | 116 | 1 | 116 | 17 | 49 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104299 | 669014 | 7106533 | 5166 | 093 | 1404 | 982 | 018 | 823 | 1183 | 305 | 017 | 009 | 491 | 117 | 3 | 124 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104300 | 669014 | 7106533 | 477 | 05 | 173 | 984 | 019 | 747 | 1484 | 197 | 016 | 004 | 3 | 142 | 12 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104386 | 676392 | 7146500 | 5373 | 037 | 1501 | 846 | 016 | 864 | 977 | 373 | 009 | 004 | 557 | 152 | 0 | 106 | 18 | 18 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104391 | 687552 | 7144198 | 5002 | 023 | 845 | 934 | 016 | 2281 | 88 | 014 | 002 | 002 | 0 | 15 | 11 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104392 | 687552 | 7144198 | 5391 | 027 | 92 | 998 | 014 | 2087 | 515 | 017 | 027 | 003 | 2508 | 1103 | 12 | 16 | 22 | 10 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393 | 687539 | 7143275 | 508 | 023 | 965 | 1025 | 01 | 289 | 004 | 0 | 001 | 001 | 0 | 3 | 5 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104394 | 687539 | 7143275 | 5594 | 05 | 1494 | 867 | 019 | 73 | 697 | 537 | 006 | 006 | 363 | 88 | 0 | 90 | 19 | 24 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104397 | 670399 | 7142584 | 4687 | 019 | 1023 | 1015 | 017 | 2496 | 726 | 015 | 001 | 001 | 2786 | 971 | 0 | 7 | 8 | 4 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104398 | 669575 | 7143518 | 5329 | 035 | 1453 | 813 | 014 | 828 | 1207 | 315 | 002 | 004 | 574 | 124 | 0 | 78 | 13 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104399 | 670423 | 7144430 | 5183 | 036 | 1491 | 866 | 016 | 932 | 1147 | 323 | 002 | 003 | 682 | 173 | 0 | 42 | 14 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104400 | 670023 | 7145280 | 4958 | 037 | 1577 | 987 | 019 | 1044 | 1082 | 291 | 002 | 003 | 510 | 124 | 0 | 68 | 17 | 15 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109487 | 638809 | 7157725 | 5719 | 043 | 1423 | 73 | 013 | 868 | 626 | 569 | 004 | 004 | 442 | 116 | 0 | 18 | 11 | 19 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109492 | 663796 | 7149130 | 5231 | 011 | 617 | 72 | 015 | 24 | 1002 | 001 | 001 | 001 | 0 | 7 | 5 | 1 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109493 | 663796 | 7149130 | 5246 | 047 | 1508 | 881 | 019 | 766 | 1218 | 247 | 064 | 005 | 478 | 90 | 6 | 72 | 15 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109504 | 670124 | 7121353 | 5396 | 048 | 149 | 859 | 015 | 716 | 1237 | 231 | 003 | 005 | 445 | 96 | 0 | 61 | 17 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109513 | 732634 | 7164722 | 5396 | 197 | 1434 | 953 | 02 | 638 | 686 | 592 | 064 | 019 | 16 | 117 | 24 | 97 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601 | 668775 | 7146298 | 5332 | 179 | 1568 | 102 | 025 | 644 | 561 | 601 | 053 | 017 | 10 | 105 | 21 | 90 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112603 | 672130 | 7147178 | 108 | 034 | 2 | 1698 | lt10 | 462 | lt4 | lt5 | lt6 | 559 | 54 | 12 | lt3 | 6 | lt2 | lt7 | 115 | lt4 | 87 | 4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 167 | 19 | 92 | 203 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604 | 672238 | 7155486 | 202 | lt001 | 3 | lt4 | 40 | 34 | 8 | lt5 | 73 | 3639 | 69 | 16 | lt3 | 38 | lt2 | lt7 | 143 | 20 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | lt2 | lt2 | 453 | 29 | 20 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112620 | 626709 | 7204920 | 33 | 001 | 2 | lt4 | 220 | 35 | lt4 | lt5 | 19 | 1377 | 78 | 22 | lt3 | 25 | lt2 | 9 | 127 | 26 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | 10 | lt2 | 358 | 22 | 13 | 182 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112621 | 626709 | 7204920 | 116 | 011 | 1 | 144 | lt10 | lt11 | lt4 | lt5 | lt6 | 2354 | 82 | 8 | lt3 | lt5 | lt2 | lt7 | 1589 | lt4 | lt2 | 9 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 131 | 6 | 72 | 20 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112624 | 661284 | 7183319 | 507 | 074 | 139 | 274 | 769 | 018 | 791 | 104 | 244 | 025 | 007 | 358 | 1007 | 1 | lt4 | lt10 | 54 | lt4 | lt5 | lt6 | 186 | 92 | 13 | lt3 | lt5 | lt2 | lt7 | 96 | lt4 | 6 | lt4 | lt4 | 97 | lt5 | lt6 | lt2 | lt2 | 264 | 18 | 77 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112625 | 661284 | 7183319 | 498 | 074 | 143 | 244 | 747 | 016 | 831 | 116 | 237 | 03 | 007 | 324 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 354 | 90 | 12 | lt3 | lt5 | lt2 | lt7 | 111 | lt4 | 4 | lt4 | lt4 | 85 | lt5 | lt6 | lt2 | lt2 | 241 | 15 | 79 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112628 | 661284 | 7183319 | 49 | 08 | 138 | 357 | 726 | 018 | 738 | 14 | 143 | 008 | 007 | 277 | 1006 | 2 | lt4 | lt10 | 147 | lt4 | lt5 | 6 | 167 | 91 | 14 | lt3 | lt5 | lt2 | lt7 | 101 | lt4 | lt2 | lt4 | lt4 | 310 | lt5 | lt6 | lt2 | lt2 | 265 | 19 | 77 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112629 | 661284 | 7183319 | 642 | 049 | 103 | 271 | 402 | 012 | 438 | 113 | 051 | 013 | 005 | 18 | 1001 | lt1 | lt4 | lt10 | 109 | lt4 | lt5 | lt6 | 113 | 58 | 12 | lt3 | lt5 | lt2 | lt7 | 60 | lt4 | 2 | lt4 | lt4 | 86 | lt5 | lt6 | lt2 | lt2 | 166 | 11 | 50 | 39 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112640 | 675227 | 7128672 | 49 | 052 | 147 | 272 | 517 | 014 | 915 | 148 | 142 | 011 | 005 | 221 | 1002 | 1 | lt4 | lt10 | 90 | lt4 | lt5 | lt6 | 277 | 38 | 13 | lt3 | lt5 | lt2 | lt7 | 160 | lt4 | 2 | 5 | lt4 | 184 | lt5 | lt6 | lt2 | lt2 | 212 | 11 | 54 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112641 | 675215 | 7127749 | 508 | 079 | 142 | 308 | 703 | 017 | 744 | 118 | 207 | 012 | 008 | 299 | 1008 | 1 | lt4 | 90 | 26 | lt4 | lt5 | lt6 | 266 | 102 | 14 | lt3 | lt5 | lt2 | lt7 | 120 | lt4 | lt2 | lt4 | lt4 | 148 | lt5 | lt6 | lt2 | lt2 | 258 | 16 | 80 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643 | 675190 | 7125902 | 275 | 205 | lt1 | 10 | 40 | 767 | lt4 | lt5 | 175 | 994 | 257 | 12 | 3 | 12 | 2 | lt7 | lt3 | 34 | lt2 | lt4 | lt4 | 43 | lt5 | lt6 | lt2 | lt2 | 272 | 13 | 96 | 25 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112645 | 663956 | 7162053 | 23 | 059 | lt1 | 7 | lt10 | 227 | lt4 | lt5 | 34 | 2117 | 390 | 3 | 12 | lt2 | 8 | lt3 | 12 | lt2 | lt4 | 8 | 10 | lt5 | lt6 | 6 | lt2 | 467 | 14 | 81 | 132 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112646 | 663956 | 7162053 | 507 | 076 | 139 | 224 | 796 | 018 | 771 | 991 | 258 | 063 | 007 | 375 | 1005 | 1 | lt4 | lt10 | 164 | lt4 | lt5 | 6 | 207 | 79 | 13 | lt3 | lt5 | lt2 | lt7 | 123 | lt4 | 16 | lt4 | lt4 | 338 | lt5 | lt6 | lt2 | lt2 | 245 | 15 | 77 | 55 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112647 | 663956 | 7162053 | 356 | 002 | 1 | 133 | 1170 | lt11 | lt4 | lt5 | 13 | 489 | 846 | 6 | 4 | 6 | lt2 | lt7 | 533 | 1491 | lt2 | 4 | lt4 | lt2 | lt5 | 8 | lt2 | lt2 | 104 | 12 | 180 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112650 | 663956 | 7162053 | 573 | 424 | 959 | 166 | 036 | lt005 | 12 | 226 | 012 | 028 | 005 | 75 | 999 | 1 | lt4 | lt10 | 423 | lt4 | lt5 | 152 | 481 | 119 | 20 | lt3 | 90 | lt2 | 27 | 171 | 10 | 12 | lt4 | lt4 | 61 | lt5 | lt6 | 6 | lt2 | 365 | 37 | 54 | 296 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112652 | 663956 | 7162053 | 526 | 088 | 133 | 253 | 762 | 022 | 745 | 741 | 31 | 081 | 008 | 474 | 1009 | 1 | lt4 | lt10 | 242 | lt4 | lt5 | lt6 | 149 | 158 | 12 | lt3 | lt5 | lt2 | lt7 | 99 | 6 | 17 | 5 | lt4 | 87 | lt5 | lt6 | 2 | lt2 | 260 | 22 | 88 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112672 | 734725 | 7164593 | 628 | 07 | 136 | 355 | 364 | 034 | 337 | 494 | 286 | 093 | 009 | 313 | 1001 | 1 | lt4 | 20 | 258 | lt4 | lt5 | 76 | 122 | 16 | 17 | lt3 | 34 | lt2 | 17 | 75 | 13 | 19 | lt4 | 4 | 164 | lt5 | lt6 | 22 | 2 | 99 | 26 | 73 | 216 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 69 | 108 | 111 | 258 | 508 | 009 | 415 | 016 | 312 | 036 | 007 | 361 | 1006 | 1 | lt4 | lt10 | 386 | lt4 | lt5 | 30 | 56 | lt4 | 14 | lt3 | 18 | lt2 | 17 | 24 | lt4 | 17 | lt4 | lt4 | 79 | lt5 | lt6 | 8 | lt2 | 239 | 19 | 79 | 119 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 633 | 136 | 113 | 297 | 736 | 012 | 617 | 025 | 21 | 012 | 018 | 499 | 1004 | 1 | lt4 | 20 | 460 | lt4 | lt5 | 18 | 19 | 56 | 14 | lt3 | 10 | lt2 | 17 | 32 | 12 | 4 | lt4 | lt4 | 30 | lt5 | lt6 | 9 | 3 | 312 | 32 | 109 | 153 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 631 | 137 | 115 | 248 | 803 | 009 | 662 | 024 | 211 | lt005 | 016 | 496 | 1008 | 1 | lt4 | 20 | 28 | lt4 | lt5 | 37 | 21 | 203 | 17 | lt3 | 17 | 3 | 19 | 30 | 6 | lt2 | lt4 | lt4 | 27 | lt5 | lt6 | 9 | 3 | 336 | 24 | 107 | 158 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 129 | 697 | lt1 | 4 | 1250 | 1768 | lt4 | lt5 | 69 | 597 | 472 | 11 | lt3 | 53 | lt2 | lt7 | 327 | 22 | 90 | lt4 | lt4 | 226 | lt5 | lt6 | 8 | 2 | 181 | 19 | 118 | 101 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112675 | 734644 | 7166319 | 569 | 025 | 767 | 183 | 429 | 013 | 153 | 768 | 303 | 007 | lt005 | 396 | 1013 | 1 | lt4 | lt10 | 55 | lt4 | lt5 | lt6 | 541 | 26 | 4 | lt3 | lt5 | lt2 | lt7 | 262 | lt4 | 2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 117 | 9 | 46 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112678 | 734655 | 7166965 | 715 | 009 | 411 | 133 | 335 | 006 | 112 | 341 | 016 | lt005 | lt005 | 442 | 999 | 1 | lt4 | lt10 | 32 | lt4 | lt5 | lt6 | 1537 | 11 | 3 | lt3 | lt5 | lt2 | lt7 | 659 | lt4 | lt2 | lt4 | lt4 | 4 | lt5 | lt6 | lt2 | lt2 | 69 | 5 | 33 | 8 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112679 | 735684 | 7171472 | 518 | 034 | 135 | 289 | 531 | 014 | 945 | 12 | 267 | lt005 | lt005 | 277 | 1011 | 1 | lt4 | lt10 | 51 | lt4 | lt5 | lt6 | 670 | 56 | 12 | lt3 | lt5 | lt2 | lt7 | 272 | lt4 | lt2 | lt4 | lt4 | 60 | lt5 | lt6 | lt2 | lt2 | 198 | 16 | 55 | 21 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112680 | 735675 | 7172519 | 515 | 037 | 148 | 282 | 565 | 015 | 864 | 991 | 357 | lt005 | lt005 | 314 | 1008 | 1 | lt4 | lt10 | 83 | lt4 | lt5 | lt6 | 470 | 88 | 12 | lt3 | lt5 | lt2 | lt7 | 192 | lt4 | lt2 | 5 | lt4 | 88 | lt5 | lt6 | lt2 | lt2 | 216 | 17 | 62 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116407 | 603693 | 7169737 | 279 | lt001 | 1 | 4 | lt10 | 126 | lt4 | lt5 | 12 | 140 | 34 | lt3 | 3 | 7 | lt2 | 11 | 191 | 7 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | 3 | lt2 | 36 | 11 | 21 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116410 | 608442 | 7170499 | 211 | lt01 | lt1 | lt4 | lt10 | 726 | lt4 | lt5 | 6 | 696 | 17 | lt3 | lt3 | 5 | lt2 | lt7 | 82 | 4 | lt2 | lt4 | lt4 | 24 | lt5 | lt6 | 2 | lt2 | 40 | 5 | 10 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116415 | 611248 | 7168937 | 904 | lt005 | 265 | 094 | 095 | lt005 | 248 | 005 | 005 | lt005 | lt005 | 263 | 1005 | lt1 | 4 | lt10 | 947 | lt4 | lt5 | lt6 | 944 | 13 | lt3 | lt3 | 5 | lt2 | lt7 | 394 | lt4 | lt2 | lt4 | lt4 | 28 | lt5 | lt6 | lt2 | lt2 | 35 | 7 | 22 | lt5 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116428 | 614781 | 7170999 | 484 | 016 | 723 | 188 | 628 | 014 | 215 | 813 | 077 | lt005 | lt005 | 61 | 1011 | 1 | 4 | lt10 | 14 | lt4 | lt5 | lt6 | 2275 | 12 | 4 | lt3 | lt5 | lt2 | lt7 | 998 | lt4 | lt2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 126 | 8 | 60 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116429 | 614810 | 7171215 | 113 | 029 | 13 | 129 | 10 | 66 | lt4 | lt5 | lt6 | 2489 | 60 | 7 | lt5 | 15 | lt7 | 1344 | lt4 | 3 | 89 | 25 | lt4 | 75 | lt5 | 8 | lt2 | lt2 | 183 | 11 | 127 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116430 | 614807 | 7170845 | 217 | 002 | 10 | 12 | 2570 | 32 | lt4 | lt5 | 22 | 1581 | 463 | 4 | lt5 | lt6 | lt7 | 286 | 109 | lt2 | lt4 | 53 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 348 | 13 | 95 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116432 | 614348 | 7169311 | 101 | 009 | 6 | 5 | 80 | 44 | lt4 | lt5 | 15 | 1757 | 116 | lt3 | 7 | lt6 | 11 | 683 | lt4 | lt2 | lt4 | 37 | lt4 | 27 | lt5 | lt6 | lt2 | lt2 | 327 | 18 | 119 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116433 | 614232 | 7168820 | 211 | 029 | lt5 | 7 | 60 | 2075 | lt4 | lt5 | 35 | 254 | 126 | 5 | 26 | lt6 | 13 | 186 | 13 | 27 | 4 | 12 | lt4 | 56 | lt5 | lt6 | 4 | lt2 | 152 | 25 | 120 | 100 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116442 | 632664 | 7159418 | 414 | 022 | 21 | 7 | 10 | 710 | lt4 | lt5 | lt6 | 39 | 716 | lt3 | lt5 | lt6 | lt7 | 35 | 4 | lt2 | lt4 | 40 | lt4 | 28 | lt5 | 6 | lt2 | lt2 | 1073 | 16 | 137 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116443 | 634091 | 7159896 | 461 | 035 | 144 | 279 | 528 | 018 | 746 | 165 | 174 | 005 | lt005 | 545 | 1005 | 2 | lt4 | lt10 | 23 | lt4 | lt5 | lt6 | 443 | 62 | 15 | lt3 | lt5 | lt2 | lt7 | 164 | lt4 | lt2 | lt4 | lt4 | 63 | lt5 | lt6 | lt2 | lt2 | 233 | 17 | 56 | 22 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116444 | 633832 | 7161837 | 11 | 021 | lt1 | 13 | lt10 | 1185 | lt4 | lt5 | 42 | 173 | 66 | 13 | lt3 | 24 | lt2 | 14 | 67 | 10 | 23 | lt4 | lt4 | 28 | lt5 | lt6 | 4 | lt2 | 245 | 18 | 61 | 87 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116446 | 633910 | 7169621 | 458 | 014 | 847 | 147 | 74 | 016 | 22 | 765 | 02 | lt005 | lt005 | 71 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 2882 | 12 | 7 | lt3 | lt5 | lt2 | lt7 | 1306 | lt4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 142 | 8 | 67 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454 | 653363 | 7152948 | 174 | 01 | lt1 | 15 | 130 | 111 | lt4 | lt5 | lt6 | 389 | 106 | 21 | lt3 | lt5 | lt2 | lt7 | 204 | lt4 | 16 | lt4 | lt4 | 12 | lt5 | lt6 | lt2 | lt2 | 450 | 10 | 122 | 55 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477 | 645436 | 7177439 | 178 | 007 | lt1 | lt4 | 30 | 52 | lt4 | lt5 | lt6 | 689 | 88 | 21 | lt3 | 55 | lt2 | lt7 | 456 | 5 | 13 | lt4 | lt4 | 5 | lt5 | lt6 | lt2 | lt2 | 435 | 98 | 350 | 69 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485 | 655767 | 7129994 | 225 | 018 | lt1 | lt4 | lt10 | 78 | lt4 | lt5 | lt6 | 5612 | 129 | 8 | 3 | lt5 | 2 | 7 | 88 | 4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 119 | 7 | 39 | 38 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487 | 655561 | 7129043 | 168 | 013 | 1 | lt4 | lt10 | 191 | lt4 | lt5 | 11 | 4578 | 8 | 6 | lt3 | lt5 | lt2 | lt7 | 464 | 11 | 10 | lt4 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 87 | 7 | 70 | 35 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116488 | 655420 | 7128860 | 156 | 012 | lt1 | lt4 | 40 | 119 | lt4 | lt5 | 19 | 135 | 279 | 31 | lt3 | 7 | 2 | 7 | 313 | 21 | 23 | lt4 | lt4 | 15 | lt5 | lt6 | 3 | 3 | 585 | 10 | 97 | 149 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 128 | 007 | lt1 | lt4 | 170 | 169 | lt4 | lt5 | lt6 | 5588 | 63 | 4 | lt3 | lt5 | lt2 | lt7 | 687 | 14 | 12 | lt4 | lt4 | 6 | lt5 | 8 | 2 | 2 | 75 | 7 | 81 | 30 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 681 | 02 | 2 | 8 | lt10 | 34 | lt4 | lt5 | lt6 | 967 | 299 | 6 | lt3 | 9 | lt2 | lt7 | 348 | lt4 | lt2 | lt4 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 469 | 35 | 110 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116490 | 655978 | 7126699 | 491 | 078 | 147 | 315 | 779 | 017 | 816 | 994 | 274 | 065 | 008 | 371 | 1012 | 1 | lt4 | 20 | 228 | lt4 | lt5 | lt6 | 191 | 103 | 13 | lt3 | lt5 | lt2 | lt7 | 116 | lt4 | 9 | lt4 | lt4 | 300 | lt5 | lt6 | lt2 | lt2 | 267 | 17 | 87 | 56 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116491 | 656084 | 7126206 | 50 | 07 | 133 | 216 | 817 | 019 | 999 | 939 | 208 | 035 | 007 | 402 | 1007 | 1 | lt4 | 10 | 329 | lt4 | lt5 | lt6 | 471 | 104 | 12 | lt3 | lt5 | lt2 | lt7 | 249 | lt4 | 6 | 4 | lt4 | 157 | lt5 | lt6 | lt2 | lt2 | 241 | 16 | 82 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116492 | 656023 | 7125806 | 10 | 27 | 10 | 213 | lt4 | lt5 | lt6 | 17 | 170 | lt3 | lt5 | 7 | lt7 | 40 | lt4 | 49 | 4 | 49 | lt4 | 38 | 803 | lt6 | lt2 | lt2 | 434 | 28 | 45 | 58 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493 | 655992 | 7125530 | 13 | 25 | 60 | 150 | lt4 | lt5 | lt6 | 24 | 393 | lt3 | 6 | 10 | lt7 | 118 | 6 | 79 | lt4 | 55 | lt4 | 31 | 269 | lt6 | lt2 | lt2 | 464 | 37 | 239 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116498 | 709849 | 7162239 | 11 | 19 | 5000 | 269 | lt4 | lt5 | lt6 | 140 | 92 | lt3 | lt5 | 6 | lt7 | 83 | lt4 | 74 | lt4 | 47 | lt4 | 50 | 301 | lt6 | lt2 | lt2 | 316 | 25 | 123 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116500 | 709011 | 7162160 | 9 | 29 | 10 | 155 | lt4 | lt5 | lt6 | 27 | 121 | lt3 | lt5 | 6 | lt7 | 39 | 5 | 33 | lt4 | 66 | lt4 | 20 | 155 | lt6 | lt2 | lt2 | 535 | 34 | 28 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501 | 708508 | 7162137 | 11 | 6 | 20 | 23 | lt4 | lt5 | lt6 | 29 | 146 | lt3 | lt5 | 6 | lt7 | 102 | lt4 | 98 | lt4 | 57 | lt4 | 31 | 195 | 6 | lt2 | lt2 | 416 | 35 | 144 | 74 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116502 | 708368 | 7162139 | 756 | 052 | lt1 | 8 | lt10 | 368 | lt4 | lt5 | 11 | 25 | 398 | lt3 | lt3 | 12 | 2 | lt7 | 151 | 6 | lt2 | lt4 | 4 | 23 | lt5 | lt6 | lt2 | lt2 | 207 | 15 | 211 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116532 | 672308 | 7165117 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | 1009 | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | 117 | 13 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 5 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 275 | 21 | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120337 | 668950 | 7146475 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | nd | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | nd | 117 | 13 | lt5 | nd | lt2 | lt7 | 104 | lt4 | nd | nd | 5 | lt4 | nd | lt4 | 129 | lt2 | 44963 | lt2 | 275 | 21 | nd | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120340 | 669175 | 7145725 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | 1009 | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | 92 | 14 | lt3 | lt5 | lt2 | lt7 | 118 | lt4 | 4 | 4 | lt4 | 132 | lt5 | lt6 | 2 | lt2 | 259 | 18 | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369 | 665175 | 7156150 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | nd | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | nd | 92 | 14 | lt5 | nd | lt2 | lt7 | 118 | lt4 | nd | nd | 4 | 40 | nd | lt4 | 132 | 2 | 46162 | lt2 | 259 | 18 | nd | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373 | 675250 | 7167875 | 50 | 078 | 146 | 288 | 732 | 017 | 757 | 112 | 256 | lt005 | 008 | 328 | 328 | 1006 | nd | lt1 | lt4 | lt10 | 101 | lt4 | lt5 | lt6 | 224 | nd | 100 | 14 | lt3 | lt5 | nd | lt2 | lt7 | 125 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 120 | lt5 | lt6 | lt2 | 46761 | lt2 | 262 | 16 | nd | 84 | 57 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432 | 673950 | 7171700 | 52 | 077 | 146 | 219 | 763 | 015 | 753 | 793 | 429 | lt005 | 008 | 326 | 326 | 1006 | nd | 1 | 4 | lt10 | 126 | lt4 | lt5 | lt6 | 266 | nd | 109 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 123 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 97 | lt5 | lt6 | lt2 | 46162 | lt2 | 257 | 21 | nd | 84 | 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120549 | 709110 | 7163260 | 851 | 045 | 827 | 064 | 028 | lt005 | 066 | 02 | 025 | 252 | lt005 | 211 | 1007 | 1 | lt4 | lt10 | 516 | lt4 | lt5 | 49 | 56 | lt4 | 10 | lt3 | 18 | lt2 | 9 | 17 | 18 | 135 | 5 | lt4 | 13 | lt5 | lt6 | 13 | 5 | 139 | 21 | 8 | 114 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120550 | 709190 | 7162721 | 516 | 087 | 135 | 324 | 901 | 021 | 646 | 957 | 246 | 031 | 008 | 362 | 101 | 1 | 4 | lt10 | 145 | lt4 | lt5 | lt6 | 17 | 70 | 15 | lt3 | lt5 | lt2 | lt7 | 70 | lt4 | 7 | lt4 | lt4 | 93 | lt5 | lt6 | 2 | 52157 | lt2 | 267 | 20 | 85 | 62 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120566 | 734201 | 7165328 | 733 | 003 | 1 | lt4 | 10 | 261 | lt4 | lt5 | 8 | 257 | 24 | 24 | lt3 | lt5 | 2 | 8 | 97 | 12 | lt2 | lt4 | lt4 | 376 | lt5 | lt6 | lt2 | lt2 | 962 | 5 | 59 | 61 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120593 | 707343 | 7160447 | 48 | 046 | 116 | 248 | 735 | 017 | 14 | 101 | 148 | lt005 | 005 | 464 | 1007 | lt1 | lt4 | lt10 | 35 | lt4 | lt5 | lt6 | 1617 | 39 | 11 | lt3 | lt5 | lt2 | lt7 | 611 | lt4 | lt2 | lt4 | lt4 | 91 | lt5 | lt6 | lt2 | lt2 | 220 | 13 | 72 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120630 | 722750 | 7168750 | 38 | 014 | 733 | 088 | 695 | 014 | 207 | 725 | 095 | lt005 | lt005 | 18 | 1009 | 1 | lt4 | 10 | 41 | lt4 | lt5 | lt6 | 2746 | 46 | 6 | lt3 | lt5 | lt2 | lt7 | 1110 | lt4 | lt2 | lt4 | lt4 | 32 | lt5 | lt6 | lt2 | lt2 | 137 | 6 | 56 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120688 | 739099 | 7173927 | 521 | 084 | 139 | 322 | 775 | 017 | 658 | 104 | 288 | 017 | 008 | 277 | 101 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 160 | 35 | 13 | lt3 | lt5 | lt2 | lt7 | 133 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | lt2 | lt2 | 317 | 20 | 78 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120692 | 738903 | 7174351 | 496 | 032 | 134 | 271 | 658 | 015 | 115 | 101 | 223 | 009 | lt005 | 405 | 101 | lt1 | lt4 | lt10 | 149 | lt4 | lt5 | lt6 | 941 | 57 | 12 | lt3 | lt5 | lt2 | lt7 | 334 | lt4 | lt2 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 205 | 13 | 61 | 32 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120698 | 735588 | 7172781 | 546 | 059 | 136 | 26 | 576 | 014 | 727 | 101 | 346 | 006 | 006 | 246 | 1008 | lt1 | 15 | lt10 | 71 | lt4 | lt5 | lt6 | 315 | 60 | 11 | lt3 | lt5 | lt2 | lt7 | 100 | lt4 | lt2 | lt4 | lt4 | 67 | lt5 | lt6 | lt2 | lt2 | 228 | 16 | 65 | 44 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120727 | 456 | 015 | 815 | 227 | 694 | 016 | 225 | 686 | 045 | lt005 | lt005 | 726 | 1009 | lt1 | lt4 | lt10 | 27 | lt4 | lt5 | lt6 | 2788 | 31 | 6 | lt3 | lt5 | lt2 | lt7 | 1075 | lt4 | lt2 | lt4 | lt4 | 14 | lt5 | lt6 | lt2 | lt2 | 141 | 7 | 69 | 25 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120728 | 687200 | 7128470 | 545 | 04 | 141 | 225 | 609 | 015 | 916 | 624 | 5 | lt005 | 005 | 324 | 1014 | lt1 | 23 | lt10 | 61 | lt4 | lt5 | lt6 | 479 | 103 | 7 | lt3 | lt5 | lt2 | lt7 | 202 | lt4 | lt2 | lt4 | lt4 | 68 | lt5 | lt6 | lt2 | lt2 | 213 | 14 | 70 | 36 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120729 | 686100 | 7128750 | 833 | 027 | 1 | 814 | lt10 | 298 | lt4 | lt5 | lt6 | 2024 | 80 | 4 | lt3 | lt5 | lt2 | 9 | 796 | 4 | 46 | 17 | lt4 | 46 | lt5 | lt6 | lt2 | lt2 | 115 | 15 | 50 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120730 | 686300 | 7128650 | 383 | 003 | 1 | 9 | lt10 | 73 | lt4 | lt5 | lt6 | 3998 | 203 | 5 | lt3 | lt5 | lt2 | 15 | 1785 | lt4 | lt2 | 4 | lt4 | 8 | lt5 | lt6 | lt2 | lt2 | 270 | 19 | 108 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120770 | 675368 | 7143153 | 11 | 138 | lt1 | 246 | lt10 | 458 | lt4 | lt5 | lt6 | 1351 | 50 | 7 | lt3 | lt5 | lt2 | 12 | 259 | 4 | 57 | 5 | lt4 | 114 | lt5 | 6 | lt2 | lt2 | 155 | 9 | 45 | 31 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120801 | 686900 | 7143160 | 916 | 213 | 1 | 169 | 660 | 1736 | lt4 | lt5 | 66 | 1275 | 594 | 5 | lt3 | 26 | lt2 | 13 | 101 | 24 | 41 | lt4 | lt4 | 94 | lt5 | 11 | lt2 | lt2 | 147 | 35 | 98 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120802 | 686900 | 7143160 | 146 | 009 | lt1 | 17 | lt10 | 130 | lt4 | lt5 | 12 | 3035 | 213 | 19 | lt3 | 6 | lt2 | 19 | 1488 | 4 | 12 | lt4 | lt4 | 31 | lt5 | lt6 | 2 | lt2 | 432 | 22 | 148 | 116 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120873 | 697233 | 7155938 | 518 | 133 | 142 | 374 | 907 | 02 | 572 | 106 | 23 | 044 | 016 | 117 | 1009 | lt1 | lt4 | lt10 | 204 | lt4 | lt5 | 23 | 72 | 232 | 18 | lt3 | 8 | lt2 | lt7 | 58 | lt4 | 40 | lt4 | lt4 | 134 | lt5 | lt6 | 3 | lt2 | 239 | 33 | 95 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120874 | 699393 | 7156313 | 503 | 062 | 148 | 29 | 648 | 016 | 812 | 112 | 313 | 01 | 006 | 31 | 1012 | lt1 | lt4 | lt10 | 124 | lt4 | lt5 | lt6 | 356 | 99 | 12 | lt3 | lt5 | lt2 | lt7 | 140 | lt4 | lt2 | lt4 | lt4 | 80 | lt5 | lt6 | lt2 | lt2 | 244 | 14 | 71 | 46 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120876 | 694754 | 7155096 | 506 | 091 | 141 | 358 | 748 | 017 | 751 | 109 | 142 | 026 | 009 | 371 | 1009 | lt1 | lt4 | lt10 | 125 | lt4 | lt5 | lt6 | 176 | 141 | 15 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 3 | lt4 | lt4 | 178 | lt5 | lt6 | lt2 | lt2 | 262 | 20 | 103 | 71 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120877 | 694754 | 7155096 | 509 | 085 | 142 | 399 | 735 | 018 | 709 | 105 | 209 | 034 | 008 | 34 | 1011 | lt1 | lt4 | lt10 | 103 | lt4 | lt5 | lt6 | 119 | 158 | 15 | lt3 | lt5 | lt2 | lt7 | 107 | lt4 | 4 | lt4 | lt4 | 182 | lt5 | lt6 | 2 | lt2 | 269 | 19 | 95 | 70 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120878 | 694149 | 7154736 | 488 | 082 | 143 | 385 | 717 | 018 | 765 | 128 | 174 | 008 | 008 | 33 | 1009 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 137 | 107 | 15 | lt3 | lt5 | lt2 | lt7 | 105 | lt4 | lt2 | lt4 | lt4 | 142 | lt5 | lt6 | lt2 | lt2 | 257 | 24 | 83 | 60 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120891 | 677938 | 7168840 | 4880 | 082 | 1430 | 385 | 717 | 018 | 765 | 1280 | 174 | 008 | 008 | 330 | 10077 | 1 | 4 | 10 | 86 | 4 | 5 | 6 | 137 | 107 | 15 | 5 | 2 | 7 | 105 | 4 | 2 | 4 | 4 | 142 | 2 | 2 | 257 | 24 | 83 | 60 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124203 | 685884 | 7169152 | 496 | 089 | 14 | 329 | 852 | 02 | 733 | 981 | 233 | 009 | 008 | 36 | 998 | lt1 | lt4 | lt10 | 53 | lt4 | lt5 | lt6 | 65 | 122 | 14 | lt3 | lt5 | lt2 | lt7 | 91 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | 2 | lt2 | 280 | 19 | 104 | 66 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124204 | 685884 | 7168152 | 511 | 082 | 135 | 254 | 81 | 019 | 74 | 106 | 235 | 033 | 008 | 343 | 1006 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 130 | 85 | 12 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 4 | lt4 | lt4 | 47 | lt5 | lt6 | lt2 | lt2 | 261 | 18 | 88 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124208 | 685884 | 7169152 | 497 | 075 | 143 | 293 | 769 | 017 | 784 | 115 | 181 | 03 | 008 | 35 | 1007 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 129 | 132 | 14 | lt3 | lt5 | lt2 | lt7 | 94 | lt4 | 5 | lt4 | lt4 | 84 | lt5 | lt6 | lt2 | lt2 | 255 | 17 | 87 | 54 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132787 | 630625 | 7198600 | 492 | 07 | 142 | 265 | 735 | 017 | 857 | 126 | 176 | 009 | 006 | 335 | 1008 | 1 | lt4 | lt10 | 75 | lt4 | lt5 | lt6 | 136 | 105 | 16 | lt3 | lt5 | lt2 | lt7 | 158 | 5 | lt2 | lt4 | lt4 | 126 | lt5 | lt6 | lt2 | lt2 | 247 | 17 | 70 | 52 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132788 | 630625 | 7198600 | 218 | lt001 | lt1 | lt4 | lt10 | 864 | lt4 | lt5 | lt6 | 454 | 9 | lt3 | lt3 | lt5 | lt2 | lt7 | 67 | lt4 | lt2 | lt4 | lt4 | 9 | lt5 | lt6 | 2 | lt2 | 41 | 3 | 7 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132789 | 602460 | 7168288 | 556 | 021 | 138 | 329 | 587 | 016 | 612 | 111 | 131 | lt005 | lt005 | 303 | 303 | 1005 | nd | lt1 | lt4 | lt10 | 130 | lt4 | lt5 | lt6 | 158 | nd | 76 | 8 | lt3 | lt5 | nd | lt2 | lt7 | 98 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 16 | lt2 | 12590 | lt2 | 204 | 13 | nd | 72 | 17 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132790 | 613877 | 7170789 | 527 | 035 | 138 | 239 | 605 | 016 | 83 | 113 | 189 | lt005 | lt005 | 338 | 338 | 1006 | nd | lt1 | lt4 | lt10 | 81 | lt4 | lt5 | lt6 | 503 | nd | 81 | 10 | lt5 | nd | lt2 | lt7 | 190 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 27 | lt5 | 9 | lt2 | 20983 | lt2 | 211 | 14 | nd | 65 | 24 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132791 | 621561 | 7169810 | 499 | 057 | 133 | 308 | 649 | 015 | 96 | 121 | 204 | 005 | 006 | 316 | 316 | 1007 | nd | lt1 | 4 | lt10 | 71 | lt4 | lt5 | lt6 | 633 | nd | 80 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 281 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 75 | lt5 | lt6 | lt2 | 34172 | lt2 | 233 | 16 | nd | 74 | 40 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132792 | 616685 | 7171750 | 503 | 084 | 134 | 527 | 637 | 017 | 813 | 104 | 107 | 005 | 007 | 432 | 1006 | lt1 | lt4 | lt10 | 12 | lt4 | lt5 | lt6 | 314 | 144 | 13 | lt3 | 6 | lt2 | lt7 | 204 | 5 | lt2 | lt4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 285 | 28 | 95 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132793 | 622866 | 7161836 | 4860 | 031 | 1350 | 362 | 510 | 013 | 1040 | 1090 | 231 | 001 | 003 | 321 | 9812 | 2 | 4 | 3 | 29 | 4 | 5 | 6 | 872 | 45 | 61 | 11 | 3 | 97 | 7 | 379 | 4 | 3 | 2 | 2 | 4 | 4 | 72 | 2 | 2 | 216 | 14 | 4 | 60 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132794 | 622866 | 7161786 | 4840 | 014 | 576 | 203 | 615 | 015 | 2160 | 863 | 033 | 001 | 001 | 549 | 9870 | 2 | 4 | 4 | 11 | 6 | 5 | 6 | 2460 | 71 | 22 | 5 | 3 | 2 | 7 | 1020 | 4 | 4 | 3 | 2 | 4 | 4 | 11 | 2 | 2 | 155 | 7 | 4 | 63 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133033 | 638351 | 7157551 | 4450 | 156 | 1110 | 611 | 440 | 020 | 318 | 1330 | 468 | 034 | 021 | 906 | 9864 | 01 | 05 | 5 | 323 | 07 | 01 | 296 | 190 | 36 | 84 | 05 | 126 | 01 | 11 | 75 | 19 | 11 | 11 | 51 | 02 | 1 | 07 | 135 | 22 | 07 | 276 | 241 | 05 | 73 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133034 | 638351 | 7157551 | 4710 | 013 | 836 | 237 | 696 | 014 | 1980 | 764 | 012 | 001 | 003 | 596 | 9862 | 02 | 12 | 2 | 18 | 45 | 01 | 32 | 3448 | 69 | 22 | 16 | 16 | 23 | 32 | 1048 | 11 | 5 | 9 | 17 | 18 | 42 | 19 | 52 | 15 | 01 | 133 | 58 | 84 | 72 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133035 | 638300 | 7157750 | 4740 | 013 | 668 | 349 | 512 | 014 | 2200 | 801 | 022 | 003 | 001 | 521 | 9844 | 02 | 07 | 6 | 52 | 14 | 01 | 11 | 2608 | 73 | 34 | 22 | 12 | 03 | 33 | 1295 | 15 | 10 | 9 | 22 | 06 | 29 | 1 | 12 | 16 | 02 | 116 | 72 | 58 | 61 | 447 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133038 | 632615 | 7159390 | 5060 | 048 | 1600 | 316 | 443 | 012 | 572 | 1410 | 150 | 032 | 006 | 267 | 022 | 102 | lt05 | 70 | 110 | lt05 | lt01 | 216 | 392 | 29 | 93 | 57 | 147 | 10 | 12 | 28 | 138 | 29 | lt2 | 3 | 179 | 297 | 31 | 74 | 141 | 21 | 28776 | 02 | 181 | 14 | 139 | 59 | 709 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133039 | 632600 | 7159000 | 5160 | 034 | 1550 | 281 | 555 | 014 | 644 | 1090 | 252 | 026 | 002 | 309 | 026 | lt01 | lt05 | 30 | 80 | lt05 | lt01 | 06 | 422 | 36 | 88 | 47 | lt05 | 6 | 05 | 33 | 183 | lt05 | lt2 | lt2 | 46 | 115 | 32 | 29 | 139 | lt05 | 20383 | lt01 | 216 | 148 | 77 | 66 | 338 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133043 | 632906 | 7159832 | 4970 | 073 | 1490 | 272 | 790 | 018 | 626 | 1260 | 171 | 031 | 006 | 236 | 022 | 03 | 21 | 30 | 412 | 09 | 01 | 46 | 66 | 37 | 129 | 05 | 61 | 8 | 06 | 41 | 121 | 48 | lt2 | 9 | 99 | 44 | 11 | 27 | 119 | 13 | 43764 | 02 | 268 | 203 | 33 | 88 | 470 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133046 | 633939 | 7161905 | 4980 | 051 | 1280 | 263 | 708 | 016 | 1070 | 1060 | 163 | 014 | 005 | 309 | 016 | lt01 | lt05 | lt2 | 48 | lt05 | lt01 | 18 | 678 | 43 | 85 | 47 | 53 | 8 | 04 | 05 | 327 | lt05 | lt2 | lt2 | 06 | 68 | 34 | 15 | 123 | lt05 | 30575 | lt01 | 227 | 147 | 51 | 76 | 443 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133047 | 633939 | 7161905 | 5200 | 079 | 1400 | 280 | 738 | 017 | 548 | 1080 | 227 | 039 | 007 | 264 | 022 | 118 | lt05 | lt2 | 60 | lt05 | lt01 | 36 | 116 | 36 | 74 | 56 | 48 | 12 | 04 | 44 | 81 | lt05 | lt2 | lt2 | 95 | 46 | 38 | 09 | 101 | lt05 | 47361 | lt01 | 261 | 193 | 45 | 77 | 673 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133048 | 633939 | 7161905 | 4800 | 053 | 1050 | 391 | 746 | 018 | 972 | 1360 | 100 | 034 | 004 | 390 | 015 | lt01 | lt05 | 30 | 63 | lt05 | lt01 | 37 | 200 | 55 | 192 | 55 | 10 | 11 | 02 | 19 | 156 | 36 | lt2 | 3 | 55 | 08 | 43 | lt05 | 110 | lt05 | 31774 | lt01 | 276 | 126 | 12 | 76 | 410 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133049 | 634427 | 7166123 | 4900 | 059 | 1390 | 361 | 656 | 016 | 658 | 1300 | 190 | 019 | 005 | 328 | 015 | lt01 | lt05 | 30 | 45 | lt05 | lt01 | 25 | 120 | 42 | 164 | 66 | 12 | 10 | 07 | 32 | 143 | 24 | lt2 | lt2 | 20 | 33 | 24 | lt05 | 101 | lt05 | 35371 | lt01 | 220 | 145 | 82 | 67 | 442 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133050 | 635551 | 7169572 | 4890 | 060 | 1280 | 365 | 706 | 017 | 698 | 1370 | 137 | 023 | 005 | 348 | 011 | lt01 | lt05 | 30 | 36 | lt05 | lt01 | 22 | 165 | 49 | 108 | 64 | 08 | 11 | 04 | 24 | 152 | 22 | lt2 | 4 | 49 | 06 | 33 | lt05 | 108 | lt05 | 35970 | lt01 | 233 | 149 | 18 | 68 | 415 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133051 | 635603 | 7169579 | 0 | 74 | 0 | 02 | 15 | 12 | 114 | 114 | 24 | 91 | 13 | 05 | 84 | 73 | 27 | 12 | 11 | 24 | 0 | 40 | 15 | 158 | 173 | 043 | 256 | 18 | 05 | 74 | 62 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133052 | 635259 | 7169444 | 5160 | 086 | 1360 | 411 | 719 | 016 | 569 | 1030 | 155 | 048 | 008 | 344 | 9906 | 038 | 01 | 05 | 2 | 151 | 05 | 01 | 94 | 148 | 37 | 136 | 33 | 11 | 03 | 34 | 93 | 05 | 2 | 2 | 105 | 02 | 24 | 05 | 145 | 05 | 01 | 296 | 191 | 05 | 85 | 718 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133054 | 634952 | 7169267 | 0 | 62 | 05 | 0 | 38 | 5 | 105 | 44 | 18 | 25 | 41 | 12 | 13 | 57 | 48 | 5 | 6 | 12 | 0 | 26 | 18 | 411 | 6 | 166 | 182 | 18 | 08 | 38 | 104 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133060 | 648256 | 7160919 | 0 | 23 | 0 | 02 | 19 | 6 | 89 | 129 | 18 | 10 | 5 | 12 | 88 | 62 | 27 | 3 | 0 | 92 | 0 | 38 | 21 | 251 | 111 | 037 | 318 | 25 | 08 | 85 | 76 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133063 | 648467 | 7150024 | 4400 | 018 | 889 | 410 | 531 | 015 | 2270 | 702 | 037 | 003 | 002 | 705 | 9982 | 011 | 01 | 05 | 2 | 7 | 05 | 01 | 05 | 3170 | 83 | 19 | 53 | 05 | 03 | 18 | 1370 | 15 | 9 | 13 | 09 | 04 | 23 | 05 | 135 | 05 | 01 | 123 | 76 | 27 | 72 | 139 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133064 | 647573 | 7150076 | 5150 | 032 | 1450 | 307 | 514 | 015 | 634 | 1390 | 178 | 001 | 003 | 244 | 9918 | 015 | 01 | 05 | 3 | 50 | 05 | 01 | 05 | 456 | 29 | 40 | 65 | 14 | 04 | 09 | 191 | 05 | 11 | 11 | 05 | 04 | 36 | 05 | 577 | 05 | 01 | 222 | 144 | 21 | 61 | 26 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133073 | 626850 | 7161292 | 5150 | 033 | 1440 | 273 | 573 | 014 | 748 | 1250 | 232 | 001 | 003 | 264 | 9981 | 011 | 01 | 05 | 3 | 43 | 05 | 01 | 05 | 467 | 38 | 78 | 32 | 19 | 02 | 29 | 202 | 14 | 13 | 12 | 05 | 03 | 32 | 05 | 497 | 05 | 01 | 219 | 137 | 05 | 61 | 258 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133076 | 626850 | 7161292 | 4990 | 074 | 1490 | 410 | 612 | 015 | 546 | 1320 | 148 | 006 | 007 | 297 | 9915 | 022 | 01 | 05 | 3 | 42 | 05 | 01 | 85 | 154 | 33 | 55 | 65 | 34 | 03 | 34 | 93 | 05 | 7 | 11 | 05 | 02 | 33 | 05 | 151 | 05 | 01 | 263 | 169 | 16 | 84 | 678 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133096 | 645954 | 7171243 | 4500 | 013 | 916 | 192 | 711 | 014 | 2110 | 744 | 015 | 002 | 001 | 699 | 9917 | 022 | 01 | 05 | 2 | 75 | 05 | 01 | 23 | 3100 | 93 | 69 | 6 | 146 | 06 | 14 | 1620 | 17 | 7 | 7 | 07 | 17 | 26 | 05 | 27 | 05 | 01 | 132 | 212 | 21 | 69 | 103 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133098 | 636053 | 7155351 | 4950 | 057 | 1510 | 228 | 646 | 014 | 728 | 1380 | 135 | 010 | 006 | 307 | 9971 | 015 | 01 | 05 | 6 | 174 | 05 | 01 | 08 | 487 | 31 | 81 | 47 | 58 | 05 | 37 | 165 | 05 | 12 | 16 | 15 | 02 | 26 | 05 | 112 | 35 | 02 | 220 | 135 | 05 | 64 | 429 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136749 | 667073 | 7199167 | 5080 | 072 | 1420 | 410 | 567 | 015 | 601 | 1330 | 166 | 022 | 007 | 221 | 9911 | 011 | 01 | 05 | 4 | 222 | 05 | 01 | 42 | 331 | 37 | 82 | 57 | 59 | 04 | 29 | 131 | 1 | 12 | 11 | 32 | 07 | 31 | 05 | 237 | 05 | 01 | 257 | 175 | 15 | 75 | 665 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136751 | 659000 | 7122223 | 0 | 12 | 0 | 0 | 98 | 3 | 209 | 68 | 15 | 62 | 34 | 04 | 44 | 86 | 2 | 9 | 7 | 43 | 0 | 34 | 09 | 304 | 053 | 021 | 207 | 15 | 09 | 48 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139131 | 621200 | 7215100 | 4790 | 065 | 1470 | 301 | 746 | 019 | 682 | 1290 | 254 | 004 | 006 | 319 | 9946 | 026 | 01 | 05 | 3 | 211 | 05 | 01 | 43 | 358 | 43 | 103 | 07 | 4 | 02 | 46 | 154 | 05 | 8 | 14 | 05 | 02 | 29 | 05 | 616 | 05 | 02 | 281 | 19 | 05 | 77 | 484 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139132 | 621190 | 7215090 | 0 | 14 | 0 | 01 | 11 | 0 | 66 | 18 | 46 | 59 | 40 | 05 | 95 | 11 | 14 | 0 | 0 | 108 | 0 | 51 | 21 | 242 | 87 | 124 | 389 | 7 | 24 | 51 | 134 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139133 | 666700 | 7193500 | 0 | 09 | 0 | 02 | 56 | 0 | 0 | 18 | 37 | 39 | 92 | 05 | 63 | 4 | 62 | 0 | 0 | 63 | 0 | 53 | 19 | 33 | 21 | 24 | 29 | 18 | 08 | 25 | 290 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139134 | 621755 | 7169255 | 0 | 08 | 0 | 0 | 85 | 3 | 3 | 3 | 15 | 63 | 14 | 09 | 06 | 0 | 2 | 0 | 0 | 73 | 0 | 06 | 08 | 76 | 129 | 05 | 4 | 3 | 03 | 3 | 35 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139135 | 621000 | 7169500 | 5016 | 037 | 1406 | 241 | 647 | 017 | 918 | 1126 | 248 | 006 | 003 | 15 | 5812 | 222 | 438 | 53 | 65 | 10 | 438 | 077 | 1320 | 100E-07 | 171 | 100E-07 | 500E-08 | 54 | 2 | 53 | 500E-08 | 500E-08 | 212 | 15 | 72 | 19 | 036 | 194 | 094 | 048 | 190 | 038 | 289 | 071 | 222 | 034 | 232 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139136 | 621000 | 7169500 | 5236 | 027 | 1373 | 239 | 577 | 016 | 897 | 1068 | 21 | 007 | 003 | 15 | 5265 | 210 | 491 | 53 | 162 | 10 | 491 | 086 | 1290 | 100E-07 | 196 | 100E-07 | 1 | 48 | 200E-07 | 62 | 500E-08 | 500E-08 | 189 | 13 | 63 | 13 | 036 | 161 | 078 | 041 | 160 | 039 | 259 | 068 | 214 | 038 | 221 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139137 | 620904 | 7169533 | 4737 | 108 | 1123 | 33 | 789 | 018 | 1191 | 106 | 203 | 008 | 012 | 15 | 13407 | 2170 | 1150 | 82 | 119 | 15 | 1150 | 897 | 1380 | 6 | 525 | 2 | 500E-08 | 39 | 4 | 143 | 1 | 500E-08 | 265 | 17 | 90 | 65 | 278 | 1143 | 314 | 124 | 391 | 066 | 391 | 084 | 222 | 031 | 187 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139138 | 620992 | 7169508 | 5075 | 03 | 141 | 177 | 678 | 017 | 996 | 925 | 264 | 044 | 002 | 05 | 7628 | 124 | 660 | 56 | 61 | 10 | 660 | 042 | 1310 | 100E-07 | 232 | 100E-07 | 55 | 49 | 2 | 62 | 500E-08 | 500E-08 | 194 | 12 | 65 | 14 | 019 | 104 | 062 | 031 | 135 | 030 | 225 | 055 | 166 | 026 | 175 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139139 | 620992 | 7169508 | 4747 | 018 | 1006 | 141 | 804 | 017 | 1989 | 829 | 089 | 002 | 001 | 500E-08 | 7171 | 148 | 1770 | 95 | 53 | 75 | 1770 | 089 | 1320 | 100E-07 | 835 | 100E-07 | 500E-08 | 39 | 2 | 225 | 500E-08 | 500E-08 | 139 | 8 | 60 | 7 | 019 | 098 | 063 | 028 | 124 | 028 | 206 | 051 | 157 | 026 | 160 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139140 | 620992 | 7169508 | 5201 | 117 | 1269 | 224 | 762 | 016 | 761 | 1089 | 239 | 025 | 013 | 05 | 8447 | 2455 | 212 | 52 | 161 | 15 | 212 | 982 | 1210 | 5 | 135 | 100E-07 | 45 | 42 | 4 | 228 | 1 | 500E-08 | 270 | 17 | 87 | 80 | 308 | 1270 | 330 | 120 | 387 | 061 | 364 | 074 | 200 | 028 | 161 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139141 | 620992 | 7169488 | 6179 | 081 | 147 | 284 | 594 | 006 | 496 | 012 | 007 | 32 | 01 | 1 | 74341 | 6413 | 414 | 41 | 31 | 19 | 414 | 2988 | 410 | 12 | 163 | 3 | 161 | 29 | 4 | 11 | 155 | 3 | 90 | 19 | 132 | 198 | 677 | 2282 | 433 | 094 | 430 | 059 | 295 | 058 | 166 | 026 | 170 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256h | 715830 | 7171470 | 6528 | 068 | 1179 | 412 | 511 | 004 | 551 | 013 | 005 | 24 | 012 | 1 | 44782 | 7429 | 348 | 39 | 2 | 15 | 348 | 3419 | 300 | 10 | 176 | 3 | 121 | 21 | 4 | 9 | 19 | 3 | 73 | 27 | 83 | 266 | 834 | 2926 | 592 | 121 | 584 | 082 | 451 | 089 | 249 | 038 | 231 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393s | 687539 | 7143275 | 3634 | 015 | 744 | 519 | 582 | 02 | 1191 | 1139 | 002 | 001 | 002 | 177 | 2109 | 066 | 2020 | 175 | 257 | 6 | 043 | 1440 | 00000001 | 1000 | 00000001 | 000000005 | 24 | 2 | 42 | 000000005 | 05 | 108 | 6 | 35 | 13 | 016 | 080 | 044 | 022 | 067 | 014 | 094 | 022 | 074 | 012 | 090 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601s | 668775 | 7146298 | 1248 | 005 | 339 | 812 | 262 | 026 | 1592 | 217 | 005 | 001 | 0 | 156 | 1400 | 058 | 850 | 63 | 46 | 25 | 066 | 1990 | 00000001 | 1010 | 1 | 000000005 | 10 | 2 | 66 | 000000005 | 000000005 | 87 | 11 | 22 | 3 | 024 | 085 | 052 | 025 | 083 | 021 | 145 | 034 | 111 | 017 | 131 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604s | 672238 | 7155486 | 7639 | 017 | 1136 | 256 | 551 | 022 | 087 | 002 | 002 | 01 | 001 | 457 | 15133 | 087 | 2260 | 9 | 10 | 8 | 031 | 1590 | 00000001 | 228 | 1 | 45 | 21 | 00000002 | 17 | 000000005 | 05 | 149 | 2 | 17 | 9 | 009 | 043 | 014 | 012 | 017 | 004 | 028 | 006 | 023 | 004 | 035 | 005 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643h | 675190 | 7125902 | 5583 | 097 | 1236 | 543 | 726 | 045 | 595 | 128 | 308 | 005 | 015 | 195 | 2804 | 1728 | 46 | 41 | 13 | 145 | 738 | 3010 | 2 | 63 | 1 | 2 | 58 | 2 | 38 | 000000005 | 000000005 | 278 | 24 | 111 | 58 | 201 | 930 | 276 | 073 | 275 | 049 | 297 | 064 | 202 | 031 | 236 | 038 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454s | 653363 | 7152948 | 2576 | 011 | 467 | 59 | 024 | 018 | 1282 | 1816 | 172 | 064 | 003 | 695 | 7663 | 012 | 1570 | 58 | 23 | 35 | 042 | 1370 | 00000001 | 620 | 2 | 34 | 15 | 00000002 | 385 | 000000005 | 000000005 | 76 | 5 | 30 | 4 | 013 | 027 | 019 | 018 | 037 | 010 | 069 | 017 | 060 | 009 | 070 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477s | 645436 | 7177439 | 2009 | 0 | 084 | 152 | 0 | 038 | 1639 | 2363 | 022 | 04 | 003 | 6 | 6838 | 126 | 31 | 10 | 19 | 000000005 | 107 | 2940 | 00000001 | 93 | 1 | 75 | 00000001 | 00000002 | 103 | 000000005 | 000000005 | 9 | 10 | 4 | 00000001 | 034 | 113 | 036 | 118 | 051 | 012 | 084 | 027 | 105 | 017 | 142 | 020 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485h | 655767 | 7129994 | 5901 | 078 | 1092 | 14 | 102 | 013 | 1024 | 016 | 003 | 0 | 008 | 65 | 744 | 774 | 86 | 47 | 39 | 125 | 276 | 965 | 2 | 136 | 00000001 | 000000005 | 62 | 2 | 15 | 000000005 | 000000005 | 304 | 15 | 85 | 45 | 099 | 490 | 138 | 035 | 148 | 026 | 164 | 036 | 114 | 018 | 143 | 023 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487h | 655561 | 7129043 | 2488 | 011 | 535 | 29 | 312 | 04 | 1401 | 2084 | 003 | 004 | 005 | 110 | 4392 | 265 | 1410 | 69 | 15 | 5 | 175 | 3200 | 00000001 | 685 | 1 | 15 | 19 | 2 | 140 | 000000005 | 05 | 99 | 5 | 42 | 14 | 048 | 147 | 045 | 021 | 054 | 010 | 063 | 013 | 045 | 007 | 052 | 008 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493h | 655992 | 7125530 | 5148 | 073 | 1516 | 172 | 1092 | 013 | 932 | 024 | 26 | 03 | 009 | 15 | 10919 | 1023 | 98 | 58 | 72 | 155 | 430 | 935 | 2 | 98 | 00000001 | 45 | 69 | 2 | 75 | 000000005 | 1 | 357 | 18 | 113 | 42 | 127 | 601 | 174 | 057 | 201 | 036 | 234 | 054 | 176 | 028 | 217 | 036 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501h | 708508 | 7162137 | 4773 | 039 | 1372 | 423 | 456 | 016 | 666 | 527 | 438 | 098 | 006 | 1 | 120917 | 449 | 56 | 49 | 35 | 13 | 1277 | 1170 | 1 | 192 | 2 | 31 | 67 | 00000002 | 51 | 000000005 | 000000005 | 284 | 29 | 114 | 20 | 154 | 703 | 155 | 116 | 228 | 033 | 198 | 048 | 147 | 020 | 136 | 024 