| Citation: |
Meng Dai, Guang-sheng Yan, Yong-sheng Li, Wen-bin Jia, Fan-yu Qi, Xing Ju, 2023. Melt extraction and mineralization: A case study from the Shuangjianzishan supergiant Ag-Pb-Zn deposit (208 Mt), Inner Mongolia, NE China, China Geology, 6, 623-645. doi: 10.31035/cg2022044
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Melt extraction and mineralization: A case study from the Shuangjianzishan supergiant Ag-Pb-Zn deposit (208 Mt), Inner Mongolia, NE China
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Abstract
The supergiant Shuangjianzishan (SJZ) Ag-Pb-Zn deposit is in the southern segment of the Great Hinggan Range (SGHR), northeast China. Previous studies suggest the ore-forming material and fluid originated from the magmatic system, and the mineralization age was consistent with the diagenetic age. However, the relationship between granitic magmatism and mineralization is still unclear in the SJZ. In this study, C-H-O-He-Ar and in-situ S-Pb isotope analyses were conducted to determine the sources of ore-forming fluids and metals, which were combined with geochemistry data of SJZ granitoids from previous studies to constrain the relationship between the magmatism and the mineralization. The C-H-O-He-Ar-S-Pb isotopic compositions suggested the SJZ ore-forming material and fluids were derived from a magmatic source, which has mixed a small amount of mantle-derived materials. In addition, the disseminated sulfide from the syenogranite has comparable S-Pb isotopic composition with the sulfide minerals from ore veins, suggesting that the generation of the SJZ ore-forming fluids has a close relationship with the syenogranite magmatism. Combining with the geochemical characters of the syenogranite, the authors proposed that the mantle-derived fingerprint of the SJZ ore-forming fluid might be caused by the parent magma of the syenogranite, which was derived from partial melting of the juvenile lower crust, and underwent the residual melts segregated from a crystal mush in the shallow magma reservoir. The extraction of the syenogranite parent magma further concentrated the fertilized fluids, which was crucial to mineralization of the SJZ Ag-Pb-Zn deposit.
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Meng Dai, Guang-sheng Yan, Yong-sheng Li, Wen-bin Jia, Fan-yu Qi, Xing Ju, 2023. Melt extraction and mineralization: A case study from the Shuangjianzishan supergiant Ag-Pb-Zn deposit (208 Mt), Inner Mongolia, NE China, China Geology, 6, 623-645. doi: 10.31035/cg2022044
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Figure 1.
a‒Tectonic scheme of the Central Asian orogenic belt (CAOB, modified from Jahn BM et al., 2000; Shen P et al., 2015); b‒geologic map of the Great Hinggan Range (GHR) in northeast China showing the distribution of the Mesozoic granites and volcanic rocks (modified from Zhai DG et al., 2017); c‒geologic map of the southern Great Hinggan Range showing the locations and timing of major ore deposits (modified from Ouyang HG et al., 2015).
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Figure 2.
a‒Map of the SJZ Ag-Pb-Zn deposit (modified from Zheng GR et al., 2015①); b‒Dashizhai Formation slate; c‒unconformity interface between the Xinmin Formation and the Dashizhai Formation; d‒coarse-grained porphyritic syenogranite; e‒NE- and NW- trending ore bodies.
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Figure 3.
Prospecting line profile map of the SJZ Ag-Pb-Zn deposit (after Cai HA et al., 2021; Wang XD et al., 2018).
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Figure 4.
Representative rock samples from SJZ Ag-Pb-Zn deposit. a‒Permian slate; b‒Xinmin Formation (Jurassic dacite lava and rhyolitic tuff); c‒diorite porphyrite; d‒the contact relationship between the syenogranite and monzogranite; e‒fine-grained syenogranite; f‒coarse-grained monzogranite; g‒Photomicrographs (in cross-polarized light) of the fine-grained syenogranite; h‒plagioclase oscillatory zones in the coarse-grained monzogranite; i‒l‒micrograph of disseminated sulfides in the syenogranite. Pl‒plagioclase; Q‒quartze; Py‒pyrite; Sp‒sphalerite; Gn‒galena. Fig. 4d‒f are modified from Dai M et al., 2022
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Figure 5.
Representative Pb-Zn-Ag ores and vein cutting relationships from the SJZ Ag-Pb-Zn deposit. a‒hydrothermal breccia of host rock; b‒c‒hydrothermal breccia of host rock and early-ore-stage quartz vein in the breccia of host rock; d‒quartz crystallized around breccia/fragments of hostrocks and with sulfides filling in the vug and interstitial to quartz, minor chalcopyrite grains distributed in sulfide veins; e‒layers of comb-textured quartz and galena; f‒late-ore stage fine-grained xenomorphic pyrite and late-ore-stage calcite vein; g‒h‒zoned texture of sphalerite; i‒chalcopyrite and sphalerite replacing galena and pyrite, and chalcopyrite veins fill in the fracture of sphalerite; j‒vein-like chalcopyrite distributed in the sphalerite fracture; k‒galena replacing pyrite; l‒late-ore stage pyrite; m‒sphalerite replacing chalcopyrite and galena, and galena intergrown with polybasite and freibergite; n‒pyrargyrite occurs as intergrowths with galena; o‒canfieldite and polybasite gains grown in the fissure between sphalerite and galena grains. Photomicrographs g‒h were taken under transmitted plane-polarized light; i‒l were taken under reflected plane-polarized light. Ccp‒chalcopyrite; Gn‒galena; Py‒pyrite; Sp‒sphalerite; Caf‒canfieldite; Frb‒freibergite; Pyr‒pyrargyrite; Pol‒polybasite; Q‒quartz; Cal‒calcite.
