Signiﬁcance of Calcite Trace Elements Contents and C-O Isotopic Compositions for Ore-Forming Fluids and Gold Prospecting in the Zhesang Carlin-Like Gold Deposit of Southeastern Yunnan, China

: The Zhesang gold deposit of southeastern Yunnan is an important component of the Dian-Qian-Gui (Yunnan, Guizhou, and Guangxi) “Golden Triangle”, which hosts a multitude of Carlin-like gold deposits (CLGDs). Calcite is one of the most common gangue minerals in Zhesang. The calcites that have been found in the mining area are classiﬁed as ore-stage and post-ore calcites. The ore-stage calcite exhibits a clear paragenetic relationship with gold-bearing arsenopyrite and with an alteration halo that has been cut by the post-ore interaction. The ore-forming ﬂuids of the Zhesang gold deposit may be associated with the intrusion of diabase that outcrops in the mining area, and that the basic magmatic activities of the Indosinian period also provided some of the ore-forming materials and heat for gold mineralization.

that the ore-forming fluid derived from crustal fluids. Gao and Huang [30] suggested that the Zhesang ore-forming fluid is a mixture of magmatic and meteoric waters. Wei et al. [28] proposed that the deep-seated magma triggered fluids of possibly meteoric origin to circulate and leach out ore-forming elements from sedimentary rocks to form the Zhesang gold deposit.
Minerals 2019, 9, x FOR PEER REVIEW 3 of 24 controversial. Pi et al. [27] and Dai et al. [31] believed that the ore-forming fluid derived from crustal fluids. Gao and Huang [30] suggested that the Zhesang ore-forming fluid is a mixture of magmatic and meteoric waters. Wei et al. [28] proposed that the deep-seated magma triggered fluids of possibly meteoric origin to circulate and leach out ore-forming elements from sedimentary rocks to form the Zhesang gold deposit. Carbonate minerals such as calcite and dolomite are the products of carbonatization recrystallization in Carlin-like (-type) gold deposits, and they are closely related to gold mineralization in these deposits [6,7,29]. In the northern gold deposits of Dian-Qian-Gui, including Shuiyindong, Banqi, Bojitian, Taipingdong, and Zimudang, it has been shown that the ore-stage calcite characteristics within these deposits are enriched in MREE and HREE [7,20,[32][33][34][35]. However, systematic studies about gold deposits in the southern part of Dian-Qian-Gui are scarce. In this paper we have analyzed the rare earth element (REE), C, and O isotopic characteristics of calcites from the Zhesang gold deposit to constrain the origins of the ore-forming fluids. More importantly, the trace elements contents (Fe, Mn, and Mg) of calcites were combined to examine possible guidelines for prospecting gold resources.

Regional Geological Setting
The Zhesang gold deposit is located at the junction between the Qiubei-Guangnan fold belt and the eastern end of the Wenshan-Funing fold belt [36], and it is controlled by the Guangnan- Carbonate minerals such as calcite and dolomite are the products of carbonatization recrystallization in Carlin-like (-type) gold deposits, and they are closely related to gold mineralization in these deposits [6,7,29]. In the northern gold deposits of Dian-Qian-Gui, including Shuiyindong, Banqi, Bojitian, Taipingdong, and Zimudang, it has been shown that the ore-stage calcite characteristics within these deposits are enriched in MREE and HREE [7,20,[32][33][34][35]. However, systematic studies about gold deposits in the southern part of Dian-Qian-Gui are scarce. In this paper we have analyzed the rare earth element (REE), C, and O isotopic characteristics of calcites from the Zhesang gold deposit to constrain the origins of the ore-forming fluids. More importantly, the trace elements contents (Fe, Mn, and Mg) of calcites were combined to examine possible guidelines for prospecting gold resources.