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116518s | 685232 | 7155526 | 3765 | 02 | 609 | 573 | 0 | 152 | 597 | 1736 | 007 | 218 | 005 | 100 | 218361 | 3411 | 55 | 39 | 15 | 7 | 1396 | 11070 | 4 | 70 | 5 | 65 | 8 | 00000002 | 77 | 55 | 1 | 60 | 12 | 38 | 38 | 321 | 1160 | 235 | 171 | 234 | 031 | 155 | 028 | 088 | 013 | 096 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120303 | 655250 | 7126000 | 2302 | 011 | 404 | 31 | 071 | 059 | 074 | 3572 | 004 | 141 | 004 | 53 | 20581 | 1117 | 285 | 7 | 4 | 45 | 720 | 4740 | 1 | 51 | 12 | 435 | 00000001 | 2 | 96 | 25 | 000000005 | 36 | 9 | 21 | 17 | 141 | 504 | 105 | 042 | 126 | 021 | 127 | 030 | 097 | 015 | 109 | 019 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339A | 669650 | 7146425 | 9409 | 001 | 03 | 425 | 065 | 002 | 003 | 005 | 0 | 006 | 003 | 155 | 1042 | 267 | 29 | 6 | 65 | 05 | 117 | 110 | 00000001 | 15 | 10 | 85 | 1 | 00000002 | 5 | 05 | 05 | 55 | 1 | 10 | 4 | 023 | 092 | 016 | 004 | 021 | 003 | 014 | 003 | 009 | 001 | 012 | 002 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339B | 669650 | 7146425 | 9632 | 0 | 002 | 319 | 053 | 001 | 0 | 001 | 0 | 0 | 001 | 5 | 2442 | 083 | 6 | 3 | 9 | 000000005 | 039 | 40 | 00000001 | 3 | 1 | 000000005 | 00000001 | 00000002 | 1 | 000000005 | 000000005 | 10 | 00000001 | 3 | 2 | 008 | 030 | 006 | 004 | 009 | 001 | 005 | 002 | 006 | 001 | 008 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369s | 665175 | 7156150 | 6131 | 098 | 1297 | 175 | 906 | 025 | 457 | 058 | 144 | 134 | 007 | 285 | 27950 | 3230 | 284 | 43 | 121 | 15 | 1406 | 1690 | 6 | 128 | 13 | 54 | 41 | 4 | 305 | 65 | 1 | 178 | 16 | 119 | 106 | 355 | 1340 | 286 | 087 | 269 | 039 | 202 | 036 | 119 | 017 | 130 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373s | 675250 | 7167875 | 5541 | 088 | 1306 | 795 | 346 | 014 | 199 | 144 | 005 | 004 | 009 | 1 | 7754 | 1109 | 26 | 29 | 74 | 225 | 521 | 1040 | 2 | 41 | 3 | 05 | 48 | 4 | 67 | 000000005 | 000000005 | 494 | 25 | 50 | 55 | 161 | 716 | 213 | 067 | 256 | 050 | 325 | 074 | 237 | 035 | 267 | 041 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432s | 673950 | 7171700 | 5469 | 078 | 1137 | 81 | 399 | 02 | 311 | 1468 | 016 | 005 | 006 | 2 | 11068 | 1433 | 62 | 44 | 22 | 20 | 634 | 1490 | 1 | 88 | 8 | 15 | 55 | 4 | 495 | 1 | 000000005 | 346 | 24 | 49 | 49 | 202 | 897 | 283 | 137 | 343 | 070 | 452 | 104 | 321 | 048 | 354 | 051 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137A | not available | 6241 | 067 | 991 | 186 | 893 | 019 | 924 | 011 | 0 | 005 | 01 | 15 | 2345 | 6927 | 595 | 43 | 123 | 12 | 3489 | 1470 | 10 | 235 | 4 | 25 | 21 | 4 | 55 | 175 | 2 | 77 | 16 | 112 | 288 | 734 | 2545 | 453 | 074 | 448 | 050 | 239 | 041 | 129 | 019 | 143 | 023 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137B | not available | 6118 | 074 | 1029 | 19 | 912 | 019 | 96 | 011 | 0 | 009 | 01 | 1 | 3042 | 6659 | 780 | 45 | 121 | 12 | 2999 | 1430 | 10 | 218 | 6 | 4 | 22 | 4 | 4 | 175 | 25 | 80 | 27 | 116 | 312 | 704 | 2493 | 499 | 095 | 542 | 075 | 415 | 083 | 249 | 037 | 262 | 039 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82144 | not available | 6901 | 044 | 1124 | 143 | 288 | 021 | 188 | 365 | 27 | 14 | 013 | 15 | 38750 | 6263 | 117 | 22 | 22 | 12 | 3381 | 1690 | 8 | 48 | 37 | 67 | 11 | 2 | 107 | 175 | 25 | 46 | 19 | 61 | 199 | 679 | 2348 | 436 | 093 | 441 | 056 | 304 | 052 | 157 | 022 | 154 | 022 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82148 | not available | 6314 | 07 | 124 | 312 | 581 | 017 | 717 | 01 | 005 | 197 | 01 | 1 | 41557 | 6431 | 505 | 53 | 22 | 15 | 3168 | 1310 | 10 | 211 | 4 | 99 | 23 | 4 | 8 | 165 | 25 | 72 | 18 | 121 | 227 | 689 | 2407 | 462 | 095 | 440 | 055 | 281 | 050 | 159 | 022 | 168 | 025 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82150 | not available | 9469 | 001 | 012 | 45 | 062 | 001 | 001 | 001 | 0 | 0 | 001 | 1150 | 13761 | 225 | 10 | 2 | 7 | 000000005 | 310 | 40 | 00000001 | 11 | 00000001 | 000000005 | 00000001 | 6 | 000000005 | 000000005 | 3800 | 00000001 | 700 | 300 | 044 | 122 | 021 | 012 | 021 | 002 | 013 | 002 | 004 | 000 | 005 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82153 | not available | 41767 | 296 | 256 | 047 | 214 | 049 | 031 | 072 | 013 | 090 | 023 | 077 | 010 | 072 | 010 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82155 | not available | 4977 | 081 | 1429 | 329 | 833 | 02 | 718 | 945 | 255 | 018 | 007 | 2 | 10432 | 1154 | 175 | 65 | 117 | 135 | 175 | 395 | 1540 | 2 | 135 | 100E-07 | 3 | 57 | 4 | 75 | 500E-08 | 500E-08 | 290 | 18 | 104 | 45 | 174 | 807 | 287 | 119 | 400 | 083 | 496 | 117 | 328 | 056 | 311 | 053 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82158 | not available | 5076 | 077 | 1356 | 336 | 794 | 019 | 714 | 996 | 197 | 035 | 006 | 15 | 16705 | 1081 | 163 | 55 | 128 | 135 | 163 | 373 | 1490 | 1 | 123 | 100E-07 | 55 | 54 | 2 | 166 | 500E-08 | 500E-08 | 268 | 17 | 98 | 43 | 159 | 772 | 261 | 108 | 365 | 070 | 470 | 107 | 304 | 046 | 279 | 042 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82160 | not available | 4799 | 033 | 127 | 192 | 57 | 017 | 1261 | 1352 | 09 | 004 | 002 | 115 | 5413 | 491 | 1360 | 52 | 50 | 105 | 1360 | 183 | 1370 | 100E-07 | 269 | 100E-07 | 05 | 46 | 4 | 87 | 500E-08 | 500E-08 | 159 | 8 | 50 | 18 | 074 | 333 | 108 | 052 | 167 | 030 | 198 | 045 | 131 | 019 | 116 | 016 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82179 | not available | 5338 | 053 | 1381 | 255 | 679 | 016 | 722 | 774 | 466 | 004 | 006 | 500E-08 | 3625 | 1347 | 326 | 50 | 48 | 115 | 326 | 523 | 1290 | 2 | 137 | 100E-07 | 500E-08 | 53 | 2 | 103 | 1 | 1 | 239 | 16 | 74 | 40 | 168 | 721 | 230 | 080 | 334 | 068 | 459 | 107 | 321 | 049 | 296 | 044 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82180 | not available | 462 | 02 | 998 | 154 | 752 | 017 | 1869 | 845 | 1 | 003 | 002 | 500E-08 | 749 | 081 | 2240 | 93 | 46 | 8 | 2240 | 029 | 1320 | 100E-07 | 795 | 100E-07 | 500E-08 | 40 | 200E-07 | 365 | 500E-08 | 500E-08 | 148 | 10 | 56 | 8 | 015 | 081 | 051 | 034 | 110 | 026 | 192 | 050 | 157 | 026 | 167 | 028 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82224 | not available | 5042 | 029 | 1394 | 187 | 675 | 015 | 976 | 1106 | 328 | 005 | 002 | 500E-08 | 1646 | 119 | 640 | 58 | 44 | 105 | 640 | 042 | 1140 | 100E-07 | 159 | 100E-07 | 500E-08 | 54 | 200E-07 | 109 | 500E-08 | 500E-08 | 204 | 12 | 41 | 14 | 022 | 124 | 075 | 041 | 160 | 036 | 265 | 063 | 195 | 031 | 206 | 032 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82225 | not available | 4701 | 022 | 1065 | 127 | 739 | 015 | 1732 | 727 | 233 | 002 | 001 | 500E-08 | 2735 | 106 | 1730 | 84 | 32 | 75 | 1730 | 062 | 1180 | 100E-07 | 690 | 100E-07 | 500E-08 | 43 | 2 | 415 | 500E-08 | 500E-08 | 159 | 11 | 58 | 9 | 023 | 128 | 063 | 031 | 125 | 028 | 204 | 050 | 161 | 026 | 162 | 025 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82226 | not available | 4256 | 014 | 689 | 357 | 494 | 011 | 2593 | 578 | 016 | 003 | 001 | 75 | 3377 | 038 | 2280 | 102 | 8 | 55 | 2280 | 015 | 835 | 100E-07 | 1380 | 100E-07 | 1 | 31 | 200E-07 | 205 | 500E-08 | 500E-08 | 104 | 5 | 46 | 6 | 008 | 042 | 027 | 010 | 058 | 013 | 097 | 025 | 075 | 012 | 078 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82228 | not available | 4399 | 016 | 796 | 185 | 65 | 014 | 246 | 647 | 017 | 001 | 001 | 500E-08 | 9402 | 076 | 2890 | 102 | 10 | 55 | 2890 | 052 | 1050 | 100E-07 | 1130 | 100E-07 | 500E-08 | 35 | 200E-07 | 65 | 500E-08 | 500E-08 | 131 | 6 | 41 | 7 | 017 | 072 | 032 | 010 | 065 | 014 | 106 | 027 | 084 | 013 | 082 | 013 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82229 | not available | 4897 | 024 | 1196 | 106 | 807 | 015 | 1448 | 71 | 298 | 003 | 002 | 500E-08 | 11033 | 081 | 1260 | 77 | 45 | 9 | 1260 | 024 | 1160 | 100E-07 | 459 | 100E-07 | 500E-08 | 46 | 200E-07 | 138 | 500E-08 | 500E-08 | 172 | 11 | 59 | 11 | 016 | 093 | 052 | 028 | 119 | 027 | 203 | 050 | 157 | 026 | 168 | 027 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82231 | not available | 509 | 027 | 1399 | 178 | 674 | 014 | 87 | 1152 | 329 | 005 | 002 | 500E-08 | 1186 | 092 | 510 | 52 | 58 | 10 | 510 | 038 | 1100 | 100E-07 | 136 | 100E-07 | 500E-08 | 57 | 2 | 144 | 500E-08 | 500E-08 | 202 | 13 | 41 | 12 | 018 | 101 | 057 | 030 | 135 | 030 | 220 | 058 | 177 | 029 | 191 | 029 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82234 | not available | 4847 | 087 | 1468 | 1174 | 022 | 874 | 1394 | 099 | 027 | 008 | 332 | 83 | 3 | 225 | 21 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82236 | not available | 5135 | 087 | 1461 | 1117 | 02 | 757 | 1032 | 274 | 109 | 008 | 228 | 70 | 15 | 329 | 19 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
135482 | Trillbar Complex | 5137 | 037 | 1481 | 232 | 561 | 016 | 869 | 1068 | 306 | 006 | 003 | 014 | 260 | 10014 | 39 | 2 | 593 | 59 | 61 | 00 | 08 | 08 | 1 | 124 | 1 | 1 | 51 | 00 | 08 | 235 | 17 | 61 | 20 | 0 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143538 | Trillbar Complex | 4961 | 141 | 1391 | 561 | 717 | 022 | 656 | 1136 | 204 | 022 | 011 | 014 | 163 | 10036 | 322 | 15 | 82 | 172 | 91 | 12 | 26 | 26 | 9 | 98 | 4 | 4 | 48 | 12 | 14 | 362 | 24 | 91 | 86 | 2 | 12 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143539 | Trillbar Complex | 4974 | 086 | 1196 | 128 | 734 | 016 | 1072 | 1395 | 237 | 009 | 006 | 013 | 150 | 10047 | 77 | 10 | 298 | 80 | 47 | 07 | 14 | 14 | 4 | 240 | 2 | 1 | 59 | 07 | 06 | 322 | 19 | 47 | 46 | 2 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
144310 | Trillbar Complex | 4711 | 115 | 1288 | 182 | 901 | 018 | 784 | 1161 | 250 | 008 | 012 | 013 | 240 | 10027 | 53 | 13 | 394 | 116 | 90 | 13 | 13 | 13 | 7 | 156 | 6 | 1 | 37 | 13 | 14 | 380 | 23 | 90 | 78 | 0 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
iii
Contents
Abstract 1Introduction 1Regional tectonic setting 3Geology stratigraphy and geochronology 4
Peak Hill Schist and Marymia Inlier 5Bryah Group 6
Karalundi Formation 6Narracoota Formation 7
Peridotitic and high-Mg basalt association 7Intrusive rocks and layered intrusions 7Mafic and ultramafic schist 8Metabasaltic hyaloclastite 9Felsic schist 9Volcaniclastic rocks 10Carbonated and silicified metavolcanic rocks 11Jasperoidal chert 11Geochemistry of the Narracoota Formation 11
Ravelstone Formation 16Horseshoe Formation 16
Padbury Group 17Labouchere Formation 18Wilthorpe Formation 19
Beatty Park and Heines Members 19Robinson Range Formation 20Millidie Creek Formation 20Unassigned units of the Padbury Group 21
Structure 21D1 structures 23D2 structures 23D3 structures and their relationship to D2 structures 25D4 structures 25
Metamorphism 25Structural synthesis 27Mineralization 32
Gold deposits 33Peak Hill Jubilee and Mount Pleasant deposits 39Harmony deposit 41Labouchere Nathans and Fortnum deposits 41Wembley deposit 42Wilgeena deposit 43Durack St Crispin and Heines Find prospects 43Ruby Well group 43Mikhaburra deposit 43Wilthorpe deposit 43Cashman deposit 44
Volcanogenic copperndashgold deposits 44Supergene manganese deposits 44Iron ore 45Talc 45Discussion 45
Tectonic model and conclusions 46Acknowledgements 48References 49
Appendix
Gazetteer of localities 52
Plate
Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
iv
Figures
1 Stratigraphy of the former lsquoGlengarry Basinrsquo 22 Simplified geology of the Bryah Padbury and Yerrida Basins 43 Rotated orthoclase porphyroblast Peak Hill Schist 54 Partially recrystallized mylonite Peak Hill Schist 55 Peak Hill Schist mylonite from the Hangingwall Sequence 56 Outcrop of quartz mylonite Peak Hill Schist 67 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric 68 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt) 89 Basaltic hyaloclastite Narracoota Formation 9
10 Mafic volcaniclastic rock Narracoota Formation 1011 Volcanic breccia intersected in diamond drillhole BD1 1012 Total alkali versus silica diagram for rocks the Narracoota Formation 1313 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the
Narracoota Formation 1414 Geochemical characteristics of the Narracoota Formation rocks 1415 Geochemical discriminant plots for Narracoota Formation 1516 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation 1617 Schematic stratigraphy of the Horseshoe Formation 1718 Major regional structures in the Bryah and Padbury Groups 2219 Simplified geological map of the Bryah and Padbury Groups 2420 Selected hypothetical cross sections through the Bryah and Padbury Groups 2721 Model of the structural development of the BryahndashPadbury Group succession 2922 New model of the structural development of the BryahndashPadbury Group succession 3123 New model for the structural development of the BryahndashPadbury Group succession
and the Peak Hill Schist 3224 Schematic north-northwest to south-southeast cross section from the Bangemall Basin
into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins 3325 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins 3626 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet 3827 Albite porphyroblasts in mylonitic schist at Mount Pleasant 3928 The Mine Sequence schist 4029 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit 4030 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and
Marker quartzite unit 4031 Diagrammatic cross section of the Harmony ore zones 4132 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and
deformed Despair Granite 4433 Sketch illustrating a conceptual model for the origin of precious and base metal
deposits in the BryahndashPadbury and Yerrida Basins 4534 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and
Padbury Basins within the context of the Capricorn Orogen 46
Tables
1 Stratigraphy of the Bryah and Padbury Groups 32 Representative chemical analyses of the Narracoota Formation 123 Magnesium numbers for the Narracoota and Killara Formations 134 Selected geochemical parameters for the Narracoota Formation 135 Sequence of deformation events in the Bryah and Padbury Basins 236 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic
minerals of the Bryah Group and deformation fabrics 287 Gold production and remaining resources in the Bryah and Padbury Groups 348 Mineral production and remaining resources in the Bryah and Padbury Groups 359 Mineral deposits and occurrences in the Bryah and Padbury Basins 36
Digital dataset (in pocket)
Whole-rock geochemical analyses of Narracoota Formation rocks (narracootacsv)
1
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Geology and mineralization of thePalaeoproterozoic Bryah and Padbury
Basins Western Australia
by
F Pirajno S A Occhipinti and C P Swager
AbstractThe Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collision zonebetween the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains a succession of maficand ultramafic rocks of mid-oceanic ridge basalt to oceanic plateau affinity overlain by clastic andchemical sedimentary rocks The Bryah Basin was formed during back-arc sea-floor spreading andrifting on the northern margin of the Yilgarn Craton The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of the Bryah Basin as a forelandstructure resulting from either the c 1800 Ma oblique collision of the Pilbara and Yilgarn Cratons(Capricorn Orogeny) or the c 2000 Ma collision of the Glenburgh terrane and the Yilgarn Craton(Glenburgh Orogeny)
Important mineral deposits are contained in both basins and include mesothermal orogenic goldcopperndashgold volcanogenic massive sulfides manganese and iron ore The origin of the goldmineralization is related to metamorphism and deformation linked to the Capricorn Orogeny at c 18 GaThe formation of other deposits is related to pre-orogenic syngenetic processes
KEYWORDS Bryah Basin Padbury Basin Palaeoproterozoic stratigraphy geochemistry maficrocks ultramafic rocks mineralization mesothermal deposits gold
IntroductionIn early 1994 the Geological Survey of Western Australia(GSWA) commenced fieldwork to reassess the geologyand mineralization of the Palaeoproterozoic GlengarryBasin as part of a program of new mapping initiativesThe Glengarry Basin as defined by Gee and Grey (1993)constitutes the western part of the greater Palaeo-proterozoic Nabberu Province which in the east includesthe Earaheedy Basin (Bunting et al 1977 Hall andGoode 1978 Gee 1990)
The new mapping initiative resulted in the reappraisalof the geology tectonic evolution and mineralizationof the Glengarry Basin which is now recognized toconsist of three main geotectonic units the BryahPadbury and Yerrida Basins As a result the volcano-sedimentary rocks of the former lsquoGlengarry Grouprsquo arenow divided into the Bryah and Yerrida Groups (Fig 1 andTable 1) characterized not only by different lithologiesbut also by different regional structures metamorphismand mineral deposit types Some formations previouslyassigned to the lsquoGlengarry Grouprsquo have been reassigned
to the Padbury Group (Martin 1992) In additionthere is evidence to suggest that the economicallyimportant lsquoPeak Hill Metamorphic Suitersquo previouslyconsidered to be part of the lsquoGlengarry Grouprsquo (Gee1987) constitutes a separate unit the Peak Hill Schistderived from a protolith of probable Archaean ageConsequently the previous nomenclature (lsquoGlengarryGrouprsquo and lsquoGlengarry Basinrsquo) is no longer used Detailsof the old and new stratigraphy are presented in Figure 1and Table 1 and discussed in later sections The revisedstratigraphy of the former lsquoGlengarry Basinrsquo is presentedin Occhipinti et al (1997) Details of the stratigraphy andstructure of the lower Padbury Group are presented inMartin (1998)
The Bryah and Padbury Basins lie within the ROBINSON
RANGE and PEAK HILL 1250 000 sheets (MacLeod 1970Elias and Williams 1980 Gee 1987) and the north-western and northeastern corners of the BELELE andGLENGARRY 1250 000 sheets (Elias 1982 Elias et al
Capitalized names refer to standard 1100 000 map sheets unless otherwisespecified
2
Pirajno et al
1982) The Bryah and Padbury Groups (Fig 2) make upthe western part of the former lsquoGlengarry Basinrsquo andare now interpreted to have developed in rift and forelandbasins respectively (Martin 1994 Pirajno 1996 Pirajnoet al 1996 Pirajno et al 1998b) The Yerrida Group(Fig 2) makes up the eastern part of the former lsquoGlengarryBasinrsquo and includes two subgroups the Windplainand Mooloogool Subgroups (Fig 2 Table 1) whichdeveloped in sag and rift basins respectively (Pirajno et al1995ab 1996) The geology and mineralization ofthe Yerrida Basin are described in a separate Report(Pirajno and Adamides 2000) The Bryah Group isin faulted contact with the Yarlarweelor gneiss complexthe Marymia Inlier of the Archaean Yilgarn Cratonand the Palaeoproterozoic Yerrida Group The contactbetween the Bryah and the Yerrida Groups is along anortheasterly trending high-angle reverse fault (the GoodinFault)
Based on structural and metamorphic criteria the areaoccupied by the Bryah and Padbury Groups and thePeak Hill Schist can be regarded as a single domainIn this Report where appropriate this domain is referred
to as the BryahndashPadbury Basin The geology newstratigraphy geochronological constraints structureand metamorphism of the Bryah and Padbury Groups arediscussed The geochemistry of the volcanic componentof the Bryah Group and mineral deposits of the Bryahand Padbury Basins are also summarized A tectonicoverview and proposed model for the geodynamicevolution of the Bryah and Padbury Basins withinthe framework of the Capricorn Orogen conclude thereport
Work in the BryahndashPadbury area involved 125 000-scale mapping to produce 1100 000-scale geologicalmaps Geological mapping was carried out using125 000-scale colour aerial photography (availablefrom the Western Australian Department of LandAdministration) aeromagnetic images (400 m line-spacedcollected by GSWA in 1994) and Landsat TM imagesResults of geological mapping were integrated withpetrographic geochemical and geochronology studiesDuring this work a total of 1450 rock samples werecollected of which 776 were thin-sectioned and 136geochemically analysed In addition logging of diamond
Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
Gee (1987)P
AD
BU
RY
BA
SIN
GR
OU
PG
LEN
GA
RR
Y B
AS
ING
RO
UP
Millidie Creek Formation
Robinson Range Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Narracoota Volcanics
Karalundi Formation
Doolgunna Formation
Johnson Cairn Shale
Thaduna Greywacke
Juderina Formation
Maraloou Formation
Crispin Conglomerate
Finlayson Sandstone
Peak Hill Metamorphics
GLE
NG
AR
RY
BA
SIN
GR
OU
P
Maraloou Formation
Thaduna Greywacke
Narracoota Volcanics
Doolgunna Formation
Johnson Cairn Shale
Juderina Formation(Finlayson SandstoneMember)
YE
RR
IDA
BA
SIN
GR
OU
P
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Peak Hill Schist
BR
YA
H B
AS
ING
RO
UP
PA
DB
UR
Y B
AS
ING
RO
UP
TE
CT
ON
IC C
ON
TA
CT
Millidie Creek Formation
Wilthorpe Formation
Labouchere Formation
Horseshoe Formation
Karalundi Formation
Ravelstone Formation
Narracoota FormationMaraloou Formation
Killarra Formation(Bartle Member)
Doolgunna Formation
Thaduna Formation
Juderina Formation
170100
Gee and Grey (1993) Occhipinti et al (1997) Pirajno et al (1998b this study)
Robinson RangeFormation
Unconformity
Unconformity
Johnson CairnFormation
NOTE New or redefined units (Occhipinti et al 1997)
(Finlayson and BubbleWell Members)
ARCHAEAN BASEMENT
FMP409a
3
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
drillcore (1100 m) and several visits to prospects andoperating mines considerably enhanced our knowledge ofthe geology of the area Most of the mapped areas werealso included in a regional regolith geochemical samplingprogram covering the PEAK HILL ROBINSON RANGE andGLENGARRY 1250 000 sheets (Subramanya et al 1995Bradley et al 1997 Crawford et al 1996)
Interim accounts of the structural and stratigraphicrelations of the BryahndashPadbury and Yerrida Basins havebeen reported by Pirajno et al (1995ab 1996) andOcchipinti et al (1997) Pirajno (1996) and Pirajno et al(1995a 1998b) discussed possible models for the tectonicevolution of the BryahndashPadbury and Yerrida Basins Thestructure and metamorphism of the BryahndashPadbury Basinhave been described by Occhipinti et al (1998abc)whereas details of mineral potential production andore deposit geology can be found in Pirajno andOcchipinti (1995) and Pirajno and Preston (1998)Published 1100 000 geological maps and accompanyingExplanatory Notes that wholly or partly cover the BryahndashPadbury Basin comprise BRYAH (Pirajno and Occhipinti1998) GLENGARRY (Pirajno et al 1998a) MILGUN (Swagerand Myers 1999) PADBURY (Occhipinti et al 1998a)DOOLGUNNA (Adamides 1998) and MARYMIA (Bagas1998) The southern portion of the JAMINDI 1100 000 mapsheet containing rocks of the Bryah Group was alsomapped The layout of these map sheets in relation to theBryahndashPadbury Basin and adjacent tectonic units is shownin Figure 2 The geology of the Bryah and Padbury Basinsis presented in Plate 1
Regional tectonic settingThe Bryah and Padbury Basins are situated along thenorthern margin of the Archaean Yilgarn Craton and arepart of the Capricorn Orogen (Fig 2 inset of Plate 1)The Capricorn Orogen also includes the Ashburton Basin
and the Gascoyne Complex and can be traced for morethan 1000 km with northwesterly to westerly trendsforming a broad belt of deformed low-grade volcano-sedimentary high-grade metamorphic and granitoidrocks
The Capricorn Orogeny resulted from the collisionbetween the Pilbara and Yilgarn Cratons at c 1800 Maand involved the closure of an intervening oceanformation of a back-arc basin and the possible accretionof microcontinental fragments (Myers 1993 Myers et al1996 Tyler et al 1998) Prior to the Capricorn Orogenythe c 2000 Ma Glenburgh Orogeny (Occhipinti et al1999) resulted in the accretion of the Glenburgh terraneonto the Yilgarn Craton The convergence between thePilbara and Yilgarn Cratons was essentially oblique andresulted in the development of easterly trending strike-slipmovements which included regional sinistral faults TheCapricorn Orogeny also affected other tectonic units suchas the Archaean Narryer Terrane Marymia Inlier SylvaniaInlier and parts of the Hamersley Basin (Tyler andThorne 1990 Myers et al 1996 Tyler et al 1998)
The Palaeoproterozoic volcano-sedimentary andsedimentary successions of the Bryah and Padbury Basinsare unconformable on the northern margin of the YilgarnCraton whereas to the north they are either unconform-ably overlain by or in faulted contact with rocksof the Bangemall Basin and the Archaean graniticrocks of the Marymia Inlier The Marymia Inlier iseconomically important because it hosts a number of golddeposits including the Peak Hill deposit (AMG 672190E7163150N) on the southwestern tip of the inlier (seeMineralization)
Localities are specified by the Australian Map Grid (AMG) system AMGcoordinates (eastings and northings) of localities discussed in the text arelisted in Appendix 1
Table 1 Stratigraphy of the Bryah and Padbury Groups
Group Age Formation Rock type(Ma)
Padbury Group Millidie Creek sericitic siltstone chloritic siltstone banded iron-formation(peripheral foreland basin) dolomitic arenite
Robinson Range ferruginous shale banded iron-formation
ltc 2000 Wilthorpe quartz-pebble conglomerate(Beatty Park and (siltstonendashwacke and polymictic conglomerate respectively)Heines Members)
Labouchere turbidite sequence (quartz wacke siltstone)
unconformable contact mdash tectonized in many places
Bryah Group (rift basin) Horseshoe banded iron-formation wacke shale
ltc 2000 Ravelstone quartzndashlithic wacke
Narracoota maficndashultramafic volcanic rocks and intercalated sedimentary rocks
Karalundi conglomerate quartz wacke
faulted contact
Yerrida Group (sag and rift basin) c 2174
SOURCE Modified after Pirajno et al (1996)
4
Pirajno et al
Geology stratigraphy andgeochronology
The BryahndashPadbury Basin contains the Bryah andPadbury Groups and the Peak Hill Schist The stratigraphyfor the Bryah and Padbury Groups is summarized in
Figure 1 and Table 1 where a comparison with previousGSWA work is also provided The Peak Hill Schist is aseparate tectono-stratigraphic unit that is discussed herewith the Marymia Inlier as basement to the Bryah GroupDetailed descriptions of the various formations and theircontact relationships are presented in Occhipinti et al(1997) Martin (1998) Adamides (1998) Pirajno and
Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins showing 1100 000 map sheet boundariesInset shows the position of the basins in relation to the Capricorn Orogen
MARYMIAINLIER
GOODININLIER
Goodin
Fault
Fault
Killara
Narracoota
30 km
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
FMP375
117deg
30
118deg
30
26deg00
25deg00
Murchison
FaultMorris
Earaheedy Group
Padbury Group
Yerrida Group
Archaean granitendashgreenstonebasement
Bangemall Group
Bryah Group
Proterozoic granites
Fault
Moorarie Padbury
MilgunMarquis
FaultCooinbar
NarryerTerrane
Murchison
Terrane
Kerba Fault
119deg
30
Gabanintha Yanganoo
MooloogoolGlengarry
Bryah Doolgunna
Jamindi Three Rivers
010300
BRYAH-PADBURY
BASINS
PROTEROZOIC
5
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Occhipinti (1998) Pirajno et al (1998b) Occhipinti et al(1998c) and Swager and Myers (1999)
In this section the geology field relations stratigraphyand geochronological constraints of the Peak Hill SchistMarymia Inlier and the formations that make up the Bryahand Padbury Groups are discussed
Peak Hill Schist and MarymiaInlierThe Peak Hill Schist (formerly called the lsquoPeak HillMetamorphic Suitersquo Gee 1987) is exposed in the lsquoPeakHill Domersquo or anticline and constitutes a tectonic unitrepresenting the southwestern tip of the Marymia Inlier(Fig 2 Thornett 1995) The Peak Hill Schist iscontinuous with the Marymia Inlier and Thornett (1995)suggested that the lsquoPeak Hill Domersquo represents thedeformed southwestern end of the Marymia Inlier Fieldobservations and petrographic and aeromagnetic datasupport this view The boundary between the Peak HillSchist and granitic rocks of the Marymia Inlier is a zoneof intense deformation and metamorphism characterizedby tectonic interleaving and duplexing Towards thenortheast the intensity of the Capricorn Orogenydeformation in the Marymia Inlier granites decreases toareas where they are undeformed The contacts betweenthe Peak Hill Schist and rocks of the Bryah Group arefaulted (probably thrusted) and tectonically interleaved inplaces
Rocks of the Peak Hill Schist include phyllonitequartzndashmuscovite schist calc-silicate schist sericite(ndashquartz) schist and quartzndashmuscovitendashbiotitendashchloriteschist locally with rotated alkali feldspar porphyroblasts(Fig 3) and minor metabasite These units have beenvariously deformed and contain a range of mylonitictextures The mylonitic fabric of these rocks is revealedby SndashC surfaces and lines of lsquomica fishrsquo (Lister and Snoke1984) in a dominantly and variably recrystallized quartz-rich matrix (Figs 4 and 5) A few discrete mylonitic units
Figure 3 Orthoclase porphyroblast with curved inclusiontrails in quartzndashmuscovite schist of the Peak HillSchist crossed polars
Figure 4 Partially recrystallized mylonite (Crispin Mylonite)from the Peak Hill Schist This sample is from amylonitic quartzndashbiotitendashalbite schist from the MineSequence in which the biotite defines C planesThe S planes were obliterated by recrystallizationto a blastomylonite crossed polars
Figure 5 Peak Hill Schist mylonite The C surfaces havesurvived recrystallization and now form thin micatrails crossed polars
form arcuate zones interpreted as early possibly thrustfault zones (see Structure) One of these units is the PeakHill Mylonite (Pirajno and Occhipinti 1998) which is arefolded quartz blastomylonite and quartz mylonite lenswithin quartzndashmuscovite schist The Peak Hill Mylonite(Figs 6 and 7) is an important unit because it is spatiallyassociated with gold mineralization (Peak Hill and MountPleasant deposits) Other less conspicuous quartzmylonite lenses are common within the Peak Hill Schistand were previously mapped as cherts or banded cherts(Windh 1992) Another important unit is the CrispinMylonite (Pirajno and Occhipinti 1998) which lies in thesouthern part of the Peak Hill Schist between sericiteschist and quartzndashmuscovite schist The Crispin Mylonitereferred to by Gee (1987) as the lsquoCrispin Conglomeratersquois characterized by square to rounded quartz arenite clastsup to 60 cm long in a sericite-rich matrix On the basisof field and petrographic observations it is concluded
6
Pirajno et al
here that this unit is not a conglomerate but a mylonite(Pirajno and Occhipinti 1998) Mylonites that resembleconglomerates (pseudo- or tectonic conglomerates) havebeen reported by Peters (1993) and Raymond (1984ab)
The Marymia Inlier (Windh 1992 lsquoMarymia Domersquoof Gee 1987) represents a fragment of northeasterlytrending Archaean granitendashgreenstone basement Rocksof the Marymia Inlier are mainly granitic but also includesmall enclaves of calc-silicate rock orthoamphibolite andminor metamorphosed banded iron-formation (BIF) ThePeak Hill Schist is also tentatively placed within theMarymia Inlier The granitic rocks are locally stronglyfoliated to gneiss or display strong cataclastic fabricsGranitic rocks include both fine-grained (aplitic) andcoarse-grained porphyritic phases Some outcropspreviously mapped as granite by Gee (1987) have beenincluded in the Peak Hill Schist The granitic rocks of theMarymia Inlier are monzogranite in the east and showincreasing cataclastic deformation towards the southwest(Pirajno and Occhipinti 1998 Bagas 1998)
Bryah GroupThe Bryah Group is divided into four formations theKaralundi Narracoota Ravelstone and HorseshoeFormations (Figs 1 and 2 Table 1) The basal unit of theBryah Group is the Karalundi Formation which is infaulted contact with the Doolgunna Formation of theYerrida Group along the Goodin Fault The KaralundiFormation predominantly consists of quartz conglomeratequartz arenite lithic wacke and shale The NarracootaFormation (parts of which were previously known aslsquoNarracoota Volcanicsrsquo Gee and Grey 1993) is thedominant lithology in the Bryah Basin and consists oftholeiitic extrusive and intrusive rocks and subordinateultramafic units intercalated with minor jasperoidal chertunits and clastic sedimentary rocks The NarracootaFormation is disconformably overlain by and locallyinterfingers with the Ravelstone Formation TheRavelstone Formation comprises a succession of lithic andquartz wacke shale and siltstone that was deposited byturbidity currents This formation is in turn conformablyoverlain by the Horseshoe Formation comprising quartzwacke manganiferous shale and banded iron-formation
The age of the Bryah Group is poorly constrainedbetween c 2000 and 1800 Ma Detrital zircons ofuncertain provenance in the Ravelstone Formation (upperBryah Group) provide a maximum age of 2014 plusmn 22 Ma(Nelson 1997) The Bryah Group must be older than theunconformably overlying Mount Leake Formation (outlierof the Earaheedy Group) which has a UndashPb (detritalzircon) maximum age of 1785 plusmn 11 Ma (Nelson 1997)The PbndashPb isochron ages obtained from pyrite from themesothermal Mikhaburra gold deposit (174 Ga Pirajnoand Occhipinti 1998) and from inferred syngenetic pyritefrom the Narracoota Formation (1920 plusmn 35 Ma Windh1992) probably represent mineralizing events in the BryahBasin rather than the depositional age of the BryahGroup
Karalundi Formation
The Karalundi Formation forms the base of the BryahGroup outcropping in a northeasterly trending belt alongthe southeastern margin of the Bryah Basin (Plate 1)Rocks of the Karalundi Formation are estimated to reacha thickness of approximately 2500 m In the southeastalong the Great Northern Highway Karalundi Formationrocks are in faulted contact with the Doolgunna Formation(Yerrida Group) On the southeastern side of the Peak HillSchist and in faulted contact with it the KaralundiFormation outcrops 35 km east of the Wilgeena mine Inthe south the Karalundi Formation is intercalated withmafic volcaniclastic rocks of the Narracoota Formation
The Karalundi Formation is characterized by immatureclastic (mainly quartzndashlithic wacke and conglomerate)units containing angular quartz and lithic fragments setin a sericitendashclay-rich matrix Other rock types includesiltstone calcareous siltstone cross-bedded areniteferruginous arenite litharenite minor dolomite andpurple green and black shale The Karalundi Formationalso contains pods of hematitic jasperoidal chert (see
Figure 6 Outcrop of quartz mylonite Peak Hill Schist Notethe flaggy nature of this rock and its steep dip
Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating atypical mylonitic fabric and SndashC planes (C planesare horizontal S planes trend from upper right tolower left between the C planes) crossed polars
7
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
below) which were interpreted by Gee (1979 1987) asfumarolic pipes
On DOOLGUNNA quartz arenite and conglomerate unitsare present within a dominantly hematitic shaly successionthat was interpreted by Adamides (1998) as a deep-waterlateral facies of the Bryah rift succession This successionalso contains olistoliths (exotic blocks) whose origin isnot clear Adamides (1998) suggested that they might havebeen derived from units of the Juderina Formation as aresult of inversion of the adjacent Yerrida Basin and upliftof the Goodin Inlier
Narracoota Formation
Rocks of the Narracoota Formation constitute a majorlithotype of the Bryah Group They form the bulk of thegroup with a thickness estimated at about 6 km (Pirajnoand Occhipinti 1998) and extend for more than 180 kmeast to west across the Bryah Basin The NarracootaFormation conformably overlies and locally interfingerswith the Karalundi Formation and also interfingers withand is in disconformable contact with the base of theoverlying Ravelstone Formation Contacts between theNarracoota Formation and Padbury Group are tectonic Inthe north regional structural relationships suggest that theNarracoota Formation is also in tectonic contact with theHorseshoe Formation Gravity modelling indicates that theNarracoota Formation forms the floor of the central partsof the Bryah Basin (Pirajno and Occhipinti 1998)
Rocks of the Narracoota Formation are affected bysea-floor metasomatism and regional prograde andretrograde metamorphism (see Structure) On the basisof field observations texture geochemistry and petrologyrocks of the Narracoota Formation can be subdivided intometamorphosed peridotitic and high-Mg metabasaltbasaltic hyaloclastite pyroclastic rocks intrusive rocksand mafic and ultramafic schist Collectively thesesubdivisions are referred to as metabasites Mafic andultramafic schists are characterized by a pervasiveschistosity but the distinction between mafic andultramafic is subtle and most clearly demonstrated usinggeochemistry In the area 2 km northeast of the Ravelstonemanganese opencuts a texture described by Hynes andGee (1986) as polygonal jointing has been observed in themetabasalt and appears to be a well-developed pencilcleavage High-Mg basalts are associated with peridotiticunits Intrusive rocks cover a range of types frompyroxenite to gabbroic rocks and dykes Metabasaltichyaloclastites are lava flows that interacted with seawaterand have a distinct spilitic character Volcaniclastic rocksincluding vent breccias are commonly present in bothbasaltic hyaloclastite and mafic schist
Typically the metabasite rocks of the NarracootaFormation contain no or very few feldspar phenocrystsOther authors have suggested that the presence ofmedium-grained embayed quartz crystals indicates theproximity of felsic volcanic rocks (Hill and Cranney1990 Windh 1992) Felsic volcanic rocks are associatedwith the upper part of the Narracoota Formation at andaround the Horseshoe Lights copperndashgold mine onJAMINDI 29 km east of the Fortnum mine on MILGUN
Fine-grained grey to black metamorphosed shale andslate are present in places as lenses of interflowsedimentary rocks within the volcanic succession Wheremore deformed and metamorphosed these slates are finelylaminated biotitendashchlorite schists South of the RobinsonRange small lenses of sedimentary rock (lithic wacke andshale) are intercalated with the volcanic rocks of theNarracoota Formation In places pods and lenses ofjasperoidal chert are associated with the volcanic rocks
Peridotitic and high-Mg basalt association
Massive layered high-Mg basaltic rocks (possibly lavaflows shown on Plate 1 as Anu) are preserved inprominent hills between Top Dimble Well and DespairBore on MILGUN Hynes and Gee (1986) described thissequence as komatiitic basalt with up to 20 MgOUnequivocal pillow structures as mentioned by Hynes andGee (1986) were not observed The rocks are meta-morphosed but their protoliths include olivine cumulate(peridotite) high-Mg basalt with plumose and harrisitictextures and medium-grained basalt Layering is mainlydefined by massive olivine cumulate layers up to 20 mthick and plumose-textured basalt layers up to 5 m thickLocally large sheaves of skeletal amphibole (afterpyroxene) are arranged at approximately right angles tothe layering and resemble harrisitic textures (Fig 8a) Thehigh-Mg basalt units are characterized by well-developedlsquospinifexrsquo-like textures with acicular tremolitendashactinoliteafter pyroxene and up to 30 interstitial plagioclase(replaced by epidote or zoisite) The high-Mg basalt isinterlayered with medium-grained basalt of similarmineralogy and composition with 8ndash9 MgO Thewhole-rock geochemistry of these rocks is discussed inGeochemistry of the Narracoota Formation
Peridotite units commonly consist of 70ndash80 fine- tomedium-grained olivine replaced by tremolite(ndashtalc)skeletal amphiboles after pyroxene and 20ndash30 fine-grained matrix of plumose-textured amphibole High-Mgbasalt contains up to 30 locally glomeroporphyriticolivine (now tremolite) lesser amounts of acicularpyroxene in a 60ndash70 amphibole plumose-texturedmatrix and 15 MgO One particular example contains35 olivine (only partly altered to talc) skeletal(lsquoswallow-tailrsquo) fresh orthopyroxene and lesser amountsof acicular skeletal amphibole prisms possibly afterclinopyroxene (Fig 8b)
Intrusive rocks and layered intrusions
A metadolerite sheeted dyke complex (shown as And onPlate 1) outcrops north of the Robinson Syncline Theserocks are associated with deformed pillow metabasalt andtend to be internally undeformed but commonly formelongate bodies subparallel to the S2 foliation Theycontain diopside amphibole epidote and minor olivine
Lenses of cumulate-textured units represented bypyroxenite or peridotite and gabbroic rocks are locallyintercalated with the mafic and ultramafic schist Alensoidal outcrop of metapyroxenite is present nearDurack Well Gabbroic rocks are common betweenTrillbar Homestead and Friday Pool on MOORARIE
8
Pirajno et al
(Occhipinti and Myers 1999) These rocks have beenmetamorphosed and folded but are largely undeformedinternally The gabbroic rocks are surrounded by higherstrain zones consisting of tremolitendashactinolite schist
The Trillbar Complex (shown as Ant on Plate 1) is a30 km long by 25 km wide layered maficndashultramaficintrusion in the westernmost part of the Bryah Basin Thecomplex consists of rhythmically layered mafic andultramafic rocks with the layering oriented at a low angleto the regional foliation (Occhipinti and Myers 1999)Rock types include rhythmically layered gabbromelanogabbro leucogabbro pyroxenite and peridotiteThese rocks are metamorphosed to greenschist facies butthe original igneous textures are locally well preservedThe Trillbar Complex rocks contain assemblages ofserpentinendashtremolitendashtalc tremolitendashtalcndashmagnetitetremolitendashactinolite and actinolitendashfeldspar Cumulaterocks include olivinendashpyroxene pseudomorphed bytremolite and sphene West of the Trillbar Homestead arelayers of metamorphosed pyroxenite and peridotite inwhich the original mineral phases are totally replaced by
tremolite talc magnetite and chlorite The TrillbarComplex is interpreted here as representing a remnant ofLayer 3 (layered gabbroic rocks) of an oceanic crustsuccession (Burke et al 1981) If this is correct thenprogressively lower levels of the Narracoota Formation areexposed from east to west and this is supported by thewidespread occurrence of volcaniclastic units in thecentral and eastern parts of the Bryah Basin
Mafic and ultramafic schist
Maficndashultramafic schist consists of actinolite(ndashchloritendashclinozoisite) schist and chlorite schist (shown as Anu andAn on Plate 1) In the south-central part of BRYAH schistoutcrops form an arcuate band (possibly an antiformstructure Gee 1987) south of and following the trendsof the Robinson Syncline and the southern limbs of theFraser Synclinorium (see Structure) North of thesestructures sparse outcrops of mafic schist are present justsouth and north of the Peak Hill Schist Within the schistare pods of less deformed or internally undeformedmetabasites in which pillow structures are locally wellpreserved Overall this large band forms a majoranastomosing sheared domain (Pirajno et al 1995b) Thedominant schistosity strikes approximately easterly orwest-northwesterly and dips steeply to the north andsouth A number of quartz veins within this shear domainalso strike easterly Maficndashultramafic schist was formedas a result of deformation and metasomatism of metabasiterocks along D2 shear zones (see Structure) In most casesall original volcanic textures are obliterated although inplaces round or elongate chlorite aggregates areinterpreted as original amygdales or fine pyroclasts
