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Article

The Origin of the Caiyuanzi Pb–Zn Deposit in SE Yunnan Province, China: Constraints from In Situ S and Pb Isotopes

by
Yongguo Jiang
1,2,
Yinliang Cui
1,2,
Hongliang Nian
2,
Changhua Yang
2,
Yahui Zhang
3,*,
Mingyong Liu
2,
Heng Xu
2,
Jinjun Cai
2 and
Hesong Liu
3
1
Faculty of Land Resources Engineering, Kunming University of Science and Technology, Kunming 650093, China
2
Yunnan Nonferrous Geological Bureau, Kunming 650051, China
3
Key Laboratory of Critical Minerals Metallogeny in Universities of Yunnan Province, School of Earth Sciences, Yunnan University, Kunming 650500, China
*
Author to whom correspondence should be addressed.
Minerals 2023, 13(2), 238; https://doi.org/10.3390/min13020238
Submission received: 29 December 2022 / Revised: 3 February 2023 / Accepted: 5 February 2023 / Published: 8 February 2023
(This article belongs to the Special Issue Pb-Zn Deposits and Associated Critical Metals)
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Versions Notes

Abstract

:
Located at the intersection of the Tethys and Pacific Rim metallogenic belts, the Laojunshan polymetallic metallogenic province in SE Yunnan Province hosts many large-scale W–Sn and Sn–Zn polymetallic deposits. The newly discovered Caiyuanzi medium-sized Pb–Zn deposit is located in the northern part of this province and has eight sulfide ore bodies. All the ore bodies occur in the siliceous rocks of the Lower Devonian Pojiao Formation (D1p). The ore bodies are conformable with stratigraphy and controlled by a lithologic horizon. The sulfide ores have banded or laminated structures. The ore minerals are mainly pyrite, chalcopyrite, sphalerite, and galena. In this study, in situ sulfur and lead isotopes were used to constrain the origin of the Caiyuanzi Pb–Zn deposit. The results show that the in situ δ34S values of pyrite, chalcopyrite, and sphalerite range from 0.1‰ to 6.0‰, with an average of 4.7‰. This δ34S signature reflects the mixing between magmatic-derived and reduced seawater sulfate sulfur. The in situ Pb isotopes characteristics of pyrite, galena, and sphalerite suggest that the sulfur and lead of ore minerals come from the upper crust. Integrating the data obtained from the studies including regional geology, ore geology, and S–Pb isotope geochemistry, we proposed that the Caiyuanzi Pb–Zn deposit is a hydrothermal deposit formed by sedimentary exhalative and magmatic hydrothermal superimposition.

1. Introduction

The Laojunshan polymetallic metallogenic province in SE Yunnan Province is located at the intersection of the Tethys and Pacific Rim metallogenic belts. This province hosts many large-scale W–Sn and Sn–Zn polymetallic deposits, such as the Dulong super-large Sn–Zn polymetallic deposit, Xinzhai large-scale Sn polymetallic deposit, and the large-scale Nanyangtian W–Sn deposit. In recent years, one large-scale (Hongshiyan Pb–Zn) and two medium-sized (Gaji Pb–Zn-Cu polymetallic and Caiyuanzi Pb–Zn) deposits have been discovered in the northern part of the province. The Pb–Zn deposits have a total Pb, Zn, and Cu metal resource of nearly 1.2 million tons, indicating that this province has good prospecting potential for these metals.
At present, the genesis of the Pb–Zn deposits is controversial [1,2,3,4,5,6], but theories include sedimentary exhalative (SEDEX) [1,2,6], and magmatic hydrothermal origins [3,4,5]. The main reason for the diversity in genetic views is the lack of understanding of the source of ore-forming materials. In this study, the in situ S and Pb isotopes of sphalerite, galena, pyrite, and chalcopyrite are used to trace the source of metallogenic elements and to discuss the ore genesis of the Caiyuanzi Pb–Zn deposit.