Regional Geological Setting
The Zhesang gold deposit is located at the junction between the Qiubei-Guangnan fold belt and the eastern end of the Wenshan-Funing fold belt [36], and it is controlled by the Guangnan-Funing Fault ( Figure 1). The faults of the area can be divided into two periods; the NE-trending faults are older faults, whereas the NW-and near EW-trending faults are younger ( Figure 2) [28]. The width of the NE-trending faults zone is approximately 800 m, length is around 3000 m, and dips to the SE with an angle from 60 • to 70 • . The NW-trending faults generally dip to the NE with an angle of about 65 • [37]. Magmatic activity is extremely intense in this region, and its intrusive rocks mainly consist of diabase and gabbro-diabase, which occur as dykes (Figures 1-3 and Figure 4a,b). The effusive rocks are generally basalts. The basic rocks can be divided into two periods, the older has zircon U-Pb age of 258 ± 5 Ma, and it is viewed as a component of the Permian Emeishan large igneous province [38]. The younger has zircon U-Pb ages between 215 ± 5 Ma and 219.9 ± 6.6 Ma, and it is suggested as the product of the Indosinian movement [27,28,39].
Minerals 2019, 9, x FOR PEER REVIEW 4 of 24 Funing Fault ( Figure 1). The faults of the area can be divided into two periods; the NE-trending faults are older faults, whereas the NW-and near EW-trending faults are younger ( Figure 2) [28]. The width of the NE-trending faults zone is approximately 800 m, length is around 3000 m, and dips to the SE with an angle from 60° to 70°. The NW-trending faults generally dip to the NE with an angle of about 65° [37]. Magmatic activity is extremely intense in this region, and its intrusive rocks mainly consist of diabase and gabbro-diabase, which occur as dykes (Figures 1, 2, 3, and 4a,b). The effusive rocks are generally basalts. The basic rocks can be divided into two periods, the older has zircon U-Pb age of 258 ± 5 Ma, and it is viewed as a component of the Permian Emeishan large igneous province [38]. The younger has zircon U-Pb ages between 215 ± 5 Ma and 219.9 ± 6.6 Ma, and it is suggested as the product of the Indosinian movement [27,28,39].      The NEE-trending Zhesang anticlinorium, with axis trending around 60 • , hinge dips to E, dip angle of around 20 • , and primarily consists of the Wujiaping Formation and Luolou Formation, is the main structure of the mining area, and the gold ore bodies are mainly located at its SE limb [27][28][29][30][31]37]. The outcropping strata in the mining area are as follows (in increasing age): The Middle Triassic Baifeng Formation (T 2 b), Lower Triassic Luolou Formation (T 1 l), Upper Permian Wujiaping Formation (P 3 w), and Upper Permian basalts (P 2 β) (Figures 2 and 3). The outcropping orebodies in this mining area include No. I-VIII, with the largest of these orebodies being No. VI and VII. The orebodies are near-parallel trending in a NE direction. The No. I, II, V, VI, and VII orebodies are located in the organic-matter-rich carbonaceous siltstones, muddy siltstones, tuffaceous siltstones, and dolomites of the Wujiaping Formation. The No. III and VIII orebodies are located near the contact zone between the diabases and siltstones of the Lower Triassic Luolou Formation (Figures 2 and 4a). A minor amount of pyritization and arsenopyritization has been observed along the margin of gabbro-diabase dykes. The orebodies occur as 50-1000 m long stratiform lenticles, with surface outcrops that are 3-40 m wide. The density of the orebodies generally varies between 1.5 and 2.6 g/t, with a maximum of 9 g/t [40].

Alteration Features
The host-rock alteration types of the Zhesang gold deposit include pyritization, arsenopyritization, carbonatization, silicification, and argillic alteration (illite). The calcites occurring at the ore district can be divided into ore-stage and post-ore stage based on the field investigation and petrographic and mineralogical observation ( Figure 4c). The ore-stage calcites occur as white or pale-yellow veins with alteration halo containing calcite, quartz, pyrite, arsenopyrite, and limonite alteration halo and are cut by the post-ore calcite. The paragenesis of calcite and gold-bearing arsenopyrite assemblages are observed in hand specimens in the ore-stage calcite veins and their alteration selvages. It is also found that the arsenopyrite exhibits a clear paragenetic relationship with the ore-stage calcites (Figure 4d), while the post-ore calcites occur as fine, white veins, and no sulfides were observed during the examination of hand specimens and microscope.

Sampling and Analytical Methods
Analytical tests were performed on seven ore-stage calcite samples and three post-ore calcite samples. The sampling locations and characteristics of each sample are shown in Table 1. Samples were firstly crushed into 40-60 mesh grains and then washed in ultrapure water to remove impurities. After the samples were dried, calcites were selected one by one using a binocular microscope. Finally, an agate mortar was used to ground the selected calcite samples to a fineness of 200 mesh. Analytical tests of trace elements and stable isotope were subsequently performed on these samples.

Trace Elements Analyses
The calcite REEs, Fe, Mn, and Mg concentrations of the studied samples were analyzed at the Institute of Geochemistry Chinese Academy of Science, using inductively coupled plasma-mass spectrometry (ICP-MS) and Inductively Coupled Plasma Optical Emission Spectrometer (ICP-OES) instrument. About 50 mg sample powder was digested with HF and HNO 3 in PTFE-lined stainless-steel bombs at 185 • C for 24 h, evaporated to dryness, and re-dissolved by 6 mL of 40% (v/v) HNO 3 at 140 • C for 3 h. The solution was introduced to ICP-MS for the measurement of REEs, and ICP-OES for Fe, Mn, and Mg analysis, and the analysis errors were ±5% and ±10%, respectively [41].

Stable Isotope Analyses
The calcite C and O isotopes of the samples were studied at the Kunming University of Science and Technology. Phosphoric acid (100%) method was used in the analytical tests. Around 60 • C, the sample reacts with phosphoric acid to release CO 2 , and the C and O isotopes were determined by stable isotope mass spectrometer (Isoprime 100). Samples were placed in the Multiflow gas preparation system infused with 4 mL 100% H 3 PO 4 and then vacuumed for 7-8 h for keeping the pressure at 4.0 Pa. CO 2 was separated by liquid helium, and the purified CO 2 gas was introduced to the mass spectrometer for the measurement of isotopic ratios. C and O isotope values are reported in per mil relative to V-PDB (Vienna-Pee Dee Belemnite) and V-SMOW (Vienna-Standard Mean Oceanic Water), respectively [42]. The analytical precision was ± 0.2% .