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Figure 6.
δD vs. δ18O diagram of the ore-forming fluids in the SJZ Ag-Pb-Zn deposit. Isotopic compositions of magmatic and metamorphic waters after Taylor HP (1974), and meteoric water line after Craig H (1961). Coeval deposit D-O isotope compositions after Mei W et al., 2015; Ouyang GH et al., 2014, 2015.
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Figure 7.
δ13CPDB vs. δ18OSMOW diagram of the calcite in the SJZ Ag-Pb-Zn deposit (after Liu YF et al., 2017).
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Figure 8.
3He/4He vs. 40Ar/36Ar diagram (a), and 3He/4He vs. 40Ar*/4He (b) of fluid inclusions in sphalerite from the SJZ Ag-Pb-Zn deposit.
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Figure 9.
Photomicrographs in reflected light showing the location of in-situ S and Pb isotope values of pyrite, galena, and sphalerite. a‒pre-ores stage pyrite; b‒syn-ore stage sphalerite, chalcopyrite, galena, and pyrite; c‒post-ore pyrite; d‒The syenogranite. Py‒pyrite; Sp‒sphalerite; Gn‒galena; Ccp‒chalcopyrite.
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Figure 10.
The δ34S of representative sulfide in the different ore stages and syenogranite.
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Figure 11.
a‒in-situ 208Pb/204Pb vs. 206Pb/204Pb diagram; b‒in-situ 207Pb/204Pb vs. 206Pb/204Pb diagram; c‒in-situ 208Pb/204Pb vs. 206Pb/204Pb diagram that presents the comparison between in-situ and bulk Pb isotope data; d‒in-situ 207Pb/204Pb vs. 206Pb/204Pb diagram that presents the Pb evolution curves of galena and diorite porphyry. The shadow area represents the Pb isotope component from the Haobugao deposit, Baiyinnuoer deposit, Huanggangliang deposit, and Weilasituo deposit; the date from Jiang SH et al., 2010, 2011a, 2011b; Ouyang HG et al., 2014; Zhai DG et al., 2014; Liu LJ et al., 2018; the Triassic intrusive rocks data from Jiang SH et al., 2017; the Cretaceous intrusive rocks data from Jiang SH et al., 2017; Mei W et al., 2015; Ouyang HG et al., 2014; Zhai DG et al., 2014; the Upper Crust, Orogen, Mantle, Lower Crust Pb evolution lines from Zartman RE and Doe BR, 1981.
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Figure 12.
Harker diagrams showing the magmatic evolution of fine-grained syengranite and coarse-grained monzogranite. Data from Dai M et al. (2022) and Zhai DG et al. (2020).
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Figure 13.
Co-variations of element concentrations and elemental ratios of the fine-grained syengranite and coarse-grained monzogranite. a‒Ba vs. Sr; b‒dEu vs. SiO2 ; c‒dEu vs. Sr; and d‒Rb vs. Sr. The symbols are the same as in Fig. 12.
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Figure 14.
Trace element modeling obtained using Sr vs. Rb (a) and Eu vs. Rb (b) diagrams. Fractionating mineral assemblage resembles that in the Shuangjianzishan monzogranite. Starting compositions (Rb=240×10−6; Sr=100×10−6; Eu=0.35×10−6) have been considered to plot within the compositional gap (see text for further information). Complementary fractional crystallization models use the same starting composition tracking evolution of melt, and the cumulate crystallized from that melt. Partition coefficients have been estimated based on the assumed mineral proportions of the Shuangjianzishan monzogranite (25% quartz, 38% plagioclase, 30% alkali-feldspar, 5% biotite, 1% hornblende, 1% accessory minerals). Symbols and numbers along the lines indicate melt fraction (F). High and low partition coefficients have been tested (Appendix S1). Partition coefficients are listed in Appendix S1. Symbols are the same as in Fig. 12.
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Figure 15.
Trace element geochemistry of the fine-grained syengranite and coarse-grained monzogranite. a‒Zr/Hf vs. dEu; b‒Nb vs. dEu; c‒La/Yb vs. Rb/Sr; d‒Gd/Yb vs. Rb/Sr. The symbols are the same as in Fig. 12.
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Figure 16.
Diagrammatical model illustrating the origin of the causative intrusion and ore-forming fluid (modified from Dai M et al., 2022).