To the northwest on MILGUN the mafic volcanicschist occurrences are in faulted or sheared contactwith rocks of the Labouchere Wilthorpe and RobinsonRange Formations Hill and Cranney (1990) documenteda sequence of ultramafic to mafic schists with orwithout jasperoidal chert lenses overlain by fragmentalvolcaniclastic rocks fine-grained siltstone and felsic(intermediate and dacitic) crystal tuffs These are in turnoverlain by the Ravelstone and Horseshoe Formations
Mineral constituents of the mafic schist are actinolitechlorite and clinozoisite with minor calcite pumpellyitesericite titanite quartz and relict albite Ultramafic schisthas a simpler and commonly almost monomineralicmineralogy consisting of actinolitendashtremolite withretrogressed patches of pale-green chlorite In zones ofmore intense deformation chlorite- or epidote-dominatedassemblages are present (chlorite schist and epidositerespectively) These minerals developed due to strongmagnesium and calcium metasomatism probably duringcirculation of H2OndashCO2 fluids (Pirajno et al 1995b) Fluidinfiltration caused the breakdown of tremolite andclinozoisite to produce chlorite calcite and silica Thesilica thus liberated was then channelled through shearzones resulting in silicification and quartz veins (Pirajnoet al 1995b) An example of this can be seen in abreakaway 13 km east of the Wembley gold mine wheremafic schist and deformed pillow lavas display chloritealteration and pervasive silicification near and along awest-northwesterly trending shear zone In high-strain
Figure 8 Maficndashultramafic volcanic rocks of the NarracootaFormation (Dimble Belt) a) Komatiitic pyroxenitewith skeletal amphibole prisms after a quench-textured pyroxene matrix b) Peridotite with olivinepartly altered to talc around the edges and pyroxenein a fine-grained tremolite matrix both in planepolarized light
9
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
zones a new fabric is defined by the alignment ofamphibole prisms elongate epidote and quartz Theseschists are commonly characterized by well-developedlsquopencil cleavagersquo as a result of two intersecting planarfabrics
Metabasite rocks commonly show relict igneoustextures of prismatic plagioclase and interstitial amphiboleand more abundant unoriented prisms or acicular grainsof fine- to medium-grained amphibole Massive sheaf-liketextures of acicular amphibole are interpreted as primaryigneous textures A few plagioclase phenocrysts (3ndash5 mm)are preserved The amphibole is colourless to pale-greenpleochroic actinolite (or actinolitendashtremolite) plagioclaseis albite and commonly pseudomorphed by clinozoisitendashepidote or sericitized in zones of alteration Minorconstituents include chlorite quartz and sphenendashleucoxene with local zones of massive epidote(ndashcarbonate)
A schistose metabasite 5 to 8 km northeast of the PeakHill opencut contains actinolite arfvedsonite calcitediopside epidote and quartz The alignment of actinoliteand arfvedsonite defines the S2 schistosity and thereforeboth these minerals were formed during prendashsyn-D2 (seeStructure) The presence of the arfvedsonite (sodicamphibole) suggests either an original sodium-rich rockor later sodic metasomatism during or prior to D2
Metabasaltic hyaloclastite
Metabasaltic hyaloclastites form a prominent outcrop areapartly covered by ferricrete and colluvium south of theMurchison River These rocks are separated from themafic and ultramafic schist by the Murchison Fault(Plate 1) and probably represent a substantial thicknessof mafic lavas and hypabyssal material Hynes and Gee(1986) and Gee (1987) estimated a total thickness rangingfrom 4 to 6 km On the northern part of the GLENGARRY
1100 000 sheet the metabasalts are intercalated withsedimentary rocks of the Karalundi Formation (Pirajnoet al 1998a) These metabasaltic rocks are interpreted ashyaloclastites mdash a term that denotes fragmentation dueto quenching (Fig 9) of lavas flowing in water or eruptingunder an ice sheet This results in non-explosive fracturingand disintegration of the quenched lavas (McPhie et al1993 Fischer and Schmincke 1984)
The metabasaltic hyaloclastites are undeformeddominantly of mafic composition and have a spiliticcharacter Spilites are basaltic rocks that become alteredthrough metasomatic exchange with seawater therebyincreasing their sodium content The hyaloclastites havenormative albite from 13 to 23 wt and Na2O contentsof up to 6 wt
The metabasaltic hyaloclastites are commonly aphyricand composed mainly of acicular crystals of actinolitearranged in sheaves together with epidote minorcarbonate prehnite quartz and titanite in a fine-grainedgroundmass of albite microlites chlorite and epidoteCoarse-grained equivalents (clinopyroxene and plagioclaselaths) display ophitic to subophitic textures North of theMikhaburra (Holdens Find) gold deposit a small shaft has
Figure 9 Basaltic hyaloclastite of the Narracoota Formationshowing cuneiform devitrified shards now replacedby silica and sericite plane polarized light
exposed a vesicular rock containing serpentinized olivinecrystals set in a very fine grained altered matrix ofactinolite probably replacing pyroxenes
These metabasalts are commonly unfoliated andmassive with a characteristic brecciated or jigsaw-fittexture outlined by epidote carbonate prehnite and quartzveining along cooling joints In places these cooling jointsmay form pseudo-pillow structures and may be mistakenfor pillow lavas (Hynes and Gee 1986) Microscalejigsaw-fit textures are also seen
Felsic schist
Felsic schists which host sulfide mineralization (seeMineralization) at the Horseshoe Lights copperndashgolddeposit are present in the northern part of the BryahBasin Stratigraphically the felsic schist are at the top ofmafic metavolcanic rocks of the Narracoota Formation andoverlain by rocks of the Ravelstone Formation (seebelow) which contain chert lenses and layers close to thiscontact The felsic rocks are offset by a northeasterlytrending fault near the mine area and extend for about75 km in a southeasterly direction where they are offsetagain by a northeasterly trending fault However they donot reappear on the other side of the fault where the maficmetavolcanic rocks are in contact with the clasticsedimentary rocks of the Ravelstone Formation
Felsic schist includes quartzndashsericite schist sericiteschist and chlorite schist all showing varying degrees ofdeformation and development of mylonite Examinationof drillcore from the Horseshoe Lights mine revealedstructures reminiscent of felsic volcaniclastic rocks suchas collapsed pumice fragments Quartzndashsericite andsericite schist are composed of quartz and feldsparporphyroclasts partially replaced by quartz and sericitecarbonate or chlorite and wrapped around by granoblasticaggregates of quartz and sericite these aggregates aretraversed by anastomosing bands of sericite Tourmalineis present in places In one example sericite schistcontains elliptical opaque fragments suggestive ofcollapsed pumice Chlorite schist is composed of chlorite
10
Pirajno et al
and granular quartz with the chlorite forming distinctmonomineralic laminae X-ray diffraction analyses ofaltered schist indicate the presence of quartz kaolinpyrite hematite goethite and dioctahedral sodianmuscovite or potassian paragonite
Based on petrographic and core examinations thefelsic schist precursor rocks may have been quartzndashfeldspar porphyry and felsic volcaniclastic rocks
Volcaniclastic rocks
Mafic volcaniclastic rocks have well-preserved eutaxiticor fragmental textures despite intensive foliation (Fig 10)In the Fortnum mine area mafic fragmental rocks andfine-grained mafic volcaniclastic rocks are spatiallyassociated with jasperoidal chert pods The fragmentalrocks are strongly schistose with flattened and stretched
fragments of chlorite schist quartzndashchlorite schist withplagioclase phenocrysts quartzndashfeldsparndashamphibole rock(metabasalt) medium-grained plagioclase grains andmore rarely quartz crystals in a fine-grained matrix Finelylayered mafic schists consist of an amphibolendashplagioclasematrix with scattered prismatic to ovoid plagioclasephenocrysts and quartz lsquoeyesrsquo Amphibole accessorybiotite and sericite lenses have a strong preferredorientation suggesting that recrystallization in these fine-grained rocks has destroyed any volcaniclastic texture
Volcanic breccia is present in at least three localitiesThe most important of these is 5 km north of the oldCashman mine in the southern part of BRYAH (seeMineralization) Outcrops of volcanic breccia are alsopresent at the Cashman mine and 3 km west of the PeakHill ndash Fortnum road junction The nature of these angularclast-supported poorly sorted blocks of mafic volcanicmaterial suggest that they are vent breccias Volcanicbreccia was intersected throughout 455 m of core indrillhole BD1 (BRYAH AMG 380380) drilled by NorthExploration Ltd in 1993 (McDonald 1994) This coreintersection is briefly described below
Drillhole BD1 was drilled to a depth of 520 m at aninclination of 70deg towards the south and intersected claysand gravels to a depth of 65 m followed by weatheredmafic volcanic breccias to 96 m Below this depth to theend of the hole at 520 m spectacular fresh proximal vent-facies material consisting of angular blocks and clasts ofbasaltic lava tuff and chert were intersected (Fig 11)Crude bedding is present locally as are thin layers oflaminated or cross-laminated cherty material The holebottomed in cross-laminated chert which is interpreted aspyroclastic surge and tuff deposits The basaltic rocksinclude fine-grained vesicular basalt and feldspar-phyricand augite-phyric basalts The porphyritic varieties arecharacterized by a microlite-rich feldspar matrixclinopyroxene granules interstitial glass and chlorite andopaque minerals (titanite or rutile) The feldspar
Figure 10 Mafic volcaniclastic rock of the NarracootaFormation showing relict glass shard (in centre)plane polarized light
Figure 11 Volcanic breccia of the Narracoota Formation intersected in diamond drillhole BD1 Clasts arepredominantly of basaltic rocks the matrix exhibits albitic alteration Width of the core trays is 040 m
11
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
phenocrysts are selectively altered to sericite whereas theaugite phenocrysts are fresh and exhibit distinct zoningVesicles are infilled (from rim to core) by albite epidotechlorite and calcite Minor sulfide specks mainlychalcopyrite may be present in the vesicular basalt Tuffscharacterized by fluidization (due to degassing) andeutaxitic textures consist of glass shards and crystal andlithic fragments set in a devitrified and variably alteredglassy matrix Alteration phases are mainly chloritecalcite quartz and albite Chalcopyrite blebs are presentin places Hydraulic fracturing and veins of calciteprehnite quartz and chlorite are abundant One sectionbetween 200 and 360 m is characterized by albiticalteration (sodium metasomatism) which imparts a pinkto reddish colouration to veinlets and patches where thealbite is present
The fragmental mafic volcanic rocks in drillhole BD1are interpreted to represent a proximal vent-facies volcanicbreccia This vent-facies material coincides withprominent magnetic and Bouguer gravity anomalies(Pirajno et al 1995a) The magnetic anomaly which isrelated to the presence of magnetite in pyroxene basalthas a well-defined northeasterly trending elliptical shapeand could conceivably indicate the remnants of a majorvolcanic edifice Magnetic modelling suggests thepresence of two tabular bodies dipping 25deg to the north(Bui Dung 1999 pers comm) The gravity anomaly isat the centre of a large regional gravity high whichunderlies most of the area occupied by the NarracootaFormation (Pirajno and Occhipinti 1998)
Carbonated and silicified metavolcanic rocks
Carbonated and silicified maficndashultramafic rocksinterpreted as part of the Narracoota Formation outcropin the Horseshoe anticlinal block (Plate 1) These rocksare compositionally heterogeneous and both underlie andare intercalated with rocks of the Horseshoe FormationThis suggests that the interleaving is tectonic becauseelsewhere in the Bryah Group the Horseshoe Formationis not observed to be in direct contact with the NarracootaFormation (Occhipinti et al 1999)
Jasperoidal chert
Jasperoidal chert pods are present locally within theNarracoota Formation (Gee 1987 Hill and Cranney1990 Pirajno and Occhipinti 1998) but are commonlytoo small to be represented individually on geologicalmaps One of the largest pods outcrops 15 km due southof Ruby Duffer Well in the southern part of BRYAH Windh(1992) investigated the chert pods in some detailgeochemically discriminated them on the basis of theirNiCr ratios and distinguished jasperoidal syngeneticexhalative chert silicified volcanic or sedimentary rockssilicified shear zone rocks and surface silicificationSeveral of these chert pods such as those in theNarracoota Formation south of the Peak Hill Schist innorthern BRYAH are quartz mylonites mdash probably Windhrsquos(1992) silicified shear zone rocks A few may be chemicalprecipitates deposited by hot springs whereas others mayrepresent silicified fault zones
The cherty material is reddish to grey colouredmassive to banded and extensively veined by quartzThe chert consists of very fine grained recrystallizedquartz with equant to elongate polygonalndashgranoblastictextures locally with a crystallographic preferredorientation Minute opaque minerals locally includingmagnetite or pyrite define trails parallel to the quartzfoliation In the Yarlarweelor opencut (Fortnum mine)pebbles of these cherts in overlying mafic fragmentalrocks suggest that the cherts formed as exhalative horizonsrelated to volcanism Alternatively the jasperoids mayrepresent iron-rich silicification along major shear zonesIn the Yarlarweelor opencut the chert pods host epigeneticgold mineralization in and around quartz(ndashpyrite) veinsystems (Hill and Cranney 1990)
Geochemistry of the Narracoota Formation
Major trace and rare earth element (REE) whole-rockanalyses of samples of metabasite rocks of the NarracootaFormation collected during this study are included in thedigital dataset in the back pocket These data were usedto characterize the geochemistry of the volcanic rocks ofthe Narracoota Formation in an attempt to better definethe rock types and gain an insight into the nature of theparent magma(s) and tectonic setting Representativeanalyses of Narracoota Formation rocks are presented inTable 2
The Narracoota metabasite rocks are commonly oftholeiitic composition with mixed mid-ocean ridge basalt(MORB) ndash oceanic island and continental geochemicalsignatures They span the range from high-Mg basalt tokomatiite and peridotitic komatiite or peridotite (possiblysubvolcanic cumulates) Common characteristics includehigh MgO high Ni and Cr moderate to low REEabundances and nearly flat chondrite-normalized REEpatterns with weak Eu anomalies possibly reflectingdepleted asthenospheric mantle sources (Pirajno and Davy1996 Pirajno et al 1996 Pirajno and Occhipinti 1998Occhipinti et al 1998ac) There are subtle chemicaldifferences between the hyaloclastites and maficndashultramafic schists (Tables 3 and 4 see below)
Hynes and Gee (1986) and Pirajno and Davy (1996)reported on the petrochemistry and tectonic setting ofthe Narracoota Formation metabasite rocks Hynesand Gee (1986) concluded that they have fairlyuniform chemistry and are of MORB affinity although theoriginal mafic volcanic rocks may have been emplacedthrough the rifting of continental crust Pirajno and Davy(1996) proposed that the Narracoota Formation meta-volcanic rocks might have formed in a setting analogousto that of the present-day Gulf of California (Lonsdaleand Becker 1985) The origin of the NarracootaFormation metabasites is discussed in Tectonic model andconclusions
Classification based on chemistry
The total alkali ndash silica (TAS) and high-Mg plot(Le Maitre 1989) indicates that the bulk of the rocks ofthe Narracoota Formation range in composition fromkomatiitendashpicrite through basalt to basaltic andesite
12
Pirajno et al
Table 2 Representative chemical analyses of the Narracoota Formation
Rock _________________ Mafic schist _________________ _______ Hyaloclastite _______ _______ Ultramafic _______ ____ Trillbar __type schist ComplexSample 132788 132789 132790 133033 133050 112643 116485 104256 132791 139138 139139 135482 143538
Percent
SiO2 5424 4945 5277 463 4907 5187 5139 5011 4923 4723 4789 5137 4961TiO2 028 113 031 019 026 073 063 053 019 016 017 037 141Al2O3 1422 1172 1466 948 794 138 1512 1503 1043 765 867 1481 1391Fe2O3 248 345 184 661 635 224 296 278 146 396 201 232 561FeO 598 824 705 741 101 848 662 529 834 548 708 561 717MnO 017 019 018 025 198 02 016 014 018 012 015 016 022MgO 929 1243 1036 1517 778 1036 83 936 2063 2877 2678 869 656CaO 1106 1107 962 1451 2262 974 1144 1514 86 641 704 1068 1136Na2O 218 212 274 003 009 216 32 145 092 018 019 306 204K2O 007 008 046 001 284 036 01 011 002 003 001 006 022P2O5 003 013 002 003 007 007 006 005 001 001 001 003 011Total 10000 10001 10001 9999 10001 10001 9998 9999 10001 10000 10000 9716 9822
Mg 6687 6615 6795 6692 6736 6377 6142 6816 792 85 843 ndash ndash
Parts per million
Ag ndash ndash ndash ndash ndash 1 ndash 1 ndash ndash ndash ndash ndashAs 155 157 052 22551 13032 ndash ndash ndash ndash 832 ndash ndash ndashAu ndash ndash ndash ndash ndash 104 ndash ndash ndash ndash ndash ndash ndash
Ba 55 140 79 27 2 846 341 127 92 74 37 102 39 322Cd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash
Co 55 86 58 223 51 ndash ndash ndash 99 113 111 ndash ndash
Cr 509 1 201 686 2 574 72 489 364 283 1 836 2 530 3 146 593 82Cu 168 124 63 327 20 108 101 39 55 9 11 59 172Ga 10 16 10 8 9 12 12 13 8 6 6 12 19Hf ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 07 14Mo ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash 08 26Nb ndash 63 ndash ndash 52 ndash ndash ndash ndash ndash ndash 1 9Ni 203 548 241 1 274 91 258 143 164 866 1 531 1 230 124 98Pb ndash 2 ndash ndash 7 ndash ndash ndash ndash ndash ndash 1 4Pd ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashPt ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashRb 1 ndash 6 ndash 85 6 ndash 2 ndash 1 ndash 1 4Sb ndash ndash ndash ndash ndash 415 ndash 511 ndash ndash ndash ndash ndashSc 50 41 51 31 10 ndash ndash ndash 40 34 38 51 48Sr 64 149 64 54 100 163 82 188 23 23 7 61 279Ta ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashTh ndash 104 ndash ndash 717 ndash ndash ndash ndash ndash ndash ndash ndashU ndash ndash ndash 064 13 ndash ndash ndash ndash ndash ndash 08 14V 196 277 202 138 78 250 249 217 144 115 143 235 362W ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndash ndashY 13 18 12 8 16 17 14 11 8 6 7 17 24Zn 65 94 68 45 50 85 73 55 62 51 45 61 91Zr 13 68 15 17 50 51 47 38 7 7 8 20 86
La 089 936 043 054 1819 36 35 35 093 017 056 2 6Ce 218 2264 129 084 4445 9 83 83 153 042 082 2 15Pr 037 29 02 02 418 12 11 13 02 009 019 0 2Nd 166 1193 108 102 1511 57 51 57 102 047 079 5 12Sm 08 328 065 056 306 15 14 15 065 03 034 ndash ndashEu 042 13 032 028 223 09 07 08 029 011 011 ndash ndashGd 166 409 141 085 305 23 17 2 129 065 071 ndash ndashTb 04 069 031 018 04 04 04 04 029 014 016 ndash ndashDy 268 408 233 12 202 27 24 24 214 108 116 ndash ndashHo 071 087 057 028 037 05 05 05 053 027 03 ndash ndashEr 222 231 173 094 115 18 15 16 162 083 091 ndash ndashTm 039 033 027 016 017 02 02 02 027 014 015 ndash ndashYb 229 196 182 115 125 15 14 15 166 086 09 ndash ndashLu ndash ndash ndash 019 02 02 02 02 ndash 013 014 ndash ndash
13
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(Fig 12) A small number of samples plot in the boniniteand andesite fields All metabasites of the NarracootaFormation (ultramafic and mafic schists and basaltichyaloclastite) are of subalkaline tholeiitic affinity (Fig 13)They commonly have restricted silica contents rangingfrom 45 to 55 wt (Fig 12)
The metabasites are all quartz albite anorthitediopside hypersthene and magnetite normative Themafic schists are hypersthene normative with lowerMgO contents (lt15 wt) and magnesium numbers (Mgmdash defined as MgO(FeO + MgO)) ranging from 43 to 74(Table 3) Some mafic schists have no quartz and areolivine normative (5ndash6 and up to 20 in some maficschists) The ultramafic schist is hypersthene and olivinenormative with MgO contents ranging from 153 to227 wt and Mg ranging from 75 to 86 (Table 3) Themetabasaltic hyaloclastites are albite and clinopyroxenenormative and have MgO contents of lt10 wt and Mgof between 47 to 68 (Table 3)
Ultramafic schist mafic schist and metabasaltichyaloclastite can be distinguished in terms of their Cr Niand Ti abundances FeOMgO ratios (Tables 3 and 4Figs 14a and 14b) and chondrite-normalized REEpatterns The hyaloclastite rocks are depleted in Cr andNi and enriched in TiO2 relative to the maficndashultramaficrocks (Fig 14c)
The Jensen (1976) cationic plot is based on theproportion of Fe2++Fe3++Ti versus Al and Mg cationsrecalculated to 100 and is particularly useful fordiscriminating subalkaline and Mg-rich metamorphosedvolcanic rocks in which the alkali content may havebeen modified during deformation and metamorphism(Rollinson 1993) In the Jensen plot (Fig 15a) the
Narracoota Formation rocks span the range of compo-sitions from high-Mg tholeiite through to komatiite andperidotitic komatiite in a trend of increasing MgO
Chondrite-normalized rare-earth element diagramscommonly regarded as the most useful of the traceelement plots in the petrogenesis of igneous rocks areused to determine the possible nature and source of themelts Particularly important are the overall patterns fromlight to heavy rare earth elements (LREE to HREE) thenormalized abundance of Eu controlled by feldspar andthat of Ce controlled by seawater or hydrothermal fluidsFor the Narracoota Formation rocks chondrite-normalizedREE abundances (Figs 15b and 15c) are commonly low(lt1 to lt40 times chondrite) The mafic schist ischaracterized by a spread in LREE from depleted toenriched (Fig 15b) with individual patterns almostidentical to those of mid-ocean ridges (OrsquoNions et al1976 Schilling 1982) and the recent basaltic lavas ofIceland (Schilling et al 1982) More specifically theLREE-depleted patterns (western Bryah Basin) arestrikingly similar to those of the Lau Basin spreadingcentre in Fiji (Pearce et al 1995) whereas slightlydepleted to slightly enriched LREE patterns (eastern Bryah
Table 3 Magnesium numbers for the Narracoota and Killara Formations
Rock Formation Range of Mg Average Mg Standard deviationof Mg
Metabasaltic hyaloclastite Narracoota 4677 ndash 6816 5716 525Mafic schist Narracoota 4337 ndash 7409 5957 669Ultramafic schist Narracoota 7516 ndash 8560 8105 254Tholeiitic basalt Killara 3504 ndash 6603 5035 739
NOTE Mg Magnesium number defined as MgO(FeO +MgO)
Table 4 Selected geochemical parameters for the NarracootaFormation
Parameters Hyaloclastite Mafic schist Ultramafic(mean values) schist
(LaYb)N 144 1702 037TiO2 (wt) 086 068 019NiCr 043 039 042Al2O3TiO2 162 205 4668MgO (wt) 731 780 2119
35 45 55 650
1
2
3
4
foidite andesite
basalt
boninite
basalticandesite
MgOgt18 picrite
basanite
tephrite
MgOgt18 amp TiO lt1 komatiite
picrobasalt
FMP365 021199
22
2
2
2
2
MgOgt18 amp TiO gt1 meimechiteMgOgt8 amp TiO lt05
SiO (wt)
Na
O +
K O
(w
t)
Figure 12 Total alkali versus silica diagram (Le Maitre1989) for rocks of the Narracoota FormationNote that a small number of samples fall withinthe boninite field this however may be due tohydrothermal alteration
14
Pirajno et al
Basin) are comparable to those of seamounts reflectinga more enriched source The nearly flat patterns havenegative Eu anomalies reflecting the primitive nature ofthe rocks presence of olivine clinopyroxene andorthopyroxene and fractionation of feldspar from themelt The patterns of the Iceland basalts that are nearlyidentical to those of the mafic schist of the Bryah Groupwere explained by Schilling et al (1982) as due toadvection of asthenospheric mantle at a mid-ocean ridgeConsidering field relations and petrological andgeochemical data it is conceivable that the NarracootaFormation metatholeiites may have had a similar originChondrite-normalized REE abundances for the meta-basaltic hyaloclastite are very low (9 to 14 timeschondrite) slightly LREE-enriched and with a distinctpositive Eu anomaly (Fig 15c) reflecting the addition ofalbite due to seawater metasomatism
The overall REE abundances and patterns of maficschist and hyaloclastite are strikingly similar to192 ndash 184 Ga mafic rocks of the Flin Flon belt in theTrans-Hudson Orogen in Canada (Lucas et al 1996)Some of the mafic rocks of the Flin Flon belt have beeninterpreted to belong to tectono-stratigraphic assemblagesof ocean floor and ocean island affinity Also the Flin Flonocean island tholeiites have REE patterns similar to
Figure 13 Total alkali versus silica diagram (Le Maitre 1989)defining limits of alkaline and subalkaline basaltsshowing the predominantly subalkaline nature ofthe Narracoota Formation
20
16
12
8
4
0
Na
O +
KO
(w
t)
22
857565554535
SiO (wt)2 11999FMP367
Hyaloclastite
Mafic schist
Ultramafic schist
Subalkaline
Alkaline
Figure 14 Geochemical characteristics of the NarracootaFormation a) TiO2 versus FeOMgO ratios notethe slight TiO2 enrichment of metabasaltichyaloclastite compared to maficndashultramafic schistb) Cr versus FeOMgO ratios note the Cr enrichmentof maficndashultramafic schist compared to meta-basaltic hyaloclastite c) TiO2ndashNindashCr triangular plotshowing Ni and Cr enrichment of maficndashultramaficschist compared to metabasaltic hyaloclastite
3
2
1
0
TiO
(wt
)2
1 2FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
4000
3000
2000
1000
0
Cr
(ppm
)
1 2 3FeO MgO (wt)
Hyaloclastite
Mafic schist
Ultramafic schist
TiO 1002
Ni Cr91199FMP368a
Hyaloclastite
Mafic schist
Ultramafic schist
a)
b)
c)
15
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Hawaiian tholeiites (Stern et al 1995) The inference fromthese comparisons is that submarine volcanoes may havebeen a component of the Narracoota Formation
Tectonic discriminant diagrams do not provide reliableinformation on the palaeotectonic environment withinwhich igneous rocks were emplaced (Duncan 1987 Wangand Glover 1992) Nevertheless if there is petrologicalevidence that the rocks have not undergone extensivecrystal fractionation and the overall geological context is
taken into account selected discriminant diagrams can beused to estimate palaeotectonic settings With the aboveconsiderations in mind and remembering that the rocksin question have a subalkaline chemistry the FeO(tot)ndashMgOndashAl2O3 plot of Pearce et al (1977) is deemedappropriate (Fig 15d) The FeO(tot)ndashMgOndashAl2O3 plot hasbeen used successfully in geologically well constrainedareas (Breitkopf and Maiden 1988) The FeO(tot)ndashMgOndashAl2O3 plot suggests that the Narracoota Formationvolcanic rocks were formed in tectonic environments of
a)
c)
b)
d)
MgO
TA
TDTR
CR CDCA
HFTBK
PKCB
HMT
Sam
ple
chon
drite
100
10
2La Pr Eu Tb Ho Tm Lu
Ce Nd Sm Gd Dy Er Yb
La Pr Eu Tb Ho Tm LuCe Nd Sm Gd Dy Er Yb
Sam
ple
chon
drite
100
10
1
6
FeO
MgO
221199
Al O32
FeO + TiO2
Al O32
FMP154
Mafic and ultramafic schist
Metsabasltic hyaloclastite(tot)
Figure 15 Geochemical discriminant plots for Narracoota Formation rocks a) Jensen (1976) cationic plot showingrange of compositions from high-Mg tholeiite (HMT) through high-Fe tholeiite (HFT) basaltic komatiite(BK) peridotitic komatiite (PK) tholeiitic andesite (TA) tholeiitic dacite (TD) calc-alkaline basalt (CB)and calc-alkaline andesite (CA) b) Chondrite-normalized rare-earth element plot of mafic (HREE-enriched) and ultramafic (HREE-depleted) schist (normalizing factors after Sun 1982) c) Chondrite-normalized rare-earth element plot of metabasaltic hyaloclastite (normalizing factors after Sun 1982) d)Triangular discriminant plot (Pearce et al 1977) showing the tectonic environment of the NarracootaFormation Tectonic fields are as follows 1) spreading-centre island 2) orogenic 3) ocean ridge andfloor 4) ocean island and 5) continental
16
Pirajno et al
MORB ndash oceanic island to continental affinity (Fig 15d)This diagram however has limitations if the rocks havebeen subjected to ocean-floor metamorphism A moreuseful plot is the TiO2ndashFeO(tot)ndashMgO plot which was usedby Breitkopf and Maiden (1988) in their study of theNeoproterozoic Matchless Amphibolite Belt of theDamara Orogen in Namibia The TiO2ndash FeO(tot)ndashMgO plotsupports the gradation from MORB towards continentalflood basalt because the hyaloclastite rocks plot closer tothe continental field than do the mafic schist (Fig 16) Thisfeature together with other considerations such as Mgand geological and petrological constraints indicate thatthe hyaloclastite was erupted on a continental rift marginThis has important implications for the tectonic evolutionof the BryahndashPadbury Basin as explained in Tectonicmodel and conclusions
Ravelstone Formation
The Ravelstone Formation is poorly exposed in scatteredlow outcrops over a wide area in the northern and centralparts of the Bryah Basin Rocks of the RavelstoneFormation were previously considered by MacLeod(1970) and Gee (1979 1987) to belong to the lsquoThadunaGreywackersquo (now Thaduna Formation of the YerridaGroup) for which the type area is about 100 km to theeast-northeast on THADUNA (Pirajno and Adamides 1998)
The Ravelstone Formation comprises a succession oflithic and quartz wacke shale and siltstone that was
deposited from turbidity currents In the north theRavelstone Formation contains lenses of chert andis unconformably overlain by the MesoproterozoicBangemall Group West of the Peak Hill opencut thelower contact with the Narracoota Formation is dis-conformable whereas the upper contact with theHorseshoe Formation appears to be conformable In thecentral and northern parts of BRYAH the RavelstoneFormation although metamorphosed has no tectonitefabric On MILGUN (around Fortnum) however a well-developed foliation is present
Drillcore from the Harmony gold deposit shows thatthe contact between the base of the Ravelstone Formationand the top of the Narracoota Formation is interfingeredpossibly due to shearing The disconformable contactbetween the base of the Ravelstone Formation and the topof the Narracoota Formation is exposed in a river bedabout 1 km due east of the Fortnum ndash Peak Hill turn-offIn this area graded layers of immature subarkosicsandstone to siltstone contain fresh plagioclaseK-feldspar sericitized lithic fragments and angular quartzgrains in a matrix composed of sericite and biotite Inaddition the siltstone contains euhedral crystals oftourmaline Metamorphic brown biotite and muscovite areabundant and replace feldspars quartz and lithicfragments Lithic fragments include massive chlorite(ndashrutile) derived from mafic precursors chert hematitendashquartz shale as well as partly sericitized feldspar grainsQuartz grains include rounded to irregular shapes andbiotite is metamorphic in origin Quartz white micachlorite and variable amounts of carbonate are part of thefine-grained matrix Well-developed foliation wherepresent is defined by aligned sericite elongate quartzand to a lesser extent feldspar grains and by mica seamsNew muscovite flakes have grown along and across thefoliation
In the Fortnum mine area on MILGUN graded beddedlithic wacke and siltstone overlie the volcanic rocks of theNarracoota Formation The wacke contains medium tocoarse-grained crystals of feldspar (plagioclase minor K-feldspar) and quartz as well as fragments (fine metabasaltand chlorite) derived from mafic volcanic rocks Thefeldspar crystals which are strongly sericitized dominateover quartz The matrix consists of sericitendashchloritendashquartz with or without carbonate The reworked rocksinclude fragmental layers with fine metabasalt debris andgraded chloritic siltstone containing plagioclase laths Thederivation of the mafic component is easily explained butthe well-preserved feldspar crystals suggest nearbygranitic or felsic volcanic precursors
Horseshoe Formation
The Horseshoe Formation occupies areas west of thePeak Hill opencut and the northern parts of BRYAH
and MILGUN This formation includes finely laminatedferruginous (hematitic) shale and siltstone fine-grainedquartzndashfeldspar wacke with interleaved iron formation andchert graded quartz wacke manganiferous shalegarnetiferous biotitendashchlorite schist and garnetiferousiron-formation Relatively high manganese contents areinferred from the abundant manganese oxide staining in
CFB
MORB
20
18
15
13
10
08
05
03
000 1 2
TiO
2
FMP168 211099Ultramafic schist
Mafic schist
Hyaloclastite rocks
(tot)FeO MgO
Figure 16 TiO2 versus FeOMgO plot (Breitkopf and Maiden1988) for the Narracoota Formation showing themid-ocean ridge basalt (MORB) affinity of the maficand ultramafic schist and the transitional chemistryof the hyaloclastites towards continental floodbasalts (CFB)
17
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
weathered and lateritic rocks and lateritic manganese orehas been mined at the Horseshoe and Mount Padburymines The type area of the Horseshoe Formation is theHorseshoe Range (Occhipinti et al 1997) where athickness of approximately 1000 m was estimated by Gee(1979) The Horseshoe Formation overlies the NarracootaFormation however the contact is either conformable ortectonic Elsewhere on JAMINDI north of BRYAH theHorseshoe Formation overlies the Ravelstone Formationand the contact is gradational and conformable TheHorseshoe Formation underlies the Labouchere Formationof the Padbury Group The nature of this upper contactappears conformable however Martin (1994) suggestedthat there is a regional unconformity between these units
Structurally the Horseshoe Formation forms a broadsyncline with its axis trending approximately easterly Thesouthern limb of this syncline is in sheared contact withrocks of the Narracoota Formation In this area theHorseshoe Formation is complexly folded with axestrending 070deg parallel to the shear zone
In the Horseshoe Range Gee (1987) recognized threeunits 1) a lowermost part consisting of regularly beddedwacke and shale similar to the underlying Ravelstonesuccession but finer grained more calcareous andcontaining less chlorite and more feldspar and quartzindicative of a granitic rather than mafic volcanicprovenance 2) a middle iron-formation member withseveral BIF (chertndashmagnetitendashstilpnomelane white chert)horizons intercalated with chloritic shale and 3) anupper unit of calcareous manganiferous shale andwacke The lowermost unit is exposed on MILGUN in thelow hills east of Fortnum airstrip where fine-grainedcarbonate-cemented wacke and shale contain dis-harmonic-folded white-chert lenses (2ndash12 cm thick) andless common discontinuous quartzndashmagnetite layers(2ndash3 cm) The quartz wacke component of the HorseshoeFormation contains quartz plagioclase microclinebiotite and muscovite all as detrital minerals Nearthe Peak Hill opencut the iron formation is made upof biotite amphibole chlorite quartz magnetite andgarnet This unusually high grade assemblage may berelated to the metamorphism of the Peak Hill Schist (seeMetamorphism)
About 1 km north of the Ravelstone manganesedeposits a reasonably good exposure of the HorseshoeFormation was examined in detail A stratigraphic columnfor this locality is shown in Figure 17 This is a foldedupward-coarsening package approximately 350 m thickwhich from base to top consists of quartzndashlithic wackewith banded chert interbeds displaying a well-developedaxial planar cleavage quartz wacke with iron formationand shale interbeds massive beds of coarse-grainedquartzndashlithic wacke intercalated with thin granular iron-formation amphibole- and garnet-bearing granular iron-formation layers and massive quartzndashlithic wackeintercalated with thin iron-formation bands The quartzndashlithic wacke contains chert clasts detrital subangularquartz fresh plagioclase crystals and biotite in a matrixof sericite green chlorite and iron oxide grains Bandedcherty material is composed of granular quartz aggregatesbrown biotite actinolite and very fine carbonate-richlaminae (this rock is best classified as a quartzndashbiotitendash
actinolite schist) The granular iron-formation consists ofgranular aggregates of quartz and iron oxides withinterstitial biotite and chlorite Syntectonic garnetporphyroblasts are replaced in part by quartz andcarbonate Massive lithic wacke consists of a packedaggregate of angular quartz feldspar and chert grains thematrix is volumetrically small and made up of biotitequartz and sericite Garnetiferous iron-formation has darklaminae of quartz granules with interstitial actinolitendashchlorite iron oxides and light-coloured microbands (1 cmthick) of quartz with actinolitendashchlorite iron oxides anddisseminated synndashlate-tectonic garnet porphyroblastsGarnet is also present as porphyroblasts growing acrossmicroband boundaries
Padbury GroupThe Padbury Group locally unconformably overliesthe Horseshoe Formation of the Bryah Group but inplaces is in faulted contact with the Bryah Group andYarlarweelor gneiss complex (Narryer Terrane Yilgarn
FMP156 020300
0
100
200
300
intercalated with thin BIF and shale interbeds
Garnetiferous BIF
Massive beds of coarse-grained lithic wackewith interbeds of garnetiferous BIF and
Banded iron-formation interbedded with massive
Banded chertQuartzndashlithic wacke with carbonate cement
wacke and soft granular iron-formation
(m)
granular iron-formation
Massive quartzndashlithic wacke layers
Micaceous wacke
Figure 17 Schematic stratigraphy of the HorseshoeFormation from an area of outcrops about 12 kmwest-northwest of the Peak Hill mine (after Pirajnoand Occhipinti 1998 width of column reflectsrelative resistance to weathering)
18
Pirajno et al
Craton Fig 2) Considerable onlap of the Padburysuccession onto the various formations of the Bryah Groupcan be inferred these contacts were faulted possibly inseveral stages during basin closure The age of thePadbury Group is poorly constrained Nelson (1997)reported a maximum age of c 20 Ga from the upper partof the Wilthorpe Formation and Windh (1992) inferred aminimum age of c 18 Ga from a leucogranite dyke
Martin (1994 1998) proposed a formal stratigraphy forthe lower Padbury Group based on detailed sediment-ological studies in the area covering the southeastern andcentral parts of MILGUN This formal stratigraphy replacedprevious stratigraphic divisions (Barnett 1975 Gee1979 1987 Windh 1992) and has since beenexpanded to include two distinct lithostratigraphic unitsas members within the Wilthorpe Formation the Heinesand Beatty Park Members (Occhipinti et al 1997) Martin(1994 1998) interpreted the Labouchere and WilthorpeFormations as an upward-coarsening deep-water turbiditecomplex overlain by shales and iron formation of theRobinson Range Formation The turbidites were derivedby erosion from the granitendashgneiss basement (YilgarnCraton) and by reworking of underlying sedimentary andmafic volcanic rocks in the Bryah Basin
The Padbury Group contains quartz wacke siltstoneconglomerate iron formations hematitic shale and minorclastic rocks and dolomite (Martin 1994 Occhipintiet al 1997) and is subdivided into four formationsLabouchere Wilthorpe Robinson Range and MillidieCreek Formations Martin (1994) interpreted the PadburyGroup to have been deposited in a retroarc foreland basinthat developed on top of the Bryah Group
Labouchere Formation
The Labouchere Formation occupies areas in thenorthwestern part of the Bryah Basin where it isfaulted against the Yarlarweelor gneiss complex Martin(1994 1998) suggested that the Labouchere Formationunconformably overlies the Horseshoe Formation(Bryah Group) based on the regional geometry inthe Fortnum mine ndash Dandy Well area on MILGUN Theregional unconformity is inferred from the low-angletruncation of an iron-formation marker unit in theHorseshoe Formation against lowermost quartz areniteof the Labouchere Formation in the area south ofYarlarweelor Creek North of the Fortnum Fault ironformation within the Horseshoe Formation is nearlyparallel to bedding in the Labouchere FormationElsewhere in the region contacts between variousformations of the Bryah and Padbury Groupsare interpreted as unconformities (Windh 1992) oralternatively as faults or shear zones (Pirajno andOcchipinti 1998 Occhipinti et al 1998b) On BRYAH theLaboucherendashHorseshoe Formation contact is marked bya conglomeratic unit The Labouchere Formation isconformably overlain by and grades into the WilthorpeFormation (Martin 1994) although this contact waspreviously described as an unconformity (Gee 1979) Gee(1979) estimated the Labouchere Formation (including theWilthorpe Formation) to be 5000 m thick extending from
Mount Labouchere on MILGUN (type area Martin 1994)to the Horseshoe Range the southern continuation ofwhich is in northwestern BRYAH Martinrsquos (1994 1998)type section is a composite stratigraphy (up to 7000 mthick) based on four separate sections in southeasternMILGUN
The Labouchere Formation consists of quartz arenitemedium- to coarse-grained sericitic quartz wacke andsericitic siltstone minor conglomerate and banded iron-formation in an upward-coarsening succession Near theHorseshoe manganese mining area the LabouchereFormation consists of a thick succession of upward-finingcycles up to 700 m thick Each cycle consists ofconglomerate or a coarse lithicndashquartzndashsericite wacke unitat the base grading up through coarse- to fine-grainedquartzndashfeldsparndashlithic wacke and sericitic siltstone to iron-rich shale These cycles however become increasinglycoarser upwards so that there is regional upwardcoarsening The base of the topmost cycle begins with aquartz-pebble conglomerate Minor and thin bands of iron-formation are locally present as intercalations within thesedimentary units
Quartz arenite contains grain-supported well-roundedquartz in a sericitic matrix and is extensively silicified Aprominent quartz arenite marker forms the ridge includingMount Labouchere north of Fortnum mine on MILGUN andcan be traced for many tens of kilometres to the southeastwhere gradually more quartz wacke is interbedded withthe arenite A second quartz arenite marker approximatelyhalfway up the Labouchere Formation is present in thearea north of the Fortnum Fault In the same area an ironformation ndash chert layer is present about 250 m above thissecond quartz arenite Martin (1994) emphasized that thedeep-water environment of this iron formation indicatesa similar depositional environment for the clastic rocksQuartz wacke has a matrix-supported framework ofvariably rounded quartz grains minor lithic fragments andfeldspar in a sericitendashchlorite matrix whereas laminatedshale consists of sericitendashchlorite Wacke and siltstoneform numerous upward-fining cycles
