# Identification of Two Types of Metallogenic Fluids in the Ultra-Large Huize Pb–Zn Deposit, SW China

Authors: Yan Zhang; Runsheng Han; Pingtang Wei; Lei Wang
Journal: Geofluids
 (2017)

---

## Abstract

This work investigates the ultra-large Huize Pb–Zn deposit, based on the results of preceding studies and detailed field geological surveys. The existing findings were reorganized and reinterpreted and supplemented with C–H–O isotopic measurements, which resulted in the identification of two different metallogenic fluids: a high temperature, low salinity, and acidic Fluid A, which originates from deep-seated fluids and is enriched in lighter C and O isotopes (−3‰ < δ13C‰ < −4‰; 10‰ < δ18O‰ < 17‰; −92‰ < δD‰ < −50‰), and a low temperature, high salinity Fluid B, which is a subsurface brine formed by atmospheric precipitation. Fluid B is characterized by heavier C–O–H isotopic compositions (−2‰ < δ13C‰ < 1‰; 2‰ < δ18O‰ < 24‰; −66‰ < δD‰ < −43‰) than Fluid A and cycles continuously within the strata. We hypothesize that the Huize Pb–Zn deposit is the result of large-scale fluid migration from deep regions of the crust. These upward-moving fluids extracted metallic elements from carbonate strata of various ages, forming a metal-rich metallogenic fluid (Fluid A). After higher-grade ores were precipitated from the fluid following decompression boiling, it then mixed with Fluid B and continued to precipitate sulfides.


---

## Body

## 1. Introduction

The Pb–Zn deposits in the Sichuan–Yunnan–Guizhou Pb–Zn polymetallic metallogenic belt (Figure1) are mainly carbonate-type deposits. Hence, carbonate-hosted Pb–Zn deposits are among the most important types of Pb–Zn deposits in the mining industry. Deposits of this type are widely distributed throughout the world and are concentrated in regions such as North America, Europe, and Southeast Asia. Carbonate-hosted Pb–Zn deposits are also the world’s most important source of lead and zinc, as they single-handedly account for 25% of the world’s reserves. These deposits tend to be large in scale, consistent in terms of ore quality, and straightforward to extract and smelt. The germanium-, lead-, and zinc-rich regions of Northeast Yunnan, which lie on the southwestern margin of the Yangtze Plate, are an important component of the Sichuan–Yunnan–Guizhou Pb–Zn polymetallic metallogenic belt, which contains 221 Pb–Zn polymetallic deposits and mineralization points. In particular, the Huize Pb–Zn deposit, which is located on either side of the N–S trending Qujing–Zhaotong concealed fracture zone at the NE end of the Jinniuchang–Kuangshanchang tectonic belt, is one of the richest ultra-large Ge–Pb–Zn enriched deposits in the world [1]. The Huize deposit has a unique metallogenic system that is characterized by large reserves of lead and zinc (over 8 Mt) and high average ore grades (Pb + Zn: 25%–35%, with some exceeding 60%) and is representative of the metallogenic zones in Sichuan, Yunnan, and Guizhou.Figure 1
Tectonic map showing distribution of Zn–Pb–(Ag–Ge) deposits in the Sichuan–Yunnan–Guizhou triangle, SW China (modified after [23]). 1: Emeishan flood basalt; 2: main fault; 3: secondary fault; 4: province boundary; 5: town; 6: river; 7: large deposit; 8: medium deposit; 9: small deposit.This particular deposit has been exhaustively studied by a number of scholars, and a series of important findings have been made in studies on the geological background of the mining areas in Northeast Yunnan [2–4], the geochemistry of the deposit [5–14], the tectonic setting of the ore fields [15–17], and the formation of the deposit [2–8, 15, 16, 18–22], thus providing a wide range of resources for this study to access and build upon. While consensus has been reached on topics such as the tectonic setting of the lead and zinc deposits in the region [11, 23–27] (boundaries of a stable platform), distribution characteristics of the deposits [23, 25, 27–29] (simultaneously controlled by lithological characteristics and tectonic structure), ore host rocks [23, 25, 28] (mainly medium-to-coarse-grained, thick-bedded dolomites), and connection between metallogenesis and large-scale fluid migration [8, 30–32], significant controversies remain regarding the origin and evolution of the metallogenic fluids, which are of great importance for deposit formation models. Liu and Lin [21] believe that the metallogenic fluids are mainly derived from water that cycles through subsurface layers, and the sulfur in the deposits comes from the reduction of marine sulfates, mainly by thermochemical sulfate reduction (TSR) [10]. In contrast, Han et al. [12, 27] believe that the sulfur in the metallogenic fluids mainly originates from carbonate strata, while the fluid itself is derived from mineral-rich metamorphic waters and deep-seated thermal fluids. Analysis of several stable isotopes also revealed that the metallogenic fluids may have different origins [8, 33]. Therefore, the origins of the metallogenic fluids in the Huize deposit remain controversial despite the comprehensive studies that have been performed in this region. It is also possible that the metallogenic fluids have undergone unique evolutionary processes.There are also significant controversies regarding the precipitatory mechanisms of sulfides in the Huize deposit, and the current views on this matter may be categorized into the following three groups. (1) Fluid mixing: based on C–O isotopic analysis, Huang et al. [8, 33–35] believe that the mixing of crust and mantle fluids is the key to metallogenesis; Luo et al. [36] proposed that mixing between fluids is the primary mechanism of precipitation, based on their summation of previous studies on fluid inclusions; Zhang et al. [37–40] believe that the processes of fluid mixing and boiling are the primary causes of sulfide precipitation, based on the results of studies on strontium isotopes and fluid inclusions. (2) Fluid boiling: Han et al. [12, 13, 23] performed a detailed study of the geological characteristics and fluid inclusions and came to the conclusion that fluid boiling is the primary mechanism of mineral enrichment and metallogenesis. (3) pH changes: several authors believe that sulfide precipitation is mainly caused by changes in pH [7, 41, 42]. Based on a review of the literature, we [43] believe that fluid mixing is very likely to be the primary mechanism of precipitation in the Huize Pb–Zn deposit.Nevertheless, some questions remain. For example, are there two different types of metallogenic fluids in the Huize mining region? What are the origins of these fluids, and what are their defining characteristics? These issues have yet to be studied in a thorough and systematic manner. In this work, we reorganized and reinterpreted the results of previous C, H, and O isotopic studies, supplemented these findings with new isotopic evidence from Kuangshanchang (which is comparatively scarce in the literature), and combined these findings with current geological information and previous studies on fluid inclusions, to discuss the origins of two different metallogenic fluids that are present in the Huize deposit, as well as their evolutionary processes. On this basis, we then hypothesized a rational process of metallogenesis for the Huize Pb–Zn deposit.


## 2. Regional Geological Setting

The Huize Pb–Zn mining area is located on the southwestern margin of the Yangtze Plate (Figure1), on the western side of the Yunnan–Guizhou fold and thrust belt, in the Jinniuchang–Kuangshanchang metallogenic belt within the Dongchuan–Zhenxiong tectonic belt, in the southeastern part of the Northeast Yunnan fold-fault system. The mining area is bordered by the Weining–Langdai depressed fold-fault bundle, the major Xiaojiang fracture zone on the eastern margin of the Kangdian Axis, the Niushoushan uplifted fold-fault bundle, and the Liangshan fold-fault bundle to the east, west, south, and north, respectively [44].The regional stratigraphy is composed of Precambrian basement overlain by a sedimentary cover sequence deposited in the Late Sinian, with an angular unconformable contact between these two units. The metamorphic basement is mainly composed of the Mesoproterozoic Hekou and Huili groups, the Neoproterozoic Yanbian and Yanjing groups, and large Neoproterozoic magmatic complexes, as well as their equivalent strata. The sedimentary cover comprises marine sediments composed of strata ranging in age from Sinian to Permian and terrestrial sediments that consist of Mesozoic and Cenozoic strata.The Sichuan–Yunnan–Guizhou Pb–Zn polymetallic metallogenic region is located within the Huili–Kunming rift [45, 46] and is surrounded by deep and large faults that act as boundaries. This region is bordered by the N–S trending Anninghe–Luzhijiang Fault, Kangding–Yiliang–Shuicheng Fault, and Mile–Shizong–Shuicheng Fault to the west, north, and south, respectively [45]. The tectonic structure of this region comprises 15 faults, which may be categorized as near-NS-, NE-, and NW-trending faults (Figure 1). In particular, the N–S trending Xiaojiang Fault and Zhaotong–Qujing concealed fault play a significant role in controlling the magmatic activity in the region, as well as the distribution and development of lead, zinc, and silver deposits [8, 16].Magmatic activity in the Sichuan–Yunnan–Guizhou Pb–Zn polymetallic metallogenic region recurs frequently and persists for long periods of time, and it is known that magma outflows occurred from the Jinning Period until the Yanshan Period. Igneous rocks are distributed widely and inhomogeneously throughout this region. In particular, the Hercynian Emeishan basalts (Figure1) are widely distributed and immensely thick and constitute the well-known Emeishan volcanic province [8].


## 3. Geological Characteristics of the Huize Deposit

The Huize deposit is located on both sides of the near-NS-trending Qujing–Zhaotong concealed fault, at the NE end of the Jinniuchang–Kuangshanchang tectonic belt. It comprises the ultra-large Kuangshanchang and Qilinchang Pb–Zn deposits, the Yinchangpo medium-sized Pb–Zn deposit (Guizhou), and the Longtoushan, Xiaoheiqing, and Lanyinchang Pb–Zn mines (Figure2).Figure 2
Geological sketch map of the Huize Pb–Zn ore deposit (modified after [16]). 1: Permian carbonate rock, Emeishan flood basalt, and shale; 2: Lower Permian Qixia–Maokou Fm. limestone and dolomitic limestones; Liangshan Fm. charcoal, shale, and sandstone; 3: Lower Permian Emeishan flood basalt; 4: Carboniferous: Maping Fm. brecciform limestone; Weining Fm. oolitic limestone; Baizuo Fm. coarse-grained dolostones and dolomitic limestones; Datang Fm. aphanitic limestone and oolitic limestone; 5: Devonian: Zaige Fm. limestone, siliceous dolostone, and dolostone; Haikou Fm. siltstone and shale; 6: Cambrian Qiongzhusi Fm. shale and sandy mudstone; 7: Sinian Dengying Fm. siliceous dolomite; 8: fault; 9: stratigraphic boundary; 10: Pb–Zn deposit.


### 3.1. Stratigraphy

The stratigraphy of the mining region is composed of Early Sinian metamorphic basement and Sinian and Paleozoic sediments. The upper Paleozoic strata are well-developed, while the Qiongzhusi Formation is the only Cambrian outcrop of the lower Paleozoic strata; the Middle and Upper Cambrian, Ordovician, Silurian, and Lower Devonian strata are missing, and outcrops of the Upper Sinian Dengying Formation and Middle-Upper Devonian strata only appear in localized sections. In particular, the Lower Carboniferous Baizuo Formation (C1b) is the main ore-bearing layer.


### 3.2. Tectonic Structure

The faults within the mining region mainly developed in NE, NW, near-NS, NNW, and near-EW orientations. In particular, the NE–SW-trending reverse shear faults are important ore-controlling tectonic structures. The Kuangshanchang, Qilinchang, and Yinchangpo faults form a tectonic structure comprising three imbricated layers, and as the main faults in this region, they control the Kuangshanchang, Qilinchang, and Yinchangpo deposits (Figure2), respectively. These faults are connected by the near-NS-trending Dongtou reverse fault [16].


