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Article

Controls on the Distribution of Invisible and Visible Gold in the Orogenic Gold Deposits of the Yangshan Gold Belt, West Qinling Orogen, China

by
Nan Li
1,
Jun Deng
1,*,
David I. Groves
1,2 and
Ri Han
1,3,4,5
1
State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing 100083, China
2
Centre for Exploration Targeting, University of Western Australia, Crawley 6009 WA, Australia
3
Key Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
4
Institutions of Earth Science, Chinese Academy of Sciences, Beijing 100864, China
5
University of Chinese Academy of Sciences, Beijing 100049, China
*
Author to whom correspondence should be addressed.
Minerals 2019, 9(2), 92; https://doi.org/10.3390/min9020092
Submission received: 11 December 2018 / Revised: 29 January 2019 / Accepted: 1 February 2019 / Published: 4 February 2019
(This article belongs to the Special Issue Polymetallic Metallogenic System)
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Abstract

:
Six orogenic gold deposits constitute the Yangshan gold belt in the West Qinling Orogen. Gold is mostly invisible in solid solution or in the sulfide lattice, with minor visible gold associated with stibnite and in quartz-calcite veins. Detailed textural and trace-element analysis of sulfides in terms of a newly-erected paragenetic sequence for these deposits, together with previously published data, demonstrate that early magmatic-hydrothermal pyrite in granitic dike host-rocks has much higher Au contents than diagenetic pyrite in metasedimentary host rocks, but lower contents of As, Au, and Cu than ore-stage pyrite. Combined with sulfur isotope data, replacement textures in the gold ores indicate that the auriferous ore-fluids post-dated the granitic dikes and were not magmatic-hydrothermal in origin. There is a strong correlation between the relative activities of S and As and their total abundances in the ore fluid and the siting of gold in the Yangshan gold ores. Mass balance calculations indicate that there is no necessity to invoke remobilization processes to explain the occurrence of gold in the ores. The only exception is the Py1-2 replacement of Py1m, where fluid-mediated coupled dissolution-reprecipitation reactions may have occurred to exchange Au between the two pyrite phases.

1. Introduction

Gold commonly has a complex distribution in gold deposits [1,2]. The gold that occurs in the structure of common sulfide minerals, or as discrete inclusions smaller than 100 nm, is referred to as ‘invisible gold’ [3]. Worldwide, pyrite and arsenopyrite are the most common hosts for invisible gold in gold deposits [4,5,6]. The other most common occurrence of gold is in the form of visible native gold, normally as distinct inclusions or filling fractures within these sulfide minerals [7,8,9,10,11,12], but also less commonly as nuggety gold in quartz veins. In orogenic gold systems, invisible gold within sulfides is normally followed by later visible gold [13,14,15,16]. Some authors have suggested that the visible native gold was remobilized from the invisible gold in sulfides [7,14,17,18,19,20], but it is unclear how gold could be first precipitated in pyrite and then become soluble in that pyrite, without transformation to pyrrhotite, and subsequently be re-precipitated from essentially the same ore fluid just a short distance away in the same ore zone [20]. In addition to this uncertainty, factors controlling the distribution of invisible and visible gold are still unclear, with metamorphic grade; arsenic concentrations; and fluid temperature, pH, and oxidation or sulfidation state all interpreted to play important roles [14,21,22].
LA-ICP-MS is now a preferred technique for trace-element analysis of sulfides and other ore minerals, offering high sensitivities and an excellent spatial resolution [23,24,25]. Detailed interpretation of pyrite textures is critical in terms of interpreting their trace-element compositions [26,27,28,29,30,31,32]. Moreover, the correlation between the distribution of invisible/visible gold and the textures of sulfides and related ore assemblages has implications for defining ore paragenesis and the mechanisms of incorporation and/or release of invisible gold from the sulfides [24].
The West Qinling Orogen is the third largest gold province in China, with a total of >1100 t gold resources and >50 gold deposits [33,34]. Yangshan is a world-class gold belt in the southern part of the West Qinling Orogen and comprises six gold deposits, including the Anba (280 t gold), Getiaowan, Guanyinba, Gaoloushan, Nishan, and Zhangjiashan deposits. These deposits share many common features. They are all structurally-controlled, orogenic gold deposits [35] in metasedimentary rocks and granitic dikes, and have similar alteration mineralogies of quartz, sericite, and calcite and ore mineralogies of auriferous arsenian pyrite and arsenopyrite, with stibnite and visible gold. The paragenesis and geochemistry of ore minerals in the gold deposits of the Yangshan gold belt have been studied previously [36,37]. However, backscattered images (BSE) show that these previous studies ignored: (1) partial dissolution textures in the early pyrite; (2) the euhedral pyrite rims associated with the replacement of early pyrite cores by main ore-stage pyrite; and (3) the complex textures of two different pyrite generations within the main ore-stage pyrite, which can constrain the mechanisms of Au incorporation in, or release of Au from, the pyrite [17,24,32]. This study presents detailed textural and trace-element analysis of sulfides in terms of a newly erected paragenetic sequence, designed together with previously published data, to investigate the factors controlling the distribution of invisible and visible gold in the Yangshan ores to further improve genetic understanding of the deposits in the gold belt.

