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Geikielite from the Naataniemi Serpentinite Massif, Kuhmo

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32'7 The Canadian M ine ralo gist Vol. 32, pp. 327-332 (1994) GEIKIELITEFROM THE NAATANIEMI SERPENTINITE MASSIF, KUHMOGREENSTONE BELT, FINLAND ruSSI P. LIPO, JOUNI I. WOLLO, VESA M. NYL{NEN ANDTALINO A. PIIRAINEN Departmentof Geology,University of Oulu,SF-90570 Oulu 57, Finland Arsrtecr Geikielite has only occasionallybeen reponed as an accessoryphase in metamorphosed,hydrothermally altered mafic and ultramafic rocks. This paperrepons a new occurence,in serpentiniteof the Niin$iniemimassif, in the Kuhmo greenstonebelt, easternFinland. Electron-microprobeanalyses show that its compositionranges from IlmroHem2GeiusPyhtrto Ilm2aGeir6Pyhto.The geikielitein theserocks is richerin Mn thanthat previously reported in serpentinizedultramafic rocks. Keywords:geikielite, serpentinite,Niiiitiiniemi, Kuhmo greenstonebelt, Finland. SoMMARS Il est assezrare de rencontrerla geikielite commephase accessoire dans les rochesmafiques et ultramafiquesqui ont subi des effets mdtamorphiqueset m6tasomatiques.Nous en d&rivons un exemple,d'une serpentinitedu massif de Niiiitiiniemi, dansla ceinturede rochesvertes de Kuhmo, dansla partie orientalede la Finlande.l,es analysesi la microsondedlectronique montrentque sa compositionvarie de llm2sFlem2Gei66Pyh,si Ilm2aGei56Pyh26. La geikielite dans ces roches est enrichieen Mn comparativementaux compositionsdocumentdes antdrieurement dans les rochesultramafiques serpentinis6es. (Traduit par la R6daction) Mots-cl6s: geikielite, serpentinite, Ndiitiiniemi, ceinture de roches vertes de Kuhmo, Finlande INTRoDUCTIoN Geikielite hasonly occasionallybeen reported as an accessoryphase in metamorphosed,hydrothermally The end membersthat comprisethe ilmenite series altered mafic and ultramafic rocks. This brief report in igneousand metamorphicrocks are ilmenite providesadditional information on its chemistryand (FeTiO3),hematite (Fe2O3), geikielite (MgTiO3), mode of occurrencein theserocks. In the courseof pyrophanite(MnTiO), and ecandrewsite(ZnTiOr) our researchon chromianspinel (Liipo et al. in prep.), (Waychunas1991). Significant solid-solution minor amountsof geikielite were discoveredin existsamong the following end-members:1) between Archeanmetadunitic serpentinite from the Niiiitiiniemi ilmenite and hematite (Ilm-Hem..), 2) benveenilme- massif.This is the first reportedoccurrence of nite and geikielite (Ilm-Gei,,), 3) betweenilmenite geikielite in Finland. and pyrophanite (Ilm-Pyh""), and 4) between ilmenite and ecandrewsite(Ilm-Eca.,) (Haggerty Locanon ANDGEoLocICAL SETTING 1976,Waychunas 1991). Geikieliteoccurs predominantly in kimberlites,as The Kuhmo greenstonebelt in easternFinland xenocrystsderived by the crystallizationof melts in (Taipaleet al. 1980,Piirainen 1988) is a typical the mantle (Haggerty& Thompkins 1984) and, less Archeangreenstone belt surroundedby granitic rocks. commonly,in carbonatites(Mitchell 1978),granulite- It forms a compositenorth-trending belt approxima- grade ferrous metapyroxenitelenses in gneisses tely 20 km wide and200 km long. The belt preserves (Scharbert1979), n lensesof retrogradedeclogite in upper-greenschist-faciesassemblages and can be gneisses(Pinet & Smith 1985,Smith & Pinet 1985), divided into three parts, namely the southern in serpentinizedultramaJic rocks (Dietrich et al.1986, (Tipasjiirvi), middle (between Kuhmo and Dymek et al. 1.988,Windley et al. 1989), and in Suomussalmi),and northern(Suomussalmi) areas marblein contactaureoles (Gier6 1987). (Fig. 1).It hasbeen dated at between2.99 (Vaasjoki& Downloaded from http://pubs.geoscienceworld.org/canmin/article-pdf/32/2/327/3446667/327.pdf by guest on 03 October 2021 Ultramaficand mafic volcanic rocks Felsicvolcanic rocks I Serpentinite Micaschist