### 3.3. Characteristics of the Orebodies

#### 3.3.1. Kuangshanchang Deposit

The Kuangshanchang deposit occurs within the area defined by the Kuangshanchang Fault, F5 Fault, and Dongtou Fault (Figure2), with the orebodies mainly occurring within the medium-to-coarse-grained dolomites of the Lower Carboniferous Baizuo Formation (C1b). Within a ~2000 m long section of land, 260 Pb–Zn orebodies of varying sizes can be found. The orebodies usually occur as sheets, lenticels, sacs, lentils, and irregular veins, and these generally propagate along interlayer fractures. Lateral end-to-end alignment of structures and expansion/contraction are usually observed along the strike and dip of the orebodies. The horizontal lengths of the orebodies range from 26 m to 233 m, with an average of 98.17 m. The horizontal widths range from 2 m to 35 m, with an average of 16.65 m, and the depths along dip exceed 1050 m. The Pb grades range from 4.73% to 44.05%, with an average of 20.60%, while the Zn grades range from 3.29% to 46.52%, with an average of 29.74%. As the depth increases, the distribution of ores changes from oxidized ores to mixed ores and finally to sulfide ores.


#### 3.3.2. Qilinchang Deposit

The Qilinchang deposit is located above the Qilinchang Fault and comprises the Qilinchang and Dashuijing mining sections. Currently, more than 70 Pb–Zn orebodies have been discovered in this deposit (with 20 possessing industrial value). The Pb–Zn reserves exceed 2.46 Mt, with an average (Zn + Pb) ore grade of 25%. All of the ores occur within the coarse-grained dolomites and limestones in the middle and upper sections of the Lower Carboniferous Baizuo Formation (C1b). The boundaries between the orebodies and the host rocks are very distinct, and the orebodies are generally formed along interlayer fractures, with some ores produced in certain locations at low angles with respect to the strata. The orebodies have a strike of 20–30° NE and a steep dip of 50–76° SE. They also have a short horizontal length and great depth along dip. In the horizontal plane, the orebodies occur as sheets, stratoids, veins, sacs, flat columns, or stockworks; in the vertical plane, the ores are primarily present as lenticels, with thinning or pinched branches at the top and tail ends.


### 3.4. Ore and Mineral Characteristics

The Huize Pb–Zn deposit mainly contains sulfide and oxide ores. Currently, most of the ores extracted from the deposit are sulfide ores. The mineral composition of the sulfide ores is relatively simple and mainly comprises sphalerite, galena, and pyrite, with sporadic occurrences of chalcopyrite, matildite, and native antimony. The host rocks are mainly calcite and dolomite, followed by quartz, barite, gypsum, and clay-type materials.The main ore structures consist of massive, disseminated, banded, veined, stockwork, miarolitic, and brecciated structures (Figure3). The primary ore textures comprise euhedral-anhedral-grained, metasomatic, edge-shared, void-filling, poikilitic, slaty cleavage, skeletal, exsolution, graphic, crumpled, and cataclastic textures (Figure 4).Figure 3
Typical structure photographs of minerals in the Huize Pb–Zn deposit. (a) Massive ore, miarolitic structure. (b) Dense massive ore, massive structures. (c) Massive ore, massive structures. (d) Massive ore, vein structure. (e) Disseminated ore, disseminated structures. (f) Banded structure. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)Figure 4
Typical texture photographs of minerals in the Huize Pb–Zn deposit. (a) Xenomorphic granular texture of Sp, (−)10 × 10. (b) Hypidiomorphic–xenomorphic granular textures of Sp and Gn, (−)10 × 2. (c) Cataclastic texture of Py, (−)10 × 4. (d) Edge-shared texture between Sp and Gn, (−)10 × 4. (e) Skeleton crystal structure of Gn replacing Py, (−)10 × 10. (f) Metasomatic texture of Gn, (−)10 × 10. (g) Harbor structure of Gn replacing Sp, (−)10 × 10. (h) Inclusion structure of Py, (−)10 × 10. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)Based on the findings of previous studies [16] and this work on the macroscopic characteristics, ore structures, and textures, and mineral assemblage characteristics of the deposit, the metallogenesis of this deposit can be divided into two periods: hydrothermal metallogenesis and supergene oxidation. The hydrothermal metallogenesis stage may be further divided into four metallogenic stages: the pyrite (sphalerite) stage, sphalerite-galena stage, galena-sphalerite stage, and pyrite-carbonate stage (Figures 5 and 6). A study by Wang [47] also demonstrated that the barite veins produced within (or on either side of) the Kuangshanchang and Qilinchang faults are usually cemented with various forms of dolomite (e.g., medium-fine-grained, coarse-grained pinhole). This indicates that barites are formed by fluids that fill voids along fractures, and these are likely to be an early product of metallogenesis.Figure 5
Typical photographs of the mineral-forming sequence of the Huize Pb–Zn deposit. (a, b) Coarse-grained Py stage (Stage I); (a) (+)10 × 2; (b) (−)10 × 2. (c) Sp–Gn stage (Stage II): edge-shared texture between Sp and Gn; the sphalerite content is far greater than galena. (d) Gn–Sp stage (Stage III): harbor structure of Gn replacing Sp; Gn is the main mineral. (e, f) Fine-grained Py–Dol–Cal stage (Stage IV); (e) (+)10 × 2; (f) (−)10 × 4. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)Figure 6
Mineral paragenesis of the Huize Pb–Zn deposit, SW China. Modified from Han et al. [16]. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite; Brt: barite; Qtz: quartz.The alteration of adjacent rocks within the deposits is relatively simple, and the alteration processes (Figure7) mainly include dolomitization, calcitization, and pyritization, with silification and argillation also occurring over a smaller distribution range. The simultaneous emergence of combinations of these alteration types is an important indicator for locating prospective deposits.Figure 7
Photographs of adjacent rock alterations. (a) Dolomitization, coarse-grained structures are shown in the dolomites, (+)10 × 2. (b) Weakly dolomitized recrystallized sparitic limestone, in which the dolomites are present as euhedral-to-semieuhedral diamond-shaped crystals, and significant recrystallization is shown in the calcites, (−)10 × 2. (c) Pyritization, with the pyrites presented as euhedral-anhedral grains, (−)10 × 10. (d) Argillation, with the clay substances occurring as cryptocrystalline microflakes with grain sizes smaller than 0.02 mm and gaps interspersed between opaque minerals, (−)10 × 2. Sp: sphalerite; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)


### 3.5. Mineralogenetic Epoch

The reported timing for the metallogenic epoch of the Huize deposit varies greatly in the literature. Based on the results of Pb isotope-based age modeling, Liu and Lin [21] concluded that metallogenesis occurred during the Hercynian and Yanshan periods. In contrast, Zhang [3] and Chen [18] concluded that the metallogenic epoch occurred during the Sinian to Permian, from analyses based on sedimentary mineralization. Huang et al. [33] obtained ages of 225-226 Ma from isochron dating of Rb–Sr in sphalerite and Sm–Nd in calcite. Han et al. [24] applied geological deductions in combination with the screening of tectonic deformations and chronology constraints from isotope dating and came to the conclusion that the thrust fault and fold orogenesis occurred during the same period as Pb–Zn metallogenesis, thus placing the metallogenic epoch in the Late Indosinian (200–230 Ma).


## 3.1. Stratigraphy

The stratigraphy of the mining region is composed of Early Sinian metamorphic basement and Sinian and Paleozoic sediments. The upper Paleozoic strata are well-developed, while the Qiongzhusi Formation is the only Cambrian outcrop of the lower Paleozoic strata; the Middle and Upper Cambrian, Ordovician, Silurian, and Lower Devonian strata are missing, and outcrops of the Upper Sinian Dengying Formation and Middle-Upper Devonian strata only appear in localized sections. In particular, the Lower Carboniferous Baizuo Formation (C1b) is the main ore-bearing layer.


## 3.2. Tectonic Structure

The faults within the mining region mainly developed in NE, NW, near-NS, NNW, and near-EW orientations. In particular, the NE–SW-trending reverse shear faults are important ore-controlling tectonic structures. The Kuangshanchang, Qilinchang, and Yinchangpo faults form a tectonic structure comprising three imbricated layers, and as the main faults in this region, they control the Kuangshanchang, Qilinchang, and Yinchangpo deposits (Figure2), respectively. These faults are connected by the near-NS-trending Dongtou reverse fault [16].


## 3.3. Characteristics of the Orebodies

### 3.3.1. Kuangshanchang Deposit

The Kuangshanchang deposit occurs within the area defined by the Kuangshanchang Fault, F5 Fault, and Dongtou Fault (Figure2), with the orebodies mainly occurring within the medium-to-coarse-grained dolomites of the Lower Carboniferous Baizuo Formation (C1b). Within a ~2000 m long section of land, 260 Pb–Zn orebodies of varying sizes can be found. The orebodies usually occur as sheets, lenticels, sacs, lentils, and irregular veins, and these generally propagate along interlayer fractures. Lateral end-to-end alignment of structures and expansion/contraction are usually observed along the strike and dip of the orebodies. The horizontal lengths of the orebodies range from 26 m to 233 m, with an average of 98.17 m. The horizontal widths range from 2 m to 35 m, with an average of 16.65 m, and the depths along dip exceed 1050 m. The Pb grades range from 4.73% to 44.05%, with an average of 20.60%, while the Zn grades range from 3.29% to 46.52%, with an average of 29.74%. As the depth increases, the distribution of ores changes from oxidized ores to mixed ores and finally to sulfide ores.


### 3.3.2. Qilinchang Deposit

The Qilinchang deposit is located above the Qilinchang Fault and comprises the Qilinchang and Dashuijing mining sections. Currently, more than 70 Pb–Zn orebodies have been discovered in this deposit (with 20 possessing industrial value). The Pb–Zn reserves exceed 2.46 Mt, with an average (Zn + Pb) ore grade of 25%. All of the ores occur within the coarse-grained dolomites and limestones in the middle and upper sections of the Lower Carboniferous Baizuo Formation (C1b). The boundaries between the orebodies and the host rocks are very distinct, and the orebodies are generally formed along interlayer fractures, with some ores produced in certain locations at low angles with respect to the strata. The orebodies have a strike of 20–30° NE and a steep dip of 50–76° SE. They also have a short horizontal length and great depth along dip. In the horizontal plane, the orebodies occur as sheets, stratoids, veins, sacs, flat columns, or stockworks; in the vertical plane, the ores are primarily present as lenticels, with thinning or pinched branches at the top and tail ends.


## 3.3.1. Kuangshanchang Deposit

The Kuangshanchang deposit occurs within the area defined by the Kuangshanchang Fault, F5 Fault, and Dongtou Fault (Figure2), with the orebodies mainly occurring within the medium-to-coarse-grained dolomites of the Lower Carboniferous Baizuo Formation (C1b). Within a ~2000 m long section of land, 260 Pb–Zn orebodies of varying sizes can be found. The orebodies usually occur as sheets, lenticels, sacs, lentils, and irregular veins, and these generally propagate along interlayer fractures. Lateral end-to-end alignment of structures and expansion/contraction are usually observed along the strike and dip of the orebodies. The horizontal lengths of the orebodies range from 26 m to 233 m, with an average of 98.17 m. The horizontal widths range from 2 m to 35 m, with an average of 16.65 m, and the depths along dip exceed 1050 m. The Pb grades range from 4.73% to 44.05%, with an average of 20.60%, while the Zn grades range from 3.29% to 46.52%, with an average of 29.74%. As the depth increases, the distribution of ores changes from oxidized ores to mixed ores and finally to sulfide ores.


## 3.3.2. Qilinchang Deposit

The Qilinchang deposit is located above the Qilinchang Fault and comprises the Qilinchang and Dashuijing mining sections. Currently, more than 70 Pb–Zn orebodies have been discovered in this deposit (with 20 possessing industrial value). The Pb–Zn reserves exceed 2.46 Mt, with an average (Zn + Pb) ore grade of 25%. All of the ores occur within the coarse-grained dolomites and limestones in the middle and upper sections of the Lower Carboniferous Baizuo Formation (C1b). The boundaries between the orebodies and the host rocks are very distinct, and the orebodies are generally formed along interlayer fractures, with some ores produced in certain locations at low angles with respect to the strata. The orebodies have a strike of 20–30° NE and a steep dip of 50–76° SE. They also have a short horizontal length and great depth along dip. In the horizontal plane, the orebodies occur as sheets, stratoids, veins, sacs, flat columns, or stockworks; in the vertical plane, the ores are primarily present as lenticels, with thinning or pinched branches at the top and tail ends.


