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Article

Metallogenic Material Source and Genesis of the Jilinbaolige Pb-Zn-Ag Deposit, the Great Xing’an Range, China: Constraints from Mineralogical, S Isotopic, and Pb Isotopic Studies of Sulfide Ores

by
Shili Han
1,2,
Sheng Wang
1,3,
Xianzhe Duan
1,2,*,
M. Santosh
4,5,
Sai Li
1,
Haoran Sun
1,
Zhenping Tang
1,2,
Kaixuan Tan
1,2,
San Liu
1,
Liang Chen
1,
Aiyang Ma
1,
Shuqin Long
1 and
Wei Liu
1
1
Department of Geology, School of Resource & Environment and Safety Engineering, University of South China, Hengyang 421001, China
2
Hunan Key Laboratory of Rare Metal Minerals Exploitation and Geological Disposal of Wastes, Hengyang 421001, China
3
Research Institute No.230, CNNC, Changsha 410007, China
4
School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China
5
Centre for Tectonics, Exploration and Research, University of Adelaide, Adelaide 5005, Australia
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(12), 1512; https://doi.org/10.3390/min12121512
Submission received: 25 October 2022 / Revised: 14 November 2022 / Accepted: 24 November 2022 / Published: 27 November 2022
(This article belongs to the Section Mineral Exploration Methods and Applications)
Browse Figures
Versions Notes

Abstract

:
The Jilinbaolige Pb-Zn-Ag polymetallic deposit is located in the eastern part of Inner Mongolia and in the central-southern part of the Great Xing’an Range, in which several large-sized Pb-Zn-Ag deposits have been found. The Jilinbaolige deposit, which occurs mainly at the contact zone between Yanshanian granite intrusion and sedimentary strata, shows strong NE-to-NNE structural control. The deposit includes three ore-forming stages: (1) the arsenopyrite–pyrite–chalcopyrite–sphalerite stage, (2) the galena–sphalerite–quartz stage, and (3) the pyrite–calcite–quartz stage. In this study, we present a systematic study on the mineralogical and geochemical characteristics (including major elements, S isotopes, and Pb isotopes) of the main sulfide ore minerals in the Jilinbaolige Pb-Zn-Ag deposit in order to evaluate the metallogenic environment, ore-forming material source, and genesis of this polymetallic deposit. The sulfide typomorphic characteristics, ore fabric, and thermometry suggest that the genesis of sulfides in the deposit is closely related to magmatic-hydrothermal activity. The early stage of mineralization might have evolved from a high-temperature hydrothermal environment. The sulfur isotopic results show that the δ34S values in the Jilinbaolige deposit range from 2.3‰ to 6.1‰, with an average value of 3.98‰, indicating that the sulfur originated from magmas with both mantle and crustal components. The Pb isotopic compositions (206Pb/204Pb = 18.214–18.330, 207Pb/204Pb = 15.478–15.615, 208Pb/204Pb = 37.957–38.292, μ = 9.24–9.50, ω = 34.49–36.49) of the sulfide ores suggest that that the lead is of crust-mantle mixed origin. The comparison between the S and Pb isotopic compositions of the Jilinbaolige deposit and the polymetallic deposits from the central-southern parts of the Great Xing’an Range suggests that these deposits have a similar metallogenic source, which is closely related to the Yanshanian granite and medium-temperature hydrothermal fluids. These ore-bearing hydrothermal fluids that evolved from deep magmatic sources migrated along the contact and fracture zones and during the subsequent gradual decrease in temperature, and the metallogenic components were deposited in the relatively open fracture and fissure space. Our results provide insights for further mineral prospecting in the south-central part of the Great Xing’an Range.

1. Introduction

The Xingmeng orogenic belt in northern China, hosting important nonferrous polymetallic deposits, is characterized by complex tectonomagmatic activities and a long history of development [1,2,3,4,5]. The central and southern parts of the Great Xing’an Range, located in the southeastern Xingmeng orogenic belt, are well known for the extensive development of nonferrous metallic deposits, attracting considerable attention in recent years [6,7,8]. The metallogenic systems include porphyries, skarns, hydrothermal veins, and alkaline granites [9]. From the Paleozoic, the movement of the Siberian and North China plates and the orogenic activity resulted in the east–west-oriented tectonic pattern of the North China Craton margin [10]. After the subduction of the Pacific plate during the Mesozoic, the central-eastern Inner Mongolia region underwent various significant episodes of faulting and volcanism. During this time, polymetallic mineralization occurred in the south-central part of the Great Xing’an Range [11,12]. In recent years, many large-sized deposits have been found in this area, including the Weilasituo and Bairendaba polymetallic deposits [13,14].
The Jilinbaolige mining area is a key region where magmatic activities were most developed during the Yanshanian period in Inner Mongolia and is located in the polymetallic metallogenic belts of the Great Xing’an Range and South Gobi–Dongwuqi (Figure 1a). Several deposits were discovered in the vicinity, including the Huanaote silver polymetallic deposit, Harhada lead–zinc, and Chaobuleng iron–zinc, indicating the potential of this region for mineralization [9,15,16,17,18,19]. Although the Jilinbaolige Pb-Zn-Ag polymetallic deposit has been investigated in previous studies, the genetic characteristics of this deposit have not been clearly understood. For example, based on the geological characteristics, prospecting indicators, and prospecting directions of the ore deposits, some studies [20,21,22] have considered that the ore deposit is genetically related to the Yanshanian granite. Some other studies [23,24] have suggested that the distribution of ore deposit is related to the Variscan intermediate–felsic magmatism.
In this study, we present results from detailed field investigations and geochemical characteristics (including major elements, S isotopes, and Pb isotopes) of the main sulfide ore minerals in the Jilinbaolige Pb-Zn-Ag deposit to understand the metallogenic environment, ore-forming material source, and genesis of the Jilinbaolige polymetallic deposit. Our results have important significance for further mineral prospecting in the central-southern part of the Great Xing’an Range.

2. Regional Geological Background

The study area (Figure 1a) is geotectonically located in the eastern part of the Dongwuqi fold belt (level IV) on the Dongwuqi–Zhalantun volcanic passive continental margin (level III) in the southeastern continental-margin accretion zone (level II) of the Siberian plate (level I; Figure 1b). During the middle part of the late Paleozoic, the Sino–Korean plate collided with the Siberian plate, and the region entered into the intracontinental orogenic stage. Formation of the Central Asian orogenic belt is related to this event, accompanied by intense volcanic activity and the intrusion of granitic magmas [27,28,29], generating a major magmatic and metallogenic belt [30,31,32,33]. The Dongwuqi area experienced the tectonic cycles of Caledonian, Hercynian, Indosinian, and Yanshanian. The transformation of oceanic and continental crusts, long-term multi-stage subduction-collision, and intracontinental orogeny occurred between the Siberian plate and the China–North Korea plate, consequently resulting in the formation of a giant orogenic belt with complex tectonic magma types [34]. A series of strong superposition, recombination, and transformation took place between the Meso–Cenozoic Binxi Pacific tectonic metallogenic domain in the NNE direction and the Paleozoic paleo-Asian tectonic metallogenic domain in the E–W direction, producing the tectonic magmatic belt of the Great Xing’an Range in the NNE–NE direction, with the formation of significant lead, zinc, silver, tin, and copper polymetallic deposits that are closely related to the Mesozoic volcanic magmatism in the study area (Figure 1c) [35,36,37].
The main ore-bearing strata in the study area are the Middle Devonian Taerbaget Formation, the Upper Devonian Angelyinwula Formation, and the lower Permian Baoligaomiao Formation. The region experienced Paleozoic rifting as well as Mesozoic intracontinental orogeny, with voluminous Paleozoic strata, accompanied with criss-cross faults and fractures and frequent magmatic activity. Hercynian and Yanshanian granites are widely distributed in the study area. The Hercynian granites are mainly island arc syncollision types, which are related to plate subduction associated with closure of the paleo-Asian Ocean, whereas those in the Yanshanian are dominated by post-orogenic granites, which were formed in an extensional tectonic setting.

