AUSTRALIAN PH ^•^TIM ESC

4. I !VONIAN

T1GRAPHIC CHA TAN

EXPLANATORY NOTES,A

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by

G.C. YOUNG

BUREAU OF MINERAL RESOURCES, GEOLOGY AND GEOPHYSICS

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•Refer to this publication as:-

YOUNG, G.C., 1989 - Australian Phanerozoic Timescales: 4. Devonian. Biostratigraphic Chartand Explanatory Notes. Bureau of Mineral Resources Record 1989/34.

SERIES EDITOR - M. OWEN

Division of Continental GeologyBureau of Mineral Resources

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•© Commonwealth of Australia, 1989

This work is copyright. Apart from any fair dealing for the purposes of study, research,criticism or review, as permitted under the Copyright Act, no part may be reproduced by anyprocess without written permission of the Director, Bureau of Mineral Resources, Geology andGeophysics. Inquiries should be directed to the Principal Information Officer, BMR, GPO Box378, Canberra, ACT 2601.

COVER ILLUSTRATION: Xystridura milesi (Chapman, 1929) from the early MiddleCambrian, Beetle Creek Formation, Mount Isa district, Queensland.

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• FOREWORD

A time framework is essential to understanding the history of all aspects of the geosphere. Itis a prerequisite to interpreting the development and structure of the sedimentary basins whichhost our major petroleum, coal, and sedimentary mineral deposits, and is important whenseeking patterns in the distribution of these resources through time. It is also critical to ourunderstanding of the interactive factors which have shaped the modern Australian environ-ment, and in determining the patterns of global change.

For the Phanerozoic (the last 570 million years, the period of 'visible life'), the most efficientway of establishing such a time framework is by the study of fossils, which represent the mostconcrete evidence for the evolution of life.

• The palaeontological study of Australian sedimentary basins began with the first fossil descrip-tions in the latter part of the eighteenth century, which during the nineteenth century wereused to establish the age of major suites of sedimentary rocks. An early example of thesystematic use of fossils as time markers for detailed correlation was the subdivision ofOrdovician rocks in Victoria using graptolites at the beginning of this century. The develop-ment of Australian biostratigraphy over the last 50 years has seen the setting up of various

• biostratigraphic schemes using the fossil remains of a wide range of organisms - from themicroscopic, such as pollen grains and spores of land plants, to the macro- and megascopic - theremains of larger invertebrates, fish, mammals, even of human artifacts.

Recent years have also seen a rapid growth in other methods of measuring geological time, usingradioactive decay of mineral elements, or reversals in the Earth's magnetic field. But no methodfor measuring geological time can operate in isolation, and a comprehensive time frameworkneeds to take into account information from a variety of sources.

This preliminary series makes available for immediate use a set of charts based on recentpalaeontological data from the specialist scientific literature, as well as unpublished informa-tion from ongoing biostratigraphic research. The charts integrate zonal schemes using differentgroups of fossils with isotopic and other data (magnetic reversal, eustasy curves), and show the

• relationship of the Australian zones to standard international times cales and their numericalcalibration, where this information is available. The aim was not to produce a separate'Australian time scale' in competition with already established international scales, but ratherto provide a set of up-to-date calibrated biostratigraphic charts for use in the Australian region.Inevitably the detail of treatment and reliability varies for different parts of the column andfor different groups of fossils, and much work still needs to be done to develop a fully integrated

• chronological scale 'comparable to those available in the Northern Hemisphere.

Biostratigraphic charts were first prepare& to provide a firm chronological base for the AMIRA(Australian Mineral Industries Research Association) sponsored Palaeogeographic Atlas ofAustralia. The charts and explanatory text produced in this series are part of the second phaseof that project, the Phanerozoic History of Australia, which is funded in part by APIRA(Australian Petroleum Industry Research Association). The charts have been compiled by

• palaeontologists in BMR, but incorporate contributions by other specialists working in StateGeological Surveys, Universities and the exploration industry, without which such a com-prehensive compilation would not have been possible.

I am confident that the charts will prove to be an essential tool for the exploration industry inAustralia.

P.J. Cook,

Chief, Division of Continental Geology

DEVONIAN^1

• INTRODUCTIONThis chart was first prepared as a contribu-tion to the BMR/APIRA PalaeogeographicMaps Project, to provide biostratigraphiccontrol for the Devonian correlation charts.The accompanying notes explain the basis foreach of the 13 columns on the chart. Copiesof an early version and explanatory noteswere distributed for comment to variouspalaeontologists and biostratigraphers inearly 1987. Suggestions and comments then

• received are incorporated in this preliminaryedition, with an update of relevant literatureto early 1989. The chart attempts to integrate(with emphasis on Australian data) currentlyavailable reliable isotopic ages for points onthe Devonian time scale, with zonal schemes

• or preliminary biostratigraphic range datafor various groups of Devonian fossils. Forfossil groups lacking organised bio-stratigraphic data sets based on Australianoccurrences, 'international' zonal schemeshave been used where available.

It is evident that various fossil groups, widelyapplied in biostratigraphic studies ofDevonian strata overseas, have been sub-jected to only a rudimentary level of inves-tigation in Australian sequences. With more

• detailed systematic and biostratigraphicpalaeontology considerable refinement of thebiostratigraphic zonation can therefore beexpected. Further revision of this chart willbe undertaken as new biostratigraphic databecome available, and will be necessary to

• take account of imminent new informationon the Devonian system not available at thetime of going to press. When published, theproceedings of the second International Sym-posium on the Devonian System (Calgary,1987) will provide extensive new data on the

• Devonian of many regions, includingAustralia. In addition, it is expected thatwithin the next year decisions will be reachedon formal definitions for all Devonian stageboundaries, some of which are still under

• discussion by the Subcommission onDevonian Stratigraphy (SDS) of the Interna-tional Commission on Stratigraphy. Thiswill eradicate confusion that has resultedfrom different usage in different countries.Apart from these developments, ongoing re-search in systematic and biostratigraphicpalaeontology of Devonian fossils, improved

isotopic dating techniques, and field studiesin new areas clarifying relationships betweenisotopically and biostratigraphically datedstrata, will necessitate both minor and majorrevisions of future versions of the chart.

COLUMN 1 -GEOCHRONOMETRIC SCALE

The calibrated scale on the left side of thechart is based on preferred dates for variousboundaries as discussed below. For com-parison the dates used by Harland et al.(1982) for the various boundaries are givenon the right side of column 1. Generally morereliance has been placed on Australianisotopic dates, where the geological settingand detailed local biostratigraphy are betterunderstood. The ages of the stage boundariesused here are as follows:-

Famennian/Tournaisian^354 MaFrasnian/Famennian^364 MaGivetian/Frasnian^370 MaEifelian/Givetian^380 MaEmsian/Eifelian^387 MaPragian/Emsian^397 MaLochkovian/Pragian^402 MaPridoli/Lochkovian^408 Ma

DEVONIAN-CARBONIFEROUS BOUNDARYA date younger than 360 Ma better accom-modates the Carboniferous data (Jones1988), and is supported by evidence fromeastern Victoria (Richards & Singleton 1981;Williams eta/. 1982; Odin 1985b). Here, datedgranites (360-366 Ma) intrude the CerbereanVolcanics (Frasnian; see below) and are un-conformably overlain by the MansfieldGroup, possibly Late Devonian in its lowerbeds, and containing a Carboniferous fishfauna in its middle part (Marsden 1976, p.109; Odin & Gale 1982, p. 495). The fishfauna is currently being revised, and containsseveral endemic taxa (see Long & Campbell1985; Long 1988a, 1989), but is most consis-tent with an Early Carboniferous age (J.A.Long pers. comm.). It should be noted that aDevonian placoderm fauna said to come fromlower in the Mansfield Group (Long 1983a;Long & Campbell 1985, p. 87) is the SouthBlue Range fauna of Hills (1936), which liesbeneath a major tectonic break in theKevington Creek Beds, and is not part of the

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Mansfield Group as depicted by Marsden(1976, fig. 5.11). Data from the Scottish Bor-derlands were used by Forster & Warrington(1985) to propose a 365±5 Ma date, but on thesame evidence McKerrow et al. (1985) suggestan age of 354 Ma, which is followed here.Odin (1985a, b) cites evidence from otherareas consistent with the date of McKerrowet al. (1985). Gale (1985) has suggested slight-ly older alternatives (356, 358 Ma).