2. Geological Background

2.1. Regional Geology

The West Qinling Orogen is the western part of the Qinling Orogen Belt, which is viewed as the product of long-lived accretion and collision between the North China Craton, North Qinling Block, South Qinling Block, and South China Craton. The Kuanping, Shangdan, and Mianlue suture zones, respectively, separate the above continental blocks [38,39,40,41] (Figure 1).
Proterozoic metavolcanic-sedimentary formations (846–776 Ma), the oldest strata in the region, are located in the southeast of the West Qinling Orogen [42]. Cambrian, Silurian, Devonian, Carboniferous, Permian, Triassic, and Cretaceous strata are widespread, with Devonian and Triassic strata being important host rocks for gold mineralization (Figure 1) [43,44,45]. Mesozoic granitoids are widespread in the West Qinling Orogen (Figure 1). They mainly occur between the Shangdan and Mianlue suture zones or within the Mianlue suture zone and have zircon U-Pb ages of 245–185 Ma [46].
The Yangshan gold belt, along with other gold districts, is located in the Mianlue suture zone within the West Qinling Orogen and formed during post-collisional tectonism between the North and South China Craton (Figure 1) [37,47]. Large igneous intrusions are absent in the gold belt. The ~215 Ma Puziba dikes, comprising granite, aplite, and porphyry dikes, were sheared into lenses along the E-W-trending Anchanghe-Guanyinba Fault, which is a secondary fault of the Mianlue suture zone [46].

2.2. Deposit Geology

The deposits of the Yangshan gold belt are mainly hosted by Devonian phyllite and Triassic granitic dikes. Among the six gold deposits in the Yangshan gold belt, the Anba gold deposit hosts more than 90% of the gold resources in the district. However, all the deposits in the gold belt have similar geological and mineralogical characteristics [50,51].
Ore bodies in the gold belt are structurally controlled by the three splays (F1, F2, and F3) of the Anchanghe-Guanyinba Fault (Figure 2). Some of the ore bodies are also controlled by competency contrasts along contact zones between granitic dikes and phyllite (Figure 3a) [37].
Major ore minerals in the gold belt include pyrite, arsenopyrite, and stibnite. Disseminated ores in phyllite or granitic dikes are the dominant ore type, with minor pyrite-arsenopyrite quartz veins, stibnite-bearing quartz veinlets, and quartz-calcite veins (Figure 3b–f) [36,37,52]. The diagenetic pyrite (Py0) has a framboidal or colloform texture and is disseminated in the metasedimentary host rocks. Hydrothermal mineralization is divided into an early ore-stage (Py1–quartz), a main ore-stage (Py2–Apy2–quartz–sericite), and a late ore-stage (Py3–Apy3–stibnite–native gold–calcite–quartz). Pyrite is rare in the post-ore-stage quartz–calcite veins [37]. The alteration developed in the deposits is dominated by silicification, carbonation, sulfidation, and sericitization (Figure 3e). Gold is mostly invisible in solid solution or in the sulfide lattice, with minor visible gold associated with stibnite [36].

