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Review

Geology and Geochemistry of Selected Gold Deposits in the Ailaoshan Metallogenic Belt, China: Origin of Ore-Forming Fluids

by
Yang Li
1,
Denghong Wang
2,
Chenghui Wang
2,*,
Yan Sun
2 and
MIMA Pu-chi
3
1
College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
2
Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
3
Bureau of Geology and Mineral Exploration and Development of Tibet Autonomous Region, Regional Geological Survey Brigade, Lhasa 851400, China
*
Author to whom correspondence should be addressed.
Minerals 2021, 11(11), 1276; https://doi.org/10.3390/min11111276
Submission received: 2 September 2021 / Revised: 9 November 2021 / Accepted: 12 November 2021 / Published: 18 November 2021
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

:
The formation of the Ailaoshan metallogenic belt was the result of: the Neoproterozoic super mantle plume, the Indosinian and South China blocks in the Late Triassic after the Paleo-Tethys Ocean closure, and Oligocene-Eocene continental-scale shearing related to the India-Eurasia collision. It is one of the most important Cenozoic gold ore province in the world. In this paper, the geological characteristics, isotopic geochemistry, and geochemical data of ore-forming fluids of four large-scale gold deposits in the Ailaoshan metallogenic belt (Mojiang Jinchang, Zhenyuan Laowangzhai, Yuanyang Daping, and Jinping Chang’an) are comprehensively compared. The features of host-rock alteration, metallogenetic periods and stages, geochronology, fluid inclusion, and C-H-O-S-Pb isotopes of gold deposits are summarized and analyzed. The gold mineralization in the Ailaoshan metallogenic belt occurred mostly in 50–30 Ma, belonging to the Himalayan period. The gold mineralization is closely related to silicification, argillation, carbonation, and pyritization due to the strong mineralization of hydrothermal fluid, the development of alteration products, and the inconspicuous spatial zonation of alteration types. The ore-forming fluid is mainly composed of mantle fluid (magmatic water) and metamorphic fluid (metamorphic water). The ore-forming materials of the Jinchang, Chang’an, and Laowangzhai gold deposits mainly originate the host-rock strata of the mining area, and the carbon is more likely to from marine carbonate. The carbon in the Daping gold deposit from the original magma formed by the partial melting of the mantle. Pb isotopes have characteristics of crustal origin, accompanied by mixing of mantle-derived materials and multisource sulfur mixing, and are strongly homogenized.

1. Introduction

The Ailaoshan metallogenic belt is a boundary tectonic-magmatic-metallogenic belt between the western margin of the Yangtze and Indosinian blocks. It encompasses the Ailaoshan-Red River shear zone (ASRRSZ) in the north east and the Ailaoshan suture zone in the north west (Wang et al., 2013; Liu et al., 2011) [1,2]. The Ailaoshan metallogenic belt is located in the southern section of the ASRRSZ (also known as the Ailaoshan fault zone), where the Yangtze plate meets the Indian plate. The Ailaoshan metallogenic belt has an overall broom-like geometric structure that converges to the northwest and expands to the southeast (Figure 1a, Metcalfe, 2013) [3]. It is divided into the eastern high-grade metamorphic belt typified by ductile shearing and the western low-grade metamorphic belt, which is further subdivided into the Jinping terrane in the South China block and a Paleo-Tethyan ophiolite belt in the Indochina block (Figure 1b). The Ailaoshan fault separates the eastern high-grade metamorphic belt from the Jinping terrane. The Ailaoshan-Tengtiaohe fault separates the western low-grade metamorphic belt from the ophiolitic belt (Wang et al., 2020) [4,5].
The Ailaoshan metallogenic belt evolved during the last continental collision. Prior to this, multiple plate gatherings considerably affected this metallogenic belt (Schärer et al., 1990; Leloup et al., 1995; Hou and Cook., 2009; Hou et al., 2015) [6,7,8,9]. The formation of the Ailaoshan metallogenic belt was the result of: super mantle plume activity in the Neoproterozoic (Li et al., 1999; Li et al., 2008; Li Xianhua et al., 2002; Zou et al., 2020) [10,11,12,13], the closure of the Paleo-Tethys Ocean in the Late Paleozoic (Liu et al., 2014, 2015; Yang et al., 2018) [14,15,16], Cenozoic India-Eurasia continental collision (Deng et al., 2014, 2017, Hou et al., 2015; Hou and Cook 2009) [8,9,17,18,19], and other multiple orogeny periods. Subsequently, a series of gold deposits formed in the complex crust above the abnormal mantle lithosphere (Figure 1b, Wang et al., 2020) [5]. From the NW to the SE, there are Mojiang Jinchang, Zhenyuan Laowangzhai, Zhenyuan Donggualin, Yuanyang Daping, Yuanyang Malutang, Jinping Tongchang, Jinping Chang’an, Xiangyun Jinchangqing, Heqing Beiya, Nanhua Yao’an, and other large- and medium-sized gold deposits as well as numerous small deposits (ore spots) (Li, 2014) [20]. Among the four major large-scale deposits (Zhenyuan Laowangzhai, Mojiang Jinchang, Jinping Chang’an, and Yuanyang Daping) (Sun et al., 2009) [21], except for the Yuanyang Daping gold deposit in a Hercynian diorite rock body (Zhao, 2014; Yang et al., 2011) [22,23], the rest are located in the Ailaoshan shallow metamorphic rock series (Deng et al., 2010a, b) [24,25]. The orebody of the gold deposit was controlled by the secondary fault structure of the regional NW-trending fault and formed in the process of Tethys composite orogeny.
Many studies have been conducted in the area, obtaining important results (Goldfarb et al., 2001; Faure et al., 2016) [27,28]. Based on previous studies, this study selected four major large-scale gold deposits (Sun et al., 2009) [21] in the Ailaoshan metallogenic belt for conducting systematic research. The data were collected from previous works and reinterpreted. We applied C-H-O-S-Pb isotopic systems for determining diagenesis, the mineralization stages, and the study of the source and evolution of ore-forming fluids in the Ailaoshan ore belt. We focused on the metallogenic characteristics of the metallogenic belt, explored the geochemical characteristics of gold mineralization under the background of the Ailaoshan compound orogen, explored the genetic mechanism and metallogenic laws of the deposit, established the corresponding metallogenic model, and provided a reliable theoretical basis for guiding the investigation.

2. Data Sources

This paper is based on a review of previous studies. The temperature measurement data of fluid inclusions are mostly derived from quartz, with a small amount of calcite. According to the microscopic temperature measurement data, for CO2-H2O three-phase inclusions, use the formula for calculating the salinity of this type of inclusion:
S = 15.52022 − 1.02342t − 0.05286t2            (−9.6 °C ≤ t ≤ 10 °C).
In the formula, S is the salinity (wt% NaCl. eqv.) and t is the dissolution temperature of CO2 hydrate (°C) (Bozzo et al., 1973) [29].
For aqueous inclusions, use the salinity calculation formula:
S = 0.00 + 1.78t − 0.0442t2 + 0.000557t3     (0–23.3% NaCl solutions).
In the formula, S is the salinity (wt% NaCl. eqv.) and t is the temperature at which the freezing point drops (°C) (Lu et al., 2004) [30].
S isotope data mostly come from pyrite and stibnite, with a small amount of chalcopyrite, galena, barite, sulfur copper antimony, iron dolomite, and arsenopyrite. C-H-O isotope data mostly come from quartz and calcite, with a small amount of scheelite, dolomite, iron dolomite, and siderite. Pb isotope data mostly come from galena. The above isotope data are from single minerals in ore and host rocks. Section 4 (Metallogenic geodynamic background) show the dating minerals and methods.

3. Geological Characteristics of Ailaoshan Gold Deposits

3.1. The Jinchang Deposit in Mojiang

The Jinchang deposit, with a resource of more than 80 t at 2.69 g/t gold, has a unique gold-nickel paragenetic assemblage (Fang et al., 2001) [31]. The host rocks mainly comprise the Early-Middle Devonian metasandstone interbedded with slate, defining an overturned fold and widely exposed Late Triassic red siltstone, siliceous metasedimentary rocks, and a large amount of brecciated Devonian ophiolites (Figure 2a,b). The ophiolites represent partially serpentinized augite peridotite and dunite (Xiong et al., 2015) [32]. Northwest-striking granitoid intrudes the Devonian-Triassic metasedimentary rocks and ophiolites (Figure 2a). In the geotectonic position, the Jinchang deposit is located near the contact zone between the Sanjiang orogenic belt and the Yangtze block and it is located in the contact zone between the Upper Devonian shallow metamorphic rock series on the east side of the Jiujia-Mojiang fault and the Jinchang ultrabasic rock pluton in the Ailaoshan ophiolitic mélange belt (Xiong et al., 2015) [32]. The mine is divided into five ore blocks in the following order: the Sishibaliangshan, Laojiniu, Lanshan, Pingpo, and Maobiliangz ore blocks (Figure 2; Xiong et al., 2015) [32].