2. Geological Setting

2.1. Regional Geology

The Laojunshan metallogenic province is located at the junction of the Cathaysian, Yangtze, and Indochina blocks (Figure 1a), and in the northern part of the Song Chay metamorphosed dome (Figure 1b). The sedimentary environment in this province is complex and diverse and has experienced multiple periods of large-scale magmatic intrusion [7,8,9,10,11].
Since the Cambrian, this province has experienced repeated transgression and regression, ending in late Triassic marine sedimentation. The exposed strata are Cambrian, Devonian, and Permian, which show a trend of decreasing metamorphism. The Lower Cambrian is mainly sandy argillaceous slate and schist. The abundance of carbonate rocks gradually increases in the upper Middle Cambrian; the Lower Devonian is sandy argillaceous slate, which overlies the Cambrian at a slight angle. The Middle and Upper Devonian are mesa facies carbonate rocks, and the Permian is a continental shelf carbonate with siliceous rocks [12]. There are mainly NNE- and NW-trending regional structures (Figure 1b); the former were formed in the Caledonian–Indosinian, and the latter were formed in the Indosinian–Himalayan [12]. The Nanwenhe and Laojunshan granites are the main igneous rocks, both of which are closely related to tin and zinc polymetallic mineralization in the area [10,13,14]. The Nanwenhe granites are known as the Song Chay granites in the Vietnamese part, and are also known as the Song Chay metamorphic dome [7,8]. They intruded during the late Silurian (420–440 Ma) [7,15,16], and then underwent deformation and metamorphism during the Indosinian, forming gneissic, banded, and eyeball-shaped structures [12]. The Laojunshan granites intruded during the Cretaceous (83–117 Ma) [13,14,17,18,19,20,21].

2.2. Ore Deposit Geology

2.2.1. Strata

The main strata exposed in the mining area are Devonian (Figure 2). The Lower Devonian Pojiao Formation (D1p) comprises shallow continental shelf clastic rocks; the Lower Devonian Gumu Formation (D1g) is a carbonate mesa marginal facies deposit; the Middle Devonian Donggangling Formation (D2d) is a sub-tidal sedimentary of the mesa; the Upper Devonian Gedang Formation (D3g) is a shallow facies carbonate mesa deposit. The Batang Wedge (bw) is an informal stratigraphic unit that belongs to the late Early Devonian–early Middle Devonian carbonate mesa slope facies [22]. The Pojiao Formation is the main ore-hosting layer in the mining area, which is in extensive contact with the overlying Batang Wedge, and has a transitional relationship with the Lower Posongchong Formation. It is mudstone, marl locally interspersed with quartz sandstone, carbonaceous mudstone, marl limestone lens, and has been metamorphosed into mica schist, quartz schist, siliceous dolomite, and locally siliceous rocks.
The Pojiao Formation can be subdivided into two sections [23]. The lower section (D1p1) can be divided into three beds from bottom to top, as follows: the first bed is quartz schist and siliceous dolomite; the second is quartz schist mixed with siliceous rocks; the third is carbonaceous mica schist and quartz mica schist. The upper section (D1p2) can be divided into four beds from bottom to top, as follows: the first bed is thick bedded siliceous rocks sandwiched between banded quartz schist; the second is quartz schist and siliceous dolomite interspersed with banded siliceous rocks; the third is siliceous dolomite interspersed with siliceous rock; the fourth is quartzite mica schist with quartz schist, locally sandwiched with thin siliceous bands, and locally contains striped pyrite.

2.2.2. Tectonic

The overall structural form of the mining area is a monocline that strikes EW and dips south (Figure 2). A secondary steep slope of compressive tensional NNW, near EW and NE faults developed, off the Xingjie fault (Fs). The strata of the mine area were strongly compressed, resulting in a series of soft wrinkles and folds, which were caused by the above-mentioned fault activity.

2.2.3. Ore Body

A total of eight conformable Pb–Zn strata-bound ore bodies have been found in the mining area, in the siliceous dolomite rocks layer of the Lower Devonian Pojiao Formation (D1p) (Figure 3). Ores have banded and laminated structures (Figure 4). The main ore body is spread along the banded siliceous dolomite on top of the siliceous rocks [23], which can be divided into lower and upper ore-bearing sections.

2.2.4. Texture and Structure

The ore minerals are mainly pyrite, chalcopyrite, sphalerite, and galena, with a small amount of hematite, pyrrhotite, and magnetite, and the gangue minerals are mainly calcite, quartz, and epidote. The ore minerals have euhedral granular, allomorphic granular and metasomatic residual textures. The sulfide ores have massive, disseminated, veined disseminated, banded, and laminated structures (Figure 5).
The galena, sphalerite, and chalcopyrite are mostly disseminated, veined, banded, and laminated. Pyrite is subhedral to euhedral granular, forming locally fine-grained aggregates; sphalerite and chalcopyrite are anhedral granular and aggregate; galena is allomorphic granular and aggregate. Pyrite is encapsulated and cemented by other sulfides or alternatively metasomatized, suggesting that pyrite formed early. Sphalerite, galena, and chalcopyrite often occur together where galena and chalcopyrite are replaced with sphalerite, indicating that the formation of sphalerite is later than galena and chalcopyrite, but the formation sequence of galena and chalcopyrite is difficult to determine (Figure 5).

