# Genesis of the Bairendaba Ag-Zn-Pb Deposit, Southern Great Xing’an Range, NE China: A Fluid Inclusion and Stable Isotope Study

Authors: Shunda Li; Keyong Wang; Yicun Wang; Xuebing Zhang; Hongyan Quan
Journal: Geofluids
 (2017)

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## Abstract

The Bairendaba deposit is the largest Ag-Zn-Pb deposit in Inner Mongolia. Vein and disseminated ores occur in biotite-plagioclase gneiss and quartz diorite along regional EW trending faults. Microthermometric data for H2O-NaCl ± CH4  ± CO2 fluid inclusions record a decrease in homogenization temperature and salinity of ore-forming fluids with time. Early and main-stage mineralization have homogenization temperatures of 242°–395°C and 173°–334°C, respectively, compared with 138°–213°C for late-stage mineralization. Fluid salinities for early mineralization have a bimodal distribution, dominantly 4.2–11.8 wt.% NaCl equivalent, with 35.2–37.8 wt.% NaCl equivalent for a small population of halite-bearing inclusions. Main- and late-stage fluids have salinities of 2.1–10.2 wt.% NaCl equivalent and 0.7–8.4 wt.% NaCl equivalent, respectively. Oxygen and hydrogen isotope data indicate the interaction of a magmatic fluid with wall rocks in early mineralization, followed by the introduction of meteoric water during late-stage mineralization. Values of –15.9‰ to –12‰ (δ13CPDB) for hydrothermal quartz indicate that organic-rich strata were the source of carbon. Sulfur had a magmatic source, based on values of –0.1‰ to 1.5‰ (δ34SV-CDT) for sulfide minerals. The Bairendaba deposit is a typical mesothermal system with mineralization controlled by structure.


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## Body

## 1. Introduction

The southern Great Xing’an Range (SGXR) occurs in southeastern Inner Mongolia and is an important metallogenic belt in China [1–3]. It is bounded by the Hegenshan-Heihe and Xar Moron faults to the north and south, respectively, and Songliao Basin to the east (Figure 1(a)). More than fifty deposits have been discovered in this area since the 1970s, including those of Bairendaba, Mengentaolegai, Aerhada, Huaaobaote, Daolundaba, and Shuangjianshan [4–9]. These deposits occur along northeast (NE) and EW trending faults, with host rocks being mainly Permian strata. Mineralization is related to magmatic-hydrothermal activity associated with Jurassic and Cretaceous intrusions [2, 10, 11].Figure 1
(a) Tectonic map of northeastern China [29]. (b) Regional geological map of the Bairendaba district [30].The large Ag-Zn-Pb Bairendaba deposit occurs on the western edge of the SGXR (Figure1(a)). It was discovered in 2001 by the Ninth Geological Prospecting Institute of Inner Mongolia and initially developed by local prospectors. The deposit is now worked by the Inner Mongolia Yindu Mining Co. Ltd. and has proven reserves of 1.4 million t Zn, 0.6 million t Pb, and 4.6 thousand t Ag. Recent studies have examined geological features, alteration, sulfur isotopes, dating of mineralization, and the origin of ore-forming fluids [12–20]. However, additional data are necessary to better characterize the mineralizing fluids and understand ore deposition in the different stages of mineralization.Data compiled from detailed field investigations were used to select samples of quartz and fluorite, from ore veins, for this study. Fluid inclusion petrography, microthermometry, and laser Raman microprobe analyses generated data to determine phase ratios, volatile constituents, and trapping temperatures for the ore-forming fluids. Types of fluids inclusions in different veins were also determined to document changes and evolution of the hydrothermal system. Origins of fluids that formed the orebodies are based on new oxygen (O), hydrogen (H), carbon (C), and sulfur (S) isotope data. By combining the results of fluid inclusion and stable isotope studies, a genetic model is proposed for the Bairendaba Ag-Zn-Pb deposit.


## 2. Geologic Background

### 2.1. Regional Geology

Rock units in the Bairendaba district include an assemblage of Carboniferous, Permian, Jurassic, and Quaternary units surrounding a medium- to high-grade metamorphic complex of amphibole-plagioclase gneiss and biotite-plagioclase gneiss (Figure1(b)) that yield U-Pb ages of 437 ± 3 to ~316 ± 3 Ma [21, 22]. Carboniferous strata consist of marine carbonates, in contrast to Permian strata of silty slate, clastic, and volcanic rocks. Fossiliferous Permian rocks rich in organic carbon represent the main host for Ag-Zn-Pb ± Cu mineralization [23–27]. Lacustrine sedimentary and continental silicic volcanic rocks make up the Jurassic strata [28]. All rock units are partially covered by unconsolidated Quaternary sediments.Significant bodies of Paleozoic and Mesozoic intrusive igneous rocks occur throughout the region (Figure1(b)). Paleozoic granitoids include diorite and tonalite that yield U-Pb ages of 323.9–326.5 Ma [14, 15]. These rocks constitute a high-potassium, calc-alkaline magmatic suite produced under a geodynamic regime of the Paleo-Asian Ocean slab break-off [31]. Surface exposure of Mesozoic granitoids is limited to the Beidashan granitic batholith, ~5 km southeast of the Bairendaba deposit (Figure 1(b)). The mineral composition of the granitoids is mainly quartz, plagioclase feldspar, potassium feldspar, and biotite. These granitoids yield ages of 139-140 Ma [30] and are characterized by high-silica and high-alkaline types [22], indicating formation within the Circum-Pacific tectonic domain.The Bairendaba deposit occurs in Carboniferous and Permian strata comprising the southeast limb of a NE trending anticline, with a core of Paleoproterozoic metamorphic rocks (Figure1(b)). Three groups of regional faults are distinguished by their trend and style of deformation. Faults with NE trends exhibit compressional shearing, EW faults are extensional-shearing, and faults with northwest (NW) trends produced extension.


### 2.2. Deposit Geology and Mineralization

Three regional-fault trends are present at the mine scale and cut units of Paleozoic biotite-plagioclase gneiss and amphibole-plagioclase gneiss that strike N36 to ~61E and dip at 35° to ~58° to the northwest (Figure2(a)). Northeast-trending faults formed in the Hercynian, whereas EW and NW trending faults formed in the Yanshanian. Orebodies at the Bairendaba deposit occur dominantly in EW faults, with NW trending faults being a secondary control on mineralization.Figure 2
(a) Geological map of the Bairendaba Ag-Zn-Pb deposit (after the Ninth Geological Prospecting Institute of Inner Mongolia 2004). (b) Geological cross-section of the number 1 ore body (after the Ninth Geological Prospecting Institute of Inner Mongolia 2004).
(a)
(b)Intermediate-silicic igneous rocks are common in the region and occur as stocks and dykes at the Bairendaba deposit (Figure2(a)). Devonian granite, with a SHRIMP U-Pb age of 382 ± 2 Ma [32], represents the first phase of igneous activity and occurs in the northeastern part of the deposit. A SHRIMP U-Pb age of 326.5 ± 1.6 Ma dates the high-potassium calc-alkaline Carboniferous quartz diorite [15], which is cut by dolerite and granite dykes with U-Pb ages of 314.1 ± 1.7 Ma and 318 ± 1.2 Ma, respectively [33].Exploration of the Bairendaba deposit has discovered 54 orebodies, including 34 concealed orebodies. The bedded-type orebodies occur in biotite-plagioclase gneiss and adjacent quartz diorite. Most orebodies strike EW and dip at 8° to ~50° to the NW, with a smaller group that strike NW and dip at 26° to ~34° to the NE (Figure2(a)).The number 1 orebody hosts 84% of proven reserves, and ore grades are 251.5 g/t Ag, 2.8 wt.% Pb, and 6.0 wt.% Zn [34]. This economically significant orebody occurs within altered quartz diorite and is 2075 m long, has an average thickness of 3.6 m, and extends to a depth of ~1135 m (Figure 2(b)). It strikes EW and dips at 16° to ~51°, mainly to the north.Ores textures are varied and include euhedral-subhedral crystals, metasomatic dissolution features, banding, veins, disseminations, and fillings of miarolitic cavities (Figures3(e)–3(h)). The assemblage of sulfide minerals includes arsenopyrite, pyrite, pyrrhotite, sphalerite, chalcopyrite, and galena, along with minor tetrahedrite, pyrargyrite, and argentite (Figures 3(e)–3(h)). Gangue minerals are quartz, fluorite, calcite, sericite, and epidote.Figure 3
Photographs and photomicrographs of ore from the Bairendaba Ag-Zn-Pb deposit. (a) Quartz-pyrite-arsenopyrite vein. (b) Quartz-pyrite-arsenopyrite vein cut by quartz-pyrrhotite-chalcopyrite-sphalerite vein. (c) Quartz-pyrrhotite-chalcopyrite-sphalerite vein cut by Ag-sulfide quartz vein. (d) Calcite-fluorite vein. (e) Galena cut by chalcopyrite-sphalerite vein. (f) Pyrite replaced by pyrrhotite-chalcopyrite-sphalerite aggregate. (g) Pyrrhotite-chalcopyrite-sphalerite aggregate replaced by galena. (h) Pyrargyrite in galena. Qz (quartz); Po (pyrrhotite); Py (pyrite); Ccp (chalcopyrite); Sp (sphalerite); Gn (galena); Pyr (pyrargyrite).Wall-rock alteration is intense and consists of silicification, sericitization, chloritization, carbonatization, and kaolin, followed by epidotization with pyrophyllite. Silicification, chloritization, and sericitization are closely associated with Ag-Pb-Zn mineralization [18, 35].The Bairendaba deposit contains numerous hydrothermal veins of different scale (Figures3(a)–3(d)). Hypogene fissure-filling mineralization is divided into three paragenetic stages (Figure 4), based on ore mineralogy and cross-cutting relationships. These stages are recognized by four types of hydrothermal veins.Figure 4
Mineral paragenesis for the Bairendaba Ag-Zn-Pb deposit.Early mineralization (Stage 1) is subeconomic and consists of quartz-pyrite-arsenopyrite veins (A veins; Figure3(a)). The main stage of mineralization (Stage 2) is widespread and yields the majority of Ag-Zn-Pb production. Characteristic minerals are milky white quartz, chalcopyrite, pyrrhotite, sphalerite, and galena, along with minor pyrargyrite, sericite, and chlorite. Stage 2 mineralization is divided into quartz-pyrrhotite-chalcopyrite-sphalerite veins (B veins, Stage 2-1; Figure 3(b)) and Ag-sulfide quartz veins (C veins, Stage 2-2; Figure 3(c)), respectively. Late-stage mineralization (Stage 3) consists of sulfide-poor calcite and fluorite veins (D veins), which have a limited distribution near the outer edge of the deposit (Figure 3(d)).