Gneissand tl metasedimentary rocks Frc. 1. Geologicalskerch map of theKuhmo greenstone belt. Modified afterTaipale (1983) and Hanski (1984). Downloaded from http://pubs.geoscienceworld.org/canmin/article-pdf/32/2/327/3446667/327.pdf by guest on 03 October 2021 GEIKIELITE. KTJI{MOGREENSTONE BELT, FINLAND 329 Sakko1991) and2.75 Ga (Vaasjokiet al. 1989)and rs presentas an inclusion in magnetite,and as composite composedprincipally of volcanicrocks and, subordi grains with magnetite.Geikielite is grey under nately,of volcano-sedimentaryand sedimentary rocks, reflectedlight, and resemblesilmenite. On the basisof which havebeen divided into threelithological units. texturesand occurrence,chromite is interpretedto be Eachunit is characterizedby its own volcanicseries: the only primary mineral in this sample. l) andesite(Luoma Broup), 2) serpentinite- tholeiite- komatiite - basaltickomatiite (Kelloj:irvi group), and ANATYilCALPnocsPunss 3) rhyolite - rhyodacite- Fe-rich tholeiite - komatiite - basaltickomatiite (Ontojiirvi group) (Taipaleet al. The mineral analyseswere performedwith a 1980). wavelength-dispersionJEOL JCXA 733 electron- The ultramaficrocks have a multistagehistory, microprobeequipped with LINK AN10 automationat affectedby at leastthree phasesof deformationand the Institute of Electron Optics,University of Oulu- two phasesof intrusion of granitic magma,and are The accelerationvoltage was l5 kV, the sample composedpredominantly of serpentinite,having been current, 15 nA, and the spot size,2 'pm.A rangeof deformedand metamorphosedunder conditionsof the natural and synthetic standardswere used (Alapieti & greenschistor upperamphibolite facies (Piquet 1982, Sivonen1983). Results were corrected with an on-line Taipale1983, Blais & Auvray 1990,Tuisku & ZAF program.Ferrous and ferric iron were distributed Sivonen1984). on the basisof stoichiometryby the methodof Carmichael(1967). PsrnocRAPHY Owing to small grain-sizeof most of the geikielite grains, only analysesfrom grains I and 2 could be In the samplescollected from the Niiiitiiniemi ser- consideredsatisfactory, i.e., not affectedby adjacent pentinite massif,one sampleof serpentinitewas found minerals. to containseveral small (G15 pm) grainsof geikielite. This sampleis dunitic in composition,and character- Mnener CmursrnY ized by a metamorphicassemblage of lizardite and antigorite,and minor olivine (Fig. 2). Serpentinemin- Geikielite occursas small grainsin or nearthe mag- eralswere formedat the expenseof olivine, which is netite of the Archeanserpentinite (Fig. 2). The two extensivelyserpentinized, though minor amountsof largestgrains of geikielitefound in this investigation olivine are still present.Accessory minerals include are about 15 pm in size,and homogeneous(Figs. 2, magnetite,Fe-rich chromite and geikielite. Magnetite 3). Electron-microprobeanalyses of geikielite (Fig. a) occurs as anhedralgrains, and chromite, as subhedral revealhigh contentsof Mg and Mn, and lead to the grains,within serpentineminerals. Geikielite is compositionsIlm2qHe2Gei66Pyhts for grain I and Ilm2rHe2Gei5aPyhr2forgrain 2. (Table 1). On the Uasii of O aio-s 5f oxygen,Mg, Mn2* and Fe2+ amountto slightly more than 2 cations,and Ti is slightly lessthan 2 cations.Mg and Mn2+seem to t"ptu." Fe2*in the octahedralsite. No Fe3+-bearing phases,such as magnetiteand hematite,are present, FIc. 2. Back-scatteredelecuon image of geikielite (grain 1) and other small grains of geikielite, and their textural relationship with associatedminerals. Symbols: GEI FIc. 3. Back-scatteredelectron image of geikielite (graln 2) geikielite, MAG magnetite,OL olivine, and SRP serpen- as an inclusion in magnetite.Symbols: GEI geikielite' tine.Scale bar: 50 pm. MAG magnetite,SRP serpentine. Scale bar: 10 pm. Downloaded from http://pubs.geoscienceworld.org/canmin/article-pdf/32/2/327/3446667/327.pdf by guest on 03 October 2021 330 TIIE CANADIAN MINERAIOGIST TABLE !. REPRESET$ATTIIE@MPOTilIIONS OF GEIKIEUTE GRATNS, core rim MATANEMT SRPENm.