| Citation: |
Ye He, Bang-Tao Sun, Hai-Peng Wang, Jia-Xi Zhou, Yan-Jun Li, Foteini Drakou, Kai Luo, Saleh Ibrahim Bute, 2025. Geology, mineralization and model of the giant Maoping carbonate-hosted Pb-Zn deposit (5 Mt), South China, China Geology, 8, 431-453. doi: 10.31035/cg2024142
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Geology, mineralization and model of the giant Maoping carbonate-hosted Pb-Zn deposit (5 Mt), South China
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Abstract
The giant Upper Yangtze Pb-Zn metallogenic province, also known as the Sichuan-Yunnan-Guizhou (SYG) Pb-Zn province hosting >500 carbonate-hosted epigenetic Pb-Zn deposits that contain >20 Mt Pb + Zn base metal reserves. The giant Maoping Pb-Zn deposit is the second largest deposit in this province and owns >5 Mt Pb + Zn metal reserves with ore grades of 12 wt.%-30 wt.% Pb + Zn. Such large tonnages and high grades make it among the top 100 similar mineral deposits in the world. The ore bodies are predominantly located within the strata of the Upper Devonian (Zaige Formation) and Lower (Baizuo Formation)-Upper (Weining Formation) Carboniferous. The principal ore minerals consist of galena (Gn), sphalerite (Sp), and pyrite (Py), while the primary gangue minerals include dolomite (Dol), calcite (Cal), and quartz (Qtz). Three mineralization stages of carbonate minerals have been identified: (1) pre-sulfide stage 1, (2) syn-sulfide stage 2, and (3) post-sulfide stage 3. Trace elements and C-O-Sr isotopes of three stages’ carbonate minerals, together with S-Pb isotopes of sulfides, revealing that the metamorphic basement rocks played the role of the metal source during the early stage of Pb-Zn mineralization, whereas the metal contribution of the sedimentary wall rocks found to be more prominent during the late stage of Pb-Zn mineralization. In addition, the dissolution of marine carbonate rocks and CO2 degassing may have also played an important role in the formation of the Maoping deposit. Furthermore, syn-sulfide stage 2 calcite has a U-Pb age of 214 ± 20 Ma obtained by LA-ICPMS in-situ analyses, suggesting that the hydrothermal mineralization occurred during the Triassic. Our study proposes a new coupled metallogenic model of fluid-structure-lithology assemblage and provides new insights about the formation and evolution of the Maoping deposit with significant implication for understanding and exploration of similar Pb-Zn deposits worldwide.
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References
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Earth and Planetary Science Letters, 196(3-4), 113–122. doi: 10.1016/S0012-821X(01)00608-2. Zhu CW, Liao SL, Wang W, Zhang YX, Yang T, Fan HF, Wen HJ. 2018. Variations in Zn and S isotope chemistry of sedimentary sphalerite, Wusihe Zn-Pb deposit, Sichuan Province, China. Ore Geology Reviews, 95, 639–648. doi: 10.1016/j.oregeorev.2018.03.018. Zou HJ, Han RS, Hu B, Liu H. 2004. New evidences of origin of metallogenic materials in the maoping pb-zn ore deposit, Zhaotong, Yunnan: R-factor analysis results of trace elements in ne-extending fractural tectonites. Geology and Exploration, 40(5), 43–48 (in Chinese with English abstract). -
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Ye He, Bang-Tao Sun, Hai-Peng Wang, Jia-Xi Zhou, Yan-Jun Li, Foteini Drakou, Kai Luo, Saleh Ibrahim Bute, 2025. Geology, mineralization and model of the giant Maoping carbonate-hosted Pb-Zn deposit (5 Mt), South China, China Geology, 8, 431-453. doi: 10.31035/cg2024142
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Figure 1.
(a) Geological map of the Upper Yangtze Pb-Zn metallogenic province (modified from Zhou JX et al., 2018b), and (b) Tectonic map of South China. Ages are from Huang ZL et al. (2004), Li WB et al (2004a, 2004b, 2007), Yin MD et al. (2009), Liu F (2005), Liu XK et al. (2022), Lin ZY et al. (2010), Mao JW et al. (2012), Wu Y (2013), Zhang CQ et al. (2008, 2014, 2015), Zhou JX et al. (2013a, 2013c, 2015), Liao KL et al. (2020), Guan HM et al. (2020), Wang J et al. (2019) and Gong HS et al. (2021).
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Figure 2.
a–Geological map of the Maoping area and b–Stratigraphic histogram map of the Maoping Pb-Zn deposit (modified from Wang L et al., 2022).
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Figure 3.
Typical cross exploration map of the Maoping Pb-Zn deposit (modified from Wei AY et al., 2015).
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Figure 4.