3. Geological Characteristics of Ore Deposit

3.1. Geological Overview of the Jilinbaolige Mining Area

The strata exposed in the Jilinbaolige mining area are mostly late Jurassic volcanic strata on the south and northwest parts (Figure 1d). In addition, the Late Devonian Angeryinwula Formation is also exposed in a large area as a set of marine-continental silty, argillaceous, and tuffaceous clastic sedimentary rocks, which have been metamorphosed to varying degrees into argillaceous silty slate, tuffaceous slate, metasandstone, sericitized rock, and metamorphosed mudstone. The strike is dominantly northeast and north–northeast, with a moderate-to-steep dip toward the northwest. Based on previous studies and the filed investigations under this study, four lithologic sections can be identified: (1) brownish-gray and brownish-green feldspar–quartz sandstone intercalated with speckled metamorphosed mudstone (D3a2−1); (2) grayish-yellow, purple-gray, and brick-red variegated speckled metamorphosed mudstone and metamorphosed silty mudstone (D3a2−2); (3) dark-gray, blue-gray, and gray-green metamorphosed mudstone, siliceous mud, and argillaceous siltstone (D3a2−3); and (4) off-white or white metamorphosed silty mudstone and metamorphosed mudstone (D3a2−4).
Magmatic rocks (mainly felsic intrusive rocks) are widely distributed in the study area. In addition, diabase dikes and quartz veins are also present. The exposed width of the diabase dykes, which are closely related to mineralization, is generally 1–2 m, extending from tens to hundreds of meters along the strike in the direction of SN–NNE, with a dip angle of 45–60. Quartz veins range in width from about 2 to 3 m and strikes mostly in the NW and NE directions. These veins are not directly related with the mineralization and are presumed to have formed during the pre-mineralization period. On the southeastern side is the Erlianhot–Hegenshan deep fault zone, and on the northwest side is the Baiyun Hubul–Mandu Hubaolige fault zone. The strike of the regional Huanaote–Erengaobi fault (Figure 1d, F1) shows a change from north-northeast toward the northeast and dips steeply toward the northwest. This fault, which is the controlling structure of the Aqinchulu intrusion on the northwest side and also the main geologic structure in the study area, obviously controls both ore and host rocks within the southeastern boundary of the intrusion. The Jilinbaolige mining area, where the faults, folds, joints, and cleavage structures are developed, is affected by multi-stage tectonic movements. The fold structure in the mining area is a component of the Aqinchulu complex anticline. The Aqinchulu complex anticline can be divided into one syncline (Jilinbaolige syncline) and two anticlines (Habutgai and Bayantala anticlines), which are composed of the Upper Devonian Angeryinwula Formation.

3.2. Characteristics of Ore Bodies, Ores, and Surrounding Rocks

The Jilinbaolige Pb-Zn-Ag deposit, which appears in the form of hidden veins, is mainly controlled by the inner and outer contact zones of the intrusion and distributed in a nearly NE–NNE direction. Structurally controlled 138 ore (mineralized) bodies, mainly hosted in the granite bodies in the inner contact zone, have been delineated in the mining area. The ore-bearing elevation is 655–1127m, containing 71 industrial ore bodies and 14 main ore bodies. The detailed characteristics of the ore bodies are summarized in Table 1. The ore minerals are mainly pyrite, sphalerite, and galena, with a small amount of chalcopyrite, arsenopyrite, argyrite, and natural silver, while the gangue minerals are mainly quartz and clay minerals. The textures of the ore include euhedral-subhedral granular, allotriomorphic granular, metasomatic residual, and metasomatic dissolution. The structures of ore mainly include disseminated, irregular, and veinlet network veins, comparable with the main features of hydrothermal deposits. The ore deposit in the study area shows typical hydrothermal mineral assemblages, such as pyrite, chalcopyrite, galena, and sphalerite.
Alteration, such as silicification, pyritization, limonitization, sericitization, kaolinization, epidote, and chlorite, can be observed in the near-ore surrounding rocks. The ore bodies are closely related to the pyritization, limonitization, sericitization, and silicification. The range and intensity of alteration in the surrounding rock are positively correlated with the scale and grade of the ore (mineralized) bodies. The surrounding rocks on the top and bottom of the ore body are biotite monzogranite, silty slate, tuffaceous slate, and metamorphosed sandstone.

3.3. Metallogenic Stages

According to the assemblage and textural relationship among minerals, the formation sequence of metallic minerals in the Jilinbaolige deposit (Table 2) is inferred as follows: arsenopyrite→early pyrite→chalcopyrite→sphalerite→galena→late pyrite. Based on the ore structure, structure, alteration characteristics of surrounding rocks, and the relationship between the ore veins, combined with the paragenetic sequence, the Jilinbaolige deposit can be further divided into three main metallogenic stages as follows:
1.
Arsenopyrite–pyrite–chalcopyrite–sphalerite stage: Arsenopyrite, pyrite, chalcopyrite, and sphalerite are the main mineral assemblages in this stage. Under the microscope, early-crystallized arsenopyrite and pyrite show good automorphism. Pyrites are mostly medium-fine-grained euhedral and subhedral cubic grains (Figure 2a), whereas arsenopyrite is mostly fine-grained euhedral and subhedral short, columnar. granular crystals, showing dissolution of the early-crystallized pyrite (Figure 2b,c). The late-crystallized pyrites are relatively less, mostly micro-fine-grained xenomorphic and filling fissures in early arsenopyrite fissures as a fine-vein metasomatic structure (Figure 2d).
2.
Galena–sphalerite–quartz stage: This stage is an important metallogenic stage of the hydrothermal period, and the ore minerals are mainly galena and sphalerite. Galena occurs as granular aggregates. Under the microscope, galena often fills along grain margins, fissures, and pores, replacing the other sulfide minerals (Figure 2e). Sphalerite occurs in solid solution with chalcopyrite and is cut by galena (Figure 2f).
3.
Pyrite–calcite–quartz stage: This assemblage marks the culmination of the hydrothermal stage, mainly represented by carbonation. The main mineral assemblage is quartz + calcite + pyrite.