### 2.3. Timing of Mineralization

Age data for the Bairendaba deposit indicate mineralization and alteration occurred in the Early Cretaceous. Rb-Sr dating of sphalerite, in a quartz vein, yielded an isochron age of 116 Ma [17] that is appreciably younger than the 139 to ~140 Ma Mesozoic granitoids and does not support ore formation through magmatic-hydrothermal processes. However, an 40Ar/39Ar age of 133 ± 2 Ma for sericite [14] is consistent with mineralization being associated with Mesozoic igneous rocks.


## 2.1. Regional Geology

Rock units in the Bairendaba district include an assemblage of Carboniferous, Permian, Jurassic, and Quaternary units surrounding a medium- to high-grade metamorphic complex of amphibole-plagioclase gneiss and biotite-plagioclase gneiss (Figure1(b)) that yield U-Pb ages of 437 ± 3 to ~316 ± 3 Ma [21, 22]. Carboniferous strata consist of marine carbonates, in contrast to Permian strata of silty slate, clastic, and volcanic rocks. Fossiliferous Permian rocks rich in organic carbon represent the main host for Ag-Zn-Pb ± Cu mineralization [23–27]. Lacustrine sedimentary and continental silicic volcanic rocks make up the Jurassic strata [28]. All rock units are partially covered by unconsolidated Quaternary sediments.Significant bodies of Paleozoic and Mesozoic intrusive igneous rocks occur throughout the region (Figure1(b)). Paleozoic granitoids include diorite and tonalite that yield U-Pb ages of 323.9–326.5 Ma [14, 15]. These rocks constitute a high-potassium, calc-alkaline magmatic suite produced under a geodynamic regime of the Paleo-Asian Ocean slab break-off [31]. Surface exposure of Mesozoic granitoids is limited to the Beidashan granitic batholith, ~5 km southeast of the Bairendaba deposit (Figure 1(b)). The mineral composition of the granitoids is mainly quartz, plagioclase feldspar, potassium feldspar, and biotite. These granitoids yield ages of 139-140 Ma [30] and are characterized by high-silica and high-alkaline types [22], indicating formation within the Circum-Pacific tectonic domain.The Bairendaba deposit occurs in Carboniferous and Permian strata comprising the southeast limb of a NE trending anticline, with a core of Paleoproterozoic metamorphic rocks (Figure1(b)). Three groups of regional faults are distinguished by their trend and style of deformation. Faults with NE trends exhibit compressional shearing, EW faults are extensional-shearing, and faults with northwest (NW) trends produced extension.


## 2.2. Deposit Geology and Mineralization

Three regional-fault trends are present at the mine scale and cut units of Paleozoic biotite-plagioclase gneiss and amphibole-plagioclase gneiss that strike N36 to ~61E and dip at 35° to ~58° to the northwest (Figure2(a)). Northeast-trending faults formed in the Hercynian, whereas EW and NW trending faults formed in the Yanshanian. Orebodies at the Bairendaba deposit occur dominantly in EW faults, with NW trending faults being a secondary control on mineralization.Figure 2
(a) Geological map of the Bairendaba Ag-Zn-Pb deposit (after the Ninth Geological Prospecting Institute of Inner Mongolia 2004). (b) Geological cross-section of the number 1 ore body (after the Ninth Geological Prospecting Institute of Inner Mongolia 2004).
(a)
(b)Intermediate-silicic igneous rocks are common in the region and occur as stocks and dykes at the Bairendaba deposit (Figure2(a)). Devonian granite, with a SHRIMP U-Pb age of 382 ± 2 Ma [32], represents the first phase of igneous activity and occurs in the northeastern part of the deposit. A SHRIMP U-Pb age of 326.5 ± 1.6 Ma dates the high-potassium calc-alkaline Carboniferous quartz diorite [15], which is cut by dolerite and granite dykes with U-Pb ages of 314.1 ± 1.7 Ma and 318 ± 1.2 Ma, respectively [33].Exploration of the Bairendaba deposit has discovered 54 orebodies, including 34 concealed orebodies. The bedded-type orebodies occur in biotite-plagioclase gneiss and adjacent quartz diorite. Most orebodies strike EW and dip at 8° to ~50° to the NW, with a smaller group that strike NW and dip at 26° to ~34° to the NE (Figure2(a)).The number 1 orebody hosts 84% of proven reserves, and ore grades are 251.5 g/t Ag, 2.8 wt.% Pb, and 6.0 wt.% Zn [34]. This economically significant orebody occurs within altered quartz diorite and is 2075 m long, has an average thickness of 3.6 m, and extends to a depth of ~1135 m (Figure 2(b)). It strikes EW and dips at 16° to ~51°, mainly to the north.Ores textures are varied and include euhedral-subhedral crystals, metasomatic dissolution features, banding, veins, disseminations, and fillings of miarolitic cavities (Figures3(e)–3(h)). The assemblage of sulfide minerals includes arsenopyrite, pyrite, pyrrhotite, sphalerite, chalcopyrite, and galena, along with minor tetrahedrite, pyrargyrite, and argentite (Figures 3(e)–3(h)). Gangue minerals are quartz, fluorite, calcite, sericite, and epidote.Figure 3
Photographs and photomicrographs of ore from the Bairendaba Ag-Zn-Pb deposit. (a) Quartz-pyrite-arsenopyrite vein. (b) Quartz-pyrite-arsenopyrite vein cut by quartz-pyrrhotite-chalcopyrite-sphalerite vein. (c) Quartz-pyrrhotite-chalcopyrite-sphalerite vein cut by Ag-sulfide quartz vein. (d) Calcite-fluorite vein. (e) Galena cut by chalcopyrite-sphalerite vein. (f) Pyrite replaced by pyrrhotite-chalcopyrite-sphalerite aggregate. (g) Pyrrhotite-chalcopyrite-sphalerite aggregate replaced by galena. (h) Pyrargyrite in galena. Qz (quartz); Po (pyrrhotite); Py (pyrite); Ccp (chalcopyrite); Sp (sphalerite); Gn (galena); Pyr (pyrargyrite).Wall-rock alteration is intense and consists of silicification, sericitization, chloritization, carbonatization, and kaolin, followed by epidotization with pyrophyllite. Silicification, chloritization, and sericitization are closely associated with Ag-Pb-Zn mineralization [18, 35].The Bairendaba deposit contains numerous hydrothermal veins of different scale (Figures3(a)–3(d)). Hypogene fissure-filling mineralization is divided into three paragenetic stages (Figure 4), based on ore mineralogy and cross-cutting relationships. These stages are recognized by four types of hydrothermal veins.Figure 4
Mineral paragenesis for the Bairendaba Ag-Zn-Pb deposit.Early mineralization (Stage 1) is subeconomic and consists of quartz-pyrite-arsenopyrite veins (A veins; Figure3(a)). The main stage of mineralization (Stage 2) is widespread and yields the majority of Ag-Zn-Pb production. Characteristic minerals are milky white quartz, chalcopyrite, pyrrhotite, sphalerite, and galena, along with minor pyrargyrite, sericite, and chlorite. Stage 2 mineralization is divided into quartz-pyrrhotite-chalcopyrite-sphalerite veins (B veins, Stage 2-1; Figure 3(b)) and Ag-sulfide quartz veins (C veins, Stage 2-2; Figure 3(c)), respectively. Late-stage mineralization (Stage 3) consists of sulfide-poor calcite and fluorite veins (D veins), which have a limited distribution near the outer edge of the deposit (Figure 3(d)).


## 2.3. Timing of Mineralization

Age data for the Bairendaba deposit indicate mineralization and alteration occurred in the Early Cretaceous. Rb-Sr dating of sphalerite, in a quartz vein, yielded an isochron age of 116 Ma [17] that is appreciably younger than the 139 to ~140 Ma Mesozoic granitoids and does not support ore formation through magmatic-hydrothermal processes. However, an 40Ar/39Ar age of 133 ± 2 Ma for sericite [14] is consistent with mineralization being associated with Mesozoic igneous rocks.


## 3. Samples and Analytical Methods

Fluid inclusions were studied in samples of quartz and fluorite of vein types A–D, representing Stages 1–3. Fluid inclusion microthermometric analyses were conducted on a Linkam THMS600 heating-freezing stage with a temperature range of –196 to 600°C. Calibration of the stage was completed using the following standards: pure water inclusions (0°C), pure CO2 inclusions (–56.6°C), and potassium bichromate (398°C). This yielded an accuracy of ±0.2°C during freezing and ±2°C for heating between 100° and 600°C. Fluid salinities for NaCl-H2O inclusions were calculated using the final melting temperature of ice [36].Fluid inclusion volatiles were analyzed using a Renishaw RM1000 Raman microprobe and Ar ion laser. Operating conditions for the Raman microprobe include the following: a surface power of 5 mW and exciting radiation of 514.5 nm; area of 20μm2 for the detector charge-coupled device (CCD); spectra set to scanning range of 1000 to 4000/cm with an accumulation time of 30 s per scan. All fluid inclusion studies were conducted at the Geological Fluid Laboratory, College of Earth Science, Jilin University, China.Samples of hydrothermal quartz from Stages1-2, excluding D veins, were analyzed for O-H-C isotopes. Quartz samples for O-C isotope analyses were treated with orthophosphoric acid at 50°C for 24 h to generate CO2 [37]. Samples of quartz for H isotope analyses were placed under vacuum and heated at 150°C for 3 h to degas labile volatiles. Water was released from fluid inclusions by heating to approximately 500°C, using an induction furnace, and then converted into H2 through interaction with Zn powder at a temperature of 410°C [38]. Finally, conventional methods were used to produce SO2 gas from different sulfide minerals to measure S isotopes [39]. All samples were analyzed using a MAT-252 mass spectrometer, with analytical uncertainty of <0.1‰, housed at the Analytical Laboratory Beijing Research Institute of Uranium Geology, China.