3.2. The Zhenyuan Deposit

From NW to SE, the Zhenyuan deposit, comprising the Langnitang, Laowangzhai, Donggualin, Daqiaoqing, and Kudumu ore-shoot clusters (Figure 3a,b, BGMRYP (Bureau of Geology and Mineral Resources of Yunnan Province), (1993a, b) [34,35], is the largest gold deposit in the belt, with a resource of more than 160 t at 5.29 g/t gold (Yang et al., 2010) [36]. The deposit is in the northern part of the ophiolite belt, characterized by complex host rocks, including Late Devonian metaquartz sandstone, Devonian-Carboniferous ophiolitic rocks, Carboniferous carbonaceous slate, Permo-Triassic quartz porphyry, Late Triassic siltstone, and Eocene lamprophyre (Deng et al., 2015a; Huang et al., 2002) [37,38]. Structural controls are dominated by combinations of faults, folds, and shear joints, with steep NW-striking faults in the Donggualin cluster and nearly EW-NE-striking faults in the Laowangzhai ore cluster (Deng et al., 2015a) [37].

3.3. The Daping Deposit in Yuanyang

The Yuanyang Daping gold deposit, with a resource of more than 60 t at 14.3 g/t gold (Yang et al., 2010) [36]. So far, 40 tons of gold have been mined. Many types of rocks are exposed in the area, among which the main host rocks are Neoproterozoic granite diorite and Silurian dolomite. Considering the Xiaoxinjie fault as the boundary, the Baishapo ore block is on the west side, the Maomushu ore block is on the north side, the Mashami ore block is in the middle section, and the Bajiaoling ore block is on the south side (Figure 4). Based on the spatial distribution of the veins and the relationship with the Xiaoxinjie fault, it can be inferred that the Xiaoxinjie fault is the main ore-conducting structure in the mining area (Yang, 2018) [39].

3.4. The Chang’an Deposit in Jinping

The Chang’an gold deposit, with more than 110 t at 5.84 g/t gold, is in the western part of the Jinping terrane (Figure 5; Yang et al., 2010) [36]. Rocks in this deposit mostly include Early Ordovician metamorphosed fine-grained quartz sandstone and quartz conglomerate, Middle-Late Silurian dolomite, and Quaternary gravel (Zhang et al., 2014) [41]. The Ordovician sandstone and conglomerate, the main host rocks, are approximately E-W-trending and N-dipping (Zhang et al., 2014; Wang et al., 2020) [4,41].

3.5. Host-Rock Alteration and Mineralization Stages

3.5.1. Characteristics of Host-Rock Alteration

The tectonic-magmatic activity in the Ailaoshan metallogenic belt is intense, forming a series of ultrabasic, basic, and intermediate-acid magmatic rocks. Most of the rock pluton is produced in the form of small rock plutons and dykes and distributed intermittently along the deep fault zone of the Ailaoshan. The Ailaoshan deep fault structural zone is mainly composed of magmatic rocks, and the fillings in the secondary fault zones are cataclastic rocks, mylonites, and hydrothermal veins. The hydrothermal veins are mostly quartz and calcite veins. The hydrothermal process is strong, and the alteration products are developed, mainly including silicification, sericitization (chromium hydromicaization), argillation, pyrite sericitization, pyritization, carbonation, iron dolomitization, and green mud petrification and serpentinization. The spatial zoning of alteration types is not obvious, and gold mineralization is closely related to silicification, clayization, carbonatization, and pyritization (Table 1, Zhao, 2014) [22].

3.5.2. Mineralization Periods and Stages Division

The mineralization of the four main gold deposits in the Ailaoshan metallogenic belt exhibits both common features and obvious differences. These features and differences relate to the complex geological processes developed in different periods of the metallogenic belt and the different metallogenic environments among the deposits. It is also controversial whether the four deposits exhibit multistage mineralization.
Based on previous viewpoints and hand specimen and microscopic identification, the main metallogenic periods in the metallogenic belt are divided into premetallogenic sedimentary diagenesis, metamorphic, hydrothermal metallogenic, and postmetallogenic supergene periods. The Jinping Chang’an gold deposit is divided into sedimentary diagenesis, tectonic-magma-hydrothermal mineralization, and supergene secondary enrichment periods (Figure 6 and Figure 7; Li, 2012; Zhang et al., 2014) [37,41]. Moreover, from detailed field observations, hand specimens, and microscopic observations, the mineral associations of various deposits were determined. The hydrothermal mineralization stage was divided according to the cutting relationship between the mineralized veins and the structural characteristics of the ore.

4. Metallogenic Geodynamic Background

Yang et al. (2010) and Zhao (2014) [22,36] collected metallogenic age data of four gold deposits in the Ailaoshan metallogenic belt, and this study makes a detailed supplement on this basis (Table 2 and Figure 8). Based on the characteristics of age data, the metallogenic ages of the four main gold deposits in the metallogenic belt are concentrated in the Himalayan period, corresponding to the India-Eurasia continental collision period. It might have experienced early (65–60 Ma), major (40–30 Ma), and late (30–25 Ma) mineralization-thermal events. Wang et al. (2005) [51] proposed that the three episodes of gold mineralization are associated with three events of tectonic-magmatism and/or fluid events. Even though the gold deposits were formed at different episodes, all of the deposits are genetically related to the tectonic movements in large-scale shear zones. The tectonic events (including large-scale strike-slip) among the Paleogene considerably affected gold mineralization, with new deposits formed and old deposits enriched or superimposed to be a higher grade by a new mineralization stage. The data indicate that gold deposits were concentrated in some areas and were mostly formed at different period boundaries, indicating that some peak stages of gold mineralization (metallogenic episodes) existed and gold deposits were mostly formed by episodic mineralization [51,52]. However, since these mineralization ages are obtained by applying different dating methods to minerals that are not directly related to gold mineralization, the reliability of the data must be verified (Yang et al., 2011) [23].
Beginning at 65 Ma, the India-Eurasia continental collision occurred under the subduction of the Neo-Tethys oceanic crust and the entire Tethys tectonic framework was strongly modified, making Ailaoshan a lateral material adjustment zone for continental collision. The Ailaoshan metallogenic belt has become a structural transformation domain, absorbing and adjusting the strain generated in the collision process (Deng et al., 2011) [72]. Due to the rapid increase in the plate convergence rate, the rocks in the Ailaoshan area have been thrust and faulted due to powerful compression, forming a large-scale thrust-nappe tectonic system. The simultaneous formation of shear strike-slip fault structures (Yang et al., 2011) [23] has significantly shortened and thickened the crust and lithosphere in western Yunnan (Chen et al., 2008) [73]. Simultaneously, along with the deep melting of landing crust, crust-mantle action, and mantle-derived magmatic activity, the tectonic framework and material basis of the Ailaoshan metallogenic belt are laid. The gold mineralization age data show that some gold mineralization occurred during the 65–50 Ma period (Figure 9, Yang et al., 2011) [23].
The main periods of gold mineralization in the Ailaoshan area occurred during 50–30 Ma. During this period, the compression stress concentration between the blocks exceeded the limit. Due to the limitation of boundary conditions, some materials and blocks were extruded to the southeast, resulting in the large-scale strike-slip shear zone of Ailaoshan. At approximately 40 Ma, the relative compression rate between India and the Yangtze block decreased significantly. Simultaneously, the direction of mutual movements between them gradually changed, which manifested as a clockwise rotation, and the regional tectonic system moved from compression to the early stage of stretch conversion (Figure 9, Yang et al., 2011) [23]. With decreasing regional compression stress, several strike-slip shear faults and alkali-rich porphyries developed in the Ailaoshan area in the early stage of tectonic regime transformation, indicating that they were uniformly controlled by the tectonic dynamic transformation system of the collision between India and the Yangtze block. The large-scale mineralization of gold in the region is closely related to the transformation of the tectonic regime and the strong interaction of the crust and mantle (Yang et al., 2011) [23].
After 30 Ma, the gold mineralization in the Ailaoshan area ended and only sporadic age records exist in the Laowangzhai mining area. During this period, the regional tectonic dynamic regime was in the late transition period, the Indian plate changed from a counterclockwise rotation in the early period to a clockwise rotation (Funahara et al., 1992, 1993; Huang and Opdyke, 1993; Chen et al., 1995; Sato et al., 1999) [74,75,76,77,78], and the regional thrust-nappe tectonic system and shear strike-slip fault activities ended (Figure 9, Yang et al., 2011) [23].