Rare Earth Element Characteristics of the Calcites and Wall Rocks
The REE and Y contents and chondrite-normalized patterns of the ore-stage, post-ore calcites, and wall rocks of the Zhesang gold deposit are shown in Table 2 and Figure 5. There are two widely used schemes for REE classification (excluding Y and Sc). In the first scheme, REEs are divided into light rare earth elements (LREE = La-Nd), middle rare earth elements (MREE = Sm-Ho), and heavy rare earth elements (HREE = Er-Lu); in the second scheme, REEs are divided into LREE* (LREE* = La-Eu) and HREE* (HREE* = Gd-Lu). In this work, the first scheme in combination with the chondrite-normalized REE diagrams has been used [43].   (1) The ore-stage calcites have ΣREE (not including Y, and the same application below) values between 7.13 and 23.01 μg/g, and they have an REE pattern typical of MREE enrichment (MREE/LREE = 1.11-1.61, MREE/HREE = 6.12-8.22). The ore-stage calcites have a weak negative Eu anomaly (Eu/Eu* = 0.75-0.82) and no significant Ce anomaly (Ce/Ce* = 0.92-1.15). (

C-O Isotopic Characteristics of the Calcites
The C-O isotopic characteristics of ore-stage and post-ore calcites from the Zhesang gold deposit are shown in Table 3. The δ 13 C V-PDB values of the seven ore-stage calcite samples ranged between −3.50 and −0.90% (maximum difference of 2.6% ), with an average of −1.72% . The δ 18 O V-SMOW values of the ore-stage calcite samples ranged between 11.03 and 12.49% (maximum difference of 1.46% ), with an average of 11.93% . Therefore, the δ 13 C V-PDB and δ 18 O V-SMOW values of the ore-stage calcite samples vary over a relatively large range. The δ 13 C V-PDB values of the three post-ore calcite samples ranged between −1.93 and −1.02% (maximum difference of 0.91% ), and their average δ 13 C V-PDB value was −1.34% . The δ 18 O V-SMOW values of these samples ranged between 16.48 and 17.14% (maximum difference of 0.66% ) with an average of 16.87% . Therefore, the δ 13 C V-PDB and δ 18 O V-SMOW values of the post-ore calcite vary over a small range.

Fe, Mn, and Mg Contents of Calcites
The Fe, Mn, and Mg contents (Table 4) of the ore-stage calcites were in the range of 4690-6300, 1007-1316, and 1080-2760 µg/g, respectively. While the post-ore calcites were in the range of 2030-2730, 1162, and 900-1680 µg/g, respectively. Hence, ore-stage calcites have significantly higher Fe contents than post-ore calcites, as the Fe contents of the former are 2-3 times of the latter. The Mn and Mg contents of the two stages samples were not significantly different.