4. Analytical Method

The samples (Table 3) in this study, which were collected from different depths of different boreholes, surface, and inclined shaft positions, were cut into thin sections and polished. The mineral assemblages were studied under a polarizing microscope. The in situ compositions of the sulfides were then analyzed using an electron probe (EPMA). Three pyrite, three galena, two sphalerite, and two arsenopyrite samples were selected for sulfur and lead isotope analyses.
EPMA analyses of pyrite were conducted at the Key Laboratory of Ministry of Education for Non-ferrous Metal Mineralisation Prediction and Geological Environment Monitoring, Central South University, Hunan, China. The instrument used was a EPMA-1720H Electron Probe Microanalyzer (Shimadzu Ltd., Kyoto, Japan). The accelerating voltage and current were 15KV and 10nA, respectively. The electron beam diameter was 1–5 μm. The data were all calibrated by standard sample detection. The analytical accuracy was 5%, and the detection limit was 0.01%. In total, 7 elements (As, S, Fe, Ag, Co, Ni, and Cu) in pyrite and arsenopyrite were analyzed.
Sulfur and lead isotopes were analyzed at the Analysis Research Center of the Beijing Geological Institute of Nuclear Industry. For S isotope analysis, the isotope mass spectrometer (Deltavplus) was used, with the international standard V-CDT with an accuracy of ± 0.2 × 10−3.
For Pb isotope analysis, the properly weighed samples were put into a polytetrafluoroethylene crucible. The isotopes of the samples were analyzed after being decomposed by sulfate acid-hydrofluoric acid-nitric acid and separated by the resin exchange method, and fully dried. A thermal ion mass spectrometer (MAT-261) (Finnigan MAT Ltd., Bremen, Germany) was used in the analysis, and the mass spectrometry measurements were corrected with the international standard sample NBS981, with accuracies of 2σ < 0.05% for the 204Pb/206Pb ratio and 2σ < 0.005% for the 208Pb/206Pb ratio.

5. Results

The EMPA analytical results of pyrites and arsenopyrite in the first metallogenic stage are given in Table 4. The As contents of pyrites were generally low and fluctuated from the core to the margin of pyrite. Pyrites were slightly depleted in sulfur, with the depletion degree decreasing gradually from the core to the margin.
The analysis results of sulfur isotopes of the sulfides (pyrite, galena, sphalerite, and arsenopyrite) are given in Table 5. The data showed a limited range in δ34S (δ34S = 2.3‰–6.1‰), with δ34S = 3.98‰, on average.
Pb isotope analysis of 10 sulfide samples are shown in Table 6. The 206Pb/204Pb ratios of sulfides were 18.214–18.330, with an average value of 18.254. The ratios of 207Pb/204Pb were 15.478–15.615, with 15.539, on average, whereas those of 208Pb/204Pb were 37.957–38.292, with an average value of 38.072, indicating Th/Pb loss. These results indicate a more or less homogenous Pb isotopic composition.

6. Discussion

6.1. Metallogenic Environment

The compositional changes in the pyrite at various stages can provide important information about the changes in the environment of ore-forming fluids in the Jilinbaolige Pb-Zn-Ag deposit. As Co and Ni replace Fe in pyrite in the form of isomorphism, and the content of Co and Ni in pyrite is controlled by the physical and chemical conditions during their precipitation, the Co and Ni in pyrite can be used to identify the environment where pyrites were formed. The pyrites of different genetic types generally have different Co/Ni ratios. For example, the Co/Ni ratios of cogenetic pyrites are usually <1, whereas those of pyrites with a volcanic origin fall in the range of 5–100. In addition, the Co/Ni ratios of hydrothermal pyrite are generally >1 [42,43]. The Co/Ni ratios (Co/Ni = 1–3) of pyrites in this study suggest that the deposit is probably magmatic-hydrothermal in origin (Figure 3a).
The theoretical ω(Fe)/ω(S) value in pyrite is 0.875. The ω(Fe)/ω(S) value can reflect the genesis of pyrite, as ω(Fe)/ω(S) >0.875 shows pyrite belonging to a hydrothermal type, whereas ω(Fe)/ω(S) <0.875 indicates pyrite as a sedimentary type. The ω(Fe)/ω(S) values of pyrites range from 0.876 to 0.922, with an average value of 0.89, higher than the standard value of 0.875 [44], indicating that the pyrites are rich in Fe and depleted in S, belonging to endogenous hydrothermal types (Figure 3b).
In addition, natural bismuth and galena are coeval in the lead–zinc sulfide ore. Combined with the melting point (274 °C) temperature of natural bismuth under normal pressure conditions [45], the lead–zinc sulfides studied may have a higher metallogenic temperature, at least belonging to medium-temperature hydrothermal conditions, with a temperature range of 200 °C–300 °C.
The near-ore surrounding rocks show silicification, pyritization, sericitization, and kaolinization. The ore body is most closely related to pyritization, limonitization, silicification, and sericitization. The alteration range and intensity are positively correlated with the scale and grade of the ore (mineralized) body. The ore structures mainly include disseminated, irregular veins and veinlet network veins. The textures of the ores are euhedral-subhedral granular (arsenopyrite and pyrite), allotriomorphic granular (pyrite, sphalerite, pyrrhotite, chalcopyrite, and galena) and metasomatic residues (pyrite and pyrrhotite), and metasomatic dissolutions (galena and sphalerite). These textures and structures are in general typical characteristics of hydrothermal deposits. In addition, the deposit in this study has typical hydrothermal mineral assemblages, such as pyrite, chalcopyrite, galena, and sphalerite, which belong to the medium-temperature hydrothermal system. Furthermore, the coexisting pyrrhotite, arsenopyrite, and sphalerite indicate medium-temperature hydrothermal conditions but with slightly higher formation temperature than the former.
The compositional change of chlorite is closely related to its formation pressure, temperature, and physical-chemical conditions. The chlorite mineral thermometer has been applied to estimate the formation of ore deposits [46,47]. As the chlorites studied are aluminum-saturated, their Fe/(Fe+Mg) ratios are not corrected. The speckled chlorite thin section in sample 11 was analyzed using the energy spectrum (Figure 4). The temperatures of four micro-zone analytical points were calculated using the temperature calculation formula t(°C) = −61.92 + 321.98AlIV. After eliminating point 4, which obviously exceeds the temperature range of the chlorite thermometer (Table 7), the obtained temperature range was 334.1 °C–363.1 °C, with an average value of 349.1 °C. In addition, the estimated arsenopyrite geothermometer, based on the EMPA results of arsenopyrites with the calculated atomic percentage of 31.733%–31.976%, indicates a formation temperature of 390 °C–420 °C (Figure 5). The temperatures obtained with various geological thermometers are consistent, suggesting that the deposit has also experienced a high-temperature hydrothermal metallogenic environment.
Sulfides and other minerals in our study provide a wealth of information about the genesis of the deposit. Based on the chemical compositions of pyrite, the texture and structure, and the calculated formation temperature of chlorite mentioned before, the genesis of sulfide in the deposit is inferred to be closely related to magmatic-hydrothermal activity, suggesting that the Jilinbaolige deposit belongs to a typical magmatic-hydrothermal Pb-Zn-Ag polymetallic type. The geothermometers also suggest that the deposit experienced a relatively short high-temperature hydrothermal stage.