5. Genesis Mechanism of Ore Deposits

This paper summarizes the microthermometric data results and C-H-O-S-Pb isotopes values of fluid inclusions of four main large gold deposits in the Ailaoshan metallogenic belt, and analyzes the geochemical characteristics and stable isotopes of the ore-forming fluid [16,20,21,42,44,45,46,47,48,49,53,54,68,79,80,81,82,83,84,85,86,87,88,89,90,91,92,93,94,95,96,97,98,99,100,101,102,103,104,105,106,107,108,109,110,111,112] (Li, 2014; Hu et al., 1995; Li et al., 1998; Deng et al., 2013a, b, c; 2015a, b; Mo et al., 2009; Huang et al., 1996; 1998; Zhang et al., 2010; Zhao et al., 2013; Zhang et al., 2019; Qu, 2019; Yang et al., 2013; Li, 1992; 1998; Zhang et al., 1987; Xie et al., 2001; Xiong, 2014; Bi et al., 1996; Zhang et al., 1984; Yang, 2018; Zhu et al., 2011; Chen et al., 2015; Shi et al., 2010; Li, 2017; Han et al., 1997; Li et al., 2000; Ge et al., 2007; Yuan et al., 2010, 2011; Yang et al., 2013; Chang et al., 2005; Zhang, 2017; Ying et al., 2006; Chen, 2010; Li et al., 2011; Fan et al., 2010; Sun et al., 2009; Li et al., 2000; Yang et al., 2021; Zhang et al., 2014; 2017; Li et al., 2013a, b; ECUT, 2007; Zhang et al., 2018).

5.1. Fluid Inclusion

The fluid inclusion composition in the Jinping Chang’an, Zhenyuan Laowangzhai, Mojiang Jinchang, and Yuanyang Daping gold deposits are mostly H2O and CO2 (Bi et al., 1997; Xie et al., 2001; Chen et al., 2010; Zhao, 2014) [22,92,107,113] and contain a small amount of CH4. The Chang’an gold deposit also contains a small amount of C4H6 (Chen et al., 2010) [107], and the Daping gold deposit contains a small amount of C2H4 and N2 (Du, 2015) [114]. Although their compositions are similar, the temperature and pressure of different deposits differ. The fluids of the main mineralization periods typically have the characteristics of medium-low temperatures and salinity (Figure 10), among which the mineralization depth is in the order of Yuanyang Daping > Zhenyuan Laowangzhai > Mojiang Jinchang > Jinping Chang’an. Ore-forming fluids are all reducing fluids, and gold might migrate in the form of Au(HS)2−. Table 3 summarizes the petrographic, physical, and chemical parameters of fluid inclusions in the four main gold deposits.

5.2. H-O Isotopes

The δD value in the four main gold deposits varies significantly, and the ore-forming fluid sources of different gold deposits are slightly different. Previous studies have shown that the ore-forming fluids of the Zhenyuan Laowangzhai and Yuanyang Daping gold deposits may mostly originate from the mixing of deep-source mantle-derived and metamorphic fluids (Sun et al., 2009; Deng et al., 2013c; Li, 2014; Chen et al., 2014; Du, 2015; Yang, 2018; Xin, 2019; Zhang et al., 2019) [20,21,39,40,82,88,115,116]. Among them, the early Daping ore-forming fluids mostly originated from metamorphic fluids (metamorphic water). The late ore-forming fluid composition is close to atmospheric precipitation (Sun et al., 2009; Zhang et al., 2018) [21,42]. The ore-forming fluids of the Mojiang Jinchang gold-nickel deposit might be deep fluids (mantle-derived or deep metamorphic fluids), with the obvious addition of atmospheric precipitation (Li, 1992; Fan et al., 2010; Xiong et al., 2015; Yang, 2018; Qu, 2019) [32,39,44,45,46]. The ore-forming fluid of the Jinping Chang’an gold deposit has obvious crust-derived characteristics (higher δ18OV-SMOW value), and the main body is a metamorphic fluid, which might be mixed with magmatic fluids and atmospheric precipitation (Deng et al., 2012) [117].
This study found that among the four gold deposits in the Ailaoshan metallogenic belt, only the δ18OV-SMOW values of fluid inclusions in the Zhenyuan Laowangzhai gold deposit and Yuanyang Daping gold deposit are within the δ18OV-SMOW value range of the generalized magmatic fluid (5.5–10‰ [118], Taylor, 1997, Figure 11a and Figure 12d,e). At the same time, their δD values are also in the δD value range of magmatic fluid (−85‰–−50‰ [118], Taylor, 1997, Figure 11a and Figure 12d,e). The Mojiang Jinchang gold deposit and the Jinping Chang’an gold deposit have only a few points located in these two areas, and the degasification of magmatic-hydrothermal fluids should lead to a decrease in the δD value (Taylor et al., 1983) [119]. Therefore, in Figure 11a, all points tend to be close to organic water area.
The H-O isotopes of the Zhenyuan Laowangzhai and Yuanyang Daping gold deposits are similar to those of the magmatic fluid; hence, the ore-forming fluid mostly comes from magmatic water (Taylor, 1974, Figure 11a) [120]. Due to the major changes in the δD values, the four gold deposits are all close to the range of organic water and extend from metamorphic to connate fluid. Deng et al. (2014b) [17] interpreted this as a reflection of isotope exchange as the metamorphic fluid migrated through the sedimentary rocks containing organic matter. The ore-forming fluids in the Ailaoshan metallogenic belt mostly comprise mantle (magmatic water) and metamorphic fluids (metamorphic water), and deposits with shallow mineralization depth are mixed with atmospheric precipitation.

5.3. C Isotopes

C isotopes are widely used to trace the source of CO2 in ore-forming fluids and are indicators to determine whether mantle fluids participate in ore-forming processes (Rollinson, 1993; Mao, 2003; Liu et al., 2003; Zhang et al., 2009) [124,125,126,127]. By comparing the δ13CV-PDB carbonate data (calcite, dolomite, iron dolomite, and siderite) in the four main gold deposits in the Ailaoshan metallogenic belt with δ13C values of different geological reservoirs (Figure 11b and Figure 12f), only the δ13C of the Daping gold deposit in Yuanyang showed an obvious mantle (−7‰ to −5‰) or continental crust (−7‰) origin. In the Zhenyuan Laowangzhai and Jinping Chang’an deposits, only a few dolomites and calcite exhibit a mantle or continental crust origin. The δ13C values of the Jinping Chang’an, Yuanyang Daping, and Zhenyuan Laowangzhai deposits overlap with the interval of magmatic rocks (−30‰ to −3‰), whereas only one sample in the Mojiang Jinchang deposit overlaps with the interval of magmatic rocks.
Simultaneously, in the four main deposits, the δ13C values partially overlap with the variation range of marine carbonate δ13C (−3‰ to 2‰). The CO2 needed in the fluid can be provided by carbonate mineral dissolution and decarbonation, the degassing of the mantle, and crystallization differentiation of magma. During the metallogenic process of the Laowangzhai gold deposit in Zhenyuan, the content of H2O in the gas phase of fluid inclusions increases gradually, while the content of CO2 decreases gradually, and the value of CO2/H2O shows a decreasing trend (Zhao, 2014) [22]. This is one of the signs that a fluid is boiling (Phillips and Evans, 2004) [128]. The volatile components escaping from the hydrothermal fluid through boiling are mostly CO2, CH4, H2S, and H2O (Xiong et al., 2015; Qu, 2019) [32,46]. Some isotope fractionation occurs between these gas components and the liquid fluid, and their loss will change the isotope composition in the hydrothermal fluid (Zheng, 2001) [129]. In the process of CO2 degasification, the CO2 released by rocks enriches heavy 13C and 18O; therefore, δ13C and δ18O values of the carbonate minerals formed by residual materials (such as calcite) decrease (Brown et al., 1985; Zheng and Hoefs, 1993) [130,131], increasing the δ13C value in the fluid (Zheng et al., 1996) [132]. Based on Zhao’s (2014) [22] research on the trace elements and H-O-S isotopes of the golden iron ore in the Zhenyuan Laowangzhai gold deposit, the carbon in the ore-forming fluid is more likely to come from the mantle or continental crust and does not exclude the contamination of marine sedimentary rocks in the shallow part.
The Mojiang Jinchang, Jinping Chang’an, and Yuanyang Daping gold deposits mostly come from the surrounding rocks of the stratum in the mining area; therefore, the carbon is more likely to come from marine carbonate. The Mojiang Jinchang is a Triassic Jinchang Formation siliceous rock, the Jinping Chang’an is a Silurian Kanglang Formation dolomite, and the Yuanyang Daping is a Middle Silurian Kanglang Formation carbonate rock. Among them, the ore-bearing host rock of the Yuanyang Daping gold deposit is Taojiazhai diorite in the north of the mining area and the Middle Silurian Kanglang Formation carbonate rock in the south of the mining area (Du, 2015) [115]. Xiong et al. (2006) [133] found granulite facies graphite inclusions in the scheelite of the Daping gold deposit. They proposed that the carbon in the deposit mostly comes from the original magma formed by the mantle’s melting and CO2 mostly comes from the decarbonization of the lower crust, which is affected by weak metasomatism.

