Tourmaline geochemistry and boron isotopic variations as a guide to fluid evolution in the Qiman Tagh W-Sn belt, East Kunlun, China
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摘要
The Qiman Tagh W-Sn belt lies in the westernmost section of the East Kunlun Orogen, NW China, and is associated with early Paleozoic monzogranites, tourmaline is present throughout this belt. In this paper we report chemical and boron isotopic compositions of tourmaline from wall rocks, monzogranites, and quartz veins within the belt, for studying the evolution of ore-forming fluids. Tourmaline crystals hosted in the monzogranite and wall rocks belong to the alkali group, while those hosted in quartz veins belong to both the alkali and X-site vacancy groups. Tourmaline in the walk rocks lies within the schorl-dravite series and becomes increasingly schorlitic in the monzogranite and quartz veins. Detrital tourmaline in the wall rocks is commonly both optically and chemically zoned,with cores being enriched in Mg compared with the rims. In the Al-Fe-Mg and Ca-Fe-Mg diagrams,tourmaline from the wall rocks plots in the fields of Al-saturated and Ca-poor metapelite, and extends into the field of Li-poor granites, while those from the monzogranite and quartz veins lie within the field of Li-poor granites. Compositional substitution is best represented by the MgFe_(-1), Al(NaR)_(-1), and AlO(Fe(OH))_(-1) exchange vectors. A wider range of δ~(11)B values from -11.1‰ to -7.1‰ is observed in the wall-rock tourmaline crystals, the B isotopic values combining with elemental diagrams indicate a source of metasediments without marine evaporates for the wall rocks in the Qiman Tagh belt. The δ~(11)B values of monzogranite-hosted tourmaline range from -10.7‰ and-9.2‰, corresponding to the continental crust sediments, and indicate a possible connection between the wall rocks and the monzogranite. The overlap in δ~(11)B values between wall rocks and monzogranite implies that a transfer of δ~(11)B values by anataxis with little isotopic fractionation between tourmaline and melts. Tourmaline crystals from quartz veins have δ~(11)B values between -11.0‰ and-9.6‰, combining with the elemental diagrams and geological features, thus indicating a common granite-derived source for the quartz veins and little B isotopic fractionation occurred. Tourmalinite in the wall rocks was formed by metasomatism by a granite-derived hydrothermal fluid, as confirmed by the compositional and geological features.Therefore, we propose a single B-rich sedimentary source in the Qiman Tagh belt, and little boron isotopic fractionation occurred during systematic fluid evolution from the wall rocks, through monzogranite, to quartz veins and tourmalinite.
The Qiman Tagh W-Sn belt lies in the westernmost section of the East Kunlun Orogen, NW China, and is associated with early Paleozoic monzogranites, tourmaline is present throughout this belt. In this paper we report chemical and boron isotopic compositions of tourmaline from wall rocks, monzogranites, and quartz veins within the belt, for studying the evolution of ore-forming fluids. Tourmaline crystals hosted in the monzogranite and wall rocks belong to the alkali group, while those hosted in quartz veins belong to both the alkali and X-site vacancy groups. Tourmaline in the walk rocks lies within the schorl-dravite series and becomes increasingly schorlitic in the monzogranite and quartz veins. Detrital tourmaline in the wall rocks is commonly both optically and chemically zoned,with cores being enriched in Mg compared with the rims. In the Al-Fe-Mg and Ca-Fe-Mg diagrams,tourmaline from the wall rocks plots in the fields of Al-saturated and Ca-poor metapelite, and extends into the field of Li-poor granites, while those from the monzogranite and quartz veins lie within the field of Li-poor granites. Compositional substitution is best represented by the MgFe_(-1), Al(NaR)_(-1), and AlO(Fe(OH))_(-1) exchange vectors. A wider range of δ~(11)B values from -11.1‰ to -7.1‰ is observed in the wall-rock tourmaline crystals, the B isotopic values combining with elemental diagrams indicate a source of metasediments without marine evaporates for the wall rocks in the Qiman Tagh belt. The δ~(11)B values of monzogranite-hosted tourmaline range from -10.7‰ and-9.2‰, corresponding to the continental crust sediments, and indicate a possible connection between the wall rocks and the monzogranite. The overlap in δ~(11)B values between wall rocks and monzogranite implies that a transfer of δ~(11)B values by anataxis with little isotopic fractionation between tourmaline and melts. Tourmaline crystals from quartz veins have δ~(11)B values between -11.0‰ and-9.6‰, combining with the elemental diagrams and geological features, thus indicating a common granite-derived source for the quartz veins and little B isotopic fractionation occurred. Tourmalinite in the wall rocks was formed by metasomatism by a granite-derived hydrothermal fluid, as confirmed by the compositional and geological features.Therefore, we propose a single B-rich sedimentary source in the Qiman Tagh belt, and little boron isotopic fractionation occurred during systematic fluid evolution from the wall rocks, through monzogranite, to quartz veins and tourmalinite.