## 4. Results

### 4.1. Fluid Inclusion Petrography

Criteria established by Roedder [40] and Hollister and Burruss [41] were used to distinguish different generations of fluid inclusions in hydrothermal quartz and fluorite. Primary inclusions are isolated or occur in random groups, compared with secondary inclusions filling microcracks. Populations of different fluid inclusion types were recognized by room temperature phase relationships, phase transitions during heating and cooling, and laser Raman spectroscopy results. Four types of fluid inclusions were identified using the nomenclature of Ramboz et al. [42], which are CH4-rich (Type Ι), CH4-CO2-H2O (Type ΙΙ), H2O-rich (Type III), and halite-bearing (Type ΙV) types.Type Ι inclusions consist of liquid water and CH4 at room temperature, with a degree of fill ranging from 0.2 to ~0.6 (Figure 5(a)). These inclusions are common in A veins (Stage 1) and occur as bands or clusters or in isolation. They have irregular or negative crystal shapes and are typically 10 to 30 μm in size.Figure 5
Photomicrographs of fluid inclusions in Stages 1–3 quartz and fluorite in the Bairendaba Ag-Zn-Pb deposit. ((a), (b), (c)) Type Ι, Type III, and Type ΙV inclusions in Stage 1 quartz. ((d), (e)) Type ΙΙ and Type III inclusions in Stage2-1 quartz. ((f), (g)) Type ΙΙ and Type III inclusions in Stage 2-1 quartz. ((h), (i)) Type III inclusions in Stage 3 fluorite. L (liquid phase), V (vapor phase), and S (halite crystal).Type ΙΙ inclusions appear similar to Type I at room temperature (Figures5(d)–5(f)). However, the addition of a CO2 component to CH4 in Type ΙΙ inclusions is evident during freezing and laser Raman microprobe measurements. These inclusions are absent from A veins and can occur in isolation but are more common as clusters and trails in B and C veins (Stage 2). They have regular shapes (e.g., ellipsoidal or negative crystal) and are 10 to 30 μm in size.Type III fluid inclusions are liquid water dominant and have vapor contents of 10% to ~45% and variable shapes (e.g., irregular and ellipsoidal), ranging in size from 5 to 20μm (Figures 5(c), 5(g)–5(i)). These inclusions are present in all stages of mineralization and commonly occur as planar arrays restricted to the interiors of quartz and fluorite grains. However, some Type III inclusions fill microfractures in Stages 1-2 quartz and Stage 3 fluorite, indicating a secondary origin (Figures 5(c) and 5(i)).Type ΙV fluid inclusions contain three phases at room temperature, which are a vapor bubble, liquid water, and halite cube (Figure5(b)). Halite-bearing inclusions are uncommon and coexist with Types I and III in A veins of Stage 1 mineralization. Type ΙV inclusions are always <20 μm in size and occur in isolation or discrete clusters, implying a primary origin [40].


### 4.2. Fluid Inclusion Microthermometry

Primary fluid inclusions larger than 5μm with a regular crystal shape, which show no signs of necking [40], were chosen for microthermometric analyses. Data for Stages 1–3 are listed in Table 1. Histograms of homogenization temperatures (Th) and salinity of different types of fluid inclusions in Stages 1-2 quartz and Stage 3 fluorite are presented in Figure 6.Table 1
Microthermometric data for fluid inclusions in hydrothermal quartz and fluorite, Bairendaba Ag-Zn-Pb deposit.
Stage
Host mineral
Inclusion Type
Tm(CO2) (°C)
Th(CO2) (°C)
Tm(clath) (°C)
Tm(ice) (°C)
Tm(NaCl) (°C)
Salinity (NaCl wt.%)
Th (°C)
Stage 1
Quartz
I (65)
−182.1 to −180.2
−99.3 to −68.4
11.2–18.9
NA
NA
NA
267–395
III (39)
NA
NA
NA
−8.1 to −2.5
NA
4.2–11.8
242–351
IV (5)
NA
NA
NA
NA
258–295
35.2–37.8
259–372
Stage2-1
Quartz
II (62)
−79.5 to −59.6
−52.1 to −2.8
7.9–16.8
NA
NA
NA
246–334
III (38)
NA
NA
NA
−6.8 to −1.6
NA
2.7–10.2
205–312
Stage2-2
Quartz
II (65)
−63.4 to −57.7
−6.9 to 10.2
9.5–13.8
NA
NA
NA
173–282
III (44)
NA
NA
NA
−5.9 to −1.2
NA
2.1–9.1
179–269
Stage 3
Fluorite
III (57)
NA
NA
NA
−5.4 to −0.4
NA
0.7–8.4
138–213
Tm(ice), temperature of final ice melting; Tm(NaCl), melting temperature of halite crystals; (65) is the number of inclusions measured.Figure 6
Histograms of microthermometric data for fluid inclusions in hydrothermal quartz and fluorite of the Bairendaba Ag-Zn-Pb deposit. (a) Homogenization temperatures for Types Ι, III, and ΙV; Stage 1 quartz. (b) Salinity for Types III and ΙV; Stage 1 quartz. (c) Homogenization temperatures for Types ΙΙ and III; Stage2-1 quartz. (d) Salinity for Type III; Stage 2-1 quartz. (e) Homogenization temperatures for Types ΙΙ and III; Stage 2-2 quartz. (f) Salinity for Type III; Stage 2-2 quartz. (g) Homogenization temperatures for Type III; Stage 3 fluorite. (h) Salinity for Type III; Stage 3 fluorite.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)Stage 1 quartz veins contain abundant Type I and III fluid inclusions, but rare Type IV inclusions. Type I inclusions freeze below –185°C and melting of the carbonic phase (TmCO2) occurs at –182.1° to –180.2°C (Table 1). This behavior indicates the vapor phase is nearly pure CH4. Homogenization of the carbonic phase (ThCO2) to vapor occurs at –99.3° to –68.4°C, and clathrate melting (TmClath) between 11.2° and 18.9°C (Table 1) is much higher than the invariant point (e.g., 10°C) of a pure CO2 clathrate [41]. Type Ι inclusions with a high degree of fill decrepitate at ~350°C, prior to final homogenization, probably due to increased internal pressures of CH4 [40]. In contrast, Type Ι inclusions with a low degree of fill have Th of 267°–395°C (Figure 6(a)). Type III inclusions homogenize to the liquid phase at 242°–351°C (Figure 6(a)) and final ice melting at –8.1° to –2.5°C indicates salinities of 4.2–11.8 wt.% NaCl equivalent (Figure 6(b)). Halite crystals in Type ΙV inclusions dissolve at 258°–295°C, indicating salinities of 35.2–37.8 wt.% NaCl equivalent, and they have final homogenization to the liquid phase at 259°–372°C (Figures 6(a) and 6(b)).Stage2-1 and 2-2 quartz veins contain Type ΙΙ and III fluid inclusions. Fluid inclusion data for Stage 2-1 are presented first. Type ΙΙ inclusions freeze below –130°C and TmCO2 occurs between –79.5° and –59.6°C (Table 1), significantly lower than melting of pure CO2 at –56.6°C. This indicates the carbonic phase, which is mostly CH4, also contains CO2 and/or N2 [42]. Homogenization of the carbonic phase to vapor occurs between –52.1° and 2.8°C and TmClath at 7.9° to 16.8°C (Table 2). Final homogenization to the liquid phase could only be determined for fluid inclusions with a low degree of fill and Th which are 246°–334°C (Figure 6(c)). Type III inclusions homogenize to the liquid phase at 205–312°C and final ice melting at –6.8° to –1.6°C indicates salinities of 2.7–10.2 wt.% NaCl equivalent (Figures 6(c) and 6(d)).Table 2
Oxygen, hydrogen, and carbon isotope data for hydrothermal quartz of Stages1-2, Bairendaba Ag–Zn–Pb deposit.
Vein type
Stages
Sample description
δ
18
O
V
-
S
M
O
W/%
δ
D
V
-
S
M
O
W/%
Th (°C)
δ
18
O
H
2
O
-
S
M
O
W/%
δ
C
V
-
P
D
B/%
A veins
1
Quartz
14.1
−113.4
320
7.9
−13.2
A veins
1
Quartz
14.2
−114.2
280
6.6
−12.8
A veins
1
Quartz
14.0
−114
320
7.8
−13.1
A veins
1
Quartz
14.1
−114.6
280
6.5
−12.9
B veins
2-1
Quartz
14.0
−116.2
300
7.1
−12.9
B veins
2-1
Quartz
13.9
−116.3
260
5.4
−15.8
B veins
2-1
Quartz
13.3
−116.7
300
6.4
−12.8
B veins
2-1
Quartz
13.2
−116.5
260
4.7
−15.7
C veins
2-2
Quartz
13.7
−117.4
240
4.3
−15.9
C veins
2-2
Quartz
13.6
−117.6
200
1.9
−12.1
C veins
2-2
Quartz
13.7
−124.4
240
4.3
−15.9
C veins
2-2
Quartz
13.5
−124.6
200
1.8
−12.0Fluid inclusion Types ΙΙ and III, representing Stage2-2, have lower Th and are less saline than Stage 2-1 (Figures 6(c)–6(f)). Type ΙΙ inclusions freeze below –100°C and TmCO2 occurs at –63.4° to –57.7°C (Table 2). This behavior is consistent with the presence of small concentrations of CH4 and/or N2 in addition to CO2 [44–46]. Homogenization of the carbonic phase to vapor occurs at –6.9° to 10.2°C and TmClath between 9.5° and 13.8°C (Table 2). Final homogenization to the liquid phase could only be determined for inclusions with a low degree of fill and occurs at 173°–282°C (Figure 6(e)). Type III inclusions homogenize to the liquid phase at 179°–269°C and final ice melting at –5.9° to –1.2°C indicates salinities of 2.1–9.1 wt.% NaCl equivalent (Figures 6(e) and 6(f)).Fluorite veins representing Stage 3 contain only Type III fluid inclusions that record the lowest Th and salinities for the Bairendaba deposit (Figures6(a)–6(h)). Homogenization to the liquid phase occurs at 138°–213°C and final ice melting at –5.4° to –0.4°C indicates salinities of 0.7–8.4 wt.% NaCl equivalent (Figures 6(g) and 6(h)).