Muscovitendashquartz schist or slate developed fromquartz wacke and siltstone in zones of high strain andhigher metamorphic grade adjacent to the Yarlarweelorgneiss complex Strongly foliated quartz wacke andmuscovitendashquartz schist occupy a 4 km-wide zone nearthe Labouchere mine on MILGUN Another belt of schistand slate is present between the Billara Fault and DespairGranite in southwestern MILGUN These strongly foliatedrocks can be traced northwards into recognizable thoughstrongly foliated pebbly quartz wacke The fine-grainedschist consists of elongate polygonalndashgranoblastic quartzwith spaced trails of aligned muscovite flakes Beddingndashcleavage relationships are found in less-deformed areaswhereas in high-strain zones differentiated layeringdeveloped from a pervasive crenulation cleavage
Sericite is abundant throughout most of the rocks ofthe Labouchere Formation The quartzndashsericite wacke iscomposed of subangular quartz grains embedded in asericitized matrix with occasional large muscovite lsquobooksrsquoand scattered small crystals of tourmaline and anatase
19
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Quartzndashfeldsparndashlithic wacke is made up of subangularquartz grains polycrystalline quartz K-feldspar andplagioclase in a matrix of quartz sericite biotite andminor detrital zircons
Wilthorpe Formation
The Wilthorpe Formation (formerly lsquoWilthorpeConglomeratersquo Gee 1987) including the Beatty Park andHeines Members comprises quartz- and chert-pebbleconglomerate quartz wacke sericitic siltstone chloritendashquartz shale quartzndashsericitendashhematite schist dolomiticsandstone and finely laminated chert lenses TheWilthorpe Formation is conformably overlain by theRobinson Range Formation
Martin (1994) measured the type section of theWilthorpe Formation (about 1300 m thick) along theTalbot Divide In this area the characteristic quartz-pebbleconglomerate forms a prominent ridge to the east of hillsunderlain by the Robinson Range Formation In theFortnumndashLabouchere area on MILGUN the exact locationof the LaboucherendashWilthorpe Formation transitionalboundary is less well defined (Swager and Myers 1999)Along the western wall of the Nathans Deep Southopencut (labelled Nathan Deep on Plate 1) severalupward-fining cycles of quartz-pebble conglomerategrading into quartz wacke and quartzndashmuscovite siltstonecan be observed These cycles are underlain by fine-grained chloritic shale interbedded with quartz wackeThis chloritic shale with detrital ilmenite is derived froma mafic precursor probably the Narracoota Formation(Windh 1992) Occhipinti et al (1998a) recognizedcomparable lsquomaficrsquo clastic rocks as a mappable unit(Beatty Park Member mdash see below) at the top of theWilthorpe Formation on PADBURY
The conglomerate contains well-rounded slightlyelongate or faceted vein-quartz clasts and less commonlychert quartzite quartz wacke and rare siltstonendashmudstoneclasts in a quartz wacke matrix Clasts range in size frompebbles to boulders Quartzite pebbles locally containfolded foliation fabrics Bunting et al (1977) suggestedthat large quartzite boulders in the southern part of thetype area were derived from the basal Finlayson Memberof the Juderina Formation (Yerrida Group) Martin (19941998) recognized two polymictic conglomerate intervalsin the type area which included silicified dolomite clastsThese intervals are similar to the polymictic conglomerateand sandstone of the Heines Member defined on BRYAH
(Pirajno and Occhipinti 1998) Siltstone forms a distinctmappable upper unit along the gradational contact withthe Robinson Range Formation
Beatty Park and Heines Members
The Beatty Park Member outcrops in the Mount Padburyarea on PADBURY and contains clastic rocks that werepossibly sourced at least in part from the mafic volcanicrocks of the underlying Narracoota Formation (BryahGroup) with sedimentary chert lenses towards its top Asensitive high-resolution ion microprobe (SHRIMP)UndashPb date obtained from detrital zircons in one of these
chert lenses suggests a maximum age of 1996 plusmn 35 Ma(Nelson 1997) The clastic rocks of the Beatty ParkMember are dominated by metamorphosed chloritendashquartzshale siltstone and wacke several conglomeratic orbreccia lenses and finely laminated chert layers in places(Occhipinti et al 1997) The contact between the BeattyPark Member and the overlying Robinson RangeFormation is gradational with chloritic siltstone and chertlayers and lenses grading into sericitendashquartz siltstone Thelower contact of the Beatty Park Member with theWilthorpe Formation appears to be gradational in the areawest of the Fraser Synclinorium (see Structure) whereferruginized kaolinitic siltstone and quartz wacke gradeinto chloritic siltstone In this area the minimum thicknessof 470 m is implied because the upper part of the BeattyPark Member is not exposed
The shalendashsiltstone layers are well bedded to finelylaminated and consist of quartz and chlorite with minorsericite epidote feldspar titanite and detrital hornblendeThese layers are accompanied by very fine grainedrecrystallized white chert beds in the upper part of theBeatty Park Member West of the Fraser Synclinoriumsedimentary structures such as bedding-parallel lamin-ations flame structures and contorted bedding can beobserved within chloritic siltstone Two types of wackeunits are present one containing quartz dolomite chloritefeldspar sericite epidote sphene and opaque minerals(either magnetite or pyrite) and the other containingquartz feldspar muscovite epidote chlorite carbonateand opaque minerals Lithic fragments in wacke layersinclude metabasalt and mafic schists in which leucoxenepseudomorphs of iron oxides can still be recognizedLenses of coarse-grained lithic wacke and conglomeratecomprise rock fragments of basalt mafic schist chertchloritendashquartz wacke and coarse detrital grains (quartzfeldspar) in a sericitendashchloritendashquartz matrix Coarseclastic rocks fill channels that cut into the fine-grainedrocks and contain numerous rip-up clasts This suggeststhat at least in part the Beatty Park Member wasdeposited distally from the source region Locally whitechert lenses crosscut erosional contacts indicating that thechert is diagenetic or epigenetic
Within all rocks of the Beatty Park Member sericiteand muscovite are of metamorphic origin They replacechlorite in the fine-grained chloritic shalendashsiltstone layersand feldspar clasts in the wacke units In several examplesfine-grained muscovite has grown along late cleavageplanes
A quartzndashchloritoidndashsericitendashchlorite(ndashsulfide) unitpreviously interpreted to be a carbonate intrusion (Lewis1971 Elias and Williams 1980) has been assigned to theBeatty Park Member The chloritoid is crystallized insprays and displays a lsquobow-tiersquo texture The presence ofabundant chloritoid indicates that this rock has a highalumina content implying either a pelitic precursor or thatthe protolith was extensively metasomatized
The Heines Member consists of an upward-finingsuccession of sedimentary rocks with a polymicticconglomerate at its base followed by clastic sedimentaryunits (sandstone to shale) The type area is near Durack
20
Pirajno et al
Well on BRYAH At this locality the Heines Memberis folded into a syncline and its southern limb is in faultedcontact with the underlying Narracoota Formation Thenorthern contact is obscured here by the Cainozoic coverThe Heines Member includes those outcrops south of theRobinson Syncline at the Heines Find prospect RandellBore and 35 km northwest of Durack Well which werepreviously mapped as lsquoWilthorpe Conglomeratersquo byGee (1987) The succession is approximately 600 mthick although basal units may have been shearedoff along the faulted contact The basal polymicticconglomerate contains clasts of mafic lithic wackelimestone quartz arenite and hematitic shale supportedby a carbonate matrix This is followed upward by a seriesof sandstonendashshale units with the shale componentbecoming volumetrically greater with stratigraphic heightThe basal conglomerate of the Heines Member containsno volcanic clasts of the underlying Narracoota Formationand this is taken as evidence that the contact with the latterformation is tectonic The provenance of the various clastsin the basal conglomerate is not known In the Heines Findprospect area the Heines Member is overlain by theRobinson Range Formation
Robinson Range Formation
The Robinson Range Formation forms elongate outcropsthat extend from east to west in the centre of the BryahndashPadbury Basin and in a northerly direction on the easternmargin of the Yarlarweelor gneiss complex on MILGUN andPADBURY (Plate 1) The Robinson Range Formation isdefined by the appearance of ferruginous or hematiticshale followed by two iron formations mdash a well-definedlower banded unit separated by 100 m of ferruginousshale from an upper unit with clastic textures as mappedby Gee (1987) which is in turn overlain by hematitendashchlorite siltstone The Robinson Range Formation isconformably overlain by the Millidie Creek Formation
The Robinson Range Formation consists of asuccession of BIF siltstone and iron-rich shale Granulariron formation is present as irregular lenses The BIFconsists of laminae up to 3 cm thick These laminationscomprise various amounts of quartz iron oxides (hematiteor magnetite) biotite and locally ferro-actinolite Theshale and siltstone consist of fine-grained sericite quartzchlorite iron oxides and in a few places minor spheneThe mesostructure microstructure and petrology ofthe BIF are relatively simple Microbands or laminae lessthan 1 to 2ndash3 mm thick are made up of alternatingmicrocrystalline quartz(ndash iron oxides) greenndashbrownbiotite(ndash iron oxides) quartz grains(ndash acicular crystals ndashiron oxides) quartz grains(ndash iron oxides ndash biotite ndashacicular crystals) Commonly the quartz grain(ndash acicularcrystal) assemblage displays a polygonized texturesuggestive of annealing due to metamorphism Theacicular crystals are weathered to iron oxides but onthe basis of their morphology they could be eitherstilpnomelane crystals or amphiboles The iron oxides areeither hematite or magnetite Incident light microscopyreveals that a primary titaniferous magnetite is replacedby hematite which in turn is replaced by goethite in thesupergene environment The biotite is porphyroblastic and
mostly grown under conditions of peak metamorphism(see Metamorphism)
Granular iron-formation is characterized by a granulartexture and the presence of elongate peloids 1 to 4 mmlong The peloids consist of microcrystalline chert outlinedby rims of iron oxides (hematite with inclusions ofilmenite) The chert peloids are enclosed in finemicrocrystalline cherty or chalcedonic material Thepeloids and chert make up bands approximately 1 to15 cm thick with occasional laminae of fine chert(ndash ironoxides)
The ferruginous shale is composed of silt-sized quartzgrains and iron oxides with abundant interstitial biotiteand minor disseminated euhedral tourmaline crystals Thetourmaline was formed either during metamorphism or ahydrothermal event
The iron formations of the Robinson Range Formationhave been correlated with the granular iron-formation ofthe Frere Formation (Earaheedy Basin) 150 to 450 km tothe east-southeast by Hall and Goode (1978) whocompared them to those of the Lake Superior region inNorth America
Millidie Creek Formation
The Millidie Creek Formation defined by Barnett (1975)and modified by Gee (1979) and Occhipinti et al (1997)forms comparatively small outcrops in the cores of theRobinson Syncline and Fraser Synclinorium (seeStructure)
Ferruginous shale and siltstone intercalated withirregularly banded manganiferous iron-formation formsthe basal unit of the formation This unit is locallylateritized and hosts many manganese deposits suchas the Millidie (or Elsa) mine (see Mineralization)The banded manganiferous iron-formation commonlyforms low ridges On PADBURY the Millidie CreekFormation consists of iron-rich shale and siltstoneirregularly banded manganiferous iron-formationdolomitic sandstone ferruginous quartz wacke andchloritic siltstone On BRYAH the Millidie Creek Formationconsists of ferruginous shales with a well-developed pencilcleavage sandstone and minor granular iron-formation
Dolomitic sandstone and quartz wacke are locallypresent within this formation The quartz wacke is wellbedded matrix supported and commonly containssubangular to subrounded quartz grains The matrix of thisrock is composed of randomly oriented fine-grainedbiotite and includes late sphene and minor sericite Thedolomitic sandstone comprises carbonate quartz andmuscovite
In low hills 3 km north of 5 Mile Well (Plate 1) finelybedded micaceous siltstonendashshale with interbeddedquartzndashdolomite siltstone layers previously assigned to theLabouchere Formation (Elias et al 1982) have beenassigned to the Millidie Creek Formation These rocks arefolded about northwesterly trending D4 fold axes andcontain S4 foliation They are unconformably overlain by
21
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
subhorizontal to shallowly dipping basal quartz arenite ofthe Bangemall Group
Chloritic siltstone at the top of the Millidie CreekFormation is compositionally similar to the Beatty ParkMember and comprises quartz feldspar lithic fragmentsof sericitendashquartz schist and detrital cordierite grains ina foliated matrix of chlorite
Unassigned units of the Padbury Group
Metasedimentary rocks and biotitendashsericite schist whichoutcrop within the Despair Granite near the Wilthorpegold mine (Plate 1) were previously referred to aschloritendashmuscovitendashquartz schist and not assigned to anygroup (Elias et al 1982) Occhipinti and Myers (1999)tentatively assigned these units to the Padbury GroupThere are two main outcrops one in the Wilthorpe mineand the other just outside the mine as a fault-boundedinclusion within the granite
Sedimentary rock found within the Despair Graniteis heterogeneously deformed and metamorphosedSedimentary structures such as cross-bedding andbedding-parallel laminations are present This rockconsists of alternating layers of very fine grained biotitequartz sericite and feldspar Accessory minerals includeopaque minerals In a few places this rock contains afoliation parallel to faults or fold-axial planes Opaqueminerals commonly crosscut the dominant (bedding)fabric The preservation of the primary sedimentarytextures suggests that strong deformation did notaccompany low-grade greenschist-facies metamorphism ofthese rocks
Within the Wilthorpe mine the metasedimentary rockscontain a slightly different mineralogy and are in faultedcontact with the sericitized Despair Granite For instancein one sample there are two distinct layers composed ofeither sericite quartz biotite and opaque minerals orbiotite sericite quartz and minor opaque minerals Thisvariation in bedding composition is consistent with thatobserved in the metasedimentary rocks outcroppingoutside the mine The rocks within the mine are coarsergrained and comprise quartz biotite sericite andandalusite Sericite and biotite overprint the foliation inthe rock
StructureThe Padbury and Bryah Basins are pervasively deformedThis deformation may have solely occurred duringthe c 18 Ga Capricorn Orogeny a period of obliquecollision between the Archaean Pilbara and YilgarnCratons (Tyler and Thorne 1990 Tyler et al 1998Fig 2) or in part during the earlier c 20 Ga GlenburghOrogeny (Occhipinti et al 1999) In addition to deformingthe Bryah and Padbury Groups this deform-ation also resulted in the reworking of parts of theArchaean Narryer Terrane and the Marymia Inlier of theYilgarn Craton (Fig 2) to form the Yarlarweelor gneisscomplex and Peak Hill Schist The rocks of the Bryah
and Padbury Groups are locally interleaved with theYarlarweelor gneiss complex in the western part of theregion (Fig 18) To the south the Bryah and PadburyGroups are tectonically juxtaposed against autochthonousrocks of the Archaean Murchison Terrane of the YilgarnCraton and the Palaeoproterozoic Yerrida Group (Fig 2)
The Yarlarweelor gneiss complex dominantly consistsof Archaean granitic gneisses that were intruded by felsicmagmas at c 1960 Ma (Sheppard and Swager 1999) and1820ndash1800 Ma (Occhipinti et al 1998b Sheppard andSwager 1999) Granite sheets and veins intruded into theArchaean gneisses were pervasively deformed into opento tight folds and metamorphosed at medium to highgrades during the Capricorn Orogeny Occhipinti andMyers (1999) suggested that these folds were originallynortherly trending however they are probably more likelyto have been northeasterly trending Dextral strike-slipshear movement involved a transition from early ductileto later brittle deformation (Occhipinti et al 1998b)coincident with uplift which probably progressed fromnortheast to southwest in the region This deformationproduced regional-scale fault-bend folds in both theYarlarweelor gneiss complex and overlying Palaeo-proterozoic Bryah and Padbury Group rocks
Deformation histories presented for the Yerrida Bryahand Padbury Groups by various authors (including Windh1992 and Gee 1990) have many elements in common(Table 5) This includes major northndashsouth compressionthat was responsible for the development of prominentregional easterly trending upright folds such as theRobinson Syncline (Fig 18) Northerly striking folds andfaults in the domain just east of the Yarlarweelor gneisscomplex have been recognized as a later deformation stage(Windh 1992 Martin 1994) Gee (1990) Windh (1992)and Martin (1994) proposed that eastward movement ofthe Narryer Terrane (here referred to as the Yarlarweelorgneiss complex) was responsible for the development ofthese northerly trending folds In their interpretation thenortherly striking folds formed in front of an advancingthrust sheet of Archaean gneiss and granite overriding theBryah and Padbury Groups Myers (1989 1990) andMyers et al (1996) on the other hand regarded the Bryahand Padbury Groups as allochthonous sheets that werethrust over Archaean granitendashgneiss
Contacts of the Bryah and Padbury Groups with theNarryer Terrane Yarlarweelor gneiss complex MarymiaInlier Murchison Terrane and the PalaeoproterozoicYerrida Group are zones of high strain and thereforeinferred to be faults Unconformable contacts between theBryah and Padbury Groups were reported by Martin(1994 1998) whereas sheared and faulted contacts werereported by Pirajno and Occhipinti (1998) Occhipintiet al (1998ac) and Occhipinti and Myers (1999) Forexample the Bryah Group is in faulted contact with theYarlarweelor gneiss complex north of Livingstones Findand the Murchison and Narryer Terranes are separatedfrom the Bryah and Padbury Groups by the steep easterlytrending Murchison Fault which has a sinistral strike-slipcomponent (Plate 1 Fig 2)
The Goodin Fault a high-angle reverse fault (Pirajnoand Occhipinti 1998) is the boundary between the
22
Pirajno et al
Yerrida and Bryah Groups (Fig 2 Plate 1) East of thisfault the Doolgunna Formation (Yerrida Group) is foldedinto isoclinal upright folds however much of thedeformation in the Yerrida Group dies out rapidly to theeast and southeast To the west the Goodin Fault mergeswith the Murchison Fault which has juxtaposed the Bryahand Padbury Groups against the Yilgarn Craton TheMurchison Fault has a sinistral strike-slip componentwhich offsets Archaean structures in the Murchison andNarryer Terranes
In this Report four distinct groups of structuresD1ndashD4 representing progressive compressional deform-ation are recognized (Table 5) This deformation historyalthough in broad agreement with the previously publishedstructural histories (eg Windh 1992) recognizes separateearly layer parallel structures The structures resultingfrom the four deformation events are not developedeverywhere or with the same intensity everywhere
The earliest deformation events are defined in the PeakHill Anticline area as D1 layer-parallel mylonitic thrustfaults and originally subhorizontal folds overprinted byD2 upright eastndashwest striking regional folds Both D1 andD2 structures developed by northndashsouth compression and
can be interpreted as successive stages of progressivedeformation Northerly trending regional D3 folds andupright foliations recording eastndashwest compression areweakly developed in the Peak Hill Anticline but betterdeveloped and largely restricted to a domain immediatelyeast of the Yarlarweelor gneiss complex However thesenortherly trending structures do not always overprint oldereasterly trending structures and in places these two setsof structures (D2 and D3) tend to be mutually exclusivesuggesting that they probably developed during the sameprogressive deformation event Late medium-scale D4structures include west-northwesterly to northwesterlytrending subvertical foliations shear zones zones ofsmall-scale folding and faults now outlined by quartzblows These locally developed structures suggest latenorth-northeast to south-southwest compression
Major fold structures in the Padbury and Bryah Basinsare the Peak Hill Anticline Robinson Syncline MillidieSyncline Fraser Synclinorium Horseshoe Anticline andPadbury Syncline (Plate 1 and Fig 18) The Peak HillAnticline Robinson Syncline Fraser Synclinorium andMillidie Syncline all represent refolded folds The easterlytrending doubly plunging Robinson Syncline andPeak Hill Anticline are D2 folds refolded during D3 D1
Figure 18 Major regional structures in the Bryah and Padbury Groups (after Occhipinti et al 1998a)
FMP371
MARYMIAINLIER
YILGARNCRATON
Goodin
Fault
GROUPBANGEMALL
Murchison Fault
118deg30 119deg30
30 km
020300
YERRIDAGROUPPeak Hill
Anticli
ne
Robinso
n
Synclin
e
Nathan Syncline
Zone of D folding3
Padbury
Horseshoe Anticline
Wilthorpe F
t
BRYAH ANDPADBURYGROUPS
GOODININLIER
EARAHEEDYGROUP
25deg30
26deg00
Syncline
Millidie Syncline
FaultD fold trace3
D fold trace2
1
D fault1
Anticline
SynclineD ndash D thrust fault2
Yarlarweelorgneiss
complex
FraserSynclinorium
23
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
folds are also present within these structures (see D1structures) The Horseshoe Anticline appears to be a D3fold contained within the fault-bounded Horseshoeanticlinal block This fault-bounded block also appears tobe cut by northwesterly trending (D4) faults
D1 structuresThe first Palaeoproterozoic deformation event (D1)produced layer-parallel folds a locally pervasive S1schistosity mylonites and faults However because thesestructures were pervasively overprinted by D2 structuresthey are rarely observed F1 folds are locally observed inthe Peak Hill Antiform Robinson Syncline FraserSynclinorium an area 5 km northeast of Mount Fraserand the Millidie Syncline These folds are also observednear the Peak Hill mine in F2 foldndashhinge zones of quartzblastomylonites of the Peak Hill Schist (Fig 6) Here theyare small-scale rootless isoclinal plunge shallowlytowards the east and strike eastndashwest In the FraserSynclinorium and Millidie Syncline the F1 folds are small-scale isoclinal folds that plunge gently towards the east-northeast or west-southwest and strike east-northeasterlyF1 folds are also inferred from aeromagnetic data to bepresent within the Fraser Synclinorium and MillidieSyncline (Figs 18 and 19)
The Goodin and Murchison Faults may be D1 faultsthat were reactivated during D2 (Occhipinti et al 1998c)The Murchison Fault (Figs 18 and 19 Plate 1) separateslargely undeformed basaltic hyaloclastite rocks in thesouth from foliated mafic schists to the north
Mesoscale F1 folds in the shale and banded iron-formation of the Robinson Range Formation are observednear Mount Padbury north-northwest of Beatty Park Bore
(Plate 1) in the hinge zone of the Robinson Synclinenorth of Tank Well and northeast of Randell Bore TheseF1 folds are tight to isoclinal with shallow plunges thattrend to the east or west The F1 folds in the area areinterpreted as originally recumbent D1 zones of highstrain and mylonite developed locally mainly in thePeak Hill Schist (Pirajno and Occhipinti 1998) andalong contacts between the Yarlarweelor gneiss complexand Palaeoproterozoic cover rocks These mylonite zonesare not observed at higher stratigraphic levels within thebasin suggesting that they are restricted to a deeper crustallevel represented by the Peak Hill Schist and basementndashcover contacts Quartz blastomylonites and the CrispinMylonite (Pirajno and Occhipinti 1998) form continuousunits within the Peak Hill Schist (Plate 1) The internalstructure of these units suggests that they may be D1shear zones which were refolded during the laterdeformation events The original nature and orientation ofthese shear zones is not known The Crispin Myloniteconsists of quartzite pebble-and boulder-sized clasts in asericitendashquartz-rich matrix and has the appearance of aconglomerate For that reason it was mapped by Gee(1987) as the lsquoCrispin Conglomeratersquo However meso-scopic and microscopic structures indicate that it is amylonite (Figs 4 and 7) Both the quartzite clasts andmatrix contain a mylonitic fabric The Crispin Myloniteis interpreted as a lsquopseudo-conglomeratersquo (Raymond1984ab) formed by shearing probably along or close toa fault plane that separated an arkosic or granitic unit froma quartz-rich unit
Like the Crispin Mylonite the quartz blastomylonitesform arcuate lenses within quartzndashmuscovite schist of thePeak Hill Schist and are refolded by F2 and F3 folds Thequartz blastomylonites contain isoclinal and sometimesrootless F1 folds and are interpreted to have beendeformed in a ductile high-strain zone (fault or shear zone)during D1 It is not possible to determine the sense ofmovement during D1 because no shear sense indicatorswere observed during mapping
D2 structuresThe D2 deformation produced large-scale uprightregional F2 folds with variably developed S2 foliationas well as faults and shear zones These structuresare easterly trending recording northndashsouth shorteningHowever more complex patterns in the Mount Fraserarea suggest complicated refolding patterns ProminentD2 folds include the doubly plunging Robinson Synclineand the Padbury Syncline which has the hinge zonelargely sheared out (Fig 18 Plate 1) Mesoscale F2folds show steeper plunges and the S2 foliation becomesmore intense to the north A pervasive S2 foliation isdeveloped over large areas in the mafic schists ofthe Narracoota Formation The Goodin Fault is a high-angle reverse fault that forms the boundary between theYerrida and Bryah Groups This fault may have developedduring D2 because south of the fault the DoolgunnaFormation is folded into tight to isoclinal upright folds(with fold-axial surfaces subparallel to the Goodin Fault)that are similar to D2 folds in the Bryah and PadburyBasins
Table 5 Sequence of deformation events in the Bryah and PadburyBasins
Deformation Compressionevent
D4 North-northeastndashsouth-southwest compressionSmall-scale folds subvertical foliation shearzones faults with quartz blows all trending
280degndash310deg
D3 Eastndashwest compressionnorthndashsouth trending folds subvertical foliationsubvertical faults or shear zones localized eastof Narryer Terrane increasingly disharmoniceast-northeasterly trending folds eastwards
D2 Northndashsouth compressionupright tightndashisoclinal eastndashwest folds andsubvertical foliation eastndashwest shear zonessouth-verging thrust faults
D1 Northndashsouth compressionsubhorizontal mylonites thrusts and foldsmesoscale recumbent folds tightndashisoclinalrootless
24
Pirajno et al
The Livingstone Synform a steep easterly plungingtight fold on MOORARIE may be part of a larger scale D2fold structure that is confined between the Kerba Fault inthe north and the Mount Seabrook Fault in the south(Occhipinti and Myers 1999)
Within the Yarlarweelor gneiss complex graniticgneisses form open to isoclinal easterly to northeasterlyand northerly trending shallowly to steeply plungingfolds These folds plunge either to the east and northeastor to the west and west-southwest indicating that on a
Figure 19 Simplified geological map of the Bryah and Padbury Groups (after Occhipinti et al 1998a) See Figures20 22 and 23 for cross sections
118deg 119deg
25deg45
10 km
MarymiaInlier
YilgarnCraton
BangemallBasin
Bill
ara
Fa
ult
Wilt
horp
eF
Fortnum
25deg30
Goo
din
Faul
t
Kinders FaultNathan
Peak Hill
B
AC
Mt Fraser
Yarlarweelor gneisscomplex
(reworked NarryerTerrane)
YerridaBasin
PADBURY GROUP
BRYAH GROUP
RAVELSTONE FORMATION lithic wacke
KARALUNDI FORMATION clastic rocks
quartzndashmuscovitendashbiotitendashstaurolite schist
HORSESHOE FORMATION shale banded iron-formation
YERRIDA GROUP
WILTHORPE FORMATION conglomerate siltstone
PA
LA
EO
PR
OT
ER
OZ
OIC
Greenstone
Peak Hill Schist
AR
CH
AE
AN
Fault
Anticline
Syncline
ME
TA
MO
RP
HO
SE
D
NARRACOOTA FORMATION maficndashultramafic volcanic rocks
LABOUCHERE FORMATION quartz wacke siltstone
Unconformity
Mine
Cross-section
Undifferentiated rocks
MILLIDIE CREEK FORMATION Lithic wacke dolomitic sandstone siltstone banded iron-formation
Granite and graniticgneiss
ROBINSON RANGE FORMATION shale granular iron-formation banded iron-formation
140300FMP373
25
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
regional scale they are doubly plunging possiblyrecording later refolding and eastndashwest shortening (D3)These folds deform both the Archaean gneiss and c 1960and c 1820 Ma granite sheets that intruded the gneiss(Sheppard and Swager 1999 Occhipinti et al 1998c)They refold tight to isoclinal subhorizontal to shallowlyplunging folds in the Archaean granitic gneisses whichmay have developed during the Archaean
The sense of shear of the steeply dipping D2 shearzones could not be determined South of the Robinson andFraser Synclines regional anastomosing D2 shear zonesdeveloped in the basaltic rocks of the NarracootaFormation To the northeast this regional structurebecomes the Jensen Fault (Pirajno and Adamides 2000)which can be shown to have displaced the Meso-proterozoic Bangemall Group suggesting that the faultwas reactivated after this time Along the southern limbof the Fraser Syncline another fault extends into the D2shear zones mentioned above A shear zone cuts thesouthern limb of the Heines Syncline which lies betweenthe Robinson and Fraser Synclines
D3 structures and theirrelationship to D2 structuresNortherly trending D3 folds faults and locally an uprightS3 foliation indicating an eastndashwest compression are welldeveloped in the area east of the Yarlarweelor gneisscomplex Further east F3 fold intensities decrease andfolds are locally more disharmonic The D3 event wasresponsible for the doubly plunging nature of theRobinson Syncline and the Peak Hill Anticline
The Kinders Fault (Fig 20 Elias and Williams 1980)is a northerly trending D3 fault separating a wedge ofmafic volcanic schists of the Narracoota Formation(Bryah Group) from the Robinson Range Wilthorpeand Labouchere Formation rocks (Padbury Group) Thisfault lies along the western limb of the sheared-out hingeof the F3 Nathan Syncline (Plate 1 and Fig 18) Thissyncline was previously correlated with the PadburySyncline to the south (Elias and Williams 1980 Martin1994 1998) Part of the southerly plunging fold hingeof the Nathan Syncline is preserved in the Nathan minearea and the closure of this syncline can be traced furthernorth The wedge of maficndashultramafic schists of theNarracoota Formation was interpreted by Occhipinti et al(1998c) and Martin (1994 1998) to represent an F3anticlinal fold-thrust wedge overlying pervasively foliatedand metamorphosed quartz wacke of the LabouchereFormation to the west (Figs 19 and 20)
West of the Kinders Fault along the Billara Faultsericitendashquartz schist locally with quartz-pebbleconglomerate layers contains a pervasive S3 fabricF3 folds however are difficult to trace East of theKinders Fault open to close and locally tight to isoclinalfolds are outlined by marker beds in the Labouchere andHorseshoe Formations S3 foliations and moderate tosteep southerly plunging small-scale F3 folds are welldeveloped in the area of the Horseshoe Syncline andfurther north
Several observations suggest that D2 and D3 structuresmay not reflect two separate events but may havedeveloped contemporaneously in different domainsIntense D3 folding is largely restricted to the area betweentwo basement highs represented by the Yarlarweelorgneiss complex in the west and the Peak Hill Schist in theeast (Figs 18 and 19) In the domain just east of andadjacent to the Yarlarweelor gneiss complex there is noevidence for D3 refolding D2 (ie upright northerlytrending D3 folds overprinting upright easterly trending D2folds) even though weak northerly trending D3 foldsdeform easterly trending F2 folds around and within thePeak Hill Anticline
In the Mount Fraser area complex fold and foliationpatterns show orientations different from and transitionalto both the regional D2 and D3 deformation Large-scaleeast-northeasterly trending F2 folds such as the RobinsonSyncline and Peak Hill Anticline die out in this area TheMillidie Syncline can be traced from a west-northwesterlystrike (subparallel to and en echelon with the RobinsonSyncline) to a west-southwesterly strike and is then cutoff to the south by D3 faults (Figs 18 and 19)
These observations suggest that the intensity and trendof the D2 and D3 structures were influenced by their spatialrelationship to the Yarlarweelor gneiss complex and PeakHill Schist
D4 structuresD4 structures include mesoscopic chevron folds kinksshear zones and faults and were locally accompanied bythe development of a foliation These D4 structuresdeveloped locally throughout the Bryah and PadburyBasins Yarlarweelor gneiss complex and the northern-most part of the Murchison Terrane In the PadburyndashBryahdomain most structures trend between west-northwest andnorthwest although in the Yarlarweelor gneiss complexa few late structures trend between north-northwest tonorth Brittle faults cutting the Yarlarweelor gneisscomplex often show dextral strike-slip shear movement
MetamorphismRegional metamorphic zones within the volcano-sedimentary succession are related to the geometry of thePeak Hill Anticline and Yarlarweelor gneiss complex Thehighest metamorphic grade assemblages are found in thecontact zones between the Yarlarweelor gneiss complexand overlying metasedimentary rocks Assemblages inthe Peak Hill Schist and within quartzndashmica schists(Labouchere Formation) along faulted contacts withthe Yarlarweelor gneiss complex record upper greenschist-to lower amphibolite-facies conditions Within theYarlarweelor gneiss complex upper amphibolite-faciesconditions were reached as incipient (minimum) meltpatches within granitic gneiss and amoeboid textures inPalaeoproterozoic coarse-grained granite probablydeveloped during D2 (Sheppard and Swager 1999) In theBryah and Padbury Groups however metamorphismtypically does not exceed greenschist facies and east of
26
Pirajno et al
0
2
4
6
Fault
Kilo
met
res
Southwest Northeast
FMP372
0
2
4
6
Kilo
met
res
West East
Billara
Fault
Kilo
met
res
0 Padbury
South North
SynclineDome
2
4
6
Yarlar-weelor
170300
Fault
Kinders
MIDDLE PROTEROZOIC
ARCHAEAN (reworked during Early Proterozoic)
Bangemall Group
Unconformity
Bedding or layering trend
Foliation
High-strain zone
Fault
Movement along fault
Movement away and towards observer
2
BRYAH GROUP
Geological boundary
Padbury Basin
Bryah Group
S N
d)
sediment fluxsediment flux
EARLY PROTEROZOICPADBURY GROUP
ARCHAEAN (in situ)
Peak Hill Schist quartzndashmuscovite schistquartz mylonite phyllonite
Granitendashgreenstone Murchison Terrane
Millidie Creek Formation sandstoneshale dolomitic siltstone
Robinson Range Formation ferruginous shalebanded iron-formation
Wilthorpe Formation quartz-pebbleconglomerate
Labouchere Formation quartz wackesiltstone quartz arenite
Horseshoe Formation ferruginous shaleiron formation
YERRIDA GROUP
Narracoota Formation metabasalt subordinatedolerite picrite and peridotite
Goodin
Normal fault reworked during D thrusting
Granite gneiss and granite with lenses of supracrustal rock Narryer Terrane
GranitendashgreenstoneMarymia Inlier ndash Murchison Terrane
Ravelstone Formation lithic wacke
Karalundi Formation clastic rocks
a) Cross section A
b) Cross section B c) Cross section C
Undifferentiated rocks
27
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
the Goodin Fault in the Yerrida Group metamorphic gradedecreases to subgreenschist facies (prehnitendashpumpellyite)The relationships between metamorphic mineral growthand deformation are summarized in Table 6
M1 was a prograde regional metamorphic event thattypically reached greenschist facies (Pirajno andOcchipinti 1998) and was probably coincident withD1 in the Bryah and Padbury Groups and Peak Hill SchistThornett (1995) suggested that some parts of the Peak HillSchist reached amphibolite-facies metamorphism withtemperatures between 500deg and 620degC and pressures of65 ndash 7 kbar Metamorphic mineral assemblages observedhowever commonly do not concur with these data Thesecond metamorphic episode M2 was commonly one ofretrogression throughout most of the Bryah and PadburyBasin and probably associated with metasomatismin high-strain zones during D2ndashD3 During M2 inthe western part of the Bryah and Padbury Basinsadjacent to the Billara Fault (Fig 18) staurolitendashandalusitendashbiotitendashmuscovitendashquartz schist developedfrom the metamorphism of Padbury Group sedimentaryrocks These rocks indicate metamorphism at amphibolitefacies Inclusion trails in staurolite and andalusiteporphyroblasts suggest that the porphyroblastic growthoccurred after D1 but before D2 The S2 foliation is definedby the alignment of muscovite and biotite which wrapsaround the porphyroblasts and probably developed in D2during M2 As staurolite is locally partially replaced byfine-grained muscovite this foliation may have developedin the greenschist facies This foliation is locallyoverprinted by chloritoid Further west at the contactbetween the Palaeoproterozoic Kerba Granite and theNarracoota Formation a quartzndashkyanitendashtremolitendashfeldspar schist indicates upper greenschist-faciesmetamorphism with the pressure of metamorphismestimated to have been between 3 and 4 kbar (Spear 1993Occhipinti and Myers 1999)
For the most part M2 involved retrogression meta-somatism and local hydrothermal alteration Mineralassemblages formed during M2 are commonly observedin high-strain zones where the S2 schistosity is welldeveloped These include a domain of well-developed D2shear zones south of the Robinson Syncline wherepervasive retrogression of metabasalts to actinolitendashchlorite schist is observed (Pirajno et al 1995a) In
addition in the Mount Pleasant opencut growth of albiteporphyroblasts and the development of chlorite at theexpense of biotite and epidote also occurred during M2
Banded iron-formation in the Robinson RangeFormation shows a change in metamorphic mineralassemblage from east to west across the trend of the D2Robinson Syncline To the west randomly oriented biotiteoverprinted quartz stilpnomelane and iron oxides Theappearance of this late-stage biotite coincides withregional geochemical trends (elevated Sb As and WDavy et al 1999) along the same structure suggesting alate- or post-D2 low-temperature metasomatic eventAlbite porphyroblasts in alteration zones associated withgold mineralization in the Peak Hill Schist also grew at alate stage because they overprint S2
South of the Murchison Fault little-deformed basaltichyaloclastites contain mineral assemblages characteristicof prehnitendashpumpellyite to lower greenschist facies Thissuggests that rocks south of the Murchison Fault were notexposed to the regional greenschist-facies metamorphismor moderate- to high-grade metamorphism that occurredelsewhere in the region
Structural synthesisA number of models have previously been presented toexplain the structural and metamorphic history of theBryahndashPadbury region For these models the driving forcewas assumed to be collisional tectonics related to theCapricorn Orogeny (eg Tyler et al 1998 Occhipintiet al 1998c Pirajno et al 1998b)
Gee (1990 p 207 Gee and Grey 1993) interpretedthe movement of the lsquoYarlarweelor Gneiss Beltrsquo andlsquoMarymia Domersquo in terms of rising lsquosolid-state crystalndashplasticrsquo domes They suggested that the resulting rise andsouthward movement of the lsquoYarlarweelor Gneiss Beltrsquoand lsquoMarymia Domersquo produced recumbent folds in theoverlying sedimentary rocks of the Bryah Basin Furtherrise and convergence of the domes following depositionof the Padbury Group caused complex refolding ThelsquoYarlarweelor Gneiss Beltrsquo was thrust to the east overthe Bryah and Padbury Groups at this time Martin(1994) interpreted the emplacement of the lsquoNarryer
Figure 20 Selected idealized cross sections through the Bryah and Padbury Groups (after Occhipinti et al 1998a) Locationsof a) to c) are shown on Figure 19 (note difference in scale)a) Northeastndashsouthwest section in the central-eastern part of the Bryah and Padbury Basins showing the fault-bendfold model for the Peak Hill Anticline and inferred suture between the Yilgarn Craton (Murchison Terrane) andreworked Archaean Marymia Inlier The extensional fault slice along the northern margin of the craton formed duringearly development of the Bryah Basin (lsquopassive marginrsquo) and was preserved in this idealized section after basinclosureb) Eastndashwest section across the zone of D3 fold and fault structures The section highlights the intense deformationacross the zone between the Billara and Kinders Faults and shows an inferred major detachment (within underlyingmafic volcanic rocks of the Narracoota Formation) zone of highly disharmonic F3 folding mapped at the surfacec) Northndashsouth section in the central-western part of the Bryah and Padbury Basins showing the Yarlarweelor Domethe sheared-out Padbury Syncline and the Murchison Fault as the suture between in situ and reworked ArchaeanNarryer Terrane Note the inferred detachment of the BryahndashPadbury succession along the contact with the NarryerTerraned) The development and onlap of the Padbury Basin onto the underlying Bryah Group
28
Pirajno et al
Gneiss Complexrsquo (lsquoYarlarweelor Gneiss Beltrsquo) as due tolsquolateral escape tectonicsrsquo resulting from the lsquotranscurrentsuturingrsquo of the Yilgarn and Pilbara Cratons during theCapricorn Orogeny Martin (1994) suggested that earlynorthndashsouth movements which changed to localized eastndashwest movements indicate the onset of lsquolateral escapetectonicsrsquo and the eastward expulsion of the northeasternpart of the lsquoYarlarweelor Gneiss Beltrsquo along the Wilthorpeand Kinders Faults In contrast Myers (1989 1990)regarded both the lsquoYarlarweelor Gneiss Beltrsquo and thevolcano-sedimentary rocks of the Bryah and PadburyGroups as allochthonous sheets that were thrust over the