## 3.4. Ore and Mineral Characteristics

The Huize Pb–Zn deposit mainly contains sulfide and oxide ores. Currently, most of the ores extracted from the deposit are sulfide ores. The mineral composition of the sulfide ores is relatively simple and mainly comprises sphalerite, galena, and pyrite, with sporadic occurrences of chalcopyrite, matildite, and native antimony. The host rocks are mainly calcite and dolomite, followed by quartz, barite, gypsum, and clay-type materials.The main ore structures consist of massive, disseminated, banded, veined, stockwork, miarolitic, and brecciated structures (Figure3). The primary ore textures comprise euhedral-anhedral-grained, metasomatic, edge-shared, void-filling, poikilitic, slaty cleavage, skeletal, exsolution, graphic, crumpled, and cataclastic textures (Figure 4).Figure 3
Typical structure photographs of minerals in the Huize Pb–Zn deposit. (a) Massive ore, miarolitic structure. (b) Dense massive ore, massive structures. (c) Massive ore, massive structures. (d) Massive ore, vein structure. (e) Disseminated ore, disseminated structures. (f) Banded structure. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)Figure 4
Typical texture photographs of minerals in the Huize Pb–Zn deposit. (a) Xenomorphic granular texture of Sp, (−)10 × 10. (b) Hypidiomorphic–xenomorphic granular textures of Sp and Gn, (−)10 × 2. (c) Cataclastic texture of Py, (−)10 × 4. (d) Edge-shared texture between Sp and Gn, (−)10 × 4. (e) Skeleton crystal structure of Gn replacing Py, (−)10 × 10. (f) Metasomatic texture of Gn, (−)10 × 10. (g) Harbor structure of Gn replacing Sp, (−)10 × 10. (h) Inclusion structure of Py, (−)10 × 10. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)Based on the findings of previous studies [16] and this work on the macroscopic characteristics, ore structures, and textures, and mineral assemblage characteristics of the deposit, the metallogenesis of this deposit can be divided into two periods: hydrothermal metallogenesis and supergene oxidation. The hydrothermal metallogenesis stage may be further divided into four metallogenic stages: the pyrite (sphalerite) stage, sphalerite-galena stage, galena-sphalerite stage, and pyrite-carbonate stage (Figures 5 and 6). A study by Wang [47] also demonstrated that the barite veins produced within (or on either side of) the Kuangshanchang and Qilinchang faults are usually cemented with various forms of dolomite (e.g., medium-fine-grained, coarse-grained pinhole). This indicates that barites are formed by fluids that fill voids along fractures, and these are likely to be an early product of metallogenesis.Figure 5
Typical photographs of the mineral-forming sequence of the Huize Pb–Zn deposit. (a, b) Coarse-grained Py stage (Stage I); (a) (+)10 × 2; (b) (−)10 × 2. (c) Sp–Gn stage (Stage II): edge-shared texture between Sp and Gn; the sphalerite content is far greater than galena. (d) Gn–Sp stage (Stage III): harbor structure of Gn replacing Sp; Gn is the main mineral. (e, f) Fine-grained Py–Dol–Cal stage (Stage IV); (e) (+)10 × 2; (f) (−)10 × 4. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)
(e)
(f)Figure 6
Mineral paragenesis of the Huize Pb–Zn deposit, SW China. Modified from Han et al. [16]. Sp: sphalerite; Gn: galena; Py: pyrite; Dol: dolomite; Cal: calcite; Brt: barite; Qtz: quartz.The alteration of adjacent rocks within the deposits is relatively simple, and the alteration processes (Figure7) mainly include dolomitization, calcitization, and pyritization, with silification and argillation also occurring over a smaller distribution range. The simultaneous emergence of combinations of these alteration types is an important indicator for locating prospective deposits.Figure 7
Photographs of adjacent rock alterations. (a) Dolomitization, coarse-grained structures are shown in the dolomites, (+)10 × 2. (b) Weakly dolomitized recrystallized sparitic limestone, in which the dolomites are present as euhedral-to-semieuhedral diamond-shaped crystals, and significant recrystallization is shown in the calcites, (−)10 × 2. (c) Pyritization, with the pyrites presented as euhedral-anhedral grains, (−)10 × 10. (d) Argillation, with the clay substances occurring as cryptocrystalline microflakes with grain sizes smaller than 0.02 mm and gaps interspersed between opaque minerals, (−)10 × 2. Sp: sphalerite; Py: pyrite; Dol: dolomite; Cal: calcite.
(a)
(b)
(c)
(d)


## 3.5. Mineralogenetic Epoch

The reported timing for the metallogenic epoch of the Huize deposit varies greatly in the literature. Based on the results of Pb isotope-based age modeling, Liu and Lin [21] concluded that metallogenesis occurred during the Hercynian and Yanshan periods. In contrast, Zhang [3] and Chen [18] concluded that the metallogenic epoch occurred during the Sinian to Permian, from analyses based on sedimentary mineralization. Huang et al. [33] obtained ages of 225-226 Ma from isochron dating of Rb–Sr in sphalerite and Sm–Nd in calcite. Han et al. [24] applied geological deductions in combination with the screening of tectonic deformations and chronology constraints from isotope dating and came to the conclusion that the thrust fault and fold orogenesis occurred during the same period as Pb–Zn metallogenesis, thus placing the metallogenic epoch in the Late Indosinian (200–230 Ma).


## 4. Methods

### 4.1. Sample Collection

Although a large accumulation of data already exists on the isotope geochemistry of the ultra-large Huize Pb–Zn deposit, most of these studies have focused on the Qilinchang deposit. While some samples have been obtained from the Kuangshanchang deposit, these samples are lacking in representativity. Hence, we chose the 15th stope of tunnel 1752 m in Kuangshanchang as the primary focus (Figure8) for C–H–O isotopic measurements in this work. We combined our findings with previous studies on fluid inclusions and systematically investigated the origins of the metallogenic fluids, in order to identify the two fluids that are present in the mixed metallogenesis of the Huize deposit. Fifteen dolomite samples and five calcite samples were obtained for C–O isotopic analysis following the selection of monomineralic rocks from the 17 dolomite or limestone samples that were acquired for this study.Figure 8
Documentation and sampling of Stope 15# in tunnel 1752 m in Kuangshanchang. (1) Oxidized Pb–Zn orebodies; (2) beige dolomites, with veined, porphyritic calcite developments; (3) light grey-to-grey-white medium-grained calcitic dolomite; (4) grey-to-dark-grey fine-grained limestones; (5) calcite. I. First stage ores are mainly coarse-grained pyrites with small quantities of deep brown sphalerites; II. Second stage ores are mainly brown sphalerites with small amounts of galena; III. Third stage ores, rose-colored sphalerite + galena. (a) Morphology of the orebody 0–5 m above head height in Stope 15# of tunnel 1752 m. Yellow-brown and reddish-brown Pb–Zn oxide orebodies were found on either side of the grey-black Pb–Zn sulfide ores, while yellow coarse-grained dolomites lie outside the ores. Several vein-shaped oxide ores were intercalated within the sulfide orebodies. (b) Morphology of the orebody 4 m into Stope 15# of tunnel 1752 m. The joint fractures are more developed in this area, the oxide orebodies formed through leaching, and sulfide orebodies occur in alternating layers. The top part of this wall is composed of ocher-red carbonates that are likely to have been produced during the later stages of hydrothermal metallogenesis. (c) Bottom part of the sulfide orebody 8 m into Stope 15# of tunnel 1752 m. The main mineral in this orebody is coarse-grained pyrite, with sporadic occurrences of deep-red sphalerites. (d) Top part of the sulfide orebody on the left wall, 8 m into Stope #15 of tunnel 1752 m. The main minerals in the orebody are yellow-brown to brown sphalerites, followed by galena. The sphalerites are distributed in porphyritic and vein-like shapes, with lead-grey star-like points of galena tightly associated with the sphalerite. (e) Sulfide orebody on the right wall, 8 m into Stope #15 of tunnel 1752 m, which we deduce to be the top part of the orebody, based on its occurrence. The main minerals found in this orebody are lead-grey-colored galena, followed by yellow-brown-colored sphalerite. The galena displays a porphyritic, vein-like distribution, while the sphalerites display a vein-like, spotted distribution. (f) Morphology of an oxide orebody and its adjacent rocks, 19.5 m into Stope 15# in tunnel 1752 m. (g) Interstratum fracture 46 m into Stope 15# of tunnel 1752 m. The surface of the fracture has a relaxed wave-like shape, and the fracture is 1–10 cm wide, is filled with yellow-brown fault gouge, and displays schistosity. This fracture acts as the boundary between the C1b and C1d strata. The hanging wall is composed of C1b light grey-to-grey white calcitic fine-grained dolomite, while the footwall is composed of C1d grey-to-dark grey limestone breccia cemented with clay, which appears to be lenticularized. The fracture is a left-lateral reverse shear fracture, with an orientation of NE45°∠40°SE.Through the collection and organization of data from previous studies, it was found that the H and O isotopes in the Huize deposit were sourced from the H of calcite fluid inclusions and mineralic O. The calculatedδ18O of the fluid may not be truly representative of the actual isotopic composition of the original metallogenic fluid because of issues such as the selection of the isotope equilibrium temperature and uncertainties in the equilibrium fractionation of mineral-water oxygen isotopes. Furthermore, calcites are products of the late stages of metallogenesis and lack information on the early stages of metallogenesis. Therefore, calcite samples are incapable of indicating the evolution of metallogenic fluids during different stages of metallogenesis. In this study, the macroscopic characteristics of orebodies were observed in the field, followed by rough division of the metallogenic stages. Microscopic identifications and hand specimen studies were then performed in a laboratory based on paragenetic sequences, textures, structures, and intercalation relationships, from which the ages of the selected monomineralic sphalerite samples were determined. Finally, three samples were selected from each of the stages (I–III) for a total of nine samples, and these samples were used for the measurements of fluid inclusion H and O isotopes in sphalerites. To track the processes of metallogenic fluid evolution in a comprehensive manner, we examined ten stage I1 barite samples (Figure 9).Figure 9
Documentation and sampling of 51# transverse tunnel 1571 m of Zhujiayakou section in Qilinchang [47]. 1: barite; 2: fault; 3: sample location and sample number; 4: Lower Carboniferous Baizuo Fm. pale-red coarse-grained dolomite.As barite is widely distributed throughout the Pb–Zn deposits in Huize, Maozu, and Jinshachang, we also performed H–O isotopic measurements on the barites in the Huize mining area. In the periphery of the Huize mining area, barites are mainly distributed within the Kuangshanchang Fault and the Zhujiayakou section of tunnel 1571 m in the Qilinchang deposit (Figure9). In the former, barites are distributed within four veins or clots that take on irregular shapes and the shape of sacs and veins, while the barites occur as white nodules, sheets, and slabs that are distributed within calcitic and debritic dolomite cements, with developments of stockwork calcites. In the latter, the barites mainly occur as white nodules, radial growths, and veins within light-flesh-colored coarse-grained dolomites.


### 4.2. C–O Isotopic Analysis Method

C–O isotope analyses were carried out by ALS Minerals. Pulverized samples of carbonate were placed in borosilicate glass vials sealed with butyl rubber septa and reacted with concentrated phosphoric acid at 72°C for at least 1 h in a heated aluminum block. The evolved CO2 gas was then conducted to an LGR Analyzer (Los Gatos Research, model 908-0021), which utilizes off-axis integrated cavity output spectroscopy (OA-ICOS), and the carbon and oxygen isotope ratios were measured and recorded from the absorption spectra of 12C16O16O, 13C16O16O and 12C16O18O in the near-infrared wavelength region.The instrument was calibrated using standard CaCO3 minerals known as the Vienna Pee Dee Belemnite (VPDB) for δ13C and Vienna Standard Mean Ocean Water (VSMOW) for δ18O, which had been previously calibrated by isotope ratio mass spectrometry relative to the international isotopic standards NBS18 and NBS19. Individual analyses were demonstrated to have an internal precision of better than 0.05% for δ13C and δ18O.