3. Analytical Techniques

Determination of mineral paragenesis was complemented by petrological work under transmitted and reflected light, and SEM. Based on careful examination of the mineral paragenesis, a suite of eight samples of pyrite from the granitic dikes (Table 1) was selected for LA-ICP-MS analyses at the U.S. Geological Survey, Denver, USA. Six samples are from the Anba gold deposit, and one sample each from the Guanyinba and Nishan gold deposits (Table 1), which are located to the east and west of Anba, respectively (Figure 2). These three deposits are considered representative of the Yangshan gold belt. Grey-green equigranular to porphyritic granitic dikes include granite, plagioclase granite, granite porphyry, and plagioclase granite porphyry, which are common to all three deposits. The primary minerals in the dikes are plagioclase, quartz, and biotite, which are commonly altered to sericite, chlorite, epidote, and clays.
The LA-ICP-MS analyses on pyrite were conducted on a Photon Machines Analyte G2 193 nm laser ablation system attached to a Perkin Elmer ELAN DRC-e ICP-MS. Laser ablation ICP-MS methods for pyrite are based on [26,53]. Both 15- and 30-micron diameter laser spots were used for the analyses. A laser fluence of 2 J/cm2 and frequency of 5 Hz were used for the analyzed spots. Helium was used as a carrier gas. Calibration was conducted using the USGS MASS-1 sulfide reference material run five to ten times at the beginning of each session, following the procedures of [54] and using Fe as the internal standard element [26]. Concentration calculations were carried out using off-line data processing following the equations of [54]. The MASS-1 reference material was run periodically to monitor for drift. During these analytical sessions, drift was less than five percent for all elements. A stoichiometric value of 46% Fe was used for the LA-ICP-MS concentration calculations. Detection limits were calculated as three times the standard deviation of the blank [54] and are shown in Table S1. Data were examined for the presence of mineral inclusions or zoning recorded in the time resolved spectra as deviations from a stable signal (e.g., [26,53]). Because some data are below the detection limits of the analytical techniques, corrections are necessary for the incorporation into the statistical method. Data qualified with a “less than” value were replaced with 0.7 times the detection limit.

4. Textures of Pyrite and Mineral Paragenesis

Core-rim zonation is common in pyrite from deposits in the Yangshan gold belt, with the earlier-formed Py0 and Py1 as the core, and the main ore-stage Py2 as the rim of the pyrite [36,37]. In this study, a more detailed analysis of pyrite textures improves paragenetic understanding of the deposits from the Yangshan gold belt.

4.1. Partial Dissolution Textures of Py1m

To distinguish different Py1 cores, the Py1 hosted by the granitic dikes is named Py1m and Py1 from metasedimentary rocks is named Py1s. Besides the normal core-rim texture formed by Py1m and Py2, the partial dissolution texture of Py1m is recognized in this study. The inner Py1m core has been partially replaced and overgrown by a Py2 rim and formed a new pyrite generation (Py1-2), which has a brighter response in BSE images than Py1m and is therefore distinguishable from Py1m and Py2 in such images. Furthermore, Py1-2 retains the shape of Py1m through pseudomorphic replacement (Figure 4a–h).

4.2. Complex Textures within Py2

Within the traditional main ore-stage Py2, an irregular bright pyrite band (a few micrometres wide) with As enrichment is recognized in BSE images. The pyrite within the bright band is named Py2a and the pyrite exterior to it is named Py2b (Figure 4c,d; Figure 5a–h). Fine-grained arsenopyrite is located around the bright band, whereas relatively coarse-grained prismatic arsenopyrite is paragenetically associated with Py2b (Figure 5a–h).

4.3. Mineral Paragenesis

Recognition of the pseudomorphic replacement texture between Py1 and Py2, and the bright band with arsenopyrite enrichment within Py2, leads to the improvement of the paragenetic sequence diagram of the Yangshan gold belt (Figure 6). The multiple generations of pyrite from early diagenesis through the peak- to post- ore-stage, as well as trace-element evolution of the sulfides during the pre- to main- ore-stage described below, indicate more complicated ore-forming processes than were previously supposed to exist in the Yangshan gold belt.