6.2. Source of Ore-Forming Materials

6.2.1. Source of Sulfur

Sulfur isotopes offer important information about the source of ore-forming materials and mineralization processes [48,49]. The source of sulfur before deposits is estimated based on the isotopic composition of total sulfur in the ore-forming hydrothermal fluid during sulfide precipitation. The sulfur isotopic composition in the hydrothermal fluid depends on not only the δ34S value of the source material but also the physico-chemical environment of sulfur-containing materials during the migration and precipitation of the ore-forming hydrothermal solution. It is a function of the total sulfur isotopic composition (δ34S∑S), oxygen fugacity (fO2), pH value, ionic strength, and temperature in the ore-forming solution [50,51]. When the hydrothermal system is dominated by H2S, under equilibrium conditions, δ34SΣ ≈ δ34S water ≈ δ34Spyrite [52]. Alternatively, if pyrrhotite occurs as a stable sulfide, the pH in the hydrothermal fluid is higher than 6, and H2S is the main sulfur-containing material when the temperature is lower than 500 °C, and the sulfur isotopic composition of the sulfide can represent that of the ore-forming hydrothermal solution [53]. In addition, at high temperature (T is higher than 400 °C), the sulfur in the hydrothermal system mainly occurs as H2S and SO2, whereas at medium and low temperatures (T is lower than 350 °C), the sulfur in the hydrothermal system mainly occurs as sulfate and H2S. Furthermore, when the oxygen fugacity is relatively low, S in the fluid mainly occurs as S2− and HS−, and the sulfur value of the sulfide formed is similar to that of the entire fluid. When the oxygen fugacity is high, sulfur exists in the form of SO2−, resulting in the loss of 34S in the ore-forming fluid [50]. The metallic mineral assemblage in this study is mainly sulfide. The sulfur-containing minerals mainly include sphalerite, galena, pyrrhotite, and pyrite but no sulfate minerals, suggesting that the deposit was formed under the condition of low oxygen fugacity. In addition, the paragenetic relationship of the metal sulfides in the deposit and the alteration characteristics of surrounding rocks indicate a medium-temperature hydrothermal system. These features suggest that the sulfur in the ore-forming hydrothermal system mainly occurs as H2S, and the sulfur isotopic composition of metal sulfide can approximately represent the total sulfur isotopic composition in the ore-forming fluid and thus can be used to trace the source of sulfur [50,53]. The δ34S values of sulfides from the deposit show the following sequence: pyrite > pyrrhotite > sphalerite > chalcopyrite > galena in the order under the condition of equilibrium sulfur isotope fractionation [53]. The δ34S values of various sulfides studied are in line with the enrichment order under equilibrium conditions, which is consistent with the previous results [54,55]. The main sulfides in the mineralization stage began to crystallize in sequence following their enrichment order with a gradual decrease in temperature, thereby gradually decreasing the δ34S value [56].
The δ34S values of the sulfides in this study were concentrated in the range of 2.3‰ to 6.1‰, with an average value of 3.98‰. The range of δ34S values was small (Table 5). The δ34S values of sulfides in magmatic-hydrothermal deposits (δ34S = −3‰–1‰; Hoefs [57]) are lower than those of the metallogenic stage studied. This may be due to the mixing of surrounding rocks with high S content, producing a high δ34S value of metal sulfide ores in this study [16]. However, the sulfur isotopic compositions are close to those of general igneous rocks (δ34S values are between −5‰ to 5‰ [51]) but higher than those of mantle-derived sulfurs (δ34S ranges from −3‰ to 3‰; Bi et al. [58]) (Figure 6). The sulfur isotopic characteristics suggest that the source of sulfur in the ores was not provided by mantle sulfur, magmatic sulfur, or sediments alone but by magmas with a mixture of mantle and crustal materials.
However, the Jilinbaolige deposits show δ34S composition characteristics similar to those of the other deposits in the area (Figure 6). In addition, there is a small variation in δ34S values, reflecting the consistency of the source of S in this area. Therefore, it can be suggested that the sulfurs in the Jilinbaolige deposit probably originated from magmatic-hydrothermal fluids and reflect the consistency of regional sulfur sources.

6.2.2. Sources of Lead

In general, Pb hardly undergoes fractionation in the process of migration and precipitation. Although the compositional characteristics of Pb are mainly influenced by radioactive U and Th decay reactions, they are not affected by the change in physico-chemical conditions. In addition, the U/Pb and Th/Pb ratios can be altered by processes such as magmatic evolution and differentiation, hydrothermal activity and metamorphism, and surface low-temperature weathering. Therefore, the composition and change of Pb isotopes can be used to trace the geological evolution history and also the source of metallogenic materials and the genesis of ore deposits [59,60]. The Pb isotopic composition of the Jilinbaolige deposit is nearly homogeneous (Table 6), with only a small variation, which indicates the characteristics of ordinary Pb, implying that the Pb in the deposit comes from a relatively stable lead source. Variation in the μ value of Pb isotopes can also be used to constrain the origin of Pb [61,62,63,64]. For example, higher μ values (>9.58) of Pb or the radiogenic Pb located on the right side of the zero isochron was considered to be derived from the upper crust where U and Th are relatively enriched [63], whereas lower μ values of Pb may be contributed by the lower crust or upper mantle [61]. In addition, low μ and low ω values of Pb are inherited from the characteristic of the upper mantle source [64], while low μ values and high ω values of Pb indicate the origin of the lower crust [62]. The μ values of Pb in 10 ore samples from the Jilinbaolige mining area are in the range of 9.24–9.50, with an average value of 9.36, higher than the μ value of Pb in the primitive mantle Pb (μ = 8.92) but smaller than that in the upper crust (μ = 9.58); see Table 8. The ω values of Pb range from 34.49 to 36.49, with 35.30, on average, lower than the crustal average value (μ = 36.84) and higher than the mantle value (μ = 31.84) [62]. In addition, the Th/U ratios of ore samples in the Jilinbaolige deposit are 3.61–3.72, with an average value of 3.65, higher than the Th/U value of the mantle (Th/U = 3.45) but lower than the Th/U value of crustal lead (Th/U ≈ 4); see Table 8. These data together indicate that the Pb in the Baolige deposit in Jilin is probably derived from a mixed source of the upper crust and mantle, which is also consistent with the mixed source of the crust and mantle shown by sulfur isotopes (Table 5).
The Pb isotopes sourced from mixed mantle-crustal materials are also supported by Figure 7, which shows the 206Pb/204Pb–207Pb/204Pb correlation, where the Pb isotopes in the Jilinbaolige ore samples are mostly distributed in the transition zone between the orogenic belt and the mantle evolution line, although some samples fall within the field between the upper crust and the orogenic belt. These features suggest that that Pb has mixed sources of the mantle and crust. The Pb isotope ratios of Chaganaobao, Aerhada, Huanaote, 1017 Highland, and Chaobuleng deposits all fall near and on both sides of the orogenic growth curve, also indicating that there is a mixture of mantle-derived and crust-derived Pb in the deposits in this area.
To compare the similarities and differences in Pb sources in the deposits in the southern part of the Great Xing’an Range, the Pb isotopic compositions of the Jilinbaolige deposit were compared with those of Paleozoic and Yanshanian intrusive rocks [65,66,67,68] as well as the Permian strata [67,69]. The Pb isotopic compositions of Yanshanian intrusive rocks are from feldspar separates from the intrusive rocks within or near the mining area of the southern part of the Great Xing’an Range. Some Paleozoic intrusive rocks whose Pb isotopic compositions come from feldspar separates or whole rock samples are corrected to 133 Ma [70,71]. It can be seen from the data (Figure 7) that the Pb isotopic compositions of the Jilinbaolige ores are consistent with those of the Yanshanian intrusive rocks and have no correlation with the Paleozoic intrusive rocks. The Pb isotopic compositions of Chaobuleng and Aerhada deposits are related to the Pb isotopic composition of the Permian strata.
According to different tectonic environments and genesis, Zhu [72] proposed that the Δβ-Δγ genetic classification diagram can eliminate the influence of time factors and has better tracing significance for studying the Pb source in ore [70]. The Pb isotope data in this study were calculated to obtain the relative deviations Δα, Δβ, and Δγ of Pb in the ores, which were plotted in the genetic classification diagram of Pb isotopes (Figure 8). The data points mainly fall in the magmatic Pb area where the materials from the mantle and upper crust are mixed. In addition, the points are almost close to the boundary of the Pb from the mixed magmatism of the upper crust and the mantle, from the orogenic belt, and from the mantle, indicating that the ore Pb of the Jilinbaolige deposit has the characteristics of a mixed origin of the crust and mantle. In addition, the δ34S values of the Jilinbaolige deposit show a small variation (Table 5), indicating that the sulfur in the deposit has the characteristics of a mixed deep magma source of mantle-derived and crust-derived materials. The compositional characteristics of Pb isotopes suggest that the Pb source is closely related to the deep magmatic activity and produced by upwelling magma of the mantle mixed with crustal materials. In addition, the sulfur and lead isotopic compositions of polymetallic deposits with metallogenic backgrounds similar to the Jilinbaolige deposit resemble those of the Jilinbaolige deposit; the ore-forming fluids in these deposits are an immiscible system of magmatic and meteoric water. In the early stage, the metallogenic fluids were mainly magmatic water, but mixed with meteoric water in the late stage, further indicating that the metallogenic materials of the Jilinbaolige deposit were derived from the magmas. The sources of sulfur and lead in the Jilinbaolige deposit are similar to the polymetallic deposits related to volcanic suites in the Great Xing’an Range, indicating that the metallogenic materials have consistent sources in the region.

