Interpretation of the lead isotopic composition fromsulfide mineralizations in the Proterozoic Sjangeliarea, northern SwedenROLF L. ROMER

Romer, R.L. 1989: Interpretation of the lead isotop ic composition from sulfide mineralizations inthe Proterozoic Siangeli area, northern Sweden . Nor. geol. unoers . Bull. 415, 57-69.

Cu-. Fe-. and Zn-mineralizations occur in the Lower Proterozoic supracrustal rocks of theSjangeli area, a tectonic basement window in the Caledonides of northern Sweden and Norway .The supracr ustal belt consists of basic and ultrabastc metavolcani tes which are intercalated withquartz-mica schists and banded carbonate-silicate rocks . The metavolcanites consist of tuffs , lavaflows , and pillow lavas. Cu-mineraliza tions , which form three diffe rent types , occur within basicmetatuffs. Two types represent epigenetic remobilizat ions of Cu-mineraliza tions . while the thirdtype is characterized by stratifor m born ite-chalcocite-quartz-magnetite layers of possible syngene-tic origin. The Fe- and Zn-mineralizations occur in quartz- mica schists and form strati form lenses.

At about 430 My a dist urbance of the lead isotope system occurred. which changed the "'UI""Pb, "'Th/""Pb, and "'Th/"' U ratios . Radiogenic lead was added to the mineralizat ions during the430 My distu rbance . The added lead component was diffe rent for the various deposi ts . Further,during the 430 My event. U was mobile. which is illustrated by the significantly increased "'U/""Pbratios of the massive pyrrhotite mineralizations.

Lead lines from the recalcula ted lead compos ition (430 My) indicate mixing model ages of 1546My to 2112 My. Since the mixed lead compo nents were non-coge netic, the model age variation ofthe mixing lines indicates differences of the mixing compo nent. rather than real age diffe rences .However. a lead source of Middle Proterozoic age can be deduced.

The Middle Proterozoic disturba nce resul ted in the formation of vein mineralizations which havepredomi nantly high-uranogenic . low-thorogenic lead. The in-situ lead growth indicates high "'UI""Pb ratios and implies that U had also been mobile during the Proterozoic metamorphism .

Model ages for the least radiogenic lead (Kopparasen) yield a minimum age of 2050 My.

R.L. Romer, Department of Economic Geology, University of Technology Lulea. S-951 87 Lutea.Sweden.

IntroductionIn the southwestward younging Baltic Shieldof northern Scandinavia (Ski6ld 1986 , 1987,Gaal & Gorbatschev 1987), the Rombak-Sjan-geli basement window forms an accret ionaryzone of the Archean eraton of probab le islandarc setting (Korneliussen et al. 1986). TheRombak-Sjangel i window is characterized byN-S striking volcano-sedimentary belts. Thevolcanites vary from basic and ultrabasic com-posit ion at the eastern border to intermediateand acidic compos ition in the west (e.g. Korne-liussen et al. 1986). The Sjangeli area repre-sents the easternmost of these Lower Protero-zoic supracr ustal belts and consists of basicvolcanites (tufts and lavas) and carbonate andpelitic sediments.

These Proterozoic suprac rustal belts of theRombak-Sjangeli window became intruded byacid to basic rocks at about 1700-1800 My

ago. This is illustrated by Rb-Sr ages deducedfrom whole-rock isochrons from granites, e.g.1691 ± 90 My (Heier & Compston 1969) and1780 ± 85 My (Gunner 1981). SUbsequently,the Proterozo ic rocks were eroded and werecovered by discontinuous metaconglomeratesand arkosic quartzites (et. Kulling 1964 , Tullet al. 1985), presumably during the Cambrian(Bergstr6m & Gee 1985). The quart zites gene-rally form thin flat-ly ing veneers , but locally

. they are bent upright along steep faults whichremobilized basement blocks (Bax 1986 , 1989).The basement react ivation is related to theCaledonian overthrust ing, which in the Rom-bak-Sjangeli area probab ly started about 450My ago (e.g. Tull et al. 1985). The overr idingof the Caledonian nappes over the basementresulted in a low-grade metamorphism rea-ching greenschist facies (e.g. Bryhni & Andre-

58 Rolf L. Romer

I°eO E

Of!~"-::~77/ /

EXPLANATION

~ 'Phanerozolc' rocks

wmoow-rt:I:jl Precam bnan

// , Z" ~ suprocrusta l rocks

:% '/ /' D Precombnon10 1< rntrusrve rocks

Fig. 1. Simplified geolog ic map of the Rombak-Sjangelibasement window (after Vogt 1950. Kulling 1964. Romer1987). Sample (Table 1) locations are indicated. For moredeta iled information about the sample loca tions in the Sjan-geli area see Fig. 2 and Romer (1987).

asson 1985. Tull et al. 1985) in the easternpart of the basement windows . which includesthe Sjangeli area.

Sulfide mineralizations occur within the sup-racrusta l belts of the Proterozo ic basement.The lead isotopic composition of sulfide mine-rals from some of these mineralizations (et.Figs. 1 & 2) has been determined. The bulkof these analyses comes from the Cu-minerali-zations of the Sjangeli area and their wall rocks .

The purpos e of this paper is (1) to use thelead isotopic composition of the samples toillustrate the effect of the Caledonian andSvecokarelian orogenies onthe isotopic com-position of the sulfide lead and the who le-rocktrace lead; and (2) to use the lead compos itionas a tracer of the source of the different leadcompo nents.