### 4.3. H–O Isotopic Analysis Method

Data on calcite samples from the late stages of metallogenesis were compiled from previous studies, while data on I1 barite samples were obtained from our measurements. The H isotope ratios in both sets of samples were determined through hydrogen gases generated from the zinc reduction of water (the samples were baked at low temperatures (100°C–120°C) for 3 h to remove all adsorbed water and secondary inclusions), while O isotope analyses were carried out using the BrF5 technique. δ18OH2O of the calcites were obtained from the conversion of δ18Ocalcite, using the formula: 1000 lnCalcite-H2O = 4.01 × 106/T2 − 4.66 × 103/T + 1.71 [50], where the temperatures T and T2 are the homogenization temperature of the calcite fluid inclusions and the average measured temperature of the sulfur isotopes (200°C), respectively. δ18OH2O values of the barites were calculated using 1000ln⁡αBarite-H2O = 3.01 × 106/T2 − 7.30, and the temperature data required for this calculation were taken from the fluid inclusion temperature data of the corresponding samples.H–O isotope analyses were also carried out by ALS Minerals. For hydrogen isotope analysis (with H in inclusions), the sorted 40 mesh sphalerite samples were baked at low temperatures (100°C–120°C) to remove adsorbed water and secondary fluid inclusions in the minerals and loaded into a zero-blank autosampler. The hydrogen isotopic composition was measured using a Thermo Finnigan thermal combustion elemental analyzer (TC/EA) coupled to a Thermo Finnigan Delta Plus XP continuous-flow isotope ratio mass spectrometer (CF-IRMS). Values ofδ2H are reported using delta (δ) notation in permil units (‰) relative to VSMOW, with a precision of 3‰.For oxygen isotope analysis (with O in inclusions), the sorted 40 mesh sphalerite samples were baked at low temperatures (100°C–120°C) to remove adsorbed water and secondary fluid inclusions in the minerals and loaded into tin capsules and placed in a Thermo Scientific TC/EA high-temperature conversion elemental analyzer, then heated to 1450°C, and cracked to release the fluid inclusions in the form of gas. The extracted oxygen reacts with carbon rods in the furnace to produce CO, which is analyzed for18O/16O using a Thermo Finnigan MAT 253 stable isotope ratio mass spectrometer. Values of δ18O were calculated by normalizing the 18O/16O ratio in the sample to that in the VSMOW international standard. Values are reported using the delta (δ) notation in permil units (‰) and are normally reproducible to 0.2‰.


## 4.1. Sample Collection

Although a large accumulation of data already exists on the isotope geochemistry of the ultra-large Huize Pb–Zn deposit, most of these studies have focused on the Qilinchang deposit. While some samples have been obtained from the Kuangshanchang deposit, these samples are lacking in representativity. Hence, we chose the 15th stope of tunnel 1752 m in Kuangshanchang as the primary focus (Figure8) for C–H–O isotopic measurements in this work. We combined our findings with previous studies on fluid inclusions and systematically investigated the origins of the metallogenic fluids, in order to identify the two fluids that are present in the mixed metallogenesis of the Huize deposit. Fifteen dolomite samples and five calcite samples were obtained for C–O isotopic analysis following the selection of monomineralic rocks from the 17 dolomite or limestone samples that were acquired for this study.Figure 8
Documentation and sampling of Stope 15# in tunnel 1752 m in Kuangshanchang. (1) Oxidized Pb–Zn orebodies; (2) beige dolomites, with veined, porphyritic calcite developments; (3) light grey-to-grey-white medium-grained calcitic dolomite; (4) grey-to-dark-grey fine-grained limestones; (5) calcite. I. First stage ores are mainly coarse-grained pyrites with small quantities of deep brown sphalerites; II. Second stage ores are mainly brown sphalerites with small amounts of galena; III. Third stage ores, rose-colored sphalerite + galena. (a) Morphology of the orebody 0–5 m above head height in Stope 15# of tunnel 1752 m. Yellow-brown and reddish-brown Pb–Zn oxide orebodies were found on either side of the grey-black Pb–Zn sulfide ores, while yellow coarse-grained dolomites lie outside the ores. Several vein-shaped oxide ores were intercalated within the sulfide orebodies. (b) Morphology of the orebody 4 m into Stope 15# of tunnel 1752 m. The joint fractures are more developed in this area, the oxide orebodies formed through leaching, and sulfide orebodies occur in alternating layers. The top part of this wall is composed of ocher-red carbonates that are likely to have been produced during the later stages of hydrothermal metallogenesis. (c) Bottom part of the sulfide orebody 8 m into Stope 15# of tunnel 1752 m. The main mineral in this orebody is coarse-grained pyrite, with sporadic occurrences of deep-red sphalerites. (d) Top part of the sulfide orebody on the left wall, 8 m into Stope #15 of tunnel 1752 m. The main minerals in the orebody are yellow-brown to brown sphalerites, followed by galena. The sphalerites are distributed in porphyritic and vein-like shapes, with lead-grey star-like points of galena tightly associated with the sphalerite. (e) Sulfide orebody on the right wall, 8 m into Stope #15 of tunnel 1752 m, which we deduce to be the top part of the orebody, based on its occurrence. The main minerals found in this orebody are lead-grey-colored galena, followed by yellow-brown-colored sphalerite. The galena displays a porphyritic, vein-like distribution, while the sphalerites display a vein-like, spotted distribution. (f) Morphology of an oxide orebody and its adjacent rocks, 19.5 m into Stope 15# in tunnel 1752 m. (g) Interstratum fracture 46 m into Stope 15# of tunnel 1752 m. The surface of the fracture has a relaxed wave-like shape, and the fracture is 1–10 cm wide, is filled with yellow-brown fault gouge, and displays schistosity. This fracture acts as the boundary between the C1b and C1d strata. The hanging wall is composed of C1b light grey-to-grey white calcitic fine-grained dolomite, while the footwall is composed of C1d grey-to-dark grey limestone breccia cemented with clay, which appears to be lenticularized. The fracture is a left-lateral reverse shear fracture, with an orientation of NE45°∠40°SE.Through the collection and organization of data from previous studies, it was found that the H and O isotopes in the Huize deposit were sourced from the H of calcite fluid inclusions and mineralic O. The calculatedδ18O of the fluid may not be truly representative of the actual isotopic composition of the original metallogenic fluid because of issues such as the selection of the isotope equilibrium temperature and uncertainties in the equilibrium fractionation of mineral-water oxygen isotopes. Furthermore, calcites are products of the late stages of metallogenesis and lack information on the early stages of metallogenesis. Therefore, calcite samples are incapable of indicating the evolution of metallogenic fluids during different stages of metallogenesis. In this study, the macroscopic characteristics of orebodies were observed in the field, followed by rough division of the metallogenic stages. Microscopic identifications and hand specimen studies were then performed in a laboratory based on paragenetic sequences, textures, structures, and intercalation relationships, from which the ages of the selected monomineralic sphalerite samples were determined. Finally, three samples were selected from each of the stages (I–III) for a total of nine samples, and these samples were used for the measurements of fluid inclusion H and O isotopes in sphalerites. To track the processes of metallogenic fluid evolution in a comprehensive manner, we examined ten stage I1 barite samples (Figure 9).Figure 9
Documentation and sampling of 51# transverse tunnel 1571 m of Zhujiayakou section in Qilinchang [47]. 1: barite; 2: fault; 3: sample location and sample number; 4: Lower Carboniferous Baizuo Fm. pale-red coarse-grained dolomite.As barite is widely distributed throughout the Pb–Zn deposits in Huize, Maozu, and Jinshachang, we also performed H–O isotopic measurements on the barites in the Huize mining area. In the periphery of the Huize mining area, barites are mainly distributed within the Kuangshanchang Fault and the Zhujiayakou section of tunnel 1571 m in the Qilinchang deposit (Figure9). In the former, barites are distributed within four veins or clots that take on irregular shapes and the shape of sacs and veins, while the barites occur as white nodules, sheets, and slabs that are distributed within calcitic and debritic dolomite cements, with developments of stockwork calcites. In the latter, the barites mainly occur as white nodules, radial growths, and veins within light-flesh-colored coarse-grained dolomites.


## 4.2. C–O Isotopic Analysis Method

C–O isotope analyses were carried out by ALS Minerals. Pulverized samples of carbonate were placed in borosilicate glass vials sealed with butyl rubber septa and reacted with concentrated phosphoric acid at 72°C for at least 1 h in a heated aluminum block. The evolved CO2 gas was then conducted to an LGR Analyzer (Los Gatos Research, model 908-0021), which utilizes off-axis integrated cavity output spectroscopy (OA-ICOS), and the carbon and oxygen isotope ratios were measured and recorded from the absorption spectra of 12C16O16O, 13C16O16O and 12C16O18O in the near-infrared wavelength region.The instrument was calibrated using standard CaCO3 minerals known as the Vienna Pee Dee Belemnite (VPDB) for δ13C and Vienna Standard Mean Ocean Water (VSMOW) for δ18O, which had been previously calibrated by isotope ratio mass spectrometry relative to the international isotopic standards NBS18 and NBS19. Individual analyses were demonstrated to have an internal precision of better than 0.05% for δ13C and δ18O.


## 4.3. H–O Isotopic Analysis Method

Data on calcite samples from the late stages of metallogenesis were compiled from previous studies, while data on I1 barite samples were obtained from our measurements. The H isotope ratios in both sets of samples were determined through hydrogen gases generated from the zinc reduction of water (the samples were baked at low temperatures (100°C–120°C) for 3 h to remove all adsorbed water and secondary inclusions), while O isotope analyses were carried out using the BrF5 technique. δ18OH2O of the calcites were obtained from the conversion of δ18Ocalcite, using the formula: 1000 lnCalcite-H2O = 4.01 × 106/T2 − 4.66 × 103/T + 1.71 [50], where the temperatures T and T2 are the homogenization temperature of the calcite fluid inclusions and the average measured temperature of the sulfur isotopes (200°C), respectively. δ18OH2O values of the barites were calculated using 1000ln⁡αBarite-H2O = 3.01 × 106/T2 − 7.30, and the temperature data required for this calculation were taken from the fluid inclusion temperature data of the corresponding samples.H–O isotope analyses were also carried out by ALS Minerals. For hydrogen isotope analysis (with H in inclusions), the sorted 40 mesh sphalerite samples were baked at low temperatures (100°C–120°C) to remove adsorbed water and secondary fluid inclusions in the minerals and loaded into a zero-blank autosampler. The hydrogen isotopic composition was measured using a Thermo Finnigan thermal combustion elemental analyzer (TC/EA) coupled to a Thermo Finnigan Delta Plus XP continuous-flow isotope ratio mass spectrometer (CF-IRMS). Values ofδ2H are reported using delta (δ) notation in permil units (‰) relative to VSMOW, with a precision of 3‰.For oxygen isotope analysis (with O in inclusions), the sorted 40 mesh sphalerite samples were baked at low temperatures (100°C–120°C) to remove adsorbed water and secondary fluid inclusions in the minerals and loaded into tin capsules and placed in a Thermo Scientific TC/EA high-temperature conversion elemental analyzer, then heated to 1450°C, and cracked to release the fluid inclusions in the form of gas. The extracted oxygen reacts with carbon rods in the furnace to produce CO, which is analyzed for18O/16O using a Thermo Finnigan MAT 253 stable isotope ratio mass spectrometer. Values of δ18O were calculated by normalizing the 18O/16O ratio in the sample to that in the VSMOW international standard. Values are reported using the delta (δ) notation in permil units (‰) and are normally reproducible to 0.2‰.