5. Trace Element Compositions of Pyrite and Arsenopyrite

As there is only minor pyrite in the diagenetic, late-, and post-ore stages, and their geochemistry is summarized by [36], the geochemistry of newly recognized Py1m, Py1-2, Py2a, and Py2b from the pre- and main-ore stage mineralization is emphasized in this paper (Table 1). A total of 119 LA-ICP-MS spot analyses were completed on various pyrite generations from Yangshan. A total of nine elements were analysed and interpreted in this study: Ag, As, Au, Bi, Co, Cu, Ni, Pb, and Sb. The pyrite results, together with Apy2b and stibnite data from [37], are given in Table S1 and elemental variation is presented in Figure 7. Representative pyrite textures and geochemistry within single pyrite grains are shown in Figure 8 and Figure 9.
The median As contents in Py1m, Py1-2, Py2a, and Py2b are 3221, 28672, 28583, and 30,868 ppm, with ranges of 109-45803, 2454-32613, 2103-39768, and 10501-48107 ppm, respectively. The median Au contents in Py1m, Py1-2, Py2a, and Py2b are 3.7, 71, 56, and 28.2 ppm, with ranges of <0.39–54, 9.88–207, 0.2–337, and <0.64–123 ppm, respectively (Table S1). Although there is considerable variation, the As and Au contents in Py1-2, Py2a, and Py2b are higher than Py1m (Figure 7a and Figure 10; Table S1), as also shown by the As and Au contents of single pyrite grains (Figure 8 and Figure 9). Py1-2 has the highest Au content compared with Py1m, Py2a, and Py2b (Figure 9 and Figure 10). There is a decreasing trend of Au contents from Py1-2, through Py2a, to Py2b (Figure 10; Table S1). Py2b has the highest As, Cu (median 347 ppm), and Sb (median 67.5 ppm) contents compared to Py1m, Py1-2, and Py2a (Figure 10; Table S1).
The median Cu contents in Py1m, Py1-2, Py2a, and Py2b are 55.2, 91.8, 103, and 347 ppm, with ranges of <13.9–708, 15.2–159, 5.43–730, and 16.5–826 ppm, respectively (Table S1). Generally, Cu contents increase from early Py1m, through Py1-2 and Py2a, to Py2b.
The median Pb contents in Py1m, Py1-2, Py2a, and Py2b are 401, 108, 48.4, and 53.4 ppm, with ranges of 0.46–3089, 28–418, 0.5–825, <0.27–338 ppm, respectively (Table S1). The median Bi contents in Py1m, Py1-2, Py2a, and Py2b are 28.6, 6.3, 4.3, and 3 ppm, with ranges of <0.98–4052, 2.41–12.4, 0.24–89.1, and <0.11–23.4 ppm, respectively (Table S1). Lead and Bi contents decrease from Py1m, through Py1-2 and Py2a, to Py2b.
The median Co contents in Py1m, Py1-2, Py2a, and Py2b are 209, 44.3, 50.2, and 44 ppm, with ranges of 7.32–2262, 15.8–354, 0.99–947, and 2.11–291 ppm, respectively. The median Ni contents in Py1m, Py1-2, Py2a, and Py2b are 82.1, 14, 23.1, and 27.7 ppm, with ranges of <18.8–2582, <3.41–133, <3.41–606, and <3.41–410 ppm, respectively (Table S1). Cobalt and Ni contents broadly parallel Pb and Bi, but there is lower Co and Ni in Py1-2 (Figure 7 and Figure 10; Table S1).
The Au-As correlation becomes weaker from early Py1m, through Py1-2 and Py2a, to Py2b (Table S2). For Py1-2, there is a strong positive correlation between Au and Cu, which is unique among all pyrite stages (Table S2). Cobalt and Ni contents show a positive correlation among all pyrite generations (Figure 7b; Table S2). Lead and Bi in Py2a and Py2b have a strong positive correlation compared with that of the same elements in Py1 and Py1-2 (Figure 7c; Table S2).
As summarized in [37], the Au content of Apy2b ranges from <0.046 to 1205 ppm (median 15.4 ppm, average 143 ppm), whereas the Au content of late ore-stage stibnite ranges from 0.02 to 0.42 ppm (median 0.08 ppm, average 0.12 ppm).