FRASNIAN-FAMENNIAN BOUNDARYThe lengths of the Late Devonian and its twostages are still poorly confined. Harland et al.(1982) gave the Frasnian and Famennianequal length of 7 Ma, but McKerrow et al.(1985) followed Ziegler (1978) in assigning 20Ma to the Late Devonian, with the Famen-nian slightly longer (11 Ma) than the Fras-nian. However there are no reliable isotopicdata for the Frasnian-Famennian boundary.Odin (1985a) cautioned against using ex-trapolation to propose ages for stage boun-daries. Sandberg et al. (1983) interpreted theFamennian as considerably longer than theFrasnian, on the assumption of approximate-ly equal lengths of Late Devonian conodontzonal timespans. With the Frasnian-Famen-nian boundary placed at the base of the mid-dle Palmatolepis triangularis conodont Zone(Ziegler & Klapper 1985), the Famenniancomprises 20 conodont zones, and the Fras-nian 8, but this difference is partly due to lackof subdivision of some Frasnian zones (theAncyrognathus triangularis Zone may have aduration of up to 1 Ma; Sandberg et al. 1988,fig. 4). The biostratigraphic evidence sug-gests however that the Famennian waslonger than the Frasnian (cf. Odin & Gale1982, p. 494), and on the chart the Famen-nian is assigned an arbitrary length of 10 Ma,which allows a convenient 0.5 Ma per con-odont zone for the Famennian, as estimatedby Sandberg & Poole (1977). This has beensuggested as an average duration, with in-dividual zones ranging perhaps from as shortas 0.3 to up to 0.7 Ma (Sandberg et al. 1988),although it is not possible to take account ofsuch variations in a chart of this nature.

GIVETIAN-FRASNIAN BOUNDARYMcKerrow et al. (1985) proposed the samedate (374 Ma) as Harland et al. (1982), withinthe 375-1-5 Ma suggested by Gale (1985). Inthe recent literature this boundary is con-

sidered well constrained on the Australianevidence (Williams et al. 1982) from the Cer-berean Volcanics of Victoria (a minimum367±2 Ma for the pre-late Frasnian), and theMount Morgan Tonalite of Queensland(369±5 Ma). The latter intrudes Givetianand is overlain by Frasnian strata, and Pick-ett (1972, p. 462) noted that some localities inthe intruded Capella Creek Beds suggestedGivetian, and others basal Frasnian ages. Areassessment of the conodont fauna in theoverlying Dee Volcanics (Druce 1970, 1974)places it in the early Frasnian Polygnathusasymmetricus Zone (Mawson et al. 1985).This more closely confines the isotopic dateto the Givetian-Frasnian boundary than hasbeen assumed in the recent literature (cf.McKerrow eta/. 1985; Gale 1985). According-ly a younger age than 374 Ma is consideredappropriate. The preferred date of 370 Magives a convenient average length of 0.75 Mafor Frasnian conodont zones, and a totalduration for the Late Devonian (16 Ma)which lies between the values (14 and 20 Ma)used by other authors.

MIDDLE DEVONIANMcKerrow et al. (1985) by extrapolation es-timate the Middle Devonian at 17 Ma dura-tion, with the Givetian (9 Ma) slightly longerthan the Eifelian. This is longer than theHarland et al. (1982) Middle Devonian (13Ma), but comparable with the 16 Ma estimateof Ziegler (1978). All agree that the Givetianis the longer stage. There are no isotopic datato constrain the Eifelian-Givetian boundary,but Richards & Singleton (1981, p. 405)report intrusions dated at 381±7 Ma whichare younger than deformed Emsian strataand the post-Emsian deformation, and olderthan the Late Devonian volcanics. This isconsistent with the date selected here, as isGale's (1985) 385±8 Ma date for the Middle-Lower Devonian boundary. Accepting Mc-Kerrow et al.'s (1985) length of 17 Ma for theMiddle Devonian allows retention of Harlandet al.'s (1982) 380 and 387 Ma dates for thebase of the Givetian and Eifelian respective-ly.

EARLY DEVONIANDuration of Early Devonian stages has beenextrapolated from the Siluro-Devonianboundary date (see below), because isotopicdata discussed in the recent literature cannot

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DEVONIAN^3

• be accurately correlated with the stage boun-daries or faunal zonation. For exampleDevonian strata within the Mathinna beds ofeastern Tasmania are dated within the sul-catus and lower kindlei conodont Zones(Pragian) on a diverse invertebrate as-

• semblage including graptolites (falcariusZone; Rickards & Banks 1979) anddacryoconarids (early late Pragian; Banks &Baillie 1989). However overlying volcanicslimiting the age of deformation of the fos-siliferous strata (Turner et al. 1986) are dated

• isotopically at 388±1 Ma, which is probablyat least four conondont zones younger (ap-proximately serotinus Zone; late Emsian).

Harland et al. (1982) assigned equal lengthsof 7 Ma to the three Early Devonian stages,

• but palaeontological assessment of duration(Ziegler 1978) suggests that the Emsian andpre-Emsian were approximately of equallength. The selected durations (10, 5, 6 Ma)for the Emsian, Pragian, and Lochkovian ap-proximate to the relative durations of Early-

• Middle Devonian stages assessed by Ziegler(1978).

For the Siluro-Devonian boundary Owen &Wyborn (1979, P. 40) suggested a 410 Madate, based on intrusions (e.g. JacksonGranite; op. cit., table 1) into strata (Moun-tain Creek Volcanics) underlying fos-siliferous limestones ofdehiscens to serotinusZone age (Emsian). A maximum age of ear-liest Devonian is provided by the early Loch-kovian conodont Icriodus woschmidti in theElmside Formation of the Bowning Group(Link & Druce 1972), which is older than theBowning event. The dated granites (Rb/Sr400-406, on the Boggy Plain igneous suite,inferred on similar chemical characteristicsto include the Mountain Creek Volcanics; seeWyborn, Turner & Chappell 1987) areyounger than the Bowning event, and aretherefore of Devonian, pre-Emsian age. Thisis consistent with the 420±2 Ma LaidlawVolcanics date for the base of the Ludlow(Wyborn et al. 1982), the 398±7 Ma minimumage for the Siluro-Devonian boundary sug-gested by Jones et al. (1981), and the pre-Pragian 402 Ma date from the Gocup Granite(Richards et al. 1977). However it excludesthe 401 Ma suggested boundary date of Joneset al. (1981) and the younger end of the range(395 to 410 Ma) for the boundary of Gale

(1985). Odin (1985a, p.96) quotes three otherradiometric studies indicating a boundaryclearly older than 400 Ma. Other evidence(e.g. the Katandin Batholith in Maine intrud-ing Oriskany (Pragian) rocks; McKerrow etal. 1985; Kirchgasser et al. 1985) might pointto an older age for the boundary than theHarland et al. (1982) date of 408 Ma. TheHarland et al. date is somewhat younger thanthe 412 Ma of McKerrow et al. (1985), but isconsistent with the relevant isotopic datalisted by Gale (1985, p. 86). It is retained herefor convenience as a close approximation tothe reliable date of Owen & Wyborn (1979).