## 5. Measurements and Reinterpretation of Existing Results

### 5.1. C–O Isotopes

It is well known that the measurement of C and O isotope compositions is an effective method for tracing the origins of CO2 within metallogenic fluids [50]. We obtained the C–O isotopic compositions of 83 samples through our measurements, as well as from the reorganization of relevant data from the literature (Table 1).Table 1
C–O isotopic compositions of sphalerite, calcite, and barite in Huize Pb–Zn deposit, SW China.
Numbers
Objects
Positions
δ
13
C
P
D
B
/
‰
δ
18
O
S
M
O
W
/
‰
Date source
HQO-99-1
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−1.94
17.09
a
HQO-109-4
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−3.27
17.79
1631-38
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.97
18.56
HQ-84
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.23
18.21
HQ-109-4
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.31
17.79
1571-2
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.30
18.21
Hui-2-3
Calcite
Tunnel 1751 m of 6# orebody in Qilinchang
−2.75
17.80
b
38-3
Calcite
Tunnel 1884 m of 6# orebody in Qilinchang
−2.80
17.10
Hui-6-10
Calcite
Tunnel 1648 m of 6# orebody in Qilinchang
−2.90
17.80
13-61
Calcite
Tunnel 1691 m of 6# orebody in Qilinchang
−2.70
18.10
Hui-1-1
Calcite
Tunnel 1836 m of 6# orebody in Qilinchang
−3.20
18.43
14-2-8
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.60
18.70
14-3-6
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.70
18.40
Hui-5-1
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.40
18.10
Hui-4-23
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.10
17.50
23-4R
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.00
17.60
Hui-8
Barite
Tunnel 1571 m of 6# orebody in Qilinchang
8.29
HQC-25
Baritization cataclasites
Tunnel 1631 m of 6# orebody in Qilinchang
0.30
20.40
a
HQC-98
Mineralization dolomitic granulitic rock
Tunnel 1631 m of 6# orebody in Qilinchang
−3.20
19.50
HQC-92
Mineralization dolomitic granulitic rock
Tunnel 1631 m of 6# orebody in Qilinchang
−1.60
17.80
41707
Altered dolomite
Tunnel 2233 m in Kuangshanchang
−0.80
20.50
c
Hui-1-2
Near ore dolomite
Tunnel 2233 m in Kuangshanchang
0.77
21.16
HE-16
Biogenic limestone
Tunnel 2233 m in Kuangshanchang
−0.44
22.45
d
HE-18
Biogenic limestone
Tunnel 2233 m in Kuangshanchang
−1.50
21.33
HE-17
Middle-fine grain dolomite
Tunnel 2233 m in Kuangshanchang
0.85
20.98
SC-33
Dolomitic limestone
Sunjiagou section of mining periphery
−0.90
21.00
a
SC-34
Coarse grain dolomite
Sunjiagou section of mining periphery
−2.20
20.50
SC-35
Coarse grain dolomite
Sunjiagou section of mining periphery
−1.20
21.40
HE11
Middle-fine grain dolomite
Zhujiayakou section of mining periphery
0.85
19.32
d
HE10
Dolomitic limestone
Zhujiayakou section of mining periphery
−3.35
19.42
HE12
Dolomitic limestone
Zhujiayakou section of mining periphery
−1.10
20.09
HE02
Middle-fine grain dolomite
Qingchaojie section of mining periphery
0.09
22.60
HE01
Biogenic limestone
Qingchaojie section of mining periphery
−1.15
22.59
HE03
Dolomitic limestone
Qingchaojie section of mining periphery
−0.53
23.14
HZ911-3
Porphyritic calcite
1# orebody
−2.20
17.50
e
HZ911-10
Lumpy calcite
1# orebody
−3.40
18.40
HZ911-15
Lumpy calcite
1# orebody
−3.50
18.60
HZQ25
Lumpy calcite
6# orebody
−2.50
17.50
HZQ40
Porphyritic calcite
6# orebody
−2.60
17.70
HZQ47
Lumpy calcite
6# orebody
−3.10
17.50
HZQ55
Vein calcite
6# orebody
−2.70
17.70
HZQ66
Lumpy calcite
6# orebody
−3.40
18.10
HZQ70
Porphyritic calcite
6# orebody
−3.30
18.10
HZQ77
Vein calcite
6# orebody
−2.80
17.80
HZQ85
Porphyritic calcite
6# orebody
−2.70
17.30
HZQ90
Porphyritic calcite
6# orebody
−2.70
17.20
HZQ96
Lumpy calcite
6# orebody
−2.10
17.50
HQ10-7
Lumpy calcite
10# orebody
−2.90
17.00
HQ10-12
Lumpy calcite
10# orebody
−3.20
18.50
HQ10-18
Lumpy calcite
10# orebody
−2.30
16.80
HQ10-25
Lumpy calcite
10# orebody
−3.00
17.90
HQ10-5
Lumpy calcite
10# orebody
−2.80
17.20
HQ8-115
Lumpy calcite
8# orebody
−2.20
17.00
HQ18-143
Lumpy calcite
8# orebody
−2.70
17.60
HQ8-98
Vein calcite
8# orebody
−3.00
17.80
HZQ35
Miarolitic calcite
Carbonate of Qixia–Maokou formation (500 m from orebody)
0.50
22.10
HZK33
Miarolitic calcite
Carbonate of Qixia–Maokou formation (500 m from orebody)
1.10
23.50
HZQ74
Whole rock of coarse grain dolomite
Host rock of Baizuo formation in number 10 ore body
−0.80
22.60
HZ2053-29
Whole rock of coarse grain dolomite
Host rock of Baizuo formation in number 1 ore body (1500 m from orebody)
0.40
23.20
HZS40
Whole rock of coarse grain dolomite
Baizuo formation in Sunjiagou section (1500 m from orebody)
0.70
22.80
HZX-3
Whole rock of coarse grain dolomite
Baizuo formation in Xiaoheiqing (1000 m from orebody)
−0.20
23.10
HZ911-4
Calcite filled in fractures
NE tectonic belt (150 m from orebody)
−3.00
16.70
HZQ28
Calcite filled in fractures
NE tectonic belt (150 m from orebody)
−3.40
16.30
Z0807-2r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−1.31
19.60
f
Z0807-3r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−2.52
17.25
Z0807-7r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.17
20.30
Z0807-8r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.75
21.90
Z0807-15r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.83
19.95
Z0807-18r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−4.11
15.80
Z0807-21r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.49
20.00
Z0807-22r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.89
20.80
Z0807-23r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.07
23.80
Z0807-24r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.13
20.50
Z0807-25r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.71
20.70
Z0807-26r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.64
21.50
Z0807-27r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.53
20.40
Z0807-28r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.54
21.40
Z0807-29r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.66
22.30
Z0807-14r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.36
16.90
Z0807-19r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−0.91
18.65
Z0807-25r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.77
21.30
Z0807-26r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−3.70
20.20
Z0807-27r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.59
20.70Figure10 shows that the C–O isotopic compositions of the Huize Pb–Zn deposit have the following characteristics:Figure 10
(a) C–O isotope composition diagram of Huize Pb–Zn deposit. (b) C–O isotope composition diagram of different orebody and wall rocks in Huize Pb–Zn deposit. Data sources: (A) previous data [6, 10, 16, 18, 21]; (B) this paper.(1) The C–O isotopic compositions of the Huize Pb–Zn deposit are relatively homogeneous. Theδ13CPDB-δ18OSMOW maps (Figure 10(a)) show that the isotopic compositions cluster within a narrow range between magmatic carbonates and marine carbonates, with the compositions edging closer to those of marine carbonates. The isotopic compositions, as a whole, display the following order of isotopic values: δ13Ccalcite < δ13Caltereddolomite < δ13Cdolomite < δ13Climestone and δ18Ocalcite < δ18Oaltereddolomite < δ18Odolomite < δ18Olimestone. The δ18O values of the Mid-to-Late Devonian marine limestones are mainly distributed around 20‰±, with δ13C = 0±. The average δ18O and δ13C values of limestones found in the Huize mining area are equivalent to these values, which decrease as dolomitization increases. However, the δ18O and δ13C isotopic compositions of calcite are noticeably different from those of the Mid-to-Late Devonian marine limestones, as the calcite δ18O and δ13C values of the orebodies and tectonic belts are clearly lower than those in the adjacent carbonate rocks.(2) Similar C–O isotopic compositions were observed for gangue calcites in different orebodies and calcites with different occurrences, withδ13CPDB values that vary within −1.9‰ to −3.5‰ and δ18OSMOW values varying within 16.8‰–18.7‰. This indicates that the metallogenic fluid has a δ13C value that is much lower than that of the host rocks.(3) The altered dolomites and bioclastic limestones of Kuangshanchang, carbonates from strata in the periphery of the mining area, and miarolitic calcites have similar C–O isotopic compositions, with most of these compositions projecting within the region of marine carbonates. This indicates that the source of carbon in these rocks is innate to the carbonate strata in this region, as their C–O isotopic compositions indicate that the carbon was produced via leaching of adjacent rocks by fluids, which is significantly different from calcites found in ores of the Huize deposit.(4) The C–O isotopic compositions of calcites from the NE-trending tectonic belt are similar to those of gangue calcites, which is distinctly different from the C–O isotopic compositions of the previously described rock strata. This is because the main channel through which the metallogenic fluids of the Huize Pb–Zn deposit pass is the NE-trending tectonic belt [15, 21, 33, 51]. Therefore, the C–O isotopic compositions of the calcites in this tectonic belt plot closest to those of the metallogenic fluid.(5) In the source region of the metallogenic fluid or organic matter-rich strata below the orebodies penetrated by the fluid, water-rock reactions will solvate adjacent carbonates and cause an exchange of C–O isotopes between the fluid and the strata. This ultimately causesδ13C of the fluid to increase and δ13C of the adjacent rocks to decrease.