6. Discussion

6.1. Invisible and Visible Gold in the Gold Ores

Py1m within granitic dike host-rocks has a low Au content (<0.39~54 ppm, median 3.7 ppm), which is lower than the Au values in later generations of pyrite, but is higher than the gold values in diagenetic pyrite in phyllite (median 0.32 ppm; [37]). The δ34S values of pyrite cores (Py1m in this study) in granitic dikes from the Yangshan gold belt have a very limited range from 0 to 1.3‰, consistent with a magmatic–hydrothermal origin [55]. Similar magmatic-hydrothermal pyrite from the Wallaby gold deposit in Western Australia has median gold values of 0.35 ppm, with individual spot data as high as 78 ppm [56]. LA-ICP-MS analysis also shows that gold contents range from <0.03 to 2.1 ppm in the magmatic-hydrothermal cores of pyrites in syenite from the Chang’an gold deposit, China [57].
The magmatic-hydrothermal Py1m has lower contents of As, Au, and Cu than ore-stage pyrite, but the values are higher than the As, Au, and Cu contents in other magmatic-hydrothermal pyrites described by [56,57]. The contrast in element patterns between Py1m and ore-stage pyrites, combined with their erratic, more negative δ34S values [50,58], indicate that the auriferous ore-fluids were not magmatic-hydrothermal in origin. Considering the sharp contact between Py1m and Py1-2, and the low metamorphic grade in the region, the replacement textures clearly shown by Py1-2 raise the possibility that the enhanced Au values of Py1m resulted from fluid-mediated coupled dissolution-reprecipitation reactions [17,20,24,32,59,60].
According to the flotation test report, the contents of pyrite, arsenopyrite, and stibnite in the primary ores are 2.02%, 0.93%, and 0.18%, respectively [61]. Based on observations under the microscope, the contents of Py0, Py1s, Py1m, Py1-2, Py2a, Py2b, Apy2b, and stibnite in the ores are estimated to be 0.005%, 0.005%, 0.005%, 0.005%, 1.5%, 0.5%, 0.93%, and 0.18%, respectively. Using the average gold contents of pyrite, arsenopyrite, and stibnite from each ore stage (0.26 ppm, 0.82 ppm, 11.81 ppm, 105.98 ppm, 70.05 ppm, 36.91 ppm, 143 ppm, 0.12 ppm, for Py0, Py1s, Py1m, Py1-2, Py2a, Py2b, Apy2b, and stibnite, respectively; Table S1) [37], the invisible gold contained in sulfide in one tonne of ore is calculated to be 1.3 × 10−5 g, 5.9 × 10−4 g, 4.1 × 10−5 g, 5.3 × 10−3 g, 1.05 g, 0.18 g, 1.33 g, and 2.2 × 10−4 g for Py0, Py1s, Py1m, Py1-2, Py2a, Py2b, Apy2b, and stibnite, respectively. Clearly, Py2a, Py2b, and Apy2b are the only significant contributors to the gold budget. The total invisible gold locked in the structures of pyrite, arsenopyrite, and stibnite in one tonne of ore is 2.57 g. As 83.73% of gold is located in sulfides with 16.27% as visible gold that is enclosed in other minerals [61], there is 0.50 g native gold in one tonne of ore. Therefore, there is a calculated 3.07 g gold in one tonne of ore. The calculated gold grade is lower than the reported average gold grade (4.76 g/t) [62], which may be caused by the limited number of arsenopyrite samples in this study. In previous studies of Yangshan gold deposits, arsenopyrite has been shown to have Au contents as high as 4719 ppm (average 2073 ppm) [63]. This average is about 15 times greater than that of this study. Using the average Au content in [63] would add 18 g Au to the total gold budget, which would clearly exceed the known gold grade. The true Au content of arsenopyrite must lie between that of [63] and this study, but closer to this study.