COLUMN 2-STAGESStage names used for the Devonian are thoserecently decided (Bassett 1985) by the Sub-commission on Devonian Stratigraphy(SDS). The name `Tournaisian' is restrictedto the Carboniferous, although 'zones' Tn1aand Tnlb are shown as part of the lateFamennian (see Jones 1985).

COLUMN 3- CONODONTSThis zonation is the current internationalstandard on which Devonian stage boun-daries as decided by the SDS were defined byZiegler & Klapper (1985) as follows:

base of Famennian - lower boundary of Mid-dle Palmatolepis triangularis Zone

base of Frasnian - lower boundary of LowerPolygnathus asymmetricus Zone

base of Givetian - lower boundary of Polyg-nathus ensensis Zone

base of Emsian - lower boundary of PoIyg-nathus dehiscens Zone

base of Pragian - lower boundary of Eog-nathus sulcatus Zone

base of Lochkovian - (approximate) lowerboundary of Icriodus woschmidti Zone

The base of the Lochkovian corresponds tothe Siluro-Devonian boundary, which is for-mally defined at the base of the Monograptusuniformis Zone (McLaren 1973; i.e. slightlybelow the first appearance of I. woschmidti).Lower boundaries for the Pragian, Emsian,and Givetian stages are still subject to discus-sion within the SDS, but those used here arecurrently most widely accepted. The Fras-

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nian-Famennian boundary is problematic,the previous recommendation (Ziegler &Klapper 1985), as used here (lower boundaryof the Middle Palmatolepis triangularisZone), having been withdrawn, because ofdifficulty in identifying the base of this zone.Current discussion within the SDS concernsplacement at the base of either the Lower orUpper Palmatolepis triangularis Zones. Inview of this uncertainty the earlier sugges-tion for this boundary (Ziegler & Mapper1985) has been retained for the present on thechart.

For the Famennian the Palmatolepis-basedsubdivision proposed by Ziegler & Sandberg(1984) is used. The subdivisions (Fala-Tnlb)for the Famennian - `Strunian' part of theBelgian succession (Dinant Basin) are shownas picks down the left margin following therecent scheme of Conil et al. (1986). Howeverthis places the base of Fa2d at a higher levelthan previously suggested (see discussion inJones 1985). The `Strunian' as used by Conilet al. (1986) comprises Fa2d, Tnla, and thelower part of Dab.

A discussion of recent research on theDevonian-Carboniferous boundary is givenin Flajs et al. (1988). Recent work on Dev-onian conodont zonation of Australian se-quences is presented by Mawson et al. (1985),and Mawson (1987), and conodont datedtransgression-regression cycles in Australiansequences were recently discussed by Talent& Yolldn (1987).

COLUMN 4CONODONTSOn the left equivalent Famennian conodontzones from the previous international zonalscheme of Ziegler (1962, 1971) are given, forcomparison with the Palmatolepis zonationof column 3. On the right is the scheme usingshallow-water icriodid species as summarisedby Sandberg & Dreesen (1984).

GRAPTOLITESThe Monograptus zonation for the EarlyDevonian is modified from Garratt (1983).This was based on Victorian sequences, andmay not be applicable elsewhere (L. Sherwin,pers. comm.). Jenkins (1982) has discussedthe relationship between graptolite and con-

dont zones near the Siluro-Devonian bound-ary in the Yass area.

COLUMN 5- AMMONOIDSThe standard ammonoid zonation for the lat-ter half of the Devonian (Maenioceras Stufenand above) is tied in with the conodontscheme following mapper & Ziegler (1979,fig. 8), House et al. (1985), and the discussionsin Ziegler & mapper (1985) and Klapper et al.(1987). For the Australian DevonianGlenister (1958) described the Frasnian am-monoids, and Petersen (1975) the Famennianammonoids from the Canning Basin. Four ofthe five classic German 'Stufen' for theUpper Devonian are developed in the Can-ning Basin, and conodont zone equivalentshave been recognised for the Wocklumeria-Stufe, which is not represented by ammonoidmaterial (Petersen 1975).

The older Anarcestes and Anetoceras Stufeapproximate to the Eifelian and Emsianrespectively (House 1979), but neither isknown from Australia, and a detailed zona-tion in relation to conodonts is not yetworked out. Cabrieroceras (Anarcestes-Stufe) is known from Australia (J.A. Talent,pers. comm.). The type localities forAustralian species Talenticeras talenti Erbenand Teicherticeras teicherti Chlupac & Turekfrom the Buchan Caves Limestone fall withinthe dehiscens and perbonus Zones respective-ly (Mawson et at. 1985). Talenticeras is veryclose to Anetoceras (House 1987), which isconsistent with the Emsian range of the lat-ter in Europe.

COLUMN 6- BRACHIOPODSZones of Veevers (1959) for the Middle-LateDevonian of the Canning Basin are shown asinterpreted by Roberts et al. (1972). The topof the Stringocephalus zone is placed abovethe base of the disparilis conodont Zone(Mawson et al. 1985), which leaves a gapbeneath the saltica brachiopod zone. Theyoungest Early Devonian zone (Spinella-Buchanathyris) is equivalent to assemblageIV of Strusz (1972), and correlates with thedehiscens conodont Zone (A.J. Wright, pers.comm.). Beneath this on the left are shownthe Boucotia zones of Garratt (1983). These

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CORALSStrusz (1972) and Pickett (1972) discussedthe coral-conodont faunal scheme of Philip &Pedder (1967) for the Early-MiddleDevonian, and the eleven zones A-K as usedthen are given here, with minor revision(Carlinastrea halysitoides replaces the'Spongophyllum' zone; see Pedder 1985). Nostratigraphic scheme was provided in thework of Hill & Jell (1970) on corals of Middle-Late Devonian age from the Canning Basin.

COLUMN 8

recorded from Australia (Jones 1968, 1974),they are very poorly known. Included on thechart are the local zones of Jones (1968, 1989)based on benthic ostracods from the LateDevonian of the Bonaparte Basin. TheFamennian zones are now known (Playford1982; Jones 1985) to cover only the latestFamennian (?Fa2c - Tnla). They correspondapproximately to assemblage A of Jones (inVeevers & Wells 1961), recorded from the'Fairfield Group' (now Gumhole Formation)in the Canning Basin. The itanaicus' zoneoccurs in the Westwood Member (late Fras-nian) of the Cockatoo Formation (Jones1968).

DACRYOCONARIDSThe scheme of Lutke (1979), which relates 12named dacryoconarid zones to the standardconodont zonation, is summarised for theEarly and Middle Devonian in column 8, withextra zones for the Lochkovian-Pragian in-terval added from Chlupac et al. (1985). Moredetailed dacryoconarid zonations are avail-able (18 named zones are used by Alberti1984) but precise correlation for some ofthese with conodont zones is not available. InAustralia, Sherrard (1967) recorded Nowakiaaff. . acuaria from the Garra Formation(pesavus-dehiscens Zones; Strusz 1972), andlower Taemas Formation (dehiscens-serotinus Zones; Mawson et al. 1985) in NewSouth Wales, and N. acuaria is widely dis-tributed in the Lower Devonian of the Mel-bourne Trough (Garratt 1983). Theseoccurrences are consistent with Lutke'sscheme. Stratigraphically significantdacryoconarids in the Taravale Formation inVictoria are noted by Mawson et al. (1985) butdetails of zonation are not yet available.Abundant dacryoconarids indicative of anearly late Pragian age, including Viriatellinasp., Metastyliolina sp. and Nowakia mattock-iensis, occur in the Mathinna beds of Tas-mania (Banks & Baillie 1989, p. 236).