Yilgarn Craton basement and subsequently folded abouteastndashwest axes
An alternative model was presented by Occhipintiet al (1998c Fig 21) who suggested that the Bryah Basindeveloped initially as a rift and the Padbury Basindeveloped over the Bryah Basin in a retroarc foreland-basin setting (see also Martin 1994) Formation of thePadbury Basin in a compressional regime was essentiallyconcommitant with the closure of the Bryah Basin and thedevelopment of D1 structures as subhorizontal shear zonesbetween the Archaean Narryer Terrane basement and the
Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group anddeformation fabrics
Formation Rock type Mineralogy Pre-S1 S1 Post-S1 S2ndashS3 Post-tectonicM1 M2
Peak Hill Schist pelite quartz biotite muscovite chlorite albite tourmaline
chemical sediment quartz spessartine magnetite
calc-silicate quartz epidote chlorite actinolite titanite magnetite
psammite quartz muscovite andesine opaques
Narracoota metabasite quartz actinolite epidote chlorite sericite arfvedsonite titanite calcite
volcanic breccia albite pumpellyite
Ravelstone pelitic tourmalinite quartz muscovite tourmaline garnet feldspar
subarkosic wacke quartz biotite albite sericite tourmaline
Horseshoe banded iron-formation quartz biotite grunerite spessartine chlorite
Robinson Range banded iron-formation quartz stilpnomelane biotite
NOTE No data are available for the Labouchere and Wilthorpe Formations
29
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
supracrustal rocks of the Bryah and Padbury Groups Theoverall movement direction was interpreted as being fromnorth to south but locally because of the possible effectof later dextral shear movement may actually have been
ram
p
Peak Hill Anticline
N S
eg Kinders Fault Peak HillAnticline
Thrust flatrsquo Lateral
ramp Obliq
ue
lateral ramp
Yarlarweelor
Basalthrustplane
2Dc)
d)
2D thrust flat
rsquo
eg Yarlarweelor gneiss complex
gneiss complex
Padbury Group
Bryah Group
Reworked Archaean granite
a)
Archaean granite
b)
2prospective D crustal thrustwith frontal ramp
1D tectonic interleaving zone(eg Peak Hill Schist)
1 2Post-D and pre-D
D tectonic interleaving between reworked Archaeancrust ( underplate) and BryahndashPadbury succession
rsquo1
Post-D D2 3
W E
Thrust ramp
Thrustfrontal
Later
al ra
mp
FMP374 011199
W E
N
Thrust flatrsquo
movement
Thrust
North to south
e)
ramprsquo
flatrsquorsquo
2D thrust flat ndash frontal ramp ndash lateral ramp geometry
Figure 21 Model of the structural development of the BryahndashPadbury Group succession (after Occhipinti et al1998a)a) Zone of D1 subhorizontal tectonic interleaving(by thrust duplexing) between reworked Archaeancrust and overlying rocks of the BryahndashPadburysuccession This zone includes high-strain ormylonitic rocks formed by lsquounderplatingrsquo of theArchaean rocks beneath the volcano-sedimentaryrocks during initial closure of the Bryah back-arcbasinb) Post-D1 geometry with trace of incipient D2crustal-scale thrust with frontal rampc) D2 geometry with fault-bend anticline developedabove the crustal D2 thrust ramp Upright folds inthe volcano-sedimentary succession (eg Padburyand Robinson Synclines) formed ahead of themain thrustd) Post-D2D3 geometry along schematic eastndashwestsection D2 fault-bend anticlines are not shownNorth-to-south movement ie movement towardsviewer leads to eastndashwest compression and hencenorthndashsouth folds and reverse or thrust faults in thedepression between (oblique) lateral ramps at thesame time as eastndashwest D2 folding occurredelsewheree) Schematic view looking north-northwest of thebasal thrust fault with frontal and lateral rampshighlighting the north-to-south movement directionof the thrust sheet
northwest to southeast Substantial movement and highstrains can be inferred from tectonic interleaving (egbetween the Billara and Wilthorpe Faults Fig 19) andfrom the development of the mylonitic zones in possiblethrust duplexes in the Peak Hill Schist Other possibleD1 structures in particular subhorizontal thrust faultsmay have locally developed along the contacts betweenthe Bryah and Padbury Groups Small-scale earlylayer-parallel folds in chert and BIF layers particularlyfrom within the Padbury Group suggest that subhorizontalD1 structures locally formed within the volcano-sedimentary succession (Pirajno and Occhipinti 1998Swager and Myers 1999) Deposition of the PadburyGroup in a retroarc foreland basin (Martin 1994)was probably contemporaneous with the early stagesof D1
The Yarlarweelor gneiss complex and Peak Hill Schistwere described by Occhipinti et al (1998c) as lsquobasement-cored anticlinesrsquo that developed above frontal thrust rampsThe overlying supracrustal rocks and their high-strain D1contact zones were folded by north to south movementover these ramps during D2 deformation In the Peak HillSchist subhorizontal D1 folds are refolded about anupright apparently easterly trending D2 antiformThe hinge of this fold may be sheared out along thecontact with the Marymia Inlier which is marked by aquartz blastomylonite previously mapped as deformedquartzite of the Juderina Formation (Adamides 1998) Theoriginal orientation of the D2 fold may have been east-northeasterly The Peak Hill Schist outcrops around adomal structure produced by refolding of the D2 fold aboutan approximately northerly trending D3 fold-axial surfaceIt was argued by Occhipinti et al (1998c) that the D3 foldsdeveloped in a structural lsquodepressionrsquo between the two
30
Pirajno et al
basement-cored anticlines which acted as lateral rampsin the thrust plane Northerly trending structures developedduring northndashsouth compression as the lateral ramps wereslightly oblique to the movement direction leading tospace problems between the basement-cored anticlinesThis resulted in either lateral shortening or verticalexpulsion (or both) of the Bryah and Padbury Groups
Occhipinti et al (1998c) assumed that the Yarlarweelorgneiss complex (referred to by them as the NarryerTerrane) was an Archaean crustal fragment that influencedthe structural deformation in the Palaeoproterozoic Bryahand Padbury Groups but was not itself largely deformedduring the Palaeoproterozoic Subsequently Sheppard andSwager (1999) and Occhipinti and Myers (1999)recognized Palaeoproterozoic deformation meta-morphism and felsic magmatism within the Yarlarweelorgneiss complex This indicates that the Yarlarweelor gneisscomplex was extensively reworked during the Palaeo-proterozoic and underwent the same D2ndashM2 metamorphicevent that has been recognized in the Bryah and PadburyGroups and Peak Hill Schist
Occhipinti et al (1998b) found that Palaeoproterozoiccoarse-grained granites and pegmatites with ages between1820 and 1780 Ma (Nelson 1998) intruded as sheetssynchronously with the D2 deformation event D McBMartin (1999 pers comm) interpreted granite exposedsouthwest of the Labouchere opencut as intruding thePadbury Group sedimentary rocks and suggested that thisgranite may also be of this age Intrusion of granitoiddykes and sheet-like plutons accompanied uplift of theYarlarweelor gneiss complex and is interpreted as beingconcomitant with dextral shearing in the region andpossibly D3 (Occhipinti et al 1998a Sheppard andSwager 1999) This movement was attributed to anoblique northndashsouth to northwestndashsoutheast collision ofthe Pilbara and Yilgarn Cratons during the CapricornOrogeny (Occhipinti et al 1998b 1999)
In the northwestern part of the Bryah and PadburyBasins the metamorphic grade increases from greenschistfacies in the east to amphibolite facies in the west Furtherwest in the Yarlarweelor gneiss complex the metamorphicgrade reached at least upper amphibolite facies (Sheppardand Swager 1999) Uplift of the Yarlarweelor gneisscomplex from 9ndash10 kbar to greenschist facies occurredbetween c 1812 and c 1800 Ma (Occhipinti et al 1998b)The c 1812 Ma granitoid sheets and dykes were meta-morphosed at high grade (see below) whereas c 1800 Magranites were only metamorphosed to greenschist facies(Occhipinti et al 1998b) Medium-grade metamorphismof the Padbury Group is solely preserved adjacent to theYarlarweelor gneiss complex between the Billara andWilthorpe Faults (see Metamorphism Fig 18 Plate 1)The drop in metamorphic grade to greenschist facies only15 ndash 25 km east of the contact suggests either a rapidincrease in temperature close to the Yarlarweelor gneisscomplex or that amphibolite-facies or upper greenschist-facies (or both) Bryah and Padbury Group rocks have beenfaulted out The latter explanation is preferred because theboundary between amphibolite-facies and lower to middlegreenschist-facies rocks of the Labouchere Formation issharp
In the Bryah and Padbury Groups and Peak Hill Schistmetasomatism accompanied retrogression of D1ndashM1assemblages to greenschist facies during M2 particularlyin D2 shear zones In the Yarlarweelor gneiss complexthere is no evidence for D1ndashM1 and M2 was initially ahigh-grade metamorphic event with the formation ofincipient minimum melt during the early stages of D2(Occhipinti et al 1998b) Post-M2 the metamorphic gradedropped significantly to greenschist facies
In the proposed model shown in Figure 22 the BryahGroup developed in a back-arc lsquorift-type settingrsquo (Pirajnoet al 1998b see Tectonic model and conclusions) If theBryah and Padbury Groups are c 20 Ga or older then D1structures could have developed during the c 20 GaGlenburgh Orogeny (Occhipinti et al 1999 Tyler 1999)as a result of west to east or northwest to southeastcompression Plutonism in the future Yarlarweelor gneisscomplex produced the 1960 Ma felsic granitoid rocksduring the late stages of D1 (Sheppard et al 1999Fig 22c) Alternatively if the Bryah and Padbury Groupswere deposited sometime between c 1945 and 1812 MaD1 could have developed during the c 18 Ga CapricornOrogeny due to north-northwest to south-southeastcompression (Figs 22 and 23) Further geochronologicalwork is required to establish the age of D1 and thedepositional age of the Bryah and Padbury Groups
In either case closure of the Bryah Basin took placeduring D1 with deposition of the Padbury Group in aretroarc foreland basin overlying the Bryah Group andpossibly the lsquofuturersquo Yarlarweelor gneiss complex(Fig 22b) D1 deacutecollements would have developedbetween the Bryah and Padbury Groups the futureYarlarweelor gneiss complex and the Peak Hill Schist(Figs 22b and 23a) Duplexes developed in the Peak HillSchist during D1 and it was detached from the MarymiaInlier (Fig 23b) In addition early D1 faults and foldsformed between and within the Bryah and PadburyGroups
The second deformation event D2 occurred during theCapricorn Orogeny Early in D2 approximately northwestto southeast compression caused further thickening of theBryah and Padbury Groups over the Yarlarweelor gneisscomplex destabilizing this piece of crust (Figs 22b and22c) The resulting increased pressure and temperaturemay have caused the underlying Archaean crust to startto melt This melt produced the c 1820 to c 1812 Mafelsic granitoid rocks (Occhipinti et al 1998a Sheppardand Swager 1999 Sheppard et al 1999) that intruded theupper parts of the Yarlarweelor gneiss complex as veinsand sheets (Sheppard and Swager 1999 Fig 22c) Asthese developed synchronously with the deformation (D2)they were commonly folded into upright steeply toshallowly plunging isoclinal to open folds These rockswere also metamorphosed at high grade during the D2deformation event Regionally this metamorphismcorresponds to M2
Padbury Group sedimentary rocks were meta-morphosed to medium grade along contact zones withthe Yarlarweelor gneiss complex during M2 This high- andmedium-grade metamorphism may have releasedfluid that moved through faults and shear zones and
31
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Figure 22 Schematic sections illustrating the proposed model of the structural development of the BryahndashPadburyGroup succession in the westa) Development of the Bryah Group pre-D1 over the Proto-Yarlarweelor gneiss complex and the northernmargin of the Yilgarn Craton in an extensional-rift settingb) Early- and syn-D1 deposition of the Padbury Group in a fold-and-thrust belt foreland-basin type settingover the Bryah Group Inversion of the Bryah rift-basin by possible reversal of D1 normal faultsDevelopment of D1 faults between the Bryah Group Padbury Group Yarlarweelor gneiss complex andYilgarn Cratonc) D2 to D3 local interleaving of the Bryah and Padbury Groups with the development of folds and faultsDeformation of the Bryah and Padbury Groups above basal detachments Early D1 faults refolded aboutD2 or D3 folds Formation of c 1810 Ma leucocratic granite locally associated with incipient minimum meltin the Archaean gneiss component of the Yarlarweelor gneiss complex Later at c 1800 Ma sheet-likeplutons developed particularly along the faulted boundaries between the Yarlarweelor gneiss complexand Bryah and Padbury Groups
Deposition of Padbury GroupEarly D
Development of fold and thrustbelt in D
1 1
Inversion of Bryah rift
1
Murchison Fault
Karalundi Formationequivalents Bryah Group
Hyaloclastites
Proto-Yarlarweelorgneiss complex
Post-rift phase
Thickening of supra-crustal succession over
Proto-Yarlarweelorgneiss complex
a)
b)
c)
v
SAO62 130300
Formation of c 1810 Ma leucocratic coarse-grained granitein Yarlarweelor gneiss complex (Sheppard et al 1999)
Deformation of the Yarlarweelor gneiss complex
NNW1
SSE
1
2 3
Early- and syn-D
Mafic and ultramaficvolcanic rocks
Early reversal of D normal faults some possible back thrustingof volcanic rocks below detachments cut by detachments
Folded c 1960 MaYamagee granite
Local plutonism into Proto-Yarlarweelor gneiss complex
at c 1960 Ma forming Yamageegranite of Sheppard and Swager (1999)
Pre-D extensionndashrift phase
D ndashD
Bryah Group
Proto-Yarlarweelorgneiss complex
Padbury Group
32
Pirajno et al
metasomatized M1 assemblages in the Bryah Group andPeak Hill Schist rocks during M2ndashD2 Elsewhere in theregion during D2 the Peak Hill Schist and Bryah andPadbury Group rocks were folded into tight to isoclinalupright folds with mainly easterly to northeasterly trends(Occhipinti et al 1998c) Post-D2 during D3 theYarlarweelor gneiss complex was uplifted and retrogressedto greenschist facies This uplift in a dextral strike-slipregime may have been accommodated by steeply dippingnormal faults between the Yarlarweelor gneiss complexand the Bryah and Padbury Groups (Figs 17 and 18) thathave now been inverted (Fig 24)
In the Peak Hill Schist subhorizontal D1 mylonitezones and rootless folds are refolded about an easterly oreast-northeasterly trending upright D2 antiform The domalshape of the Peak Hill Schist is an artefact of a northerlytrending upright D3 antiform refolding the D2 antiformThe Yarlarweelor gneiss complex apparently does notcontain D1 folds although shearing along basementndashcovercontacts between the Yarlarweelor gneiss complex and theBryah and Padbury Groups may have developed duringD1 (Fig 22b) The D2 fold-axial surfaces within the
Yarlarweelor gneiss complex parallel the arcuate faultedboundary with the Bryah and Padbury Group rocks Thischange in the trend of D2 may be explained in terms of afault-bend fold developed during dextral shearing(Occhipinti and Myers 1999) that may have accompanieduplift during D3
MineralizationThe mineral resources of the Peak Hill SchistBryah Group and Padbury Group are considerableconsidering the relatively small total area of thesebasins (about 6000 km2) These resources include goldmanganese iron ore talc and silver Pirajno andOcchipinti (1995) discussed the mineral potential of theBryah Basin and Pirajno and Preston (1998) described themineral deposits of the BryahndashPadbury region and PeakHill Schist Mineral production and defined resourceswithin these tectonic units as at 30 June 1999 arepresented in Tables 7 and 8 Known deposits andoccurrences are listed in Table 9
Figure 23 Schematic section illustrating the proposed model for the structural development of theBryahndashPadbury Group succession and the Peak Hill Schist a) Development of the BryahGroup in a rift setting pre-D1 over the Marymia Inlier (Yilgarn Craton) b) D1 closure of theBryah lsquoriftrsquo inversion of normal faults deposition of the Padbury Group and formation ofthe Peak Hill Schist
Future D fault
NNW SSE
Bryah Group
Basement
Proto-Peak Hill Schist
Pre-D extensionndashrift phase1
1Peak Hill Schist
D faults1
1
Rift closes Peak HillSchist develops as a
strongly duplexed packageof rock
Marymia Inlier
a)
b)
SAO63 150300
Padbury Group
Early- and syn-D
Mafic and ultramafic volcanic rocks
33
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The mineral deposits of the Peak Hill Schist andBryah and Padbury Groups include mesothermal-stylegold-only lodes volcanogenic massive sulfide (VMS)copperndashgold supergene-enriched manganese bandediron-formation iron ore and talc in metasomatizeddolomitic rocks The distribution of these mineral depositsis shown in Figures 25 and 26 and Plate 1
Gold depositsThe most important mineral deposits exploited to datehave been the mesothermal-style gold-only lodes all ofwhich are in the Peak Hill Schist and the Bryah andPadbury Groups If the area occupied by these groupsalone is taken into account (about 6000 km2) then theidentified contained gold per unit area is 125 kg goldkm2The mesothermal gold deposits including past and presentproducers include Peak Hill Jubilee and Mount Pleasantin the Peak Hill Schist Harmony Mikhaburra WembleyCashman and Ruby Well in the Bryah Group (Figs 25and 26) and Horseshoe Labouchere Nathans DeepSouth and Fortnum in the Padbury Group The Wilthorpedeposit is hosted in Upper Archaean granitic rocks whichare tectonically interleaved with rocks of the Bryah andPadbury Groups
The total gold produced is 595 t with total (producedplus remaining inferred indicated and measured)resources estimated at approximately 75 t of containedgold The Labouchere and Fortnum areas containthe regionrsquos largest pre-mining resource estimated as 333 tof contained gold at a grade of about 24 gt goldApproximately two-thirds (225 t) has been exploited
largely between 1989 and 1995 with the remainingresource (107 t) being in the Fortnum area Details of theLabouchere and Fortnum deposits can be found in Hannaand Ivey (1990) and Hill and Cranney (1990) respectivelyThe area around the Peak Hill opencut (includingRavelstone) has produced approximately 20 t of fine goldat an average grade of 4 gt gold more than half of whichhas been extracted in the last 13 years Remainingmeasured and indicated resources are estimated at about47 t of contained gold The Harmony deposit (NewBaxters Find) which was recently exhausted had totalpre-mining resources estimated at about 92 t with a gradeof 35 gt gold
The lode deposits are hosted in mylonitic schistmetasedimentary rocks metavolcanic rocks or along theircontact zones They are spatially associated with high-strain zones and hydrothermal alteration dominated bypyrite quartz muscovite biotite and alkali feldspars Themineralization is in ductile and brittlendashductile shears (egPeak Hill) and in discrete brittle fractures (eg Cashman)indicating a relationship of structural style with therheology of the host rocks The development of ductilebrittlendashductile and brittle structures (zones of highpermeability) was accompanied by infiltration ofhydrothermal fluids which produced alteration andmineralization The precise timing of the mineralizationis difficult to ascertain Windh (1992) suggested syn-D3but from field and petrological observations it is morelikely that circulation of mineralizing fluids occurredduring a continuum related to D1ndashD2 tectonism andmetamorphism under conditions of ductile or brittlendashductile regimes with perhaps some remobilization intobrittle structures occurring during D3 Lead isotope data
Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneisscomplex and then into the Bryah and Padbury Basins showing the possible present-day configuration of these units
Kerba FaultBangemall BasinFault boundary
YILGARNCRATON
vv
v
vv
v
vv
vv v
v
v
v vv v
vvv
vvv
vvv
vv
Errabiddy
Shear ZoneGascoyneComplex
Possible currenterosion level
SAO64 130300
NW SE
SeabrookndashMurchison Fault
v v
Bangemall Group
Yarlarweelor gneiss complex
Bryah and Padbury Group rocks
Cooinbar Fault
34
Pirajno et al
Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
_______________________ Production (P) _______________________ _______ Remaining resources (R) ________ TotalMining centre Ore Contained Alluvial Dollied Total Resource Ore Contained pre-miningor mine metal contained type metal resources
metal (P+R)(kt) (kg) (kg) (kg) (kg) (kt) (kg) (kg)
Pre-1986
Mount Fraser Mining Centre 09 24 27 13 288 ndash ndash ndash 288Mount Seabrook Mining Centre 17 383 ndash 02 385 ndash ndash ndash 385Ravelstone Mining Centre 49 1058 ndash 32 109 ndash ndash ndash 109Wilthorpe Mining Centre 01 15 ndash ndash 15 ndash ndash ndash 15Peak Hill sundry parcels 27 7706 889 139 8734 ndash ndash ndash 8734Peak Hill Mint deposits(a) ndash ndash 25 33 58 ndash ndash ndash 58Ruby Well Mining Centre 85 146 325 142 1927 ndash ndash ndash 1927Horseshoe Mining Centre 9049 2 9669 352 889 3 091 ndash ndash ndash 3 091Peak Hill Mining Centre 6217 8 200 367 628 8 2995 ndash ndash ndash 8 2995
1986 to 30 June 1999
Horseshoe Lights(b) mine 9059 3 7373 217 ndash 3 759 ndash ndash ndash 3 759Fortnum mine 5 832 15 6025 377 ndash 15 6402 MES + IND 2 221 7 542 23 1822
INF 991 3 194 3 194Labouchere mine 2 9108 6 9052 ndash ndash 6 9052 ndash ndash ndash 6 9052Mount Pleasant mine 1449 433 ndash ndash 433 ndash ndash ndash 433Peak Hill mine 6 5738 20 1266 908(c) ndash 20 2174 MES + IND 2 200 4 760 24 9774
Total 17 9128 59 0577 3487 1878 59 595 5 412 15 496 75 091
NOTES (a) Gold from the Peak Hill Mining Centre deposited at the Perth Mint(b) Horseshoe Lights also produced 261 675 t of copper concentrates containing 25803 kg of gold(c) Includes 625 kg of gold produced from retreated tailingsMES Measured resources IND Indicated resources INF Inferred resources
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
35
GSW
A R
eport 59G
eology and mineralization of the P
alaeoproterozoic Bryah and P
adbury Basins W
A
Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
_____ Production (P) to 300699 _____ __________________ Remaining resources (R) __________________ Total resource (P+R)Commodity Mine Ore or concentrate Contained metal Resource type Ore or concentrate Contained metal Contained metal
(t) (t) (t) (t) (t)
Copper and Cashman 7 11 ndash ndash ndash 11cupreous ore Peak Hill sundry 63 223 223
Horseshoe Lights 261 675 49 159 Indicated 2 080 000 22 897 72 056Inferred 3 340 000 22 879 22 879
Total 261 745 49 1824 5 420 000 45776 94 9584
Manganese Horseshoe 489 895 203 899 Measured + Indicated 80 000 21 000 224 899Inferred 205 000 100 000 100 000
Mount Fraser 228 108 Measured + Indicated 32 000 9 000 9 108Mount Padbury 7 319 3 498 Measured + Indicated 5 000 2 000 5 498Ravelstone (Peak Hill) 76 237 36 938 ndash ndash ndash 36 938Total 573 679 244 443 Measured + Indicated 117 000 32 000 276 443
Inferred 205 000 100 000 100 000
Iron Robinson Range ndash ndash Inferred 10 000 000 6 000 000 6 000 000
Talc Mount Seabrook ndash Livingstone ndash 540 416 Indicated ndash 1 470 000 2 010 416Inferred ndash 250 000 250 000
Total ndash 540 416 ndash 1 720 000 2 260 416
Silver Horseshoe Lights (post-1982) ndash 72 7194 kg ndash ndash ndash 72 7194 kg(by-product) Peak Hill general ndash 1182 kg ndash ndash ndash 1182 kg
(including Horseshoe pre-1983)Total ndash 72 8376 kg ndash ndash ndash 72 8376 kg
SOURCE Data are from the Western Australia Department of Minerals and Energyrsquos mines and mineral deposits information (MINEDEX) database
36
Pirajno et al
Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins (modified from Pirajnoand Preston 1998 see also Plate 1)
Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
Mine (M) AMG coordinates Principal Mineralization style Expression Ore minerals Relationshipprospect (P) or Easting Northing commodity to hostoccurrence (O)
Cashman (M) 662129 7126994 Gold Regolith enrichment Outcrop Gold Discordantand mesothermal lode
Durack (P) 670440 7150520 Gold Mesothermal lode Drill Gold pyrite Discordantintersections magnetite
Harmony (M) 664145 7161267 Gold Regolith enrichment Drill Gold chalcopyrite Discordantand primary intersections pyrrhotite scheelitemesothermal lode pentlandite pyrite
Heines Find (P) 682759 7145164 Gold Mesothermal lode Outcrop Gold Discordant
Horseshoe (P) 656994 7183734 Gold Eluvial Gold ndash
Horseshoe (P) 657579 7184413 Gold Eluvial Gold ndash
Horseshoe (P) 661219 7182977 Gold Eluvial Gold ndash
Horseshoe (P) Copperndashgold Multiple veins Outcrop Gold Discordant
Horseshoe 662648 7193894 Copperndashgold Supergene enrichment Gossan Chalcocite pyrite DiscordantLights (M) of VHMS chalcopyrite native
copper and gold
Jubilee (M) 671889 7165443 Gold Mesothermal lode Quartz vein Gold pyrite Discordant
Labouchere (M) 627730 7204710 Gold Mesothermal lode Not known Gold pyrite Discordant
Livingstone (M) 567540 7171032 Talc Replacement Outcrop Talc Discordant
Mikhaburra (P) 656252 7130396 Gold Multiple veins Outcrop Gold Discordant
Mount Pleasant (M) 674287 7162089 Gold Mesothermal lode Outcrop Gold pyrite Discordant
Mount Seabrook (M) 572631 7168338 Talc Replacement Outcrop Talc Discordant
Nathans Deep 631713 7198812 Gold Mesothermal lode Not known Gold pyrite DiscordantSouth (M)
Peak Hill (M) 672190 7163003 Gold Mesothermal lode Quartz vein Gold pyrite altaite Discordantchalcopyritebismuthotelluridemolybdenite magnetite
Ravelstone (M) 665734 7166777 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ravelstone (M) 669313 7166423 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Ruby Well area (M) 674665 7129915 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 672600 7124378 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 674142 7127027 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677928 7129727 Gold Eluvial ndash Gold ndash
Ruby Well area (P) 677408 7130112 Gold Eluvial ndash Gold ndash
St Crispin (P) 691358 7158940 Gold Mesothermal lode Outcrop Gold Discordant
Trevs Starlight (M) 636412 7198887 Gold Mesothermal lode Not known Gold pyrite Discordant
Unnamed (O) 611598 7168985 Variscite Not known Not known Variscite Discordant
Unnamed (O) 611909 7167084 Variscite Not known Not known Variscite Discordant
Unnamed (P) 656664 7185310 Manganese Supergene enrichment Outcrop Mn oxides Stratabound
Wembley (P) 663983 7149044 Gold Mesothermal lode Outcrop Gold Discordant
Wilgeena (M) 685369 7155622 Gold Mesothermal lode Outcrop Gold Discordant
Wilthorpe (M) 630414 7176521 Gold Mesothermal lode Outcrop Gold pyrite galena Discordantarsenopyrite
Yarlarweelor (M) 636723 7196423 Gold Mesothermal lode Not known Gold pyrite Discordant
37
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
MARYMIAINLIER
MARYMIAINLIER
Jenkin
FaultGROUPBANGEMALL
Murchison Fault
NARRYERGNEISS
TERRANE
Padbury Bryahand
Yerrida Basins
FMP100b 181099
1000 km
5
67 16
8
9
17
23
4
11
10
15
1213 14
19
18
21
20
1
GOODININLIER
YILGARNCRATON
YILGARN
CRATON
Goodin
Fault
118deg30 119deg30
Killara
Narracoota
Mt Padbury
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
Yandil
119deg30
Milgun30 km
Jamindi Three Rivers Marymia
PEAK HILLROBINSON
RANGE
Padbury Bryah Doolgunna Thaduna
Glengarry Mooloogool Mount Bartle
MerewetherYanganooGabanintha
119deg00
25deg30
26deg30
26deg00
25deg30
GLENGARRY
Milgun
Mesothermal Au AundashCu
Shear zone-hosted Cu
Epigenetic Pb
Supergene Mn
2 Jubilee
5 Labouchere
7 Fortnum group8 Horseshoe Lights9 Horseshoe gold
10 Wilthorpe11 Wembley
12 Mikhaburra13 Cashman14 Ruby Well
group (including Elsa)
16 Horseshoe magnagese17 Ravelstone18 Robinson Range BIF
(no specific locality)19 Thaduna20 PGE-bearing gossan21 Magellan
3 Mount Pleasant4 Harmony
(New Baxters Find)Fault
Geological boundary
Bouguer gravity anomaly
Peak Hill Schist
Karalundi FormationGR
OU
PB
RY
AH
Padbury Group
Horseshoe and Ravelstone Formations
schistmetabasaltic hyaloclastiteNarracoota Formation mafic and ultramafic
Archaean basement
Earaheedy Group
WindplainSubgroup
MooloogoolSubgroup
YE
RR
IDA
GR
OU
P
Maraloou Formationintercalated Killara and Maraloou FormationsDoolgunna and Thaduna Formationswith intercalated Killara FormationJuderina and Johnson Cairn Formations
Homestead
Bangemall Group
Microgabbro dyke
BryahPEAK HILL
1100 000 map sheet 1250 000 map sheet
Aeromagnetic lineament
6 Nathans Deep South
15 Mount Padbury ndash Mount Fraser
Volcanogenic massive sulfide
Shale-hosted stratabound sulfides
MINERALIZATION STYLE
MINERAL DEPOSITS
38
Pirajno et al
Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH
1100 000 map sheet (after Pirajno and Occhipinti 1998)
Ravelstone Formation
Karalundi Formation
Horseshoe Formation
Granitoid rock and gneiss
Narracoota Formation
10 km
040400
Yerrida Group
Bangemall Group
Earaheedy Group
Padbury Group
Bry
ah G
roup
Prospect
Producer
JubileeGroup
Peak Hill
Harmony
Wilgeena
Wembley
DurackWell
HeinesFind
Mikhaburra
CashmanGroup
Ruby WellGroup
Goodin Find
Ravelstone Group
(Hit or Miss)
St CrispinWilsons Find
25deg30
118deg
30
119deg
00
26deg00
Mar
ymia
Inlie
r mylonite
Syncline
Anticline
Overturned syncline
Peak Hill Schist
Thrust fault
Fault
Strike-slip fault
FMP162a
Supergene manganese deposit
Alluvialndasheluvial gold deposit
Mesothermal gold lodes
Mount Pleasant
39
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
(palaeo-isochrons) suggest that in the Bryah and PadburyBasins mineralization occurred between 192 and 17 Ga(Windh 1992 Thornett 1995) The results of lead isotopicstudies also indicate that the lead was derived from YilgarnCraton rocks (Dyer 1991 Windh 1992 Thornett 1995)although there is a suggestion that the lead from thePeak Hill deposit is similar to that from a galena in theMarymia gold deposit in the Marymia Inlier (McMillan1993)
The nature of the mineralizing fluids is poorlyconstrained Alteration assemblages at the Peak Hill andMount Pleasant deposits indicate that the ore fluids wereenriched in Fe K Na S B CO2 SiO2 and H2O (Thornett1995) Fluid inclusion studies of mineralized materialsfrom the Fortnum and Labouchere gold deposits (Dyer1991 Windh 1992) indicate that the ore fluids wererich in H2O and H2OndashCO2 with salinities of 7ndash12 wtand 5ndash17 wt NaCl equivalent respectively Micro-thermometric measurements (Dyer 1991 Windh 1992)indicate temperatures ranging from approximately 170degto 320degC
Peak Hill Jubilee and Mount Pleasantdeposits
Mine geologists subdivided the Peak Hill Jubilee andMount Pleasant lithologies into the Core sequence HoneyQuartzite Intermediate sequence Mine sequence MarkerQuartzite and Hangingwall sequence
The Core sequence is at the structural base and wellexposed in the Mount Pleasant opencut where it reachesa thickness of 55 m The contact with the Intermediatesequence is marked by the Honey Quartzite which is amylonite consisting of laminated or ribbon quartz TheCore sequence rocks have a mylonitic fabric and are madeup of quartzndashbiotitendashcarbonatendashmuscovite(ndashepidotendashhornblendendashgarnetndashmagnetitendashpyrite) locally withabundant very fine zircons and monazite in the biotite-richvarieties (Barrett 1989) At Mount Pleasant as mentionedabove graphitic schist is present near the top andassociated with a zone of chloritendashbiotite(ndashgarnet) schistwith albite porphyroblasts (Fig 27) containing inclusionsof monazite and zircon Geochemical discriminant plotsusing immobile elements suggest either a granitic (Nb SrLa and Ce) or maficndashintermediate (Ni Cr and Ti)protolith (Thornett 1995) Barrett (1989) on the otherhand proposed that much of the Core sequence could bederived from a sedimentary protolith The origin of thealbite porphyroblasts is uncertain Based on geochemistrypetrology and textural features Thornett (1995) advocateda combined hydrothermal ndash retrograde metamorphicorigin and compared the Peak Hill ndash Mount Pleasantalbites to those studied by Watkins (1983) in the Dalradianschists of Scotland Another possibility that could accountfor the presence of the albite porphyroblasts is lsquoreactionsofteningrsquo as proposed by Dixon and Williams (1983)These authors advanced the hypothesis supported bygeochemical and mineralogical data that mylonitizationof a quartzofeldspathic parent may be accompanied bymineralogical changes involving the breakdown ofplagioclase with release of Na2O and to a lesser extent
CaO and formation of muscovite This would result in theproduction of quartzndashmuscovite mylonites and sodium-rich fluids
The Intermediate sequence is discontinuous withlayers up to 2 m thick and is composed of a quartzndashmylonite-bearing white mica The Intermediate sequencelies above the Honey Quartzite has an estimated thicknessof between 200 and 400 m and forms the footwall to theMine sequence at Peak Hill and the hangingwall to theore zones at Mount Pleasant The Intermediate sequenceis dominantly quartzndashmuscovite schist with minorplagioclase biotite microcline carbonate and chloriteBarrett (1989) interpreted this rock as either a felsicporphyry or an arkose The lower part of the Intermediatesequence consists of mainly biotite schist with garnet andepidote Rocks of the Intermediate sequence exhibitmillimetre-scale metamorphic differentiation layeringwhich define a dominant S2 schistosity (Thornett 1995)This is interpreted by the present authors as a typicalmylonitic structure
The Mine sequence mostly found in drillholes ischaracterized by biotite ndash white mica(ndashchloritendashcarbonatendashamphibolendashgarnetndashalbite) schist and graphite schist(Fig 28) and may be 40 to 50 m thick Drillcore samplesof a hornblendendashplagioclasendashquartz rock (with garnetporphyroblasts) have been interpreted as an unalteredamphibolite (Barrett 1989 Thornett 1995)
The Marker Quartzite is a recrystallized quartzmylonite (lsquoMarker Chertrsquo of mine geologists)1 to 3 m thick at the top of the Mine sequenceOutcrops of Marker Quartzite exhibit radiating iron-oxidepseudomorphs after acicular crystals and iron-oxidepseudomorphs after porphyroblasts Windh (1992)identified these acicular crystals using the scanningelectron microscope as grunerite The porphyroblastpseudomorphs are possibly after garnet
The Hangingwall sequence can be up to 700 m thickand is made up of white mica ndash magnetite(ndashgarnetndashchlorite) mafic schist and metabasite The latter is locally
Figure 27 Albite porphyroblasts in mylonitic schist at theMount Pleasant deposit
40
Pirajno et al
garnetiferous and characterized by a metamorphic (andhydrothermal) assemblage containing variable amountsof hornblende plagioclase quartz garnet epidote andtitanite The metabasite is overlain by mylonitic schistcontaining mainly quartzndashplagioclasendashbiotite and locallyassociated with zones of albitendashmuscovite and garnetndashepidote (calc-silicate)
The Peak Hill Jubilee and Mount Pleasant depositswere studied by Barrett (1989) who based most of hiswork on drillcore samples and Thornett (1995) Theseauthors provided much of the information summarizedbelow augmented by data from this study The Peak HillJubilee and Mount Pleasant gold deposits are situated inthe west-northwestern portion of the Peak Hill Anticlineand hosted in the Peak Hill Schist (Figs 4ndash7 and 26) Inthe mine areas the rocks are intensely weathered to depthslocally exceeding 200 m Weathering products arepredominantly kaolinitic clays and iron oxyhydroxidesThis weathering is particularly well developed in zonesof hydrothermal alteration which in turn are related tohigh-strain zones the latter having facilitated percolationof meteoric waters Hydrothermal alteration is dominatedby sulfidation (pyrite) and alkali metasomatism (biotiteand albite) and contained within late-stage quartzndashcarbonate veins hosted in highly strained metabasites andquartz mylonites Other important alteration mineralsinclude iron-rich chlorite sericite garnet tourmalinedolomite and calcite In all about 20 t of gold has beenproduced
The Peak Hill mineralization was exploited in threeadjoining pits which from north to south are FivewaysPeak Hill Main and Mini In plan view (Fig 29) the entirePeak Hill mineralized system is contained within apackage of mylonitic schist (Mine sequence) at thefootwall of northerly trending and westerly dippingshear zones The mylonitic schist contains quartz podsveins lenses and stringers and locally graphitic quartzmylonite units (Marker Quartzite see below and Fig 30)The Mine sequence contains lenses of mafic rocks (egmetadolerite) The overall picture is one of a complex zoneof shearing and tectonic interleaving between rocks of the
FIVEWAYSPIT
MINIPIT
MAINPIT
100 m
sequence
Mine sequence
Intermediate sequence
Vein quartz
Marker Quartzite
Shear zone
Anticline
FMP160 271099
Hangingwall
Geology notmapped
Geology notmapped
N40
42
45
40
25
45
45 26
30
42
45
Fault42
Cleavage
Foliation
Figure 28 The Mine Sequence schist at the Peak Hill depositshowing biotite alteration the biotite is partlyretrogressed to chlorite plane polarized light
Figure 29 Schematic geological map of the Fiveways Mainand Mini opencuts Peak Hill deposit (after Thornett1995)
Figure 30 Peak Hill Mini opencut showing the ore-bearingmylonitic schist graphitic schist (dark bands) andMarker quartzite unit (above the upper graphiticschist)
41
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
Narracoota Formation and Peak Hill Schist Kinematicindicators (CndashS surfaces) indicate a thrust movement fromwest to east (Thornett 1995)
The main orebody has a westerly dip ranging from20deg to 50deg (averaging 35deg) and is hosted in rocks of theMine sequence High-grade zones can contain up to30ndash40 gt gold The ore zones are characterized bypervasive alteration consisting of chloritendashbiotitendashquartzndashcarbonatendashgraphite The principal ore minerals arepyrite chalcopyrite and gold Other ore minerals includealtaite tetrahedrite bismuthotelluride molybdenite andvarious bismuthndashleadndashtellurium compounds The goldmineralization is thought to have been emplaced in at leasttwo stages In the first stage gold mineralization wasemplaced along the contact between the Marker Quartziteand the Mine sequence (see below) During the secondstage cross-faults were formed with the gold beingredistributed or rearranged along these cross-faults
The Jubilee deposit was at first mined underground in1892 from a number of workings but the production isunknown In 1992 a small pit was excavated based onprobable reserves of approximately 50 000 t at 4 gt goldIn this pit gold mineralization is hosted in rocks of theHangingwall sequence and is in a complex quartzstockwork system emplaced along the margins of a 250 m-thick undeformed metabasite The gold is on both thehangingwall and footwall sides of the metabasite bodyTourmaline is present in the ore-bearing material Near theJubilee pit a northerly striking westerly dipping quartzvein almost perpendicular to the dominant foliation trendextends for about 200 m This vein was mined in the pastand contained maximum grades of approximately 30 gtgold
Mining at Mount Pleasant began at the turn of thecentury with the production of 8000 t of ore with anaverage grade of 9 gt gold Mining resumed in the 1980swhen about 145 000 t of ore was extracted with anaverage grade of 3 gt gold and 04 t of gold wasproduced The ore zones are nearly flat lying and wereemplaced in subparallel fashion one above the other Thedeeper northern zone is hosted by the Core sequence Goldis in quartzndashcarbonate veins associated with zones ofalbite (Fig 27) iron-rich chlorite sericite carbonate andpyrite alteration as well as zones of nearly flat lyinggraphitic schist (dip is 10deg to the south) The veins areeither vertical or of saddle-reef type lodged in anticlinalfolds
Harmony deposit
The Harmony (also known as New Baxters Find orContact) gold deposit is located approximately 10 km westof Peak Hill in a featureless area of no outcrops andcovered by colluvium lateritic duricrust and hardpanmaterial Details of the geology of the Harmony depositcan be found in Harper et al (1998) from whom the briefreview that follows is taken
The Harmony gold deposit consists of a subhorizontalsupergene zone hosted in ferruginous lateritic materials
(transported and residual regolith) a northeasterlytrending subvertical primary vein system and carbonate-bearing breccias Most of the ore is contained within thevein system which is hosted in rocks of the NarracootaFormation and at the contact between the Narracoota andRavelstone Formation (Fig 31) with lesser low-grademineralization in laterite The Harmony mineralization ishosted in a northwesterly plunging antiform (Enigmastructural zone) of a southwesterly dipping succession ofaltered mafic rocks at the top of the Narracoota Formationand within a shear zone along the contact with overlyingmetasedimentary rocks of the Ravelstone Formation Themineralized array of quartz veins become locally closelyspaced forming a stockwork that is commonly associatedwith high-grade ore Primary ore minerals include pyritewith gold inclusions pyrrhotite pentlandite chalcopyriteand scheelite The primary mineralization was enrichedby supergene processes
Hydrothermal alteration is characterized mainly bysilicification carbonitization and locally chloritizationHarper et al (1998) reported that mafic rocks show aparagenetic sequence of early albite and quartz followedby muscovite and chlorite Alteration in the metasedi-mentary rocks in the hangingwall is characterized mainlyby sericite and chlorite This primary alteration grades intozones of supergene alteration containing limonitekaolinite smectite group minerals and hematite Theweathered bedrock extends to approximately 60 m depthRegolith studies from drillholes have revealed anomalousAu W As Sb and Se in the ferruginous materials
Labouchere Nathans and Fortnumdeposits
In the northwestern part of the BryahndashPadbury Basin (onMILGUN) three distinct zones of gold mineralization havebeen recognized in high-strain zones associated with themargin of the Yarlarweerlor gneiss complex (Fig 25 andPlate 1) The Labouchere group (Labouchere and CentralValley deposits) and Nathans group (Labouchere-NathansNathan Bitter and Nathans Deep South deposits) had early
Figure 31 Diagrammatic cross section of the Harmony orezones (modified from Harper et al 1998)
50 m
FMP159
Supergene ore
Primary ore
Pit outline
50
100
150
200
Met
res
Mafic rocks
Formation)
Ultramafic rocks
Formation)(Ravelstone
(Narracoota
(NarracootaFormation)
Pelitic rocks
SW NE
211099
42
Pirajno et al
mining activity recorded from 1939 to the early 1940swith additional discoveries in the mid-1980s (Hanna andIvey 1990) The Fortnum deposits (Trevs StarlightTwilight Ricks Toms Hill Alton Eldorado Callies D39and Yarlarweelor) were discovered in the early 1980s (Hilland Cranney 1990)
