Geochronology and mineralogy of the Weishan carbonatite in Shandong province, eastern China
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摘要
The Weishan REE deposit is located at the eastern part of North China Craton(NCC), western Shandong Province. The REE-bearing carbonatite occur as veins associated with aegirine syenite. LA-ICP-MS bastnaesite Th-Pb ages(129 Ma) of the Weishan carbonatite show that the carbonatite formed contemporary with the aegirine syenite. Based on the petrographic and geochemical characteristics of calcite, the REEbearing carbonatite mainly consists of Generation-1 igneous calcite(G-1 calcite) with a small amount of Generation-2 hydrothermal calcite(G-2 calcite). Furthermore, the Weishan apatite is characterized by high Sr, LREE and low Y contents, and the carbonatite is rich in Sr, Ba and LREE contents. The δ~(13)Cv-PDB(-6.5‰ to -7.9‰) and δ~(13)OV-SMOW(8.48‰-9.67‰) values are similar to those of primary, mantlederived carbonatites. The above research supports that the carbonatite of the Weishan REE deposit is igneous carbonatite. Besides, the high Sr/Y, Th/U, Sr and Ba of the apatite indicate that the magma source of the Weishan REE deposit was enriched lithospheric mantle, which have suffered the fluid metasomatism. Taken together with the Mesozoic tectono-magmatic activities, the NW and NWW subduction of Izanagi plate along with lithosphere delamination and thinning of the North China plate support the formation of the Weishan REE deposit. Accordingly, the mineralization model of the Weishan REE deposit was concluded: The spatial-temporal relationships coupled with rare and trace element characteristics for both carbonatite and syenite suggest that the carbonatite melt was separated from the CO_2-rich silicate melt by liquid immiscibility. The G-1 calcites were crystallized from the carbonatite melt, which made the residual melt rich in rare earth elements. Due to the common origin of G-1 and G-2 calcites, the REE-rich magmatic hydrothermal was subsequently separated from the melt. After that, large numbers of rare earth minerals were produced from the magmatic hydrothermal stage.
The Weishan REE deposit is located at the eastern part of North China Craton(NCC), western Shandong Province. The REE-bearing carbonatite occur as veins associated with aegirine syenite. LA-ICP-MS bastnaesite Th-Pb ages(129 Ma) of the Weishan carbonatite show that the carbonatite formed contemporary with the aegirine syenite. Based on the petrographic and geochemical characteristics of calcite, the REEbearing carbonatite mainly consists of Generation-1 igneous calcite(G-1 calcite) with a small amount of Generation-2 hydrothermal calcite(G-2 calcite). Furthermore, the Weishan apatite is characterized by high Sr, LREE and low Y contents, and the carbonatite is rich in Sr, Ba and LREE contents. The δ~(13)Cv-PDB(-6.5‰ to -7.9‰) and δ~(13)OV-SMOW(8.48‰-9.67‰) values are similar to those of primary, mantlederived carbonatites. The above research supports that the carbonatite of the Weishan REE deposit is igneous carbonatite. Besides, the high Sr/Y, Th/U, Sr and Ba of the apatite indicate that the magma source of the Weishan REE deposit was enriched lithospheric mantle, which have suffered the fluid metasomatism. Taken together with the Mesozoic tectono-magmatic activities, the NW and NWW subduction of Izanagi plate along with lithosphere delamination and thinning of the North China plate support the formation of the Weishan REE deposit. Accordingly, the mineralization model of the Weishan REE deposit was concluded: The spatial-temporal relationships coupled with rare and trace element characteristics for both carbonatite and syenite suggest that the carbonatite melt was separated from the CO_2-rich silicate melt by liquid immiscibility. The G-1 calcites were crystallized from the carbonatite melt, which made the residual melt rich in rare earth elements. Due to the common origin of G-1 and G-2 calcites, the REE-rich magmatic hydrothermal was subsequently separated from the melt. After that, large numbers of rare earth minerals were produced from the magmatic hydrothermal stage.