6.3. Origin of Ore Deposits in the Region

The Great Xing’an Range area preserves the records of the link among magmatism, mineralization, and regional tectonics. The deposits in the central-southern part of the Great Xing’an Range were formed by tectonomagmatic activities in different stages, during which various metallogenic materials migrated, enriched, and precipitated during magma evolution. As mentioned before, the sulfur and lead isotopic compositions in the Jilinbaolige deposit indicate that the metallogenic materials have mixed crust-mantle characteristics. The source of metallogenic materials in the polymetallic deposits (e.g., Huanaote, 1017 Highland, Diyanqin’Amu, Alhada, Chagan’Aobao, Chaobuleng) from the central-southern parts of the Great Xing’an Range is consistent with that in the Jilinbaolige deposit and is closely related to the granitic intrusion in the Yanshanian period. Combined with the geological characteristics of the deposit, the Yanshanian deep-sourced intrusive rocks might have provided the main metallogenic materials. The contamination of deep-sourced magmas with crustal materials would increase the contents of ore-forming elements in magmas.
In addition to the granitic intrusion, the polymetallic deposits studied are also controlled by the regional structure. The Jilinbaolige mining area, located in the eastern part of the near-EW-trending Erlian–Dongwuqi polymetallic metallogenic belt, shows similarities with the Erlian–Dongwuqi polymetallic metallogenic belt, which is affected by the metallogenic events of the Great Xing’an Range metallogenic belt. During the magma intrusion, in addition to the superimposed fold deformation, the adjacent regional faults and the NE, NNE, and NWW faults show strong activity, also generating the NW-trending secondary faults, thereby facilitating the structural channel for the post-magmatic-hydrothermal fluid migration to the direction of low temperature and low pressure. The contact interface between the Aqinchulu granite body and the shallow metamorphic strata of the Angelyinwula Formation on the northwest side of the mining area is generally inclined to SE, which was conducive to the effective direct contact of the pluton and the various lithological fabrics of the Angelyinwula Formation, as well as the formation of local tension and fracture space along the interface, thus providing room for the effective accumulation of ore-forming hydrothermal fluids (Figure 9).
The extraction and leaching of ore-hosting wall rocks by mixed-source fluids is an important mechanism leading to the accumulation of ore-forming components [73]. The hydrogen and oxygen isotopic compositions of the ore-forming fluids of other typical lead–zinc–silver deposits in the Great Xing’an Range indicate the mixed characteristics of magmatic and meteoric water [55]. The ore-forming fluids of Pb-Zn-Ag polymetallic deposits in the Great Xing’an Range area are mainly magmatic water in the early stage of mineralization but dominated by atmospheric water in the late stage [55]. The deposits in this study also conform to this feature. On the basis of the geological characteristics combined with S and Pb isotopic compositions of the deposit, it is suggested that the deep-sourced magmatic-hydrothermal fluids migrated upward along structural faults, accompanied by material exchange with the surrounding rocks during the migration process, thereby gradually enriching the hydrothermal ore-forming fluids with Pb, Zn, and Ag. The mixing of magmatic and meteoric water and the water–rock reaction led to further evolution of the ore-forming hydrothermal solutions. These fluids migrated from deep to shallow levels, from the inside of the rock mass to the outer strata of the contact zone, along the contact zone and the active fracture zone, as well as the structural interface of the Angelyinwula Formation, to reduced-pressure conditions and greater relative permeability. As the temperature of the ore-forming hydrothermal solution decreased, the metals were precipitated in the relatively open fracture and fissure space, forming ore bodies, veins, ore reticulates, and patches, and thus producing the Jilinbaolige Pb-Zn-Ag polymetallic deposit (Figure 9).

7. Conclusions

The Jilinbaolige deposit is a typical magmatic-hydrothermal Pb-Zn-Ag polymetallic deposit formed under a medium-temperature hydrothermal metallogenic environment. The early stage of mineralization might have evolved from a high-temperature hydrothermal metallogenic environment.
The S and Pb isotopic compositions of sulfide ores in the deposit suggest that the sulfurs in the ores probably originated from a magmatic source, with a mixture of mantle and crustal materials. The S–Pb isotopic compositions of the Jilinbaolige deposits show a close similarity to those of the polymetallic deposits in the central-southern parts of the Great Xing’an Range, suggesting that these deposits have a similar source of metallogenic materials, which are closely related to the granite intrusion in the Yanshanian period.
Based on the systematic studies on the regional metallogenic and geological background, characteristics of ore deposits, and source of metallogenic materials, it is suggested that the Jilinbaolige deposit formed through the gradual evolution of deep magmatic fluids. These ore-bearing hydrothermal fluids migrated along the contact zone of the intrusion and fracture zones. With the gradual decrease in temperature of the ore-forming fluids, the metallogenic elements were precipitated in the relatively open fracture and fissure space, finally producing the Jilinbaolige Pb-Zn-Ag polymetallic deposit.

Author Contributions

Conceptualization, S.H. and X.D.; methodology, S.H., S.W. and X.D.; validation, S.H., X.D., S.W., K.T. and Z.T.; data curation, S.H., S.W., S.L. (Sai Li), S.L. (San Liu) and L.C.; writing—original draft preparation, S.H., X.D., M.S., S.W., S.L. (Sai Li), S.L. (San Liu), S.L. (Shuqin Long), H.S., L.C., A.M., S.L. and W.L.; writing—review and editing, S.H., X.D., M.S., K.T. and Z.T. All authors have read and agreed to the published version of the manuscript.

Funding

This work was financially supported by the National Foreign Expert Project (G2022029012L), the Outstanding Youth Project of Education Department of Hunan Province (15B201), and the Talent foundations of University of South China (2014XQD08, 2018XQD22).