Ore field photos of the Maoping Pb-Zn deposit. (a) Dol/Cal-1 veinlets in host-rocks; (b) Pb-Zn ores and Dol/Cal-1 veins interspersed by ore bodies; (c) Lumpy Dol/Cal-2 coexists with Pb-Zn ore bodies; (d), (f) Lumpy Cal-2 and Pb-Zn ores interspersed by Dol/Cal-3 veinlets; (e) Lumpy Dol-2 and Pb-Zn ores interspersed by Dol/Cal-3 veinlets. Stage 1: Dol/Cal-1, stage 2: Dol/Cal-2, stage 3: Dol/Cal-3.
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Figure 5.
Photographs of hand specimens from the Maoping deposit. (a) Two forms of calcite: agglomerates and clusters of holes, banded Sp-2 and granular Gn-1; (b) Banded Py-3 interspersed by Dol/Cal-3 veinlets; (c-d) Massive Py-2 and lumpy Dol/Cal-2 intersperses with banded Gn-2; (e) Massive Py-2 coexists with lumpy Cal-2 and Qtz; (f) Banded Sp-1 intersperses with Dol/Cal-1 veins and is interspersed by Dol/Cal-3 veinlets; (g) Massive Gn-1 coexists with lumpy Cal-2; (h) Massive Gn-1 and banded Sp-1 interspersed by Dol/Cal-3 veinlets; (i) Crystal hole clustered calcite, reddish brown Sp-1. stage 1 pyrite (Py-1), stage 2 pyrite (Py-2), stage 2 sphalerite (Sp-1), galena (Gn-1), stage 3 pyrite (Py-3), sphalerite (Sp-2), galena (Gn-2).
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Figure 6.
Textural and structural features of minerals in the Maoping Pb-Zn deposit. (a) Dol/Cal-1 veinlets within HR, and star shaped Py-1, and banded Sp-2 coexists with Dol/Cal-2; (b) Py-2 coexists with Cal-2, Banded Gn-2 interspersed with Py-2; (c) Banded Py-3 interspersed by Dol/Cal-3 veinlets; (d) Cataclastic Sp-1 coexists with Cal-2; (e) Banded Py-2 coexists with Cal-2 and intersperses Dol/Cal-1 veins, but Py-3 is interspersed by Dol/Cal-3 veinlet; (f) Gn-1 is associated with Cal-2, and is partially replaced by Sp-2, and Py-2 is fragmentary (g) Sulfides intersperse with Dol/Cal-1 stockwork with high content dolomite; (h) Cal-2 is bright yellow and coexists with sulfides; Dol-2 is bright red and coexists with sulfides; Dol/Cal-3 vein with high content dolomite intersperse with sulfides; (i) Dol/Cal-1 stockwork with high content dolomite; Dol/Cal-3 vein with high content dolomite intersperse with sulfides
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Figure 7.
Textural and structural features of minerals in the Maoping deposit under a microscope. (a) Gn-1 replaces Py-2, and both coexists with Dol-2; (b) Hypidiomorphic-xenomorphic Py-1 coexists Dol/Cal-1 veinlets in the HR, but both interspersed by Sp-1; (c) Cal-2 coexists with banded Gn-2; (d) Cal-2 coexists with Sp-1, and replaces granular Py-2; (e) Cal-2 coexists with Gn-1, and both replace fragmentary Py-2; (f-h) Sp-2 coexists with granular Py-2 and Cal-2, but interspersed by Dol/Cal-3 veinlets; (i) Py-3 replaced by Dol/Cal-3 veinlets.
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Figure 8.
Textural and structural features of minerals in the Maoping Pb-Zn deposit under a scanning electron microscope (SEM). (a) Cal-1 vein interspersed by Py-2 in host rocks; (b) mineral assemblage: quartz (Qtz) + galena (Gn-1) + sphalerite (Sp-1), Qtz replaces Gn-1 and Sp-1; (c) Cal-2 and banded Gn-2 fill fractures in the Py-2; (d) automorphic-hypidiomorphic granular Py-2 and banded Gn-2 fill fractures in the Sp-1; (e) mineral assemblage: Qtz + Sp-1 + Gn-1; (f) mineral assemblage: Qtz + Gn-2 + Py-2 + Sp-1; granular Py-2 is wrapped by Sp-1; Sp-1 and Qtz replace Gn-2; (g) Cal-2 coexists with Py-2; Dol-3 vein intersperses with Py-2; Py-2 and Cal-2 replace Gn-2 in vein; (h) Cal-2 coexists with Py-2, Gn-2 vein fills fractures in the Py-2; (i) hypidiomorphic Py-1 and vein Cal-1 in host rocks.
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Figure 9.