Geology of the Sjangeli areaThe Sjangeli supracrustal belt lies at the eas-tern border of the Rombak-Sjangeli window

GU - BULL 4 15. 1989

FIg. 2. Simplified geologic map of the Sjanqe h supracrus-tals (after Romer 1987). Show ing the orstnounon of hevolcanic uruts and the sample locations.

(Fig. 1) and is corr elated with the Kopp arasenand the Gautelis supracrustal rocks (et. Ada-mek 1975. Romer 1987). The Sjangeli suprac -rustal belt, which is about 10 km long andreaches a width of 5 km, strikes approximate-ly N-S and the units dip steeply to the west(70-85°). The belt is characterized by a strike-parallel 'zebra-stripe' pattern consisting ofvolcanic units which are intercalated with sedi-mentary and volcano-sed imentary units.

To the east (Fig. 2), the metamorphosedvolcanic rocks are lava flows . that are em-bedded in basic metatuffs, and which common-ly are strongly mylonitized. The lava flowsoccur only in this easternmost volcanic unit.and they do not contain any mineralizations.The waterlain basic metatuffs. hereafter some-times simply called tuff s, conta in thin layersof banded silicate-carbonate rock . The tuffsare the most intensely mineralized part of theSjangeli area. Most of the stratabound minera-lizations are stratiform, but locally discordantquartz-bornite veins also occur , which couldrepresent remobilizations of stratabound mine-ralizat ions.

NGU - BULL. 415.1989 Interpretation of the lead isotopic composition from sulfide 59

The central volcanic unit consists of high-Mgbasalts (12-18 % MgO) which contain lensesof serpentinites. The amphibolites consistmainly of layered metatuffs, but locally conta-in pillow lavas and thin layers of banded car-bonate-silicate rock. The high-Mg basalts havehigh contents of Cr and Ni (Romer 1987) andshow platinum group element ratios similar tokomatiites (Barnes et al. 1988). The amphiboli-tes do not contain Cu-mineralizations. A rneta-somatic alteration zone which contains a mag-netite layer with bornite occurs at the NE con-tact between the mica schists and a serpentini-te lense.

The western volcanic unit consists of pillowlavas which locally are interlayered with thindiscontinuous layers of banded carbonate-silicate rock. This unit does not contain Cu-mineralizations.

Quartz-mica schists and banded silicate-carbonate rocks intercalate with the volcanicand volcano-sedimentary units. At Ruvssot(Fig. 2) the quartz-mica schists contain strati-form Cu-mineralizations in the vicinity of themetasomatized alteration zone of the amphibo-lites. The quartz-mica schists contain additio-nal stratiform Fe-mineralizations and at Cuno-javre (cf. Fig. 2) they contain a stratiform Zn-mineralization.

The amphibolites show Early Proterozoicamphibolite facies mineral assemblages. Theother volcanic units have been extensivelyretrograded and show greenschist facies mine-ral assemblages.

Two metamorphic events and possibly thespilitization of the volcanic rocks have distur-bed the isotope systems. The youngest event,which partially reset the isotope systems, isthe Caledonian orogeny. Here, the term Cale-donian is used rather loosely and refers toany event in the approximate time range 380to 480 My. Rb-Sr whole-rock data yield mixinglines with an apparent age of 488 ± 64 My(Romer 1989). Similarly, mineral Rb-Sr isotopedata indicate a partial remobilization of theisotope systems at that time. Since the mixinglines do not yield ages, no precice time cons-traints for the Caledonian overthrusting canbe deduced for these lines. Tull et al. (1985)refer to a dynamometamorphic event prior toc. 450 My ago to the west of the Rombak-Sjangeli area, while mineral ages from Vestvaq-0Y vary from c. 460 My (amphiboles) to c. 350My for bictites (Tull et al. 1985). For the recal-culation of the lead isotope composition, an

age of 430 My was arbitrarily chosen.Whole-rock lead lines indicates ages of 1600

- 1800 My (Romer 1989). These ages coincidewith the ages of the Svecokarelian granites,to which the granites and syenites of theRombak-Sjangeli window belong (cf. Gorbat-schev 1985). Similar metamorphic ages wereobtained for the Vesteraten area (e.g. Griffinet al. 1978, Jacobsen & Wasserburg 1978).

Rb-Sr whole-rock data yield a date of 2324± 15 My (Romer 1989). Since this date isbased on only 3 analyses and as the area hasbeen metamorphosed twice, it probably doesnot represent a reliable age and is probablytoo high by 100 to 150 My (cf. Romer 1989).Ages in excess of 2000 My have been repor-ted from the Vesteralen area (Griffin et al.1978). Where metavolcanites yield ages ofabout 2200 My.

Mineralization typesIn the Sjangeli area, mineralizations of Cu, Fe,and Zn predominately form strati form lensesand layers. However, Cu-mineralizations alsoform remobilizations in discordant veins andmetasomatized contact zones. In the followingdiscussions, the minerallzations are classifiedaccording to their main metal and, in addition,the Cu-mineralizations are classified into types(i), (ii), and (iii), while the Fe-mineralizationsare separated into magnetite and pyrrhotitemineralizations.

Cu-mineralizations occur within the basictuffs at Unna Atakats, Siangeri, and further tothe north at Valfojokk (Fig. 2). ComparableCu-mineralizations occur in similar wall-rockat Ruvsojaure and in the quartz-mica schistsat Ruvssot. In addition, Cu-mineralizations atRuvssot are related to a magnetite band inthe metasomatic alteration zone between theultra basic volcanites and the mica schists (Fig.2).