2.2.5. Altered Wall Rocks

The wall rock alteration mainly includes silicification, skarnization, pyritization, and calcitization. The wall rock alteration has an enrichment effect on the Pb–Zn–Cu polymetallic mineralization in the mining area. Skarns include actinolite epidote skarn, and chlorite epidote skarn, which are limited to the siliceous limestone in the Pojiao Formation.

3. Sampling and Analytical Methods

3.1. Samples

All the samples were collected from the PD2 tunnel of the Caiyuanzi ore deposit. The detailed information about those samples is listed in Table 1.

3.2. Analysis Methods

The micro area in situ sulfur isotope test of sulfide was completed in Nanjing Polyspectrum Testing Technology Co., Ltd., and the galena, sphalerite, pyrite, and chalcopyrite of samples CYZ-2, CYZ-5, and CYZ-7 were selected for sulfur isotope analyses. The mass spectrometer model is the Nu Plasma II MC-ICPMS, and the laser model is Analytical Excite. The deep ultraviolet beam generated by the laser generator is focused on the sulfide surface through the homogenizing optical path. First, the gas background is collected for 40 s, and then the appropriate beam spot (pyrite 33 μm; sphalerite 40 μm; chalcopyrite 50 μm) at a 5 Hz frequency for 35 s, before the aerosol is sent out of the denudation pool by helium, mixed with argon, and then enters the MC-ICPMS (single integration time is 0.3 s, and there are about 110 groups of data within the denudation time of 35 s). We used a GBW07267 pyrite cake pressed by National Geological Experimental Testing Center of Chinese Academy of Geological Sciences (δ34S = 3.6‰) and GBW07268 chalcopyrite cake pressing (δ34S = −0.3‰), and NIST SRM 123 crushed zinc blender particles (δ34S = 17.1‰) as the data quality control, and the long-term external reproducibility is about ±0.6‰ (1 SD).
Micro area in situ lead isotope testing of sulfide was completed in two testing units, respectively. The lead isotope composition analysis of samples CYZ-2 and CYZ-5 was completed in Wuhan Shangpu Analysis Technology Co., Ltd. The instrument model is the MC-ICPMS (Neptune Plus) with multi-receiver mass spectrometry, GeoLas HD with a 193 nm exciter laser ablation system, and a beam spot of 90–120 μm. Energy intensity is 6 mJ/cm2, the frequency is 8 Hz, the carrier gas (He) is 500 mL/min, collected data (pulses) are 500, and the recommended values of standard samples (Sph HYLM) are 208Pb/204Pb (38.519), 207Pb/204Pb (15.764), and 206Pb/204Pb (18.217). The lead isotope analyses of samples CYZ-1 and CYZ-3 were completed in the National Key Laboratory of Continental Dynamics, Northwest University. The mass spectrometer model is Nu Plasma II MC-ICPMS, the laser model is Quantronix Integra HE Ti 266 nm NWR UP Femto (ESI, Hartland, WI, USA), and the erosion radius is 15–65 μm. The laser frequency is 5–50 Hz, the erosion mode is 3 μm/s lines scanning, and the He airflow is 0.7 L/min. The sample standard sample cross method is adopted. The standard sample is NIST610, and the analysis error is better than 0.003 (1 σ).

4. Results

4.1. In Situ S Isotopic Compositions

The results of in situ S isotopic compositions of pyrite, chalcopyrite, and sphalerite are shown in Table 2 and Figure 6. Pyrite, chalcopyrite, and sphalerite have δ34S values between 0.1‰ and 6‰, with an average of 4.7‰ (Figure 7). Pyrite has δ34S values ranging from 4.3‰ to 6‰ (except 0.1‰ for one point), with an average of 5.40‰; sphalerite has δ34S values are between 4.7‰ and 5.3‰, with an average of 5.08‰; chalcopyrite has δ34S values are between 4.3‰ and 4.9‰, with an average of 4.67‰.

4.2. In Situ Pb Isotopic Ratios

The results of LA-MC-ICPMS in situ Pb isotopes of galena are listed in Table 3. The Pb isotopic ratios of galena are relatively uniform, with 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios of 18.134–18.202 (mean 18.158), 15.698–15.735 (mean 15.715), and 38.430–38.542 (mean 38.46), respectively.