### 5.2. H–O Isotopes

As H2O is an important component of metallogenic fluids, it is important to elucidate the source of H2O in order to investigate the origin of the metallogenic fluid. The H and O isotopic compositions of gangue minerals, ore minerals, and their related alteration minerals are the most direct and effective indicators of the source of H2O in metallogenic fluids. The δD value measured in calcite fluid inclusions reflects the H–O isotopic composition of metallogenic hydrothermal solutions more accurately than δD measurements in quartz [51, 52]. Therefore, previous researchers have generally chosen to use calcites to determine the H–O isotopic composition of the metallogenic fluid; these results are shown in Table 2.Table 2
H–O isotopic compositions of sphalerite, calcite, and barite in Huize Pb–Zn deposit, SW China.
Numbers
Positions
Objects
δ
18
O
H
2
O
‰
δ
D
‰
Date source
HZ911-10
1# orebody
Lumpy calcite
8.6
−59.8
a
HZ911-15
1# orebody
Lumpy calcite
8.8
−52.4
HZQ25
6# orebody
Lumpy calcite
7.7
−50.2
HZQ40
6# orebody
Porphyritic calcite
7.9
−55.6
HZQ47
6# orebody
Lumpy calcite
7.7
−57.9
HZQ55
6# orebody
Vein calcite
7.9
−54.1
HZQ66
6# orebody
Lumpy calcite
8.3
−53.9
HZQ77
6# orebody
Vein calcite
8.0
−58.0
HZQ85
6# orebody
Porphyritic calcite
7.5
−52.7
HQ10-12
10# orebody
Lumpy calcite
8.7
−53.2
HQ10-18
10# orebody
Lumpy calcite
7.0
−57.3
HQ10-25
10# orebody
Porphyritic calcite
8.1
−53.0
HQ10-5
10# orebody
Vein calcite
7.4
−52.8
HQ8-115
8# orebody
Lumpy calcite
7.2
−55.2
HQ8-143
8# orebody
Lumpy calcite
7.8
−54.1
HQ8-98
8# orebody
Vein calcite
8.0
−54.3
HQO-99-1
Qilinchang
Calcite
7.8
−43.5
b
HQO-109-4
Qilinchang
Calcite
10.1
−54.8
1631-38
Qilinchang
Calcite
7.8
−48.0
HQ-84
Qilinchang
Calcite
9.7
−51.5
HQ-109-4
Qilinchang
Calcite
7.6
−43.5
1751-2
Qilinchang
Calcite
7.7
−55.4
HW-2-3
Qilinchang
Calcite
7.1
−55.8
c
38-3
Qilinchang
Calcite
6.4
−64.0
Hui-6-10
Qilinchang
Calcite
7.1
−75.0
13-61
Qilinchang
Calcite
8.0
−57.0
14-2-8
Qilinchang
Calcite
−2.1
−66.0
Hui-8
Kuangshanchang
Barite
7.8
−86.0
Z0807-1r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
28.0
−52.0
d
Z0807-4r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
5.5
−50.0
Z0807-5r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
2.2
−55.0
Z0807-6r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
25.5
−50.0
Z0807-10r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
17.1
−27.0
Z0807-11r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
4.0
−43.0
Z0807-12r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
13.2
−49.0
Z0807-13r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
12.2
−57.0
Z0807-17r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
28.9
−51.0
JS-11-1
Qilinchang
Barite
−91.3
11.6
e
JS-11-2
Qilinchang
Barite
−85.5
9.9
JS-11-3
Qilinchang
Barite
−87.8
11.8
JS-12-1
Qilinchang
Barite
−77.4
11.8
JS-12-3
Qilinchang
Barite
−80.5
11.7
JS-13-1
Qilinchang
Barite
−79.8
12.4
JS-40-3
Kuangshangchang
Barite
−73.7
12.4
JS-40-5
Kuangshangchang
Barite
−63.9
13.7
JS-41-1
Kuangshangchang
Barite
−75.1
13.4
JS-42-2
Kuangshangchang
Barite
−61.7
13.4
a, b, c, d, and e: data from Li et al. [10], Han et al. [16], Liu and Lin [21], this paper, and Wang [47]. Different stages of sphalerite from the same ores can be separated based on textural and structural observations (Figures 3, 4, 6, and 8).In the Huize deposit, the characteristics of sphalerites from different stages of metallogenesis are very distinct. Isotope exchange reactions do not happen between fluid inclusions and minerals in later stages, and fluid inclusion petrography has shown that inclusions in sphalerite are mainly comprised of primary and pseudosecondary inclusions, with few secondary inclusions [48, 49]. As the adsorbed water and the associated secondary inclusions have been removed from the sphalerite samples during the measurement process, the direct measurement of the H and O isotopic composition of sphalerite inclusions from different stages of metallogenesis is representative of the native isotopic composition of the metallogenic fluids, and these data also allow us to track the evolution of metallogenic fluids during different stages of metallogenesis.Figure11 shows the following.Figure 11
Plot ofδD versus δ18OH2O values from Huize Pb–Zn deposit. Data sources: (a) previous data [10, 16, 21]; (b) this paper; (c) Wang [47].(1) Similar to the C and O isotopic composition characteristics, the H–O isotopic compositions of the Huize Pb–Zn deposit are also relatively stable, withδD ranging within −43.5‰ to −66‰, with an average of −56.3‰, and δ18OH2O values ranging within −2.05‰–10.08‰, with an average of 7.55‰.(2) The H–O isotopic compositions of calcites from different orebodies, with different occurrences, do not differ significantly from one another. This characteristic reflects the presence of two different fluids within the metallogenic system, that is, a deeply sourced fluid, and a fluid sourced from atmospheric precipitation. Based on the geological conditions for metallogenesis and comparison between the H–O isotopic compositions of the metallogenic fluid and those of orogenic mineral deposits [53–64], we deduced that the metallogenic fluid is a mix between deeply sourced fluids and basin brines.However, it is worth noting that theδ18OH2O value was calculated from the isotope equilibrium fractionation equation. During these calculations, the determination of the isotope equilibrium temperature significantly affects the δ18OH2O value of the metallogenic fluid. Researchers in the past have chosen an average temperature of 200°C for this calculation, but this leads to an excessive aggregation of δ18OH2O values in the distribution, as shown in the plot (6‰–10‰). Apart from that, measurements of the temperature of the fluid inclusion are somewhat subjective and limited, and only statistical analysis of a large quantity of data can provide a reasonable approximation of reality. We collected all of the fluid inclusion temperature measurement data that are currently available for the Huize Pb–Zn deposits [48, 49] (Figure 12); based on analysis of these data and our measurements, the temperatures of the metallogenic fluid in Stages I, II, III, and IV are (190°C–205°C), (170°C–190°C), (145°C–170°C), and (130°C–150°C), respectively. Since calcites are products of Stages III and IV, 200°C is an overestimation of the average temperature. Studies have shown that the δ18OH2O value and average temperature are proportionally related [65, 66]; therefore, the projection of the actual δ18OH2O values (for calcites) should be biased towards atmospheric precipitation, such that the distribution range of its H–O isotopic compositions should be similar to or the same as that of Stage III sphalerite fluid inclusions.Figure 12
Distributions of homogenization temperatures and salinity in sphalerite and calcite (Zhang et al. [48]). Data sources: (a) Han et al. [49]; (b) Zhang et al. [48]; (c) Zhang [39]. There is no information from (c) in the salinity-frequency diagram because the data is incomplete; (a, c) Qilinchang deposit; (b) Kuangshanchang deposit.(3) Among the nine sphalerite samples, except for Z0807-10r, which appears to be an outlier, the eight remaining samples are aggregated according to their stage of metallogenesis, in three clumps of 3, 2, and 3, respectively. This indicates that the distribution of H and O isotopic compositions in the sphalerite fluid inclusions aggregate according to their stage of metallogenesis. Therefore, the results obtained here are representative of the native isotopic composition of metallogenic fluids during different stages of metallogenesis. The change in H isotopic compositions only varies slightly between Stages I, II, and III. In the figure, the range of distribution of samples from different stages contracts only slightly in the upwards direction. Changes in the isotopic composition of O are much more distinct, varying from (25.5‰–28.9‰) → (12.2‰–17.1‰) → (2.2‰–5.5‰) from Stage I to Stage III. This indicates that the metallogenic fluid evolved from a deeply sourced fluid in Stage I to a fluid with increasing levels of mixing from atmospheric precipitation in Stage III.(4) The calculatedδ18OH2O values of the six Qilinchang barites range within 9.85‰–12.36‰, with an average of 11.49‰. The δD values range within −91.3‰ to −79.8‰, with an average of −83.1‰. The δ18OH2O values of the four Kuangshanchang barites range within 12.39‰–13.69‰, with an average of 13.20‰; the δD values range within −75.1‰ to −61.7‰, with an average of −65.7‰. As a whole, the water in the inclusions within the Kuangshanchang barites is significantly more deuterium-enriched than the Qilinchang fluid inclusion water. The ranges of H–O isotopic compositions of stage I1 barites and stage I2 sphalerites are essentially the same in this figure.(5) The H–O isotopic composition of the fluid shows systematic changes from Stage I (barite, sphalerite) → Stage II (sphalerite) → Stage III (sphalerite, calcite) → Stage IV (calcite), as the metallogenic fluid gradually evolved from a deeply source fluid to a fluid that was mainly composed of atmospheric precipitation, which also reflects the gradual increase of basin brine mixing during metallogenesis (Figure11).