The Cu-mineralizations form three main ty-pes, that differ in respect to the field occurren-ce and the main copper sulfide (Romer 1987):

Type (i) is the predominate mineralization inthe Sjangeli area. It forms massive bands andlenses that contain more than 50% sulfidesand oxides, with sulfides dominating over oxi-des. The bands are up to 5 cm broad and upto 50 m long while the lenses have a lengthof 20 to 50 cm and are 2 to 5 cm thick. The

60 Rolf L. Romer

bands and lenses contain mainly bornite, chal-eocite and magnetite. Epidote and quartz arethe main gangue minerals, while Fe-actinoliteis minor.

Type (ii), which is only found at Unna Ala-kats, forms schistosity-parallel quartz veinswhich are discordant to the bedding. The qu-artz veins, about 5 cm broad, are paralleled bya sulfide band on one or both sides. The sulfi-de bands contain bornite and chalcocite toget-her with minor magnetite. These bands wereprobably formed during the Proterozoic meta-morphism and deduced their metal contentfrom preexisting mineralizations of type (i).

Type (iii) occurs at Ruvsojaure and is diffe-rent from the other two types since borniteand chalocite are absent and chalcopyrite al-most exclusively occurs in small veins. Themineralization is bound to an intensely epidoti-zed and partly actinolitized amphibolite, whichresembles the basic metatuffs from Unna Ala-kats.

In addition to these three main types (i-iii),a 1-3 m thick, 100 m long magnetite zonewith abundant bornite occurs at Ruvssot. Thiszone is part of the metasomatic alterationzone between the serpentinites and the quartz-mica schists (Romer 1987).

Within the mica schists, banded quartz-magnetite mineralizations form strati form bodi-es up to 1 m thick and 40 to 60 m long. POly-crystalline 'globules' of coarse pyrite and chal-copyrite, about 1 cm in diameter, occur local-ly within the magnetite bands. Near Cunojavrea stratiform Zn-mineralization, about 100 mlong, forms a thin (5-10 cm) schlstostty-concor-dant 'sheet'. Sphaler\te is the main mineralof this massive mineralization, but minor pyrr-hotite, chalcopyrite and pyrite also occur. Furt-her, within the amphibolites, a 50 m long, 5-30cm broad stratiform pyrrhotite mineralizationoccurs, consisting exclusively of pyrrhotite andquartz.

MethodsAll isotope measurements were performedduring a research visit at the University ofCalifornia, Santa Barbara. Ion exchange techni-ques were used to separate Pb, U, and Th(Grunenfelder et al. 1986). Contents of Pb, Uand Th were determined by isotope dilutionusing a composite 2°'Pb-2JlU-''''Th tracer. Pbwas measured using a Re single filament sili-

NGU - BULL. 415.1989

ca-gel technique (e.g. Cameron et al. 1969) ona Finnigan MAT 261 multi-collector mass spect-rometer. The Pb mass fractionation correctionfactors were calculated for NBS 981 Pb-standard, using 208Pb/~Pb = 2.16715 (Todt etal. 1984). The lead composition was measuredwith a 2a precision better than ± 0.08% (~Pbl""Pb). U and Th were measured on an AVCOsingle collector solid source mass spectrome-ter, using a Re single filament 'carbon sand-wich' technique (HNO-Ioad of U and Th bet-ween two carbon layers; G.R. Tilton, pers.comm.). Uncertainties in the concentrationdata are c. 0.3% for Pb and 1% for U and Th.

The decay constants recommended by Stei-ger & Jager (1977) were used.

Sample description and resultsThe lead compositions of sulfide concentratesfrom mineralizations in the Sjangeli area andthe Rombak-Sjangeli window are reported inTable 1. The locations of the samples are indi-cated in Figs. 1 & 2.

Sample M11 belongs to the Cu-mineralizati-ons of type (ii), while all other Mx samplesand sample Sja-1 belong to the Cu-mineralizati-ons of type (i). Samples M2 and M3 originatefrom the same mineralization. Sample M3comes from the massive. central part of themineralization, while M2 comes from a lessmineralized section. Samples M4 and M6 aredisseminated sulfides from the wall rock ofmassive mineralizations, and samples M9 andSja-1 come from massive mineralizations.Samples H7 and H9 are from Cu-mineralizati-on type (iii) from Ruvsojaure.

Three sulfide concentrates from the pyrite-chalcopyrite .globules' from the magnetitemineralization have been analyzed (N45, 334,338). Samples N24, N25a, and N25b originateform the pyrrhotite mineralization. PyrrhotitesN25a and N25b come from the same speci-men; however, pyrrhotite N25b is more strong-ly magnetic than pyrrhotite N25a. Sample N37was obtained from the bornite-mineralizedmagnetite band in the above-mentioned rneta-somatized alteration zone at Ruvssot.

Samples H44 and G55 are from impregnati-ons in the quartz-mica schists, while samplesN12 and N13 are from massive mineralizations.

Lead isotope data have also obtained fromthe various igneous (now metamorphosed)

NGU·B Ul L.415.1989

Sulfides from the Sjangeli area

Cu-m ineralizat ions

Interpretation of the lead isotopic composition from sulfide 61

samp le

H7H9M2M3M4M6M9M11Sja-1

Fe-minere tizettons

sample

N24N25aN25bN37N45334338

Zn-mtneretizet ions

sample

N1 2N13

Other mineralizations

sample

G55H44

minera l

pypypypybo-cctbo- cctpy-bo-cctpy+ccpbo+ccp

mineral

popoposphpypy+ccppy

mineral

posph

minera l

asppy

""I,..