5. Discussion

5.1. Source and Formation Mechanism of Reduced Sulfur

Sulfur isotopes are one of the most important bases for determining the source of sulfur and the formation process of sulfide deposits [24,25,26,27,28,29,30,31,32,33,34,35,36,37,38,39,40,41,42,43,44,45,46,47,48,49,50,51,52,53,54,55,56,57,58,59,60,61]. Three sources of sulfur have been proposed, as follows: (1) mantle-derived sulfur, δ34S = −3‰ to 3‰ (average 0‰); (2) sedimentary sulfur (marine sulfate), which could form reduced sulfur by thermo-chemical sulfate reduction (TSR) or bacterial sulfate reduction (BSR) [32,37]; and (3) mixed sulfur of the above two types [31].
The ore mineral assemblages of the Caiyuanzi Pb–Zn deposit are simple, with mainly pyrite, sphalerite, and galena and other sulfides. The δ34S values of the Caiyuanzi deposit are relatively homogeneous (0.1‰ to 6‰, with a mean value of 4.7‰) and positive, which may represent the δ34S∑S of the ore-forming hydrothermal fluids.
The δ34S values differ significantly from the values found in typical Mississippi Valley-type (MVT) Pb–Zn deposits, whose reduced sulfur was mainly formed by TSR and/or BSR; for example, the δ34S values of sulfides in the Daliangzi (MVT) Pb–Zn deposit are mainly 10‰ to 20‰ [39,41], while the in situ δ34S values of sulfides in the Maoping (MVT) Pb–Zn deposit ore are −20.4‰ to 25.6‰ [33,35,40].
In addition, the sulfur isotopic compositions of the Caiyuanzi Pb–Zn deposit are similar to those of the adjacent Gejiu Sn and Dulong Sn–Zn polymetallic deposits (Figure 8), whose sulfur was mainly derived from the magmatic rocks, with less marine sulfate [13,14]. For example, the δ34S values of the Gejiu deposit are mainly −3.1‰ to 8.4‰ [51], and the δ34S values of the Dulong deposit are mainly 4.2‰ to 12.4‰, most being 5.2‰–9.4‰ [10,42]. Hence, we propose that the sulfur for the Caiyuanzi deposit is mainly derived from the magmatic rocks, although some contribution from the wall rock cannot be excluded.

5.2. Source of Metals

Due to the low contents of U and Th, the proportion of radiogenic Pb in sulfide minerals is negligible. Therefore, Pb isotopes of galena could represent the Pb isotopes of the ore-forming fluids without age correction [49,50]. The in situ Pb isotopic ratios of galena from the Caiyuanzi Pb–Zn deposit obtained in this study has a narrow range (Table 3), suggesting either a single source or a high degree of homogenization in the ore-forming metals in this deposit [39]. In this paper, we collected Pb isotopic data from the Laojunshan granites, marble, schist, and ores in Dulong (Table 3). The samples of the Caiyuanzi deposit fall on the average upper crustal growth curve and mantle curve in the corresponding Figure 9a,b, respectively. The whole rock Pb isotope ratios of marble and schist are significantly different from those of the Caiyuanzi deposit (Figure 9), so the wall rocks (marble and schist) may not have provide lead to the deposit. The data of Yanshanian granites are concentrated between the orogenic belt and the upper crust, close to the upper crust, and its 208Pb/204Pb and 207Pb/204Pb ratios are consistent with the data of Caiyuanzi sample points. The Pb isotope ratios of the Caiyuanzi and Dulong deposits and the Yanshanian granites have the same distribution range and trend and are projected between the orogenic belt and the upper crustal evolution curve, indicating that the Laojunshan granites might have provided metals for the Caiyuanzi deposit. Another end member should be the underlying Proterozoic rocks, with relatively unradiogenic crustal Pb.
In addition, the μ values (238U/204Pb) of the Caiyuanzi deposit range from 9.71 to 9.76, which are between the mantle or lower crust Pb (μ = 7.86–7.94) and upper crust Pb (μ = 9.81), and so could be a mixture between them. The average value of ω is 39.14, which is closer to the upper crust Pb between normal lead (ω = 35.55 ± 0.59) and the upper crust Pb (41.860) [38]. The Th/U average value is 3.89, which is close to normal Pb (Th/U = 3.92 ± 0.9), slightly higher than the upper crust of the Chinese mainland (Th/U = 3.76). In the corresponding Pb isotope △β–△γ genetic classification diagram [55], the data point of the Caiyuanzi deposit falls in the upper crust Pb source area (Figure 10).
The Pb isotopes of the Dulong deposit and the Yanshanian granites span two source areas of upper crustal Pb and magmatic Pb, and generally show a trend from magmatic Pb to crustal Pb, suggesting that the intermediate-acidic magma rich in deep-source low μ-value Pb has been contaminated by shallow-source high μ-value Pb during ascent. The μ values of the Dulong deposit (9.56) and the Dulong Yanshanian granites (μ = 9.62) are similar to that of the Caiyuanzi deposit (μ = 9.72).
The degree of crustal contamination of magmatic hydrothermal fluids is positively correlated with the μ values [44], suggesting that the intermediate-acid magmatic hydrothermal fluids related to the Caiyuanzi Pb–Zn deposit are greatly contaminated by crustal materials. In addition, the Pb isotope of sulfides in the Caiyuanzi deposit is significantly higher in U/Pb (208Pb/204Pb > 18.000, 207Pb/204Pb > 15.300), and slightly lower in Th/Pb (208Pb/204Pb < 39.000), suggesting that the ore-forming material is dominated by upper crust lead, with a small amount of deep crust-derived magmatic Pb, showing the characteristics of orogenic belt Pb.

