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• W868282015 abstract "The Kara scheelite-magnetite deposit is located in northwestem Tasmania 40kmsouth of Burnie at latitude 41°18' S and longitude 145° 48'E. The deposit consists of severalskam bodies with total remaining mineable ore reserves estimated at 1. 7 Mt magnetite @>30% Fe, and 0.3 Mt scheelite @ 0.52 % W03 by 1992. The major orebodies at Kara arehosted by limestone or calcareous sandstones of the Ordovician Gordon LimestoneSubgroup which are in contact with the Devonian Housetop Granite or separated from it bythe Ordovician Moina Sandstone or Owen Conglomerate.The predominant skarn minerals display a zonation that ranges from epidote-quartzto garnet, magnetite-amphibole, vesuvianite and clinopyroxene zones away from the granitecontact. Mineral paragenetic studies reveal at least four stages of skarn formation and oredeposition:1) Stage I --clinopyroxene-gamet-vesuvianite±wollastonite±quartz±scheelite,2) Stage II -gamet-vesuvianite-magnetite±scheelite±apatite±quartz,3) Stage III -magnetite-amphibole-epidote-fluorite±quartz±gamet±vesuvianite±chlorite±scheelite±sphene±hematite±pyrite±clinopyroxene, and4) Stage IV -hematite±fluorite±calcite±quartz.Stages I and II mineral assemblages represent early skarn formation and are dominated byanhydrous minerals of clinopyroxene and garnet. Stages ill and IV minerals represent lateskam-forming phases and pervasively replace early mineral assemblages. Scheelite occursin Stages I-III and generally shows a close spatial association with hydrous minerals(vesuvianite in Stage I/II and amphibole in Stage III). Abundant scheelite is found in Stageill where it forms very coarse grains up to >5cm. Magnetite occurs in Stages II and m butis also more abundant in Stage III.Microprobe analyses indicate that the majority of the skam minerals are calcic, andhave high Fe3+fFe2+. Clinopyroxene is diopside-rich generally having a mole composition of >80% diopside and <25% hedenbergite, while garnet composition from Stages I to III areandradite-rich, displaying mole proportions of> 70% andradite and <30% grossular. Garnetappears to have the highest levels of tin (up to 0.37 wt. % Sn02) and may be the majorcarrier of tin in the skarn. Amphiboles are largely of hastingsite and magnesian hastingsitecomposition. Scheelite contains moderate amounts of molybdenum ( <3 wt. % Mo03) whichgive powellite mole proportions of up to 6% and is unaccompanied by molybdenite.Fluid inclusion microthermometric measurements of primary fluid inclusions forskam minerals reveal systematic declining temperatures from early mineral assemblages tolater stages, but salinity values are variable. Stage I clinopyroxene yielded ahomogenisation temperature range of 460° to 620°C (modes at 520°C and 600°C). TheStage II minerals gave a homogenisation temperature range of 350° to 570°C (mode at500°C). The Stage ill mineral assemblage yielded homogenisation temperatures rangingfrom 240° to 360°C (mode at 300°C). Stage I clinopyroxene gave salinity values from 2.0to 10.0 equiv. wt.% Naa. The Stage II mineral assemblages showed salinities of 12.0 to16.0 equiv. wt.% NaCL The Stage ill mineral assemblage yielded salinity values of0.2 to19.8 equiv. wt. % Naa (modes at 5 and 15 equiv. wt .. % Naa).Isotopic measurements of the protolith Gordon Limestone reveal o13c compositionfrom -1.6 to -4.4 %0 (PDB) and o18o composition of 10 to 23%0 (SMOW) which are bothdepleted with respect to the unmetamorphosed Gordon Limestone values (o13c = -1.5 to1.8%0, PDB; 0180 = 22 to 27 %0, SMOW). The isotopic compositions of the Stages ill andIV skarn calcite range from -1.7 to -7.3%0 (PDB) (mean -4.5%0) for carbon and 3.4 to14.0%0 (SMOW) (mean 11 %0) for oxygen. Calculated isotopic compositions yield S13Cco2values of 0.0 to -5.0%0 (PDB) (mean -3%o) and B180H2o values of 0.0 to 10.0%0 (SMOW)(mean 7%o). Depletion in isotopic values for_the protolith marble are interpreted to bedominantly due to interaction with magmatic fluids from the nearby granite which are alsoresponsible for the formation of skam calcite. The values below the magmatic range in theskam calcite are interpreted to be due to minor contribution from meteoric fluids. Oxygenisotope values of Stages II to ill magnetite vary from 2.7 to 4.7%o (SMOW) and yieldo18oH20 values of 12.3 to 13.9%0, whereas oxygen isotopic compositions of Stages II to ill scheelite vary from 5.2 to 6.4%0 (SMOW) and yield o180H20 values of 6.0 to 9.0%0. Theseol80H20 values are generally in agreement with the isotope values from skam calcite andconfirm a magmatic source for the fluids.The geological, mineral paragenesis, mineral chemistry, fluid inclusion and stableisotope studies indicate that the Kara deposit formed in stages as a proximal skamassemblage in carbonate host rocks following the emplacement of the Devonian HousetopGranite and was characterised by early, high temperature (up to >600°C) mineralassemblages dominated by anhydrous minerals, and late low temperature (300°C)assemblages with abundant mineralisation (scheelite, magnetite) and hydrous minerals.Fluid inclusion and stable isotope data indicate that early skam formation was probablysolely due to magmatic fluids, while later skam formation and ore deposition wasdeveloped from magmatic fluids mixed with minor meteoric fluids. Chemistries ofclinopyroxene, garnet and scheelite (unaccompanied by molybdenite) suggest that the Karaskam deposit was formed under highly oxidised conditions. The deposit differs significantlyfrom other scheelite deposits such as CanTung in the abundance of magnetite (up to >90vol. % ) and lack of sulphides ( eg. pyrrhotite )." @default.
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• W868282015 date "1995-01-01" @default.
• W868282015 modified "2023-09-27" @default.
• W868282015 title "Mineral paragenesis, geochemistry and fluid characteristics of the Kara scheelite-magnetite skarn deposit, Northwestern Tasmania" @default.
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