44.485119.2818.73015.91131.57136.69937.39722.89925.428

38.03824.28434.01425.70318.28522.80428.621

""I,..

23.60726.962

""I,..

16.57817.489

201/ :»1

18.57929.57915.61615.26917.24017.42817.90016.05916.448

207/ 2\)4

17.76016.22917.40516.50915.60716.15917.105

201/2\)4

16.16216.559

207/ 2\)4

15.36815.519

""I,..

37.39141.17439.42635.92348.35647.46638.82239.92440.470

44.09139.27043.63542.64436.88540.92043.312

41.75941.632

36.23336.369

Pb

2.36.15.2

62.3.95.4.19.79.9

Pb

2.03.94.6.668.93.51.6

Pb

999.010.0

Pb

4.45.8

u

.87

.0170.0033

.018

.064

.026.55

u

1.432.88

.24.069.046

.024

u

.082

.042

u

.215

.02

Th

.107

.05.0038.007

.017

.023.0005

Th

.33

.23.073.065.025

.027

Th

.126 .

.048

Th

.245

.029

Sulfides from other supracrustal belts in the Rombak-Sjangeli area

sample

KopparasenGautelisSildviksercai

mineral

gaaspsphpy+ccp

""I,..

15.29320.85015.76519.756

15.19215.88015.31115.690

2O'/~

35.08339.13935.48337.292

Pb

7.914.33.7

u

.18

.03

Th

.11.053

Table 1. l ead composition and contents (in ppm) of Pb, U. and Th of suifides from the Sjangeli and related areas. Forsample location compare Figs. 1 & 2. py = pyrite; po = pyrrhotite; bo = born ite; sph = sphalerite ; ga = galena; ccp =cnalcopyrite: cct = chalcocite: asp = arseno pyrite .

rocks of the Sjangeli area. The whole-rocklead isotope data for the tufts , the amphibol i-tes, the lava flows , and the granites is presen-ted in Romer (1987, 1989).

Since most samples contained only tracelead (0.6-62 ppm Pb) and also contained tra-ces of U and Th (up to 2.9 ppm U and 0.33ppm Th; see Table 1), the lead compos itions

62 Bott L. Romer GU · BULl. 415. 1989

Fig. 3. Lead Isotope ratios from sumoes from the differentrnineralizanon types of the SJangeli area . Recalculated ISOtO'pie compos.nons tor 430 My (open symbols) are also shownif the recalculated and measured ratio s di ffer beyond draf-ting reso lut ion. Tre-hnas connect the recalculated and themeasu red com position . Regress ion lines for the vanou snuneratrzauon types are used to calculate model ages andapparent ratios (see Table 2).

46

8070

• Cu· ~ro ::': o()t'l$• ~. . fora lot ()"'lS• I n·t'''\,.... rct let I• Suit e mor~noh~

0--- '

------;,.

"", _ - 0

• Metom . tuff s. 0 Cu- mlOeralizatKJns typeh) & type Ill)• Fe -mineraliza tlC)ns lmognetlte I• Fe .mlnerahzc1.ans fpyrrhot lle J

,. .0---.. ....

20

,, 0---0

31.0

,,..

• •.

175

.0a..~ ~5

---.0~a.. 155/ ,.. "

51l, l~

30 50 601/ 20' Pb (ppm-l )Fig. 4. Pb' ''''Pb · l /"" Pb and " Pb/""Pb . 1,""Pb rruxmt plitfor lead composmons recalculated 10 430 My (except torthe ope n symbols. which represent present-day lead). Tra-ce lead data from sutnces of Cu- and Fe-mmerauzanonsare recalculated ram Table 1. The data for the tu ts arereca lcuta ed from Romer (1987).

have been altered by in-situ radiogenic leadgeneration. To obtain the lead compositionat the time of the last disturbance. the leadhas to be recalculated based on the assumpt i-on hat he contents of U. Th and Pb remai-ned unchanged after the last event. The timefor recalculation was arbitrarily set to 430 My(see also the section on the geology of theSjangeli area). The recalculation eliminates theeffect of in-situ radiogenic lead addition. andmixing relationships should become more ob-vious. ote that the recalculation of the isoto-pic compo sition of the lead is based on theassumption of no gain/loss of U. Th, and Pb.

The isotopic composition of thesulfide lead at 430 MyThe sulfide lead isotopic compositions , shownin Fig. 3, form a rather well defined lineararray in the lO6PbP"Pb - lOl PbP" Pb plot. Howe-ver. in the lO6PbP" Pb - lOlPbJ204Pb diagram, thesamples scatte r, and there are samples withhigh "'Pb/""Pb ratios and anomalously lowlO Pb/""Pb ratios (e.g. H7, M9). The lead isoto-pic composition of the Fe-mineralizations andthe Cu-mineralizat ions differs (et, Fig. 6). The-re are also differe nces between the variousCu-mineralizations and, further , between themagnetite and the pyrrhotite Fe-mineralizat i-ons.

The Cu-mineralizations define a single leadline in the lO6Pb/""Pb - lOl Pb Pb diagram. whi-le in the ""Pb/""Pb - lOlPb/""Pb diagram twodifferent lead trends are obvious. One trend.defined by most Mx samples and Sja-l showsa lO PbJ204Pb ratio of about 0.75, while the se-cond trend defined by Hx and M9 falls clearlybelow this trend (ct. Fig. 3).

Samples H7 and H9 belong to the mineraliza-tions of type (iii) , while M9 belongs to minerali-zation type (i). Lead from these Cu-mineralizati-ons indicates a lead growth in a high ~ ell UI""Pb). Iow m ("'ThJ204Pb) environment.