5.3. Ore Genesis

At present, the ore genesis of the Pb–Zn deposits in the Laojunshan area is still controversial. The focus is whether it belongs to a SEDEX deposit or a magmatic hydrothermal deposit. In this paper, the in situ S and Pb isotopes of the Caiyuanzi Pb–Zn deposit show that the sulfur was mainly derived from the mixed sources of magmatic rocks and marine sulfate, and the source of metal Pb is the upper crust. The ore bodies are strata-bound and stratiform, which resembles the SEDEX deposits (Table 4). However, the Caiyuanzi Pb–Zn deposit is characterized by epigenetic mineralization with extensive pyrrhotite and skarnization, which can be compared to the general metallogenic characteristics of magmatic hydrothermal deposits. Most of ore bodies and ores underwent some fractures and deformation. Therefore, all of these observations suggest that the Caiyuanzi Pb–Zn deposit was a product of syn-sedimentary hydrothermal exhalative and superimposed magmatic–hydrothermal ore-forming processes.
In South China, the Devonian is widely exposed and consists of carbonate and clastic deposition of large transgressive-regressive cycles [63]. The Devonian sedimentary rocks in South China host numerous SEDEX pyrite deposits, such as Dajiangping [64], and sedimentary reworking deposits, such as Huodehong [65]. The reducing environment within the early Devonian sea floor led to the rapid burial of organic matter. The reduction of marine sulfate by organic matter formed S2− and then mixed with deeply-derived Pb and Zn, etc., and eventually formed the syn-sedimentary sulfide ore bodies. During the Cretaceous, extensional tectonics developed in South China. The southeastern Yunnan–northern Guangxi and the large-scale mineralization in Late Mesozoic in western South China were controlled by a similar continental dynamic background [48]. After 135 Ma, the movement direction of the Izanagi plate in eastern China changed, from the subduction of the Eurasian continent to rapid strike-slip along a NE direction [46], and the South China region underwent lithospheric extension. As a result of the extension of the lithosphere, the lithospheric mantle has undergone underplating and upwelling, resulting in a large amount of ferromagnesian magmatism. Upwelling of this magma and underplating of the lower crust, as well as the partial melting of the lower crust, may have produced granitic melt that invaded the upper crust [45]. During this period, a large number of granite bodies were formed in southeastern Yunnan, such as the Gejiu, Laojunshan, and Bozhushan granites. At the same time, a number of world-class W–Sn polymetallic deposits related to granites were formed, such as the Gejiu, Dulong, Dachang, and Bainiuchang deposits. The newly obtained S and Pb isotopic data from Caiyuanzi suggest that the mineralization is related to the Yanshanian granites in Laojunshan. The regional magmatic hydrothermal events contributed to the Dulong Sn (diopside, garnet, and tremolite skarn) and Zn mineralization (epidote skarn, although some parts show a lack of skarn minerals), and Caiyuanzi skarnization (epidote, garnet skarn).

6. Conclusions

(1)
The sulfur and lead of ore minerals come from the upper crust and mantle.
(2)
The Caiyuanzi Pb–Zn deposit is a hydrothermal deposit formed by the superimposed magma of sedimentary exhalative.

Author Contributions

Investigation, Y.J. and Y.Z.; writing–original draft preparation, Y.J.; writing–review and editing, H.N., C.Y., M.L., H.X., J.C. and H.L.; supervision, Y.C. and Y.Z.; funding acquisition, Y.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This research was financially supported by the National Natural Science Foundation of China (No. 41802087) and the Basic Research Program of Yunnan Provincial Department of Science and Technology, China (No. 2019FB144).