(a) Tera-Wasserburg concordia diagram (238U/206Pb vs. 207Pb/206Pb) of LA- ICPMS U-Pb ages of Cal-2 from the Maoping deposit. Error ellipses are 2σ, MSWD-mean square of weighted deviates, (b) Massive calcite co-occurring with sphalerite and galena, (c) Crystal-hole clustered calcite co-occurring with sphalerite and galena, and (d-e) Corresponding mineral relationships cartoon.
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Figure 10.
Box plots of (a) Sr, (b) Mn, (c) Fe, (d) ΣREE, (e) ΣLREE/ΣHREE, (f) (La/Yb) N, (g) Eu/Eu*, (h)Ce/Ce*, and (i) Y values of hydrothermal calcites from the Maoping Pb-Zn deposit.
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Figure 11.
(a) Distribution model of rare earth elements, (b) Y-ΣREE diagram of carbonate host rocks and hydrothermal carbonate minerals, (c) distribution range of C-O isotopes of carbonate host rocks and hydrothermal carbonate minerals, (d) comparison plot of 87Sr/86Sr200Ma ratios between hydrothermal minerals and sedimentary rocks. Data are from Zhou JX et al. (2018a), Deng HL et al. (2000), Shi H et al. (2003), Jiang YH and Li SR (2005), and Chen HS and Ran CY (1992).
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Figure 12.
Distribution map of S isotopes of foreign MVT Pb-Zn deposits; (b) Distribution map of S isotopes of MVT Pb-Zn deposits in the Upper Yangtze province. Data for foreign deposits are from Leach DL et al. (2005). Data for domestic deposits are from He YF et al. (2020); Ren SL et al. (2018); Xiang ZZ et al. (2020); Tan SC et al. (2019a, 2019b); Wang L et al. (2023); Xu SH et al. (2023); Yang Q et al. (2019); Yang Q (2021); Zhao WC et al. (2023); Guo X (2012); Liu HC and Lin WD (1999); Wang T (2018); Shen TLY et al. (2011); Miao Y et al. (2023); Zhou JX et al. (2011, 2013a, 2013b, 2013d, 2014a, 2014b, 2018a); Jin ZG et al. (2016); Zhang YX et al. (2014); Bai JH et al. (2013); Luo K et al. (2022); Zhang H et al. (2016); Zhu CW et al. (2018).
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Figure 13.
(a) Histogram of S isotopes distribution of the Maoping deposit; (b) Comparison of δ34S values of different types of Pb-Zn deposits and related geological bodies; δ34S values of TSR, BSR, and TDS are from Chen X and Xue CJ (2016).
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Figure 14.
(a) Comparison of 207Pb/204Pb and 206Pb/204Pb in Maoping deposit; (b) Comparison of 208Pb/204Pb and 206Pb/204Pb; Pb evolution curves for Mantle (A), Orogenic Belt (B), Upper Crust (C), and Lower Crust (D). Solid lines represent 80% of all data points in each region, and dashed lines represent the mean values (adapted from Zartman RE and Doe BR, 1981). Data for Emeishan basalts, sedimentary rocks, and basement rocks are from Liu HC and Lin WD (1999), Huang ZL et al. (2004) and Zhou JX et al. (2013c).
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Figure 15.
(a) H2CO3 and (b) HCO3- as the dominant carbon species in simulation diagram of CO2 degassing for the hydrothermal carbonate minerals; (c) simulation diagram of water-rock interaction for hydrothermal carbonate minerals.
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Figure 16.
(a) Statistics on the results of different dating methods for the Pb-Zn deposits in the Upper Yangtze province. Ages are from Huang ZL et al. (2004), Li WB et al (2004a, 2004b, 2007), Yin DM et al. (2009), Liu F (2005), Liu XK et al. (2022), Lin ZY et al. (2010), Mao JW et al. (2012), Wu Y (2013), Zhang CQ et al. (2008, 2014, 2015), Zhou JX et al. (2013a, 2013b, 2015), Shen ZW et al. (2016), Yang Q and Zhang J (2018), Yang B et al. (2018), Yang Q (2021), Wang WY et al. (2017), Tang YY et al. (2019), Liao KL et al. (2020), Guan HM et al. (2020), Gong HS et al. (2021), and this study. (b) Distribution of total contained Zn + Pb metal in global MVT deposits versus the measured mineralization age data during the Phanerozoic (data from Leach DL et al., 2010; modified from Xiong SF et al., 2022).
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Figure 17.
(a) A regional metallogenic model was proposed for the formation of Pb-Zn deposits in the Upper Yangtze province (QBOB-Qinling-Dabie Orogenic Belt; JNOB-Jiangnan Orogenic Belt; JBCS-Jinshajiang-Bangxi-Chenxing Suture; modified from Hu RZ et al., 2017), (b) A coupled metallogenic model of fluid-structure-lithology assemblage was proposed for the formation of the Maoping deposit.