In contrast to these samples, samples frommineralization type (i) (except M9) show a high-ly variable lead composition. with low radioge-nic lead for massive mineralizations and withmore radiogenic lead in low-grade (usuallydisseminated) mineralizations . The radiogen ityof the lead composition of this type correlatesnegatively with the lead contents (ct. Fig. 4)and therefore the lead line of the type (i) mine-ralizatlons could be the result of isotopic mix-

NGU . BULL. 415. 1989 Interpretation of the lead isotopic composit ion from sulfide 63

Fig . 5. Lead isotope ratiosfrom diffe rent units f' om theSjangeli area (reca lculatedfor 430 My). Data from Tab-le 1 and Romer (1987). Fordiscussion see text.

50.0

..0 46.00....~

oN

~42.0..00....

CO

2 38.0

34.0

..0 17.50....~oN

~ 16.5..00....

r--~ 15.5

Cl Amphib olites .• Metam. la va flowsla Met am. tu fts~ Acid lintermediote~ In t r usions •

••

••

• Cu - mine rolizat ions• Fe - mineralizations... Zn - mineral iza tions

• Other minera lizatlans

ing of two isotopically different lead compositi-ons. This would explain the constant K ratio('32Th/lJ 'U) necessary to obtain a linear trendin the lIl6Pbl'04Pb - 2°'Pb/204Pb diagram . Further,there would be no need for a negative correla-tion between the isotopic ratios and the leadcontents, as an in-situ lead growth interpretati-on would imply (since lead content and leadradiogen ity correlate negatively, cf. Fig. 4). Theslope of the tie-line of samples M2 and M3reflects a higher 2O'Pbl'06pb ratio than all othertrends (Fig. 3). This indicates that if there hadbeen mixing , the mixing lead compos ition can-not have been completely homogenous. Theadded lead compos ition, which could havebeen introduced at different times near 430My, must have had local variations in its isoto-pic composition. Sample M11, which is theonly sample from Cu-mineralization type (ii),falls on the trend defined by samples fromCu-mineralization type (i).

The lead composition from the Fe-mineral iza-tions differs widely. Sulfide lead from themagnet ite mineralizations follows the sametrend as the Cu-mineral ization type (i) lead.However , the lead from the magnet ite mineral i-zations has a higher 201Pb/204Pb ratio for a gi-ven 206Pbl'04Pb ratio (et. Fig. 6). The pyrrhotitelead from the pyrrhotite mineral ization is cha-racter ized by a large in-situ decay correction,since pyrrhotite has large contents of U. Notethat the pyrrhotite has rather low Th contents.The lead line through the recalculated sampleshas a flatter slope in the lIl6Pb/204Pb - 201Pb/204Pband the lIl6Pb/204Pb - 2O'Pb/204Pb diagram than thetype (i) Cu-mineral izations and the magnet itemineralizations .

The recalculation of the pyrrhotite lead (N24.N25, N25b) to 430 My aligns all three samplesalong a straight line, which has a differentslope than the in-situ decay correction tie li-nes, indicating that after 430 My the lead evol-

64 Rolf L. Romer GU -B ULL.4 15. 1989

Fig. 6. Sulf ide tra ce leadiso tope ra tios from minerali -zanons from the Rombak -Sjan geli basement win do w(Fig. 1) and the asa fjeetlw indow. The rat ios are re-calculated for 430 My . ex-cept for the open symbols.For comparison. the fielddefined by the lead compo-sitions of sam ples from theSjange li area (Fig. 5) areshown.

..00....

3N

':er0....

cooN

50.0

46.0

[.2.0

38.0

34.0

S••K

[.2.0380

GAUTElISKOPPARAs E

ASAFJA l lS Sil O IKsv SVA GERAIVES ~ 5 RDAl

SJA GElI

~ Cu- mmerou zcnonsFe - rmnerc uzcnons

34022018.0

17.5

..00....

165 ~~0(,J

~II

0.... 15.5r--0N

14 .5KO

ved with different ~ and lil rat ios . The 430My line betwee n the different pyrr hot ite samp-les could be a mixing line between a primarylow rad iogen ic lead composition , poss ibly simi-lar to N25a, and a more rad iogen ic lead. Asso-ciated with such a mixing , U could have beenintroduced into the pyrrhotites . This mixingprocess would provide a mecha nism to select i-vely add U and Pb to the pyr rhot ite.

The lead compos ition of the Zn-minera lizati-on is highly rad iogenic although both samples(N12 and N13) come from a massive minera li-zation and have high Pb contents. In addition,me tie- line of the two samples N12 and N13has a flat, negat ive lO'Pb/206Pb slope . This sug-ges ts that the lead of the Zn-mineralizationsrepresents a mixture of two non-cogeneticlead components.

The isotopic compos ition andsource of the 'contamination' leadThe reca lculated lead compositions of sulfidesfrom the diffe rent mineralizations fall on diffe -

rent linear trend s (Fig. 3; 206Pb/2O'pb - lO'Pb Pbdiagram). If these lines represent mixing lines,th is demonstrates that there is no commonmixing component. Since these mineralizationtypes are geographically separated and someof them are related to differe nt lithologies (et.Fig. 2), it is poss ible that the lead of the host-roc ks has cont ributed to the mixing lead,whi ch wou ld give the mixing lead a local mod i-fication and var iation .

For example, the lead composition of thetype (i) Cu-mineralizations and their host-rocks, the tuffs , plot in fields wh ich overlap(et. Fig. 5). However, for the same lO'Pb/2O' pbratio the tuffs have a wider var iation of he206Pb/2O'pb ratio and usually also have higherlO6Pb/"" Pb ratios.