6.2. Controls on the Distribution of Invisible and Visible Gold

The replacement of Au-As-poor Py1 by Au-As-rich Py2 and the formation of As-Au-rich Py1-2 indicate that the pre-ore magmatic-hydrothermal Py1m became unstable and was partially replaced during ingress of the auriferous ore fluid, with Py1-2 rimming the Py1m cores and tending to form crystal shapes. No arsenopyrite was developed in this stage to compete with pyrite for Au distribution, leading to the high Au concentrations in Py1-2, which was then overgrown by Py2a, b.
The bright pyrite band between Py2a and Py2b in BSE images, which is the reaction front of replacement [17], has a high As content (Figure 8), indicating that the ore fluid evolved to be As-rich during the late main-ore stage. Py2b has the highest As content, but the lowest Au content, of all main ore-stage pyrites, consistent with its very low Au-As correlation coefficient (Table S2). This is due to the fact that Au preferentially entered the lattice of arsenopyrite that was intimately intergrown with Py2b, as also shown by [51]. Py2b contains more Sb than Py1m, Py1-2, and Py2a, which indicates Sb enrichment during the late main ore-stage. Once stibnite formed in the absence of pyrite or arsenopyrite, there was no suitable host for invisible gold and free gold was deposited in cracks or on grain surfaces of the earlier-formed sulfides, as also described by [36,37].
The physicochemical parameters of ore formation in the Yangshan gold belt are estimated as follows. Based on the micro-thermometry of primary fluid inclusion, the mineralization temperatures of the main ore-stage and late ore-stage were 288~300 °C, and 271~288 °C, respectively [51,52]. The sulfur fugacity during the main ore-stage at the Yangshan gold belt can be estimated to have been 10−10.3~10−11.1, which is similar to the calculated sulfur fugacity (10−10.4) based on the As contents in arsenopyrite [51]. The sulfur fugacity during the late ore-stage is estimated to have been 10−13.5~10−11.1 (Figure 11). Temperature and sulfur fugacity are two important factors controlling the stability of stibnite [64,65]. During the main ore-stage, pyrite and arsenopyrite precipitated at temperatures between 288 and 300 °C, and the majority of gold occurred within the lattices of pyrite and arsenopyrite. The precipitation of pyrite and arsenopyrite reduced the concentration of available reduced sulfur in the ore fluid. During the late ore-stage, the temperature decreased to 271~288 °C and the sulfur fugacity to 10−13.5~10−11.1, leading to the decrease of antimony solubility and precipitation of stibnite and native gold [64,66].

7. Conclusions

The textural and geochemical characteristics of sulfides indicate multiple pulses of evolving hydrothermal fluids, with As becoming more abundant and S species less abundant with time until cessation of the main ore-stage. Arsenian pyrite was the dominant host for invisible gold until arsenopyrite became a common ore mineral and became the main host for invisible gold. Only once both pyrite and arsenopyrite ceased to be deposited did free gold become the dominant gold phase. There is thus a strong correlation between the relative activities of S and As and their total abundances in the ore fluid and the siting of gold in the Yangshan gold ores. Mass balance calculations indicate that there is no necessity to invoke remobilization processes to explain the occurrence of either invisible or visible gold in the ores. The only exception is for the Py1-2 replacement of Py1m, where fluid-mediated coupled dissolution-reprecipitation reactions may have occurred to exchange Au between the two pyrite phases.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/9/2/92/s1, Table S1: LA-ICP-MS elemental data for pyrite in typical gold deposits from Yangshan gold belt (in parts per million); Table S2: Correlation coefficient matrix diagram of trace-element contents of pyrite in this study.

Author Contributions

N.L. and J.D. conceived this contribution; N.L. and R.H. prepared the experiments; N.L. performed the experiments and wrote the original draft; N.L. and D.I.G. reviewed and edited the draft, with D.I.G. making several significant additions to interpretations.

Funding

This study was financially supported by the National Natural Science Foundation of China (Grant No. 41702072); the National Basic Research Program of China (Grant No. 2015CB452605); the Public Welfare Scientific Research Funding of China (Grant No. 201411048); the Geological investigation work project of the China Geological Survey (Grant No. 12120114038301); 111 Project of the Ministry of Education, China (Grant No. B07011); and the MOST Special Fund from the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Grant No. MSFGPMR201804).