### 4.3. Laser Raman Microprobe Analysis

The data obtained by laser Raman microprobe analyses of fluid inclusions in Stages1-2 quartz and Stage 3 fluorite are presented in Figure 7. Type Ι inclusions for Stage 1 contain a vapor phase dominated by CH4 (Figures 7(a) and 7(b)), whereas Type ΙΙ inclusions for Stage 2 contain different amounts of CH4 and CO2 (Figures 7(c)–7(e)). No pure CO2 inclusions were identified in this study. The vapor phase of Type III inclusions consists solely of water (Figure 7(f)).Figure 7
Laser Raman microspectrometry of primary fluid inclusions in hydrothermal quartz and fluorite of the Bairendaba Ag-Zn-Pb deposit. ((a), (b)) Type Ι inclusions in Stage 1 quartz. ((c), (d)) Type ΙΙ inclusions in Stage2-1 quartz. (e) Type ΙΙ inclusions in Stage 2-2 quartz. (f) Type III inclusions in Stage 3 fluorite.
(a)
(b)
(c)
(d)
(e)
(f)


### 4.4. Oxygen, Hydrogen, and Carbon Isotopes

Isotope data for 12 quartz samples representing A-C veins in the Bairendaba deposit are reported asδ18OV-SMOW, δDV-SMOW, and δ13CPDB values. Ranges in the data are limited and are as follows: 13.2‰ to 14.2‰ (δ18OV-SMOW); –124.6‰ to –113.4‰ (δDV-SMOW); –15.9‰ to –12.0‰ (δ13CPDB; Table 2). Values of 1.8‰ to 7.9‰ (δ18OH2O-SMOW; Table 2) were calculated using the formula of Clayton et al. [59] and Th of fluid inclusions. These δD and δ18O values are consistent with previously published data [17, 33, 47, 60]. The C isotope data in this study are unique, because this is the first time C isotopes were measured for the gas phase of fluid inclusions in hydrothermal quartz representing Stages 1-2 of the Bairendaba deposit. Previous work by Ouyang [33] generated data strictly for Stage 3 fluorite-calcite veins.


### 4.5. Sulfur Isotopes

Sulfur isotope analyses were completed for mineral separates of pyrite, pyrrhotite, galena, and sphalerite extracted from ore veins. All data are reported asδ34V-CDT values. Sulfide minerals from the number 1 orebody of the Bairendaba Ag-Zn-Pb deposit have a limited range of –0.1‰ to 1.5‰ (Table 3), which are consistent with previously published data [17, 33, 47].Table 3
Sulfur isotope data for ore minerals of the Bairendaba Ag-Zn-Pb deposit.
Sample
Mineral
δ
34
S
C
D
T/‰
Sample location
BR1-1
Pyrite
0.2
Number 1 orebody at 1275 m level
BR1-2
Pyrite
−0.1
Number1 orebody at 1145 m level
BR2-1
Pyrrhotite
1.5
Number 1 orebody at 1275 m level
BR2-2
Pyrrhotite
1.4
Number 1 orebody at 1145 m level
BR3
Sphalerite
0.5
Number 1 orebody at 1270 m level
BR4
Sphalerite
0.9
Number 1 orebody at 1142 m level
BR5
Galena
0.5
Number 1 orebody at 1270 m level
BR6
Galena
0.5
Number 1 orebody at 1142 m level


## 4.1. Fluid Inclusion Petrography

Criteria established by Roedder [40] and Hollister and Burruss [41] were used to distinguish different generations of fluid inclusions in hydrothermal quartz and fluorite. Primary inclusions are isolated or occur in random groups, compared with secondary inclusions filling microcracks. Populations of different fluid inclusion types were recognized by room temperature phase relationships, phase transitions during heating and cooling, and laser Raman spectroscopy results. Four types of fluid inclusions were identified using the nomenclature of Ramboz et al. [42], which are CH4-rich (Type Ι), CH4-CO2-H2O (Type ΙΙ), H2O-rich (Type III), and halite-bearing (Type ΙV) types.Type Ι inclusions consist of liquid water and CH4 at room temperature, with a degree of fill ranging from 0.2 to ~0.6 (Figure 5(a)). These inclusions are common in A veins (Stage 1) and occur as bands or clusters or in isolation. They have irregular or negative crystal shapes and are typically 10 to 30 μm in size.Figure 5
Photomicrographs of fluid inclusions in Stages 1–3 quartz and fluorite in the Bairendaba Ag-Zn-Pb deposit. ((a), (b), (c)) Type Ι, Type III, and Type ΙV inclusions in Stage 1 quartz. ((d), (e)) Type ΙΙ and Type III inclusions in Stage2-1 quartz. ((f), (g)) Type ΙΙ and Type III inclusions in Stage 2-1 quartz. ((h), (i)) Type III inclusions in Stage 3 fluorite. L (liquid phase), V (vapor phase), and S (halite crystal).Type ΙΙ inclusions appear similar to Type I at room temperature (Figures5(d)–5(f)). However, the addition of a CO2 component to CH4 in Type ΙΙ inclusions is evident during freezing and laser Raman microprobe measurements. These inclusions are absent from A veins and can occur in isolation but are more common as clusters and trails in B and C veins (Stage 2). They have regular shapes (e.g., ellipsoidal or negative crystal) and are 10 to 30 μm in size.Type III fluid inclusions are liquid water dominant and have vapor contents of 10% to ~45% and variable shapes (e.g., irregular and ellipsoidal), ranging in size from 5 to 20μm (Figures 5(c), 5(g)–5(i)). These inclusions are present in all stages of mineralization and commonly occur as planar arrays restricted to the interiors of quartz and fluorite grains. However, some Type III inclusions fill microfractures in Stages 1-2 quartz and Stage 3 fluorite, indicating a secondary origin (Figures 5(c) and 5(i)).Type ΙV fluid inclusions contain three phases at room temperature, which are a vapor bubble, liquid water, and halite cube (Figure5(b)). Halite-bearing inclusions are uncommon and coexist with Types I and III in A veins of Stage 1 mineralization. Type ΙV inclusions are always <20 μm in size and occur in isolation or discrete clusters, implying a primary origin [40].