Data Availability Statement

The data used to support this study are included within the article.

Acknowledgments

The field work was supported and assisted by workers of the No. 317 Geological Teams of Yunnan Nonferrous Geological Bureau. The experimental process was guided and assisted by the staff of the two laboratories. We would like to express our heartfelt thanks to them! We sincerely thank the Editorial Board members and anonymous reviewers for their constructive comments.

Conflicts of Interest

The authors declare that they have no known competing financial interest or personal relationships that could have appeared to influence the work reported in this paper.

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Figure 1. Geotectonic location map of the study area ((a), modified according to [9]) and the regional geological map ((b), quoted from [10]).
Figure 1. Geotectonic location map of the study area ((a), modified according to [9]) and the regional geological map ((b), quoted from [10]).
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Figure 2. Geological map of mining area.
Figure 2. Geological map of mining area.
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Figure 3. Profile of exploration line 0# in the Caiyuanzi Pb–Zn mining area.
Figure 3. Profile of exploration line 0# in the Caiyuanzi Pb–Zn mining area.
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Figure 4. Strata-bound ore body (a) and ores with laminated structure (b). Abbreviations are as follows: Py, pyrite; Gn, galena; Sph, sphalerite.
Figure 4. Strata-bound ore body (a) and ores with laminated structure (b). Abbreviations are as follows: Py, pyrite; Gn, galena; Sph, sphalerite.
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Figure 5. Hand specimens and microscopic photos of the ores from the Caiyuanzi deposit. (a) Disseminated-banded Pb–Zn ore sample (CYZ-1); (b) disseminated-net vein Pb–Zn ore (CYZ-2); (c) pyrite replaced and enclosed by galena and sphalerite; (d) sphalerite, galena, and chalcopyrite, forming network veins occurring along the wall rock fractures, where galena and chalcopyrite alternate with sphalerite. Abbreviations are as follows: Py, pyrite; Gn, galena; Sph, sphalerite; Qz, quartz; Ccp, chalcopyrite; Ep, epidote; Cal, calcite.
Figure 5. Hand specimens and microscopic photos of the ores from the Caiyuanzi deposit. (a) Disseminated-banded Pb–Zn ore sample (CYZ-1); (b) disseminated-net vein Pb–Zn ore (CYZ-2); (c) pyrite replaced and enclosed by galena and sphalerite; (d) sphalerite, galena, and chalcopyrite, forming network veins occurring along the wall rock fractures, where galena and chalcopyrite alternate with sphalerite. Abbreviations are as follows: Py, pyrite; Gn, galena; Sph, sphalerite; Qz, quartz; Ccp, chalcopyrite; Ep, epidote; Cal, calcite.
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Figure 6. In situ S isotope analyses of the Caiyuanzi deposit. (a,b,d) Microscopic photos of metal sulfide and corresponding in situ sulfur isotope values; (c) in situ S isotope test specimen of sulfide ores.
Figure 6. In situ S isotope analyses of the Caiyuanzi deposit. (a,b,d) Microscopic photos of metal sulfide and corresponding in situ sulfur isotope values; (c) in situ S isotope test specimen of sulfide ores.
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Figure 7. The histogram of S isotopes.
Figure 7. The histogram of S isotopes.
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Figure 8. Comparison of sulfur isotopic composition between Pb–Zn deposits in strata of different ages in the Laojunshan region and seawater- and mantle-derived sulfur in the same period (the isotopic composition range of mantle derived sulfur is according to [52]; the sulfur isotopic composition range of seawater in the same period is according to [54]; the sulfur isotopic composition range of ore deposits is according to [10,42,51]).