COLUMNS 9,10 - VERTEBRATESThe oldest Devonian fish remains inAustralia dated by conodonts are scales of theacanthodian Nostolepis in the Coopers CreekFormation, which contains conodonts of theearly Pragian sulcatus Zone (Philip 1965;Klapper & Ziegler 1979). The Tumblongmicrofauna described by Pickett, Turner &

• are based on Victorian sequences, and are notreadily applied to the shallow water as-semblages of western New South Wales (L.Sherwin, pers. comm.). An informal zonationbased on assemblages (Sherwin 1980) hasproved useful in this area, but much

• taxonomic work is required before a formalzonal scheme can be proposed. Sherwin (inGlen et al. 1985, figs. 10, 11) outlined aninformal scheme of five assemblage zones forthe Cobar Supergroup of western New SouthWales which is included on the right side of

• column 6, with Spinella characterising hisyoungest faunal assemblage. Most of the taxain these assemblages are either undescribed,or in need of revision. For a recentmonographic treatment of AustralianDevonian brachiopods see Lenz & Johnson

• (1985a, b).

COLUMN 7BRACHIOPODS

• The five Famennian productid zones of Mc-Kellar (1970) from the Star. Basin inQueensland are given, as modified by theconodont work of Pickett (1981), whodemonstrated that the boundary betweenMcKellar's profunda and minuta zones lay

• within the Lower marginifera conodontZone. The five brachiopod zones are thereforeplaced at a lower level than interpreted byMcKellar (1970). The relationship of thesezones to the Tournaisian tenuistriata Zone isdiscussed by Roberts (1975).

OSTRACODSMost useful biostratigraphically (e.g. Gooday

• & Becker 1979) are the pelagic entomozoanostracods, but although these have been

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Myers (1985) contains similar Nostolepisscales, associated with the thelodont Turiniaand shark scales (Ohiolepis). Ohiolepis is wellknown in the Taemas-Buchan fauna, sug-gesting a slightly younger age than theCoopers Creek fauna for the Tumblongfauna. The Silverband fauna from the Gram-pians (Turner 1986) is of possibly equivalentage or older, based on the presence of T.fuscina, a primitive species of Turinia.Isotopic dates for associated intrusive rocksindicate a yougest possible age for the Gram-pians Group of 400±3 Ma (Warren et al.1986). More widespread is Turiniaaustraliensis, reported by Turner (1984, andpers. comm.) from the Yarra Yarra CreekGroup, Talingaboolba Formation, MineralHill Volcanics, Belvedere Formation, Con-dobolin Formation, Trundle Group andGarra Formation in New South Wales, theGraveyard Creek Formation and MartinsWell Limestone in the Broken River area ofQueensland, and the Point Hibbs Limestonein Tasmania. The Martins Well Limestone islate Lochkovian-early Pragian (pesavus-sul-catus Zones; Mawson et al. 1985), as is theGarra Formation (Strusz 1972), and theGraveyard Creek Formation is slightly older(Wyatt & Jell 1980). Other occurrences datedby conodonts or invertebrate macrofossils arethe Lochkovian Mineral Hill Volcanics,Talingaboolba Formation, Condobolin For-mation, and Trundle Group (Sherwin 1980),and the Point Hibbs Limestone (sulcatusZone). Thus there is good evidence that mostof these occurrences are Emsian or older, incontrast to the T. australiensis from theMulga Downs Group and Cravens Peak Beds(Turner et al. 1981), which must be younger(see below). This apparent discrepancy maybe due to the fact that the latter occurrencesare in very near-shore to non-marine facies.

The Taemas-Buchan assemblage is an abun-dant and diverse fauna of Emsian age (dehis-cens to serotinus Zones). Cheiracanthoides,Ohiolepis, Ohioaspis, Ligulalepis, 'Skarn-olepis' , buchanosteid and acanthothoracidscales etc. occur in the microfauna. The mac-rofauna contains abundant and diverseplacoderms (arthrodires exemplified byBuchanosteus, various acanthothoracids,petalichthyids and ptyctodontids),lungfishes, acanthodians, onychodontids,and porolepiforms (see Young 1981, 1985b;

Long 1984a, 1986). The distinctive palaeonis-coid Ligulalepis is also known from the Con-dobolin Formation, is associated withSkamolepis in the Jesse Limestone (Turner1982a), and has been provisionally identifiedin the Early Devonian of Western Australia(Turner et al. 1981).

A maximum age for the Wuttagoonaspisfauna of the Mulga Downs Group in westernNew South Wales (Ritchie 1973) is providedby the underlying marine Cobar Supergroup.Pickett (1980) identified conodont faunasranging from woschmidti to dehiscens or per-bonus Zones, but more recent studies havenot corroborated the presence of Polyg-nathus, so the younger date may not be reli-able (J. Pickett, pers. comm.), and the CobarSupergroup is probably older than any Polyg-

nathus zone. At its oldest, therefore, the Wut-tagoonaspis fauna is possibly contempor-aneous with the upper Taemas-Buchanfauna, and may extend into the MiddleDevonian. This fauna was apparentlywidespread in Australia, and is now recordedfrom western New South Wales, and the Can-ning (Gross 1971), Georgina (Turner et al.1981; Young 1984), Amadeus (Young 1985b,1988b; Young et al. 1987) and Officer Basins(Long et al. 1988).

Other Eifelian faunas are poorly representedand/or poorly known. The Hatchery Creekfauna was assigned a late Eifelian age byYoung & Gorter (1981), but may be younger(see below). Eifelian fishes in the BrokenRiver sequence include large brachythoracidarthrodires, asterolepid antiarchs etc.Microfaunas contain turiniid thelodonts andcheiracanthid and machaeracanthid acan-thodians (Turner 1982a, 1986, and pers.comm.). An isolated placoderm or dipnoanplate from the subsurface (Bury Limestonemember of the Log Creek Formation) in theAdavale Basin resembles material in both theTaemas-Buchan and Broken River faunas.Recovery of vertebrate microfossils from thissequence has not yet been attempted.Givetian faunas also occur in marine lime-stones of the Broken River sequence, and theHatchery Creek is a non-marine fauna inwhich bothriolepid antiarchs (Monarolepis)and turiniid thelodonts are associated withasterolepids, phlyctaeniid arthrodires etc.This association is unique, and a Middle

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DEVONIAN^7

• Devonian age is probable, representing over-lap in stratigraphic range of freshwaterturiniids with the earliest bothriolepid an-tiarchs. Another, probably younger(?Givetian-Frasnian), turiniid occurrence isAustralolepis in the marine Gneudna Forma-tion, Western Australia (Turner & Dring1981), where it is associated with the lungfishChirodipterus australis (Smith & Campbell1987).

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For Late Devonian non-marine fish faunasthe bothriolepid antiarch Bothriolepis is com-mon and widely distributed (e.g. Long 1983a;Long& Turner 1984; Long & Werdelin 1986).Its earliest well-dated Australian occurrenceis in the basal Frasnian Gogo Formation ofthe Canning Basin (Young 1974), but anolder first appearance is possible, as in China(Eifelian). On the chart a first appearance inthe Givetian varcus Zone is assumed, as isdemonstrated in Euramerica (Young 1988a).In southeastern Australia the downwardrange of associated placoderms Pambulaspis,Austrophyllolepis, and Placolepis, and theacanthodian Culmacanthus (Long 1983b,1984b; Ritchie 1984; Young 1983, 1989) is notknown, but they are unlikely to extend farbeneath the Givetian-Frasnian boundary. Aswell as Bothriolepis, the diverse fish faunafrom the Gogo Formation (Long 1988b) con-tains various genera (Holonema, Griphog-nathus, Holodipterus, Chirodipterus, Moy-thomasia) which overseas are generally in-dicative of a Givetian-Frasnian age (e.g. Gar-diner & Miles 1975). Abundant marinemicrofaunas are also known from the earlyLate Devonian, but except for the Gneudnaassemblage (see above), faunal content is notyet documented.

the latest Famennian (Yellow DrumSandstone; Young 1987), but neither Phyl-lolepis nor Groenlandaspis has yet beenrecorded from the west. Famennianmicrofaunas from marine rocks in the Can-ning include osteichthyans and elas-mobranchs (J.A. Long, pers. comm.). InQueensland the elasmobranchs Har-pagodens, Protacrodus, and Phoebodus arerecorded by Turner (1982b), the last tworeferred on conodonts to the marginiferaZone (Pickett 1981).