## 4.2. Fluid Inclusion Microthermometry

Primary fluid inclusions larger than 5μm with a regular crystal shape, which show no signs of necking [40], were chosen for microthermometric analyses. Data for Stages 1–3 are listed in Table 1. Histograms of homogenization temperatures (Th) and salinity of different types of fluid inclusions in Stages 1-2 quartz and Stage 3 fluorite are presented in Figure 6.Table 1
Microthermometric data for fluid inclusions in hydrothermal quartz and fluorite, Bairendaba Ag-Zn-Pb deposit.
Stage
Host mineral
Inclusion Type
Tm(CO2) (°C)
Th(CO2) (°C)
Tm(clath) (°C)
Tm(ice) (°C)
Tm(NaCl) (°C)
Salinity (NaCl wt.%)
Th (°C)
Stage 1
Quartz
I (65)
−182.1 to −180.2
−99.3 to −68.4
11.2–18.9
NA
NA
NA
267–395
III (39)
NA
NA
NA
−8.1 to −2.5
NA
4.2–11.8
242–351
IV (5)
NA
NA
NA
NA
258–295
35.2–37.8
259–372
Stage2-1
Quartz
II (62)
−79.5 to −59.6
−52.1 to −2.8
7.9–16.8
NA
NA
NA
246–334
III (38)
NA
NA
NA
−6.8 to −1.6
NA
2.7–10.2
205–312
Stage2-2
Quartz
II (65)
−63.4 to −57.7
−6.9 to 10.2
9.5–13.8
NA
NA
NA
173–282
III (44)
NA
NA
NA
−5.9 to −1.2
NA
2.1–9.1
179–269
Stage 3
Fluorite
III (57)
NA
NA
NA
−5.4 to −0.4
NA
0.7–8.4
138–213
Tm(ice), temperature of final ice melting; Tm(NaCl), melting temperature of halite crystals; (65) is the number of inclusions measured.Figure 6
Histograms of microthermometric data for fluid inclusions in hydrothermal quartz and fluorite of the Bairendaba Ag-Zn-Pb deposit. (a) Homogenization temperatures for Types Ι, III, and ΙV; Stage 1 quartz. (b) Salinity for Types III and ΙV; Stage 1 quartz. (c) Homogenization temperatures for Types ΙΙ and III; Stage2-1 quartz. (d) Salinity for Type III; Stage 2-1 quartz. (e) Homogenization temperatures for Types ΙΙ and III; Stage 2-2 quartz. (f) Salinity for Type III; Stage 2-2 quartz. (g) Homogenization temperatures for Type III; Stage 3 fluorite. (h) Salinity for Type III; Stage 3 fluorite.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)Stage 1 quartz veins contain abundant Type I and III fluid inclusions, but rare Type IV inclusions. Type I inclusions freeze below –185°C and melting of the carbonic phase (TmCO2) occurs at –182.1° to –180.2°C (Table 1). This behavior indicates the vapor phase is nearly pure CH4. Homogenization of the carbonic phase (ThCO2) to vapor occurs at –99.3° to –68.4°C, and clathrate melting (TmClath) between 11.2° and 18.9°C (Table 1) is much higher than the invariant point (e.g., 10°C) of a pure CO2 clathrate [41]. Type Ι inclusions with a high degree of fill decrepitate at ~350°C, prior to final homogenization, probably due to increased internal pressures of CH4 [40]. In contrast, Type Ι inclusions with a low degree of fill have Th of 267°–395°C (Figure 6(a)). Type III inclusions homogenize to the liquid phase at 242°–351°C (Figure 6(a)) and final ice melting at –8.1° to –2.5°C indicates salinities of 4.2–11.8 wt.% NaCl equivalent (Figure 6(b)). Halite crystals in Type ΙV inclusions dissolve at 258°–295°C, indicating salinities of 35.2–37.8 wt.% NaCl equivalent, and they have final homogenization to the liquid phase at 259°–372°C (Figures 6(a) and 6(b)).Stage2-1 and 2-2 quartz veins contain Type ΙΙ and III fluid inclusions. Fluid inclusion data for Stage 2-1 are presented first. Type ΙΙ inclusions freeze below –130°C and TmCO2 occurs between –79.5° and –59.6°C (Table 1), significantly lower than melting of pure CO2 at –56.6°C. This indicates the carbonic phase, which is mostly CH4, also contains CO2 and/or N2 [42]. Homogenization of the carbonic phase to vapor occurs between –52.1° and 2.8°C and TmClath at 7.9° to 16.8°C (Table 2). Final homogenization to the liquid phase could only be determined for fluid inclusions with a low degree of fill and Th which are 246°–334°C (Figure 6(c)). Type III inclusions homogenize to the liquid phase at 205–312°C and final ice melting at –6.8° to –1.6°C indicates salinities of 2.7–10.2 wt.% NaCl equivalent (Figures 6(c) and 6(d)).Table 2
Oxygen, hydrogen, and carbon isotope data for hydrothermal quartz of Stages1-2, Bairendaba Ag–Zn–Pb deposit.
Vein type
Stages
Sample description
δ
18
O
V
-
S
M
O
W/%
δ
D
V
-
S
M
O
W/%
Th (°C)
δ
18
O
H
2
O
-
S
M
O
W/%
δ
C
V
-
P
D
B/%
A veins
1
Quartz
14.1
−113.4
320
7.9
−13.2
A veins
1
Quartz
14.2
−114.2
280
6.6
−12.8
A veins
1
Quartz
14.0
−114
320
7.8
−13.1
A veins
1
Quartz
14.1
−114.6
280
6.5
−12.9
B veins
2-1
Quartz
14.0
−116.2
300
7.1
−12.9
B veins
2-1
Quartz
13.9
−116.3
260
5.4
−15.8
B veins
2-1
Quartz
13.3
−116.7
300
6.4
−12.8
B veins
2-1
Quartz
13.2
−116.5
260
4.7
−15.7
C veins
2-2
Quartz
13.7
−117.4
240
4.3
−15.9
C veins
2-2
Quartz
13.6
−117.6
200
1.9
−12.1
C veins
2-2
Quartz
13.7
−124.4
240
4.3
−15.9
C veins
2-2
Quartz
13.5
−124.6
200
1.8
−12.0Fluid inclusion Types ΙΙ and III, representing Stage2-2, have lower Th and are less saline than Stage 2-1 (Figures 6(c)–6(f)). Type ΙΙ inclusions freeze below –100°C and TmCO2 occurs at –63.4° to –57.7°C (Table 2). This behavior is consistent with the presence of small concentrations of CH4 and/or N2 in addition to CO2 [44–46]. Homogenization of the carbonic phase to vapor occurs at –6.9° to 10.2°C and TmClath between 9.5° and 13.8°C (Table 2). Final homogenization to the liquid phase could only be determined for inclusions with a low degree of fill and occurs at 173°–282°C (Figure 6(e)). Type III inclusions homogenize to the liquid phase at 179°–269°C and final ice melting at –5.9° to –1.2°C indicates salinities of 2.1–9.1 wt.% NaCl equivalent (Figures 6(e) and 6(f)).Fluorite veins representing Stage 3 contain only Type III fluid inclusions that record the lowest Th and salinities for the Bairendaba deposit (Figures6(a)–6(h)). Homogenization to the liquid phase occurs at 138°–213°C and final ice melting at –5.4° to –0.4°C indicates salinities of 0.7–8.4 wt.% NaCl equivalent (Figures 6(g) and 6(h)).


## 4.3. Laser Raman Microprobe Analysis

The data obtained by laser Raman microprobe analyses of fluid inclusions in Stages1-2 quartz and Stage 3 fluorite are presented in Figure 7. Type Ι inclusions for Stage 1 contain a vapor phase dominated by CH4 (Figures 7(a) and 7(b)), whereas Type ΙΙ inclusions for Stage 2 contain different amounts of CH4 and CO2 (Figures 7(c)–7(e)). No pure CO2 inclusions were identified in this study. The vapor phase of Type III inclusions consists solely of water (Figure 7(f)).Figure 7
Laser Raman microspectrometry of primary fluid inclusions in hydrothermal quartz and fluorite of the Bairendaba Ag-Zn-Pb deposit. ((a), (b)) Type Ι inclusions in Stage 1 quartz. ((c), (d)) Type ΙΙ inclusions in Stage2-1 quartz. (e) Type ΙΙ inclusions in Stage 2-2 quartz. (f) Type III inclusions in Stage 3 fluorite.
(a)
(b)
(c)
(d)
(e)
(f)


## 4.4. Oxygen, Hydrogen, and Carbon Isotopes

Isotope data for 12 quartz samples representing A-C veins in the Bairendaba deposit are reported asδ18OV-SMOW, δDV-SMOW, and δ13CPDB values. Ranges in the data are limited and are as follows: 13.2‰ to 14.2‰ (δ18OV-SMOW); –124.6‰ to –113.4‰ (δDV-SMOW); –15.9‰ to –12.0‰ (δ13CPDB; Table 2). Values of 1.8‰ to 7.9‰ (δ18OH2O-SMOW; Table 2) were calculated using the formula of Clayton et al. [59] and Th of fluid inclusions. These δD and δ18O values are consistent with previously published data [17, 33, 47, 60]. The C isotope data in this study are unique, because this is the first time C isotopes were measured for the gas phase of fluid inclusions in hydrothermal quartz representing Stages 1-2 of the Bairendaba deposit. Previous work by Ouyang [33] generated data strictly for Stage 3 fluorite-calcite veins.


## 4.5. Sulfur Isotopes

Sulfur isotope analyses were completed for mineral separates of pyrite, pyrrhotite, galena, and sphalerite extracted from ore veins. All data are reported asδ34V-CDT values. Sulfide minerals from the number 1 orebody of the Bairendaba Ag-Zn-Pb deposit have a limited range of –0.1‰ to 1.5‰ (Table 3), which are consistent with previously published data [17, 33, 47].Table 3
Sulfur isotope data for ore minerals of the Bairendaba Ag-Zn-Pb deposit.
Sample
Mineral
δ
34
S
C
D
T/‰
Sample location
BR1-1
Pyrite
0.2
Number 1 orebody at 1275 m level
BR1-2
Pyrite
−0.1
Number1 orebody at 1145 m level
BR2-1
Pyrrhotite
1.5
Number 1 orebody at 1275 m level
BR2-2
Pyrrhotite
1.4
Number 1 orebody at 1145 m level
BR3
Sphalerite
0.5
Number 1 orebody at 1270 m level
BR4
Sphalerite
0.9
Number 1 orebody at 1142 m level
BR5
Galena
0.5
Number 1 orebody at 1270 m level
BR6
Galena
0.5
Number 1 orebody at 1142 m level