Calcite Genesis
A calcite sample may belong to one of the three genetic regimes (pegmatitic, hydrothermal, and sedimentary genesis) depending on its Yb/La and Yb/Ca ratio. Accordingly, Yb/La and Yb/Ca ratios can be used to determine the genesis and evolution of a calcite sample [44][45][46]. The ore-stage and post-ore calcites of the Zhesang gold deposit were projected onto a Yb/La-Yb/Ca diagram, and it was observed that all the samples fell in the hydrothermal region ( Figure 6). This indicates that all calcites were formed via hydrothermal activity. As the geochemical properties of each REE are different, the cogeneity of gangue minerals in a metallogenic system can be examined by comparing their LREE and HREE ratios [47][48][49]. Based on a study about the REE geochemistry of calcites in the Tannenboden and Beihilfe deposits, Bau and Dulski [48] observed that cogenetic gangue minerals generally exhibit a horizontal distribution in the Y/Ho-La/Ho diagram. The post-ore calcites from Zhesang show constant Y/Ho values and are horizontally distributed on the La/Ho-Y/Ho diagram, while ore-stage calcites show significantly different Y/Ho values and they do not project onto the same horizontal line (Figure 7). This may imply that post-ore calcites are cogenetic and they may have formed by a single fluid, but ore-stage calcites may be formed by a mixing of different fluids.  As the geochemical properties of each REE are different, the cogeneity of gangue minerals in a metallogenic system can be examined by comparing their LREE and HREE ratios [47][48][49]. Based on a study about the REE geochemistry of calcites in the Tannenboden and Beihilfe deposits, Bau and Dulski [48] observed that cogenetic gangue minerals generally exhibit a horizontal distribution in the Y/Ho-La/Ho diagram. The post-ore calcites from Zhesang show constant Y/Ho values and are horizontally distributed on the La/Ho-Y/Ho diagram, while ore-stage calcites show significantly different Y/Ho values and they do not project onto the same horizontal line (Figure 7). This may imply that post-ore calcites are cogenetic and they may have formed by a single fluid, but ore-stage calcites may be formed by a mixing of different fluids. As the geochemical properties of each REE are different, the cogeneity of gangue minerals in a metallogenic system can be examined by comparing their LREE and HREE ratios [47][48][49]. Based on a study about the REE geochemistry of calcites in the Tannenboden and Beihilfe deposits, Bau and Dulski [48] observed that cogenetic gangue minerals generally exhibit a horizontal distribution in the Y/Ho-La/Ho diagram. The post-ore calcites from Zhesang show constant Y/Ho values and are horizontally distributed on the La/Ho-Y/Ho diagram, while ore-stage calcites show significantly different Y/Ho values and they do not project onto the same horizontal line (Figure 7). This may imply that post-ore calcites are cogenetic and they may have formed by a single fluid, but ore-stage calcites may be formed by a mixing of different fluids.   [50]. On the other hand, ultrabasic-basic magmatic rocks are characterized by O isotope compositions of about 5% [51], and the O isotopes > 8% are characteristic of supra crustal rocks like granite or rocks that have assimilated crustal materials [52]. There are five mechanisms by which CO 2 enters ore-forming fluids from these source regions: The dissolution and decarbonation of carbonate minerals, the carboxyl and oxidation of sedimentary organic matter, and the degassing that accompanies the fractional crystallization of mantle magmas [53]. As these mechanisms also lead to the co-fractionation of C and O isotopes, the mutual constraints arising from these mechanisms can be used to trace the source of CO 2 in a geological fluid [44,54,55]. The C and O isotopic data of the ore-stage and post-ore calcites were projected onto a δ 18 O V-SMOW -δ 13 C V-PDB diagram ( Figure 8). The two stages of calcites fell on the same trend of marine carbonate dissolution; however, they differ significantly in their O isotopic characteristics, and the ore-stage calcites fell on the side closer to basic rocks. As it is shown before, some orebodies of Zhesang are hosted by the diabases (Figures 2 and 4a), and the mineralization age (215.3 ± 1.9 Ma) of Zhesang is in good accordance with the forming age (219.9 ± 6.6 Ma) of basic rocks in the region [27,28]. Therefore, it is reasonable that the ore-forming fluids may be associated with the diabase outcropped in the mining district. However, there is no apparent difference in C isotope; this may have resulted from the significant differences between C and O composition in basic magma, in which O content (44.57%) is apparently higher than C content (0.14%) [54]. Li and Yao [56] showed that the average water content in basic magma is around 2.02%, and basic magma is usually poor of volatiles. This may imply that the amount of ore-forming fluids provided by the diabase is limited. Therefore, it can be concluded that the C and O isotopes of both stages of fluids were mainly sourced from meteoric water and marine carbonate interaction, but the ore-stage fluid was contaminated by a small amount of basic magmatic fluids. 8‰ are characteristic of supra crustal rocks like granite or rocks that have assimilated crustal materials [52]. There are five mechanisms by which CO2 enters ore-forming fluids from these source regions: The dissolution and decarbonation of carbonate minerals, the carboxyl and oxidation of sedimentary organic matter, and the degassing that accompanies the fractional crystallization of mantle magmas [53]. As these mechanisms also lead to the co-fractionation of C and O isotopes, the mutual constraints arising from these mechanisms can be used to trace the source of CO2 in a geological fluid [44,54,55]. The C and O isotopic data of the ore-stage and post-ore calcites were projected onto a δ 18 OV-SMOW-δ 13 CV-PDB diagram (Figure 8). The two stages of calcites fell on the same trend of marine carbonate dissolution; however, they differ significantly in their O isotopic characteristics, and the ore-stage calcites fell on the side closer to basic rocks. As it is shown before, some orebodies of Zhesang are hosted by the diabases (Figures 2 and 4a), and the mineralization age (215.3 ± 1.9 Ma) of Zhesang is in good accordance with the forming age (219.9 ± 6.6 Ma) of basic rocks in the region [27,28]. Therefore, it is reasonable that the ore-forming fluids may be associated with the diabase outcropped in the mining district. However, there is no apparent difference in C isotope; this may have resulted from the significant differences between C and O composition in basic magma, in which O content (44.57%) is apparently higher than C content (0.14%) [54]. Li and Yao [56] showed that the average water content in basic magma is around 2.02%, and basic magma is usually poor of volatiles. This may imply that the amount of ore-forming fluids provided by the diabase is limited. Therefore, it can be concluded that the C and O isotopes of both stages of fluids were mainly sourced from meteoric water and marine carbonate interaction, but the ore-stage fluid was contaminated by a small amount of basic magmatic fluids. The Dian-Qian-Gui Golden Triangle contains a large number of CLGDs. By reviewing the C isotopic data of calcites in the Zhesang, Shuiyindong [58], Bojitian [33], Miaolong-Paiting [59], and Taipingdong-Zimudang gold deposits [34], it was discovered that the C isotopic compositions of the calcites of the Dian-Qian-Gui region generally ranged between −8.80 and 3.51‰ V-PDB ( Figure 9). Therefore, it may be concluded that the carbon in the CLGD of Dian-Qian-Gui primarily originated from marine carbonates and the deep mantle. The Dian-Qian-Gui Golden Triangle contains a large number of CLGDs. By reviewing the C isotopic data of calcites in the Zhesang, Shuiyindong [58], Bojitian [33], Miaolong-Paiting [59], and Taipingdong-Zimudang gold deposits [34], it was discovered that the C isotopic compositions of the calcites of the Dian-Qian-Gui region generally ranged between −8.80 and 3.51% V-PDB ( Figure 9). Therefore, it may be concluded that the carbon in the CLGD of Dian-Qian-Gui primarily originated from marine carbonates and the deep mantle.