The sulfide lead composition cou ld be ex-plained with a simp le two component mixingproc ess. One lead component wou ld have alow radiogen ic lead com position , similar tosample M3 or the Kopparase n galena, wh ilethe other lead component has to be morerad ioge nic than sample M4 or M6. Setting

NGU - BULL. 415,1989 Interpretation of the lead isotopic composition from sulfide 65

206Pb/204Pb arbitrarily to 38.0, the other ratiosare fixed at 207Pb/204Pb = 18.06 and 2°'Pbp04Pb= 50.0 (cf. Fig. 3). Such an end member couldalso partially explain the variation of the leadcomposition of the tuff lead composition. Theremaining lead variability of the tuft lead com-position would be due to another lead compo-nent, which formed in a low K environment,or would be due to in-situ lead growth in a lowK environment. The 206Pbpo'Pb ratio of such alead component would indicate a potentialsource with an average Th/U atomic ratio ofabout 2.85 for the time interval from 1800 Myto 430 My.

Alternatively, the lead variation of type (i)Cu-mineralizations could be due to accumulati-on of lead which was leached from the imme-diate wall rock. If the wall rock of all type (i)mineralizations had the same ratio, then themixing with a highly variable lead extractedfrom the wall rock still yield a linear sulfidelead trend. If sulfides and the wall rock oncehad the same isotopic composition, then themixing line would represent the time of isoto-pic homogenization of sulfides and wall rock,Le. it would represent the time of formationor the time of a metamorphic homogenization.The anomalous widening of the metatuft leadcomposition field for more radiogenic lead inthe 206Pb/204Pb - 2O'Pb/204Pb diagram could bedue to the addition of low ID lead, or a negati-ve correlation of I.l and K.

This is compatible with the observation thatthe whole-rock lead composition usually ismore radiogenic than the lead compositionof the coexisting sulfides. The sulfides couldrepresent a mixture of a low radiogenic leadcomponent and a radiogenic lead componentwhich was derived from wall rock leaching atabout 430 My.

These two models can be tested in mixingdiagrams (fig. 4). The sulfide samples from thetype (i) Cu-mineralizations yield a good linearalignment in both mixing diagrams, 206Pbp04Pb- 1P04Pb [pprn-'] and 2O'Pb/204Pb - 1/204Pb [ppm-'].The sulfide data could therefore be explainedwith simple mixing.

However, the tuff lead composition is notcompatible with such a simple mixing. Themixing trend in the 206Pb/204Pb - lI204Pb [ppm-']diagram is scattered and delineates a fieldrather than a straight line. This field shows anegative correlation between the 206Pb/204Pb

ratio and the 204Pb content. In the 2O'Pb/204Pb -1/204Pb [ppm-'] diagram, the tuffs form a wide

sub-horizontal field (Fig. 4). The 2O'Pb/204Pb ra-tio does not vary systematically with the 204Pbcontent of the samples, and therefore, therehas been no mixing or the mixing componentdid not contain 2O'Pb. Alternatively, if all themetatufts had been enriched in U for a longtime, then the variation in radiogenity of thetuffs is mainly due to variable I.l ratios for thedifferent samples. However, to obtain a linearfield (in Fig. 4), there should be at least aweak correlation between I.l and 204Pb ppm.Assuming a homogeneous lead compositionof the tuffs at the time of infiltration and noexternal lead addition, the slope of the tuftfield in the 206Pbp04Pb - 207Pb/204Pb diagram (Fig.3) indicates a model age of 1910 My.

The obvious contrast between the sulfidelead and the tuff lead in the mixing diagrams(cf. Fig. 4) probably indicates a differentialacceptance of externally added lead in thesulfides and in the whole-rock sample. If onlythe sulfides received externally derived lead,while the silicates of the whole-rock samplesdid not accept additional lead, then the sulfidelead would show mixing lines, while the silica-te lead would show in-situ lead growth. Sincethe tuffs also contain a minor amount of sulfi-des, they would, according to the above reaso-ning, also have obtained an external lead addi-tion, although only a minor one. However, forthis model, the metatuff lead line has no strictage meaning, since there is an external, pro-bably non-cogenetic lead component present.

The Fe-mineralizations also yield lineartrends which could be interpreted as mixinglines. However, they received an isotopicallydifJerent lead component (cf. Fig. 3).

Lead from a low K sourceIf an oxidized fluid infiltrates a permeable rockwhich reduces the fluid, then the U in the flu-id would precipitate. Such a process couldhave caused the U enrichment of the tufts, theselective U enrichment of the pyrrhotite minera-Iizations and the pyrites of sample H7 (cf. flat0-430 My tie lines in the 206Pb/204Pb - 2O'Pb/204Pb

diagram Fig. 3).For the metatuffs, such an U infiltration

would have happened about 1600 - 1800 Myago, probably in connection with the Svecoka-relian metamorphism and the intrusion of theProterozoic granites and syenites into theRombak-Sjangeli supracrustal rocks.

66 Rolf L. Romer

The infiltration of U into the pyrrhotite minera-lization, however, happened about 430 My ago(cf. Fig. 3 and section on 430 My lead compo-sition). The pyrrhotite line in Fig. 3 could repre-sent a mixing line similar to the magnetitemineralization line and the type (i) Cu-minerali-zation line. However, in a mixing diagram (Fig.4) the pyrrhotite points do not form a line.Since the primary lead contents of samplescould have been different, this does not neces-sarily rule out mixing. The pyrrhotite line yieldsa model age for cogenetic lead of 1550 Myand an apparant K ratio of 1.22. The slope ofthe pyrrhotite line in the 206PbfO'Pb - 2O'Pb/204Pb

diagram (Fig. 3) indicates lead growth in anenvironment with a higher ratio than after theU addition.