## 5. Discussion

### 5.1. Sources of Ore-Forming Materials

Sulfur isotopes are an important tool for determining the source(s) of ore-forming materials in deposits [57, 61–63]. The Bairendaba Ag-Zn-Pb deposit has δ34S values of –4.0‰ to 1.7‰ with an average of –1.0‰ (Figure 8). These data show a normal distribution (Figure 8) and are similar to δ34S values of –3‰ to 1‰ reported for magmatic-hydrothermal deposits [57, 63, 64]. Therefore, we propose a magmatic source for sulfur, with minor crustal contamination.Figure 8
Histogram of S isotope data, Bairendaba Ag-Zn-Pb deposit. The published S isotope data are from Ouyang [33], Jiang et al. [17], and Mei et al. [47].Lead (Pb) isotopes provide additional information to constrain the source(s) of ore-forming materials in deposits [65, 66]. A compilation of data for sulfide minerals from the Bairendaba Ag-Zn-Pb deposit shows values of 18.3–18.5 (206Pb/204Pb), 15.5–15.7 (207Pb/204Pb), and 38.1–38.6 (208Pb/204Pb) [17, 33] that are richer in uranogenic Pb but poorer in thorogenic Pb. The majority of Pb isotope data for the ore sulfides cluster between the orogenic and mantle growth curves on an uranogenic plot, with a small population above the orogenic growth curve (Figure 9(a)). A thorogenic plot shows Pb isotope data for the ore sulfides are close to the orogenic growth line (Figure 9(b)). We interpret these data to reflect a hybrid crustal-mantle source of lead.Figure 9
Lead isotope compositions for sulfides and host rocks in the Bairendaba Ag-Zn-Pb deposit. (a)207Pb/204Pb versus 206Pb/204Pb plot; (b) 208Pb/204Pb versus 206Pb/204Pb plot. UC (upper crust), O (orogen), M (mantle), and LC (lower crust). The average growth curve is from Zartman and Doe [48]. Lead isotope data for ore are from Ouyang [33] and from Jiang et al. [17], Chu et al. [49], and Zeng et al. [50] for Permian strata; Jiang et al. [17] for gneiss; and Jiang et al. [17] and Wang [51] for the Beidashan granite.
(a)
(b)Additional Pb isotope data exist for unmineralized rock units in the region [17, 49–51] and allow for a comparison with the Bairendaba deposit. These data plot over a broader range than the ore sulfides from the Bairendaba deposit (Figures 9(a) and 9(b)). Generally, if Pb from different geological units is derived from the same source, the Pb isotope compositions and variation trends should be similar. The Pb isotope composition of the Bairendaba ores is clearly different from that of gneiss and partially overlaps with the Beidashan granite and Permian strata. The Pb isotope composition of the Bairendaba ores shows a linear correlation with, and similar minimum values to, the Beidashan granite, which indicates they may have a common origin. The range in Pb isotope data may result from later contamination.Given the similar ages of the 139–140 Ma Beidashan granite [30] and the 133 ± 2 Ma mineralization at the Bairendaba deposit [14], we propose the Beidashan granite was a source of heat and ore-forming materials for the deposit. Sulfur isotope data support this view, but Pb isotopes suggest a hybrid crustal-mantle source. Previous studies documented that more than 60% of polymetallic deposits occur in Permian strata of the SGXR [67]. Geochemical analyses of unaltered Permian strata [43, 68] indicate high concentrations of ore-forming materials including Ag, As, Sn, Pb, and Zn (Table 4). Therefore, ore-forming materials in the Bairendaba deposit were derived from both the Beidashan granite and Permian strata.Table 4
Element abundance in lithologies of Permian strata, SGXR [43].
Element content
Sandstone (ppm)
Slate (ppm)
Arkose (ppm)
Tuff (ppm)
Clarke (ppm)
Mn
933.16
972.24
825.08
957.55
950.00
V
96.85
96.07
69.42
121.00
135.00
Ti
4241.18
4457.84
3457.62
4464.76
5700.00
Cu
43.41
52.12
40.50
44.60
55.00
Pb
15.35
14.87
69.88
11.80
12.60
Zn
81.27
84.17
76.73
81.46
70.00
As
9.61
11.61
9.46
10.94
1.80
Sn
5.18
6.38
5.48
3.23
2.00
Ag
0.18
0.17
0.15
0.17
0.07
Mo
1.42
1.19
1.25
1.19
1.50
Ni
23.60
24.27
14.61
15.35
75.00


### 5.2. Fluid Sources and Evolution of the Hydrothermal System

Fluid inclusion microthermometric data and the different types of inclusions in Stages1-2 quartz and Stage 3 fluorite at the Bairendaba Ag-Zn-Pb deposit highlight distinct changes in the hydrothermal system with time. Histograms show a sharp decrease in temperature and salinity from Stages 1 to 3 (Figure 6). Fluid inclusion types also record a progressive change from a saline CH4-rich system to a mixed CH4 + CO2 system and late low-salinity water-dominant system.The presence of CH4 in fluid inclusions of Stages 1-2 at the Bairendaba deposit requires further discussion. Mineralizing fluids for other deposits in the SGXR, including the Weilasituo deposit that occurs 4 km to the west of Bairendaba, also contain CH4 [69]. Previous studies have proposed that CH4 originated from a deep source of reduced magma. Fluids exsolved from a reduced melt would be enriched in CH4 and not CO2 [70–75]. However, cross-cutting relationships indicate dolerite dykes, derived from a deep source, predate the mineralization [14]. The metamorphism of organic-rich formations could also be a source of CH4 [41, 76]. As the Permian strata are carbon-rich [21], metamorphism caused by late magmatic activity could have produced CH4 in mineralizing fluids.Carbon isotope data for quartz and calcite provide additional clues to the source of CH4 in ore-forming fluids. Hydrothermal quartz analyzed in this study has a broader range of δ13CPDB values (−15.9‰ to −12‰) than calcite (−13.5‰ to −12.8‰) [33]. Although quartz and calcite represent different stages of mineralization at the Bairendaba Ag-Zn-Pb deposit, most samples plot within the field of organically derived carbon on a δ13CPDB versus δ18OSMOW diagram (Figure 10). Therefore, we propose that metamorphism of carbon-rich Permian strata was the source of CH4 in the ore-forming fluids.Figure 10
δ
13C versus δ18O diagram showing the distribution of carbon and oxygen isotope data for the Bairendaba Ag-Zn-Pb deposit relative to fields for marine and magmatic carbonates [52] and organically derived carbon [53]. The data for calcite are from Ouyang [33].A potentially important point to consider is why fluids in Stage 1 are CH4-rich, whereas CO2 increases and CH4 decreases in Stage 2. Rios et al. [77] documented that fluid inclusions in ore-bearing quartz veins at a shallow level in the Pedra Preta wolframite deposit, southern Pará, are rich in CH4 compared with deep samples containing high levels of CO2, but minor CH4. This distribution of different fluid-inclusion types was attributed to the deep Musa intrusion and the oxidation of CH4 to CO2 following the reaction: CH4(g) + 2O2(g) = CO2(g) + H2O(g). This reaction confirms how an increase in fO2 of a hydrothermal system could change a reduced CH4-rich fluid into an oxidized fluid containing CO2. However, a change in fO2 could also result from the addition of oxidized meteoric water to the hydrothermal system during mineralization.The possibility of having fluids, with different origins, in the hydrothermal system that formed the Bairendaba deposit is addressed using H and O isotope data. Ranges in values ofδD and calculated δ18OH2O (Table 2) for hydrothermal quartz, calcite, and fluorite suggest multiple sources of oxygen. Values of δD for Stage 1 quartz are lighter than those for magmatic water (−50‰ to −80‰) [64] and when paired with calculated δ18OH2O values, they plot under the magmatic water box on a δD versus δ18OH2O diagram (Figure 11). Data for Stage 2-1 and Stage 2-2 quartz show a slight shift towards the meteoric water line. In contrast, O-H isotope data for paragenetically younger calcite and fluorite define a trend towards the meteoric water line (Figure 11). The differences in these data could reflect magma degassing, fluid mixing, and/or water-rock interaction.Figure 11
δD versus δ18O diagram for quartz, calcite, and fluorite representing different stages of mineralization at the Bairendaba Ag-Zn-Pb deposit. The data of calcite and fluorite are from Ouyang [33]. Trend lines included for reference are based on data from the Gulf Coast, Illinois, and Michigan basins [54]; Alberta Basin [55]; and California Tertiary geothermal brines [56]. Fields for metamorphic and primary magmatic waters are from Taylor Jr.  [57]. Data used to derive a present-day meteoric water line for China are from Chen and Wang [58].Magma degassing can produce significant ranges inδD and δ34S through fractionation [78]. Different degrees of degassing, in an open system, could cause δD for ore-forming fluids derived from magmatic water to be depleted by 50%–80% [79]. Fractionation of sulfur through magma degassing will also lead to a significant decrease in δ34S for different sulfide minerals [80]. However, δ34S data for the Bairendaba deposit have a limited range and this indicates fractionation did not occur and produce the observed δD depletion.The mixing of meteoric water with magmatically derived ore fluids will cause a decrease inδD, as indicated by isotope data for Stages 1–3 at the Bairendaba deposit. Values of δD ranging from −75‰ to −132‰ [33] are intermediate between the δD of magmatic water (−50‰ to −80‰) [64] and local Mesozoic meteoric water in the SGXR (−149‰) [25]. Therefore, fluid mixing could account for the δD depletion.Another possibility involves fluid interaction with common rock-forming minerals such as biotite and hornblende, which can haveδD of −170‰ [81]. Water-rock interaction will lead to isotopic exchange and result in a decrease of δD for the evolved fluid [57, 82].At the Bairendaba deposit, water-rock interaction is suggested by the limited range ofδ18OH2O values and CH4-rich fluid in Stage 1. An evolved meteoric water entering the hydrothermal system during Stages 2-3 could explain δ18O values that trend towards the meteoric water line. Fluid inclusion data recording a decrease in CH4 content, Th, and salinity from Stages 1-3 support the addition of meteoric water to the hydrothermal system with time. Therefore, we conclude the ore fluid was derived from a magmatic source that interacted with crustal rocks and mixed with meteoric water, which became more pronounced in the hydrothermal system during Stage 3.