5.4. Pb Isotopes

This paper presents the 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios of different host rocks and ores in the four main gold deposits in the Ailaoshan metallogenic belt. The results showed that the Pb isotope compositions in the metallogenic zone are similar to some extent, indicating that all gold deposits in the Ailaoshan metallogenic belt might have the same Pb source. Wang et al. (2013) [1] found that the Pb isotope composition of the crust of the Yangtze block can represent the Pb isotope characteristics of the crust where the Ailaoshan metallogenic belt is located. Therefore, Zhao (2014) [22] collected the Pb isotopic composition of the peraluminous leucogranites produced in the ASRRSZ, representing the characteristics of the upper crust of the Yangtze at the same collision stage, and the Pb isotopic composition of amphibolite capture bodies in the Eocene potassium-bearing felsic intrusive rocks in western Yunnan to represent the Pb isotopic characteristics of the middle and lower crust of the Yangtze (Zhao, 2004) [22]. By collecting published Pb isotope data and putting the data into Pb-Pb isotope diagrams (Figure 12 and Figure 13), we can highlight the following details. The Pb isotopic composition of the four main gold deposits in the Ailaoshan metallogenic belt is slightly different, mostly concentrated between the upper crust and the middle and lower crusts of the Yangtze, showing obvious crust source characteristics. The 207Pb/204Pb and 206Pb/204Pb curves of the Laowangzhai Gold deposit in Zhenyuan shifted to the left, mostly falling in the range of leucogranites in the Ailaoshan metallogenic belt, and partly falling in the amphibolite in the western Yunnan and enriched mantle (EMII) area (Lu et al., 2013, Figure 13a,b) [134].
Deng et al. (2014b) [17] proposed that the EMII might be caused by the recirculation of upper crust material into the mantle. The Pb isotopic characteristics show that the Pb of the Laowangzhai gold deposit in Zhenyuan is mostly derived from the upper crust, accompanied by many mantle-derived materials. The Pb isotopic characteristics of the Daping gold deposit in Yuanyang overlap with the upper crust and middle and lower crusts. The Pb isotopes of the Daping gold deposit in Yuanyang are more concentrated in the range of amphiboles in Western Yunnan, and their characteristics are similar to the upper, middle, and lower crusts. Simultaneously, some points are located in the EMII, exhibiting obvious characteristics of crust-mantle mixing. The Pb isotopic composition of the Jinchang gold-nickel deposit in Mojiang is relatively scattered, and some data are relatively deviated, which might be anomalous Pb. Two of these points fall within the block silicate earth range, showing that Pb mostly comes from the middle and lower crusts, with a small number of other sources involved (Deng et al., 2014b) [17]. The Pb isotopic characteristics of the Chang’an gold deposit in Jinping have similar characteristics to the upper crust, and a small number of points are in the range of the EMII. Therefore, Pb is more likely to originate from the upper crust with higher maturity, possibly accompanied by a small amount of mantle material. Typically, the Pb isotopes in the four main gold deposits in the Ailaoshan metallogenic belt have the characteristics of multiple sources. Both the upper crust and the middle and lower crusts are involved, accompanied by the mixing of mantle-derived materials. Some gold deposits have a mixture of stratum Pb in the shallow part (Zhao, 2014) [22].
The ratio range of 207Pb/204Pb and 206Pb/204Pb of light-colored granite is closer to the upper crust than amphibolite, indicating that light-colored granite is generally formed in the shallower part of the crust compared with amphibolite in western Yunnan. Correspondingly, the source of ore-forming fluids of the Laowangzhai gold deposit in Zhenyuan is shallower than that of the Daping gold deposit in Yuanyang. This is consistent with the result of mineralization depth estimated by measuring the temperatures of fluid inclusions and calculating the captured pressure in the previous article (1.9–3.3 km in Zhenyuan; 5.1–12.9 km in Daping).

5.5. S Isotopes

This paper summarizes previous research results and analyzes the S isotope characteristics of various deposits in the Ailaoshan metallogenic belt. The study of S isotopes in ore deposits must analyze the total S isotope composition of sulfide. In a reducing mineralization system, the δ34S of sulfide in ore minerals can roughly represent the total S isotope composition of ore-forming hydrothermal fluids (Ohmoto, 1972; Ohmoto and Rye, 1979) [141,142]. Many studies have shown that S in the gold ore-forming fluid in the Ailaoshan area is mostly in the form of HS− and S2− (Zhao, 2014; Bi et al., 1996; Xie et al., 2001; Xiong et al., 2007; Li, 2012) [22,50,54,92,114]. It shows that the original ore-forming fluid is a reducing fluid, and no sulfate production is found in each gold deposit. Therefore, the S isotope composition δ34S of the sulfide in each gold deposit can approximately represent the S isotope composition δ34SΣS of the total sulfur in the ore-forming fluid. In particular, in low-to-medium hydrothermal deposits with low ore-forming temperatures, the total S isotope composition δ34SΣS in the hydrothermal fluid can be represented by δ34S of pyrite (Butler et al., 2004; Zhang et al., 2014; Liu et al., 2013) [41,143,144].
The S isotope composition analysis shows that the δ34S value of the ore-forming fluid of the Laowangzhai gold deposit in Zhenyuan is distributed in a tower-like manner near the zero value, not significantly different from the δ34S value of the pyrite in the formation. It shows obvious mantle source characteristics; however, it could be because of the homogenization of deep metamorphic fluids after undergoing metamorphic and alteration processes, indicating that the sulfur source might be the mantle or deep crust and not from the shallow metamorphic rock strata in the mining area. The δ34S values of various host rocks and ores of the Mojiang Jinchang gold-nickel deposit exhibit a tower-like distribution near −5‰ and are lower than the mantle source δ34S values. This indicates that the fluid has an extensive material exchange with the surrounding rock, and the homogenization between different sulfur sources is strong. However, the δ34S value of the altered ultrabasic rock and the closely related nickel ore is low, indicating that the deep-source sulfur in the ore-forming fluid is significantly mixed with the sulfur in the formation, providing more sulfur sources. The δ34S values of the ore-forming fluids of the Daping gold deposit in Yuanyang are positive, similar to the typical tower-like distribution characteristics of the S isotopes of the Laowangzhai gold deposit in Zhenyuan (+1‰ to +2‰), and the value distribution is wide. The δ34S value is closer to the mantle-sourced sulfur and only deviates in the positive direction, indicating that the sulfur in the ore-forming fluid mostly comes from deep sources. The δ34S values of various ores and magmatic rocks and strata in the Jinping Chang’an gold deposit are all concentrated around 0‰, indicating that different sulfur sources are mixed and uniform. The δ34S values of some breccia ore and pyrite are low, reflecting that the source of sulfur might be related to the biological sulfur of sedimentation. These characteristics indicate that the sulfur in the ore-forming fluid mostly come from the surrounding rock, and some are mixed with magma sources (Figure 14).