Cu-mineralizations of type (ii) and type (iii)are characterized by low K lead. Since thesemineralizations do not contain high K lead andthe possible mixing components, which havebeen recognized, have developed in a high Kenvironment, it is suggested that these minera-lizations are older than the mixing event atabout 430 My. These mineralization types (iiand Hi) could have formed during the sameevent which caused the U infiltration into thetufts. If they had acquired a high Jl ratio atthe same time, their Jow K lead could be dueto in situ lead growth.

The isotopic composition andsource of the 'primary' leadThe most primitive lead composition found inthe Sjangeli area was found in sample M3.However, in the northward continuation of theSjangeli area, the Kopparasen area, galenawith a less radiogenic isotopic compositionhas been found. This galena lead falls on thesame lead line as the type (i) Cu-mineralizationlead, and probably represents an uncontamina-ted lead composition. Alternatively, the moreradiogenic character of M3 could be explainedby a complete or partial homogenization of thesulfide lead with its surrounding whole-rockat about 1600 - 1800 My.

Model ages for the galena lead compositionvary from 1950 My (Stacey & Kramers 1975)to 2050 My (Zartman & Doe 1981). In a Zart-man & Doe (1981) model, the galena leadwould represent a mixture of lower crust leadwith upper crust lead at about 2050 My. Howe-ver, the galena composition could also be

NGU-BULL.415.1989

modelled with a mixture of an old lower crustlead and a younger upper crust lead. In thiscase, the older component could have preser-ved its low radiogenic composition as galena,from the time of separation to the time ofmixing. At the time of mixing, this old leadwould have mixed with a younger lead compo-nent. Using a upper crust lead of 1600 Myage, the corresponding lower crust lead wouldhave an age of more than 2200 My. For thismodel, the galena lead composition would givea minimum model age of the supracrustalrocks. Note that such model ages rely on thecorrectness of the model, and could yieldmodel ages considerably higher than indicatedby other methods (e.g. Vaasjoki 1981, Sund-blad & Besholt 1986).

The lead isotope constraints onthe alteration of the Sjangeli mine-ralizationsFrom the mixing lines and mineral tie lines (0- 430 My) in Fig. 3, model ages can be cal-culated. These model ages are based on theassumption of cogenetic mixing components.The same assumption also allows for the cal-culation of an apparant ratio for the time fromthe separation of the two lead reservoirs tothe time of mixing. The mineral tie lines ref-lect the in-situ K ratio which also can be cal-culated from the U and Th contents in Table1. These model parameters are summarizedfor the various mineralization types in Table 2.

The variation of the model ages representsthe effect of a variable non-cogenetic mixingcomponent instead of different ages. Howe-ver, the consistency of the model ages indica-tes that the source rocks probably were ofEarly to Middel Proterozoic age. Alternatively,there could have been an Early to Middle Prote-rozoic 'homogenization' event, during whichthe lead of the mineralizations and the sourcerocks of the 430 My lead homogenized. Bothexplanations are compatible with a Svecokare-lian orogeny with the intrusion of granites andsyenites (et. Heier & Compston 1969, Gunner1981, Gorbatschev 1985) and related meta-morphism.

A comparison of the pre-mixing and post-mixing ratios shows a strong decrease for thepyrrhotite and probably the type (ii) Cu-minera-lizations. This indicates that for these minerali-

NGU - BULL. 415, 1989 Interpretation of the lead isotopic composition from sulfide 67

model pre-mixing post430My modeltimeofmixingage K K UlThseparation

Cu-type(i) 1630 2,05 0,27-3,02Cu-type (ii) 1630(7) 2,05(7) 0,91Cu-type (iii) (2040) (0,17) 0,056 1600-1800 4307Femagnetite 2110 2,15 0,56-1,15Fepyrrhotite 1550 1,22 0,078-0,245 430Zn 1700 7

Table 2, Model mixing ages and apparent pre-mixing k (fora homogenization time of 1700 My) calculated from thedata in Table 1 and fig, 3. Note that the model rruxmqages and the apparent k ratios assume cogenetic mixinglead components. The post-rnixinq (430 My) ratios are cal-culated from Table 1, The model time of UITh separationis estimated from changes in the lead growth trends at c.430 My and c. 1800 My respectively. Values in parenthe-ses (type iii) represent maximum model ages and minimumpre-mixing ratios (only one sample was recalculated). Thetype (ii) Cu-mineralization data in parentheses are Inferredfrom type (i) Cu-mineralization data.

zations a separation of U and Th occurredat approximately 430 Ma. The contrast ofsolubility of U and Th in oxidized fluids (e.g.Boyle 1982) suggests a hydrothermal trans-port. The pre-mixing K ratio indicates an up-per crustal lead source, since other reservoirshave higher K ratios, e.g. bulk Earth 4.2 (Alleg-re et al. 1986), lower crust ~5.9 - 10 (Heier& Thoresen 1971, Dostal & Capedri 1978,Zartman & Doe 1981) and mantle ~3 - 4 (Zart-man & Doe 1981).

The anomalously low thorogenic lead com-position at 430 My of the type (iii) Cu-minerali-zations and the tuffs (cf. Figs. 3 & 5) indicatesthat there had been an earlier separation ofU and Th, which was possibly related to theSvecokarelian metamorphism. This 1600 -1800 My metamorphism probably representsthe time of formation of the remobilized Cu-mineralizations of type (ii) and type (iii).