Data Availability Statement

All data generated or used during the study appear in the submitted article.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 12 01512 g001 550
Figure 1. (a) Map showing the location of the study area. (b) Simplified map showing the structural outline of Inner Mongolia (Huang et al. [25]). (c) Geological and mineral map of the middle and southern Great Xing’an Range (Zhang et al. [26]). (d) Simplified geologic map of Jilinbaolige (the study area). Note: 1, Indosinian granite; 2, early Yanshanian granite; 3, Middle Hercynian Granite; 4, Late Hercynian granite and granodiorite; 5, deposit point; 6, brown gravel and sand; 7, metamorphosed silty mudstone and mudstone; 8, metamorphosed mudstone, siliceous mud, and argillaceous siltstone; 9, mottled and speckled metamorphosed mudstone and metamorphosed silty mudstone; 10, feldspathic quartz sandstone intercalated with speckled metamorphosed mudstone; 11, biotite monzonite granite; 12, quartz vein; 13, limonite mineralization and silicification–alteration zone; 14, sampling location and number; 15, concealed monzonite granite.
Figure 1. (a) Map showing the location of the study area. (b) Simplified map showing the structural outline of Inner Mongolia (Huang et al. [25]). (c) Geological and mineral map of the middle and southern Great Xing’an Range (Zhang et al. [26]). (d) Simplified geologic map of Jilinbaolige (the study area). Note: 1, Indosinian granite; 2, early Yanshanian granite; 3, Middle Hercynian Granite; 4, Late Hercynian granite and granodiorite; 5, deposit point; 6, brown gravel and sand; 7, metamorphosed silty mudstone and mudstone; 8, metamorphosed mudstone, siliceous mud, and argillaceous siltstone; 9, mottled and speckled metamorphosed mudstone and metamorphosed silty mudstone; 10, feldspathic quartz sandstone intercalated with speckled metamorphosed mudstone; 11, biotite monzonite granite; 12, quartz vein; 13, limonite mineralization and silicification–alteration zone; 14, sampling location and number; 15, concealed monzonite granite.
Minerals 12 01512 g001
Minerals 12 01512 g002 550
Figure 2. Photomicrographs of mineral assemblages, showing mineralogical characteristics of the ore samples from the Jilinbaolige deposit. (a) Cubic pyrite, (b,c) dissolution and metasomatism by arsenopyrite pyrite, (d) late pyrite filling the early arsenopyrite fissures, (e) galena replacing other sulfide minerals, and (f) galena filling along sphalerite fissures surrounding pyrite residues. Apy, arsenopyrite; Ccp, chalcopyrite; Gn, galena; Py, pyrite; Sp, sphalerite.
Figure 2. Photomicrographs of mineral assemblages, showing mineralogical characteristics of the ore samples from the Jilinbaolige deposit. (a) Cubic pyrite, (b,c) dissolution and metasomatism by arsenopyrite pyrite, (d) late pyrite filling the early arsenopyrite fissures, (e) galena replacing other sulfide minerals, and (f) galena filling along sphalerite fissures surrounding pyrite residues. Apy, arsenopyrite; Ccp, chalcopyrite; Gn, galena; Py, pyrite; Sp, sphalerite.
Minerals 12 01512 g002
Minerals 12 01512 g003 550
Figure 3. Pyrite typological characteristics. (a) Co-Ni contents of pyrite; (b) Fe-S contents of pyrite.
Figure 3. Pyrite typological characteristics. (a) Co-Ni contents of pyrite; (b) Fe-S contents of pyrite.
Minerals 12 01512 g003
Minerals 12 01512 g004 550
Figure 4. (a–d) Chlorite EDAX micro-area energy spectrum analysis.
Figure 4. (a–d) Chlorite EDAX micro-area energy spectrum analysis.
Minerals 12 01512 g004
Minerals 12 01512 g005 550
Figure 5. The relationship between sulfur fugacity and temperature in the stable area of arsenopyrite.
Figure 5. The relationship between sulfur fugacity and temperature in the stable area of arsenopyrite.
Minerals 12 01512 g005
Minerals 12 01512 g006 550
Figure 6. Distribution of sulfur isotopic composition of the Jilinbaolige deposit and polymetallic deposits in the Great Xing’an Range. Some data of the ore sulfur isotope compositions are sourced from Zhang et al. [9], Yang [15], Jia et al. [40], Ke [39], Chen [41], and Wang [19].
Figure 6. Distribution of sulfur isotopic composition of the Jilinbaolige deposit and polymetallic deposits in the Great Xing’an Range. Some data of the ore sulfur isotope compositions are sourced from Zhang et al. [9], Yang [15], Jia et al. [40], Ke [39], Chen [41], and Wang [19].
Minerals 12 01512 g006
Minerals 12 01512 g007 550
Figure 7. Comparison of the lead isotopic compositions of the Jilinbaolige deposit with other deposits in the central-southern parts of the Great Xing’an Range, as well as the Paleozoic and Yanshanian intrusive rocks and the Permian strata. Some data of the ore lead isotope compositions are sourced from Zhang et al.[9], Yang [15], Jia et al. [40], Ke [39], and Chen [41]; the lead isotope compositions of the Palaeozoic and Yanshanian intrusive rocks and the Permian strata are from Zhao and Zhang [65], Zhu et al. [66], Chu et al. [67], Jiang et al. [68], and Zeng et al. [69]; and the mantle, orogen, and upper crust evolution curves are from Zartman and Doe [63].
Figure 7. Comparison of the lead isotopic compositions of the Jilinbaolige deposit with other deposits in the central-southern parts of the Great Xing’an Range, as well as the Paleozoic and Yanshanian intrusive rocks and the Permian strata. Some data of the ore lead isotope compositions are sourced from Zhang et al.[9], Yang [15], Jia et al. [40], Ke [39], and Chen [41]; the lead isotope compositions of the Palaeozoic and Yanshanian intrusive rocks and the Permian strata are from Zhao and Zhang [65], Zhu et al. [66], Chu et al. [67], Jiang et al. [68], and Zeng et al. [69]; and the mantle, orogen, and upper crust evolution curves are from Zartman and Doe [63].
Minerals 12 01512 g007
Minerals 12 01512 g008 550