Figure 8. Comparison of sulfur isotopic composition between Pb–Zn deposits in strata of different ages in the Laojunshan region and seawater- and mantle-derived sulfur in the same period (the isotopic composition range of mantle derived sulfur is according to [52]; the sulfur isotopic composition range of seawater in the same period is according to [54]; the sulfur isotopic composition range of ore deposits is according to [10,42,51]).
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Figure 9. The Pb model diagram for the Caiyuanzi deposit (base map is modeled after [38,62], and lead isotope data of samples in the Dulong ore area are quoted from [43]). (a) The samples of the Caiyuanzi deposit fall on the average upper crustal growth curve. (b) The mantle curve in the corresponding.
Figure 9. The Pb model diagram for the Caiyuanzi deposit (base map is modeled after [38,62], and lead isotope data of samples in the Dulong ore area are quoted from [43]). (a) The samples of the Caiyuanzi deposit fall on the average upper crustal growth curve. (b) The mantle curve in the corresponding.
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Figure 10. Lead isotope Δβ-Δγ genetic classification diagram (base map is modeled after [55], and lead isotope data of samples in the Dulong ore area are quoted from [43]).
Figure 10. Lead isotope Δβ-Δγ genetic classification diagram (base map is modeled after [55], and lead isotope data of samples in the Dulong ore area are quoted from [43]).
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Table
Table 1. Information of the samples.
Table 1. Information of the samples.
No.LocationsFeaturesPurposes
CYZ—1PD2Disseminated banded oresPb isotope analyses
CYZ—1(1)PD2Banded oresPb isotope analyses
CYZ—2PD2Disseminated oresS isotope analyses
CYZ—3PD2Skarn oresPb isotope analyses
CYZ—4PD2Sulfide-bearing limestone
CYZ—5PD2Sulfide-bearing calcium siliceous rocksS and Pb isotope analyses
CYZ—6PD2Skarn ores
CYZ—7PD2Sulfide-bearing schistose marbleS isotope analyses
Table
Table 2. In situ sulfur isotopic compositions of ore sulfides.
Table 2. In situ sulfur isotopic compositions of ore sulfides.
No.Point No.Mineralδ34S (‰)
cyz-2cpy-sp-1Sphalerite4.70
cpy-sp-3Chalcopyrite4.50
cpy-sp-4Chalcopyrite4.90
cpy-sp-5Chalcopyrite4.90
py-sp-1Pyrite0.10
py-sp-2Pyrite5.00
py-sp-3Sphalerite4.70
py-sp-4Pyrite6.00
cyz-5cpy-Gn-1Chalcopyrite4.70
cpy-Gn-2Chalcopyrite5.10
pyd-pyx-sp-cpy-1Pyrite5.30
pyd-pyx-sp-cpy-2Pyrite5.90
pyd-pyx-sp-cpy-3Pyrite5.50
pyd-pyx-sp-cpy-4Sphalerite4.90
pyd-pyx-sp-cpy-5Sphalerite5.20
sp-cpy-1Sphalerite5.30
sp-cpy-2Chalcopyrite4.90
cyz-7cpy-1Chalcopyrite4.40
cpy1-1Chalcopyrite4.80
cpy-2Chalcopyrite4.30
cpy-5Sphalerite4.30
Table
Table 3. In situ Pb isotopes of sphalerite, pyrite, and chalcopyrite.
Table 3. In situ Pb isotopes of sphalerite, pyrite, and chalcopyrite.
No.DepositsPoint Nos.Mineral206Pb/204Pb1s207Pb/204Pb1s208Pb/204Pb1s
CYZ-1CaiyuanziGN-1Galena18.1480.00115.7120.00138.4490.002
1-GN-2Galena18.1460.00115.7110.00138.4470.002
1-GN-7Galena18.1420.00415.7070.00438.4320.010
1-GN-8Galena18.1340.00115.6980.00138.4100.003
CYZ-1GN-1Galena18.1530.00115.7190.00138.4640.002
GN-10Galena18.1470.00115.7100.00138.4450.002
GN-11Galena18.1480.00115.7110.00138.4440.002
GN-2Galena18.1510.00115.7170.00138.4610.002
GN-3Galena18.1530.00115.7180.00138.4630.002
GN-4Galena18.1470.00115.7120.00138.4490.003
GN-5Galena18.1460.00115.7110.00138.4460.002
GN-6Galena18.1450.00115.7090.00138.4370.002
GN-7Galena18.1430.00115.7070.00138.4350.002
GN-8Galena18.1440.00115.7080.00138.4380.002
GN-9Galena18.1420.00115.7070.00138.4340.002
SP-1Sphalerite18.1620.02215.7200.02038.4730.052
CYZ-2Caiyuanzi01Pyrite18.1700.00315.7280.00338.5100.006
04Pyrite18.1670.00215.7210.00238.4920.006
CYZ-5Caiyuanzi02Pyrite18.1470.00615.7200.00438.4670.011
CYZ-3CaiyuanziGN-1Galena18.1470.00115.7030.00138.4300.003
GN-10Galena18.1540.00115.7090.00138.4440.003