COLUMNS 11,12 -PALYNOMORPHS

Column 12 summarises two recently publish-ed zonal schemes for the Old Red SandstoneContinent (Richardson & McGregor 1986),and the Ardenne-Rhenish region of Europe(Streel et al. 1987). Both works providedetailed integration with the standard con-odont zonation for the marine Devonian. Aninformal Australian scheme is given incolumn 11, which is based for the Early-Mid-dle Devonian on the work of de Jersey (1966)and unpublished reports by Price (1980) andPrice et al. (1985) on the subsurface sequencein the Adavale Basin. This work has beenrecently discussed in a study ofpalynomorphs from the Gneudna Formationin Western Australia by Balme (1988). Theunpublished work is not supported by sys-tematic studies and remains to be tested inother areas. Geminospora lemurata in theEtonvale Formation suggests an ageequivalent to the varcus Zone or younger (seebelow), and comparison with detailed recentwork on plant microfossils from the GneudnaFormation supports de Jersey's (1966) con-clusion that the highest levels are Middlerather than Late Devonian in age (Balme1988). Beneath this assemblage Price et al.(1985, table 6) list five informal zones astentatively shown in the lower part of thecolumn. The PD2 and lower PD3 zones areassigned to the Early Devonian. Macrofossilevidence from the Log Creek Formation indi-cates a possible Emsian but more probablyEifelian age (Pickett 1972).

The highest palynostratigraphic unit of Price(1980), in the uppermost part of the EtonvaleFormation, probably corresponds to the op-tivus-triangulatus Zone of Richardson & Mc-

• In the Famennian a Bothriolepis-Phyllolepis-Remigolepis- Groenlandaspis association istypical in non-marine rocks of easternAustralia (e.g. Hervey Group, MerrimbulaGroup in central and southeastern New.South Wales, Trapyard Hill fauna in eastern

• Victoria), and also occurs in central Australia(upper Dulcie Sandstone in the GeorginaBasin; Young 1988b). A sinolepid antiarchassemblage (including Bothriolepis andRemigolepis) may represent the youngestFamennian nonmarine assemblage, as it does

• in China (Pan 1981; Pan & Dineley 1988).Antiarchs in the Canning Basin extend into

•8^G.C. YOUNG

Gregor (1986), if systematic studies confirmthe provisional identifications (Balme 1988,p. 160). This indicates a late Givetian age.This zone contains Geminospora lemurata, ataxon reviewed by Playford (1983), who sug-gested a total range from the varcus Zone(middle Givetian) or younger, through theFrasnian and possibly into the early Famen-nian. Balme (1988, fig. 8) has suggested adifferent range, from Eifelian to middle Fras-nian, with a doubtful younger extension intothe basal Famennian. McGregor (1979, fig. 8)estimated a much greater (Emsian-Famen-nian) range for the possibly synonymous G.svalbardiae. Geminospora sp. is listed byAnan-Yorke (1975) from the FrasnianBellbird Creek Formation of the MerrimbulaGroup, and G. lemurata is abundant in theBrewer Conglomerate palynoflora of theAmadeus Basin (Playford et al. 1976), but isabsent from the Gogo Formation in the Can-ning Basin (Grey 1975; Balme 1988). TheBrewer palynoflora also contains six species(Grandispora clandestina, Hystricosporitesporrectus tc.) in common with the lateFamennian Fairfield Formation palynofloraof the Canning Basin (Playford 1976). UsingPlayford's (1983) assessment of the range ofG.lemurata, the Brewer assemblage would beplaced in the early Famennian, but alterna-tively the clear late Famennian elementmight indicate that G. lemurata is reworkedin this assemblage (Balme 1988).

Late Devonian acritarchs were listed fromsoutheastern Australia (Merrimbula Group)by Anan-Yorke (1975), and described fromthe Fairfield Group and Gneudna Formationin the west by Playford (1976, 1981) andPlayford & Dring (1981). From the FrasnianBellbird Creek Formation Anan-Yorke(1975) listed seven genera (Evittia, Maran-hites, Navifusa, Stellinium, Tunis-phaeridium, Veryhachium, Cymatiosphaera)and one species (Multiplicisphaeridiumramusculosum) which also occur in theGneudna Formation (Playford & Dring1981). Downie (1979) lists Maranhites asage-diagnostic for the Late Devonian.Playford & Dring (1981, p. 74) considered theassociation of Chomotriletes vedugensis,Daillydium pentaster , Unellium piriforme, U.winslowae, and Cymatiosphaera peri-membrana as the best evidence of a Frasnianage for the Gneudna Formation. For the

younger (Famennian) Worange Point Forma-tion of the Merrimbula Group only twogenera (Cymatiosphaera, Stellinium) arecommon to the Fairfield Group assemblage.

The Retispora lepidophyta assemblage in theCanning Basin is associated (Playford 1976,p. 8) with the Icriodus platys conodont as-semblage of Nicoll & Druce (1979). I. platys isa junior synonym of I, raymondi, which dis-appears at the top of the Middle expansa Zone(Sandberg & Dreesen 1984). Playford (1982,p. 155) cites opinion that the first appearanceof R. lepidophyta postdates the middlestyriacus Zone (equivalent to the base of theexpansa Zone). On this evidence the 'I,platys' association in the Canning Basin mustbe near the base of the range of R.lepidophyta, and the base of this assemblagezone is placed at the base of the Middle expan-sa Zone. This is somewhat older than thelevel given in Conil et al. (1986; within theUpper expansa Zone), but compares well withthat ofPaproth & Street (1979; just above thebase of the Lower costatus Zone).

COLUMN 13 - MACROPLANTSThe Wilson Creek Shale in the MelbourneTrough contains the type locality of Barag-wanathia longifolia, lycophyte and key mem-ber of the Baragwanathia Flora. This shalehas been correlated with the Humevale For-mation which also contains elements of theFlora in the Yea and Lilydale districts. Gar-ratt (1983) placed this in the Boucotialoyolensis Assemblage Zone (early Pragian,sulcatus Zone). Best preserved material oc-curs in the Turtons Creek inlier (LiptrapFormation), correlated by VandenBerg(1975) with the Norton Gully Sandstonewhich also contains the assemblage in theupper Yarra area. Further details on theBaragwanathia Flora are included in Gould(1975), Hueber (1983), and Tims & Chambers(1984). Early Devonian vascular plants in-cluding Baragwanathia and Hostimella arealso reported from Tasmania (Banks & Bail-lie 1989).

In the Middle Devonian the lycopodsProtolepidodendron lineare, P. yalwalense,and ?Lepidodendron clarkei are recordedfrom possible Givetian sediments insoutheastern New South Wales. Chaloner &

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•

The most widespread Late Devonian lycopodin Australia is Leptophloeum australe, whichis however recorded from rocks of possibleEmsian age (Gould 1975) beneath the Sulcor

• Limestone (mainly Eifelian; Mawson et al.1985) in the Yarrimie Formation of the NewEngland fold belt. In view of the typical LateDevonian occurrence elsewhere (e.g.Chaloner & Sheerin 1979), field relationshipsof this occurrence require checking. L.australe is also recorded from probable EarlyCarboniferous rocks in the Canning Basin(Veevers et al. 1967), and associated withTournaisian brachiopods in New SouthWales (Jones et al. 1973). A more diverse LateDevonian flora from eastern Victoria, sum-

• marised in Marsden (1988), also includes L.australe in probable Frasnian and Famen-nian assemblages. Other genera in the AvonRiver Group include ?Asterocalamites, Ar-chaeopteris, Sphenopteris, and Rhacopteris.Phyllotheca occurs in the Moroka Glen For-

• mation, Taeniocrada in the WellingtonRhyolite, and Cordaites, Sphenopteris, andArchaeopteris in the Mount Kent Con-glomerate and Snowy Plains Formation. As-sociated fishes (Long 1983a) indicate thatthese occurrences are probably Frasnian, ex-cept for the Snowy Plains Formation(Famennian). The Genoa River Beds(Famennian) also contain Leptophloeum,Cordaites, Archaeopteris, Sphenopteris, andBarinophyton?, the last-mentioned having awide (Emsian-Famennian) range according

• to Chaloner & Sheerin (1979).