The Qiman Tagh W-Sn belt lies in the westernmost section of the East Kunlun Orogen, NW China, and is associated with early Paleozoic monzogranites, tourmaline is present throughout this belt. In this paper we report chemical and boron isotopic compositions of tourmaline from wall rocks, monzogranites, and quartz veins within the belt, for studying the evolution of ore-forming fluids. Tourmaline crystals hosted in the monzogranite and wall rocks belong to the alkali group, while those hosted in quartz veins belong to both the alkali and X-site vacancy groups. Tourmaline in the walk rocks lies within the schorl-dravite series and becomes increasingly schorlitic in the monzogranite and quartz veins. Detrital tourmaline in the wall rocks is commonly both optically and chemically zoned,with cores being enriched in Mg compared with the rims. In the Al-Fe-Mg and Ca-Fe-Mg diagrams,tourmaline from the wall rocks plots in the fields of Al-saturated and Ca-poor metapelite, and extends into the field of Li-poor granites, while those from the monzogranite and quartz veins lie within the field of Li-poor granites. Compositional substitution is best represented by the MgFe_(-1), Al(NaR)_(-1), and AlO(Fe(OH))_(-1) exchange vectors. A wider range of δ~(11)B values from -11.1‰ to -7.1‰ is observed in the wall-rock tourmaline crystals, the B isotopic values combining with elemental diagrams indicate a source of metasediments without marine evaporates for the wall rocks in the Qiman Tagh belt. The δ~(11)B values of monzogranite-hosted tourmaline range from -10.7‰ and-9.2‰, corresponding to the continental crust sediments, and indicate a possible connection between the wall rocks and the monzogranite. The overlap in δ~(11)B values between wall rocks and monzogranite implies that a transfer of δ~(11)B values by anataxis with little isotopic fractionation between tourmaline and melts. Tourmaline crystals from quartz veins have δ~(11)B values between -11.0‰ and-9.6‰, combining with the elemental diagrams and geological features, thus indicating a common granite-derived source for the quartz veins and little B isotopic fractionation occurred. Tourmalinite in the wall rocks was formed by metasomatism by a granite-derived hydrothermal fluid, as confirmed by the compositional and geological features.Therefore, we propose a single B-rich sedimentary source in the Qiman Tagh belt, and little boron isotopic fractionation occurred during systematic fluid evolution from the wall rocks, through monzogranite, to quartz veins and tourmalinite.
引文
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Gao, Y.B., Li, W.Y., Li, Z.M., Wang, J., Keiko, H., Zhang, Z.W., Geng, J.Z., 2014. Geology,Geochemistry, and genesis of tungsten-tin deposits in the Baiganhu district,northern Kunlun belt, Northwest China. Economic Geology 109,1787-1799.
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Chen, Y.X., Pei, X.Z., Li, R.B., Liu, Z.Q., Li, Z.C., Zhang, X.F., Chen, G.C., Liu, Z.G.,Ding, S.P., Guo, J.F., 2011. Zircon U-Pb age of Xiaomiao Formation of proterozoic in the Eastern section of the East Kunlun orogenic belt. Geoscience 25, 510-521(in Chinese with English abstract).