6. Regional Metallogenic Model

Recently, many scholars considered the crust-mantle interaction as the main metallogenic mechanism of the Ailaoshan metallogenic belt; however, there is still some controversy regarding the source of specific minerals and fluids. From the results of previous studies, the metamorphism of the middle and lower crusts provides mostly metallogenic material and fluid sources in the mineralization zone. The mantle activity might provide the energy required for crust degassing (Powell et al., 1991; Haeussler et al., 1995) [146,147] and the source of some materials and fluids (Rock and Groves, 1988) [148]. A series of Cenozoic porphyry-skarn gold deposits developed in the Ailaoshan metallogenic belt, in which most deposits are related to the Eocene alkali-rich porphyry intrusion (Deng et al., 2015; Hou et al., 2017) [149,150]. The amphibolite enclaves in the alkali-rich porphyry body confirmed the existence of the Neoproterozoic lower crust, whereas the high gold and copper content in the amphibolite proved that the metal components originated from the Neoproterozoic lower crust (Hou et al., 2017) [150]. The Neoproterozoic super mantle plume (Figure 15a) and Paleozoic subduction events caused metal enrichment in the young lower crust (Figure 15b), and the partial melting of the Cenozoic lithospheric mantle triggered partial melting of the young lower crust (Figure 15c), forming ore-bearing plutonic rocks (Deng et al., 2014, 2015; Hou et al., 2017) [17,18,149,150].
A close relation exists among the subcontinental lithospheric mantle (SCLM), lower crust, and magmatic-hydrothermal-type gold deposits (Muntean et al., 2011; Hronsky et al., 2012; Griffin et al., 2013; Hou et al., 2017) [150,151,152,153]. The original SCLM is deficient in Au (Rudnick and Gao, 2003) [154] but can be replaced by Au-rich fluids (Wang et al., 2020) [59]. The magma from this enriched SCLM transports Au to the crust. The magma might emplace in the upper part of the crust to form gold deposits or to accumulate at the bottom of the crust to form new metal-rich reservoirs. Furthermore, Au stored in the lower crust can be transported to the upper crust during subsequent reactivation. The evolution of the Ailaoshan metallogenic belt is inextricably linked to the tectonic history of the supercontinent of Rodinia, the spread and closure of the Paleo-Tethyan Ocean, subsequent India-Asia continental collision, and postcollisional deformation and exhumation (Wang et al., 2020) [59]. During the Neoproterozoic period, the impact of the mantle plume on the bottom of the South China lithosphere caused heat conduction within the lithosphere, inducing a large proportion of the water-bearing SCLM to undergo partial melting (Li et al., 1999; Li et al., 2002; 2008; Zou et al., 2020) [10,11,12,13], forming the lower continental crust and Au-rich SCLM (Figure 15a; Lu et al., 2013; He et al., 2016; Hou et al., 2017; Cai et al., 2014) [134,150,155,156]. Both of these regions remobilized and transported gold to the shallow crust (Figure 15c). Hou et al.’s (2017) [150] study on the alkali-rich porphyry internal amphibolite and garnet amphibolite xenolith related to the Beiya gold deposit indicated that xenoliths originated in the lower crust and are the remnants of Neoproterozoic magma. This type of juvenile crust is more enriched in Cu, Au, and other metallogenic elements than the normal continental crust. The Au in the lower crust is enriched by Eocene magmatic rocks to the surface. Au aggregates and migrates more easily in an environment with a weak melt oxidation state and moderate water content.
However, Au is precipitated with the crystallization of Ti-Fe oxides in the middle crust (Figure 15b). Consequently, the Au-poor magma emplaces the upper crust and Au-rich middle crust; however, Au might still migrate to the shallow crust to form a localized mineralization zone (Shi et al., 2012) [159]. The postcollisional lithosphere extension after the Cenozoic triggered large-scale magmatic activity (43–32 Ma), accompanied by strong shearing and gold mineralization (Figure 15c). The Au-rich lower crustal ore-forming fluids rose through deep faults and formed many gold deposits in the Ailaoshan metallogenic belt. The Au-rich middle crust during the Triassic period is also a probable source of Au in this metallogenic belt (Wang et al., 2020) [59].
The four main gold deposits in the Ailaoshan metallogenic belt are the Laowangzhai in Zhenyuan, the Jinchang in Mojiang, the Daping in Yuanyang, and the Chang’an in Jinping from the west to the east. Metallogenic types include altered rock type, altered rock and quartz vein mixed type, and quartz vein type. Although the mineralization types of the four gold deposits are different, the gold mineralization is consistent in age and all the deposits belong to the early Himalayan orogen. Therefore, they might be under the same tectonic background, enriched by ore-forming fluids of the same periods, and then mineralized. C-H-O-S-Pb isotope data indicate that the main fluid sources of the gold deposits mentioned above are characterized by mixed crust and mantle sources. In summary, the delamination of the lithospheric mantle led to the upwelling of the asthenospheric mantle, and a large number of mantle-derived materials induced deep metamorphism.
The metamorphic hydrothermal fluid moves up and reacts with the surrounding rock and precipitates under suitable metallogenic conditions to form the Ailaoshan gold mineralization zone. Based on the metallogenic characteristics of the gold deposits in the Ailaoshan metallogenic belt, the continuous mineralization mechanism of the crust can be used for reference to establish a regional metallogenic model (Groves, 1993; Groves et al., 1998) [160,161]. In the early Himalayas, affected by the continental collision of the India-Yangtze plate, the Ailaoshan area was squeezed in both directions from the southwest to the northeast, forming a large-scale thrust-nappe tectonic system. Simultaneously, the shear strike-slip fault structure was formed, which significantly shortened and thickened the crust and lithosphere in the Ailaoshan area (Chen et al., 2008) [73]. Strong deformation and metamorphism occurred in the middle and lower crust, accompanied by the activity of mantle-derived magma. The middle and lower crust degassed to form metamorphic Au and CO2-rich fluids, which might be mixed with some upwelling mantle-derived materials. Subsequently, due to the tectonic system’s transformation, many deep shear zones were formed in the Ailaoshan area. The ore-bearing fluid rose along the shear zone, further extracting the surrounding rock-forming minerals, evolving into a high-salinity ore-forming fluid. The fluid is rich in Au, Pb, Cu, and other ore-forming elements. When the ore-forming fluid rises to the brittle-ductile transition zone, due to the formation of brittle fractures, the fluid temperatures and pressures drop rapidly, making the CO2-rich ore-bearing fluid immiscible, and fluid boiling allows a large amount of CO2 to escape. This led to the loss of stability of the Au(HS)2− complex compounds, resulting in a large amount of gold precipitation and the formation of the Daping gold deposit at the tough-brittle structural level.
In the shallow crust, metamorphic fluids, rich in Au, As, and other ore-forming elements produced by metamorphism of the low greenschist facies, are continuously added to the upper crust. The materials from multiple sources in the fluid are fully mixed and uniform: Au, As, and S in the ore-forming fluid form (Au, As)2−, (Au[As, S3])2−, and other complex compounds, migrating in the hydrothermal fluid. In the early stage of mineralization, (S2)2− enters the pyrite lattice in the form of isomorphism. When the fluid migrates to the brittle-ductile structure level, the fluid boils under a reduced pressure and CO2 continues to escape, making the (AuAsS3)2− and Au(HS)2− complexes in the fluid unstable, triggering the precipitation of gold and forming the Laowangzhai gold deposit. In the ore-forming fluids of the Daping and Laowangzhai gold deposits, mantle-derived fluids (magmatic water) containing Au and S are added and atmospheric precipitation might be mixed simultaneously. When the fluid reaches the shallower crust, atmospheric precipitation is continuously added to the ore-forming fluid. The mixed fluid has a strong water-rock reaction with the surrounding rock and extracts Au, CO2, and S in the Silurian strata. Simultaneously, as the physical and chemical conditions of the ore-forming fluid change, a large amount of sulfide precipitates in the brittle structural space, reducing the activity of the reduced sulfur in the hydrothermal fluid. Consequently, the continuous decomposition of Au(HS)2− complex compounds precipitated gold and other minerals, forming the Mojiang and Chang’an gold deposits (Figure 16, Zhao, 2014) [22].

7. Conclusions

(1)
The geological characteristic analysis of the four main gold deposits in the Ailaoshan metallogenic belt showed that the area has a strong tectonic-magmatic activity, forming a series of ultrabasic, basic, and intermediate-acid magmatic rocks. The hydrothermal effect is strong, the alteration products are developed, and the spatial zoning of alteration types is not obvious. Gold mineralization is closely related to silicification, argillation, carbonation, and pyrite mineralization.
(2)
Based on the existing radiometric age data characteristics in the Ailaoshan metallogenic belt, this paper proposes that the metallogenic-thermal events experienced by the Ailaoshan metallogenic belt can be divided into early (65–60 Ma), major (40–30 Ma), and late (30–25 Ma) phases. The gold mineralization mostly occurred between 30 and 50 Ma, belonging to the early Himalayan period.
(3)
Research on the composition of ore-forming fluid inclusions and the physicochemical properties of ore-forming reveals that the ore-forming fluid in the Ailaoshan metallogenic belt exhibits the characteristics of medium-low temperatures (150–300 °C) and medium-low salinity (an average of around 7 wt% NaCl). The cations in the fluid are mostly Na+ and K+, the anions are Cl− and SO42−, and the gas phase composition mostly comprises CO2; furthermore, the content is between 1% and 37%, representative of a H2O-NaCl-CO2 (-ΣS) system. The fluid is in a neutral, weakly alkaline, and relatively reductive state. Different deposits also exhibit certain differences, mostly reflected in the mineralization temperatures, pressures, depths, and CO2 content. From Yuanyang Daping → Zhenyuan Laowangzhai → Mojiang Jinchang → Jinping Changan, there is a decreasing trend.
(4)
The joint study of C-H-O-S-Pb isotopes shows that regional ore-forming fluids mostly comprise mantle (magmatic water) and metamorphic fluids (metamorphic water) and the metamorphic fluids are mostly in the middle and lower crust. Deposits with relatively shallow ore-forming depths might be mixed with meteoric water. The ore-forming materials exhibit the characteristics of multiple sources. Both the upper crust and the middle-lower crust are involved, and the mixing of mantle-derived materials also occurs. Some shallow host rocks provide numerous ore-forming materials.
(5)
Based on the analysis of the geological characteristics, metallogenic geodynamic background, and genetic mechanism of the gold deposits in the Ailaoshan metallogenic belt, the regional metallogenic model was established by referring to the continuous metallogenic mechanism of the crust combined with the metallogenic characteristics of the Ailaoshan metallogenic belt.

Author Contributions

Conceptualization, D.W. and Y.L.; data curation, Y.L.; writing—original draft preparation, Y.L.; supervision, D.W., Y.L. and C.W.; project administration, Y.S. and M.P.-c., funding acquisition, D.W., Y.L. and Y.S. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by [Geology of Mineral Resources in China] grant number [DD20190379], and [Comprehensive investigation and evaluation of a large-scale lithium-beryllium polymetallic resource base in Songpan-Ganzi Lithium Belt] grant number [DD20190173]. And The APC was funded by [DD20190379].

Acknowledgments

The constructive comments and careful revisions from the editor, associate editor, and two reviewers are greatly appreciated. During the writing process of the article, This paper received the help of Cao Huawen, from Chengdu Center, China Geological Survey, Lu Yan, deputy chief engineer; Li Yubin, senior engineer from Tibet Institute of Geological Survey; Liu Hang, from Chengdu Univerisity of Technology; Jiang Xiuwei, from Northwest University, amongothers, and put forward constructive suggestions for the article. This study was financially supported by Geology of Mineral Resources in China, China Geological Survey (DD20190379) and Comprehensive investigation and evaluation of a large-scale lithium-beryllium polymetallic resource base in Songpan-Ganzi Lithium Belt (DD20190173).