OTHER GROUPSVarious other macro- and microfossil groups

• have proved biostratigraphically useful over-seas, but have not yet been studied in suffi-cient detail for their utility in Australian

•

DEVONIAN^9

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•

Sheerin (1979) give Protolepidodendron anEmsian-Givetian range. Pr. scharianum isrecorded with Astralocaulis in the FrasnianDotswood Formation of Queensland (Gould1975). Chaloner & Sheerin (1979) considerAstralocaulis to have a Givetian-Frasnianrange. Other Frasnian records fromAustralia are ?Cordaites and ?Archaxosigil-laria listed from the Twofold Bay Formationby Fergusson et al. (1979), the latter havinga Givetian-Tournaisian range according toChaloner & Sheerin (1979).

Devonian sequences to be assessed. Devonianprotozoans (Radiolaria and Foraminifera)were discussed by Toomey & Mamet (1979).Radiolarians have potential bio-stratigraphicvalue for Upper Devonian strata, andHoldsworth & Jones (1980) put forward apreliminary zonation. Late Devonian (Fras-nian) Radiolaria from the Gogo Formation ofthe Canning Basin were described byNazarov et al. (1982) and Nazarov & Ormis-ton (1983), and they have recently been usedto date siliceous rocks from the New EnglandFold Belt (Ishiga et al. 1988; Aitchison 1989).Calcareous Foraminifera underwent theirfirst major radiation in the late MiddleDevonian, and with agglutinated forms havebio-stratigraphic potential for the UpperDevonian, although much taxonomic work isrequired to sort out both groups (Toomey &Mamet 1979). Conkin & Conkin (1968)described Upper Devonian Foraminiferafrom Western Australia. Teichert et al. (1979)summarised the biostratigraphic distribu-tion of some 209 nautiloid genera thought tobe restricted to the Devonian. Over half ofthese are recorded from only onestratigraphic stage or finer stratigraphic sub-division, indicating significantbiostratigraphic potential. Trilobites haveproved valuable in world-wide correlation ofLower and Middle Devonian strata (Alberti1979). Recent systematic studies onAustralian Devonian trilobites include Chat-terton et al. (1979), Holloway & Neil (1982),and Chatterton & Wright (1986). Amongstother arthropods only eurypterids, con-chostracans and phyllocarids are sufficientlyabundant to yield biostratigraphic data(Rolfe & Edwards 1979). Briggs & Rolfe(1983) described phyllocarids from WesternAustralia. The biostratigraphic utility ofthese and other groups in Australian sequen-ces will depend on detailed systematics beingcarried out to provide a basis for determiningthe ranges of described taxa.

ACKNOWLEDGMENTSMany colleagues have assisted in the compila-tion of this chart. For much advice on con-odont and ostracod zonation, and particularproblems related to the Devonian-Car-boniferous boundary, I am indebted to Dr P.J.Jones (BMR). For helpful comments on anearly version of the chart I thank Dr B. Balme

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10^GC. YOUNG

(University ofWA.), Dr J. Douglas (VictorianDept Mines), Dr J. Long (University of Tas-mania), Dr J. Pickett and Mr L Sherwin(New South Wales Dept. of Mines), Dr G.Playford and Dr J. Jell (University ofQueensland), Professor J. Talent and Dr R..Mawson (Macquarie University), Dr S.Turner (Queensland Museum), Dr B. Webby(University of Sydney), and Dr A. Wright(University of Woolongong). Drs I. Williamsand J. Claoue Long discussed isotopic data,and Professor J. Talent, Dr R. Mawson (Mac-quarie University), Dr E.M. Truswell, Dr D.Strusz (BMR), and Dr N. Morris (Universityof Newcastle) provided information on con-odont, macroplant, and brachiopod occurren-ces respectively. Mr P. Brown drafted thechart, and Drs M. Owen and R. Ryburnprovided computing advice and assistance.

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BALME, B.E. 1988—Miospores from LateDevonian (early Frasnian) strata, Car-narvon Basin, Western Australia.Palaeontographica B209, 109-166.

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• DRUCE, E.C. 1974—Australian Devonianand Carboniferous Conodont faunas. inBOUCKAERT, J. & STREEL, M.(Editors). International Symposium onBelgian Micropalaeontological limitsfrom Emsian to Visean. Namur, Publica-

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McKELLAR, R.G. 1970—The Devonianproductoid brachiopod faunas ofQueensland. Publications of the Geologi-cal Survey of Queensland, Palaeontologi-cal Papers, 18, 1-40.

McKERROW, W.S., LAMBERT, R.ST.J., &COCKS, L.R.M. 1985—The OrdovicianSilurian and Devonian Periods. InSNELLING, N.J. (Editor) The Chronol-ogy of the Geological Periods. Memoirs ofthe Geological Society of London, 10, 73-80.

McLAREN, D.J. 1973—The Siluro-DevonianBoundary. Geological Magazine 110,302-303.

NAZAROV, B.B., COCKBAIN, A.E. &PLAYFORD, P.E. 1982—UpperDevonian Radiolaria from the Gogo For-mation, Canning Basin, WesternAustralia. Alcheringa 6, 161-174.

NAZAROV, B.B. & ORMISTON, A.R. 1983—Upper Devonian (Frasnian) radiolarianfauna from the Gogo Formation,Western Australia. Micropalaeontology29, 454-466.

NICOLL, R.S. & DRUCE, E.C. 1979—Con-odonts from the Fairfield Group, Can-ning Basin, Western Australia. Bureau

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of Mineral Resources, Australia Bulletin190.

ODIN, G.S. 1985a—Remarks on the numeri-cal scale of Ordovician to Devoniantimes. In SNELLING, N.J. (Editor) TheChronology of the Geological Periods.Memoirs of the Geological Society of Lon-don, 10, 93-98.

ODIN, G.S. 1985b—Comments on thegeochronology of the Carboniferous toTriassic times. In SNELLING, N.J.(Editor) The Chronology of the Geologi-cal Periods. Memoirs of the GeologicalSociety of London, 10, 114-116.

ODIN, G.S. & GALE, N.H. 1982. Numericaldating of Hercynian times (Devonian toPermian). pp. 487-500, In ODIN, G.S.(Editor) Numerical Dating in Stratig-raphy. John Wiley and Sons.

OWEN, M. & WYBORN, D. 1979—Geologyand geochemistry of the Tantangara andBrindabella area. Bureau of MineralResources Australia, Bulletin, 204.

PAN J. 1981—Devonian antiarch biostratig-raphy of China. Geological Magazine,118, 69-75.

PAN, J. & DINELEY, D.L. 1988—A review ofearly (Silurian and Devonian) vertebratebiogeography and biostratigraphy ofChina. Proceedings of the Royal Societyof London, B235, 29-61.

PAPROTH, E., & STREEL, M. 1979—TheDevonian-Carboniferous boundary inwestern Europe. XIV Pacific ScienceCongress USSR. Field ExcursionGuidebook Supplement 8, 155-164.