## 5.1. C–O Isotopes

It is well known that the measurement of C and O isotope compositions is an effective method for tracing the origins of CO2 within metallogenic fluids [50]. We obtained the C–O isotopic compositions of 83 samples through our measurements, as well as from the reorganization of relevant data from the literature (Table 1).Table 1
C–O isotopic compositions of sphalerite, calcite, and barite in Huize Pb–Zn deposit, SW China.
Numbers
Objects
Positions
δ
13
C
P
D
B
/
‰
δ
18
O
S
M
O
W
/
‰
Date source
HQO-99-1
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−1.94
17.09
a
HQO-109-4
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−3.27
17.79
1631-38
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.97
18.56
HQ-84
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.23
18.21
HQ-109-4
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.31
17.79
1571-2
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.30
18.21
Hui-2-3
Calcite
Tunnel 1751 m of 6# orebody in Qilinchang
−2.75
17.80
b
38-3
Calcite
Tunnel 1884 m of 6# orebody in Qilinchang
−2.80
17.10
Hui-6-10
Calcite
Tunnel 1648 m of 6# orebody in Qilinchang
−2.90
17.80
13-61
Calcite
Tunnel 1691 m of 6# orebody in Qilinchang
−2.70
18.10
Hui-1-1
Calcite
Tunnel 1836 m of 6# orebody in Qilinchang
−3.20
18.43
14-2-8
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.60
18.70
14-3-6
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.70
18.40
Hui-5-1
Calcite
Tunnel 1631 m of 6# orebody in Qilinchang
−2.40
18.10
Hui-4-23
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.10
17.50
23-4R
Calcite
Tunnel 1571 m of 6# orebody in Qilinchang
−3.00
17.60
Hui-8
Barite
Tunnel 1571 m of 6# orebody in Qilinchang
8.29
HQC-25
Baritization cataclasites
Tunnel 1631 m of 6# orebody in Qilinchang
0.30
20.40
a
HQC-98
Mineralization dolomitic granulitic rock
Tunnel 1631 m of 6# orebody in Qilinchang
−3.20
19.50
HQC-92
Mineralization dolomitic granulitic rock
Tunnel 1631 m of 6# orebody in Qilinchang
−1.60
17.80
41707
Altered dolomite
Tunnel 2233 m in Kuangshanchang
−0.80
20.50
c
Hui-1-2
Near ore dolomite
Tunnel 2233 m in Kuangshanchang
0.77
21.16
HE-16
Biogenic limestone
Tunnel 2233 m in Kuangshanchang
−0.44
22.45
d
HE-18
Biogenic limestone
Tunnel 2233 m in Kuangshanchang
−1.50
21.33
HE-17
Middle-fine grain dolomite
Tunnel 2233 m in Kuangshanchang
0.85
20.98
SC-33
Dolomitic limestone
Sunjiagou section of mining periphery
−0.90
21.00
a
SC-34
Coarse grain dolomite
Sunjiagou section of mining periphery
−2.20
20.50
SC-35
Coarse grain dolomite
Sunjiagou section of mining periphery
−1.20
21.40
HE11
Middle-fine grain dolomite
Zhujiayakou section of mining periphery
0.85
19.32
d
HE10
Dolomitic limestone
Zhujiayakou section of mining periphery
−3.35
19.42
HE12
Dolomitic limestone
Zhujiayakou section of mining periphery
−1.10
20.09
HE02
Middle-fine grain dolomite
Qingchaojie section of mining periphery
0.09
22.60
HE01
Biogenic limestone
Qingchaojie section of mining periphery
−1.15
22.59
HE03
Dolomitic limestone
Qingchaojie section of mining periphery
−0.53
23.14
HZ911-3
Porphyritic calcite
1# orebody
−2.20
17.50
e
HZ911-10
Lumpy calcite
1# orebody
−3.40
18.40
HZ911-15
Lumpy calcite
1# orebody
−3.50
18.60
HZQ25
Lumpy calcite
6# orebody
−2.50
17.50
HZQ40
Porphyritic calcite
6# orebody
−2.60
17.70
HZQ47
Lumpy calcite
6# orebody
−3.10
17.50
HZQ55
Vein calcite
6# orebody
−2.70
17.70
HZQ66
Lumpy calcite
6# orebody
−3.40
18.10
HZQ70
Porphyritic calcite
6# orebody
−3.30
18.10
HZQ77
Vein calcite
6# orebody
−2.80
17.80
HZQ85
Porphyritic calcite
6# orebody
−2.70
17.30
HZQ90
Porphyritic calcite
6# orebody
−2.70
17.20
HZQ96
Lumpy calcite
6# orebody
−2.10
17.50
HQ10-7
Lumpy calcite
10# orebody
−2.90
17.00
HQ10-12
Lumpy calcite
10# orebody
−3.20
18.50
HQ10-18
Lumpy calcite
10# orebody
−2.30
16.80
HQ10-25
Lumpy calcite
10# orebody
−3.00
17.90
HQ10-5
Lumpy calcite
10# orebody
−2.80
17.20
HQ8-115
Lumpy calcite
8# orebody
−2.20
17.00
HQ18-143
Lumpy calcite
8# orebody
−2.70
17.60
HQ8-98
Vein calcite
8# orebody
−3.00
17.80
HZQ35
Miarolitic calcite
Carbonate of Qixia–Maokou formation (500 m from orebody)
0.50
22.10
HZK33
Miarolitic calcite
Carbonate of Qixia–Maokou formation (500 m from orebody)
1.10
23.50
HZQ74
Whole rock of coarse grain dolomite
Host rock of Baizuo formation in number 10 ore body
−0.80
22.60
HZ2053-29
Whole rock of coarse grain dolomite
Host rock of Baizuo formation in number 1 ore body (1500 m from orebody)
0.40
23.20
HZS40
Whole rock of coarse grain dolomite
Baizuo formation in Sunjiagou section (1500 m from orebody)
0.70
22.80
HZX-3
Whole rock of coarse grain dolomite
Baizuo formation in Xiaoheiqing (1000 m from orebody)
−0.20
23.10
HZ911-4
Calcite filled in fractures
NE tectonic belt (150 m from orebody)
−3.00
16.70
HZQ28
Calcite filled in fractures
NE tectonic belt (150 m from orebody)
−3.40
16.30
Z0807-2r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−1.31
19.60
f
Z0807-3r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−2.52
17.25
Z0807-7r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.17
20.30
Z0807-8r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.75
21.90
Z0807-15r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.83
19.95
Z0807-18r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−4.11
15.80
Z0807-21r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.49
20.00
Z0807-22r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.89
20.80
Z0807-23r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.07
23.80
Z0807-24r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.13
20.50
Z0807-25r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.71
20.70
Z0807-26r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.64
21.50
Z0807-27r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.53
20.40
Z0807-28r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
0.54
21.40
Z0807-29r
Dolostone
15# stope of tunnel 1752 m in Kuangshanchang
−0.66
22.30
Z0807-14r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.36
16.90
Z0807-19r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−0.91
18.65
Z0807-25r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.77
21.30
Z0807-26r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−3.70
20.20
Z0807-27r
Calcite
15# stope of tunnel 1752 m in Kuangshanchang
−1.59
20.70Figure10 shows that the C–O isotopic compositions of the Huize Pb–Zn deposit have the following characteristics:Figure 10
(a) C–O isotope composition diagram of Huize Pb–Zn deposit. (b) C–O isotope composition diagram of different orebody and wall rocks in Huize Pb–Zn deposit. Data sources: (A) previous data [6, 10, 16, 18, 21]; (B) this paper.(1) The C–O isotopic compositions of the Huize Pb–Zn deposit are relatively homogeneous. Theδ13CPDB-δ18OSMOW maps (Figure 10(a)) show that the isotopic compositions cluster within a narrow range between magmatic carbonates and marine carbonates, with the compositions edging closer to those of marine carbonates. The isotopic compositions, as a whole, display the following order of isotopic values: δ13Ccalcite < δ13Caltereddolomite < δ13Cdolomite < δ13Climestone and δ18Ocalcite < δ18Oaltereddolomite < δ18Odolomite < δ18Olimestone. The δ18O values of the Mid-to-Late Devonian marine limestones are mainly distributed around 20‰±, with δ13C = 0±. The average δ18O and δ13C values of limestones found in the Huize mining area are equivalent to these values, which decrease as dolomitization increases. However, the δ18O and δ13C isotopic compositions of calcite are noticeably different from those of the Mid-to-Late Devonian marine limestones, as the calcite δ18O and δ13C values of the orebodies and tectonic belts are clearly lower than those in the adjacent carbonate rocks.(2) Similar C–O isotopic compositions were observed for gangue calcites in different orebodies and calcites with different occurrences, withδ13CPDB values that vary within −1.9‰ to −3.5‰ and δ18OSMOW values varying within 16.8‰–18.7‰. This indicates that the metallogenic fluid has a δ13C value that is much lower than that of the host rocks.(3) The altered dolomites and bioclastic limestones of Kuangshanchang, carbonates from strata in the periphery of the mining area, and miarolitic calcites have similar C–O isotopic compositions, with most of these compositions projecting within the region of marine carbonates. This indicates that the source of carbon in these rocks is innate to the carbonate strata in this region, as their C–O isotopic compositions indicate that the carbon was produced via leaching of adjacent rocks by fluids, which is significantly different from calcites found in ores of the Huize deposit.(4) The C–O isotopic compositions of calcites from the NE-trending tectonic belt are similar to those of gangue calcites, which is distinctly different from the C–O isotopic compositions of the previously described rock strata. This is because the main channel through which the metallogenic fluids of the Huize Pb–Zn deposit pass is the NE-trending tectonic belt [15, 21, 33, 51]. Therefore, the C–O isotopic compositions of the calcites in this tectonic belt plot closest to those of the metallogenic fluid.(5) In the source region of the metallogenic fluid or organic matter-rich strata below the orebodies penetrated by the fluid, water-rock reactions will solvate adjacent carbonates and cause an exchange of C–O isotopes between the fluid and the strata. This ultimately causesδ13C of the fluid to increase and δ13C of the adjacent rocks to decrease.


## 5.2. H–O Isotopes

As H2O is an important component of metallogenic fluids, it is important to elucidate the source of H2O in order to investigate the origin of the metallogenic fluid. The H and O isotopic compositions of gangue minerals, ore minerals, and their related alteration minerals are the most direct and effective indicators of the source of H2O in metallogenic fluids. The δD value measured in calcite fluid inclusions reflects the H–O isotopic composition of metallogenic hydrothermal solutions more accurately than δD measurements in quartz [51, 52]. Therefore, previous researchers have generally chosen to use calcites to determine the H–O isotopic composition of the metallogenic fluid; these results are shown in Table 2.Table 2
H–O isotopic compositions of sphalerite, calcite, and barite in Huize Pb–Zn deposit, SW China.
Numbers
Positions
Objects
δ
18
O
H
2
O
‰
δ
D
‰
Date source
HZ911-10
1# orebody
Lumpy calcite
8.6
−59.8
a
HZ911-15
1# orebody
Lumpy calcite
8.8
−52.4
HZQ25
6# orebody
Lumpy calcite
7.7
−50.2
HZQ40
6# orebody
Porphyritic calcite
7.9
−55.6
HZQ47
6# orebody
Lumpy calcite
7.7
−57.9
HZQ55
6# orebody
Vein calcite
7.9
−54.1
HZQ66
6# orebody
Lumpy calcite
8.3
−53.9
HZQ77
6# orebody
Vein calcite
8.0
−58.0
HZQ85
6# orebody
Porphyritic calcite
7.5
−52.7
HQ10-12
10# orebody
Lumpy calcite
8.7
−53.2
HQ10-18
10# orebody
Lumpy calcite
7.0
−57.3
HQ10-25
10# orebody
Porphyritic calcite
8.1
−53.0
HQ10-5
10# orebody
Vein calcite
7.4
−52.8
HQ8-115
8# orebody
Lumpy calcite
7.2
−55.2
HQ8-143
8# orebody
Lumpy calcite
7.8
−54.1
HQ8-98
8# orebody
Vein calcite
8.0
−54.3
HQO-99-1
Qilinchang
Calcite
7.8
−43.5
b
HQO-109-4
Qilinchang
Calcite
10.1
−54.8
1631-38
Qilinchang
Calcite
7.8
−48.0
HQ-84
Qilinchang
Calcite
9.7
−51.5
HQ-109-4
Qilinchang
Calcite
7.6
−43.5
1751-2
Qilinchang
Calcite
7.7
−55.4
HW-2-3
Qilinchang
Calcite
7.1
−55.8
c
38-3
Qilinchang
Calcite
6.4
−64.0
Hui-6-10
Qilinchang
Calcite
7.1
−75.0
13-61
Qilinchang
Calcite
8.0
−57.0
14-2-8
Qilinchang
Calcite
−2.1
−66.0
Hui-8
Kuangshanchang
Barite
7.8
−86.0
Z0807-1r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
28.0
−52.0
d
Z0807-4r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
5.5
−50.0
Z0807-5r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
2.2
−55.0
Z0807-6r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
25.5
−50.0
Z0807-10r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
17.1
−27.0
Z0807-11r
15# stope of tunnel 1752 m in Kuangshanchang
3rd stage sphalerite
4.0
−43.0
Z0807-12r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
13.2
−49.0
Z0807-13r
15# stope of tunnel 1752 m in Kuangshanchang
2nd stage sphalerite
12.2
−57.0
Z0807-17r
15# stope of tunnel 1752 m in Kuangshanchang
1st stage sphalerite
28.9
−51.0
JS-11-1
Qilinchang
Barite
−91.3
11.6
e
JS-11-2
Qilinchang
Barite
−85.5
9.9
JS-11-3
Qilinchang
Barite
−87.8
11.8
JS-12-1
Qilinchang
Barite
−77.4
11.8
JS-12-3
Qilinchang
Barite
−80.5
11.7
JS-13-1
Qilinchang
Barite
−79.8
12.4
JS-40-3
Kuangshangchang
Barite
−73.7
12.4
JS-40-5
Kuangshangchang
Barite
−63.9
13.7
JS-41-1
Kuangshangchang
Barite
−75.1
13.4
JS-42-2
Kuangshangchang
Barite
−61.7
13.4
a, b, c, d, and e: data from Li et al. [10], Han et al. [16], Liu and Lin [21], this paper, and Wang [47]. Different stages of sphalerite from the same ores can be separated based on textural and structural observations (Figures 3, 4, 6, and 8).In the Huize deposit, the characteristics of sphalerites from different stages of metallogenesis are very distinct. Isotope exchange reactions do not happen between fluid inclusions and minerals in later stages, and fluid inclusion petrography has shown that inclusions in sphalerite are mainly comprised of primary and pseudosecondary inclusions, with few secondary inclusions [48, 49]. As the adsorbed water and the associated secondary inclusions have been removed from the sphalerite samples during the measurement process, the direct measurement of the H and O isotopic composition of sphalerite inclusions from different stages of metallogenesis is representative of the native isotopic composition of the metallogenic fluids, and these data also allow us to track the evolution of metallogenic fluids during different stages of metallogenesis.Figure11 shows the following.Figure 11
Plot ofδD versus δ18OH2O values from Huize Pb–Zn deposit. Data sources: (a) previous data [10, 16, 21]; (b) this paper; (c) Wang [47].(1) Similar to the C and O isotopic composition characteristics, the H–O isotopic compositions of the Huize Pb–Zn deposit are also relatively stable, withδD ranging within −43.5‰ to −66‰, with an average of −56.3‰, and δ18OH2O values ranging within −2.05‰–10.08‰, with an average of 7.55‰.(2) The H–O isotopic compositions of calcites from different orebodies, with different occurrences, do not differ significantly from one another. This characteristic reflects the presence of two different fluids within the metallogenic system, that is, a deeply sourced fluid, and a fluid sourced from atmospheric precipitation. Based on the geological conditions for metallogenesis and comparison between the H–O isotopic compositions of the metallogenic fluid and those of orogenic mineral deposits [53–64], we deduced that the metallogenic fluid is a mix between deeply sourced fluids and basin brines.However, it is worth noting that theδ18OH2O value was calculated from the isotope equilibrium fractionation equation. During these calculations, the determination of the isotope equilibrium temperature significantly affects the δ18OH2O value of the metallogenic fluid. Researchers in the past have chosen an average temperature of 200°C for this calculation, but this leads to an excessive aggregation of δ18OH2O values in the distribution, as shown in the plot (6‰–10‰). Apart from that, measurements of the temperature of the fluid inclusion are somewhat subjective and limited, and only statistical analysis of a large quantity of data can provide a reasonable approximation of reality. We collected all of the fluid inclusion temperature measurement data that are currently available for the Huize Pb–Zn deposits [48, 49] (Figure 12); based on analysis of these data and our measurements, the temperatures of the metallogenic fluid in Stages I, II, III, and IV are (190°C–205°C), (170°C–190°C), (145°C–170°C), and (130°C–150°C), respectively. Since calcites are products of Stages III and IV, 200°C is an overestimation of the average temperature. Studies have shown that the δ18OH2O value and average temperature are proportionally related [65, 66]; therefore, the projection of the actual δ18OH2O values (for calcites) should be biased towards atmospheric precipitation, such that the distribution range of its H–O isotopic compositions should be similar to or the same as that of Stage III sphalerite fluid inclusions.Figure 12
Distributions of homogenization temperatures and salinity in sphalerite and calcite (Zhang et al. [48]). Data sources: (a) Han et al. [49]; (b) Zhang et al. [48]; (c) Zhang [39]. There is no information from (c) in the salinity-frequency diagram because the data is incomplete; (a, c) Qilinchang deposit; (b) Kuangshanchang deposit.(3) Among the nine sphalerite samples, except for Z0807-10r, which appears to be an outlier, the eight remaining samples are aggregated according to their stage of metallogenesis, in three clumps of 3, 2, and 3, respectively. This indicates that the distribution of H and O isotopic compositions in the sphalerite fluid inclusions aggregate according to their stage of metallogenesis. Therefore, the results obtained here are representative of the native isotopic composition of metallogenic fluids during different stages of metallogenesis. The change in H isotopic compositions only varies slightly between Stages I, II, and III. In the figure, the range of distribution of samples from different stages contracts only slightly in the upwards direction. Changes in the isotopic composition of O are much more distinct, varying from (25.5‰–28.9‰) → (12.2‰–17.1‰) → (2.2‰–5.5‰) from Stage I to Stage III. This indicates that the metallogenic fluid evolved from a deeply sourced fluid in Stage I to a fluid with increasing levels of mixing from atmospheric precipitation in Stage III.(4) The calculatedδ18OH2O values of the six Qilinchang barites range within 9.85‰–12.36‰, with an average of 11.49‰. The δD values range within −91.3‰ to −79.8‰, with an average of −83.1‰. The δ18OH2O values of the four Kuangshanchang barites range within 12.39‰–13.69‰, with an average of 13.20‰; the δD values range within −75.1‰ to −61.7‰, with an average of −65.7‰. As a whole, the water in the inclusions within the Kuangshanchang barites is significantly more deuterium-enriched than the Qilinchang fluid inclusion water. The ranges of H–O isotopic compositions of stage I1 barites and stage I2 sphalerites are essentially the same in this figure.(5) The H–O isotopic composition of the fluid shows systematic changes from Stage I (barite, sphalerite) → Stage II (sphalerite) → Stage III (sphalerite, calcite) → Stage IV (calcite), as the metallogenic fluid gradually evolved from a deeply source fluid to a fluid that was mainly composed of atmospheric precipitation, which also reflects the gradual increase of basin brine mixing during metallogenesis (Figure11).