Acknowledgments

We are grateful to Liqiang Yang, who made constructive comments on the manuscript. We would like to thank Xingzhong Ji, Zhichao Zhang, and Yuchen Zhao from China University of Geosciences, Beijing, for their assistance with field work. We are grateful for constructive comments by the reviewers.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Simplified geological map of the West Qinling Orogen, showing the distribution of major crustal blocks, fault systems, and Mesozoic granitoids [47,48,49]. CCO, Central China Orogen; M, Mianlue; NCB, North China Block; SCB, South China Block; SCS, South China Sea; TLF, Tancheng–Lujiang Fault. (a): Tectonic overviews showing the position of West Qinling Orogen: (b): Schematic map showing the tectonic setting and distribution of gold deposits in West Qinling.
Figure 1. Simplified geological map of the West Qinling Orogen, showing the distribution of major crustal blocks, fault systems, and Mesozoic granitoids [47,48,49]. CCO, Central China Orogen; M, Mianlue; NCB, North China Block; SCB, South China Block; SCS, South China Sea; TLF, Tancheng–Lujiang Fault. (a): Tectonic overviews showing the position of West Qinling Orogen: (b): Schematic map showing the tectonic setting and distribution of gold deposits in West Qinling.
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Figure 2. Geological map and cross-section of the Yangshan gold belt. Red stars and blue box are the sampling locations [37].
Figure 2. Geological map and cross-section of the Yangshan gold belt. Red stars and blue box are the sampling locations [37].
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Figure 3. Ore styles and ore minerals from the Anba gold deposit. (a) The fault contact between granite porphyry dike and phyllite. (b) Pyrite is developed along the fault contact between granite porphyry and phyllilte. (c) Pyrite in phyllite and quartz vein. (d) Pyrite in granite porphyry. (e) Silicification, sericitization, and pyrite mineralization in granite porphyry. (f) Arsenopyrite coexists with the outer rim of pyrite. Apy, arsenopyrite; Cal, calcite; Py, pyrite; Qz, quartz; Ser, sericite.
Figure 3. Ore styles and ore minerals from the Anba gold deposit. (a) The fault contact between granite porphyry dike and phyllite. (b) Pyrite is developed along the fault contact between granite porphyry and phyllilte. (c) Pyrite in phyllite and quartz vein. (d) Pyrite in granite porphyry. (e) Silicification, sericitization, and pyrite mineralization in granite porphyry. (f) Arsenopyrite coexists with the outer rim of pyrite. Apy, arsenopyrite; Cal, calcite; Py, pyrite; Qz, quartz; Ser, sericite.
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Figure 4. BSE images showing the pseudomorphous replacement textures of Py1 and Py2. (a,b): Sample number SM1-3-2; (c,d): Sample number SM1-3-3; (e,f): Sample number SM1-3-4; (g,h): Sample number SM4-2-25-2.
Figure 4. BSE images showing the pseudomorphous replacement textures of Py1 and Py2. (a,b): Sample number SM1-3-2; (c,d): Sample number SM1-3-3; (e,f): Sample number SM1-3-4; (g,h): Sample number SM4-2-25-2.
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Figure 5. BSE images showing the bright band and replacement textures of Py2a and Py2b. (a,b): Sample number AB10PD4-108(2)-5; (c,d): Sample number YS-AB-10-PD1-03-4; (e,f): Sample number AB10PD4-108(2)-11; (g,h): Sample number AB10PD4-108(2)-12.
Figure 5. BSE images showing the bright band and replacement textures of Py2a and Py2b. (a,b): Sample number AB10PD4-108(2)-5; (c,d): Sample number YS-AB-10-PD1-03-4; (e,f): Sample number AB10PD4-108(2)-11; (g,h): Sample number AB10PD4-108(2)-12.
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Figure 6. Paragenetic sequence of gold mineralization and alteration of the gold deposits of the Yangshan gold belt. The bold lines indicate high abundance, the thin lines represent the minor amounts, and the discontinuous lines indicate uncertainty in the determination of the paragenetic sequence due to the lack of a clear textural relationship [35].
Figure 6. Paragenetic sequence of gold mineralization and alteration of the gold deposits of the Yangshan gold belt. The bold lines indicate high abundance, the thin lines represent the minor amounts, and the discontinuous lines indicate uncertainty in the determination of the paragenetic sequence due to the lack of a clear textural relationship [35].
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Figure 7. Trace-element binary plots of Au against (a) As, (b) Ni, (c) Pb, and (d) Ag for Yangshan pyrites. The line in (a) is the inferred solubility limit of gold in arsenian pyrite [21]. The trace-element concentrations are from Table S1, or calculated using 0.7 times mdl (minimum detection limit) values for all measurements <mdl.