Couch, E.L., Grim, R.E., 1968. Boron fixation by illites. Clays and Clay Minerals 16,249-256.
Da Costa, I.R., Mourao, C., Recio, C., Guimaraes, F., Antunes, I.M., Ramos, J.F.,Barriga, F.J.A.S., Palmer, M.R., Milton, J.A., 2014. Tourmaline occurrences within the Penamacor-Monsanto granitic pluton and host-rocks(Central Portugal):genetic implications of crystal-chemical and isotopic features. Contributions to Mineralogy and Petrology 167, 993.
Gao, Y.B., Li, W.Y., Li, K., Qian, B., Zhang, Z.W., Zhou, A.S., Wu, Y.S., Zhang, J.W.,Guo, Z.P., Wang, Y.L., 2012. Genesis and chronology of Baiganhu-Jialesai W-Sn mineralization belt, Qimantage, east Kunlun mountain, NW China. Northwestern Geology 45, 229-241(in Chinese with English abstract).
Gao, Y.B., Li, W.Y., Li, Z.M., Wang, J., Keiko, H., Zhang, Z.W., Geng, J.Z., 2014. Geology,Geochemistry, and genesis of tungsten-tin deposits in the Baiganhu district,northern Kunlun belt, Northwest China. Economic Geology 109,1787-1799.
Garba, I., 1996. Tourmalinization related to late Proterozoic-early Palaeozoic lode gold mineralization in the Bin Yauri area, Nigeria. Mineralium Deposita 31,201-209.
Garda, G.M., Trumbull, R.B., Beljavskis, P., Wiedenbeck, M., 2009. Boron isotope composition of tourmalinite and vein tourmalines associated with gold mineralization, Serra do Itaberaba Group, central Ribeira Belt, SE Brazil.Chemical Geology 264, 207-220.
Guo, T.Z., Tan, S.X., Chang, G.H., Ding, Y.J., Zhang, Z.Q., 2012. 40Ar/39Ar dating of the muscovite in the sericite of the Qiman Tagh ductile shear zone and itsgeological significance. Northwestern Geology 45, 94-101(in Chinese with English abstract).
Harder, H., 1970. Boron content of sediments as a tool in facies analysis. Sedimentary Geology 4,153-175.
Harraz, H.Z., El-Sharkawy, M.F., 2001. Origin of tourmaline in the metamorphosed Sikait politic belt, south Eastern Desert, Egypt. Journal of African Earth Sciences33, 391-416.
Hawthorne, F.C., Dirlam, D.M., 2011. Tourmaline the indicator mineral:from atomic arrangement to Vilking navigation. Elements 7, 307-312.
Hawthorne, F.C., Henry, D.J., 1999. Classification of the minerals of the tourmaline group. European Journal of Mineralogy 11, 201-215.
Heinrich, C.A., 1990. The chemistry of hydrothermal tin(-tungsten)ore deposition.Economic Geology 85, 457-481.
Henry, D.J., Dutrow, B.L., 1992. Tourmaline in a low grade clastic metasedimentary rock:an example of the petrogenetic potential of tourmaline. Contributions to Mineralogy and Petrology 112, 203-218.
Henry, D.J., Dutrow, B.L., 2012. Tourmaline at diagenetic to low-grade metamorphic conditions:its petrologic applicability. Lithos 154,16-32.
Henry, D.J., Dutrow, B.L., 1990. Ca substitution in Li-poor aluminous tourmaline. The Canadian Mineralogist 28,101-114.
Henry, D.J., Dutrow, B.L., 1996. Metamorphic tourmaline and its petrologic applications. In:Grew, E.S., Anovitz, L.M.(Eds.), Boron:Mineralogy, Petrology and Geochemistry. Reviews in Mineralogy, vol. 33, pp. 503-557.
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