## 6. Identification of the Two Fluid Types

We have previously studied the fluid inclusions of this deposit in detail [48, 49] and found that the homogenization temperature and salinity of sphalerite fluid inclusions in Kuangshanchang are the same as those of the Qilinchang deposit, which is consistent with the findings of Liu and Lin [21]; that is, the homogenization temperatures were distributed within 150°C–320°C, and the decrepitation temperatures of the metallic minerals (pyrite, sphalerite, and galena) ranged within 140°C–480°C.The homogenization temperatures of sphalerite fluid inclusions in the Huize Kuangshanchang deposit covered a wide range, from 126°C to 280°C (Figures12 and 13(b)), with a correspondingly high level of salinity, which ranged within 3.2%–22.7%; the dolomite fluid inclusions had homogenization temperatures that ranged within 86°C–163°C, with comparatively low levels of salinity, which ranged from 1.1% to 14.8%.Figure 13
Identification diagram for the two fluid types in the Huize Pb–Zn deposit. (a) H–O isotope composition diagram. (b) Homogenization temperature-salinity diagram. (c) C–O isotope composition diagram.
(a)
(b)
(c)The dolomite and sphalerite that correspond to each of the three stages of metallogenesis have fluid inclusions that display highly distinct distribution characteristics in their salinities and homogenization temperatures. From the first stage of metallogenesis (hydrothermal metallogenesis) to the alteration of adjacent rocks, the fluids evolved according to the following pattern: moderate-to-high temperatures and moderate-to-high salinity → moderate temperatures and moderate-to-high salinity → moderate-to-low temperatures and moderate-to-high salinity → moderate-to-low temperatures and low salinity. Patterns related to the mixing of moderate-to-high temperature-moderate-to-high salinity fluids with moderate temperature-moderate-to-high salinity fluids were also observed in the first stage of metallogenesis. The mixing of fluids with different levels of salinity under isothermal (moderate-to-low temperatures) conditions was observed for the Sp–Gn and Gn–Sp stages of metallogenesis (i.e., the primary stages of metallogenesis), while mixing between fluids with moderate-to-high levels of salinity with fluids of low salinity under moderate-to-low temperatures was observed in the alteration of adjacent rocks.It is thus shown that a minimum of two fluids with different levels of salinity participated in hydrothermal metallogenesis. Hence, the mixing of fluids was likely the primary mechanism of mineral precipitation in the Huize deposit. This is consistent with the immiscibility represented by the coexistence of purely gaseous and gas-liquid inclusions, which were observed in fluid inclusion studies [48, 49, 67].The C–O and H–O isotopic compositions and the homogenization temperature-salinity distribution map obtained from the results of previous fluid inclusion studies (Figure13) are both indicative of fluid mixing during metallogenesis. In particular, the H–O isotopic composition of stage I1 barites and the C–O isotopic compositions of calcites from the NE-trending tectonic belt show that the metallogenic Fluid A of the Huize Pb–Zn deposit originates from deep-seated sources and is rich in lighter C and O isotopes. The C–O isotopic compositions of wall rocks in the periphery of the mining area and the H–O isotopic compositions of early-stage sphalerites indicate that Fluid B comprises subsurface brines formed by atmospheric precipitation that leached adjacent carbonate rocks and extracted reduced sulfurs from various strata. This fluid has heavier C–O and H–O isotopic compositions than Fluid A. When fluids A and B were mixed, their isotopes were exchanged, which led to the final mixed fluid having C–O and H–O compositions that are in between those of the two metallogenic fluids.Based on the geological characteristics of the deposit and the findings of fluid inclusion studies, the high-temperature barites that occur within the fracture zone and side fractures were precipitated from Fluid A because of high oxygen fugacity and oversaturation; hence, the geological body that corresponds to Fluid A is high-temperature barite. In contrast, Fluid B is composed of stratigraphic brine formed by atmospheric precipitation that leached adjacent carbonates and extracted reduced sulfides from the strata, and its corresponding geological bodies are carbonate strata, as well as pyrite and gypsum strata formed during sedimentation and diagenesis. The mixing of fluids A and B caused the precipitation of sulfides; hence, the geological bodies that correspond to the mixed fluid are zinc and lead sulfide ores. Information on the two types of fluids and the mixed fluid is shown in Table3.Table 3
Characteristics of the two fluid types in the Huize Pb–Zn deposit, SW China.
Fluid A
Fluid B
Mixed fluid
Source
Deep
Brine water from atmospheric Precipitation leaching the host rock
Mixed A and B
Salinity
<10 wt% NaCl
>20 wt% NaCl
2–23 wt% NaCl
pH
<3.6
>6
5–8
CO2
Abundant
Abundant
First increased, then decreased
S
O
4
2
-
70 ppm
No
No
HS−
No
Sulfate strata reduction
Precipitated as sulfides
Pb, Zn complex
Cl-complex
Little or none
Sulfide precipitation
δ
13C‰
-
3
‰
<
δ
13
C
‰
<
-
4
‰
-
2
‰
<
δ
13
C
‰
<
1
‰
-
4
‰
<
δ
13
C
‰
<
1
‰
δD‰
-
92
‰
<
δ
D
‰
<
-
50
‰
-
66
‰
<
δ
D
‰
<
-
43
‰
-
75
‰
<
δ
D
‰
<
-
43
‰
δ
18O‰
10
‰
<
δ
18
O
‰
<
17
‰
2
‰
<
δ
18
O
‰
<
24
‰
7
‰
<
δ
18
O
‰
<
22
‰
Property
Acid oxidation
Neutral-alkaline and reducing
Near neutral
Corresponding major minerals
Barite and sphalerite in I stage
Calcite in IV stage
Galena, sphalerite in II and III stagesBased on the above characteristics, we hypothesize that the metallogenesis of the Huize Pb–Zn deposit occurred according to the following process: tectonic activity during the Indosinian caused large-scale upward movement of deep-seated fluids; as these fluids flowed through the carbonate strata, they exchanged C and H isotopes with these strata and extracted the metallic elements, thus forming the metal-rich, acidic, moderate-to-high temperature and low salinity Fluid A, whose lead and zinc contents mainly exist as Pb–Zn–Cl compounds. Furthermore, as the carbonate strata provided sufficientCO32- and HCO3- to buffer the pH of the metallogenic fluid, Pb–Zn–Cl compounds were stably maintained within the fluid (because of its acidity), which prevented the precipitation of lead and zinc sulfides from the fluid [48]. As the metallogenic fluid moved towards ore-containing strata along large ore-inducing tectonic structures, decompression boiling occurred when the fluids penetrated the NE-trending interstratum reverse shear fracture [48, 49], causing the metallogenic substances to become even more concentrated and enriched, which led to the partial precipitation of sphalerites and galena. Sulfides precipitated in this manner have a high temperature, ~300°C. This fluid then mixed with Fluid B, causing its temperature to decrease and its pH to increase, resulting in the precipitation of large quantities of sulfides. The sulfides precipitated in this stage have a lower temperature, between 170°C and 230°C, and overlap with the sulfides formed during the boiling of the fluid, thus forming the primary orebodies.


## 7. Conclusion

Based on C–O and H–O isotopic compositions and the findings of fluid inclusion studies, it was found that there are two metallogenic fluids present in the Huize Pb–Zn deposit: Fluid A and Fluid B. Fluid A originates from deep-seated fluid sources and is enriched in lighter C and O isotopes, whereas Fluid B is composed of subsurface brine formed by atmospheric precipitation that leached carbonate wall rocks and extracted thermochemically reduced sulfurs from stratigraphic pyrites and carbonates (gypsum). Fluid B is characterized by heavier C–O and H–O isotopic compositions than Fluid A. These fluids mixed during metallogenesis, which resulted in the exchange of isotopes between the two fluids. Consequently, the final mixed fluid has C–O and H–O isotopic compositions that lie between those of the two metallogenic fluids.Therefore, the metallogenesis of the Huize Pb–Zn deposit can be summarized as follows. During tectonic activity in the Indosinian Period, deep-seated fluids moved upwards on a large scale through carbonate strata of various ages. The fluids extracted the metallic elements of these strata to form a metal-rich metallogenic fluid, which underwent gas-liquid separation under the process of decompression boiling in structurally favorable spaces. After further enrichment and concentration and precipitation of some of the higher-grade ores, this fluid then mixed with Fluid B and continued to precipitate sulfides within the Huize Pb–Zn deposit.



---

*Source: 6345810-2017-08-27.xml*