PEDDER, A.E.H. 1985—Lower Devonianrugose corals of Lochkovian age fromYukon Territory. Geological Survey ofCanada Paper 85- 1A, 587-602.

PETERSEN, M.S. 1975—Upper Devonian(Famennian) ammonoids from the Can-ning Basin, Western Australia. Journalof Paleontology Vol. 49 Supplement.Paleontological Society Memoir, 8, 1-55.

PHILIP, G.M. 1965—Lower Devonian con-odonts from the Tyers area, Gippsland,Victoria. Proceedings of the Royal Societyof Victoria, 79, 95-117.

PHILIP, G.M., & PEDDER, A.E.H. 1967—Acorrelation of some Devonian limestonesof New South Wales and Victoria.Geological Magazine, 104, 232-239.

PICICETT, J. 1972—Correlation of the Mid-dle Devonian formations of Australia.Journal of the Geological Society ofAustralia, 18, 457-466.

PICKETT, J. 1980—Conodont assemblagesfrom the Cobar Supergroup (EarlyDevonian), New South Wales. Alcherin-ga, 4, 67-88.

PICKETT, J. 1981—Late Devonian andEarly Carboniferous conodonts from theMyrtlevale Beds and Hardwick Forma-tion, Star Basin—Queensland Govern-ment Mining Journal, 82, 24-27.

PICKETT, J., TURNER, S. & MYERS, B.1985—The age of marine sediments nearTumblong, southwest of Gundagai.Quarterly Notes of the Geological Surveyof New South Wales, 58, 12-15.

PLAYFORD, G. 1976—Plant microfossilsfrom the Upper Devonian and LowerCarboniferous of the Canning Basin,Western Australia. PalaeontographicaB158, 1-71.

PLAYFORD, G. 1981—Late Devonianacritarchs from the Gneudna Formationin the western Carnarvon Basin,Western Australia. Geobios 14, 145-171.

PLAYFORD, G. 1982—A latest Devonianpalynoflora from the Buttons Beds,Bonaparte Gulf. Basin, WesternAustralia. BMR Journal of AustralianGeology & Geophysics, 7, 149-157.

PLAYFORD, G. 1983—The Devonianmiospore genus Geminospora Balme1962: a reappraisal based on topotypic G.lemurata (type species). Memoirs of theAssociation of Australasian Palaeon-tologists, 1, 311-325.

PLAYFORD, G. & DRING, R.S. 1981—LateDevonian acritarchs from the CarnarvonBasin, Western Australia. Special Papersin Palaeontology, 27, 1-78.

PLAYFORD, G., JONES, B.G., & KEMP,E.M. 1976—Palynological evidence forthe age of the synorogenic Brewer Con-

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Upper Devonian rocks of Australia.Journal of the Geological Society ofAustralia, 18, 467-490.

ROLFE, W.D.I. & EDWARDS, V.A. 1979—Devonian Arthropoda (Trilobita andOstracoda excluded). Special Papers inPalaeontology 23, 325-329.

SANDBERG, CA., & DREESEN, R. 1984—Late Devonian icriodontid biofaciesmodels and alternate shallow-water con-odont zonation. Geological Society ofAmerica, Special Paper. 196, 143-178.

SANDBERG, C.A., GUTSCHICK, R.C.,JOHNSON, J.G., POOLE, F.G., &SANDO, W.J. 1983—Middle Devonian toLate Mississippian geologic history ofthe Overthrust belt region, westernUnited States. Rocky Mountain Associa-tion of Geologists, Geologic Studies of theCordilleran Thrust Belt, 2, 691-719.

SANDBERG, CA., & POOLE, F.G. 1977—Conodont biostratigraphy and deposi-tional complexes of Upper Devoniancratonic-platform and continental-shelfrocks in the western United States. InMURPHY, M.A., BERRY, W.B.N., &SANDBERG, C.A. (Editors). WesternNorth America; Devonian. CaliforniaUniversity, Riverside, Campus MuseumContributions 4, 144-182.

SANDBERG, C.A., ZIEGLER, W.,DREESEN, R. & BUTLER, J.L. 1988—Late Frasnian mass extinction: conodontevent stratigraphy, global changes, andpossible causes. Courier Forschung-sinstitut Senckenberg 102, 267-307.

SHER.RARD, K. 1967—Tentaculitids fromNew South Wales, Australia. Proceed-ings of the Royal Society of Victoria, 80,229-246.

SHERWIN, L. 1980—Faunal correlations ofthe Siluro-Devonian units, Mineral Hill-Trundle, Peak Hill area. Quarterly Notesof the Geological Survey NSW, 39, 1-14.

SMITH, M.M. & CAMPBELL, K.S.W. 1987—Comparative morphology, histology andgrowth of the dental plates of theDevonian dipnoan Chirodipterus.Philosophical Transactions of the RoyalSociety of London (B), 317, 329-363.

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• glomerate, Amadeus Basin, CentralAustralia. Alcheringa, 1, 235-243.

PRICE, P.L. 1980—Biostratigraphy of theDevonian section from selected wells inA to P 232P0, Adavale Basin, Queens-land. Mines Administration Pty, Ltd.Palynology Facility Report No. 208/1(unpublished).

PRICE, P.L., FILATOFF, J. WILLIAMS, A.J.PICKERING, S.A. & WOOD, G.R.1985—Late Palaeozoic and Mesozoic

• palynostratigraphic units. Mines Ad-ministration Pty Ltd., PalynologyFacility Report No 274/25 (unpublished).

RICHARDS, J.R., BARKAS, J.P. & VAL-LANCE, T.G. 1977—A Lower Devonian

• point in the geological time scale.Geochemical Journal, 11, 147-153.

RICHARDS, J.R. & SINGLETON, O.P.1981—Palaeozoic Victoria, Australia: ig-neous rocks, ages and their interpreta-tion. Journal of the Geological Society ofAustralia, 28, 395-421.

RICHARDSON, J.B. & McGREGOR, D.C.1986—Silurian and Devonian sporezones of the Old Red Sandstone Con-tinent and adjacent regions. Geological

• Survey of Canada, Bulletin 364.RICKARDS, R.B. & BANKS, M.R. 1979—An

Early Devonian monograptid from theMathinna beds, Tasmania. Alcheringa 3,307-311.

• RITCHIE, A. 1973—Wuttagoonaspis gen.nov., an unusual arthrodire from theDevonian of Western New South Wales,Australia. Palaeontographica, 143A, 58-72.

• RITCHIE, A. 1984—A new placoderm,Placolepis gen. nov. (Phyllolepidae) fromthe Late Devonian of New South Wales,Australia. Proceedings of the LinneanSociety of N.S.W., 107, 321-353.

ROBERTS, J. 1975—Early CarboniferousBrachiopod Zones of Eastern Australia.Journal of the Geological Society ofAustralia 22, 1-32.

ROBERTS, J., JONES, P.J., JELL, J.S.JENKINS, T.B.H., MARSDEN, MA.H.,

• McICELLAR, R.G., McKELVEY, B.C., &SEDDON, G. 1972—Correlation of the

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STREEL, M. HIGGS, K., LOBOZIAK, S.,RIEGEL, W. & STEEMANS, P. 1987—Spore stratigraphy and correlation withfaunas and floras in the type marineDevonian of the Ardenne-Rhenishregions. Review of Palaeobotany andPalynology 50, 211-229.

STRUSZ, D.L. 1972—Correlation of theLower Devonian rocks of Australasia.Journal of the Geological Society ofAustralia, 18, 427-455.

TALENT, J.A. & YOLKIN, E.A. 1987—Transgression-regression patterns forthe Devonian of Australia and southernWest Siberia. Courier Forschung-sinstitut Senckenberg, 92, 235-249.

TEICHERT, C., GLENISTER, B.F., &CRICK, RE. 1979—Biostratigraphy ofDevonian nautiloid cephalopods. SpecialPapers in Palaeontology 23,259-262.