The Weishan REE deposit is located at the eastern part of North China Craton(NCC), western Shandong Province. The REE-bearing carbonatite occur as veins associated with aegirine syenite. LA-ICP-MS bastnaesite Th-Pb ages(129 Ma) of the Weishan carbonatite show that the carbonatite formed contemporary with the aegirine syenite. Based on the petrographic and geochemical characteristics of calcite, the REEbearing carbonatite mainly consists of Generation-1 igneous calcite(G-1 calcite) with a small amount of Generation-2 hydrothermal calcite(G-2 calcite). Furthermore, the Weishan apatite is characterized by high Sr, LREE and low Y contents, and the carbonatite is rich in Sr, Ba and LREE contents. The δ~(13)Cv-PDB(-6.5‰ to -7.9‰) and δ~(13)OV-SMOW(8.48‰-9.67‰) values are similar to those of primary, mantlederived carbonatites. The above research supports that the carbonatite of the Weishan REE deposit is igneous carbonatite. Besides, the high Sr/Y, Th/U, Sr and Ba of the apatite indicate that the magma source of the Weishan REE deposit was enriched lithospheric mantle, which have suffered the fluid metasomatism. Taken together with the Mesozoic tectono-magmatic activities, the NW and NWW subduction of Izanagi plate along with lithosphere delamination and thinning of the North China plate support the formation of the Weishan REE deposit. Accordingly, the mineralization model of the Weishan REE deposit was concluded: The spatial-temporal relationships coupled with rare and trace element characteristics for both carbonatite and syenite suggest that the carbonatite melt was separated from the CO_2-rich silicate melt by liquid immiscibility. The G-1 calcites were crystallized from the carbonatite melt, which made the residual melt rich in rare earth elements. Due to the common origin of G-1 and G-2 calcites, the REE-rich magmatic hydrothermal was subsequently separated from the melt. After that, large numbers of rare earth minerals were produced from the magmatic hydrothermal stage.
引文
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Castor, S.B., 2008. The Mountain Pass rare-earth carbonatite and associated ultrapotassic rocks, California. Canadian Mineralogist 46, 779-806.
Chakhmouradian, A.R., Mumin, A.H., Demeny, A., Elliott, B., 2008. Postorogenic carbonatites at Eden Lake, Trans-Hudson Orogen(northern Manitoba, Canada):geological setting, mineralogy and geochemistry. Lithos 103, 503-526.
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Cherniak, D.J., 2000. Rare earth element diffusion in apatite. Geochimica et Cosmochimica Acta 64, 3871-3885.
Dalton, J.A., Wood, B.J., 1993. The compositions of primary carbonate melts and their evolution throng wallrock reaction in the mantle. Earth and Planetary Science Letters 119, 511-525.
Dalton, J.A., Prenall, D.C., Dean, C., 1998. The continuum of primary carbonatitickimberlitic melt compositions in equilibrium with lherzolite:data from the system CaO-MgO-Al2O3-SiO2-CO2 at 6 GPa. Journal of Petrology 39,1953-1964.
Demeny, A., Ahijado, A., Casillas, R., Vennemann, T.W., 1998. Crustal contamination and fluid/rock interaction in the carbonatites of Fuerteventura(Canary Islands,Spain):a C, O, H isotope study. Lithos 44,101-115.
Deng, J., Chen, Y.M., Liu,Q., Yang, L.Q., 2010. The Gold Metallogenic System and Mineral Resources Exploration of Sanshandao Fault Zone. Geological Publishing House, Shandong Province. Beijing, pp. 1-371(in Chinese with English abstract).
Eggins, S.M., Woodhead, J.D., Kinsley, L.P.J., Mortimer, G.E., Sylvester, P.,McCulloch, M.T., Hergt, J.M., Handler, M.R., 1997. A simple method for the precise determination of>40 trace elements in geological samples by ICP-MS using enriched isotope internal standardisation. Chemical Geology 134,311-326.
Eggler, D.H., 1989. Carbonatites, primary melts, and mantle dynamics. In:Bell, K.(Ed.), Carbonatites:Genesis and Evolution. Unwin Hyman, London,pp. 561-579.
Freestone, I.C., Hamilton, D.L., 1980. The role of liquid immiscibility in the genesis of carbonatites-an experimental study. Contributions to Mineralogy and Petrology73,105-117.
Frietsch, R., Perdahl, J.A., 1995. Rare earth elements in apatite and magnetite in Kiruna-type iron ores and some other iron ore types. Ore Geology Reviews 9,489-510.
Halama, R.,Vennemann, T., Siebel,W.,Markl,G.,2005. The Gronnedal-Ika carbonatite-syenite complex, South Greenland:carbonatite formation by liquid immiscibility. Journal of Petrology 46,191-217.
Harmer, R.E., Gittins, J., 1998. The case for primary, mantle-derived carbonatite magma. Journal of Petrology 39,1895-1903.
Hou, Z.Q., Tian, S.H., Yuan, Z.X., Xie, Y.L., Yin, S.P., Yi, L.S., Fei, H.C., Yang, Z.M., 2006.The Himalayan collision zone carbonatites in western Sichuan, SW China:petrogenesis, mantle source and tectonic implication. Earth and Planetary Science Letters 244, 234-250.
Hu, Z.C., Liu, Y.S., Chen, L., 2011. Contrasting matrix induced elemental fractionation in NIST SRM and rock glasses during laser ablation ICP-MS analysis at high spatial resolution. Journal of Analytical Atomic Spectrometry 26, 425-430.
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