GN-11Galena18.1510.00115.7060.00138.4380.002
GN-12Galena18.1520.00115.7080.00138.4450.002
GN-2Galena18.1490.00115.7050.00138.4360.003
GN-3Galena18.1580.00115.7160.00138.4680.002
GN-4Galena18.1580.00115.7170.00138.4700.002
GN-5Galena18.1570.00115.7160.00138.4690.003
GN-6Galena18.1530.00115.7110.00138.4550.003
GN-7Galena18.1510.00115.7080.00138.4450.003
GN-8Galena18.1490.00115.7060.00138.4430.002
GN-9Galena18.1560.00115.7110.00138.4530.002
Table
Table 4. Summary and comparison of principal characteristics of SEDEX, MVT, magmatic hydrothermal vein-type, and the Caiyuanzi Pb–Zn deposit.
Table 4. Summary and comparison of principal characteristics of SEDEX, MVT, magmatic hydrothermal vein-type, and the Caiyuanzi Pb–Zn deposit.
FeaturesSedimentary Exhalative (SEDEX)Mississippi Valley-Type (MVT)Magmatic Hydrothermal Vein-TypeCaiyuanzi Deposit
Ore-forming ageSyngenetic—early diageneticEpigeneticEpigeneticSyngenetic, epigenetic
Geological settingExtensional first and second-order basinsCarbonate platform sequences and thrust belts, rare occurrences in extensional basinsVariedThrust belt
Host rocksVaried. Mainly sandstones, siltstones, limestones, dolomites, cherts, and turbiditesLimestones, dolostones, and rare micritesVaried. Sandstone, siltstone, and carbonatesSiliceous dolomite, quartz schist
Structural controlsSyn-sedimentary faults controlling sub-basins and associated fractures and brecciasNormal, trans-tensional, and wrench faults and associated fractures and brecciasFault zone/strataLithologic interface
Associated igneous activityNo direct association with igneous activity, but tuffs related to synchronous distal volcanism may be presentNot associated with igneous activityAssociated with igneous activityAssociated with igneous activity
Ore-body morphologySingle or multiple wedge- or lens-shaped, or sheeted/stratiform morphologyCommonly discordant on a deposit scale but strata-bound on a regional scaleVeins, stratiform-like morphologyStratiform-like morphology
MineralogySp, Gn, and Py (±Pyr) and common Brt, Ap, and very rare FlSp, Gn, Py, Mar, minor Dol, Cal, Fl (rare), Cpy, and Brt (minor to absent)Sp, Gn, Py, Cpy, and minor BrtSp, Gn, Py, Ccp, minor Hem, Po, Mag, Grt, and Chl
Host rock alterationSilicification, chloritization, epidotization, albitizationCarbonatization, silicificationSilicification, pyritic and carbonate alterationSilicification, skarnization
References[56][57,58,59][60,61]This paper
Abbreviations are as follows: Sp, sphalerite; Gn, galena; Py, pyrite; Brt, barite; Ap, apatite; Cpy, chalcopyrite; Fl, fluorite; hem, hematite; Po, pyrrhotite; Mag, magmatite, Grt, garnet, Chl, chlorite.
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Jiang, Y.; Cui, Y.; Nian, H.; Yang, C.; Zhang, Y.; Liu, M.; Xu, H.; Cai, J.; Liu, H. The Origin of the Caiyuanzi Pb–Zn Deposit in SE Yunnan Province, China: Constraints from In Situ S and Pb Isotopes. Minerals 2023, 13, 238. https://doi.org/10.3390/min13020238

AMA Style

Jiang Y, Cui Y, Nian H, Yang C, Zhang Y, Liu M, Xu H, Cai J, Liu H. The Origin of the Caiyuanzi Pb–Zn Deposit in SE Yunnan Province, China: Constraints from In Situ S and Pb Isotopes. Minerals. 2023; 13(2):238. https://doi.org/10.3390/min13020238

Chicago/Turabian Style

Jiang, Yongguo, Yinliang Cui, Hongliang Nian, Changhua Yang, Yahui Zhang, Mingyong Liu, Heng Xu, Jinjun Cai, and Hesong Liu. 2023. "The Origin of the Caiyuanzi Pb–Zn Deposit in SE Yunnan Province, China: Constraints from In Situ S and Pb Isotopes" Minerals 13, no. 2: 238. https://doi.org/10.3390/min13020238

APA Style

Jiang, Y., Cui, Y., Nian, H., Yang, C., Zhang, Y., Liu, M., Xu, H., Cai, J., & Liu, H. (2023). The Origin of the Caiyuanzi Pb–Zn Deposit in SE Yunnan Province, China: Constraints from In Situ S and Pb Isotopes. Minerals, 13(2), 238. https://doi.org/10.3390/min13020238

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