Significance of Calcite REE Characteristics
It is possible to discern the origin of the ore-forming materials of a deposit by comparing the REE patterns of various geological bodies to those of the hydrothermal minerals [61]. The formation of calcites is intimately accompanied with the entire mineralization process in the Zhesang gold deposit. Therefore, the REE geochemistry of the calcites can reflect the REE characteristics of the ore-forming fluids of the deposit.
The ore-stage calcites of Zhesang exhibit a typical MREE enrichment, similar to the ore-stage calcites found in many of the CLGDs in Qianxinan [22,[32][33][34]59]. Such a characteristic is inconsistent with the significant LREE enrichment observed in post-ore calcites and the host strata (which consists of phyllitic calcareous slate, rhyolitic tuff, spilite, diabase, muddy siltstone, and tuff) [29,62]. In addition, hydrothermal fluids originated from meteoric water usually have low REE concentrations (ranging from 1 to nearly 10 -6 times chondrite) and show an LREE-enriched pattern [61]. It is shown that REEs were not simply derived from meteoric water or host rocks. Castorina et al. [63] and Ehya [64] suggested that the REE abundance in hydrothermal fluids depends mainly on the deposition order of the REE-bearing minerals, regardless of the ultimate REE source. However, in the Zhesang ore district, or even in the whole "Dian-Qian-Gui golden triangle" region, the dominant minerals are quartz, pyrite, arsenopyrite, and calcite. It is widely accepted that these minerals, except calcite, usually have extremely low REE contents, and they do not show any tendency in combination with different types of REE (e.g., LREE, MREE or HREE). Also, there have no minor minerals typical enrichment of LREE or HREE been reported. Combined with the above discussion about C and O isotopes, and the study of the H-O isotopic characteristics (H: −70.2 -−46.5‰; O: 6.7 -13.9‰) of fluid inclusions within quartz conducted by Gao and Huang [30], they suggested that the ore-forming fluids of the primary metallogenic stage of the deposit were derived from a mix of meteoric water and magmatic water. Hence, it is inferred that partial REE of ore-forming fluids may be sourced from basic magmatic fluids. Nonetheless, it cannot be ignored that rare earth fractionation could also have been caused by complexation, coprecipitation, adsorption, desorption, and other processes [61,[65][66][67].

Significance of Calcite REE Characteristics
It is possible to discern the origin of the ore-forming materials of a deposit by comparing the REE patterns of various geological bodies to those of the hydrothermal minerals [61]. The formation of calcites is intimately accompanied with the entire mineralization process in the Zhesang gold deposit. Therefore, the REE geochemistry of the calcites can reflect the REE characteristics of the ore-forming fluids of the deposit.
The ore-stage calcites of Zhesang exhibit a typical MREE enrichment, similar to the ore-stage calcites found in many of the CLGDs in Qianxinan [22,[32][33][34]59]. Such a characteristic is inconsistent with the significant LREE enrichment observed in post-ore calcites and the host strata (which consists of phyllitic calcareous slate, rhyolitic tuff, spilite, diabase, muddy siltstone, and tuff) [29,62]. In addition, hydrothermal fluids originated from meteoric water usually have low REE concentrations (ranging from 1 to nearly 10 -6 times chondrite) and show an LREE-enriched pattern [61]. It is shown that REEs were not simply derived from meteoric water or host rocks. Castorina et al. [63] and Ehya [64] suggested that the REE abundance in hydrothermal fluids depends mainly on the deposition order of the REE-bearing minerals, regardless of the ultimate REE source. However, in the Zhesang ore district, or even in the whole "Dian-Qian-Gui golden triangle" region, the dominant minerals are quartz, pyrite, arsenopyrite, and calcite. It is widely accepted that these minerals, except calcite, usually have extremely low REE contents, and they do not show any tendency in combination with different types of REE (e.g., LREE, MREE or HREE). Also, there have no minor minerals typical enrichment of LREE or HREE been reported. Combined with the above discussion about C and O isotopes, and the study of the H-O isotopic characteristics (H: −70.2-−46.5% ; O: 6.7-13.9% ) of fluid inclusions within quartz conducted by Gao and Huang [30], they suggested that the ore-forming fluids of the primary metallogenic stage of the deposit were derived from a mix of meteoric water and magmatic water. Hence, it is inferred that partial REE of ore-forming fluids may be sourced from basic magmatic fluids. Nonetheless, it cannot be ignored that rare earth fractionation could also have been caused by complexation, coprecipitation, adsorption, desorption, and other processes [61,[65][66][67].
The post-ore calcites exhibit a significant degree of LREE enrichment, which is similar to the REE pattern of muddy siltstones in the host strata [31]. However, the host rocks have higher REE contents than these calcites, which also exhibit positive Eu anomalies. This indicates that the post-ore calcites were mainly formed by fluids (like meteoric water) that leached the host rocks of the mining area. The difference between the post-ore calcites and host rocks in terms of their total REE contents is indicative of the degree of REE leaching from the host rocks.
In summary, the REE, C-O isotopic data characteristics of the calcites, and H-O isotopic characteristics of fluid inclusions in quartz form the Zhesang gold deposit indicate the following: the ore-forming fluids were mainly derived from crustal fluids and a small amount of basic magmatic fluids, whereas post-ore fluids were consisted of crustal fluids generated by the infiltration of meteoric water through the host rocks.
The ore-stage calcites show weak, negative Eu anomaly, while post-ore calcites show significant, positive Eu anomaly. Generally, REE 3+ has different properties from Ce 4+ and Eu 2+ . In some geochemical processes, the separation of Ce 4+ , Eu 2+ , and REE 3+ will occur, and the Ce and Eu anomalies will be positive or negative [61,[68][69][70]. Temperature is the most important parameter controlling the Eu/Eu* redox potential in a hydrothermal environment [66]. Möller et al. [71] suggested Eu anomaly is lacking or slightly positive in fluorite precipitated from a fluid with a temperature < 200 • C. At temperatures > 200 • C, Eu 3+ is reduced to Eu 2+ , which is very mobile and difficult to be incorporated into the fluorite structure, and therefore tends to remain in the fluid; this produces negative Eu anomalies in fluorites precipitated from a fluid with > 200 • C. The ore-stage calcites may have formed above 200 • C, which is proved by the fluid inclusion study (the homogenization temperature of ore fluids in Zhesang, 194-295 • C) conducted by Gao and Huang [30]. The high temperature may reduce Eu 3+ to Eu 2+ . The weak, negative Eu anomalies also indicate that the precipitation of the ore-forming fluids occurred in a weakly reducing environment. This is consistent with the large amounts of sulfides (e.g., arsenopyrites and pyrites) that appeared during the mineralization epoch. The post-ore calcite was formed under 200 • C (unpublished), and the low temperature could oxidize Eu +2 , which is derived from host rocks, to Eu +3 . Therefore, the Eu anomaly of calcites may be mainly affected by temperature [72].