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (a) Generalized geological map showing major tectonic structures caused by to the India-Eurasia collision (revised from [4,26]) and (b) geological map of the Ailaoshan gold belt along the Ailaoshan shear zone showing the high-grade metamorphic belt, ophiolite belt, and Jinping terrane (modified from [17]).
Figure 1. (a) Generalized geological map showing major tectonic structures caused by to the India-Eurasia collision (revised from [4,26]) and (b) geological map of the Ailaoshan gold belt along the Ailaoshan shear zone showing the high-grade metamorphic belt, ophiolite belt, and Jinping terrane (modified from [17]).
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Figure 2. (a) Geological map of the Jinchang gold deposit showing granitoid, meta-(ultra) mafic rocks and ore bodies. (b) geological profile of Jinchang gold deposit exploration line (modified from [33]).
Figure 2. (a) Geological map of the Jinchang gold deposit showing granitoid, meta-(ultra) mafic rocks and ore bodies. (b) geological profile of Jinchang gold deposit exploration line (modified from [33]).
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Figure 3. (a) Geological map and cross-section of the Zhenyuan gold deposit showing felsic, mafic, and lamprophyre dykes and gold ore bodies. (b) Drill sections from the Donggualin ore-shoot cluster of the Zhenyuan ore deposit (modified from [4,34,35]).
Figure 3. (a) Geological map and cross-section of the Zhenyuan gold deposit showing felsic, mafic, and lamprophyre dykes and gold ore bodies. (b) Drill sections from the Donggualin ore-shoot cluster of the Zhenyuan ore deposit (modified from [4,34,35]).
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Figure 4. Geological map of Yuanyang Daping gold deposit (modified from [40]).
Figure 4. Geological map of Yuanyang Daping gold deposit (modified from [40]).
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Figure 5. (a) Geological map showing lamprophyre and syenite dykes, widespread host-rock alteration, and gold ore bodies in the Chang’an gold deposit. (b) geological profile of Chang’an gold deposit exploration line (modified from [41]).
Figure 5. (a) Geological map showing lamprophyre and syenite dykes, widespread host-rock alteration, and gold ore bodies in the Chang’an gold deposit. (b) geological profile of Chang’an gold deposit exploration line (modified from [41]).
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Figure 6. Minerals of the Zhenyuan Laowangzhai, Yuanyang Daping, and Mojiang Jinchang gold deposits (modified from [22]).
Figure 6. Minerals of the Zhenyuan Laowangzhai, Yuanyang Daping, and Mojiang Jinchang gold deposits (modified from [22]).
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Figure 7. Minerals of the Jinping Chang’an gold deposits (modified from [41]).
Figure 7. Minerals of the Jinping Chang’an gold deposits (modified from [41]).
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Figure 8. Age histograms and scatter plots of gold deposits and related magmatic activities in the Ailaoshan metallogenic belt (data from Table 2; Ar-Ar: using the step-heating 40Ar-39Ar method; K-Ar: 40K-40Ar isochron dating method; Electron Spin Resonance (ESR) dating; Rb-Sr: 87Rb–86Sr isochron dating method; fission track (F-T) dating method; Laser Ablation Inductively Coupled Plasma-Mass Spectrometry (LA-ICP-MS) zircon U-Pb dating; SHRIMP: dating by single grain zircon ion probe mass spectrometry; Re-Os: 187Re-187Os isotope dating method).
Figure 8. Age histograms and scatter plots of gold deposits and related magmatic activities in the Ailaoshan metallogenic belt (data from Table 2; Ar-Ar: using the step-heating 40Ar-39Ar method; K-Ar: 40K-40Ar isochron dating method; Electron Spin Resonance (ESR) dating; Rb-Sr: 87Rb–86Sr isochron dating method; fission track (F-T) dating method; Laser Ablation Inductively Coupled Plasma-Mass Spectrometry (LA-ICP-MS) zircon U-Pb dating; SHRIMP: dating by single grain zircon ion probe mass spectrometry; Re-Os: 187Re-187Os isotope dating method).
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Figure 9. Tectonic-metallogenic evolution sequence of the Ailaoshan metallogenic belt (modified from [23]).
Figure 9. Tectonic-metallogenic evolution sequence of the Ailaoshan metallogenic belt (modified from [23]).
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Figure 10. Homogenization Temperature-Salinity map of ore-forming fluid in the Ailaoshan gold deposit. Note: The different colored ellipses indicate the main scope of "Homogenization Temperature-Salinity" in different deposits.
Figure 10. Homogenization Temperature-Salinity map of ore-forming fluid in the Ailaoshan gold deposit. Note: The different colored ellipses indicate the main scope of "Homogenization Temperature-Salinity" in different deposits.
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Figure 11. Scatter diagrams of H-O (a) and C-O isotopes (b) in the ore-forming fluid from the Ailaoshan tectonic belt, SW China [121]. The dashed, green box in panel b represents the C-O isotopes ranges of calcites expected to precipitate from magmatic water at the indicated temperatures [122]. The H-O isotopes of magmatic, metamorphic, and organic fields are from [123]. Note: The different colored ellipses in Figure 11b indicate the main scope of “δ18OV-SMOW -δ13CV-PDB” in different deposits. And the same color represents the same deposit, and different shapes represent different tested minerals.
Figure 11. Scatter diagrams of H-O (a) and C-O isotopes (b) in the ore-forming fluid from the Ailaoshan tectonic belt, SW China [121]. The dashed, green box in panel b represents the C-O isotopes ranges of calcites expected to precipitate from magmatic water at the indicated temperatures [122]. The H-O isotopes of magmatic, metamorphic, and organic fields are from [123]. Note: The different colored ellipses in Figure 11b indicate the main scope of “δ18OV-SMOW -δ13CV-PDB” in different deposits. And the same color represents the same deposit, and different shapes represent different tested minerals.
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Figure 12. C-H-O-S-Pb isotopes scatter diagram of gold deposits in the Ailaoshan metallogenic belt. (a) 206Pb/204Pb. (b) 207Pb/204Pb. (c) 208Pb/204Pb. (d) D isotopes. (e) O isotopes. (f) C isotopes. Note: In the figure, the isotopic compositions of different tested minerals in four different deposits are represented from bottom to top: Zhenyuan Laowangzhai, Mojiang Jinchang, Yuanyang Daping and Jinping Chang’an. The same color represents the same deposit, and different shapes represent different tested minerals.
Figure 12. C-H-O-S-Pb isotopes scatter diagram of gold deposits in the Ailaoshan metallogenic belt. (a) 206Pb/204Pb. (b) 207Pb/204Pb. (c) 208Pb/204Pb. (d) D isotopes. (e) O isotopes. (f) C isotopes. Note: In the figure, the isotopic compositions of different tested minerals in four different deposits are represented from bottom to top: Zhenyuan Laowangzhai, Mojiang Jinchang, Yuanyang Daping and Jinping Chang’an. The same color represents the same deposit, and different shapes represent different tested minerals.
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Figure 13. Pb isotopic composition of sulfide in the Ailaoshan metallogenic belt (modified from [134]). Mantle source reservoirs BSE, MORB, DMM, EM I, and EM II are fromZindler and Hart (1986) [135]. Indian MORB and Pacific MORB are after Guo et al. (2005) [136]. The Northern Hemisphere Reference Line (NHRL) is from Hart (1984) [137]. Data for leucogranite are fromZhang and Schärer (1999) [138] and those for amphibolite xenoliths in the potassic felsic intrusion are fromDeng et al. (1998) [139] and Zhao et al. (2004) [140]. Note: The same color represents the same deposit, and different shapes represent different tested minerals.