{IE MAssF to is correlatedwith decreasein concentration of Mg, Mn, and Ji. An interestingfeature of the 1a x456 chemistryof the GEitr 1 Gnin 2 chromitein the samesamples as the geikielite is the high Mn contentfound in their core(up to 6.13wtTo MnO). ra2 57J6 Xfr s9.14 58.9 5&A fi,67 FeCJS 3I)1 2.77 0.m 0m 792 L79 The magnetiteenclosing the geikielite showsno FeO 1113 l^gl 13.09 1244 113 1039 differencecompared grains MrO 1007 rLyl 7037 1060 98 995 to other of magnetite l'lSO 1860 16J4 1667 16J0 18,9 1825 occuring in tfie samesample; it containsa relatively gzt Tdd tm36 99A9 98a1 9891 98.45 high level of Mg (Table2). Nmbq of iq bced o 6 at@s of qtg6 The main serpentiniteminerals are lizardite and 11.. 1.X87 1.ffi6 1.989t LXn L9431 Ls426 antigorite, the former conespondingto the lizardite tr Fdl 0J998 0.091:1 o(m 0.m 0&r describedbvBrais.ff:::t' F*+ 0.4tm o.4sn 0.487 0,67 0.42t0 Mn 03161 0.4545 0398 0.&5 03494 lvIS ^ 1.45 L1055 7.tt12 t.121 12115 M&/Rz+ 0.6m6 05493 05574 |Xy 0.61a lffi Molg Ipt€trt @d B@ber Geikieliteshould be expectedonly in extremely Ilaaite 79.92 X.98 u.x 8.4t m.n ts magnesianassemblages, in which Mgi(Mg + Fez+) HeBatite 2'42 Z,Z, 0.m otr 158 (Windley Caitielito 5938 53.70 55J4 5636 @]6 ;X [Xrr] in spinelis at least0.90 et al.1989) or 4trophuite 1816 n.@ 19.69 m2t n.a 18.6s olivine is more magnesianthan Fon, (Frost 1991).In the samplestudied, the Xrn value of the chromite !@R2+ - vd(vg+uotrl*) rangesfrom 0.26 in the coreto 0.08 in the outerrim, andolivine compositions range from Foq to Foe6. Becauseof extensivemetamorphism, which has obliteratedall primary textures,it is unclearif eitheras inclusionsor as exsolutionlenses in geikielite representsthe product of recrystallizationof geikielite. Calculationsof stoichiometrvindicate small an ilmenite poorer in Mg or a primary igneous amountsof Fe3*in thegeikietite.
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  • A Specific Gravity Index for Minerats

    A Specific Gravity Index for Minerats

    A SPECIFICGRAVITY INDEX FOR MINERATS c. A. MURSKyI ern R. M. THOMPSON, Un'fuersityof Bri.ti,sh Col,umb,in,Voncouver, Canad,a This work was undertaken in order to provide a practical, and as far as possible,a complete list of specific gravities of minerals. An accurate speciflc cravity determination can usually be made quickly and this information when combined with other physical properties commonly leads to rapid mineral identification. Early complete but now outdated specific gravity lists are those of Miers given in his mineralogy textbook (1902),and Spencer(M,i,n. Mag.,2!, pp. 382-865,I}ZZ). A more recent list by Hurlbut (Dana's Manuatr of M,i,neral,ogy,LgE2) is incomplete and others are limited to rock forming minerals,Trdger (Tabel,l,enntr-optischen Best'i,mmungd,er geste,i,nsb.ildend,en M,ineral,e, 1952) and Morey (Encycto- ped,iaof Cherni,cal,Technol,ogy, Vol. 12, 19b4). In his mineral identification tables, smith (rd,entifi,cati,onand. qual,itatioe cherai,cal,anal,ys'i,s of mineral,s,second edition, New york, 19bB) groups minerals on the basis of specificgravity but in each of the twelve groups the minerals are listed in order of decreasinghardness. The present work should not be regarded as an index of all known minerals as the specificgravities of many minerals are unknown or known only approximately and are omitted from the current list. The list, in order of increasing specific gravity, includes all minerals without regard to other physical properties or to chemical composition. The designation I or II after the name indicates that the mineral falls in the classesof minerals describedin Dana Systemof M'ineralogyEdition 7, volume I (Native elements, sulphides, oxides, etc.) or II (Halides, carbonates, etc.) (L944 and 1951).