Calcite Formation Process and Au Deposition
Many studies have demonstrated that gold deposition in Carlin-like (-type) gold deposits is closely related to the decarbonatization of their host strata, as this process provides the Fe required by the sulfidation processes that occurs during gold precipitation [14,20,73]. CO 2 was likely the principal acid volatile in the ore fluids and could promote dissolution of the ferroan calcite in the host rocks [1,14]: Reaction (2) is representative of decarbonation reactions in Carlin-type systems. This reaction provides Fe elements for calcites. Fe is probably mobilized as Cl complexes in fluids, (e.g., FeCl 2 ). The formation of Fe-rich carbonate is due to the ion radii of Fe 2+ being similar to Ca 2+ , so that Fe 2+ can easily enter the lattice of carbonate to replace Ca 2+ . The precipitation of gold and Fe-containing sulfides (e.g., arsenopyrite and pyrite) in large quantities will also form large amounts of Fe-rich calcite simultaneously. Hence, Fe-rich carbonate is always an important product in the mineralization of Carlin-like (-type) gold deposits.
In Table 4 and Figure 10, it is shown that the Fe contents of ore-stage calcites are significantly higher than those of post-ore calcites. The different concentration of Fe 2+ in calcite at different stages may be due to the different initial fluid Fe content. According to previous discussion about the source of ore-forming fluid, it is found that the ore-stage fluid not only comes from the crustal fluid by meteoric water leaching wall rocks, but also from the basic magmatic fluid, and the post-ore fluid mainly comes from the dissolution of host rocks by meteoric water. These calcites are possibly formed by the following Reactions (3) and (4), respectively:  Therefore, the ore-stage calcite Fe is not only from the dissolution of the host rocks, but also from the basic magma, while the Fe constituent of post-ore calcite mainly comes from the dissolution of host rocks.
Gold is commonly associated with sulfide minerals such as pyrite and arsenopyrite in Carlin-like (-type) gold deposits [74]. Much of this gold is present as "invisible" gold (particles less than 0.1 µm), and many studies have shown that the gold consists either of submicroscopic metallic particles or is incorporated as "chemically bound" gold [75][76][77][78][79]. Simon et al. [80,81] concluded that gold in arsenian pyrite occurs in solid solution (Au 1+ ) and as nanoparticles of native gold (Au 0 ). In ore-forming fluids, the most likely ligands for complexation with Au + are HS − , Cl − , and OH − [82]. Deposition from gold sulfide complexes is of importance in gold precipitation processes [83]. Most models for deposition of gold are based on the assumption that Au is transported as bisulphide complexes (e.g., Au(HS) − 2 ) [84]. Numerous studies of Carlin-type gold deposits in Nevada have concluded that gold-rich arsenian pyrite precipitated from H 2 S-rich fluids, which sulfurized iron-bearing minerals in the host rocks [1,14,85]. The predominant As species was H 3 AsO 0 3 (aq) . Such as determined from the geochemical modeling calculations above, Zhesang gold deposit could have deposited gold-bearing arsenopyrite, possibly by the following reaction: This reaction is strongly dependent on the activity of reduced sulfur (as H 2 S or HS − ), and a decrease in H 2 S produced by sulfidation would promote the formation of arsenopyrite. The reaction involves reduction of As(3+) and Au(1+) by consumption of H 2(g) , which can be provided by reaction of the metal-transporting fluids with the local organic-rich sediments [16]. So Au, S, and As are migrated in the form of [Au(HS) 2 ] − , H 2 S, and H 3 AsO 0 3 (aq) in the ore-forming fluid. When H 2 is added to the ore-forming fluids, Au, S, and As precipitate to form invisible gold-bearing arsenopyrite and pyrite. Through the above discussion about the source of Fe constituent of calcite, it is inferred by this reaction that Au is also sourced from the host rocks and basic magmas. Such inference is also supported by the previous studies about gold contents of wall rocks and diabases and S-Pb isotopes in the Zhesang gold deposit [30,31,62]. High Au abundances have been observed in the carbonaceous and muddy siltstones of the Upper Permian Wujiaping Formation, and the fine sandstones and diabases of the Lower Triassic Luolou Formation; their Au abundances are 91.7, 6.5, and 59.5 times the Clarke value of gold (0.001 ppm) [86], respectively. Furthermore, according to the S-Pb isotopic characteristics, it is suggested that the Pb elements of the deposit mainly originated from the upper crust, with some from magmatic components [39]. Therefore, it can be concluded that the ore-forming materials of the Zhesang gold deposit include contributions both from the host strata and basic diabase rocks.
Summing up the above discussion and previous studies [27,30,31,40,87], a conceptual genetic model of the Zhesang gold deposit is proposed as follows: (1) From Late Permian to Early Triassic, large amounts of gold-bearing sandstone strata were deposited in Funing County. During Indosinian movement, the NE-striking faults and secondary fold structures were formed. Then the lithosphere began to stretch, and the NE-striking faults and secondary fold structures took place and had tensional activity, thus forming passages that enabled the flow of ore-forming fluids, as well as storage spaces for mineral deposition. (2) The intrusion of large amounts of basic magma (at about 215 Ma) [27] in this region provided some of the ore-forming materials, fluids and heat that led to gold deposition. This basic magma also heated deep-circulating waters derived from meteoric water, which leached the source strata. This led to the activation and migration of ore-forming elements (including Au) from the source strata, and ultimately induced the gold mineralization.