Gold mineralization is structurally controlled in hostrocks of both the Bryah and Padbury Groups (Hill andCranney 1990) Windh (1992) concluded from detailedstudies at the Labouchere Nathans Deep South andFortnum mines that aqueous fluids of high temperatureand moderate salinity were responsible for mineralizationConstraints on temperature are derived from the lowerto middle greenschist-facies alteration assemblages(muscovitendashchloritendashalbite(ndashbiotite)) and fluid inclusiontrapping temperatures of up to 320degC Based on leadisotope work (galena from Nathans Deep South) Windh(1992) suggested that the syn-D4 gold mineralizationoccurred between 19 and 18 Ga The main features ofthe ore deposits are described below from the availableliterature
At the Labouchere-Nathans mine gold mineralizationis hosted in pyritic chert lenses or pods that lie withinmaficndashultramafic schist and along the contact withoverlying quartz wacke of the Labouchere FormationWindh (1992) described volcanic breccia (with high Niand Cr) with fuchsitic ultramafic and chert clasts similarto the reworked clastic rocks immediately overlying themaficndashultramafic volcanic rocks in the NarracootaFormation at the Fortnum mine The maficndashultramaficschist lies in the core of a southerly plunging anticlineand is here interpreted as part of the NarracootaFormation The Narracoota Formation ndash LabouchereFormation contact is interpreted as an early (D1ndashD2) faultor shear zone that was tightly folded during D3 Thestructure is crosscut and slightly offset by D4 faultstrending 270degndash290deg including a shear that forms thesouthern limit to the mineralization (Hanna and Ivey1990) Gold is associated with quartz veining and pyritein the altered chert with sideritendashmuscovitendashpyritealteration around the veins (Windh 1992) Productionfigures are only known for the combined output of theLabouchere-Nathans and Nathans Deep South opencuts(nearly 7 t of gold over five years Table 7)
At the Nathans group of workings the Nathan Bittershafts within the upper Labouchere Formation or lowerWilthorpe Formation have a recorded production of about8 kg over the period 1943ndash1950 (Swager and Myers1999) About 500 m to the north-northwest shallow shaftslie along the Kinders Fault between coarse and pebblyquartz wacke to the east and ultramafic schist of theNarracoota Formation to the west The Nathans DeepSouth mineralization lies approximately 1 km south-southeast of Nathan Bitter and was discovered in 1986(Hanna and Ivey 1990) The mineralization is hosted byfinely laminated chloritic shale interbedded with coarsequartz wacke and overlain by coarse units grading fromquartz-pebble conglomerate to quartzndashsericite shale Theentire succession is here described as part of the WilthorpeFormation including the chloritic shale which is mostlikely derived from mafic volcanic precursors (Hanna and
Ivey 1990 Windh 1992) Occhipinti et al (1998a)mapped similar units in the Wilthorpe Formation as aseparate member the Beatty Park Member The westerlyyounging succession contains a northndashsouth S3 foliationaxial planar to a few small-scale parasitic D3 foldsplunging steeply south and is overprinted by F4microfolds and kinks trending 290deg Gold mineralizationis within pyrite which has replaced finely bedded chloriteshale near crosscutting D4 quartzndashankerite veins Highestgrades are found adjacent to D4 faults These and otherstructural observations led Windh (1992) to infer a syn-D4 timing of mineralization However small quartz-veinnetworks possibly related to low-grade mineralization inthe overlying coarsely graded units are deformed by D4microfolding
The Fortnum gold mineralization is hosted by theNarracoota Formation which is truncated to the northagainst the Fortnum Fault and wedges out to the southThe package contains maficndashultramafic schist withoverlying reworked fragmental and volcaniclastic rocksincluding rocks with a supposed felsic volcanic derivationoverlain by the Ravelstone Formation (Hill and Cranney1990)
Mineralization at Trevs (and closely associatedorebodies including a recent discovery named Starlight)is hosted by quartz-vein systems in a westerly dippingsuccession of graded sericitic siltstone and coarse wackewith medium- to coarse-grained feldspar quartz and lithicfragments at least partly derived from the underlyingmaficndashultramafic volcanic rocks The Yarlarweelormineralization is hosted by ovoid lenses of jasperoidalchert within variably schistose maficndashultramafic volcanicrocks including interleaved fine tuffaceous and coarsefragmental layers (Hill and Cranney 1990) The chertlenses are within a westerly dipping reverse D3 shear zonecharacterized by quartzndashchloritendashsericite alteration Gold-bearing quartz(ndashpyrite) veins within the chert pods andwithin magnetite-bearing chlorite schist trend at 120deg dipsteeply north and are parallel to small sinistral D4 faults(D3 in Windh 1992) Windh (1992) also reported a minorset of (dextral) faults trending 070deg and crosscutting theD3 shear zones This may suggest a conjugate fault setrecording eastndashwest compression possibly late during D3rather than during north-northeastndashwest-southwest D4compression
Mining at the Fortnum group of workings from 1990to 1998 yielded 11 928 kg of gold from 4685 Mt of orewith an average recovered grade of 254 gt gold (Swagerand Myers 1999) Remaining measured and indicatedresources at Fortnum including Trevs and Starlightcontain an additional 17 970 kg of gold with a further4340 kg of gold estimated within inferred resources(Perilya Mines NL 1998)
Wembley deposit
The Wembley deposit is located approximately 18 kmsouthwest of Peak Hill and 25 km southeast of MurphyWell (from the Peak Hill road) Although rewarding(average grade of 175 gt gold) ore production was verysmall (less than 1800 t)
43
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
The Wembley mineralization is hosted in alteredmetabasite rocks within a major shear zone trending 120degThe mineralized zone strikes at 075deg and dips 63deg to thenorthwest A quartz vein near the old workings strikes at060deg and dips 54deg to the northwest Sedimentary units areintercalated with the volcanic rocks and consist ofturbiditic rocks (greywackendashshale) As at the Durackprospect (see below) quartz mylonite units trending120degndash140deg are within the metabasites
Wilgeena deposit
The Wilgeena (or Hit or Miss) gold mine area is located15 km southeast of the Peak Hill mine Production wasless than 15 000 t at an average grade of 26 gt gold
The deposit is within rocks of the Peak Hill Schist andmore specifically along the contact between the mylonitesand quartzndashsericite schist A northerly trending easterlydipping stoped-out ore lens was approximately 2 m thickThe mineralization is hosted in quartzndashmuscovitendashmagnetite schist Grab samples from the old excavationsreturned values ranging from 3 to 14 gt gold (Mountford1984) Whitfield (1987) estimated inferred resources asapproximately 600 000 t at 244 gt gold
Durack St Crispin and Heines Findprospects
The Durack prospect lies about 12 km south of Peak Hillalong and immediately west of the Old Peak Hill telegraphroad This gold deposit is blind being covered by soil andlateritic material and consists of primary mineralizationand a supergene mineralized zone The prospect wasidentified by a soil anomaly containing up to 100 ppb gold(Sabminco Annual Report 1994)
The prospect area is underlain by rocks ofthe Narracoota Formation which include metabasite(medium- to coarse-grained metabasalts) and maficpyroclastic rocks Thin magnetite-bearing chert bands(possibly chemical sediments) intercalated within themetabasites define a broad synclinal structure A numberof mylonite zones trending 120degndash125deg cut across theNarracoota Formation rocks and contain most of theprimary mineralization Grades intersected during drillingare in the order of 15 gt gold over widths of 4 to 6 m
The primary mineralization is contained within quartzndashsulfide veins and stockworks hosted by altered metabasiterocks The mineralized area is about 14 km long and200 m wide Hydrothermal alteration is pervasive andconsists of quartz chlorite biotite and iron-rich carbonate(ankerite) Pyrite is present as fine disseminations andveinlets Selvages of silicandashpyritendashcarbonate surround themineralized zones
The supergene mineralization at the Durack prospectis controlled by subhorizontal redox fronts within theregolith material Supergene enrichment shows grades ofup to 12 gt gold over an interval of about 5 m In somecases the redox-front-related mineralization developed upto 45 m on each side of the primary zone
The St Crispin prospect is situated 20 km east-southeast of Peak Hill The mineralization is along a north-northwesterly trending structure and hosted in sericite(ndashgraphite) schist of the Peak Hill Schist Quartz veins arepresent in the schists and may host the mineralization
The Heines Find prospect is located 20 km south-southeast of Peak Hill Mineralization can be traced forabout 6 km along the easterly trending contact betweenrocks of the Narracoota Formation and the HeinesMember of the Wilthorpe Formation This contact has adip of 80deg to the north and is sheared In this area theNarracoota Formation consists of strongly deformedpillow lavas and chlorite schist The sedimentary rocks ofthe overlying Heines Member include a basal polymicticconglomerate
Ruby Well group
The Ruby Well area includes a number of mineral leasesfrom which gold has been produced either from surfacematerials or from hard rock (02 t Table 7) The RubyWell leases lie on the northern side of the Great NorthernHighway about 80 km from Meekatharra and 4ndash5 km eastof the Peak Hill turn-off
The area is underlain by the Narracoota Doolgunnaand Karalundi Formations The Hard To Find Ruby Anneand Lucky Call deposits within mafic schist of theNarracoota Formation were exploited between 1912 and1917 Most of the current production (figures notavailable) is from a number of dry-blowing workingssurrounding these old mines
Mikhaburra deposit
The old Mikhaburra gold mine (also known as HoldensFind) is in Narracoota Formation volcanic rocks in thesouthwestern part of BRYAH (Fig 25) The recordedproduction of the Mikhaburra mine is about 226 kg ofgold (MacLeod 1970) The mineralization is associatedwith a system of auriferous quartz veins emplaced alonga shear zone trending about 130deg to 150deg and dipping 68degto the southwest The volcanic rocks include mainlychlorite schist A quartz vein with a strike of 120deg and dipof 58deg southwest lies to the west of the old workings Thisvein is about 1 m wide and locally displays a laminatedstructure
Wilthorpe deposit
The Wilthorpe deposit is hosted by granitic rocks of theDespair Granite (Fig 32) which contains xenoliths ofmafic material Gold mineralization is confined to a zonecontaining quartz veins and flanked by bleached andsilicified wallrocks The ore zone is hydrothermallyaltered with assemblages of chloritendashsericitendashbiotite andquartzndashmuscovitendashbiotitendashtourmaline flanked by near-pervasive silicification In addition to gold the mineralizedveins also contain pyrite galena arsenopyrite andchalcopyrite The wallrock granite has a cataclastic textureand consists of quartz and feldspar lsquoeyesrsquo surrounded bya network of granulated quartz and sericite
44
Pirajno et al
Cashman deposit
The Cashman area on BRYAH includes a number of smallmineral occurrences and deposits containing copperand copperndashgold The old Cashman copper mine isapproximately 250 m from the gold workings In 1917 thismine produced about 7 t of copper ore grading 165copper (Marston 1979) The copper mineralizationconsists of a metre-wide cupriferous limonite vein with astrike of 042deg and a shallow dip to the northwest Oreminerals are chrysocolla and malachite as disseminationsand veinlets (Marston 1979)
In 1937 there was a small production of gold ore fromquartz veins In 1986ndash87 the gold potential of theCashman area was reassessed and on the basis of thiswork a small opencut was excavated from which 8000 tof ore material was produced and stockpiled (Whitfield1987) Gold mineralization is hosted in quartz veins withinmetabasaltic hyaloclastite A 01 m-thick quartz vein in thepit has a strike of 115deg and dips 35deg to the northeast Atand near the surface supergene enrichment is present ina horizon about 30 m wide and dipping about 20deg to thenorth (Whitfield 1987)
Volcanogenic copperndashgolddepositsThe Horseshoe Lights copperndashgold deposit on JAMINDI hasproduced nearly 9 t of gold of which almost 26 t wasrecovered from the copper concentrate operation between1988 and 1993 (Table 7) The Horseshoe Lights depositis hosted in felsic schist of the Narracoota Formation(Bryah Group) The mineralization consists of massivesulfides overlying and flanked by disseminated andstringer sulfides Ore minerals are mainly chalcocitepyrite and chalcopyrite Native copper is also present(Parker and Brown 1990) The host rocks are mylonitizedchlorite schist kaolinitendashsericite schist and quartzndashsericiteschist The geometry of the ore zones (massive sulfidesand stringer zone) alteration patterns (silicificationsericitic and chloritic alteration) predominantly felsiccomposition of the host rocks and metal association (CundashAundashAgndashPbndashZn) suggest that the deposit was originally ofthe volcanogenic massive sulfide type but subsequentlyenriched by supergene processes Average grades havebeen about 8 gt gold about 10 copper and 300 ppmsilver The stringer mineralization is of low gradeaveraging between 02 and 03 gt gold Production ceasedin 1994 Remaining resources (Table 8) are of low-grademineralization
Supergene manganese depositsManganese mineralization is part of a historicallyimportant manganese field first recognized in 1905 withdeposits in the Mount Fraser Mount Padbury Ravelstone(Peak Hill) and Horseshoe areas The manganesemineralization is of supergene origin and related tomanganiferous and hematitic shale units and BIF of theHorseshoe Formation (Bryah Group) as well as units ofthe Padbury Group The chief ore minerals are pyrolusiteand cryptomelane The ore is lateritic locally pisolitic innature and in places forms caps overlying the primarymanganese-rich sedimentary material In places notablyat Horseshoe there is evidence to suggest that someenrichment may have taken place in a palaeodrainagechannel lake or swamp environment (MacLeod 1970)In the Ravelstone area just north of the Peak Hill golddeposit the manganese supergene enrichment appears tohave a structural control
The Horseshoe area has been the main producingregion with production from two deposits 2 and 3 kmnorth and northwest of the Horseshoe townsite (Plate 1)The main production period was from 1948 to 1971 when490 000 t was mined (Table 8) all but 5000 t of whichwas classified as metallurgical-grade ore The enrichedzone was 3 to 45 m thick and typically extended overlengths of 400 to 500 m The North deposit averaged 30 min width whereas the South deposit was fan shapedopening from 20 to 300 m wide at its maximum extentOre consisted of mixed manganese and iron oxides withhighly variable manganese and iron contents Gradesprogressively decreased from 42 to 35ndash38 after 1966
There are several small deposits in the Mount Fraserndash Mount Padbury area about 30 km west of Peak Hill
Figure 32 The west wall of the Wilthorpe opencut showingthe contact between biotitendashsericitendashquartz schistand deformed Despair Granite
45
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
They contain patches of high-grade ore within largedeposits of ferruginous manganese material Productionof high-grade ore occurred sporadically since 1949 andamounted to 7547 t at grades in excess of 46 manganeseA third mining operation commenced at the Millidie (orElsa) deposit in the early 1990s but this has notprogressed to a full-scale commercial operation High-grade mineralization in the area is estimated to containmeasured plus indicated resources of approximately11 000 t of manganese (Table 8)
In the Ravelstone area immediately north-northwestof Peak Hill mining occurred between 1956 and 1964producing 76 237 t of ore at 70ndash90 manganese oxide(Table 8) Remainng measured and indicated resources areestimated as 132 000 t of contained metal (Table 8)Manganese production at Ravelstone was from easterlystriking orebodies reaching lengths of up to 100 m andwidths of 30 m but commonly small and narrow Detailedexamination of one specimen of ore revealed that it wascomposed mainly of cryptomelane and accessorypyrolusite A partial geochemical analysis of the samesample provided the following results 064 wt SiO2465 wt Al2O3 0011 wt P 033 wt MgO 268 wtK2O 7038 wt MnO 119 wt Fe 005 ppm Au650 ppm Co 31 ppm Cu 53 ppm Ni 20 ppm Pb and98 ppm Zn
The manganese ore is characterized by high bariumabundances (3000 ppm to 30 at Mount Fraser3000 ppm to 1 at Horseshoe and 3943 to 9000 ppm atRavelstone)
Iron oreThe Robinson Range Formation (Padbury Group) containsunits of banded iron-formation (Fig 2) within which areareas of supergene enrichment of hematite and goethiteThese constitute demonstrated (pre-JORC code) iron-oreresources estimated at approximately 10 Mt with gradesin excess of 60 iron (Table 8) Enrichment is above twoBIF units approximately 100 m thick separated by ahematitic shale horizon Iron grades of the primary BIFvary between 20 and 50 Hematite and hematitendashgoethite surficial enrichment contains grades in excess of50 iron as determined from the sampling of one ofabout 200 small pods of potentially ore grade material(Sofoulis 1970)
TalcTalc in the Mount Seabrook ndash Livingstone ndash Trillbarregion is present within metasedimentary and meta-volcanic rocks and minor mafic and ultramafic rocks Talcis hosted in metasomatized dolomite orebodies (Plate 1)as a series of steeply plunging lenses (Lipple 1990) TheMount Seabrook deposit was discovered in 1965 and hasproduced over 540 000 t of talc mostly of cosmetic gradebetween 1973 and 1995 Indicated and inferred resourcesredefined at Mount Seabrook and Livingstone amount to172 Mt of ore with a significantly greater potentialbecause the orebodies are open along strike
DiscussionThe Horseshoe Lights VMS-type copperndashgold deposit issyn-volcanic and pre-orogenic All other deposits are ofepigenetic origin and syn- to post-orogenic
Figure 33 schematically depicts a simple regionalmodel of ore genesis for the epigenetic mineral depositsin the BryahndashPadbury ndash Peak Hill Schist (BPPS) tectono-metamorphic domain and the adjacent Yerrida Basin TheYerrida Basin and BPPS domain were tectonicallyjuxtaposed along the northeasterly trending Goodin FaultDeformation which affected the BPPS domain wastransmitted across the Goodin Fault for a few kilometresinto the Yerrida Basin This deformation becomes weakerfrom the Goodin Fault eastward The BPPS domain wassubjected to metamorphism (upper to lower greenschistfacies) At least two phases of metamorphism arerecognized a prograde phase overprinted by a retrogradephase Geothermometry and geobarometry studies inthe area around Peak Hill by Thornett (1995)indicated temperatures of around 500ndash620degC for peakprograde metamorphism and 65 to 7 kbar for minimumpressure of the prograde assemblages The timing ofthis metamorphism is probably linked to the collisionbetween the Pilbara and Yilgarn Cratons (see Tectonicmodel and conclusions) which is postulated to haveoccurred between 1820 and 1800 Ma (Occhipinti et al1999)
A genetic model proposed by Pirajno and Preston(1998) envisages that fluids were generated during phasesof dynamic and thermal metamorphism in the BPPSdomain and that these fluids were largely responsible forthe deposition of mesothermal gold-only and shear-zone-hosted deposits The paragenesis of the alterationassemblages associated with the mesothermal depositsand textural relationships suggest that metamorphism
Figure 33 Sketch illustrating a conceptual model for the originof precious and base metal epigenetic deposits inthe BryahndashPadbury and Yerrida Basins (after Pirajnoand Preston 1998)
FMP71a
Bryah and Padbury Groups
Mooloogool Subgroup
Windplain Subgroup
Direction of fluid movement
170300
Fault Cleavagedevelopment
ARCHAEANBASEMENT
NARRYERTERRANE
Area of Au deposition
Collisionzone
Cleavagelate epigeneticmineralisation
Metamorphism
Basin fluids
YERRIDA
and deformation
Goo
din
Faul
t
development
BRYAHndashPADBURYBASINS BASIN
NW SE
46
Pirajno et al
and mineralization were broadly contemporaneousalthough alteration was in most cases from peak toretrograde metamorphism Exceptions to this are localizedzones of sodium metasomatism (albite and arfvedsonite)which overprint the retrograde assemblages This sodiummetasomatism may be related to central zones ofhigher temperatures within the mineralized structuresOne possible explanation for the widespread sodiummetasomatism is granite magmatism however there is noevidence in either the Bryah or the Padbury Basin ofgranitic plutons intruding the volcano-sedimentarysuccessions Therefore a possible role of graniticmagmatism as one of the heat and metal sources for thehydrothermal solutions based on our present knowledgeis excluded
Hydrothermal solutions responsible for the emplace-ment of mesothermal lodes are considered to be generatedin tectonically active regions and are associated withcompressional and extensional tectonics (Kerrich andCassidy 1994) The mesothermal-style gold-only lodesof the BPPS domain were formed in a compressionalsetting characterized by thin-skinned thrusting associatedwith prograde and retrograde mineral assemblages(Pirajno 1996) Dyer (1991) concluded that the hydro-thermal mineralization in the LaboucherendashFortnumarea was generated by the mixing of two fluids ofdifferent density and salinity Deeply sourced hot salineCO2-bearing fluids were mixed with cooler less salinenear-surface aqueous fluids The available evidencepoints to the conclusion that the mineralizing fluids wereat first generated during compression and dehydrationand moved along ductile to brittle structures Duringsubsequent phases meteoric fluids would have infiltratedalong the same structures and mixed with the hottermetamorphic solutions The whole mechanism couldhave been repeated again in the next phase of compressionand extension leading to multiphase ore genesis processesin which the latest phase leaves the most detect-able imprint There is no obvious link with magmaticactivity
Other metal deposits in the BryahndashPadbury Basin aresupergene manganese and iron ore (Pirajno and Preston1998) The timing of the weathering event that led to thesupergene enrichment of the manganese and iron ores isnot known although it may be possible that the warm andhumid climate during the middle Tertiary (Cockbain andHocking 1990) played a major role in the genesis of thissupergene mineralization
Tectonic model andconclusions
Gee (1979) Hynes and Gee (1986) Windh (1992) andGee and Grey (1993) interpreted the geodynamicevolution of the lsquoGlengarry Basinrsquo as defined by Gee andGrey (1993) in terms of an ensialic or intracontinentalbasin Tyler and Thorne (1990) Myers (1993) Martin(1994) and Myers et al (1996) proposed models in whichthe former lsquoGlengarry Basinrsquo would have formed in aback-arc setting during the convergence of the Pilbara andYilgarn Cratons between 2000 and 1800 Ma
In the light of the re-interpretation of the formerlsquoGlengarry Basinrsquo into the Bryah Padbury and YerridaBasins some modification of the above tectonic schemesis necessary Lack of sufficient geochronological datahowever poses the problem of the precise timing ofevents This lack of information must be taken intoaccount when modelling basin tectonics Pirajno (1996)and Pirajno et al (1998b) suggested two models for thegeodynamic evolution of the BryahndashPadbury and YerridaBasins 1) the basins were formed during convergence andsubsequent collision in a back-arcndashforeland basin settingin which these basins were opened and infilled duringsouthward subduction of oceanic crust (extensional backarc) and subsequently overlain by sediments in a newlydeveloped foreland basin (syn-collisional) and 2) thebasins were formed at the time of the oblique collisionbetween the Pilbara and Yilgarn Cratons as pull-apartstructures in a strike-slip setting with transitions fromextensional (transtension) to compressional (transpression)regimes
In this study we propose a model whereby the BryahBasin was formed as a back-arc rift with a component ofrifting along the Yilgarn continental margin a kind ofproto-oceanic rift comparable to that of the present-day Guayamas Basin in the Gulf of California (Lonsdaleand Becker 1985) The Padbury Basin developed as aforeland basin on top of the Bryah Basin during theoblique collision of the Pilbara and Yilgarn Cratons Ourmodel is shown in Figure 34 in which two stages areschematically depicted and briefly discussed below
The Bryah Basin was formed by processes of back-arc opening during subduction of oceanic crust beneaththe northern margin of the Yilgarn Craton approximately
Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins withinthe context of the Capricorn Orogen (modified from Myers 1990 1993 and Myers et al 1996)a) At about 1960ndash1950 Ma development of Andean-type magmatic arc on a microcontinental active margin back-arcrifting and spreading with creation of oceanic crust (dominantly high-Mg and high-Fe tholeiite associated withsubvolcanic peridotitic cumulates representing future maficndashultramafic schist of the Narracoota Formation) anderuption of basaltic hyaloclastites probably from the same source as the maficndashultramafic material occurs on passivemargin of Yilgarn Craton Insets schematically show geochemical signatures of these volcanic rocks (see text fordetails)b) Capricorn Orogeny involved collision between the Pilbara and Yilgarn Cratons with formation of fold-and-thrustbelts on both northern and southern sides of orogen and thrusting of oceanic crust over hyaloclastite and margin ofYilgarn Craton The thrust separating oceanic crust material from hyaloclastite is represented by the Murchison Fault(see Plate 1) Chondrite-normalized REE patterns for metabasites and hyaloclastites of the Narracoota Formation areshown in the insets
47
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
N S
N S
Marymia In
lier
YILGARN
Backarc riftMicrocontinent
andvolcanic arc
Seafloor
Seafloor
Oceaniccrust
lt 1960ndash1950 Ma
PILBARA
PILBARAYILGARN
Fold-and-thrustbelt
PadburyBasin Bryah Basin
1820ndash1800 Ma
Present-dayBryahndashPadbury
area
Lithosphere
FMP376 170300
4000
3000
2000
1000
00 21 3
FeOMgO FeOMgO Ni Cr
1
2
0
3
0 1 2
La Eu Lu
Sam
ple
chon
drite
100
10
16
Sam
ple
chon
drite
100
10
2La Eu Lu
2
Cr
(ppm
)
TiO
(
)
TiO x1002
Mid-oc
ean r
idge
2
Clastic rocks
Padbury Group
Archaean basement
Metabasic rocksof Narracoota FormationHyaloclastites(Narracoota Formation)
Karalundi Formation
Oceanic crust
a)
b)
48
Pirajno et al
between 1960 and 1950 Ma (Occhipinti et al 1999Fig 34a) Myers (1993) speculated that a southwardoceanic subduction system with a south-facing Andean-type magmatic arc had developed off the northern passivemargin of the Yilgarn Craton Remnants of arc magmaticsuites have not been found but may be buried under theMesoproterozoic Bangemall Basin Back-arc rifting alsoaffected the northern margin of the Yilgarn Craton whererift propagation is postulated to have progressivelyadvanced from west to east through a succession ofcrustalndashlithospheric thinning rupture and grabenformation In this model the Marymia Inlier is a remnantof a rift shoulder (Fig 34a)
The closing of the ocean between the Pilbara andYilgarn Cratons was followed by the oblique collisionbetween the rifted passive margin on the Pilbara side aninferred active magmatic arc and the passive northernmargin of the Yilgarn Craton Closure of the interveningocean (1820ndash1800 Ma) resulted in inversion of the Bryahback-arc rift and thrusting of oceanic crust (nowNarracoota Formation) over the Yilgarn Cratonrsquos northernmargin (Fig 34b) During and following this collisionevent the southern side of the Pilbara was tectonicallysliced by major thrusts whereas most of the tectonictransport of the inferred magmatic and oceanic crust rockswas towards the south (Myers 1993)
High-Mg tholeiitic rocks with pillow structuressheeted dykes the Trillbar layered complex sea-floor metasomatism and trace and rare-earth elementgeochemistry support the oceanic crust model for theorigin of the mafic and ultramafic schist of the NarracootaFormation The hyaloclastites on the other hand wereerupted in shallow waters and locally characterized byexplosive activity and have mixed and overlappinggeochemical signatures with the mafic schist This featurecan be interpreted as suggesting a more continentalenvironment of emplacement and therefore were emplacedon Yilgarn crust (Fig 34a) In contrast to the maficndashultramafic schist the hyaloclastites are relativelytectonically undeformed Their contact with the maficndashultramafic schist is along the Murchison Fault (Plate 1)We conclude that the Murchison Fault represents atectonic boundary between these two components of theNarracoota Formation and that oceanic crust material(precursors of the maficndashultramafic schist) were thrustover the continental hyaloclastites during the CapricornOrogeny as shown in Figure 34b The suggested Gulf ofCalifornia-type palaeoenvironmental setting with thefuture Marymia Inlier as one of the rift shoulders(analogous to the California peninsula) is shown inFigure 34a
The absence of volcanic rocks of intermediate(andesitic) compositions suggests that the NarracootaFormation metabasites were not formed in a subduction-related volcanic-arc setting as proposed by Myers et al(1996) However we concur with Sun (1997) that theboninitic component in the chemistry of the metabasites(see inset of Fig 34 and Figs 12ndash15) needs explanationWe suggest that these boninitic characteristics of theNarracoota Formation can be compared to the boninitesof the Koh Ophiolite in New Caledonia (Meffre et al
1996) which are considered to have formed in a back-arc spreading centre
The overall high MgO and low TiO2 abundancesdepleted REE and low LaYb ratios of the NarracootaFormation are also consistent with the origin of theNarracoota Formation metabasites from a mantle plume(Pirajno et al 1998a)
The Padbury Basin was interpreted by Martin (1994)as a retroarc foreland basin recording the collision of theYilgarn and Pilbara Cratons During and followingcollision between 1820 and 1800 Ma (Occhipinti et al1999) back-arc volcanism ceased and a foreland basindeveloped on top of the back-arc succession (BryahGroup) This basin was filled by siliciclastic rocks only(Padbury Group) During continued regional compressionthe BryahndashPadbury Basin developed into a fold-and-thustbelt and was partly thrust over the Yerrida Basin alongthe Goodin Fault
In summary the convergence between the ArchaeanPilbara and Yilgarn Cratons resulted in progressivecompressional deformation that affected the Bryah andPadbury Groups as a coherent package At least fourgroups of structures are recognized in the regionaldeformation of the volcano-sedimentary succession andtheir reworked basement (ie Yarlarweelor GneissComplex) This same deformation and associatedmetamorphism was responsible for the mesothermal gold-only lodes of the Bryah and Padbury Basins
AcknowledgementsWe acknowledge the contribution of colleagues whoparticipated in the Glengarry mapping program JohnMyers N G Adamides and P G Le Blanc SmithRichard Davy first introduced the senior author to the areaWe are also grateful to the local pastoral community fortheir hospitality The geological staff of LabouchereFortnum Peak Hill and Harmony gold mines are thankedfor sharing their knowledge with us
49
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
References
ADAMIDES N G 1998 Geology of the Doolgunna 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BAGAS L B 1998 Geology of the Marymia 1100 000 sheetWestern Australia Geological Survey 1100 000 Geological SeriesExplanatory Notes 23p
BARNETT J C 1975 Some probable Lower Proterozoic sedimentsin the Mount Padbury area Western Australia Geological SurveyAnnual Report 1974 p 52ndash54
BARRETT F 1989 A study of wallrock alteration associated withgold mineralization mdash Peak Hill and Mt Pleasant area WesternAustralia Geological Survey M-series Item 7706 A41555(unpublished)
BRADLEY J J FAULKNER J A and SANDERS A J 1997Geochemical mapping of the Robinson Range 1250 000 sheetWestern Australia Geological Survey 1250 000 RegolithGeochemistry Series Explanatory Notes 57p
BREITKOPF J H and MAIDEN K J 1988 Tectonic setting of theMatchless Belt pyritic copper deposits Namibia EconomicGeology v 83 p 710ndash723
BUNTING J A COMMANDER D P and GEE R D 1977Preliminary synthesis of Lower Proterozoic stratigraphy andstructure adjacent to the northern margin of the Yilgarn BlockWestern Australia Geological Survey Annual Report 1976p 43ndash48
BURKE K C KIDD W S F TURCOTTE L DEWEY J FMOUGINIS-MARK P J PARMENTIER E M SENGORA M and TAPPONIER P E 1981 Tectonics of basalticvolcanism in Basaltic volcanism on the terrestrial planets HoustonLunar and Planetary Institute p 803ndash898
COCKBAIN A E and HOCKING R M 1990 Regolith in Geologyand mineral resources of Western Australia Western AustraliaGeological Survey Memoir 3 p 591ndash602
CRAWFORD R A FAULKNER J A SANDERS A J LEWISJ D and GOZZARD J R 1996 Geochemical mapping ofthe Glengarry 1250 000 sheet Western Australia GeologicalSurvey 1250 000 Regolith Geochemistry Series Explanatory Notes57p
DAVY R PIRAJNO F SANDERS A J and MORRIS P A1999 Regolith geochemical mapping as an adjunct to geologicalmapping and exploration examples from three contiguousProterozoic basins in Western Australia Journal of GeochemicalExploration v 66 p 37ndash53
DIXON J and WILLIAMS G 1983 Reaction softening in mylonitesfrom the Arnaboll thrust Sutherland Scottish Journal of Geologyv 19 p 157ndash168
DUNCAN A R 1987 The Karoo igneous province mdash a problemarea for inferring tectonic setting from basalt geochemistry Journalof Volcanology and Geothermal Research v 32 p 13ndash34
DYER F L 1991 The nature and origin of gold mineralization atthe Fortnum Nathans and Labouchere deposits Glengarry BasinWestern Australia University of Western Australia BSc Honoursthesis (unpublished)
ELIAS M 1982 Belele WA Western Australia Geological Survey1250 000 Geological Series Explanatory Notes 21p
ELIAS M BUNTING J A and WHARTON P H 1982 GlengarryWA Western Australia Geological Survey 1250 000 GeologicalSeries Explanatory Notes 27p
ELIAS M and WILLIAMS S J 1980 Robinson Range WAWestern Australia Geological Survey 1250 000 Geological SeriesExplanatory Notes 32p
FISHER R V and SCHMINCKE H-U 1984 Pyroclastic rocksBerlin Springer-Verlag 472p
GEE R D 1979 The geology of the Peak Hill area Western AustraliaGeological Survey Annual Report 1978 p 55ndash62
GEE R D 1987 Peak Hill WA (2nd edition) Western AustraliaGeological Survey 1250 000 Geological Series Explanatory Notes24p
GEE R D 1990 Nabberu Basin in Geology and mineral resourcesof Western Australia Western Australia Geological SurveyMemoir 3 p 202ndash210
GEE R D and GREY K 1993 Proterozoic rocks on the Glengarry1250 000 sheet mdash stratigraphy structure and stromatolitebiostratigraphy Western Australia Geological Survey Report 4130p
HALL W D M and GOODE A D T 1978 The Early ProterozoicNabberu Basin and associated iron formations of Western AustraliaPrecambrian Research v 7 p 129ndash184
HANNA J P and IVEY M E 1990 Labouchere and Deep Southgold deposits in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 667ndash670
HARPER M HILL M G RENTON J I and THORNETTS E 1998 Gold deposits of the Peak Hill area WesternAustralia in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 81ndash87
HILL A D and CRANNEY P J 1990 Fortnum golddeposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 665ndash666
HYNES A and GEE R D 1986 Geological setting andpetrochemistry of the Narracoota Volcanics Capricorn OrogenWestern Australia Precambrian Research v 31 p 107ndash132
JENSEN L S 1976 A new cation plot for classifying subalkalicvolcanic rocks Canada Ontario Division of Mines MP 66 22p
KERRICH R and CASSIDY K F 1994 Temporal relationships oflode gold mineralization to accretion magmatism metamorphismand deformation mdash Archaean to present a review Ore GeologyReviews v 9 p 263ndash310
LE MAITRE R W 1989 A classification of igneous rocksand glossary of terms Oxford Blackwell Scientific Publications193p
50
Pirajno et al
LEWIS J D 1971 The geology of some carbonate intrusions in theMount Fraser area Peak Hill Goldfield Western Australia WesternAustralia Geological Survey Annual Report 1970 p 50ndash56
LIPPLE S L 1990 Talc in Geology and mineral resources of WesternAustralia Western Australia Geological Survey Memoir 3p 678ndash679
LISTER G S and SNOKE A W 1984 SndashC mylonites Journal ofStructural Geology v 6 p 617ndash638
LONSDALE P and BECKER K 1985 Hydrothermal plumes hotsprings and conductive heat flow in the southern trough ofGuayamas Basin Earth and Planetary Science Letters v 73p 211ndash225
LUCAS S B STERN R A SYME E C REILLY B A andTHOMAS D J 1996 Intraoceanic tectonics and the developmentof continental crust 192 ndash 184 Ga evolution of the Flin Flon beltCanada Geological Society of America Bulletin 108 p 602ndash629
MacLEOD W N 1970 Peak Hill WA (1st edition) WesternAustralia Geological Survey 1250 000 Geological SeriesExplanatory Notes 21p
MARSHAK S TINKHAM D ALKMIN F BRUECKNER Hand BORNHORST T 1997 Dome-and-keel provinces formedduring Palaeoproterozoic orogenic collapse mdash core complexesdiapirs or neither examples from the Quadrilatero Ferrifero andthe Penkean orogen Geology v 25 p 415ndash418
MARSTON R J 1979 Copper mineralization in Western AustraliaWestern Australia Geological Survey Bulletin 13 208p
MARTIN D McB 1992 Turbidite facies and depositionalenvironment of the Precambrian Labouchere Formation PadburyGroup Western Australia Geological Society of AustraliaAbstracts 32 p 168ndash170
MARTIN D McB 1994 Sedimentology sequence stratigraphy andtectonic setting of a Palaeoproterozoic turbidite complex LowerPadbury Group Western Australia University of Western AustraliaPhD thesis (unpublished)
MARTIN D McB 1998 Lithostratigraphy and structure of thePalaeoproterozoic Padbury Group Milgun 1100 000 sheet WesternAustralia Western Australia Geological Survey Report 62 57p
McDONALD I R 1994 Final Report on the Glengarry nickel projectES502 and E51384 Western Australia Geological SurveyM-series Item 7706 A41555 (unpublished)
McMILLAN N M 1993 Structure metamorphism alteration andtiming of gold mineralisation at Marymia Gold Project in theMarymia Dome in An international conference on crustal evolutionmetallogeny and exploration of the Eastern Goldfields ExtendedAbstracts compiled by P R WILLIAMS and J A HALDANEAustralian Geological Survey Organisation Record 199354p 243ndash244
McPHIE J DOYLE M and ALLEN R 1993 Volcanic texturesHobart Tasmanian Government Printing Office 198p
MEFFRE S AITCHISON J C and CRAWFORD A J 1996Geochemical and tectonic significance of boninites and tholeiitesfrom the Koh Ophiolite New Caledonia Tectonics v 15p 67ndash83
MOUNTFORD B R 1984 Preliminary geological report onProspecting Licences 52104 and 52105 Mt Padbury area WesternAustralia Western Australia Geological Survey M-series Item3688 A16393 (unpublished)
MYERS J S 1989 Thrust sheets on the southern foreland of theCapricorn Orogen Robinson Range Western Australia WesternAustralia Geological Survey Report 26 Professional Papersp 127ndash130
MYERS J S 1990 Capricorn Orogen in Geology and mineralresources of Western Australia Western Australia GeologicalSurvey Memoir 3 p 197ndash198
MYERS J S 1993 Precambrian history of the West Australian cratonand adjacent orogens Annual Reviews of Earth and PlanetaryScience v 21 p 453ndash485
MYERS J S SHAW R D and TYLER I M 1996 Tectonicevolution of Proterozoic Australia Tectonics v 15 p 1431ndash1446
NELSON D R 1997 Compilation of SHRIMP UndashPb zircongeochronology data 1996 Western Australia Geological SurveyRecord 19972 189p
NELSON D R 1998 Compilation of SHRIMP UndashPb zircongeochronology data 1997 Western Australia Geological SurveyRecord 19982 242p
OrsquoNIONS R K PANKHURST R J and GRONVOLD K 1976Nature and development of basalt magma sources beneath Icelandand the Reykjanes ridge Journal of Petrology v 17 p 315ndash338
OCCHIPINTI S A GREY K PIRAJNO F ADAMIDES N GBAGAS L DAWES P and LE BLANC SMITH G 1997Stratigraphic revision of Palaeoproterozoic rocks of the YerridaBryah and Padbury Basins (former Glengarry Basin) WesternAustralia Geological Survey Record 19973 57p
OCCHIPINTI S A and MYERS J S 1999 Geology of the Moorarie1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 20p
OCCHIPINTI S A MYERS J S and SWAGER C P 1998aGeology of the Padbury 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes29p
OCCHIPINTI S A SHEPPARD S NELSON D R MYERS J Sand TYLER I M 1998b Syntectonic granite in the southernmargin of the Palaeoproterozoic Capricorn Orogen WesternAustralia Australian Journal of Earth Sciences v 45 p 509ndash512
OCCHIPINTI S A SHEPPARD S and TYLER I M 1999Palaeoproterozoic tectonic evolution of the southern margin of theCapricorn Orogen Western Australia Last Conference of theMillenium Halls Gap WA Abstract volume p 173ndash174
OCCHIPINTI S A SWAGER C P and PIRAJNO F 1998cStructuralndashmetamorphic evolution of the Palaeoproterozoic Bryahand Padbury Groups during the Capricorn Orogeny WesternAustralia Precambrian Research v 90 p 141ndash158
PARKER T W H and BROWN T 1990 Horseshoe goldndashcopperndashsilver deposit in Geology of the mineral deposits of Australia andPapua New Guinea Volume 1 edited by F E HUGHESAustralasian Institute of Mining and Metallurgy Monograph 14p 671ndash675
PEARCE J A ERNEWEIN M BLOOMER S H PARSON L MMURTON B J and JOHNSON L E 1995 Geochemistry ofLau Basin volcanic rocks influence of ridge segmentation and arcproximity Geological Society Special Publication v 81p 53ndash75
PEARCE T H GORMAN B E and BIRKETT T C 1977 Therelationship between major element chemistry and tectonicenvironment of basic and intermediate volcanic rocks Earth andPlanetary Science Letters v 36 p 121ndash132
PERILYA MINES NL 1998 Annual report for the year ending30 June 1998 60p
PETERS S G 1993 Polygenetic meacutelange in the Hodgkinsongoldfield Northern Tasman Orogenic Zone Australian Journal ofEarth Sciences v 40 p 115ndash129
PIRAJNO F 1996 Models for the geodynamic evolution of thePalaeoproterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1995ndash96 p 96ndash103
PIRAJNO F and ADAMIDES N G 2000 Geology andmineralization of the Palaeoproterozoic Yerrida Basin WesternAustralia Western Australia Geological Survey Report 60 43p
51
GSWA Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins WA
PIRAJNO F and ADAMIDES N G 1998 Geology of the Thaduna1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 24p