Figure 7. Trace-element binary plots of Au against (a) As, (b) Ni, (c) Pb, and (d) Ag for Yangshan pyrites. The line in (a) is the inferred solubility limit of gold in arsenian pyrite [21]. The trace-element concentrations are from Table S1, or calculated using 0.7 times mdl (minimum detection limit) values for all measurements <mdl.
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Figure 8. The core-rim texture of pyrite in sample SM1-3-3 and the trace-element contents analysed by LA-ICP-MS within each zone.
Figure 8. The core-rim texture of pyrite in sample SM1-3-3 and the trace-element contents analysed by LA-ICP-MS within each zone.
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Figure 9. The core-rim texture of pyrite in sample YS-AB-10-PD1-03-7 and the trace-element contents analysed by LA-ICP-MS within each zone.
Figure 9. The core-rim texture of pyrite in sample YS-AB-10-PD1-03-7 and the trace-element contents analysed by LA-ICP-MS within each zone.
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Figure 10. Box plot of trace-element concentrations of Yangshan pyrite. Boxes represent interquartile range (data between 25th and 75th percentiles), with top and bottom lines extending 1.5 times the interquartile range toward the maximum and minimum, respectively.
Figure 10. Box plot of trace-element concentrations of Yangshan pyrite. Boxes represent interquartile range (data between 25th and 75th percentiles), with top and bottom lines extending 1.5 times the interquartile range toward the maximum and minimum, respectively.
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Figure 11. Temperature versus log fs2 (g) diagram showing stability fields of minerals recorded in main and late-ore stages at the Yangshan gold belt [67]. Orange represents the stability field of main-ore stage pyrite and arsenopyrite, and red represents the stability field of late ore-stage stibnite. As-arsenic, Asp-arsenopyrite, Lo-loellingite, Orp-orpiment, Po-pyrrhotite, Py-pyrite, Rl-realgar, S-sulfur, Sb0-native antimony, Stb-stibnite.
Figure 11. Temperature versus log fs2 (g) diagram showing stability fields of minerals recorded in main and late-ore stages at the Yangshan gold belt [67]. Orange represents the stability field of main-ore stage pyrite and arsenopyrite, and red represents the stability field of late ore-stage stibnite. As-arsenic, Asp-arsenopyrite, Lo-loellingite, Orp-orpiment, Po-pyrrhotite, Py-pyrite, Rl-realgar, S-sulfur, Sb0-native antimony, Stb-stibnite.
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Table
Table 1. Descriptions of the samples analysed in this study. Samples listed in a hierarchical manner under Deposit and then Sample Number.
Table 1. Descriptions of the samples analysed in this study. Samples listed in a hierarchical manner under Deposit and then Sample Number.
DepositSample NumberLithologyPyrite Stage
AnbaAB10PD4-102Granite porphyry dike with quartz-calcite veinPy1m
AnbaAB10PB4-108_2Granite porphyry dike with quartz veinPy2a, Py2b
AnbaSM1-3GranitePy1m, Py1-2, Py2a, Py2b
AnbaYS-AB-10-PD1-01Plagioclase granite dike with quartz-calcite veinsPy1m, Py2b
AnbaYS-AB-10-PD1-03Granite dike in fault zone with quartz veinPy1m, Py1-2, Py2a, Py2b
AnbaYS-AB-10-PD1-04Plagioclase granite porphyry dike with quartz veinPy1m, Py2b
GuanyinbaZK054-4GranitePy2a, Py2b
NishanYS-NS-10-05Plagioclase granite porphyry dikePy2b

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Li, N.; Deng, J.; Groves, D.I.; Han, R. Controls on the Distribution of Invisible and Visible Gold in the Orogenic Gold Deposits of the Yangshan Gold Belt, West Qinling Orogen, China. Minerals 2019, 9, 92. https://doi.org/10.3390/min9020092

AMA Style

Li N, Deng J, Groves DI, Han R. Controls on the Distribution of Invisible and Visible Gold in the Orogenic Gold Deposits of the Yangshan Gold Belt, West Qinling Orogen, China. Minerals. 2019; 9(2):92. https://doi.org/10.3390/min9020092

Chicago/Turabian Style

Li, Nan, Jun Deng, David I. Groves, and Ri Han. 2019. "Controls on the Distribution of Invisible and Visible Gold in the Orogenic Gold Deposits of the Yangshan Gold Belt, West Qinling Orogen, China" Minerals 9, no. 2: 92. https://doi.org/10.3390/min9020092

APA Style

Li, N., Deng, J., Groves, D. I., & Han, R. (2019). Controls on the Distribution of Invisible and Visible Gold in the Orogenic Gold Deposits of the Yangshan Gold Belt, West Qinling Orogen, China. Minerals, 9(2), 92. https://doi.org/10.3390/min9020092

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