Indications that the metamorphic fluids wereoxidized and could have transported U comefrom the chemical composition of epidotesfrom the tuffs and lava flows (cf. Romer1987). Epidotes from the Sjangeli area havea Xpistacite~.33, and indicate that they haveequilibrated with an oxidized fluid (Bird &Helgeson 1981). In such a fluid, U is predomi-nantly in the 6+ state (Langmuir 1978, Rom-berger 1984), and therefore mobile.

The lead compositions of the Cu-mineralizati-ons and the Fe-mineralizations differ (Fig. 6).Since these two mineralization types are reia-

ted to different lithologies, the isotopic differen-ce may indicate that there was some wallrock leaching or that the lead composition ofthe fluid was different in the various myloniticzones.

No isotopic constraints can be given for thegenesis' of type (i) Cu-mineralizations, sincethere probably had been a rather extensiveisotopic homogenization during the Svecokare-lian orogeny. However, the stratiform natureand their selective occurrence in the tuffs indi-cates a possible syngenetic origin in a suba-quatic shallow-water depositional environ-ment. Such an environment is indicated by theoccurrence of tuffs (Romer 1987) and lapilli(Adamek 1975) in the Kopparasen area (seeFig. 1).

Comparison of other sulfide leadcompositions with the Sjangelisulfide leadThere are only a few lead isotope analysesavailable from other supracrustal units of theRombak window. Samples from mineralizati-ons have been provided by Are Korneliussen(NGU, Trondheim) from Sildvik and S0rdal andby Frank-Dieter Priesemann (Folldal Verk A/S,Folldal) from Gautelis. The other data consistof analyses from galena mineralizations fromSvanqeralve (Johansson 1983) and from Nasa-fjall (Johansson 1983), a basement windowabout 300 km south of the Sjangeli area.

The limited amount of data from these sup-racrustal units (Table 1) does not allow foran equally thorough discussion of the dataas for the Sjangeli area. Instead, these samp-les are compared with the sulfide samplesfrom the Sjangeli area (Fig. 6).

(1) The lead composition of massive sulfidemineralizations from supracrustal belts withinthe Rombak-Sjangeli window show the samevariation as the type (i) Cu-mineralizations ofthe Sjangeli area, and could therefore havebeen affected by similar processes. The Svan-geraive samples (Johansson 1983), however,have significantly higher 2osPb/204Pb ratios at agiven 206Pb/204Pb ratio, and further the 207Pb/206Pb

ratios are slightly higher than for the type (i)Cu-mineralizations.

Johansson (1983) interpreted the lead com-position of the Svanqsraive deposit (20 kmnorth of Sjangeli) as the result of the addition

68 Ralf L. Ramer

of a preferentially leached, radiogenic, Karelianlead component. The lead isotopic compositionof granites form the Sjangeli area shows thesame thorogenic lead as the Svanqeralve de-posits (cf. Figs. 5 & 6), and therefore it ispossible that lead leached from granites andsyenites with a similar lead composition as theSjangeli granites could have been involved inthe formation of the Svanqeraive galena mine-ralizations. However, if the lead compositionof the leached lead and the old lead compo-nent were non-cogenetic, model ages suchas c. 1970 My for Svanqeralve and c. 1660My for Nasafjall (Johansson 1983) do not givethe age of the source.

(2) The lead addition during the Caledonianmetamorphism seems to be common for base-ment mineralizations throughout the entireRombak-Sjangeli basement window. The deg-ree of observed lead radiogeneity dependsnot only on the amount of circulating fluid andthe effectiveness of lead precipitation, but alsoon the lead concentrations and the totalamount of lead present in the mineralizations.The low radiogenity of lead from Kopparasenand Sildvik may reflect that their original leadcomposition is less contaminated by a radioge-nic lead component.

ConclusionsThe trace lead of sulfides from CU-, Fe-, andZn-mineralizations from the Sjangeli area showat least two events of isotopic contaminationand homogenization during which U and Pbwere mobile.

(1) At about 1600 - 1800 My strati form Cu-mineralizations became remobilized into veindeposits. Some of these discordant depositsalso acquired high Jl ratios and low K ratios.The sulfide lead of the strati form Cu-mineraliza-tions and their host-rock, the basic metatuffs,was probably re-equilibrated, and the tuffsobtained U.

(2) At about 430 My, externally derived high-ly radiogenic lead was added to the sulfidesof the various Fe- and Cu-mineralizations, asseen by mixing lines. Further, U was addedto massive pyrrhotite mineralizations.

(3) The two events of isotopic disturbanceare related to the Svecokarelian orogeny andthe Caledonian orogeny. 80th events resultedin metamorphism with the redistribution oflead and uranium. The generated fluids musthave been sufficiently oxidized to transport U.

NGU - BULL. 415.1989

AcknowledgementsI am very grateful to G.R. Tuton for teaching me mass-spectrometry and providing laboratory space at the Universi-ty of California. Santa Barbara, during the academic year1985/86. I thank A. Korneliussen (NGU. Trondheim) forcommenting on the manuscript. M. Vnuk for skilfully drat-ting the figures. and T.M. Boundy for patiently correctingthe language. Financial support was obtained from theUniversity of Technology. Lutea, and Th. Nordstroms Fond(Stockholm). 1 thank K. Sundblad for his critical review ofthe manuscript.

NGU - BULL. 415. 1989 Interpretation of the lead isotopic composition from sulfide 69

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