PIRAJNO F ADAMIDES N G and FERDINANDO D D 1998aGeology of the Glengarry 1100 000 sheet Western AustraliaGeological Survey 1100 000 Geological Series Explanatory Notes16p
PIRAJNO F ADAMIDES N G OCCHIPINTI S A SWAGERC P and BAGAS L 1995a Geology and tectonic evolution ofthe early Proterozoic Glengarry Basin Western Australia WesternAustralia Geological Survey Annual Review 1994ndash95 p 71ndash80
PIRAJNO F BAGAS L SWAGER C P OCCHIPINTI S A andADAMIDES N G 1996 A reappraisal of the stratigraphy of theGlengarry Basin Western Australia Western Australia GeologicalSurvey Annual Review 1995ndash96 p 81ndash87
PIRAJNO F and DAVY R 1996 Mafic volcanism in thePalaeoproterozoic Glengarry Basin Western Australia andimplications for its tectonic evolution Geological Society ofAustralia Abstracts no 41 p 343
PIRAJNO F and OCCHIPINTI S A 1995 Base metal potential ofthe Palaeoproterozoic Glengarry and Bryah Basins WesternAustralia Recent developments in base metal geology andexploration Australian Institute of Geoscientists Bulletin 16p 51ndash56
PIRAJNO F and OCCHIPINTI S A 1998 Geology of the Bryah1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 41p
PIRAJNO F OCCHIPINTI S LE BLANC SMITH G andADAMIDES N G 1995b Pillow lavas in the Peak Hill terranesWestern Australia Geological Survey Annual Review 1993ndash94p 63ndash66
PIRAJNO F OCCHIPINTI S A and SWAGER C P 1998bGeology and tectonic evolution of the Palaeoproterozoic BryahPadbury and Yerrida Basins (formerly Glengarry Basin) WesternAustralia Precambrian Research v 90 p 119ndash140
PIRAJNO F and PRESTON W A 1998 Mineral deposits of thePadbury Bryah and Yerrida Basins in Geology of Australian andPapua New Guinean mineral deposits edited by D A BERKMANand D H MACKENZIE Australasian Institute of Mining andMetallurgy Monograph 22 p 63ndash69
RAYMOND L A 1984a Classification of meacutelanges GeologicalSociety of America Special Paper 198 p 7ndash20
RAYMOND L A 1984b Meacutelanges their nature origin andsignificance Geological Society of America Special Paper 198170p
ROLLINSON H R 1993 Using geochemical data evaluationpresentation interpretation Singapore Longman 352p
SABMINCO ANNUAL REPORT 1994 Annual report on miningleases M52202ndash203 vol 1 2 and 3 Western Australia GeologicalSurvey M-series Item 8967 A42856 (unpublished)
SCHILLING J-G 1982 Galapagos hot spot ndash spreading centersystem 1 Spatial petrological and geochemical variations (83degWndash101degW) Journal of Geophysical Research v 87p 5593ndash5610
SCHILLING J-G MEYER P S and KINGSLEY R H 1982Evolution of the Iceland hot spot Nature v 296 p 313ndash320
SHEPPARD S and SWAGER C P 1999 Geology of the Marquis1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 21p
SHEPPARD S OCCHIPINTI S A NELSON D and TYLERI M 1999 Granites of the southern Capricorn Orogen WesternAustralia Geological Society of Australia Abstracts no 56p44-46
SOFOULIS J 1970 Iron deposits of the Robinson Range Peak HillGoldfield WA Western Australia Geological Survey Record19706 10p
SPEAR F S 1993 Metamorphic phase equilibria and pressurendashtemperaturendashtime paths Mineralogical Society of AmericaMonograph p 799
STERN R A SYME E C and LUCAS S B 1995 Geochemistryof 19 Ga MORB and OIB-like basalts from the Amisk collageFlin Flon belt Canada evidence for an intra-oceanic originGeochimica et Cosmochimica Acta v 59 p 3131ndash3154
SUBRAMANYA A G FAULKNER J A SANDERS A J andGOZZARD J R 1995 Geochemical mapping of the Peak Hill1250 000 sheet Western Australia Geological Survey 1250 000Regolith Geochemistry Series Explanatory Notes 59p
SUN S-S 1982 Chemical composition and origin of the Earthrsquosprimitive mantle Geochimica et Cosmochimica Acta v 46p 179ndash192
SUN S-S 1997 Chemical and isotopic features of Palaeoproterozoicmafic igneous rocks of Australia implications for tectonic processesAustralian Geological Survey Organisation Record 19974p 119ndash122
SWAGER C P and MYERS J S 1999 Geology of the Milgun1100 000 sheet Western Australia Geological Survey 1100 000Geological Series Explanatory Notes 27p
THORNETT S E 1995 The nature origin and timing of goldmineralization in Proterozoic rocks of the Peak Hill District WAUniversity of Western Australia MSc thesis (unpublished)
TYLER I M 1999 Palaeoproterozoic orogeny in Western AustraliaGeological Society of Australia Abstracts no 56 p 47ndash49
TYLER I M PIRAJNO F BAGAS L MYERS J S andPRESTON W A 1998 The geology and mineral deposits of theProterozoic in Western Australia Australian Geological SurveyOrganisation Journal of Geology and Geophysics v 17p 223ndash244
TYLER I M and THORNE A M 1990 The northern margin ofthe Capricorn Orogen Western Australia mdash an example of anEarly Proterozoic collision zone Journal of Structural Geologyv 12 p 685ndash701
WANG P and GLOVER L 1992 A tectonic test of the mostcommonly used geochemical discriminant diagrams and patternsEarth Science Reviews v 33 p 111ndash131
WATKINS K P 1983 Petrogenesis of Dalradian albite porphyroblastschists Journal of the Geological Society of London v 140p 601ndash618
WHITFIELD G B 1987 Wilgeena gold mine Progress report MS52111 and 112 Western Australia Geological Survey M-seriesItem 5862 A28194 (unpublished)
WINDH J 1992 Tectonic evolution and metallogenesis of the EarlyProterozoic Glengarry Basin Western Australia University ofWestern Australia PhD thesis (unpublished)
52
Pirajno et al
Appendix
Gazetteer of localities
Locality AMG coordinateEasting Northing
5 Mile Well 616500 7158100Beatty Park Bore 632200 7163500Cashman opencut 662129 7126994Dandy Well 646400 7188740Despair Bore 625300 7169600Durack prospect 670440 7150520Durack Well 671600 7143000Fortnum mine 636372 7197627Friday Pool 558620 7178625Harmony (New Baxters Find) opencut 664145 7161267Heines Find prospect 682759 7145164Horseshoe Lights opencut 662648 7193894Horseshoe Mn mine 656990 7186510Horseshoe Au prospect 661219 7182977Jubilee mine 671889 7165443Labouchere mine 627730 7204710Livingstone mine 567540 7171032Lucky Call prospect (Ruby Well group) 676747 7127188Mikhaburra (Holdens Find) opencut 656252 7130396Millidie (Elsa) deposit 643000 7160000Mount Fraser 639200 7163300Mount Labouchere 630360 7212620Mount Padbury 627400 7164100Mount Padbury mine 635100 7165100Mount Pleasant opencut 674287 7161900Mount Seabrook mine 572631 7168338Nathan Bitter mine 631100 7199820Nathans Deep South mine 631713 7198812Peak Hill opencut 672190 7163003Peak Hill townsite 673000 7163150Randell Bore 688000 7145200Ravelstone Group 669000 7167500Ravelstone opencut (Mn) 665734 7166777Ravelstone opencut (Mn) 669313 7166423Ruby Duffer Well 675290 7136000Ruby Well group 677900 7129700St Crispin prospect 691358 7158940Tank Well 675400 7147000Top Dimble Well 616600 7167600Trevs (and Starlight) opencut 636412 7198887Trillbar Homestead 576023 7170846Wembley mine 663983 7149044Wilgeena (Hit or Miss) mine 685369 7155622Wilthorpe mine 630414 7176521Yarlarweelor opencut 636723 7196423
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting
The Palaeoproterozoic Bryah and Padbury Basins are part of the Capricorn Orogen a collisionzone between the Archaean Pilbara and Yilgarn Cratons The Bryah Basin contains maficndashultramafic igneous rocks turbidites and chemical sedimentary rocks formed duringback-arc sea-floor spreading and rifting on the northern margin of the Yilgarn Cratonat or near a mid-oceanic ridge The Padbury Basin contains a succession ofclastic and chemical sedimentary rocks and was formed on top of theBryah Basin as a foreland structure resulting from either thec 1800 Ma oblique collision of the Pilbara and YilgarnCratons (Capricorn Orogeny) or the c 2000 Ma collisionof the Glenburgh Terrane and the Yilgarn Craton (GlenburghOrogeny) Important mineral deposits include orogenicgold-only lode deposits copperndashgold volcanogenic massivesulfides sedimentary and lateritic manganese and iron oreThe origin of the gold mineralization is related tometamorphism and deformation linked to the CapricornOrogeny at c 18 Ga The formation of other deposits isrelated to pre-orogenic syngenetic processes
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone (08) 9222 3459 Fax (08) 9222 3444wwwdmewagovau
Wandery
Creek
Wandery
Gum
Creek
Beda
burra
Easter
nCr
eek
Dim
ble
Dimble
Cree
k
Mt Fr
aser
Creek
Creek
Mt Fraser
Millidie CreekMURCHISONRIVER
MURCHISON
RIVER
GASCOYNE
RIVE
R
GASCOYNE
RIVER
Ck
Cree
k
Creek
Beatty Park B (abd)
Reefer W(abd)
YARLAR
WEELOR
MILGUN
ROAD
MEEKATHARRA
ROAD
ASHBURTON DOWNS
TrillbarYarlarweelor
ROADTRILLBAR
Mt Padbury
Yd
Yd
Yd
Yd
Yd Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd
MT CLARE
MEEKATHARRA
ROAD
Bryah
Narracoota
Old Peak Hill (ruin)
Mikhaburra
Yd
Yd
Yd
Yd
(ruin)Bilyuin Hotel
Yulga Jinna Community
Doolgunna
Yd
YdYd
Yd
THADUNACOPPER MINE ROAD
Yd
Karalundi
Yd
Yd
Yd
Yd
Bryah
Yd
Mikhaburra
Yarla
rwee
lor H
omes
tead
44
km
Milgun Homestead 4 km
Milgun Homestead 72 km
Meekatharra 108 km
Meekatharra 53 km
Mooloog
ool Ho
mestead
35 km
Diamond
Well
Homest
ead 68
km
Neds
Creek
Homest
ead 33
km
Kumerina Homestead 98 km
Three Rivers Homestead 42 km
MT LABOUCHERE
MT ARAPILES
CM 15
MT BEASLEY
MT SEABROOK
TALB
OT
DIVIDE
RED HILL
722 m
Yd
Yd
Yd
Yds
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
Yd
YdYd Yd
Yd
Yd
Yd
Yd
628 m
MT PADBURYMT FRASER
MT MAITLAND
R O B I N S O N
591 m
695 m
799 m
Yd
Yd
GREAT
NORTH
ERN
HIGH
WAY
HILL
THRE
E RIVER
S
ROAD
PEAK
MEEKATHARRA
ROAD
ROAD
PEAK HILL
R A N G E
Peak Hill
MC 14
NOONYEREENA HILL
MT LEAKE
MC 13
MC 12
MC 11
ASHBURTON DOWNS
core yard
602 m
605 m
640 m
Peak Hill
Yd
Earrie W Daulby W
Jilly Jilly W
Outcamp W (abd)
Watt W
Curly W
B
6 Mile B4 Corners W
Laurel W (abd)Bull W
Labouchere W
Sam W
Duffey W
Horseshoe W
Dandy W (PD)(abd)
Carlyon B (PD)
Kinder B (PD)
Vacation B
Garret W
Kylie B
Camel B
W (abd)Billarra W
Bull Paddock WAlarm B
Carlyon RH (PD)
Yaddyarra W
Mowara BGullgogo B
Horseshoe No 2 W (PD)Horseshoe No 1 W (PD)
Stink W (PD)
Crain B
Windalah B
Yandinhah W
Coomballey B
No 1 B
4 Corners W (abd)
Cement Tank W (abd)
Cork Tree B
Southern Cross W3 Corners B
Thompson B (abd)
W (abd)
Tommy B
Seabrook W17 Mile W (abd)
Midnight B
Gidgie WW (abd)
Snake W Dry W
Black Hill W
Minniarra W
Top Minniarra W
Doherty W
The Hut W
W
Red Hill W
Randall W
Dooley W
Walebie W
Mandora B
Babbawiri Pool
Winja B
WHWH
PBedaburra P
Friday P
Kerba P
S
Wandery P
W
Valley B
Quartz B
House WSouthern Cross W
P
Peak Hill B Shed W
Boundary B
No 3 W
McPherson B
Pinnacle B
WH
Mt Leake B
Hill B
Jack W
W
Mt Leake B
John B
No 2 B
Cow Hole B
WH
Red B
WH
No 6 W
Marck W
No 11 W
Limestone W
Dummy B
No 1 B
No 8 B
D
Government W
Central B
Gale W
W
West W
No 6 B
Ealgareengunna WH
Noonyereena P
Beefwood T
Narracoota B
WH
WH
Railway B
Meek W32 Mile W (Govt)
32 Mile W
Ruby W
Ruby South W
W (abd)
Scotty W
Ord W
Little Mill B
Killarney W
West WMillie W
D
Ord W (abd)
W(abd)
Eastern Stock W No 8(abd)
Gigbywabby W (PD)(abd)
No1 W
Paddy B (abd)
Kelly BRelief B
Top Dimble W
Despair B
Boundary B (PD)
B (abd)
Padbury W
Govt W (abd)
Bottom Dimble WHaystack W
Wandarrie W
Middle B
W
WW
W
No 3 B
Fish Pond B
Wooly Paddock B
5 Mile W
Knox W
Sleepy Hollow W (abd)
Old Homestead WB
Widespread W
W
Kennedy W
W
Deep W
Ross B
Gibbywabby WDandy W (PD)
Brunsden W
17 Mile WBrown Creek B (abd)
7 Mile BDavid W
17 Mile B (PD)
Lefeuvre W
Mick W
W (abd)
WH
WHWH
WH
WH
WH WH
S
Gum W (abd)
Wilthorpe W (PD)
1 Mile W
Bullgullan B
Wongawar B
Jinglegunna W
No 13 B
Orchard W
Fraser WW
Sorenson B
Central B
Tank W (abd)Bitter W (abd)
Murphy W
Trudgeon W
Moore W Spelling W
Randell B
Deadhorse W (abd) McLean W
Bore Hole BOHara W
Murchison W (abd)
McCarthy W2 Tank W (abd)
Hill W
Telegraph W
Cashman B (abd)
Ruby Centre W
White WW
McCann W (abd)
Holden W
Gum W
McDonald W
Don BNo 2 BNo 1 B
Bull W
D
D
DD
Gum Well P
Malleah P
Fremanga P
Yallaginda W (abd)
No 7 B (abd)
Stalley W (abd)
Durack W
No 26 W (abd)
Ruby Duffer W (abd)
WHs
WHs
WHWH
WH
WHWH
WH
P
PP
P
P
P
P
P
P
P
P
P
Ruby W (abd)
Narracoota W (abd)
WH S
P
B W
D T
(abd) (PD)
Cheroona W(abd)
Ti Tree B
56ocircocircocircocircYacute E 58 62 64 66 68 72
icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
56ocircocircocircocircYacute E 58 60 62 64 66 68 70 72 icirc40ocircocircocircocircYacute E
icirc12ocircocircocircocircYacute N
14
16
18
20
icirc22ocircocircocircocircYacute N
74ocircocircocircocircYacute E7060
0frac34 0frac34 30Agrave
1frac34
Chalba Fault
CoolinbarFault
Fortnum Fault
BillaraFault
Wilthorpe
Fault
KindersFault
GoodinFault
Goodi
n
Fault
Murchison
Fault
Goodin
Fault
Padbury
Syncline
Millidie
Syncline
Peak HillAnticline
Robinso
n
Synclin
e
HorseshoeAnticline
3
33
3 3
3
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E
E
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E
E
E
E 118961
118956
142851
88YacuteEcirc168
igraveAnd
TrevsYacuteYacuteYacuteStarlight
Yarlarweelor
Horseshoe
NathanDeep
Mt Seabrook
Labouchere
Wilthorpe
Wilgeena
Wembley
Livingstone
Harmony
Jubilee
Peak HillMt Pleasant
St Crispin
Durack
Heines Find
Mikhaburra
Cashman
Horseshoe Lights
Horseshoe
Yarlarweelor
Mn
T
MnMn
CuAu
Cu
Au
Mn
T
CuAu
HOLDENS
BAXTER
RAVELSTONE
PEAK HILL
HORSESHOE
HOLDENS
Ruby Well
Fortnum
Fortnum
M U R C H I S O N M I N E R A L F I E L D
M E E K A T H A R R A D I S T R I C T
P E A K H I L L M I N E R A L F I E L D
Goodin Fault Murchison Fault
Goodin Fault Murchison Fault
thrust
latera
l ramp
Billara Fault Kinders Fault
NARRYER
TERRANE
YILGARN
CRATON
Goodin F
ault
GOODIN
INLIER
Jenkin
Fault
Fault
Goodin
MARYMIA
INLIER
thrust ramp
Robinson Syncline
Peak Hill Anticline
Peak Hill Anticline
Horseshoe Anticline Millidie Syncline
Yarlarweelor gneiss belt
Marymia Inlier
40
MOUNT LEAKE FORMATION quartz arenite
DESPAIR GRANITE foliated to locally massive coarse-grained biotite granite late Archaean
30 km
Bangemall Group
Earaheedy Group
Padbury Group
Bryah Group
Mooloogool SubgroupDoolgunna_Thaduna Formations
Windplain Subgroup
Geological boundary
Fault
Finlayson Member quartz arenite
117frac34Yacute30Agrave
25frac34Yacute00Agrave
45Agrave118frac34Yacute00Agrave 15Agrave 30Agrave 45Agrave 119frac34Yacute00Agrave 15Agrave 119frac34Yacute30Agrave
25frac34Yacute00Agrave
15Agrave
30Agrave
45Agrave
26frac34Yacute00Agrave
26frac34Yacute10Agrave
119frac34Yacute30Agrave15Agrave119frac34Yacute00Agrave45Agrave15Agrave 30Agrave
118frac34Yacute00Agrave45Agrave117frac34Yacute30Agrave
26frac34Yacute10Agrave
26frac34Yacute00Agrave
45Agrave
30Agrave
15Agrave
Proterozoic granite
Q TR S
SEA LEVEL
5 km
11 km
F G
SEA LEVEL
5 km
11 km
L M O
SEA LEVEL
5 km
11 km
N
J K
SEA LEVEL
5 km
10 km
10 km
SEA LEVEL
5 km
H I
Archaean granitoid rock and greenstone
YerridaGroup
Maraloou_Killara Formations
SEA LEVEL
5 km
10 km
C D E
SEA LEVEL
5 km
10 km
A B
MILLIDIE CREEK FORMATION sandstone and shale minor granular iron-formation
ROBINSON RANGE FORMATION ferruginous shale and siltstone minor banded iron-formation
Beatty Park Member chloritic siltstone sandstone and breccia numerous mafic volcanic fragments
Heines Member quartz wacke siltstone and shale with minor polymictic conglomerate
LABOUCHERE FORMATION quartz wacke and siltstone local quartz pebble conglomerate layers turbiditic
KARALUNDI FORMATION sandstone with minor shale and conglomerate
JOHNSON CAIRN FORMATION siltstone and shale minor sandstone
JUDERINA FORMATION quartz wacke siltstone quartz arenite and quartz pebble conglomerate
PEAK HILL SCHIST quartz muscovite schist mylonitic schist and phyllonite
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS REPORT 59 PLATE 1
2
Trillbar Complexwith local magmatic layering well-preserved
interleaved foliated and metamorphosed basalt gabbro microgabbro pyroxenite and serpentinized peridotite
HORSESHOE FORMATION ferruginous chloritic shale and quartzEcircfeldspar wacke partly manganiferous andcalcareous minor iron-formation and chert
BANGEMALL
EARAHEEDY
PADBURYBASIN
BASINBRYAH
YERRIDABASIN
WILTHORPE FORMATION quartz pebble to boulder conglomerate predominant vein quartz clasts and some chert quartz wackeand granitoid rock clasts quartz wacke and finely bedded siltstone locally chloritic graded beds
1 2 3 4
C
58
78
75
20
15
SHEET INDEX
intruded by granite during the Capricorn Orogeny
High-grade gneissic granite and granite foliated derived predominantly from biotite monzogranite with numerouslenses of supracrustal rocks early middle and late Archaean components overprinted by structures and
NARRACOOTA FORMATION metabasalt and maficEcircultramafic schist locally pillowed with interflow sedimentary layers
Capr
icorn
Oro
geny
Mar
ymia
Inlie
r_re
work
ed d
uring
the
met
amor
phism
_Ca
prico
rn O
roge
nyup
per g
reen
schist to
lowe
r am
phib
olite
facie
s
gree
nsto
ne b
eltM
ount
Mai
tland
2672YacuteucircYacute3
lt1996YacuteucircYacute35
High-grade granitic gneiss derived predominantly from biotite monzogranite with numerous lenses ofsupracrustal rocks early middle and late Archaean components includes Palaeoproterozoicgranite sheets and dykes extensively deformed during Capricorn Orogeny
SCHEMATIC TECTONIC RELATIONSHIPS
BANGEMALL BASIN
1600 Ma and youngerc
EARAHEEDY BASIN
2000 Ma and youngercBRYAH BASIN
2000 Mac
YERRIDA BASIN
2200 Ma and youngerc
YILGARN CRATON
2600 Ma and olderc
PADBURY BASINyounger than 2000 Ma
BASIN
BASIN
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igraveAnf
ntildeg
ntildegn
ntildeng
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igravePmi
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igravePrg
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igraveAk
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ethp
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igravePriigravePr
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ntildegMla
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WA
NT
SA
NSW
Vic
Qld
Tas
ACT
GEOLO
G IC A L SUR VEY
WE
ST
E R N A U S T R AL
IA
GEOLOGICAL SURVEY OF
WESTERN AUSTRALIA
DAVID BLIGHT DIRECTOR
DEPARTMENT OF MINERALS
AND ENERGY
L C RANFORD DIRECTOR GENERAL
GOVERNMENT OF WESTERN AUSTRALIA
HON NORMAN MOORE MLC
MINISTER FOR MINES
Bangemall Group undivided
Mafic dyke interpreted from aeromagnetic data + positive anomaly - negative anomaly
Granite includes muscovite-bearing leucogranite and pegmatite
Padbury Group undivided metamorphosed and variably foliated metasedimentary rocks
Iron-formation and chert
Banded iron-formation minor ferruginous sandstone and shale
Bedded dolomite and dolomitic siltstone
Granular iron-formation
Banded iron-formation
Banded iron-formation and ferruginous chert
Quartz arenite minor interleaved quartz wacke and siltstone
Iron-formation and quartzEcircmagnetite(Ecircstilpnomelane) schist garnetiferous white chert in lenses
lithic wacke and siltstone turbiditic
Chert
Felsic schist derived from felsic volcanic and volcaniclastic rockDolerite in sills and dykesBasaltic hyaloclastiteMetaperidotite and picrite ultramafic schistBasaltic vent brecciaJasperoidal chert
Quartz mylonite
Foliated to mylonitic and massive granitoid rock
Amphibolite
Banded iron-formation
Granite with minor greenstone locally overprinted by structures formed during Capricorn Orogeny
Basalt ultramafic rock dolerite felsic schist banded iron-formation and chert
RAVELSTONE FORMATION
MES
OPRO
TERO
ZOIC
PALA
EOPR
OTER
OZOI
CAR
CHAE
AN
Bang
emal
lGr
oup
Eara
heed
yGr
oup
Padb
ury G
roup
Brya
h Gr
oup
Yerri
da G
roup
Win
dpla
in S
ubgr
oup
Moo
loog
ool S
ubgr
oup
Yarla
rwee
lor g
neiss
belt
Narry
er T
erra
ne
lowe
r gre
ensc
hist to
upp
er a
mph
ibol
ite fa
cies
met
amor
phism
_Ca
prico
rn O
roge
ny
Mur
chiso
n Te
rrane
YILG
ARN
CRAT
ONYE
RRID
A BA
SIN
BRYA
H BA
SIN
preh
niteEcirc
pum
pelly
ite to
mid
-gre
ensc
hist fa
cies
met
amor
phism
_Ca
prico
rn O
roge
ny
PADB
URY
BASI
N
Undivided MARALOOU DOOLGUNNA THADUNA and KILLARA FORMATIONS
Contact Bryah Group_Padbury Group
Structural symbols are numbered according totheir age of formation where known
Middle Proterozoic
Early Proterozoic
interpreted movement
Fold showing direction of plunge
Small-scale fold axial surface showing strike and dip
Bedding showing strike and dip
Foliation showing strike and dip
Lineation showing direction of plunge
Single zircon UEcircPb SHRIMP geochronology data
Nutman A P Bennett V C Kinny P D and Price R 1993 Large scale crustalstructure of the northwestern Yilgarn Craton Western Australia evidence fromNd isotopic data and zircon geochronology Tectonics v12 p 971-981
Nelson D R 1997 Geological Survey of Western Australia Record 19972
Nelson D R in prep Geological Survey of Western Australia Record 19982Mineral occurrence
Edited by D Ferdinando and G Loan
Cartography by P Taylor and B Williams
Topography from the Department of Land Administration Sheets SG 50-7 -8 -11 -12with modifications from geological field survey
Published by the Geological Survey of Western Australia Copies available fromthe Information Centre Department of Minerals and Energy 100 Plain StreetEast Perth WA 6004 Phone (08) 9222 3459 Fax (08) 9222 3444
This map is also available in digital form
Printed by the Sands Print Group Western Australia
The recommended reference for this map isSWAGER C P OCCHIPINTI S A and PIRAJNO F 1998 Interpreted Geology of thePalaeoproterozoic Bryah and Padbury Basins Western Australia Geological Survey Report 59 Plate 1
Unconformity (section only)
unconformity with local major onlap reworked as a fault
Geological boundary
Edmund fold belt unspecified
Capricorn Orogeny unspecified
Capricorn Orogeny DOtilde DUcirc Dccedil Deacute
Fault
Reactivated normal fault
lateral (plan view) dip slip (section)
away from observer
Strongly foliated rock
anticline
syncline
overturned anticline
overturned syncline
towards observer
Minor fold showing direction of plunge
inclined
vertical
inclined
vertical
overturned
bedding or layering trend
inclined
vertical
trend (section only)
GSWA identification number
mineral lineation
intersection lineation
Nutman et al identification number
interpreted age of intrusion in Ma with reference number
youngest detrital zircon
Highway with national route marker
Formed road
Track
Landing ground
Townsite population less than 1000
Mineral field boundary
Homestead
Locality
Building yard
Microwave repeater station
Horizontal control major
Watercourse ephemeral pool
Waterhole spring
Bore well windpump
Dam tank
Abandoned position doubtful
Mining centre
Mining locality
Mine (gold unless otherwise indicated)
Major opencut
Opencut
Alluvial workings
Prospect
Copper
Gold
Manganese
Talc
PILBARACRATON
CAPRICORN OROGEN
CRATONYILGARN
0 5 10 15 20 255000
Metres Kilometres
VERTICAL DATUM AUSTRALIAN HEIGHT DATUM
SCALE 1Yacute250Yacute000
Grid lines indicate 20Yacute000 metre interval of the Map Grid Australia Zone 50
HORIZONTAL DATUM GEOCENTRIC DATUM OF AUSTRALIA 1994UNIVERSAL TRANSVERSE MERCATOR PROJECTION
The Map Grid Australia (MGA) is based on the Geocentric Datum of Australia 1994 (GDA94)
GEOCENTRIC DATUM OF AUSTRALIA
GDA94 positions are compatible within one metre of the datum WGS84 positions
Reference points to align maps based on the previous datum AGD84 have been placed near the map corners
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
REPORT 59 PLATE 1
BRYAH AND PADBURY BASINS
2344
2345
2346
2347
2444
2445
2446
2447
2544
2545
2546
2547
2644
2645
2646
2647
2744
2745
2746
2747
2844
2845
2846
2847
KALLI
MILEURA
GOULD
ERRABIDDY
MADOONGA
KOONMARRA
MOORARIE
MARQUIS
MEEKATHARRA
TIERACO
PADBURY
MILGUN
GABANINTHA
GLENGARRY
BRYAH
JAMINDI
YAGANOO
MOOLOOGOOL
DOOLGUNNA
MEREWETHER
THADUNA
MARYMIA
MOUNT BARTLE
THREE RIVERS
118958
88YacuteEcirc168
BELELE GLENGARRY
ROBINSON RANGE PEAK HILL
SG 50-7 SG 50-8
SG 50-11 SG 50-12
1100Yacute000 maps shown in black
Compiled by C P Swager S A Occhipinti and F Pirajno 1997
N
P
Geology from 1100Yacute000 GSWA maps (see sheet index)
See current GSWA map catalogue for the full range of published products
and by S A Occhipinti C P Swager 1995 1997 and J S Myers 1995
Published 1100Yacute000 maps used in compilation
1250Yacute000 maps shown in brown
+ means declination is east and correction must be
subtracted from compass bearing to give true bearing
Annual change is 1Agrave easterly
The lines indicate magnetic declination 1995
added to compass bearing to give true bearing
- means declination is west and correction must be
SEA LEVEL
5 km
11 km
brvbar Western Australia 1998
117frac34 30Agrave25frac3400Agrave
118frac3400Agrave 119frac3400Agrave 120frac3400Agrave
26frac3400Agrave
INTERPRETED GEOLOGY OF THE PALAEOPROTEROZOIC
AREA OF THIS MAP
GSWA
REPORT 60
PLATE 1
E
Version 11 _ May 2004
Q
R
S
T
F
G
L
M
O
P
N
J
K
C
D
E
A
B
H
I
1 2 3
1
2
3
cc 3300
1
lt1996YacuteucircYacute352
lt2014YacuteucircYacute222
lt1785YacuteucircYacute112
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- Report 59 Geology and mineralization of the Palaeoproterozoic Bryah and Padbury Basins Western Australia
-
- Contents
- Abstract
- Introduction
- Regional tectonic setting
- Geology stratigraphy and geochronology
-
- Peak Hill Schist and Marymia Inlier
- Bryah Group
-
- Karalundi Formation
- Narracoota Formation
-
- Peridotitic and high-Mg basalt association
- Intrusive rocks and layered intrusions
- Mafic and ultramafic schist
- Metabasaltic hyaloclastite
- Felsic schist
- Volcaniclastic rocks
- Carbonated and silicified metavolcanic rocks
- Jasperoidal chert
- Geochemistry of the Narracoota Formation
-
- Ravelstone Formation
- Horseshoe Formation
-
- Padbury Group
-
- Labouchere Formation
- Wilthorpe Formation
-
- Beatty Park and Heines Members
-
- Robinson Range Formation
- Millidie Creek Formation
- Unassigned units of the Padbury Group
-
- Structure
-
- D1 structures
- D2 structures
- D3 structures and their relationship to D2 structures
- D4 structures
-
- Metamorphism
- Structural synthesis
- Mineralization
-
- Gold deposits
-
- Peak Hill Jubilee and Mount Pleasant deposits
- Harmony deposit
- Labouchere Nathans and Fortnum deposits
- Wembley deposit
- Wilgeena deposit
- Durack St Crispin and Heines Find prospects
- Ruby Well group
- Mikhaburra deposit
- Wilthorpe deposit
- Cashman deposit
-
- Volcanogenic copperndashgold deposits
- Supergene manganese deposits
- Iron ore
- Talc
- Discussion
-
- Tectonic model and conclusions
- Acknowledgements
- References
- Appendix Gazetteer of localities
- Plate 1 Interpreted geology of the Palaeoproterozoic Bryah and Padbury Basins
- Figures
-
- Figure 1 Stratigraphy of the former lsquoGlengarry Basinrsquo
- Figure 2 Simplified geology of the Bryah Padbury and Yerrida Basins
- Figure 3 Rotated orthoclase porphyroblast Peak Hill Schist
- Figure 4 Partially recrystallized mylonite Peak Hill Schist
- Figure 5 Peak Hill Schist mylonite from the Hangingwall Sequence
- Figure 6 Outcrop of quartz mylonite Peak Hill Schist
- Figure 7 Peak Hill Schist (Crispin Mylonite) illustrating a typical mylonitic fabric
- Figure 8 Maficndashultramafic volcanic rocks of the Narracoota Formation (Dimble Belt)
- Figure 9 Basaltic hyaloclastite Narracoota Formation
- Figure 10 Mafic volcaniclastic rock Narracoota Formation
- Figure 11 Volcanic breccia intersected in diamond drillhole BD1
- Figure 12 Total alkali versus silica diagram for rocks the Narracoota Formation
- Figure 13 Total alkali versus silica diagram defining limits of alkaline and subalkaline basalts of the Narracoota Formation
- Figure 14 Geochemical characteristics of the Narracoota Formation rocks
- Figure 15 Geochemical discriminant plots for Narracoota Formation
- Figure 16 TiO2 versus FeOMgO plot for maficndashultramafic rocks of the Narracoota Formation
- Figure 17 Schematic stratigraphy of the Horseshoe Formation
- Figure 18 Major regional structures in the Bryah and Padbury Groups
- Figure 19 Simplified geological map of the Bryah and Padbury Groups
- Figure 20 Selected hypothetical cross sections through the Bryah and Padbury Groups
- Figure 21 Model of the structural development of the BryahndashPadbury Group succession
- Figure 22 New model of the structural development of the BryahndashPadbury Group succession
- Figure 23 New model for the structural development of the BryahndashPadbury Group succession and the Peak Hill Schist
- Figure 24 Schematic north-northwest to south-southeast cross section from the Bangemall Basin into the Yarlarweelor gneiss complex and then into the Bryah and Padbury Basins
- Figure 25 Distribution of mineral deposits and occurrences in the BryahndashPadbury and Yerrida Basins
- Figure 26 Distribution of mineral deposits and occurrences in the Bryah Group within the BRYAH 1100 000 map sheet
- Figure 27 Albite porphyroblasts in mylonitic schist at Mount Pleasant
- Figure 28 The Mine Sequence schist
- Figure 29 Schematic geological map of the Fiveways Main and Mini opencuts Peak Hill deposit
- Figure 30 Peak Hill Mini opencut showing the ore-bearing mylonitic schist graphitic schist and Marker quartzite unit
- Figure 31 Diagrammatic cross section of the Harmony ore zones
- Figure 32 The west wall opencut showing the contact between biotitendashsericitendashquartz schist and deformed Despair Granite
- Figure 33 Sketch illustrating a conceptual model for the origin of precious and base metal deposits in the BryahndashPadbury and Yerrida Basins
- Figure 34 Schematic illustration showing the preferred model of the tectonic evolution of the Bryah and Padbury Basins within the context of the Capricorn Orogen
-
- Tables
-
- Table 1 Stratigraphy of the Bryah and Padbury Groups
- Table 2 Representative chemical analyses of the Narracoota Formation
- Table 3 Magnesium numbers for the Narracoota and Killara Formations
- Table 4 Selected geochemical parameters for the Narracoota Formation
- Table 5 Sequence of deformation events in the Bryah and Padbury Basins
- Table 6 Mineral paragenesis of the Bryah Group and relationships between diagnostic metamorphic minerals of the Bryah Group and deformation fabrics
- Table 7 Gold production and remaining resources in the Bryah and Padbury Groups
- Table 8 Mineral production and remaining resources in the Bryah and Padbury Groups
- Table 9 Mineral deposits and occurrences in the Bryah and Padbury Basins
-
GEOCHEMICAL ANALYSES OF ROCKS FROM THE NARRACOOTA FORMATION For details of analytical techniques see in text of Report 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
Sample | Easting | Northing | SiO2 | TiO2 | Al2O3 | Fe2O3 | FeO | MnO | MgO | CaO | Na2O | K2O | P2O5 | LOI | H2O- | H2O+ | TOTAL | CO2 | Ag | As | Au | Ba | Bi | Cd | Ce | Cr | Co | Cu | Ga | Ge | La | Li | Mo | Mn | Nb | Ni | Pb | Pd | Pt | Rb | Sb | Sc | Sn | Sr | Ta | Te | Th | Ti | U | V | Y | W | Zn | Zr | Hf | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm | Yb | Lu | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86342 | 746314 | 7198282 | 5151 | 032 | 1523 | 928 | 018 | 1049 | 1007 | 269 | 019 | 003 | 673 | 166 | 1 | 95 | 12 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86383 | 670171 | 7163822 | 5353 | 091 | 1468 | 115 | 019 | 744 | 863 | 299 | 005 | 008 | 253 | 100 | 1 | 85 | 21 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86384 | 670171 | 7163822 | 5048 | 062 | 1444 | 991 | 016 | 1135 | 933 | 362 | 004 | 005 | 640 | 209 | 1 | 157 | 16 | 33 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
86397 | 799422 | 7201118 | 5529 | 026 | 1502 | 817 | 017 | 1136 | 416 | 549 | 005 | 002 | 1174 | 244 | 0 | 44 | 15 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104248 | 722651 | 7168587 | 4925 | 022 | 1137 | 963 | 017 | 1818 | 948 | 159 | 009 | 002 | 1 | 80 | 9 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104249 | 722651 | 7168587 | 4911 | 026 | 1065 | 973 | 017 | 2016 | 855 | 126 | 009 | 003 | 1 | 34 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104254 | 715830 | 7171470 | 4948 | 023 | 1121 | 95 | 016 | 2035 | 706 | 194 | 005 | 002 | 1877 | 647 | 1 | 49 | 11 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104255 | 715830 | 7171470 | 52 | 033 | 143 | 847 | 017 | 1071 | 1087 | 31 | 002 | 003 | 664 | 209 | 0 | 133 | 13 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256 | 715830 | 7171470 | 5244 | 067 | 1455 | 1007 | 019 | 834 | 983 | 376 | 007 | 007 | 0 | 140 | 17 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104257 | 713820 | 7171502 | 5144 | 092 | 1453 | 1078 | 02 | 689 | 1244 | 248 | 023 | 009 | 265 | 79 | 3 | 195 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104264 | 685287 | 7155494 | 5303 | 062 | 1391 | 94 | 017 | 768 | 1239 | 265 | 01 | 006 | 720 | 222 | 1 | 90 | 15 | 32 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104265 | 685287 | 7155494 | 5332 | 025 | 1592 | 97 | 017 | 658 | 1215 | 184 | 003 | 004 | 353 | 67 | 1 | 30 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104288 | 661877 | 7126843 | 5979 | 024 | 1346 | 798 | 016 | 522 | 1265 | 042 | 004 | 004 | 283 | 46 | 0 | 17 | 15 | 11 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104289 | 656054 | 7130760 | 5446 | 014 | 1559 | 955 | 017 | 826 | 957 | 204 | 019 | 003 | 358 | 116 | 4 | 43 | 8 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104292 | 657132 | 7123177 | 5103 | 09 | 1369 | 971 | 017 | 827 | 1334 | 272 | 009 | 008 | 0 | 165 | 18 | 51 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104294 | 664424 | 7119210 | 5108 | 095 | 1449 | 1021 | 018 | 879 | 1094 | 283 | 046 | 008 | 523 | 141 | 5 | 123 | 19 | 52 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104295 | 664424 | 7119210 | 5228 | 096 | 1446 | 1022 | 018 | 946 | 856 | 364 | 016 | 009 | 465 | 132 | 2 | 79 | 19 | 54 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104298 | 669014 | 7106533 | 5233 | 087 | 1367 | 939 | 017 | 778 | 1189 | 373 | 01 | 008 | 514 | 116 | 1 | 116 | 17 | 49 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104299 | 669014 | 7106533 | 5166 | 093 | 1404 | 982 | 018 | 823 | 1183 | 305 | 017 | 009 | 491 | 117 | 3 | 124 | 18 | 53 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104300 | 669014 | 7106533 | 477 | 05 | 173 | 984 | 019 | 747 | 1484 | 197 | 016 | 004 | 3 | 142 | 12 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104386 | 676392 | 7146500 | 5373 | 037 | 1501 | 846 | 016 | 864 | 977 | 373 | 009 | 004 | 557 | 152 | 0 | 106 | 18 | 18 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104391 | 687552 | 7144198 | 5002 | 023 | 845 | 934 | 016 | 2281 | 88 | 014 | 002 | 002 | 0 | 15 | 11 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104392 | 687552 | 7144198 | 5391 | 027 | 92 | 998 | 014 | 2087 | 515 | 017 | 027 | 003 | 2508 | 1103 | 12 | 16 | 22 | 10 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393 | 687539 | 7143275 | 508 | 023 | 965 | 1025 | 01 | 289 | 004 | 0 | 001 | 001 | 0 | 3 | 5 | 6 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104394 | 687539 | 7143275 | 5594 | 05 | 1494 | 867 | 019 | 73 | 697 | 537 | 006 | 006 | 363 | 88 | 0 | 90 | 19 | 24 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104397 | 670399 | 7142584 | 4687 | 019 | 1023 | 1015 | 017 | 2496 | 726 | 015 | 001 | 001 | 2786 | 971 | 0 | 7 | 8 | 4 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104398 | 669575 | 7143518 | 5329 | 035 | 1453 | 813 | 014 | 828 | 1207 | 315 | 002 | 004 | 574 | 124 | 0 | 78 | 13 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104399 | 670423 | 7144430 | 5183 | 036 | 1491 | 866 | 016 | 932 | 1147 | 323 | 002 | 003 | 682 | 173 | 0 | 42 | 14 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104400 | 670023 | 7145280 | 4958 | 037 | 1577 | 987 | 019 | 1044 | 1082 | 291 | 002 | 003 | 510 | 124 | 0 | 68 | 17 | 15 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109487 | 638809 | 7157725 | 5719 | 043 | 1423 | 73 | 013 | 868 | 626 | 569 | 004 | 004 | 442 | 116 | 0 | 18 | 11 | 19 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109492 | 663796 | 7149130 | 5231 | 011 | 617 | 72 | 015 | 24 | 1002 | 001 | 001 | 001 | 0 | 7 | 5 | 1 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109493 | 663796 | 7149130 | 5246 | 047 | 1508 | 881 | 019 | 766 | 1218 | 247 | 064 | 005 | 478 | 90 | 6 | 72 | 15 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109504 | 670124 | 7121353 | 5396 | 048 | 149 | 859 | 015 | 716 | 1237 | 231 | 003 | 005 | 445 | 96 | 0 | 61 | 17 | 22 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
109513 | 732634 | 7164722 | 5396 | 197 | 1434 | 953 | 02 | 638 | 686 | 592 | 064 | 019 | 16 | 117 | 24 | 97 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601 | 668775 | 7146298 | 5332 | 179 | 1568 | 102 | 025 | 644 | 561 | 601 | 053 | 017 | 10 | 105 | 21 | 90 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112603 | 672130 | 7147178 | 108 | 034 | 2 | 1698 | lt10 | 462 | lt4 | lt5 | lt6 | 559 | 54 | 12 | lt3 | 6 | lt2 | lt7 | 115 | lt4 | 87 | 4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 167 | 19 | 92 | 203 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604 | 672238 | 7155486 | 202 | lt001 | 3 | lt4 | 40 | 34 | 8 | lt5 | 73 | 3639 | 69 | 16 | lt3 | 38 | lt2 | lt7 | 143 | 20 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | lt2 | lt2 | 453 | 29 | 20 | 34 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112620 | 626709 | 7204920 | 33 | 001 | 2 | lt4 | 220 | 35 | lt4 | lt5 | 19 | 1377 | 78 | 22 | lt3 | 25 | lt2 | 9 | 127 | 26 | lt2 | lt4 | lt4 | 10 | lt5 | lt6 | 10 | lt2 | 358 | 22 | 13 | 182 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112621 | 626709 | 7204920 | 116 | 011 | 1 | 144 | lt10 | lt11 | lt4 | lt5 | lt6 | 2354 | 82 | 8 | lt3 | lt5 | lt2 | lt7 | 1589 | lt4 | lt2 | 9 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 131 | 6 | 72 | 20 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112624 | 661284 | 7183319 | 507 | 074 | 139 | 274 | 769 | 018 | 791 | 104 | 244 | 025 | 007 | 358 | 1007 | 1 | lt4 | lt10 | 54 | lt4 | lt5 | lt6 | 186 | 92 | 13 | lt3 | lt5 | lt2 | lt7 | 96 | lt4 | 6 | lt4 | lt4 | 97 | lt5 | lt6 | lt2 | lt2 | 264 | 18 | 77 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112625 | 661284 | 7183319 | 498 | 074 | 143 | 244 | 747 | 016 | 831 | 116 | 237 | 03 | 007 | 324 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 354 | 90 | 12 | lt3 | lt5 | lt2 | lt7 | 111 | lt4 | 4 | lt4 | lt4 | 85 | lt5 | lt6 | lt2 | lt2 | 241 | 15 | 79 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112628 | 661284 | 7183319 | 49 | 08 | 138 | 357 | 726 | 018 | 738 | 14 | 143 | 008 | 007 | 277 | 1006 | 2 | lt4 | lt10 | 147 | lt4 | lt5 | 6 | 167 | 91 | 14 | lt3 | lt5 | lt2 | lt7 | 101 | lt4 | lt2 | lt4 | lt4 | 310 | lt5 | lt6 | lt2 | lt2 | 265 | 19 | 77 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112629 | 661284 | 7183319 | 642 | 049 | 103 | 271 | 402 | 012 | 438 | 113 | 051 | 013 | 005 | 18 | 1001 | lt1 | lt4 | lt10 | 109 | lt4 | lt5 | lt6 | 113 | 58 | 12 | lt3 | lt5 | lt2 | lt7 | 60 | lt4 | 2 | lt4 | lt4 | 86 | lt5 | lt6 | lt2 | lt2 | 166 | 11 | 50 | 39 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112640 | 675227 | 7128672 | 49 | 052 | 147 | 272 | 517 | 014 | 915 | 148 | 142 | 011 | 005 | 221 | 1002 | 1 | lt4 | lt10 | 90 | lt4 | lt5 | lt6 | 277 | 38 | 13 | lt3 | lt5 | lt2 | lt7 | 160 | lt4 | 2 | 5 | lt4 | 184 | lt5 | lt6 | lt2 | lt2 | 212 | 11 | 54 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112641 | 675215 | 7127749 | 508 | 079 | 142 | 308 | 703 | 017 | 744 | 118 | 207 | 012 | 008 | 299 | 1008 | 1 | lt4 | 90 | 26 | lt4 | lt5 | lt6 | 266 | 102 | 14 | lt3 | lt5 | lt2 | lt7 | 120 | lt4 | lt2 | lt4 | lt4 | 148 | lt5 | lt6 | lt2 | lt2 | 258 | 16 | 80 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643 | 675190 | 7125902 | 275 | 205 | lt1 | 10 | 40 | 767 | lt4 | lt5 | 175 | 994 | 257 | 12 | 3 | 12 | 2 | lt7 | lt3 | 34 | lt2 | lt4 | lt4 | 43 | lt5 | lt6 | lt2 | lt2 | 272 | 13 | 96 | 25 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112645 | 663956 | 7162053 | 23 | 059 | lt1 | 7 | lt10 | 227 | lt4 | lt5 | 34 | 2117 | 390 | 3 | 12 | lt2 | 8 | lt3 | 12 | lt2 | lt4 | 8 | 10 | lt5 | lt6 | 6 | lt2 | 467 | 14 | 81 | 132 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112646 | 663956 | 7162053 | 507 | 076 | 139 | 224 | 796 | 018 | 771 | 991 | 258 | 063 | 007 | 375 | 1005 | 1 | lt4 | lt10 | 164 | lt4 | lt5 | 6 | 207 | 79 | 13 | lt3 | lt5 | lt2 | lt7 | 123 | lt4 | 16 | lt4 | lt4 | 338 | lt5 | lt6 | lt2 | lt2 | 245 | 15 | 77 | 55 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112647 | 663956 | 7162053 | 356 | 002 | 1 | 133 | 1170 | lt11 | lt4 | lt5 | 13 | 489 | 846 | 6 | 4 | 6 | lt2 | lt7 | 533 | 1491 | lt2 | 4 | lt4 | lt2 | lt5 | 8 | lt2 | lt2 | 104 | 12 | 180 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112650 | 663956 | 7162053 | 573 | 424 | 959 | 166 | 036 | lt005 | 12 | 226 | 012 | 028 | 005 | 75 | 999 | 1 | lt4 | lt10 | 423 | lt4 | lt5 | 152 | 481 | 119 | 20 | lt3 | 90 | lt2 | 27 | 171 | 10 | 12 | lt4 | lt4 | 61 | lt5 | lt6 | 6 | lt2 | 365 | 37 | 54 | 296 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112652 | 663956 | 7162053 | 526 | 088 | 133 | 253 | 762 | 022 | 745 | 741 | 31 | 081 | 008 | 474 | 1009 | 1 | lt4 | lt10 | 242 | lt4 | lt5 | lt6 | 149 | 158 | 12 | lt3 | lt5 | lt2 | lt7 | 99 | 6 | 17 | 5 | lt4 | 87 | lt5 | lt6 | 2 | lt2 | 260 | 22 | 88 | 63 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112672 | 734725 | 7164593 | 628 | 07 | 136 | 355 | 364 | 034 | 337 | 494 | 286 | 093 | 009 | 313 | 1001 | 1 | lt4 | 20 | 258 | lt4 | lt5 | 76 | 122 | 16 | 17 | lt3 | 34 | lt2 | 17 | 75 | 13 | 19 | lt4 | 4 | 164 | lt5 | lt6 | 22 | 2 | 99 | 26 | 73 | 216 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 69 | 108 | 111 | 258 | 508 | 009 | 415 | 016 | 312 | 036 | 007 | 361 | 1006 | 1 | lt4 | lt10 | 386 | lt4 | lt5 | 30 | 56 | lt4 | 14 | lt3 | 18 | lt2 | 17 | 24 | lt4 | 17 | lt4 | lt4 | 79 | lt5 | lt6 | 8 | lt2 | 239 | 19 | 79 | 119 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112673 | 734708 | 7165209 | 633 | 136 | 113 | 297 | 736 | 012 | 617 | 025 | 21 | 012 | 018 | 499 | 1004 | 1 | lt4 | 20 | 460 | lt4 | lt5 | 18 | 19 | 56 | 14 | lt3 | 10 | lt2 | 17 | 32 | 12 | 4 | lt4 | lt4 | 30 | lt5 | lt6 | 9 | 3 | 312 | 32 | 109 | 153 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 631 | 137 | 115 | 248 | 803 | 009 | 662 | 024 | 211 | lt005 | 016 | 496 | 1008 | 1 | lt4 | 20 | 28 | lt4 | lt5 | 37 | 21 | 203 | 17 | lt3 | 17 | 3 | 19 | 30 | 6 | lt2 | lt4 | lt4 | 27 | lt5 | lt6 | 9 | 3 | 336 | 24 | 107 | 158 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112674 | 734644 | 7166319 | 129 | 697 | lt1 | 4 | 1250 | 1768 | lt4 | lt5 | 69 | 597 | 472 | 11 | lt3 | 53 | lt2 | lt7 | 327 | 22 | 90 | lt4 | lt4 | 226 | lt5 | lt6 | 8 | 2 | 181 | 19 | 118 | 101 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112675 | 734644 | 7166319 | 569 | 025 | 767 | 183 | 429 | 013 | 153 | 768 | 303 | 007 | lt005 | 396 | 1013 | 1 | lt4 | lt10 | 55 | lt4 | lt5 | lt6 | 541 | 26 | 4 | lt3 | lt5 | lt2 | lt7 | 262 | lt4 | 2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 117 | 9 | 46 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112678 | 734655 | 7166965 | 715 | 009 | 411 | 133 | 335 | 006 | 112 | 341 | 016 | lt005 | lt005 | 442 | 999 | 1 | lt4 | lt10 | 32 | lt4 | lt5 | lt6 | 1537 | 11 | 3 | lt3 | lt5 | lt2 | lt7 | 659 | lt4 | lt2 | lt4 | lt4 | 4 | lt5 | lt6 | lt2 | lt2 | 69 | 5 | 33 | 8 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112679 | 735684 | 7171472 | 518 | 034 | 135 | 289 | 531 | 014 | 945 | 12 | 267 | lt005 | lt005 | 277 | 1011 | 1 | lt4 | lt10 | 51 | lt4 | lt5 | lt6 | 670 | 56 | 12 | lt3 | lt5 | lt2 | lt7 | 272 | lt4 | lt2 | lt4 | lt4 | 60 | lt5 | lt6 | lt2 | lt2 | 198 | 16 | 55 | 21 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112680 | 735675 | 7172519 | 515 | 