### 5.3. Genesis of the Bairendaba Ag-Zn-Pb Deposit

Fluid inclusion and stable isotope data need to be interpreted in context with geologic relationships, at both a regional and deposit scale, to develop a coherent genetic model. The Bairendaba Ag-Zn-Pb deposit occurs within a region that underwent compressional tectonism caused by the pre-Mesozoic collision of the Siberian and North China plates  [29, 83]. A structural fabric of NE and EW trending faults formed during this deformational event. By the early Mesozoic period, the closing of Paleo-Asian oceans and final collision between the Siberian Plate and north China resulted in a gradual transition to the Circum-Pacific tectonic domain [84–87].During the Early Cretaceous period, subduction of the Pacific Plate beneath the Eurasian Plate caused large-scale volcanic events across NE China and at the Bairendaba deposit. Zircon U-Pb ages for these intrusions are 119 to ~140 Ma, with a peak at 125−140 Ma [29, 88, 89]. Geochemical characteristics of the intrusive rocks, which are closely related to mineralization in the region, show a uniform isotopic composition of low 87Sr/86Sr(i) and high εNd(t) values [90–92]. This is a result of melting and differentiation of mantle materials and contamination by crustal rocks [90, 93]. The identification of metamorphic core complexes [94], bimodal volcanic rocks [94–97], and widespread anorogenic A-type granites  [93] suggest Early Cretaceous magmatism and related mineralization occurred while the SGXR was undergoing extension [98–102].The timing of mineralization at different ore deposits in the SGXR is documented by Ar-Ar dating of sericite and muscovite, K-Ar dating of sericite, Re-Os dating of molybdenite, and U-Pb dating of hydrothermal zircon [14, 103–105]. These data indicate the interval of 120 to ~135 Ma is an important metallogenic period for the SGXR. Deposits of this age have similar δ18O and δD data that support ore-forming fluids of magmatic origin mixing with meteoric water. Sulfur isotope data for these deposits also indicate a magmatic-hydrothermal origin [1, 4, 106–108]. Although different types of mineralization and alteration are evident in the region, all likely represent a metallogenic event that occurred during an extensional tectonic regime.A geodynamic model involving crustal thinning and magmatism is proposed for mineralization in the region, including the Bairendaba Ag-Zn-Pb deposit. Mineralization coincided with large-scale lithospheric thinning and magmatic underplating during the Early Cretaceous period [29, 109]. Asthenospheric upwelling initiated crustal thinning, reactivated structures, and provided a heat source to circulate fluids on a regional scale. Crust-mantle interaction generated large bodies of silicic magma associated with mineralization. The process of magma emplacement and crystallization evolved fluids rich in volatiles and metals. These fluids caused alteration (e.g., silicification and chloritization), and the convective circulation of groundwater around cooling igneous intrusions leached additional metals from country rocks.Hydrothermal fluids in a relatively closed, reducing environment transported Ag, Zn, and Pb as aqueous Cl– and HS– complexes [81, 110]. Factors causing the deposition of metals from ore-forming fluids in the Bairendaba deposit include a change in temperature, water-rock interaction, and fluid mixing. Fluid inclusions in samples of Stage 1 and Stage 3 mineralization record Th values of 242–395°C and 138–213°C (Table 1), respectively. As the solubility of Cl– and HS– complexes is correlated with temperature, the documented decrease in Th for Stages 1–3 would cause hydrothermal fluids to precipitate metals [111].Water-rock interaction at the Bairendaba deposit is indicated by O-H isotope data (Figure11). Reactions between the wall rocks and hydrothermal fluids would have included the following: PbCln(n-2)-(aq) + HS–(aq) = PbS(galena) + nCl− + H+(aq) and ZnCln(n-2)-(aq) + HS-(aq) = ZnS(sphalerite) + nCl-(aq) + H+(aq) [112]. Metasomatism would have consumed H+ and driven the reaction forward. A corresponding increase in pH would have destabilized metal complexes and caused sulfide minerals to precipitate.The occurrence of fluid mixing at the Bairendaba deposit is supported by the change in fluid inclusion types, Th, and salinities from Stages1-3 (Figures 5 and 6). The initial magmatic fluid in Stage 1 mixed with progressively greater amounts of evolved meteoric water in Stages 2-3. The mixing of fluids with different sources in the hydrothermal system would have occurred according to the following reactions: PbCln(n-2)-(aq) + 2H2S(g) + 1/2O2(g) = PbS2 + 2H+(aq) + H2O(l) + nCl–(aq) and ZnCln(n-2)-(aq) + 2H2S(g) + 1/2O2(g) = ZnS2 + 2H+(aq) + H2O(l) + nCl–(aq) [113]. A decrease in H+ and Cl− concentrations of the hydrothermal fluid due to mixing would drive the reactions forward and increase fO2 of a hydrothermal system, leading to the precipitation of sulfide minerals. These processes of ore deposition were common in the SGXR, where sulfide minerals precipitated within extensional structures produced by regional tectonic processes, forming large deposits.


## 5.1. Sources of Ore-Forming Materials

Sulfur isotopes are an important tool for determining the source(s) of ore-forming materials in deposits [57, 61–63]. The Bairendaba Ag-Zn-Pb deposit has δ34S values of –4.0‰ to 1.7‰ with an average of –1.0‰ (Figure 8). These data show a normal distribution (Figure 8) and are similar to δ34S values of –3‰ to 1‰ reported for magmatic-hydrothermal deposits [57, 63, 64]. Therefore, we propose a magmatic source for sulfur, with minor crustal contamination.Figure 8
Histogram of S isotope data, Bairendaba Ag-Zn-Pb deposit. The published S isotope data are from Ouyang [33], Jiang et al. [17], and Mei et al. [47].Lead (Pb) isotopes provide additional information to constrain the source(s) of ore-forming materials in deposits [65, 66]. A compilation of data for sulfide minerals from the Bairendaba Ag-Zn-Pb deposit shows values of 18.3–18.5 (206Pb/204Pb), 15.5–15.7 (207Pb/204Pb), and 38.1–38.6 (208Pb/204Pb) [17, 33] that are richer in uranogenic Pb but poorer in thorogenic Pb. The majority of Pb isotope data for the ore sulfides cluster between the orogenic and mantle growth curves on an uranogenic plot, with a small population above the orogenic growth curve (Figure 9(a)). A thorogenic plot shows Pb isotope data for the ore sulfides are close to the orogenic growth line (Figure 9(b)). We interpret these data to reflect a hybrid crustal-mantle source of lead.Figure 9
Lead isotope compositions for sulfides and host rocks in the Bairendaba Ag-Zn-Pb deposit. (a)207Pb/204Pb versus 206Pb/204Pb plot; (b) 208Pb/204Pb versus 206Pb/204Pb plot. UC (upper crust), O (orogen), M (mantle), and LC (lower crust). The average growth curve is from Zartman and Doe [48]. Lead isotope data for ore are from Ouyang [33] and from Jiang et al. [17], Chu et al. [49], and Zeng et al. [50] for Permian strata; Jiang et al. [17] for gneiss; and Jiang et al. [17] and Wang [51] for the Beidashan granite.
(a)
(b)Additional Pb isotope data exist for unmineralized rock units in the region [17, 49–51] and allow for a comparison with the Bairendaba deposit. These data plot over a broader range than the ore sulfides from the Bairendaba deposit (Figures 9(a) and 9(b)). Generally, if Pb from different geological units is derived from the same source, the Pb isotope compositions and variation trends should be similar. The Pb isotope composition of the Bairendaba ores is clearly different from that of gneiss and partially overlaps with the Beidashan granite and Permian strata. The Pb isotope composition of the Bairendaba ores shows a linear correlation with, and similar minimum values to, the Beidashan granite, which indicates they may have a common origin. The range in Pb isotope data may result from later contamination.Given the similar ages of the 139–140 Ma Beidashan granite [30] and the 133 ± 2 Ma mineralization at the Bairendaba deposit [14], we propose the Beidashan granite was a source of heat and ore-forming materials for the deposit. Sulfur isotope data support this view, but Pb isotopes suggest a hybrid crustal-mantle source. Previous studies documented that more than 60% of polymetallic deposits occur in Permian strata of the SGXR [67]. Geochemical analyses of unaltered Permian strata [43, 68] indicate high concentrations of ore-forming materials including Ag, As, Sn, Pb, and Zn (Table 4). Therefore, ore-forming materials in the Bairendaba deposit were derived from both the Beidashan granite and Permian strata.Table 4
Element abundance in lithologies of Permian strata, SGXR [43].
Element content
Sandstone (ppm)
Slate (ppm)
Arkose (ppm)
Tuff (ppm)
Clarke (ppm)
Mn
933.16
972.24
825.08
957.55
950.00
V
96.85
96.07
69.42
121.00
135.00
Ti
4241.18
4457.84
3457.62
4464.76
5700.00
Cu
43.41
52.12
40.50
44.60
55.00
Pb
15.35
14.87
69.88
11.80
12.60
Zn
81.27
84.17
76.73
81.46
70.00
As
9.61
11.61
9.46
10.94
1.80
Sn
5.18
6.38
5.48
3.23
2.00
Ag
0.18
0.17
0.15
0.17
0.07
Mo
1.42
1.19
1.25
1.19
1.50
Ni
23.60
24.27
14.61
15.35
75.00