TIMS, J.D. & CHAMBERS, T.C. 1984—Rhyniophytina and Trimerophytinafrom the early land flora of Victoria,Australia. Palaeontology 27, 265-279.

TOOMEY, D.F. & MAMET, B.L. 1979—Devonian Protozoa. Special Papers inPalaeontology 23, 189-192.

TURNER, N.J. BLACK, L.P. & HIGGINS,N.C. 1986—The St Marys porphyrite - aDevonian ash-flow tuff and its feeder.Australian Journal of Earth Sciences 33,201-218.

TURNER, S. 1982a—Thelodonts and cor-relation. pp. 128-132, In P.V. RICH & E.THOMPSON (Editors)The Fossil Ver-tebrate Record of Australasia. MonashUniversity Offset Printing Unit, Mel-bourne.

TURNER, S. 1982b—Middle Palaeozoic elas-mobranch remains from Australia. Jour-nal of Vertebrate Paleontology, 2,117-131.

TURNER, S. 1984 Studies on PalaeozoicThelodonti (Craniata:Agnatha). Un-published Ph.D. Thesis, University ofNewcastle-upon-Tyne.

TURNER, S. 1986—Vertebrate fauna of theSilverband Formation, Grampians,western Victoria. Proceedings of theRoyal Society of Victoria, 98, 53-62.

• TURNER, S. & DRING, R.S. 1981—LateDevonian thelodonts (Agnatha) from theGneudna Formation, Carnarvon Basin,Western Australia. Alcheringa 5, 39-48.

TURNER, S., JONES, P.J., & DRAPER, J.J.1981—Early Devonian thelodonts (Ag-natha) from the Toko Syncline, westernQueensland, and a review of otherAustralian discoveries. BMR Journal of

• Australian Geology & Geophysics, 6, 51--69.

VANDENBERG, A.H.M. 1975—Definitionsand description of Middle Ordovician toMiddle Devonian rock units of the War-burton district, east central Victoria.Geological Survey of Victoria, Report1975/6.

VEEVERS, J.J. 1959—Devonian brach-iopods from the Fitzroy Basin, WesternAustralia. Bureau of Mineral Resources,Australia. Bulletin, 45.

VEEVERS, J.J., ROBERTS, J., WHITE,M.E., & GAMUTS, I. 1967—Sandstoneof probable Lower Carboniferous age inthe north- eastern Canning Basin.Australian Journal of Science, 29, 330-331.

VEEVERS, J.J. & WELLS A.T. 1961—Thegeology of the Canning Basin, WesternAustralia. Bureau of Mineral Resources,Australia, Bulletin, 60, 1-323.

WARREN, A., JUPP, R. & BOLTON, B.1986—Earliest tetrapod trackway. Al-cheringa, 10, 183-186.

WILLIAMS, -I.S., TETLEY, N.W., COM-PSTON, W. & McDOUGALL, I. 1982—Acomparison of K-Ar and Rb-Sr ages ofrapidly cooled igneous rocks: two pointsin the Palaeozoic time scale re-evaluated.Journal of the Geological Society of Lon-don, 139, 557- 568.

WYATT, D.H. & JELL, J.S. 1980—Devonianand Carboniferous stratigraphy of thenorthern Tasman orogenic zone in theTownsville hinterland, NorthQueensland. pp.201-228, In HENDER-SON, R.A. & STEPHENSON, P.J.(Editors) The Geology and Geophysicsof northeastern Australia. GeologicalSociety of Australia, Queenslanddivision.

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WYBOFtN, D., OWEN, M., COMPSTON, W.& McDOUGALL, I. 1982—The LaidlawVolcanics: a Late Silurian point on thegeological time scale. Earth andPlanetary Science Letters, 59, 90-100.

WYBORN, D., TURNER, B.S. & CHAP-• PELL, B.W. 1987—The Boggy Plain Su-

persuite - a distinctive belt of I-typeigneous rocks of potential economic sig-nificance in the Lachlan Fold Belt.Australian Journal of Earth Sciences 34,21-43.

YOUNG, G.C. 1974—Stratigraphic occur-rence of some placoderm fishes in theMiddle and Late Devonian. Newsletterson Stratigraphy, 3,243-261.

• YOUNG, G.C. 1981—New Early Devonianbrachythoracids (placoderm fishes) fromthe Taemas - Wee Jasper region of NewSouth Wales. Alcheringa, 5,247-271.

YOUNG, G.C. 1983—A new antiarchan fish(Placodermi) from the Late Devonian of

• southeastern Australia. BMR Journalof Australian Geology and Geophysics,8, 71-81.

YOUNG, G.C. 1984—An asterolepidoid an-tiarch (placoderm Fish) from the EarlyDevonian of the Georgina Basin, centralAustralia. Alcheringa, 8, 65--80.

YOUNG, G.C. 1985a—Further petalichthyidremains (placoderm fishes, EarlyDevonian) from the Taemas - Wee Jasperregion of New South Wales. BMR Jour-nal of Australian Geology and Geo-physics, 9, 121-131.

YOUNG, G.C. 1985b—New discoveries ofDevonian vertebrates from the AmadeusBasin, central Australia. BMR Journal of

• Australian Geology & Geophysics, 9, 239-254.

YOUNG, G.C. 1987—Devonian fish remainsfrom Billiluna, eastern Canning Basin,Western Australia. BMR Journal of

• Australian Geology & Geophysics, 10,179-192.

YOUNG, G.C. 1988a—Antiarchs (placodermfishes) from the Devonian AztecSiltstone, southern Victoria Land, An-tarctica. Palaeontographica A202, 1-125.

YOUNG, G.C. 1988b—New occurrences ofphyllolepid placoderms from theDevonian of central Australia. BMRJournal of Australian Geology &Geophysics, 10, 363-376.

YOUNG, G.C. 1989—New occurrences of cul -macanthid acanthodians (Pisces:Devonian) from Antarctica andsoutheastern Australia. Proceedings ofthe Linnean Society of N.S.W., 111, 12-25.

YOUNG G.C., & GORTER, J.D. 1981—Anew fish fauna of Middle Devonian agefrom the Taemas/Wee Jasper region ofNew South Wales. Bureau of MineralResources Geology & Geophysics, Bul-letin, 209, 83-147.

YOUNG, G.C., TURNER, S., OVVEN, M.,NICOLL, R.S., LAURIE, J. & GORTER,J. 1987—Anew Devonian fish fauna, andrevision of post- Ordovician stratigraphyin the Ross River Syncline, AmadeusBasin, central Australia. BMR Journal ofAustralian Geology & Geophysics, 10,233-242.

ZIEGLER, W. 1962—Taxionomie undPhylogenie Oberdevonischer Conodon-ten und ihre stratigraphischeBedeutung. Beitragshefte HessischenLandesamtes fiir Bodenforschung, 38, 1-

. 166.ZIEGLER, W. 1971—Conodont stratigraphy

of the European Devonian. In SWEET,W.C. & BERGSTROM, S.M. (eds) Sym-posium of Conodont biostratigraphy.Memoir of the Geological Society ofAmerica, 127, 227-284.

ZIEGLER, W. 1978—Devonian. In CONEE,G.V., GLAESSNER, M.F., & HED-BERG, H.D. (Editors). Contributions tothe Geological Timescale. AAPG Studiesin Geology, 6, 337-339.

ZIEGLER, W. & }CLAPPER, G. 1985—Stagesof the Devonian system. Episodes 8, 104-109.

ZIEGLER, W. & SANDBERG, CA. 1984—Palmatolepis-based revision of upperpart of standard Late Devonian conodontzonation. Geological Society of America,Special Paper 196, 179-194.

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DEVONIAN BIOSTRATIGRAPHIC CHART ( I89 EDITION)

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