Figure 8. Diagram of Δγ–Δβ genetic classification of lead isotopes of main metal deposits in the southern part of the Great Xing’an Range. Some data of the ore lead isotope compositions are from Yang [15], Zhang et al. [9], Chen [41], and Jia et al. [40]. Figure modified according to Zhu [72].
Figure 8. Diagram of Δγ–Δβ genetic classification of lead isotopes of main metal deposits in the southern part of the Great Xing’an Range. Some data of the ore lead isotope compositions are from Yang [15], Zhang et al. [9], Chen [41], and Jia et al. [40]. Figure modified according to Zhu [72].
Minerals 12 01512 g008
Minerals 12 01512 g009 550
Figure 9. Schematic illustration of the metallogenic model of the Jilinbaolige mining area. Note: 1, Devonian Talbat Formation; 2, Devonian Angelyinwula Formation; 3, Carboniferous Baoligemiao Formation; 4, intrusive rock; 5, atmospheric precipitation; 6, magma; 7, ore body; 8, fault.
Figure 9. Schematic illustration of the metallogenic model of the Jilinbaolige mining area. Note: 1, Devonian Talbat Formation; 2, Devonian Angelyinwula Formation; 3, Carboniferous Baoligemiao Formation; 4, intrusive rock; 5, atmospheric precipitation; 6, magma; 7, ore body; 8, fault.
Minerals 12 01512 g009
Table
Table 1. Detailed characteristics of Jilinbaolige ore bodies.
Table 1. Detailed characteristics of Jilinbaolige ore bodies.
Ore Body NumberThe Maximum Length/mAverage Thickness of Ore Body/mAverage GradeOccurrence
Pb/%Zn/%Ag/10−6TowardTendencyInclination
26102.260.651.0745.260–10°270°35–50°
44101.080.491.5219.880–10°270–280°45–55°
52001.020.783.0034.3222–47°292–317°30–53°
142902.321.042.1629.7115–30°285–300°35–70°
14-12301.620.740.7739.0515–30°285–30035–70°
171302.810.811.8623.7820–40°290–310°50–55°
231102.650.720.8037.3220–30°290–300°35–55°
331442.681.371.8825.4620–40°290–310°48–60°
371392.850.811.5123.5730–35°300–305°40–50°
452452.330.380.8631.0610–15°280–285°30–50°
621553.540.841.3132.120°270°30–47°
631521.940.601.6233.05345°255°42°
662503.900.481.7633.550°270°25–47°
731101.290.691.0418.9010°280°38–43°
Table
Table 2. Mineral formation sequence of the Jilinbaolige deposit.
Table 2. Mineral formation sequence of the Jilinbaolige deposit.
Mineral NameHydrothermal Period
Early StageMiddle StageLate Stage
ArsenopyriteMinerals 12 01512 i001
PyriteMinerals 12 01512 i002Minerals 12 01512 i003Minerals 12 01512 i004
ChalcopyriteMinerals 12 01512 i005
SphaleriteMinerals 12 01512 i006Minerals 12 01512 i007
Galena Minerals 12 01512 i008
Calcite Minerals 12 01512 i009
Table
Table 3. Information about the samples analyzed in this study.
Table 3. Information about the samples analyzed in this study.
NumberPositionLithologyLight Flake
S01Makido North Peak ASilty argillaceous slateFlakes
S02Makido North Peak BSilty argillaceous slateFlakes
S03Makido North Peak CSilty slateFlakes
S04ZK2801-380 mMetamorphosed siltstoneLight sheets and flakes
S05ZK3001-221 mComplexly veined pyrite–sphalerite oreLight sheets
S06ZK3001-350 mVeinlet filled with disseminated pyrite + chloriteLight sheets and flakes
S07ZK3001-360 mMassive pyrite–sphalerite–arsenopyrite oreLight sheets
S08ZK3201-113 mVein filled with sphalerite–arsenopyrite–pyrite oreLight sheets
S09ZK3201-279 mIrregular-vein dolomite + calcite with iron–galena–sphalerite oreLight sheets
S10ZK3202-80 mSilt-bearing muddy slateLight sheets and flakes
S11ZK3202-87 mMetamorphosed siltstoneLight sheet and flake
S12ZK3202-271 mSilty argillaceous slateFlakes
S13ZK3202-315 mLight-gray and brownish argillaceous slateFlakes
S14Survey area surfaceHorned purplish-red iron-bearing sandy slateFlakes
S15Area of detailed investigation, within inclined wellLight-gray medium-grained biotite monzonite graniteFlakes
Table
Table 4. EMPA results of pyrite and arsenopyrite in the first metallogenic stage.
Table 4. EMPA results of pyrite and arsenopyrite in the first metallogenic stage.
MineralPoint NumberFeSAsAgCuCoNi
PyriteS08a-146.15152.6720.22300.0200.0430
246.40251.7360.175000.0680
346.73951.8970.226000.1000
446.26052.2710.1850.01000.0620
S08b-146.59353.1030.220000.0380
246.44552.4030.94600.0380.0270
346.73152.4610.1940.00500.0880
S10a-146.88652.3580.225000.0340.029
246.84052.6110.294000.0430.011
346.65452.1200.2950.01100.0310.013
446.71752.0010.22900.0140.0560.022
S10b-147.10551.9950.1930.00500.1210.321
247.05751.0110.2140.0060.0230.0830.020
346.65852.0580.42300.0420.0850.054
446.31652.1160.4270.00200.0870.062
ArsenopyriteS08c-134.89920.95844.5800.0330.0230.029
235.24620.96445.090.0240.0480.0680.026
S08d-134.97320.80744.89500.0240.060
234.88520.9845.07400.0050.040
Note: “Point number” shows the analysis position of the point from the core to the edge.
Table
Table 5. Sulfur isotopic compositions of the sulfides in the Jilinbaolige deposit and the polymetallic deposits in the Great Xing’an Range.
Table 5. Sulfur isotopic compositions of the sulfides in the Jilinbaolige deposit and the polymetallic deposits in the Great Xing’an Range.
DepositSample NumberTest Objectδ34S/‰Data Source
JilinbaoligeY-01Pyrite2.40This study
Y-02Pyrite3.90
Y-03Pyrite5.60
Y-04Galena2.30
Y-05Galena2.40
Y-06Galena3.30
Y-07Sphalerite4.50
Y-08Sphalerite3.40
Y-09Arsenopyrite6.10
Y-10Arsenopyrite5.90
Huanaote14GDSK2-40Galena7.05[15]
14GDSK2-40Galena6.48
14GDSK2-40Galena6.90
14GDSK2-40Galena6.55
14GDSK2-40Pyrite5.68
14GDSK2-40Pyrite6.23
14GDSK2-40Pyrite5.16
14GDSK2-40Pyrite7.12
SK2-72Sphalerite7.38
SK2-72Sphalerite7.32
SK2-72Sphalerite7.94
SK2-72Sphalerite7.48
14GD-22Galena6.28
14GD-22Galena5.64
14GD-22Pyrite5.42
GDSK2-44Galena4.28
GDSK2-44Galena2.44
GDSK2-44Galena3.35
GDSK2-44Galena4.26
14GDSK2-87Galena5.50
14GDSK2-87Galena5.34
14GDSK2-87Galena4.61
14GDSK2-87Galena4.59
14GDSK2-87Galena4.59
14GDSK2-87Galena5.37
1017 HighlandDW-73Pyrite6.60[18]
DW-74Pyrite6.80
DW-75Galena6.60
DW-77Pyrite8.00
DW-79Galena5.70
DW-82Sphalerite7.40
DW-93Pyrite3.40
DW-99Pyrite4.70
DW-101Pyrite5.10