Guidelines Provided by Calcite REE, Fe, and O Isotopic Compositions for Gold Prospecting
All calcites found in the mining area were either ore-stage or post-ore calcites. There are significant differences between these calcites in terms of their REE patterns, Fe contents, and O isotopic compositions. Therefore, the MREE/LREE, MREE/HREE, and LREE/HREE ratios, Fe contents, and δ 18 O V-SMOW values of the calcite samples have been analyzed to examine possible guidelines that could be of use for gold prospecting (Figures 10-12).   The average MREE/HREE ratios of the seven ore-stage calcite samples (7.16) and three post-ore calcite samples (4.21) were used as the representative MREE/HREE ratios of all ore-stage and post-ore calcites, respectively. The average MREE/HREE ratio of the ore-stage and post-ore calcites (5.69) was treated as the boundary between ore-stage and post-ore calcites in terms of the MREE/HREE ratio. A correlation diagram was plotted between the Fe contents and the MREE/HREE ratios of the calcite samples, which was then divided into four quadrants according to the average Fe content (3827 μg/g) and MREE/HREE ratio (5.69) of these samples (Figure 10b). The average Fe content of the seven ore-stage calcite samples (5367 µg/g) was treated as the Fe content of all ore-stage calcites; similarly, the average Fe content of the three post-ore calcite samples (2287 µg/g) was treated as the Fe content of all post-ore calcites. The average Fe content of these calcites (3827 µg/g) was then treated as the boundary between ore-stage and post-ore calcites in terms of Fe content.
Similarly, the average MREE/LREE ratios of the ore-stage and post-ore calcite samples were treated as the MREE/LREE ratios of the ore-stage and post-ore calcites (1.34 and 0.50, respectively). The average MREE/LREE ratio (0.92) of the calcite samples was then used as the boundary between ore-stage and post-ore calcites in terms of the MREE/LREE ratio. A correlation diagram was plotted between the Fe contents and the MREE/LREE ratios of the calcite samples, which was then divided into four quadrants according to the average Fe content (3827 µg/g) and MREE/LREE ratio (0.92) of the samples (Figure 10a).
The average MREE/HREE ratios of the seven ore-stage calcite samples (7.16) and three post-ore calcite samples (4.21) were used as the representative MREE/HREE ratios of all ore-stage and post-ore calcites, respectively. The average MREE/HREE ratio of the ore-stage and post-ore calcites (5.69) was treated as the boundary between ore-stage and post-ore calcites in terms of the MREE/HREE ratio. A correlation diagram was plotted between the Fe contents and the MREE/HREE ratios of the calcite samples, which was then divided into four quadrants according to the average Fe content (3827 µg/g) and MREE/HREE ratio (5.69) of those samples (Figure 10b).
The average LREE/HREE ratios of the seven ore-stage calcite samples (5.40) and three post-ore calcite samples (9.67) were used as the representative LREE/HREE ratios of all ore-stage and post-ore calcites, respectively. The average LREE/HREE ratio between the ore-stage and post-ore calcites (7.54) was treated as the boundary that delineates ore-stage and post-ore calcites in terms of the LREE/HREE ratio. A correlation diagram was plotted between the Fe contents and the LREE/HREE ratios of the calcite samples, which was then divided into four quadrants according to the average Fe content (3827 µg/g) and LREE/HREE ratio (7.54) of the samples (Figure 10c).
The average MREE/HREE ratios of the seven ore-stage calcite samples (7.16) and three post-ore calcite samples (4.21) were used as the representative MREE/HREE ratios of all ore-stage and post-ore calcites, respectively. The average MREE/HREE ratio of the ore-stage and post-ore calcites (5.69) was treated as the boundary between ore-stage and post-ore calcites in terms of the MREE/HREE ratio. A correlation diagram was plotted between the Fe contents and the MREE/HREE ratios of the calcite samples, which was then divided into four quadrants according to the average Fe content (3827 µg/g) and MREE/HREE ratio (5.69) of these samples (Figure 10b).
The average δ 18 O V-SMOW value of the seven ore-stage calcite samples (11.93% ) and three post-ore calcite samples (16.87% ) were used as the representative δ 18 O V-SMOW value of all ore-stage and post-ore calcites, respectively. The average δ 18 O V-SMOW value of the ore-stage and post-ore calcites (14.40% ) was treated as the boundary between ore-stage and post-ore calcites in terms of the δ 18 O V-SMOW value. A correlation diagram was then plotted between the Fe contents and the δ 18 O V-SMOW values of the calcites, which was divided into four quadrants using the average Fe content (3827 µg/g) and δ 18 O V-SMOW (14.40% ) value of the calcite samples ( Figure 11). Similarly, δ 18 O V-SMOW versus MREE/LREE and δ 18 O V-SMOW versus MREE/LREE correlation diagrams were plotted (Figure 10a,b), which were divided into quadrants using the average δ 18 O V-SMOW value (14.40% ), MREE/LREE value (0.92), and MREE/HREE value (5.69) of the ore-stage and post-ore calcite samples. In Figure 11c, it is shown that the LREE/HREE ratio cannot be used to distinguish the two stages calcites, which indicates that it is difficult to use the LREE/HREE ratio of a calcite sample as a prospecting guideline. Therefore, a correlation diagram was not plotted between the LREE/HREE ratios and the δ 18 O V-SMOW values of the calcite samples.