Figure 13. Pb isotopic composition of sulfide in the Ailaoshan metallogenic belt (modified from [134]). Mantle source reservoirs BSE, MORB, DMM, EM I, and EM II are fromZindler and Hart (1986) [135]. Indian MORB and Pacific MORB are after Guo et al. (2005) [136]. The Northern Hemisphere Reference Line (NHRL) is from Hart (1984) [137]. Data for leucogranite are fromZhang and Schärer (1999) [138] and those for amphibolite xenoliths in the potassic felsic intrusion are fromDeng et al. (1998) [139] and Zhao et al. (2004) [140]. Note: The same color represents the same deposit, and different shapes represent different tested minerals.
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Figure 14. S isotope composition of sulfide in the Ailaoshan metallogenic belt. The background curve is the δ34S values of seawater carbonate and sedimentary orogenic gold deposits during the geological periods, modified from [145].
Figure 14. S isotope composition of sulfide in the Ailaoshan metallogenic belt. The background curve is the δ34S values of seawater carbonate and sedimentary orogenic gold deposits during the geological periods, modified from [145].
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Figure 15. Schematic diagram showing the gold enrichment process in the lithosphere of the western South China block during the Neoproterozoic, Triassic, and Cenozoic (ZL: Zhenyuan Laowangzhai; MJ: Mojiang Jinchang; YD: Yuanyang Daping; JC: Jinping Chang’an, modified from [59,150,157,158]). (a) and (b). The Neoproterozoic supermantle plume and Paleozoic subduction events caused metal enrichment in the young lower crust. (c). The partial melting of the Cenozoic lithospheric mantle triggered partial melting of the young lower crust, forming ore-bearing plutonic rocks.
Figure 15. Schematic diagram showing the gold enrichment process in the lithosphere of the western South China block during the Neoproterozoic, Triassic, and Cenozoic (ZL: Zhenyuan Laowangzhai; MJ: Mojiang Jinchang; YD: Yuanyang Daping; JC: Jinping Chang’an, modified from [59,150,157,158]). (a) and (b). The Neoproterozoic supermantle plume and Paleozoic subduction events caused metal enrichment in the young lower crust. (c). The partial melting of the Cenozoic lithospheric mantle triggered partial melting of the young lower crust, forming ore-bearing plutonic rocks.
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Figure 16. Regional metallogenic model of the Ailaoshan gold belt (ZL: Zhenyuan Laowangzhai; MJ: Mojiang Jinchang; YD: Yuanyang Daping; JC: Jinping Chang’an, modified from [22]).
Figure 16. Regional metallogenic model of the Ailaoshan gold belt (ZL: Zhenyuan Laowangzhai; MJ: Mojiang Jinchang; YD: Yuanyang Daping; JC: Jinping Chang’an, modified from [22]).
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Table
Table 1. Geological characteristics of the main gold deposits in Ailaoshan metallogenic belt.
Table 1. Geological characteristics of the main gold deposits in Ailaoshan metallogenic belt.
Gold DepositZhenyuan LaowangzhaiMojiang JinchangYuanyang DapingJinping Chang’an
Proven reserves (t)22.48431.7406031.155
Average grade (g/t)5.292.6914.305.84
Structural settingAilaoshan epi-metamorphic rock beltAilaoshan epi-metamorphic rock beltSouthwest of Jinping nappeAilaoshan epi-metamorphic rock belt
Ore-controlling structureW-trending Jiujia-Mojiang fault and EW-trending Bankan river fault intersection site, the secondary EW-trending thrust brittle-ductile fault and its derived interlayer fault zoneNW-trending NNE-trending secondary normal fault and translation fault on the east side of Jiujia-Mojiang faultNW to both sides of the Jinzi river fault, between the Sanjia river fault and the Xiaozhai-Jinping faultNW-trending Tongjiao river fault and Ailaoshan fault intersection site, secondary NW-trending nappe structure slip surface and conjugate NE-trending fault
MagmatiteIt is dominated by ultrabasic rocks and basic rocks, followed by lamprophyre and quartz porphyryThe ultrabasic Jinchang rock plutonHercynian Taojiazhai diorite, Yanshanian monzogranite and graniteHimalayan olivine pyroxenite, diabase, gabbro, syenite porphyry, syenite, fine grained syenite and granite and lamprophyre
Host rockThe Lower Carboniferous altered basalt and lamprophyre are dominated, with a small amount of carbonaceous siliceous slate and sandstone.Upper Devonian metamorphic quartz sandstone, carbon-bearing slate, silicified sandstone, siliceous rock and pebbly quartziteHercynian Taojiazhai dioriteMiddle-Upper Silurian dolomite, Lower Ordovician siltstone intercalated with mudstone and conglomerate, and altered diabase of the Himalayan period
Mineralization styleDisseminated, veined, reticulated and breccia altered rock typesBanded, fine vein disseminated and breccia quartz vein type and altered rock typeVeinlets disseminated quartz vein typeVeined, reticulated and brecciated altered rock types and quartz vein types
Morphology of ore bodyThe ore bodies produced along the faults are mainly veins and irregular veins; the ore bodies produced along the layers are layered and lenticularThe ore bodies produced in quartzite are mostly layered and lenticular, and the ore bodies produced in quartz veins are often arranged in geese and appear in groupsThin veins, not far apart and spread out in parallelFlame shaped, lenticular structure
Orebody scaleLength >1000 m, thickness > 1 mLength >1000 m, width >100 m, the average thickness is 16.25 mLength >150 m, thickness >2 m1800 m long, >40 m thick, with an average thickness of 25 m
Ore typeMainly mineralized ultrabasic-basic rocks, sandy (siliceous) sericite and metamorphic sandstone, and some are mineralized basalt and lamprophyre.Gold-bearing quartz veins, disseminated gold-bearing quartzite, and gold-bearing variable residual siltstone.Sulfide-quartz vein type, fracture zone altered rock type and breccia type.Veinlets disseminated sulfide ores and breccia-like oxide ores.
Gold-bearing mineralMainly pyriteMainly pyrite, pyrrhotite and marcasiteMainly pyrite and galenaQuartz, pyrite, arsenopyrite
Ore mineralPyrite, arsenopyrite, arsenopyrite, stibnite, scheelite, galena, sphalerite, chalcopyrite, arsenopyrite, etc.Pyrite, pyrrhotite, white ore, chalcopyrite, bornite, stibnite, galena, sphalerite, etc.Pyrite, galena, chalcopyrite, sphalerite, wolframite, arsenic tetrahedrite, etc.Pyrite, arsenopyrite, hematite, etc.
Gangue mineralQuartz, iron dolomite, sericite, etc.Quartz, chalcedony, cryptocrystalline siliceous, opal, sericite, chlorite, albite, etc.Quartz, iron dolomite, barite, etc.Quartz, feldspar, sericite, clay minerals, Muscovite, dolomite, calcite, etc.
Occurrence of goldNatural gold and silver gold minesNatural gold, silver gold mine, selenium gold silver mine, iridium gold mine and palladium gold mineNatural gold and silver gold minesNatural gold and silver gold mines
Element associationAu-As-Hg-SbAu-Ni-Ag-Co-Se-PGEAu-CuAu-As-Cu
Alteration characteristicsMetasomatic quartzification, silicification, sericitization, carbonation and associated sulfidationSilicification, pyritization, chromium hydromica, liquification, and carbonationSilicification, pyritization, sericitization, chloritization, epidote and carbonationSilicification, carbonation, sericite, pyrite, etc.
References[20,42,43][32,39,44,45,46][4,21,40,42][16,47,48,49,50]
Table
Table 2. Mineralization and magmatic age of the main gold deposits in Ailaoshan metallogenic belt.
Table 2. Mineralization and magmatic age of the main gold deposits in Ailaoshan metallogenic belt.
No.DepositSample No.Sample DescriptionMineralDating MethodsAge/MaReferences
1Mojiang JinchangL3Nickel oreChromium sericite40Ar-39Ar63.09 ± 0.16[33]
2Mojiang JinchangL5Nickel oreChromium sericite40Ar-39Ar62.05 ± 0.14[33]
3Mojiang-JinchangSh4Nickel oreChromium sericite40Ar-39Ar61.55 ± 0.23[33]
4Mojiang Jinchang Gold oreChromium hydromica40K-40Ar61[53]