DW-105Pyrite3.80
DW-106Pyrite3.70
DW-180Galena4.30
DW-181Galena3.40
ChaganaobaoCG7Pyrite2.20[9]
CG6Pyrite1.30
CG2Pyrite−1.20
CG23-1Sphalerite12.40
CG32Sphalerite8.90
CG46-1Sphalerite9.90
CG53Sphalerite10.10
CG52Sphalerite10.00
AerhadaTW1Galena1.20[16]
TW4Galena4.70
TW7Galena5.30
TW8Galena3.90
TW9Galena4.20
TW11Galena4.70
TW7Sphalerite6.90
TW8Sphalerite5.50
TW9Sphalerite7.50
TW10Sphalerite7.40
TW11Sphalerite7.00
TW2Pyrite8.60
TW3Pyrite7.00
TW5Pyrite7.20
TW8Pyrite6.10
TW9Pyrite6.66
TW10Pyrite7.00
TW4Arsenopyrite6.80
TW7Arsenopyrite6.60
TW11Arsenopyrite6.40
ChaobulengCBLN04Pyrite−1.70[38]
CBLN06Pyrite−0.80
CBLN07Pyrite−0.60
CBLN08Pyrite1.20
CBLN09Chalcopyrite1.40
CBLN12Chalcopyrite1.20
CBLN13Chalcopyrite2.30
CBLN14Sphalerite4.30
CBLN15Sphalerite3.80
CBLN16Galena2.50
CBLN17Galena1.80
CBLN18Pyrite2.50
CBLN19Pyrite3.20
CBLN20Galena1.60
CBLN21Sphalerite4.50
CBLN22Sphalerite6.00
CBLN23Sphalerite3.80
CBLN24Galena2.60
CBLN25Pyrite3.40
CBLN26Pyrite2.80
CBLN27Pyrite3.60
CBLN28Pyrite6.80
CBLN29Pyrite−1.20
CBLN30Pyrite−0.80
CBLN31Pyrite2.40
DiyanqinamuDYW-3Pyrite4.50[19]
DY-10Pyrite4.05
DY-25Pyrite6.80
DYS-62Pyrite8.60
DYS-35Chalcopyrite5.95
DYS-17-1Chalcopyrite10.41
DYS-17Sphalerite5.67
DYW-4Sphalerite4.40
DYW-4Galena1.78
DYW-5Galena2.27
DYW-5Galena2.36
Table
Table 6. Lead isotopic compositions of the sulfides in the Jilinbaolige deposit and the polymetallic deposits in the Great Xing’an Range.
Table 6. Lead isotopic compositions of the sulfides in the Jilinbaolige deposit and the polymetallic deposits in the Great Xing’an Range.
DepositSample NumberTest Object206Pb/204Pb207Pb/204Pb208Pb/204PbData Source
JilinbaoligeY-01Pyrite18.21915.47837.964This study
Y-02Pyrite18.21415.48737.957
Y-03Pyrite18.21915.52638.005
Y-04Galena18.32115.58238.254
Y-05Galena18.28215.60038.112
Y-06Galena18.23815.51937.958
Y-07Sphalerite18.23115.48837.987
Y-08Sphalerite18.22515.49637.994
Y-09Arsenopyrite18.33015.61538.292
Y-10Arsenopyrite18.26415.60138.201
Aerhada14AEHD-17Galena18.43915.65038.458[39]
14AEHD-18Galena18.42715.64138.400
14AEHD-23Galena18.68415.75039.298
14AEHD-30Galena18.68515.75039.301
15AEHD-18Galena18.45915.68338.565
15AEHD-23Galena18.39815.54738.172
HuanaoteGD-22Galena18.29415.54838.080[15]
GD-22Galena18.29315.54538.073
SK2-44Galena18.30315.54938.095
SK2-44Galena18.30215.54938.096
SK2-44Galena18.29815.54838.090
SK2-44Galena18.29815.54738.088
SK2-44Galena18.29315.54338.076
SK2-44Galena18.29415.54438.081
SK2-44Galena18.31015.55038.095
SK2-87Galena18.31115.54838.090
SK2-87Galena18.30915.55038.095
SK2-87Galena18.30115.54538.087
SK2-87Galena18.31315.55338.115
SK2-87Galena18.30415.54638.089
SK2-87Galena18.30415.54538.087
SK2-87Galena18.30715.54638.087
SK2-87Galena18.29815.54538.081
ChaganaobaoCG23-1Sphalerite18.24015.49537.922[9]
CG32Sphalerite18.28815.53437.988
CG46-1Sphalerite18.25515.50437.919
CG52Sphalerite18.23815.55138.113
CG53Sphalerite18.43015.69138.460
CG2Pyrite17.94915.51838.165
CG6Pyrite18.22115.48537.875
CG7Pyrite18.28715.51538.042
1017 HighlandDW-73Sphalerite18.40015.56238.177[40]
DW-74Galena18.39415.55938.163
DW-75Sphalerite18.39315.55938.162
DW-77Galena18.39115.55738.158
DW-79Sphalerite18.28615.54038.036
DW-80Pyrite18.28915.54238.044
Chaobuleng15CBL-20Pyrite18.48215.53938.244[41]
15CBL-21Pyrite18.46615.61438.358
15CBL-2Galena18.48615.62938.416
14CBL-20Galena18.44215.65938.476
15CBL-6Sphalerite18.45515.56238.211
14CBL-22Sphalerite18.42715.55438.176
14CBL-20Galena18.43115.56738.235
14CBL-20Galena18.42715.56338.222
14CBL-20Galena18.42415.56138.221
14CBL-20Sphalerite18.43015.56638.217
15CBL-1Galena18.43515.56738.221
15CBL-1Galena18.43315.56538.228
15CBL-1Galena18.44115.57338.254
Table
Table 7. Chlorite mineral thermometer estimation.
Table 7. Chlorite mineral thermometer estimation.
Micro-Area Analysis Point NumberChemical FormulaTemperature
1(Mg1.84Fe2.32AlVI1.84)[(AlIV1.28Si2.72)O10](OH)8350.2 °C
2(Mg1.93Fe2.18AlVI1.90)[(AlIV1.23Si2.77)O10](OH)8334.1 °C
3(Mg1.69Fe2.48AlVI1.83)[(AlIV1.32Si2.68)O10](OH)8363.1 °C
4(Mg1.74Fe2.74AlVI1.52)[(AlIV1.49Si2.51)O10](OH)8417.8 °C
Table
Table 8. Lead isotopic characteristics of metallic sulfides in the Jilinbaolige deposit.
Table 8. Lead isotopic characteristics of metallic sulfides in the Jilinbaolige deposit.
Sample NumberT/MaμωTh/U△α△β△γ
Y-011549.2434.493.6161.3110.0219.73
Y-021699.2634.573.6162.1710.6720.18
Y-032149.3435.093.6465.9513.4223.42
Y-042109.4436.083.7071.6117.0629.95
Y-052609.4835.873.6673.2718.4728.31
Y-061929.3234.743.6165.3512.8621.2
Y-071579.2634.613.6262.2410.6920.47
Y-081729.2834.753.6263.0511.2721.31
Y-092449.5036.493.7274.8119.3732.46
Y-102749.4836.353.7173.3218.631.33
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Han, S.; Wang, S.; Duan, X.; Santosh, M.; Li, S.; Sun, H.; Tang, Z.; Tan, K.; Liu, S.; Chen, L.; et al. Metallogenic Material Source and Genesis of the Jilinbaolige Pb-Zn-Ag Deposit, the Great Xing’an Range, China: Constraints from Mineralogical, S Isotopic, and Pb Isotopic Studies of Sulfide Ores. Minerals 2022, 12, 1512. https://doi.org/10.3390/min12121512

AMA Style

Han S, Wang S, Duan X, Santosh M, Li S, Sun H, Tang Z, Tan K, Liu S, Chen L, et al. Metallogenic Material Source and Genesis of the Jilinbaolige Pb-Zn-Ag Deposit, the Great Xing’an Range, China: Constraints from Mineralogical, S Isotopic, and Pb Isotopic Studies of Sulfide Ores. Minerals. 2022; 12(12):1512. https://doi.org/10.3390/min12121512

Chicago/Turabian Style

Han, Shili, Sheng Wang, Xianzhe Duan, M. Santosh, Sai Li, Haoran Sun, Zhenping Tang, Kaixuan Tan, San Liu, Liang Chen, and et al. 2022. "Metallogenic Material Source and Genesis of the Jilinbaolige Pb-Zn-Ag Deposit, the Great Xing’an Range, China: Constraints from Mineralogical, S Isotopic, and Pb Isotopic Studies of Sulfide Ores" Minerals 12, no. 12: 1512. https://doi.org/10.3390/min12121512

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