In Figure 10a,b, it is shown that all ore-stage calcites fall in the second quadrant, whereas all post-ore calcites fall in the third quadrant. In Figure 10c, all ore-stage calcites fall in the fourth quadrant, whereas all post-ore calcites fall in the first and third quadrants. In Figure 11, all ore-stage calcites fall in the fourth quadrant, whereas all post-ore calcites fall in the first quadrant. In Figure 12a,b, all ore-stage calcites fall in the first quadrant, whereas all post-ore calcites fall in the fourth quadrant.
As a whole, it is shown that the ore-stage calcites generally have Fe contents greater than 3827 µg/g, whereas the post-ore calcites lower than 3827 µg/g. In terms of REE ratios, the ore-stage calcites generally have MREE/LREE ratios greater than 0.92, whereas the post-ore calcites lower than 0.92. The MREE/HREE ratios of the ore-stage calcites and post-ore calcites are generally greater and lower than 5.69, respectively, thus indicating that the ore-stage calcites have a greater degree of MREE enrichment than the post-ore calcites. In terms of the O isotopic indicator (δ 18 O V-SMOW ), the ore-stage and post-ore calcites generally have δ 18 O V-SMOW values lower and greater than 14.40% , respectively. Therefore, the MREE/LREE ratio (0.92), MREE/HREE ratio (5.69), Fe content (3827 µg/g), and δ 18 O V-SMOW value (14.40% ) of calcites in the Zhesang gold deposit can be used as prospecting guidelines. If a calcite sample falls in the second quadrant of Figure 10a,b, the fourth quadrant of Figure 11, and the first quadrant of Figure 12a,b, it is implied that the calcite sample was present during the hydrothermal event that occurred during gold mineralization. Hence, these geochemical features could potentially serve as prospecting guidelines. The mineralization of CLGD leads to the formation of calcites enriched in MREEs and relatively depleted in LREEs and HREEs. Other than the Zhesang gold deposit, this characteristic is also widely observed in the CLGD of Qianxinan Prefecture [7,22,[32][33][34][35]. Wang et al. [32] discovered that calcites in the Banqi gold deposit of Qianxinan are enriched in Fe and MREEs. Yan et al. [88] found that the C-O isotope and La/Gd ratio of calcite in the CLGD of Qianxinan could be used to construct the function model to guide the prospecting guidelines, and the accuracy was as high as 100%. Tan et al. [35] suggested that C and O isotope ratios have a significant role in mineral exploration by delineating regions of rocks that have been altered by ore-forming fluids. On the other hand, C and O isotope compositions from typical unaltered limestone to high-grade ores have been used to map the extent of hydrothermal systems and have provided useful guides for the exploration of hydrothermal deposits worldwide [89][90][91][92][93], particularly for Carlin-type gold deposits in Nevada, USA. O isotopes of carbonate in host rocks were measured and show marked depletion proximal to gold mineralization for Carlin-type gold deposits at Vantage [94], Carlin [95], Pipeline [96,97], Screamer [98], and Banshee [99]. Calcites are major gangue minerals in Carlin-like (-type) gold deposits, and are found in most of the CLGD of southeastern Yunnan. Therefore, the aforementioned indicators may serve as important guidelines for gold prospecting in this region.

Conclusions
(1) The calcites that outcrop in the mining area of the Zhesang gold deposit are either ore-stage or post-ore calcites. Although both stages of calcites were formed by hydrothermal fluids, they have different sources. Based on the REE and C-O isotopic characteristics of the calcites, it is determined that the precipitating fluids of ore-stage calcite were mainly derived from crustal fluids and a small amount of basic magmatic fluids, while the formation of post-ore calcite might be derived from fluid/rock interaction between meteoric water and marine carbonates. Hence, the diabases outcropping in the mining area may be related to gold mineralization. It is further deduced that the basic magmatic activity during the Indosinian movement provided some of the ore-forming materials and fluids and heat for gold mineralization in Zhesang.
(2) The ore-stage calcites from Zhesang gold deposit exhibit a significant enrichment of MREE, a relative enrichment of Fe, and somewhat low δ 18 O V-SMOW values. If a calcite sample exhibits a MREE/LREE ratio greater than 0.92, MREE/HREE ratio greater than 5.69, Fe content greater than 3827 µg/g, and δ 18 O V-SMOW value less than 14.40% , it is an ore-stage calcite, and these are important prospecting guidelines.