5Mojiang Jinchang9704Auriferous quartz veinQuartz40Ar-39Ar56.49 ± 0.34[33]
6Mojiang JinchangM4Auriferous quartz veinQuartz40Ar-39Ar59.67 ± 0.16[33]
7Mojiang JinchangSh2-aAuriferous quartz veinQuartz40Ar-39Ar54.02 ± 0.19[33]
8Mojiang JinchangSh2-cAuriferous quartz veinQuartz40Ar-39Ar55.74 ± 0.34[33]
9Mojiang JinchangHBM-62Auriferous quartz veinQuartzESR66.4[54]
10Mojiang JinchangHBM-63Auriferous quartz veinQuartzESR29[54]
11Mojiang JinchangHBM-105Auriferous quartz veinQuartzESR44.8[54]
12Zhenyuan Laowangzhai LamprophyrePhlogopite87Rb-86Sr35.6[53]
13Zhenyuan Laowangzhai LamprophyrePhlogopite87Rb-86Sr43[53]
14Zhenyuan Laowangzhai MinetteApatiteF-T22.7 ± 3.3[38]
15Zhenyuan Laowangzhai MinetteApatiteF-T27.1 ± 2.8[38]
16Zhenyuan LaowangzhaiLWZ-1LamprophyrePhlogopite40Ar-39Ar30.8 ± 0.4[55]
17Zhenyuan LaowangzhaiLWZ-2LamprophyrePhlogopite40Ar-39Ar34.3 ± 0.2[55]
18Zhenyuan Laowangzhai Mineralized lamprophyreTotal rock87Rb-86Sr28.2[56]
19Zhenyuan Laowangzhai Mineralized lamprophyrePhlogopite40Ar-39Ar26.4 ± 0.2[55]
20Zhenyuan Laowangzhai Mineralized ultrabasic rocksChromium hydromica87Rb-86Sr32.8[56]
21Zhenyuan Laowangzhai Mineralized ultrabasic rocksChromium hydromica87Rb-86Sr39.6[56]
22Zhenyuan Laowangzhai Altered minetteBiotite87Rb-86Sr49.3[57]
23Zhenyuan LaowangzhaiL-48Auriferous quartz veinQuartzESR37.9[54]
24Zhenyuan LaowangzhaiL-12Auriferous quartz veinQuartzESR54.2[54]
25Zhenyuan LaowangzhaiW-26Auriferous quartz veinQuartzESR47.4[54]
26Zhenyuan Laowangzhai Sericite40K-40Ar50[58]
27Zhenyuan LaowangzhaiC02-11Quartz porphyryZirconSHRIMP248 ± 1[59]
28Zhenyuan LaowangzhaiC02-11Quartz porphyryZirconLA-ICP-MS247.7 ± 1.7[59]
29Zhenyuan LaowangzhaiC03-19Quartz porphyryZirconLA-ICP-MS255.1 ± 2[59]
30Zhenyuan Donggualin LamprophyrePhlogopite40Ar-39Ar36.1[53]
31Zhenyuan Donggualin Auriferous quartz veinQuartz40Ar-39Ar51.8 ± 1.7[58]
32Zhenyuan Donggualin Altered mineralized rockSericite87Rb-86Sr48.9[57]
33Zhenyuan Kudumu Alkaline lamprophyreTotal rock87Rb-86Sr29.1[60]
34Zhenyuan Kudumu Altered mineralized rockChromium hydromica87Rb-86Sr64.2[57]
35Zhenyuan Kudumu Altered mineralized rockSericite87Rb-86Sr61.1[57]
36Zhenyuan Langnitang LamprophyrePhlogopite40K-40Ar30.39 ± 0.46[53]
37Zhenyuan Langnitang LamprophyrePhlogopite40K-40Ar30.95 ± 0.46[53]
38Zhenyuan Xiachahe Auriferous quartz vein, mylonite, hypermyloniteHydrothermal Phlogopite40Ar-39Ar43.68 ± 0.32[61]
39Yuanyang DapingHBD-42Auriferous quartz veinQuartzESR58[54]
40Yuanyang DapingHBD-20Auriferous quartz veinQuartzESR41.3[54]
41Yuanyang DapingHBD-27Auriferous quartz veinQuartzESR48.3[54]
42Yuanyang Daping Sericitization dioriteSericite40Ar-39Ar33.76 ± 0.65[62]
43Yuanyang Daping Lamprophyre 40K-40Ar49.38[53]
44Yuanyang Daping Altered tectoniteSericite40Ar-39Ar33.76 ± 0.65[62]
45Yuanyang Daping DioriteZirconSHRIMP773 ± 12[63]
46Yuanyang Daping DioriteZirconLA-ICP-MS761.6 ± 7.4[47]
47Yuanyang Daping Biotite monzonitic graniteZirconLA-ICP-MS731 ± 18[47]
48Jinping Chang’an Altered quartz syenite porphyryTotal rock40K-40Ar36[64]
49Jinping Chang’an Premineralization hornblende syenite porphyryBiotite87Rb-86Sr36[65]
50Jinping Chang’anCAl7LamprophyreBiotite40Ar-39Ar35.62 ± 0.16[66]
51Jinping Chang’an LamprophyreBiotite40Ar-39Ar35.27 ± 0.74[66]
52Jinping Chang’an Mo oreMolybdeniteRe-Os34.54 ± 0.69[67]
53Jinping Chang’anCA11P32Syenite porphyryZirconLA-ICP-MS34.49 ± 0.14[68]
54Jinping Chang’anCA11P115Syenite porphyryZirconLA-ICP-MS34.47 ± 0.07[68]
55Jinping Chang’anCAC07Biotite granite porphyryZirconLA-ICP-MS33.66 ± 0.06[68]
56Jinping Chang’anCAC09Biotite granite porphyryZirconLA-ICP-MS34.30 ± 0.05[68]
57Jinping Tongchang Aplite syeniteZirconLA-ICP-MS36.0 ± 0.19[69]
58Jinping Tongchang OrthophyreZirconLA-ICP-MS34.6 ± 0.2[69]
59Jinping Tongchang Porphyry copper-molybdenum oreMolybdeniteRe-Os34.38 ± 0.46[52]
60Jinping Tongchang Mo oreMolybdeniteRe-Os34.04 ± 0.54[67]
61Jinping Tongchang Amphibole syenite porphyryBiotite40K-40Ar36[70]
62Jinping TongchangX30-13Quartz syenite porphyryWhole rock87Rb-86Sr33.9[52]
63Jinping TongchangX30-14Quartz syenite porphyryWhole rock87Rb-86Sr35.9[52]
64Jinping TongchangX30-22Quartz syenite porphyryWhole rock87Rb-86Sr36.1[52]
65Jinping Tongchang Syenite porphyryBiotite40K-40Ar37.7 ± 0.7[70]
66Jinping TongchangTC78Monzogranite porphyryZirconLA-ICP-MS35.1 ± 0.3[71]
Table
Table 3. Physical and chemical conditions of ore-forming fluids in main gold deposits in Ailaoshan metallogenic belt.
Table 3. Physical and chemical conditions of ore-forming fluids in main gold deposits in Ailaoshan metallogenic belt.
Gold DepositZhenyuan LaowangzhaiMojiang JinchangYuanyang DapingJinping Chang’an
Fluid inclusionIt is mainly composed of gas-liquid two-phase aqueous solution inclusions, CO2~H2O three-phase inclusions and two-phase CO2 inclusions, with a gas-liquid ratio of 10% to 60%Mainly gas-liquid and pure liquid inclusions, the gas-liquid ratio is generally less than 20%, containing a small amount of CO2 rich inclusions, and local fluid inclusions containing daughter crystalsBasically composed of pure CO2 inclusions, CO2~H2O three-phase inclusions, with varying CO2/H2O ratio (0–100%), with fluid inclusions containing daughter crystals locally, and rich in granulite facies quartz inclusions in the early stage.Two-phase inclusions in brine are dominant, three-phase inclusions of CO2 are rare, and the gas-liquid ratio is mostly 4% to 15%.
Homogenization temperatures of the main mineralization periods130–350 °C, the peak value is 180–240 °C200–300.0 °C279–406.5 °C,the peak value is 320–360 °C210–260 °C and 120–170 °C (two intervals)
Pressure54–81 MPa60.0–72.8 MPaEarly metallogenic stage 190–440 MPa, average 290 MPa; main metallogenic stage 133.5–340.0 MPa24–73 MPa
Depth1.9–3.3 km2.2–2.6 kmEarly metallogenic stage 7.2–16.6 km, average 11.0km; main metallogenic stage 5.1–12.9 km, average 9.4 km0.90–2.74 km
Fluid compositionsCO2-H2O-NaCl-ΣS type fluid, XCO2 < XH2O, the fluid is boiling and immiscible. The gas phase composition is basically CO2, with a small amount of CH4 in the early stage.CO2-H2O-NaCl-ΣS type fluid, XCO2 < XH2O, no obvious boiling phenomenon, gas phase composition is mainly CO2, a small amount of N2, CH4, H2.CO2-H2O-NaCl (-ΣS) type fluid, XCO2 ≥ XH2O, the fluid has boiling and immiscibility.The gas phase composition is basically CO2 with a small amount of N2 in the early stage.CO2-H2O-NaCl (-ΣS) type fluid, XCO2 < XH2O
Salinity w(NaCleqv) %2.89–13.66, the average of 7.484.9–11.03.70–14.64, the peak value is 7.2–9.06–18
EhReducing fluidReducing fluidReducing fluidReducing fluid
Migration patterns of goldAu(HS)2−, [AuAsS3]2−Au(HS)2−Au(HS)2−-
The precipitation mechanism of goldFluid boiling-Fluid immiscibility-
References[22,85,86,87].[33,91,92,93][95,96,97,98,100,101,102,103,104,114][41,48,50,107,111,112]
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Li, Y.; Wang, D.; Wang, C.; Sun, Y.; Pu-chi, M. Geology and Geochemistry of Selected Gold Deposits in the Ailaoshan Metallogenic Belt, China: Origin of Ore-Forming Fluids. Minerals 2021, 11, 1276. https://doi.org/10.3390/min11111276

AMA Style

Li Y, Wang D, Wang C, Sun Y, Pu-chi M. Geology and Geochemistry of Selected Gold Deposits in the Ailaoshan Metallogenic Belt, China: Origin of Ore-Forming Fluids. Minerals. 2021; 11(11):1276. https://doi.org/10.3390/min11111276

Chicago/Turabian Style

Li, Yang, Denghong Wang, Chenghui Wang, Yan Sun, and MIMA Pu-chi. 2021. "Geology and Geochemistry of Selected Gold Deposits in the Ailaoshan Metallogenic Belt, China: Origin of Ore-Forming Fluids" Minerals 11, no. 11: 1276. https://doi.org/10.3390/min11111276

APA Style

Li, Y., Wang, D., Wang, C., Sun, Y., & Pu-chi, M. (2021). Geology and Geochemistry of Selected Gold Deposits in the Ailaoshan Metallogenic Belt, China: Origin of Ore-Forming Fluids. Minerals, 11(11), 1276. https://doi.org/10.3390/min11111276

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