## 5.2. Fluid Sources and Evolution of the Hydrothermal System

Fluid inclusion microthermometric data and the different types of inclusions in Stages1-2 quartz and Stage 3 fluorite at the Bairendaba Ag-Zn-Pb deposit highlight distinct changes in the hydrothermal system with time. Histograms show a sharp decrease in temperature and salinity from Stages 1 to 3 (Figure 6). Fluid inclusion types also record a progressive change from a saline CH4-rich system to a mixed CH4 + CO2 system and late low-salinity water-dominant system.The presence of CH4 in fluid inclusions of Stages 1-2 at the Bairendaba deposit requires further discussion. Mineralizing fluids for other deposits in the SGXR, including the Weilasituo deposit that occurs 4 km to the west of Bairendaba, also contain CH4 [69]. Previous studies have proposed that CH4 originated from a deep source of reduced magma. Fluids exsolved from a reduced melt would be enriched in CH4 and not CO2 [70–75]. However, cross-cutting relationships indicate dolerite dykes, derived from a deep source, predate the mineralization [14]. The metamorphism of organic-rich formations could also be a source of CH4 [41, 76]. As the Permian strata are carbon-rich [21], metamorphism caused by late magmatic activity could have produced CH4 in mineralizing fluids.Carbon isotope data for quartz and calcite provide additional clues to the source of CH4 in ore-forming fluids. Hydrothermal quartz analyzed in this study has a broader range of δ13CPDB values (−15.9‰ to −12‰) than calcite (−13.5‰ to −12.8‰) [33]. Although quartz and calcite represent different stages of mineralization at the Bairendaba Ag-Zn-Pb deposit, most samples plot within the field of organically derived carbon on a δ13CPDB versus δ18OSMOW diagram (Figure 10). Therefore, we propose that metamorphism of carbon-rich Permian strata was the source of CH4 in the ore-forming fluids.Figure 10
δ
13C versus δ18O diagram showing the distribution of carbon and oxygen isotope data for the Bairendaba Ag-Zn-Pb deposit relative to fields for marine and magmatic carbonates [52] and organically derived carbon [53]. The data for calcite are from Ouyang [33].A potentially important point to consider is why fluids in Stage 1 are CH4-rich, whereas CO2 increases and CH4 decreases in Stage 2. Rios et al. [77] documented that fluid inclusions in ore-bearing quartz veins at a shallow level in the Pedra Preta wolframite deposit, southern Pará, are rich in CH4 compared with deep samples containing high levels of CO2, but minor CH4. This distribution of different fluid-inclusion types was attributed to the deep Musa intrusion and the oxidation of CH4 to CO2 following the reaction: CH4(g) + 2O2(g) = CO2(g) + H2O(g). This reaction confirms how an increase in fO2 of a hydrothermal system could change a reduced CH4-rich fluid into an oxidized fluid containing CO2. However, a change in fO2 could also result from the addition of oxidized meteoric water to the hydrothermal system during mineralization.The possibility of having fluids, with different origins, in the hydrothermal system that formed the Bairendaba deposit is addressed using H and O isotope data. Ranges in values ofδD and calculated δ18OH2O (Table 2) for hydrothermal quartz, calcite, and fluorite suggest multiple sources of oxygen. Values of δD for Stage 1 quartz are lighter than those for magmatic water (−50‰ to −80‰) [64] and when paired with calculated δ18OH2O values, they plot under the magmatic water box on a δD versus δ18OH2O diagram (Figure 11). Data for Stage 2-1 and Stage 2-2 quartz show a slight shift towards the meteoric water line. In contrast, O-H isotope data for paragenetically younger calcite and fluorite define a trend towards the meteoric water line (Figure 11). The differences in these data could reflect magma degassing, fluid mixing, and/or water-rock interaction.Figure 11
δD versus δ18O diagram for quartz, calcite, and fluorite representing different stages of mineralization at the Bairendaba Ag-Zn-Pb deposit. The data of calcite and fluorite are from Ouyang [33]. Trend lines included for reference are based on data from the Gulf Coast, Illinois, and Michigan basins [54]; Alberta Basin [55]; and California Tertiary geothermal brines [56]. Fields for metamorphic and primary magmatic waters are from Taylor Jr.  [57]. Data used to derive a present-day meteoric water line for China are from Chen and Wang [58].Magma degassing can produce significant ranges inδD and δ34S through fractionation [78]. Different degrees of degassing, in an open system, could cause δD for ore-forming fluids derived from magmatic water to be depleted by 50%–80% [79]. Fractionation of sulfur through magma degassing will also lead to a significant decrease in δ34S for different sulfide minerals [80]. However, δ34S data for the Bairendaba deposit have a limited range and this indicates fractionation did not occur and produce the observed δD depletion.The mixing of meteoric water with magmatically derived ore fluids will cause a decrease inδD, as indicated by isotope data for Stages 1–3 at the Bairendaba deposit. Values of δD ranging from −75‰ to −132‰ [33] are intermediate between the δD of magmatic water (−50‰ to −80‰) [64] and local Mesozoic meteoric water in the SGXR (−149‰) [25]. Therefore, fluid mixing could account for the δD depletion.Another possibility involves fluid interaction with common rock-forming minerals such as biotite and hornblende, which can haveδD of −170‰ [81]. Water-rock interaction will lead to isotopic exchange and result in a decrease of δD for the evolved fluid [57, 82].At the Bairendaba deposit, water-rock interaction is suggested by the limited range ofδ18OH2O values and CH4-rich fluid in Stage 1. An evolved meteoric water entering the hydrothermal system during Stages 2-3 could explain δ18O values that trend towards the meteoric water line. Fluid inclusion data recording a decrease in CH4 content, Th, and salinity from Stages 1-3 support the addition of meteoric water to the hydrothermal system with time. Therefore, we conclude the ore fluid was derived from a magmatic source that interacted with crustal rocks and mixed with meteoric water, which became more pronounced in the hydrothermal system during Stage 3.


## 5.3. Genesis of the Bairendaba Ag-Zn-Pb Deposit

Fluid inclusion and stable isotope data need to be interpreted in context with geologic relationships, at both a regional and deposit scale, to develop a coherent genetic model. The Bairendaba Ag-Zn-Pb deposit occurs within a region that underwent compressional tectonism caused by the pre-Mesozoic collision of the Siberian and North China plates  [29, 83]. A structural fabric of NE and EW trending faults formed during this deformational event. By the early Mesozoic period, the closing of Paleo-Asian oceans and final collision between the Siberian Plate and north China resulted in a gradual transition to the Circum-Pacific tectonic domain [84–87].During the Early Cretaceous period, subduction of the Pacific Plate beneath the Eurasian Plate caused large-scale volcanic events across NE China and at the Bairendaba deposit. Zircon U-Pb ages for these intrusions are 119 to ~140 Ma, with a peak at 125−140 Ma [29, 88, 89]. Geochemical characteristics of the intrusive rocks, which are closely related to mineralization in the region, show a uniform isotopic composition of low 87Sr/86Sr(i) and high εNd(t) values [90–92]. This is a result of melting and differentiation of mantle materials and contamination by crustal rocks [90, 93]. The identification of metamorphic core complexes [94], bimodal volcanic rocks [94–97], and widespread anorogenic A-type granites  [93] suggest Early Cretaceous magmatism and related mineralization occurred while the SGXR was undergoing extension [98–102].The timing of mineralization at different ore deposits in the SGXR is documented by Ar-Ar dating of sericite and muscovite, K-Ar dating of sericite, Re-Os dating of molybdenite, and U-Pb dating of hydrothermal zircon [14, 103–105]. These data indicate the interval of 120 to ~135 Ma is an important metallogenic period for the SGXR. Deposits of this age have similar δ18O and δD data that support ore-forming fluids of magmatic origin mixing with meteoric water. Sulfur isotope data for these deposits also indicate a magmatic-hydrothermal origin [1, 4, 106–108]. Although different types of mineralization and alteration are evident in the region, all likely represent a metallogenic event that occurred during an extensional tectonic regime.A geodynamic model involving crustal thinning and magmatism is proposed for mineralization in the region, including the Bairendaba Ag-Zn-Pb deposit. Mineralization coincided with large-scale lithospheric thinning and magmatic underplating during the Early Cretaceous period [29, 109]. Asthenospheric upwelling initiated crustal thinning, reactivated structures, and provided a heat source to circulate fluids on a regional scale. Crust-mantle interaction generated large bodies of silicic magma associated with mineralization. The process of magma emplacement and crystallization evolved fluids rich in volatiles and metals. These fluids caused alteration (e.g., silicification and chloritization), and the convective circulation of groundwater around cooling igneous intrusions leached additional metals from country rocks.Hydrothermal fluids in a relatively closed, reducing environment transported Ag, Zn, and Pb as aqueous Cl– and HS– complexes [81, 110]. Factors causing the deposition of metals from ore-forming fluids in the Bairendaba deposit include a change in temperature, water-rock interaction, and fluid mixing. Fluid inclusions in samples of Stage 1 and Stage 3 mineralization record Th values of 242–395°C and 138–213°C (Table 1), respectively. As the solubility of Cl– and HS– complexes is correlated with temperature, the documented decrease in Th for Stages 1–3 would cause hydrothermal fluids to precipitate metals [111].Water-rock interaction at the Bairendaba deposit is indicated by O-H isotope data (Figure11). Reactions between the wall rocks and hydrothermal fluids would have included the following: PbCln(n-2)-(aq) + HS–(aq) = PbS(galena) + nCl− + H+(aq) and ZnCln(n-2)-(aq) + HS-(aq) = ZnS(sphalerite) + nCl-(aq) + H+(aq) [112]. Metasomatism would have consumed H+ and driven the reaction forward. A corresponding increase in pH would have destabilized metal complexes and caused sulfide minerals to precipitate.The occurrence of fluid mixing at the Bairendaba deposit is supported by the change in fluid inclusion types, Th, and salinities from Stages1-3 (Figures 5 and 6). The initial magmatic fluid in Stage 1 mixed with progressively greater amounts of evolved meteoric water in Stages 2-3. The mixing of fluids with different sources in the hydrothermal system would have occurred according to the following reactions: PbCln(n-2)-(aq) + 2H2S(g) + 1/2O2(g) = PbS2 + 2H+(aq) + H2O(l) + nCl–(aq) and ZnCln(n-2)-(aq) + 2H2S(g) + 1/2O2(g) = ZnS2 + 2H+(aq) + H2O(l) + nCl–(aq) [113]. A decrease in H+ and Cl− concentrations of the hydrothermal fluid due to mixing would drive the reactions forward and increase fO2 of a hydrothermal system, leading to the precipitation of sulfide minerals. These processes of ore deposition were common in the SGXR, where sulfide minerals precipitated within extensional structures produced by regional tectonic processes, forming large deposits.


## 6. Conclusions

Distinct populations of fluid inclusions in Stage 1–3 quartz and fluorite at the Bairendaba deposit record a progressive change from a saline CH4-rich system to a mixed CH4 + CO2 system and a late-stage system dominated by low-salinity water. The decrease in fluid salinity was accompanied by a decrease in temperature.Ore-forming fluids with a magmatic source interacted with wall rocks and mixed with meteoric water, as evidenced by changes in values forδ18Ofluid and δDfluid. Sulfur isotope data indicate a magmatic source, whereas δ13C values for fluid inclusions in hydrothermal quartz support the derivation of carbon from organic-rich Permian strata.The Bairendaba Ag-Zn-Pb deposit is a typical mesothermal deposit that formed in an extensional environment related to Early Cretaceous subduction of the Pacific Plate.



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*Source: 1206587-2017-07-13.xml*