037 | 148 | 282 | 565 | 015 | 864 | 991 | 357 | lt005 | lt005 | 314 | 1008 | 1 | lt4 | lt10 | 83 | lt4 | lt5 | lt6 | 470 | 88 | 12 | lt3 | lt5 | lt2 | lt7 | 192 | lt4 | lt2 | 5 | lt4 | 88 | lt5 | lt6 | lt2 | lt2 | 216 | 17 | 62 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116407 | 603693 | 7169737 | 279 | lt001 | 1 | 4 | lt10 | 126 | lt4 | lt5 | 12 | 140 | 34 | lt3 | 3 | 7 | lt2 | 11 | 191 | 7 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | 3 | lt2 | 36 | 11 | 21 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116410 | 608442 | 7170499 | 211 | lt01 | lt1 | lt4 | lt10 | 726 | lt4 | lt5 | 6 | 696 | 17 | lt3 | lt3 | 5 | lt2 | lt7 | 82 | 4 | lt2 | lt4 | lt4 | 24 | lt5 | lt6 | 2 | lt2 | 40 | 5 | 10 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116415 | 611248 | 7168937 | 904 | lt005 | 265 | 094 | 095 | lt005 | 248 | 005 | 005 | lt005 | lt005 | 263 | 1005 | lt1 | 4 | lt10 | 947 | lt4 | lt5 | lt6 | 944 | 13 | lt3 | lt3 | 5 | lt2 | lt7 | 394 | lt4 | lt2 | lt4 | lt4 | 28 | lt5 | lt6 | lt2 | lt2 | 35 | 7 | 22 | lt5 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116428 | 614781 | 7170999 | 484 | 016 | 723 | 188 | 628 | 014 | 215 | 813 | 077 | lt005 | lt005 | 61 | 1011 | 1 | 4 | lt10 | 14 | lt4 | lt5 | lt6 | 2275 | 12 | 4 | lt3 | lt5 | lt2 | lt7 | 998 | lt4 | lt2 | lt4 | lt4 | 22 | lt5 | lt6 | lt2 | lt2 | 126 | 8 | 60 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116429 | 614810 | 7171215 | 113 | 029 | 13 | 129 | 10 | 66 | lt4 | lt5 | lt6 | 2489 | 60 | 7 | lt5 | 15 | lt7 | 1344 | lt4 | 3 | 89 | 25 | lt4 | 75 | lt5 | 8 | lt2 | lt2 | 183 | 11 | 127 | 14 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116430 | 614807 | 7170845 | 217 | 002 | 10 | 12 | 2570 | 32 | lt4 | lt5 | 22 | 1581 | 463 | 4 | lt5 | lt6 | lt7 | 286 | 109 | lt2 | lt4 | 53 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 348 | 13 | 95 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116432 | 614348 | 7169311 | 101 | 009 | 6 | 5 | 80 | 44 | lt4 | lt5 | 15 | 1757 | 116 | lt3 | 7 | lt6 | 11 | 683 | lt4 | lt2 | lt4 | 37 | lt4 | 27 | lt5 | lt6 | lt2 | lt2 | 327 | 18 | 119 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116433 | 614232 | 7168820 | 211 | 029 | lt5 | 7 | 60 | 2075 | lt4 | lt5 | 35 | 254 | 126 | 5 | 26 | lt6 | 13 | 186 | 13 | 27 | 4 | 12 | lt4 | 56 | lt5 | lt6 | 4 | lt2 | 152 | 25 | 120 | 100 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116442 | 632664 | 7159418 | 414 | 022 | 21 | 7 | 10 | 710 | lt4 | lt5 | lt6 | 39 | 716 | lt3 | lt5 | lt6 | lt7 | 35 | 4 | lt2 | lt4 | 40 | lt4 | 28 | lt5 | 6 | lt2 | lt2 | 1073 | 16 | 137 | 23 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116443 | 634091 | 7159896 | 461 | 035 | 144 | 279 | 528 | 018 | 746 | 165 | 174 | 005 | lt005 | 545 | 1005 | 2 | lt4 | lt10 | 23 | lt4 | lt5 | lt6 | 443 | 62 | 15 | lt3 | lt5 | lt2 | lt7 | 164 | lt4 | lt2 | lt4 | lt4 | 63 | lt5 | lt6 | lt2 | lt2 | 233 | 17 | 56 | 22 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116444 | 633832 | 7161837 | 11 | 021 | lt1 | 13 | lt10 | 1185 | lt4 | lt5 | 42 | 173 | 66 | 13 | lt3 | 24 | lt2 | 14 | 67 | 10 | 23 | lt4 | lt4 | 28 | lt5 | lt6 | 4 | lt2 | 245 | 18 | 61 | 87 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116446 | 633910 | 7169621 | 458 | 014 | 847 | 147 | 74 | 016 | 22 | 765 | 02 | lt005 | lt005 | 71 | 101 | 1 | lt4 | lt10 | 66 | lt4 | lt5 | lt6 | 2882 | 12 | 7 | lt3 | lt5 | lt2 | lt7 | 1306 | lt4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 142 | 8 | 67 | 11 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454 | 653363 | 7152948 | 174 | 01 | lt1 | 15 | 130 | 111 | lt4 | lt5 | lt6 | 389 | 106 | 21 | lt3 | lt5 | lt2 | lt7 | 204 | lt4 | 16 | lt4 | lt4 | 12 | lt5 | lt6 | lt2 | lt2 | 450 | 10 | 122 | 55 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477 | 645436 | 7177439 | 178 | 007 | lt1 | lt4 | 30 | 52 | lt4 | lt5 | lt6 | 689 | 88 | 21 | lt3 | 55 | lt2 | lt7 | 456 | 5 | 13 | lt4 | lt4 | 5 | lt5 | lt6 | lt2 | lt2 | 435 | 98 | 350 | 69 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485 | 655767 | 7129994 | 225 | 018 | lt1 | lt4 | lt10 | 78 | lt4 | lt5 | lt6 | 5612 | 129 | 8 | 3 | lt5 | 2 | 7 | 88 | 4 | lt2 | lt4 | lt4 | 7 | lt5 | lt6 | lt2 | lt2 | 119 | 7 | 39 | 38 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487 | 655561 | 7129043 | 168 | 013 | 1 | lt4 | lt10 | 191 | lt4 | lt5 | 11 | 4578 | 8 | 6 | lt3 | lt5 | lt2 | lt7 | 464 | 11 | 10 | lt4 | lt4 | 11 | lt5 | lt6 | lt2 | lt2 | 87 | 7 | 70 | 35 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116488 | 655420 | 7128860 | 156 | 012 | lt1 | lt4 | 40 | 119 | lt4 | lt5 | 19 | 135 | 279 | 31 | lt3 | 7 | 2 | 7 | 313 | 21 | 23 | lt4 | lt4 | 15 | lt5 | lt6 | 3 | 3 | 585 | 10 | 97 | 149 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 128 | 007 | lt1 | lt4 | 170 | 169 | lt4 | lt5 | lt6 | 5588 | 63 | 4 | lt3 | lt5 | lt2 | lt7 | 687 | 14 | 12 | lt4 | lt4 | 6 | lt5 | 8 | 2 | 2 | 75 | 7 | 81 | 30 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116489 | 655489 | 7127659 | 681 | 02 | 2 | 8 | lt10 | 34 | lt4 | lt5 | lt6 | 967 | 299 | 6 | lt3 | 9 | lt2 | lt7 | 348 | lt4 | lt2 | lt4 | lt4 | lt2 | lt5 | lt6 | lt2 | lt2 | 469 | 35 | 110 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116490 | 655978 | 7126699 | 491 | 078 | 147 | 315 | 779 | 017 | 816 | 994 | 274 | 065 | 008 | 371 | 1012 | 1 | lt4 | 20 | 228 | lt4 | lt5 | lt6 | 191 | 103 | 13 | lt3 | lt5 | lt2 | lt7 | 116 | lt4 | 9 | lt4 | lt4 | 300 | lt5 | lt6 | lt2 | lt2 | 267 | 17 | 87 | 56 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116491 | 656084 | 7126206 | 50 | 07 | 133 | 216 | 817 | 019 | 999 | 939 | 208 | 035 | 007 | 402 | 1007 | 1 | lt4 | 10 | 329 | lt4 | lt5 | lt6 | 471 | 104 | 12 | lt3 | lt5 | lt2 | lt7 | 249 | lt4 | 6 | 4 | lt4 | 157 | lt5 | lt6 | lt2 | lt2 | 241 | 16 | 82 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116492 | 656023 | 7125806 | 10 | 27 | 10 | 213 | lt4 | lt5 | lt6 | 17 | 170 | lt3 | lt5 | 7 | lt7 | 40 | lt4 | 49 | 4 | 49 | lt4 | 38 | 803 | lt6 | lt2 | lt2 | 434 | 28 | 45 | 58 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493 | 655992 | 7125530 | 13 | 25 | 60 | 150 | lt4 | lt5 | lt6 | 24 | 393 | lt3 | 6 | 10 | lt7 | 118 | 6 | 79 | lt4 | 55 | lt4 | 31 | 269 | lt6 | lt2 | lt2 | 464 | 37 | 239 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116498 | 709849 | 7162239 | 11 | 19 | 5000 | 269 | lt4 | lt5 | lt6 | 140 | 92 | lt3 | lt5 | 6 | lt7 | 83 | lt4 | 74 | lt4 | 47 | lt4 | 50 | 301 | lt6 | lt2 | lt2 | 316 | 25 | 123 | 67 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116500 | 709011 | 7162160 | 9 | 29 | 10 | 155 | lt4 | lt5 | lt6 | 27 | 121 | lt3 | lt5 | 6 | lt7 | 39 | 5 | 33 | lt4 | 66 | lt4 | 20 | 155 | lt6 | lt2 | lt2 | 535 | 34 | 28 | 86 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501 | 708508 | 7162137 | 11 | 6 | 20 | 23 | lt4 | lt5 | lt6 | 29 | 146 | lt3 | lt5 | 6 | lt7 | 102 | lt4 | 98 | lt4 | 57 | lt4 | 31 | 195 | 6 | lt2 | lt2 | 416 | 35 | 144 | 74 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116502 | 708368 | 7162139 | 756 | 052 | lt1 | 8 | lt10 | 368 | lt4 | lt5 | 11 | 25 | 398 | lt3 | lt3 | 12 | 2 | lt7 | 151 | 6 | lt2 | lt4 | 4 | 23 | lt5 | lt6 | lt2 | lt2 | 207 | 15 | 211 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116532 | 672308 | 7165117 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | 1009 | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | 117 | 13 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 5 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 275 | 21 | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120337 | 668950 | 7146475 | 508 | 075 | 142 | 254 | 825 | 019 | 774 | 103 | 223 | 024 | 007 | 342 | nd | 4 | lt4 | lt10 | 140 | lt4 | lt5 | lt6 | 168 | nd | 117 | 13 | lt5 | nd | lt2 | lt7 | 104 | lt4 | nd | nd | 5 | lt4 | nd | lt4 | 129 | lt2 | 44963 | lt2 | 275 | 21 | nd | 94 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120340 | 669175 | 7145725 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | 1009 | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | 92 | 14 | lt3 | lt5 | lt2 | lt7 | 118 | lt4 | 4 | 4 | lt4 | 132 | lt5 | lt6 | 2 | lt2 | 259 | 18 | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369 | 665175 | 7156150 | 505 | 077 | 144 | 347 | 666 | 015 | 731 | 118 | 234 | 008 | 007 | 314 | nd | 1 | lt4 | lt10 | 625 | lt4 | lt5 | 7 | 263 | nd | 92 | 14 | lt5 | nd | lt2 | lt7 | 118 | lt4 | nd | nd | 4 | 40 | nd | lt4 | 132 | 2 | 46162 | lt2 | 259 | 18 | nd | 76 | 57 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373 | 675250 | 7167875 | 50 | 078 | 146 | 288 | 732 | 017 | 757 | 112 | 256 | lt005 | 008 | 328 | 328 | 1006 | nd | lt1 | lt4 | lt10 | 101 | lt4 | lt5 | lt6 | 224 | nd | 100 | 14 | lt3 | lt5 | nd | lt2 | lt7 | 125 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 120 | lt5 | lt6 | lt2 | 46761 | lt2 | 262 | 16 | nd | 84 | 57 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432 | 673950 | 7171700 | 52 | 077 | 146 | 219 | 763 | 015 | 753 | 793 | 429 | lt005 | 008 | 326 | 326 | 1006 | nd | 1 | 4 | lt10 | 126 | lt4 | lt5 | lt6 | 266 | nd | 109 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 123 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 97 | lt5 | lt6 | lt2 | 46162 | lt2 | 257 | 21 | nd | 84 | 59 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120549 | 709110 | 7163260 | 851 | 045 | 827 | 064 | 028 | lt005 | 066 | 02 | 025 | 252 | lt005 | 211 | 1007 | 1 | lt4 | lt10 | 516 | lt4 | lt5 | 49 | 56 | lt4 | 10 | lt3 | 18 | lt2 | 9 | 17 | 18 | 135 | 5 | lt4 | 13 | lt5 | lt6 | 13 | 5 | 139 | 21 | 8 | 114 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120550 | 709190 | 7162721 | 516 | 087 | 135 | 324 | 901 | 021 | 646 | 957 | 246 | 031 | 008 | 362 | 101 | 1 | 4 | lt10 | 145 | lt4 | lt5 | lt6 | 17 | 70 | 15 | lt3 | lt5 | lt2 | lt7 | 70 | lt4 | 7 | lt4 | lt4 | 93 | lt5 | lt6 | 2 | 52157 | lt2 | 267 | 20 | 85 | 62 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120566 | 734201 | 7165328 | 733 | 003 | 1 | lt4 | 10 | 261 | lt4 | lt5 | 8 | 257 | 24 | 24 | lt3 | lt5 | 2 | 8 | 97 | 12 | lt2 | lt4 | lt4 | 376 | lt5 | lt6 | lt2 | lt2 | 962 | 5 | 59 | 61 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120593 | 707343 | 7160447 | 48 | 046 | 116 | 248 | 735 | 017 | 14 | 101 | 148 | lt005 | 005 | 464 | 1007 | lt1 | lt4 | lt10 | 35 | lt4 | lt5 | lt6 | 1617 | 39 | 11 | lt3 | lt5 | lt2 | lt7 | 611 | lt4 | lt2 | lt4 | lt4 | 91 | lt5 | lt6 | lt2 | lt2 | 220 | 13 | 72 | 37 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120630 | 722750 | 7168750 | 38 | 014 | 733 | 088 | 695 | 014 | 207 | 725 | 095 | lt005 | lt005 | 18 | 1009 | 1 | lt4 | 10 | 41 | lt4 | lt5 | lt6 | 2746 | 46 | 6 | lt3 | lt5 | lt2 | lt7 | 1110 | lt4 | lt2 | lt4 | lt4 | 32 | lt5 | lt6 | lt2 | lt2 | 137 | 6 | 56 | 13 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120688 | 739099 | 7173927 | 521 | 084 | 139 | 322 | 775 | 017 | 658 | 104 | 288 | 017 | 008 | 277 | 101 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 160 | 35 | 13 | lt3 | lt5 | lt2 | lt7 | 133 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | lt2 | lt2 | 317 | 20 | 78 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120692 | 738903 | 7174351 | 496 | 032 | 134 | 271 | 658 | 015 | 115 | 101 | 223 | 009 | lt005 | 405 | 101 | lt1 | lt4 | lt10 | 149 | lt4 | lt5 | lt6 | 941 | 57 | 12 | lt3 | lt5 | lt2 | lt7 | 334 | lt4 | lt2 | lt4 | lt4 | 129 | lt5 | lt6 | lt2 | lt2 | 205 | 13 | 61 | 32 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120698 | 735588 | 7172781 | 546 | 059 | 136 | 26 | 576 | 014 | 727 | 101 | 346 | 006 | 006 | 246 | 1008 | lt1 | 15 | lt10 | 71 | lt4 | lt5 | lt6 | 315 | 60 | 11 | lt3 | lt5 | lt2 | lt7 | 100 | lt4 | lt2 | lt4 | lt4 | 67 | lt5 | lt6 | lt2 | lt2 | 228 | 16 | 65 | 44 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120727 | 456 | 015 | 815 | 227 | 694 | 016 | 225 | 686 | 045 | lt005 | lt005 | 726 | 1009 | lt1 | lt4 | lt10 | 27 | lt4 | lt5 | lt6 | 2788 | 31 | 6 | lt3 | lt5 | lt2 | lt7 | 1075 | lt4 | lt2 | lt4 | lt4 | 14 | lt5 | lt6 | lt2 | lt2 | 141 | 7 | 69 | 25 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120728 | 687200 | 7128470 | 545 | 04 | 141 | 225 | 609 | 015 | 916 | 624 | 5 | lt005 | 005 | 324 | 1014 | lt1 | 23 | lt10 | 61 | lt4 | lt5 | lt6 | 479 | 103 | 7 | lt3 | lt5 | lt2 | lt7 | 202 | lt4 | lt2 | lt4 | lt4 | 68 | lt5 | lt6 | lt2 | lt2 | 213 | 14 | 70 | 36 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120729 | 686100 | 7128750 | 833 | 027 | 1 | 814 | lt10 | 298 | lt4 | lt5 | lt6 | 2024 | 80 | 4 | lt3 | lt5 | lt2 | 9 | 796 | 4 | 46 | 17 | lt4 | 46 | lt5 | lt6 | lt2 | lt2 | 115 | 15 | 50 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120730 | 686300 | 7128650 | 383 | 003 | 1 | 9 | lt10 | 73 | lt4 | lt5 | lt6 | 3998 | 203 | 5 | lt3 | lt5 | lt2 | 15 | 1785 | lt4 | lt2 | 4 | lt4 | 8 | lt5 | lt6 | lt2 | lt2 | 270 | 19 | 108 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120770 | 675368 | 7143153 | 11 | 138 | lt1 | 246 | lt10 | 458 | lt4 | lt5 | lt6 | 1351 | 50 | 7 | lt3 | lt5 | lt2 | 12 | 259 | 4 | 57 | 5 | lt4 | 114 | lt5 | 6 | lt2 | lt2 | 155 | 9 | 45 | 31 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120801 | 686900 | 7143160 | 916 | 213 | 1 | 169 | 660 | 1736 | lt4 | lt5 | 66 | 1275 | 594 | 5 | lt3 | 26 | lt2 | 13 | 101 | 24 | 41 | lt4 | lt4 | 94 | lt5 | 11 | lt2 | lt2 | 147 | 35 | 98 | 37 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120802 | 686900 | 7143160 | 146 | 009 | lt1 | 17 | lt10 | 130 | lt4 | lt5 | 12 | 3035 | 213 | 19 | lt3 | 6 | lt2 | 19 | 1488 | 4 | 12 | lt4 | lt4 | 31 | lt5 | lt6 | 2 | lt2 | 432 | 22 | 148 | 116 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120873 | 697233 | 7155938 | 518 | 133 | 142 | 374 | 907 | 02 | 572 | 106 | 23 | 044 | 016 | 117 | 1009 | lt1 | lt4 | lt10 | 204 | lt4 | lt5 | 23 | 72 | 232 | 18 | lt3 | 8 | lt2 | lt7 | 58 | lt4 | 40 | lt4 | lt4 | 134 | lt5 | lt6 | 3 | lt2 | 239 | 33 | 95 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120874 | 699393 | 7156313 | 503 | 062 | 148 | 29 | 648 | 016 | 812 | 112 | 313 | 01 | 006 | 31 | 1012 | lt1 | lt4 | lt10 | 124 | lt4 | lt5 | lt6 | 356 | 99 | 12 | lt3 | lt5 | lt2 | lt7 | 140 | lt4 | lt2 | lt4 | lt4 | 80 | lt5 | lt6 | lt2 | lt2 | 244 | 14 | 71 | 46 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120876 | 694754 | 7155096 | 506 | 091 | 141 | 358 | 748 | 017 | 751 | 109 | 142 | 026 | 009 | 371 | 1009 | lt1 | lt4 | lt10 | 125 | lt4 | lt5 | lt6 | 176 | 141 | 15 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 3 | lt4 | lt4 | 178 | lt5 | lt6 | lt2 | lt2 | 262 | 20 | 103 | 71 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120877 | 694754 | 7155096 | 509 | 085 | 142 | 399 | 735 | 018 | 709 | 105 | 209 | 034 | 008 | 34 | 1011 | lt1 | lt4 | lt10 | 103 | lt4 | lt5 | lt6 | 119 | 158 | 15 | lt3 | lt5 | lt2 | lt7 | 107 | lt4 | 4 | lt4 | lt4 | 182 | lt5 | lt6 | 2 | lt2 | 269 | 19 | 95 | 70 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120878 | 694149 | 7154736 | 488 | 082 | 143 | 385 | 717 | 018 | 765 | 128 | 174 | 008 | 008 | 33 | 1009 | lt1 | lt4 | lt10 | 86 | lt4 | lt5 | lt6 | 137 | 107 | 15 | lt3 | lt5 | lt2 | lt7 | 105 | lt4 | lt2 | lt4 | lt4 | 142 | lt5 | lt6 | lt2 | lt2 | 257 | 24 | 83 | 60 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120891 | 677938 | 7168840 | 4880 | 082 | 1430 | 385 | 717 | 018 | 765 | 1280 | 174 | 008 | 008 | 330 | 10077 | 1 | 4 | 10 | 86 | 4 | 5 | 6 | 137 | 107 | 15 | 5 | 2 | 7 | 105 | 4 | 2 | 4 | 4 | 142 | 2 | 2 | 257 | 24 | 83 | 60 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124203 | 685884 | 7169152 | 496 | 089 | 14 | 329 | 852 | 02 | 733 | 981 | 233 | 009 | 008 | 36 | 998 | lt1 | lt4 | lt10 | 53 | lt4 | lt5 | lt6 | 65 | 122 | 14 | lt3 | lt5 | lt2 | lt7 | 91 | lt4 | lt2 | lt4 | lt4 | 124 | lt5 | lt6 | 2 | lt2 | 280 | 19 | 104 | 66 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124204 | 685884 | 7168152 | 511 | 082 | 135 | 254 | 81 | 019 | 74 | 106 | 235 | 033 | 008 | 343 | 1006 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 130 | 85 | 12 | lt3 | lt5 | lt2 | lt7 | 104 | lt4 | 4 | lt4 | lt4 | 47 | lt5 | lt6 | lt2 | lt2 | 261 | 18 | 88 | 51 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
124208 | 685884 | 7169152 | 497 | 075 | 143 | 293 | 769 | 017 | 784 | 115 | 181 | 03 | 008 | 35 | 1007 | lt1 | lt4 | lt10 | 105 | lt4 | lt5 | lt6 | 129 | 132 | 14 | lt3 | lt5 | lt2 | lt7 | 94 | lt4 | 5 | lt4 | lt4 | 84 | lt5 | lt6 | lt2 | lt2 | 255 | 17 | 87 | 54 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132787 | 630625 | 7198600 | 492 | 07 | 142 | 265 | 735 | 017 | 857 | 126 | 176 | 009 | 006 | 335 | 1008 | 1 | lt4 | lt10 | 75 | lt4 | lt5 | lt6 | 136 | 105 | 16 | lt3 | lt5 | lt2 | lt7 | 158 | 5 | lt2 | lt4 | lt4 | 126 | lt5 | lt6 | lt2 | lt2 | 247 | 17 | 70 | 52 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132788 | 630625 | 7198600 | 218 | lt001 | lt1 | lt4 | lt10 | 864 | lt4 | lt5 | lt6 | 454 | 9 | lt3 | lt3 | lt5 | lt2 | lt7 | 67 | lt4 | lt2 | lt4 | lt4 | 9 | lt5 | lt6 | 2 | lt2 | 41 | 3 | 7 | lt5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132789 | 602460 | 7168288 | 556 | 021 | 138 | 329 | 587 | 016 | 612 | 111 | 131 | lt005 | lt005 | 303 | 303 | 1005 | nd | lt1 | lt4 | lt10 | 130 | lt4 | lt5 | lt6 | 158 | nd | 76 | 8 | lt3 | lt5 | nd | lt2 | lt7 | 98 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 16 | lt2 | 12590 | lt2 | 204 | 13 | nd | 72 | 17 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132790 | 613877 | 7170789 | 527 | 035 | 138 | 239 | 605 | 016 | 83 | 113 | 189 | lt005 | lt005 | 338 | 338 | 1006 | nd | lt1 | lt4 | lt10 | 81 | lt4 | lt5 | lt6 | 503 | nd | 81 | 10 | lt5 | nd | lt2 | lt7 | 190 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 27 | lt5 | 9 | lt2 | 20983 | lt2 | 211 | 14 | nd | 65 | 24 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132791 | 621561 | 7169810 | 499 | 057 | 133 | 308 | 649 | 015 | 96 | 121 | 204 | 005 | 006 | 316 | 316 | 1007 | nd | lt1 | 4 | lt10 | 71 | lt4 | lt5 | lt6 | 633 | nd | 80 | 12 | lt3 | lt5 | nd | lt2 | lt7 | 281 | lt4 | nd | nd | lt2 | lt4 | nd | lt4 | 75 | lt5 | lt6 | lt2 | 34172 | lt2 | 233 | 16 | nd | 74 | 40 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132792 | 616685 | 7171750 | 503 | 084 | 134 | 527 | 637 | 017 | 813 | 104 | 107 | 005 | 007 | 432 | 1006 | lt1 | lt4 | lt10 | 12 | lt4 | lt5 | lt6 | 314 | 144 | 13 | lt3 | 6 | lt2 | lt7 | 204 | 5 | lt2 | lt4 | lt4 | 114 | lt5 | lt6 | lt2 | lt2 | 285 | 28 | 95 | 59 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132793 | 622866 | 7161836 | 4860 | 031 | 1350 | 362 | 510 | 013 | 1040 | 1090 | 231 | 001 | 003 | 321 | 9812 | 2 | 4 | 3 | 29 | 4 | 5 | 6 | 872 | 45 | 61 | 11 | 3 | 97 | 7 | 379 | 4 | 3 | 2 | 2 | 4 | 4 | 72 | 2 | 2 | 216 | 14 | 4 | 60 | 21 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
132794 | 622866 | 7161786 | 4840 | 014 | 576 | 203 | 615 | 015 | 2160 | 863 | 033 | 001 | 001 | 549 | 9870 | 2 | 4 | 4 | 11 | 6 | 5 | 6 | 2460 | 71 | 22 | 5 | 3 | 2 | 7 | 1020 | 4 | 4 | 3 | 2 | 4 | 4 | 11 | 2 | 2 | 155 | 7 | 4 | 63 | 13 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133033 | 638351 | 7157551 | 4450 | 156 | 1110 | 611 | 440 | 020 | 318 | 1330 | 468 | 034 | 021 | 906 | 9864 | 01 | 05 | 5 | 323 | 07 | 01 | 296 | 190 | 36 | 84 | 05 | 126 | 01 | 11 | 75 | 19 | 11 | 11 | 51 | 02 | 1 | 07 | 135 | 22 | 07 | 276 | 241 | 05 | 73 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133034 | 638351 | 7157551 | 4710 | 013 | 836 | 237 | 696 | 014 | 1980 | 764 | 012 | 001 | 003 | 596 | 9862 | 02 | 12 | 2 | 18 | 45 | 01 | 32 | 3448 | 69 | 22 | 16 | 16 | 23 | 32 | 1048 | 11 | 5 | 9 | 17 | 18 | 42 | 19 | 52 | 15 | 01 | 133 | 58 | 84 | 72 | 108 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133035 | 638300 | 7157750 | 4740 | 013 | 668 | 349 | 512 | 014 | 2200 | 801 | 022 | 003 | 001 | 521 | 9844 | 02 | 07 | 6 | 52 | 14 | 01 | 11 | 2608 | 73 | 34 | 22 | 12 | 03 | 33 | 1295 | 15 | 10 | 9 | 22 | 06 | 29 | 1 | 12 | 16 | 02 | 116 | 72 | 58 | 61 | 447 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133038 | 632615 | 7159390 | 5060 | 048 | 1600 | 316 | 443 | 012 | 572 | 1410 | 150 | 032 | 006 | 267 | 022 | 102 | lt05 | 70 | 110 | lt05 | lt01 | 216 | 392 | 29 | 93 | 57 | 147 | 10 | 12 | 28 | 138 | 29 | lt2 | 3 | 179 | 297 | 31 | 74 | 141 | 21 | 28776 | 02 | 181 | 14 | 139 | 59 | 709 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133039 | 632600 | 7159000 | 5160 | 034 | 1550 | 281 | 555 | 014 | 644 | 1090 | 252 | 026 | 002 | 309 | 026 | lt01 | lt05 | 30 | 80 | lt05 | lt01 | 06 | 422 | 36 | 88 | 47 | lt05 | 6 | 05 | 33 | 183 | lt05 | lt2 | lt2 | 46 | 115 | 32 | 29 | 139 | lt05 | 20383 | lt01 | 216 | 148 | 77 | 66 | 338 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133043 | 632906 | 7159832 | 4970 | 073 | 1490 | 272 | 790 | 018 | 626 | 1260 | 171 | 031 | 006 | 236 | 022 | 03 | 21 | 30 | 412 | 09 | 01 | 46 | 66 | 37 | 129 | 05 | 61 | 8 | 06 | 41 | 121 | 48 | lt2 | 9 | 99 | 44 | 11 | 27 | 119 | 13 | 43764 | 02 | 268 | 203 | 33 | 88 | 470 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133046 | 633939 | 7161905 | 4980 | 051 | 1280 | 263 | 708 | 016 | 1070 | 1060 | 163 | 014 | 005 | 309 | 016 | lt01 | lt05 | lt2 | 48 | lt05 | lt01 | 18 | 678 | 43 | 85 | 47 | 53 | 8 | 04 | 05 | 327 | lt05 | lt2 | lt2 | 06 | 68 | 34 | 15 | 123 | lt05 | 30575 | lt01 | 227 | 147 | 51 | 76 | 443 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133047 | 633939 | 7161905 | 5200 | 079 | 1400 | 280 | 738 | 017 | 548 | 1080 | 227 | 039 | 007 | 264 | 022 | 118 | lt05 | lt2 | 60 | lt05 | lt01 | 36 | 116 | 36 | 74 | 56 | 48 | 12 | 04 | 44 | 81 | lt05 | lt2 | lt2 | 95 | 46 | 38 | 09 | 101 | lt05 | 47361 | lt01 | 261 | 193 | 45 | 77 | 673 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133048 | 633939 | 7161905 | 4800 | 053 | 1050 | 391 | 746 | 018 | 972 | 1360 | 100 | 034 | 004 | 390 | 015 | lt01 | lt05 | 30 | 63 | lt05 | lt01 | 37 | 200 | 55 | 192 | 55 | 10 | 11 | 02 | 19 | 156 | 36 | lt2 | 3 | 55 | 08 | 43 | lt05 | 110 | lt05 | 31774 | lt01 | 276 | 126 | 12 | 76 | 410 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133049 | 634427 | 7166123 | 4900 | 059 | 1390 | 361 | 656 | 016 | 658 | 1300 | 190 | 019 | 005 | 328 | 015 | lt01 | lt05 | 30 | 45 | lt05 | lt01 | 25 | 120 | 42 | 164 | 66 | 12 | 10 | 07 | 32 | 143 | 24 | lt2 | lt2 | 20 | 33 | 24 | lt05 | 101 | lt05 | 35371 | lt01 | 220 | 145 | 82 | 67 | 442 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133050 | 635551 | 7169572 | 4890 | 060 | 1280 | 365 | 706 | 017 | 698 | 1370 | 137 | 023 | 005 | 348 | 011 | lt01 | lt05 | 30 | 36 | lt05 | lt01 | 22 | 165 | 49 | 108 | 64 | 08 | 11 | 04 | 24 | 152 | 22 | lt2 | 4 | 49 | 06 | 33 | lt05 | 108 | lt05 | 35970 | lt01 | 233 | 149 | 18 | 68 | 415 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133051 | 635603 | 7169579 | 0 | 74 | 0 | 02 | 15 | 12 | 114 | 114 | 24 | 91 | 13 | 05 | 84 | 73 | 27 | 12 | 11 | 24 | 0 | 40 | 15 | 158 | 173 | 043 | 256 | 18 | 05 | 74 | 62 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133052 | 635259 | 7169444 | 5160 | 086 | 1360 | 411 | 719 | 016 | 569 | 1030 | 155 | 048 | 008 | 344 | 9906 | 038 | 01 | 05 | 2 | 151 | 05 | 01 | 94 | 148 | 37 | 136 | 33 | 11 | 03 | 34 | 93 | 05 | 2 | 2 | 105 | 02 | 24 | 05 | 145 | 05 | 01 | 296 | 191 | 05 | 85 | 718 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133054 | 634952 | 7169267 | 0 | 62 | 05 | 0 | 38 | 5 | 105 | 44 | 18 | 25 | 41 | 12 | 13 | 57 | 48 | 5 | 6 | 12 | 0 | 26 | 18 | 411 | 6 | 166 | 182 | 18 | 08 | 38 | 104 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133060 | 648256 | 7160919 | 0 | 23 | 0 | 02 | 19 | 6 | 89 | 129 | 18 | 10 | 5 | 12 | 88 | 62 | 27 | 3 | 0 | 92 | 0 | 38 | 21 | 251 | 111 | 037 | 318 | 25 | 08 | 85 | 76 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133063 | 648467 | 7150024 | 4400 | 018 | 889 | 410 | 531 | 015 | 2270 | 702 | 037 | 003 | 002 | 705 | 9982 | 011 | 01 | 05 | 2 | 7 | 05 | 01 | 05 | 3170 | 83 | 19 | 53 | 05 | 03 | 18 | 1370 | 15 | 9 | 13 | 09 | 04 | 23 | 05 | 135 | 05 | 01 | 123 | 76 | 27 | 72 | 139 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133064 | 647573 | 7150076 | 5150 | 032 | 1450 | 307 | 514 | 015 | 634 | 1390 | 178 | 001 | 003 | 244 | 9918 | 015 | 01 | 05 | 3 | 50 | 05 | 01 | 05 | 456 | 29 | 40 | 65 | 14 | 04 | 09 | 191 | 05 | 11 | 11 | 05 | 04 | 36 | 05 | 577 | 05 | 01 | 222 | 144 | 21 | 61 | 26 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133073 | 626850 | 7161292 | 5150 | 033 | 1440 | 273 | 573 | 014 | 748 | 1250 | 232 | 001 | 003 | 264 | 9981 | 011 | 01 | 05 | 3 | 43 | 05 | 01 | 05 | 467 | 38 | 78 | 32 | 19 | 02 | 29 | 202 | 14 | 13 | 12 | 05 | 03 | 32 | 05 | 497 | 05 | 01 | 219 | 137 | 05 | 61 | 258 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133076 | 626850 | 7161292 | 4990 | 074 | 1490 | 410 | 612 | 015 | 546 | 1320 | 148 | 006 | 007 | 297 | 9915 | 022 | 01 | 05 | 3 | 42 | 05 | 01 | 85 | 154 | 33 | 55 | 65 | 34 | 03 | 34 | 93 | 05 | 7 | 11 | 05 | 02 | 33 | 05 | 151 | 05 | 01 | 263 | 169 | 16 | 84 | 678 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133096 | 645954 | 7171243 | 4500 | 013 | 916 | 192 | 711 | 014 | 2110 | 744 | 015 | 002 | 001 | 699 | 9917 | 022 | 01 | 05 | 2 | 75 | 05 | 01 | 23 | 3100 | 93 | 69 | 6 | 146 | 06 | 14 | 1620 | 17 | 7 | 7 | 07 | 17 | 26 | 05 | 27 | 05 | 01 | 132 | 212 | 21 | 69 | 103 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
133098 | 636053 | 7155351 | 4950 | 057 | 1510 | 228 | 646 | 014 | 728 | 1380 | 135 | 010 | 006 | 307 | 9971 | 015 | 01 | 05 | 6 | 174 | 05 | 01 | 08 | 487 | 31 | 81 | 47 | 58 | 05 | 37 | 165 | 05 | 12 | 16 | 15 | 02 | 26 | 05 | 112 | 35 | 02 | 220 | 135 | 05 | 64 | 429 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136749 | 667073 | 7199167 | 5080 | 072 | 1420 | 410 | 567 | 015 | 601 | 1330 | 166 | 022 | 007 | 221 | 9911 | 011 | 01 | 05 | 4 | 222 | 05 | 01 | 42 | 331 | 37 | 82 | 57 | 59 | 04 | 29 | 131 | 1 | 12 | 11 | 32 | 07 | 31 | 05 | 237 | 05 | 01 | 257 | 175 | 15 | 75 | 665 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
136751 | 659000 | 7122223 | 0 | 12 | 0 | 0 | 98 | 3 | 209 | 68 | 15 | 62 | 34 | 04 | 44 | 86 | 2 | 9 | 7 | 43 | 0 | 34 | 09 | 304 | 053 | 021 | 207 | 15 | 09 | 48 | 23 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139131 | 621200 | 7215100 | 4790 | 065 | 1470 | 301 | 746 | 019 | 682 | 1290 | 254 | 004 | 006 | 319 | 9946 | 026 | 01 | 05 | 3 | 211 | 05 | 01 | 43 | 358 | 43 | 103 | 07 | 4 | 02 | 46 | 154 | 05 | 8 | 14 | 05 | 02 | 29 | 05 | 616 | 05 | 02 | 281 | 19 | 05 | 77 | 484 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139132 | 621190 | 7215090 | 0 | 14 | 0 | 01 | 11 | 0 | 66 | 18 | 46 | 59 | 40 | 05 | 95 | 11 | 14 | 0 | 0 | 108 | 0 | 51 | 21 | 242 | 87 | 124 | 389 | 7 | 24 | 51 | 134 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139133 | 666700 | 7193500 | 0 | 09 | 0 | 02 | 56 | 0 | 0 | 18 | 37 | 39 | 92 | 05 | 63 | 4 | 62 | 0 | 0 | 63 | 0 | 53 | 19 | 33 | 21 | 24 | 29 | 18 | 08 | 25 | 290 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139134 | 621755 | 7169255 | 0 | 08 | 0 | 0 | 85 | 3 | 3 | 3 | 15 | 63 | 14 | 09 | 06 | 0 | 2 | 0 | 0 | 73 | 0 | 06 | 08 | 76 | 129 | 05 | 4 | 3 | 03 | 3 | 35 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139135 | 621000 | 7169500 | 5016 | 037 | 1406 | 241 | 647 | 017 | 918 | 1126 | 248 | 006 | 003 | 15 | 5812 | 222 | 438 | 53 | 65 | 10 | 438 | 077 | 1320 | 100E-07 | 171 | 100E-07 | 500E-08 | 54 | 2 | 53 | 500E-08 | 500E-08 | 212 | 15 | 72 | 19 | 036 | 194 | 094 | 048 | 190 | 038 | 289 | 071 | 222 | 034 | 232 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139136 | 621000 | 7169500 | 5236 | 027 | 1373 | 239 | 577 | 016 | 897 | 1068 | 21 | 007 | 003 | 15 | 5265 | 210 | 491 | 53 | 162 | 10 | 491 | 086 | 1290 | 100E-07 | 196 | 100E-07 | 1 | 48 | 200E-07 | 62 | 500E-08 | 500E-08 | 189 | 13 | 63 | 13 | 036 | 161 | 078 | 041 | 160 | 039 | 259 | 068 | 214 | 038 | 221 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139137 | 620904 | 7169533 | 4737 | 108 | 1123 | 33 | 789 | 018 | 1191 | 106 | 203 | 008 | 012 | 15 | 13407 | 2170 | 1150 | 82 | 119 | 15 | 1150 | 897 | 1380 | 6 | 525 | 2 | 500E-08 | 39 | 4 | 143 | 1 | 500E-08 | 265 | 17 | 90 | 65 | 278 | 1143 | 314 | 124 | 391 | 066 | 391 | 084 | 222 | 031 | 187 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139138 | 620992 | 7169508 | 5075 | 03 | 141 | 177 | 678 | 017 | 996 | 925 | 264 | 044 | 002 | 05 | 7628 | 124 | 660 | 56 | 61 | 10 | 660 | 042 | 1310 | 100E-07 | 232 | 100E-07 | 55 | 49 | 2 | 62 | 500E-08 | 500E-08 | 194 | 12 | 65 | 14 | 019 | 104 | 062 | 031 | 135 | 030 | 225 | 055 | 166 | 026 | 175 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139139 | 620992 | 7169508 | 4747 | 018 | 1006 | 141 | 804 | 017 | 1989 | 829 | 089 | 002 | 001 | 500E-08 | 7171 | 148 | 1770 | 95 | 53 | 75 | 1770 | 089 | 1320 | 100E-07 | 835 | 100E-07 | 500E-08 | 39 | 2 | 225 | 500E-08 | 500E-08 | 139 | 8 | 60 | 7 | 019 | 098 | 063 | 028 | 124 | 028 | 206 | 051 | 157 | 026 | 160 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139140 | 620992 | 7169508 | 5201 | 117 | 1269 | 224 | 762 | 016 | 761 | 1089 | 239 | 025 | 013 | 05 | 8447 | 2455 | 212 | 52 | 161 | 15 | 212 | 982 | 1210 | 5 | 135 | 100E-07 | 45 | 42 | 4 | 228 | 1 | 500E-08 | 270 | 17 | 87 | 80 | 308 | 1270 | 330 | 120 | 387 | 061 | 364 | 074 | 200 | 028 | 161 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
139141 | 620992 | 7169488 | 6179 | 081 | 147 | 284 | 594 | 006 | 496 | 012 | 007 | 32 | 01 | 1 | 74341 | 6413 | 414 | 41 | 31 | 19 | 414 | 2988 | 410 | 12 | 163 | 3 | 161 | 29 | 4 | 11 | 155 | 3 | 90 | 19 | 132 | 198 | 677 | 2282 | 433 | 094 | 430 | 059 | 295 | 058 | 166 | 026 | 170 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104256h | 715830 | 7171470 | 6528 | 068 | 1179 | 412 | 511 | 004 | 551 | 013 | 005 | 24 | 012 | 1 | 44782 | 7429 | 348 | 39 | 2 | 15 | 348 | 3419 | 300 | 10 | 176 | 3 | 121 | 21 | 4 | 9 | 19 | 3 | 73 | 27 | 83 | 266 | 834 | 2926 | 592 | 121 | 584 | 082 | 451 | 089 | 249 | 038 | 231 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
104393s | 687539 | 7143275 | 3634 | 015 | 744 | 519 | 582 | 02 | 1191 | 1139 | 002 | 001 | 002 | 177 | 2109 | 066 | 2020 | 175 | 257 | 6 | 043 | 1440 | 00000001 | 1000 | 00000001 | 000000005 | 24 | 2 | 42 | 000000005 | 05 | 108 | 6 | 35 | 13 | 016 | 080 | 044 | 022 | 067 | 014 | 094 | 022 | 074 | 012 | 090 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112601s | 668775 | 7146298 | 1248 | 005 | 339 | 812 | 262 | 026 | 1592 | 217 | 005 | 001 | 0 | 156 | 1400 | 058 | 850 | 63 | 46 | 25 | 066 | 1990 | 00000001 | 1010 | 1 | 000000005 | 10 | 2 | 66 | 000000005 | 000000005 | 87 | 11 | 22 | 3 | 024 | 085 | 052 | 025 | 083 | 021 | 145 | 034 | 111 | 017 | 131 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112604s | 672238 | 7155486 | 7639 | 017 | 1136 | 256 | 551 | 022 | 087 | 002 | 002 | 01 | 001 | 457 | 15133 | 087 | 2260 | 9 | 10 | 8 | 031 | 1590 | 00000001 | 228 | 1 | 45 | 21 | 00000002 | 17 | 000000005 | 05 | 149 | 2 | 17 | 9 | 009 | 043 | 014 | 012 | 017 | 004 | 028 | 006 | 023 | 004 | 035 | 005 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
112643h | 675190 | 7125902 | 5583 | 097 | 1236 | 543 | 726 | 045 | 595 | 128 | 308 | 005 | 015 | 195 | 2804 | 1728 | 46 | 41 | 13 | 145 | 738 | 3010 | 2 | 63 | 1 | 2 | 58 | 2 | 38 | 000000005 | 000000005 | 278 | 24 | 111 | 58 | 201 | 930 | 276 | 073 | 275 | 049 | 297 | 064 | 202 | 031 | 236 | 038 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116454s | 653363 | 7152948 | 2576 | 011 | 467 | 59 | 024 | 018 | 1282 | 1816 | 172 | 064 | 003 | 695 | 7663 | 012 | 1570 | 58 | 23 | 35 | 042 | 1370 | 00000001 | 620 | 2 | 34 | 15 | 00000002 | 385 | 000000005 | 000000005 | 76 | 5 | 30 | 4 | 013 | 027 | 019 | 018 | 037 | 010 | 069 | 017 | 060 | 009 | 070 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116477s | 645436 | 7177439 | 2009 | 0 | 084 | 152 | 0 | 038 | 1639 | 2363 | 022 | 04 | 003 | 6 | 6838 | 126 | 31 | 10 | 19 | 000000005 | 107 | 2940 | 00000001 | 93 | 1 | 75 | 00000001 | 00000002 | 103 | 000000005 | 000000005 | 9 | 10 | 4 | 00000001 | 034 | 113 | 036 | 118 | 051 | 012 | 084 | 027 | 105 | 017 | 142 | 020 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116485h | 655767 | 7129994 | 5901 | 078 | 1092 | 14 | 102 | 013 | 1024 | 016 | 003 | 0 | 008 | 65 | 744 | 774 | 86 | 47 | 39 | 125 | 276 | 965 | 2 | 136 | 00000001 | 000000005 | 62 | 2 | 15 | 000000005 | 000000005 | 304 | 15 | 85 | 45 | 099 | 490 | 138 | 035 | 148 | 026 | 164 | 036 | 114 | 018 | 143 | 023 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116487h | 655561 | 7129043 | 2488 | 011 | 535 | 29 | 312 | 04 | 1401 | 2084 | 003 | 004 | 005 | 110 | 4392 | 265 | 1410 | 69 | 15 | 5 | 175 | 3200 | 00000001 | 685 | 1 | 15 | 19 | 2 | 140 | 000000005 | 05 | 99 | 5 | 42 | 14 | 048 | 147 | 045 | 021 | 054 | 010 | 063 | 013 | 045 | 007 | 052 | 008 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116493h | 655992 | 7125530 | 5148 | 073 | 1516 | 172 | 1092 | 013 | 932 | 024 | 26 | 03 | 009 | 15 | 10919 | 1023 | 98 | 58 | 72 | 155 | 430 | 935 | 2 | 98 | 00000001 | 45 | 69 | 2 | 75 | 000000005 | 1 | 357 | 18 | 113 | 42 | 127 | 601 | 174 | 057 | 201 | 036 | 234 | 054 | 176 | 028 | 217 | 036 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116501h | 708508 | 7162137 | 4773 | 039 | 1372 | 423 | 456 | 016 | 666 | 527 | 438 | 098 | 006 | 1 | 120917 | 449 | 56 | 49 | 35 | 13 | 1277 | 1170 | 1 | 192 | 2 | 31 | 67 | 00000002 | 51 | 000000005 | 000000005 | 284 | 29 | 114 | 20 | 154 | 703 | 155 | 116 | 228 | 033 | 198 | 048 | 147 | 020 | 136 | 024 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
116518s | 685232 | 7155526 | 3765 | 02 | 609 | 573 | 0 | 152 | 597 | 1736 | 007 | 218 | 005 | 100 | 218361 | 3411 | 55 | 39 | 15 | 7 | 1396 | 11070 | 4 | 70 | 5 | 65 | 8 | 00000002 | 77 | 55 | 1 | 60 | 12 | 38 | 38 | 321 | 1160 | 235 | 171 | 234 | 031 | 155 | 028 | 088 | 013 | 096 | 015 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120303 | 655250 | 7126000 | 2302 | 011 | 404 | 31 | 071 | 059 | 074 | 3572 | 004 | 141 | 004 | 53 | 20581 | 1117 | 285 | 7 | 4 | 45 | 720 | 4740 | 1 | 51 | 12 | 435 | 00000001 | 2 | 96 | 25 | 000000005 | 36 | 9 | 21 | 17 | 141 | 504 | 105 | 042 | 126 | 021 | 127 | 030 | 097 | 015 | 109 | 019 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339A | 669650 | 7146425 | 9409 | 001 | 03 | 425 | 065 | 002 | 003 | 005 | 0 | 006 | 003 | 155 | 1042 | 267 | 29 | 6 | 65 | 05 | 117 | 110 | 00000001 | 15 | 10 | 85 | 1 | 00000002 | 5 | 05 | 05 | 55 | 1 | 10 | 4 | 023 | 092 | 016 | 004 | 021 | 003 | 014 | 003 | 009 | 001 | 012 | 002 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120339B | 669650 | 7146425 | 9632 | 0 | 002 | 319 | 053 | 001 | 0 | 001 | 0 | 0 | 001 | 5 | 2442 | 083 | 6 | 3 | 9 | 000000005 | 039 | 40 | 00000001 | 3 | 1 | 000000005 | 00000001 | 00000002 | 1 | 000000005 | 000000005 | 10 | 00000001 | 3 | 2 | 008 | 030 | 006 | 004 | 009 | 001 | 005 | 002 | 006 | 001 | 008 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120369s | 665175 | 7156150 | 6131 | 098 | 1297 | 175 | 906 | 025 | 457 | 058 | 144 | 134 | 007 | 285 | 27950 | 3230 | 284 | 43 | 121 | 15 | 1406 | 1690 | 6 | 128 | 13 | 54 | 41 | 4 | 305 | 65 | 1 | 178 | 16 | 119 | 106 | 355 | 1340 | 286 | 087 | 269 | 039 | 202 | 036 | 119 | 017 | 130 | 021 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120373s | 675250 | 7167875 | 5541 | 088 | 1306 | 795 | 346 | 014 | 199 | 144 | 005 | 004 | 009 | 1 | 7754 | 1109 | 26 | 29 | 74 | 225 | 521 | 1040 | 2 | 41 | 3 | 05 | 48 | 4 | 67 | 000000005 | 000000005 | 494 | 25 | 50 | 55 | 161 | 716 | 213 | 067 | 256 | 050 | 325 | 074 | 237 | 035 | 267 | 041 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
120432s | 673950 | 7171700 | 5469 | 078 | 1137 | 81 | 399 | 02 | 311 | 1468 | 016 | 005 | 006 | 2 | 11068 | 1433 | 62 | 44 | 22 | 20 | 634 | 1490 | 1 | 88 | 8 | 15 | 55 | 4 | 495 | 1 | 000000005 | 346 | 24 | 49 | 49 | 202 | 897 | 283 | 137 | 343 | 070 | 452 | 104 | 321 | 048 | 354 | 051 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137A | not available | 6241 | 067 | 991 | 186 | 893 | 019 | 924 | 011 | 0 | 005 | 01 | 15 | 2345 | 6927 | 595 | 43 | 123 | 12 | 3489 | 1470 | 10 | 235 | 4 | 25 | 21 | 4 | 55 | 175 | 2 | 77 | 16 | 112 | 288 | 734 | 2545 | 453 | 074 | 448 | 050 | 239 | 041 | 129 | 019 | 143 | 023 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82137B | not available | 6118 | 074 | 1029 | 19 | 912 | 019 | 96 | 011 | 0 | 009 | 01 | 1 | 3042 | 6659 | 780 | 45 | 121 | 12 | 2999 | 1430 | 10 | 218 | 6 | 4 | 22 | 4 | 4 | 175 | 25 | 80 | 27 | 116 | 312 | 704 | 2493 | 499 | 095 | 542 | 075 | 415 | 083 | 249 | 037 | 262 | 039 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82144 | not available | 6901 | 044 | 1124 | 143 | 288 | 021 | 188 | 365 | 27 | 14 | 013 | 15 | 38750 | 6263 | 117 | 22 | 22 | 12 | 3381 | 1690 | 8 | 48 | 37 | 67 | 11 | 2 | 107 | 175 | 25 | 46 | 19 | 61 | 199 | 679 | 2348 | 436 | 093 | 441 | 056 | 304 | 052 | 157 | 022 | 154 | 022 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82148 | not available | 6314 | 07 | 124 | 312 | 581 | 017 | 717 | 01 | 005 | 197 | 01 | 1 | 41557 | 6431 | 505 | 53 | 22 | 15 | 3168 | 1310 | 10 | 211 | 4 | 99 | 23 | 4 | 8 | 165 | 25 | 72 | 18 | 121 | 227 | 689 | 2407 | 462 | 095 | 440 | 055 | 281 | 050 | 159 | 022 | 168 | 025 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82150 | not available | 9469 | 001 | 012 | 45 | 062 | 001 | 001 | 001 | 0 | 0 | 001 | 1150 | 13761 | 225 | 10 | 2 | 7 | 000000005 | 310 | 40 | 00000001 | 11 | 00000001 | 000000005 | 00000001 | 6 | 000000005 | 000000005 | 3800 | 00000001 | 700 | 300 | 044 | 122 | 021 | 012 | 021 | 002 | 013 | 002 | 004 | 000 | 005 | 001 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82153 | not available | 41767 | 296 | 256 | 047 | 214 | 049 | 031 | 072 | 013 | 090 | 023 | 077 | 010 | 072 | 010 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82155 | not available | 4977 | 081 | 1429 | 329 | 833 | 02 | 718 | 945 | 255 | 018 | 007 | 2 | 10432 | 1154 | 175 | 65 | 117 | 135 | 175 | 395 | 1540 | 2 | 135 | 100E-07 | 3 | 57 | 4 | 75 | 500E-08 | 500E-08 | 290 | 18 | 104 | 45 | 174 | 807 | 287 | 119 | 400 | 083 | 496 | 117 | 328 | 056 | 311 | 053 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82158 | not available | 5076 | 077 | 1356 | 336 | 794 | 019 | 714 | 996 | 197 | 035 | 006 | 15 | 16705 | 1081 | 163 | 55 | 128 | 135 | 163 | 373 | 1490 | 1 | 123 | 100E-07 | 55 | 54 | 2 | 166 | 500E-08 | 500E-08 | 268 | 17 | 98 | 43 | 159 | 772 | 261 | 108 | 365 | 070 | 470 | 107 | 304 | 046 | 279 | 042 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82160 | not available | 4799 | 033 | 127 | 192 | 57 | 017 | 1261 | 1352 | 09 | 004 | 002 | 115 | 5413 | 491 | 1360 | 52 | 50 | 105 | 1360 | 183 | 1370 | 100E-07 | 269 | 100E-07 | 05 | 46 | 4 | 87 | 500E-08 | 500E-08 | 159 | 8 | 50 | 18 | 074 | 333 | 108 | 052 | 167 | 030 | 198 | 045 | 131 | 019 | 116 | 016 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82179 | not available | 5338 | 053 | 1381 | 255 | 679 | 016 | 722 | 774 | 466 | 004 | 006 | 500E-08 | 3625 | 1347 | 326 | 50 | 48 | 115 | 326 | 523 | 1290 | 2 | 137 | 100E-07 | 500E-08 | 53 | 2 | 103 | 1 | 1 | 239 | 16 | 74 | 40 | 168 | 721 | 230 | 080 | 334 | 068 | 459 | 107 | 321 | 049 | 296 | 044 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82180 | not available | 462 | 02 | 998 | 154 | 752 | 017 | 1869 | 845 | 1 | 003 | 002 | 500E-08 | 749 | 081 | 2240 | 93 | 46 | 8 | 2240 | 029 | 1320 | 100E-07 | 795 | 100E-07 | 500E-08 | 40 | 200E-07 | 365 | 500E-08 | 500E-08 | 148 | 10 | 56 | 8 | 015 | 081 | 051 | 034 | 110 | 026 | 192 | 050 | 157 | 026 | 167 | 028 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82224 | not available | 5042 | 029 | 1394 | 187 | 675 | 015 | 976 | 1106 | 328 | 005 | 002 | 500E-08 | 1646 | 119 | 640 | 58 | 44 | 105 | 640 | 042 | 1140 | 100E-07 | 159 | 100E-07 | 500E-08 | 54 | 200E-07 | 109 | 500E-08 | 500E-08 | 204 | 12 | 41 | 14 | 022 | 124 | 075 | 041 | 160 | 036 | 265 | 063 | 195 | 031 | 206 | 032 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82225 | not available | 4701 | 022 | 1065 | 127 | 739 | 015 | 1732 | 727 | 233 | 002 | 001 | 500E-08 | 2735 | 106 | 1730 | 84 | 32 | 75 | 1730 | 062 | 1180 | 100E-07 | 690 | 100E-07 | 500E-08 | 43 | 2 | 415 | 500E-08 | 500E-08 | 159 | 11 | 58 | 9 | 023 | 128 | 063 | 031 | 125 | 028 | 204 | 050 | 161 | 026 | 162 | 025 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82226 | not available | 4256 | 014 | 689 | 357 | 494 | 011 | 2593 | 578 | 016 | 003 | 001 | 75 | 3377 | 038 | 2280 | 102 | 8 | 55 | 2280 | 015 | 835 | 100E-07 | 1380 | 100E-07 | 1 | 31 | 200E-07 | 205 | 500E-08 | 500E-08 | 104 | 5 | 46 | 6 | 008 | 042 | 027 | 010 | 058 | 013 | 097 | 025 | 075 | 012 | 078 | 011 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82228 | not available | 4399 | 016 | 796 | 185 | 65 | 014 | 246 | 647 | 017 | 001 | 001 | 500E-08 | 9402 | 076 | 2890 | 102 | 10 | 55 | 2890 | 052 | 1050 | 100E-07 | 1130 | 100E-07 | 500E-08 | 35 | 200E-07 | 65 | 500E-08 | 500E-08 | 131 | 6 | 41 | 7 | 017 | 072 | 032 | 010 | 065 | 014 | 106 | 027 | 084 | 013 | 082 | 013 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82229 | not available | 4897 | 024 | 1196 | 106 | 807 | 015 | 1448 | 71 | 298 | 003 | 002 | 500E-08 | 11033 | 081 | 1260 | 77 | 45 | 9 | 1260 | 024 | 1160 | 100E-07 | 459 | 100E-07 | 500E-08 | 46 | 200E-07 | 138 | 500E-08 | 500E-08 | 172 | 11 | 59 | 11 | 016 | 093 | 052 | 028 | 119 | 027 | 203 | 050 | 157 | 026 | 168 | 027 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82231 | not available | 509 | 027 | 1399 | 178 | 674 | 014 | 87 | 1152 | 329 | 005 | 002 | 500E-08 | 1186 | 092 | 510 | 52 | 58 | 10 | 510 | 038 | 1100 | 100E-07 | 136 | 100E-07 | 500E-08 | 57 | 2 | 144 | 500E-08 | 500E-08 | 202 | 13 | 41 | 12 | 018 | 101 | 057 | 030 | 135 | 030 | 220 | 058 | 177 | 029 | 191 | 029 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82234 | not available | 4847 | 087 | 1468 | 1174 | 022 | 874 | 1394 | 099 | 027 | 008 | 332 | 83 | 3 | 225 | 21 | 48 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
82236 | not available | 5135 | 087 | 1461 | 1117 | 02 | 757 | 1032 | 274 | 109 | 008 | 228 | 70 | 15 | 329 | 19 | 49 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
135482 | Trillbar Complex | 5137 | 037 | 1481 | 232 | 561 | 016 | 869 | 1068 | 306 | 006 | 003 | 014 | 260 | 10014 | 39 | 2 | 593 | 59 | 61 | 00 | 08 | 08 | 1 | 124 | 1 | 1 | 51 | 00 | 08 | 235 | 17 | 61 | 20 | 0 | 5 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143538 | Trillbar Complex | 4961 | 141 | 1391 | 561 | 717 | 022 | 656 | 1136 | 204 | 022 | 011 | 014 | 163 | 10036 | 322 | 15 | 82 | 172 | 91 | 12 | 26 | 26 | 9 | 98 | 4 | 4 | 48 | 12 | 14 | 362 | 24 | 91 | 86 | 2 | 12 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
143539 | Trillbar Complex | 4974 | 086 | 1196 | 128 | 734 | 016 | 1072 | 1395 | 237 | 009 | 006 | 013 | 150 | 10047 | 77 | 10 | 298 | 80 | 47 | 07 | 14 | 14 | 4 | 240 | 2 | 1 | 59 | 07 | 06 | 322 | 19 | 47 | 46 | 2 | 7 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||
144310 | Trillbar Complex | 4711 | 115 | 1288 | 182 | 901 | 018 | 784 | 1161 | 250 | 008 | 012 | 013 | 240 | 10027 | 53 | 13 | 394 | 116 | 90 | 13 | 13 | 13 | 7 | 156 | 6 | 1 | 37 | 13 | 14 | 380 | 23 | 90 | 78 | 0 | 8 | |||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||||