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Article

Geochronology of the Baishi W-Cu Deposit in Jiangxi Province and Its Geological Significance

by
Li Li
1,2,
Hai-Li Li
3,4,*,
Guo-Guang Wang
2,* and
Jian-Dong Sun
3
1
School of Civil Engineering, Jiangsu Urban and Rural Construction College, Changzhou 213147, China
2
State Key Laboratory for Mineral Deposits Research, Institute of Geo-Fluids, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210023, China
3
Nanjing Center, China Geological Survey, Nanjing 210016, China
4
CAS Key Laboratory of Crust-Mantle Materials and Environments, School of Earth and Space Sciences, University of Science and Technology of China, Hefei 230026, China
*
Authors to whom correspondence should be addressed.
Minerals 2022, 12(11), 1387; https://0-doi-org.brum.beds.ac.uk/10.3390/min12111387
Submission received: 12 September 2022 / Revised: 22 October 2022 / Accepted: 28 October 2022 / Published: 30 October 2022
(This article belongs to the Special Issue Critical Metal Minerals)
Browse Figures
Versions Notes

Abstract

:
The Baishi W-Cu deposit is located in the Nanling metallogenic belt, which is famous for its numerous W deposits and reserves. The formation age of this deposit remains unclear. In order to further infer the formation age of the deposit, this study conducted detailed LA-ICP-MS U-Pb isotopic analyses of zircon and monazite selected from ore-related Baishi granite. The LA-ICP-MS zircon U-Pb weighted average ages of Baishi granite were determined to be 223 ± 2 Ma and 226 ± 1 Ma, and the LA-ICP-MS U-Pb weighted average ages of monazite were determined to be 224 ± 2 Ma and 223 ± 1 Ma. The BSE image of monazite was homogeneous, and the pattern of rare earth elements had an obvious negative Eu anomaly, indicating that monazite was of magmatic origin. Combining the ages of zircon and monazite, this study inferred that Baishi granite and the Baishi W-Cu deposit formed in the Triassic. The determination of the ore-forming event of the Baishi W-Cu deposit provides new data regarding the important Indosinian (Triassic) mineralization events in the Nanling metallogenic belt and suggests that geologists should strengthen the prospecting work of Indosinian tungsten deposits in the Nanling area. In terms of tectonic setting, it was inferred that the Triassic Baishi W-Cu deposit was formed in the extensional environment after intracontinental orogeny.

1. Introduction

China has the richest tungsten resources in the world, and most of the tungsten deposits are concentrated in South China. Among them, the Nanling metallogenic belt is the most famous tungsten polymetallic metallogenic belt, and the study of tungsten polymetallic mineralization related to Mesozoic granites is a hot topic for geologists [1,2,3,4]. The Yanshanian (Jurassic–early Cretaceous) is considered as the most important stage of large-scale felsic magmatism and mineralization in the Nanling region [5,6,7,8,9,10,11]. Recently, with the expansion of the research scope and the progress of research techniques and methods, Indosinian granites and related W mineralization in the Nanling metallogenic belt, and even in the whole of South China, have been reported in an increasing number of papers [12,13,14,15,16,17]. Indosinian metallogenic events are considered to have good metallogenic potential, and the prospecting work carried out on Indosinian deposits should be strengthened [18,19,20,21,22].
Among the isotope dating methods, U-Th-Pb isotope chronology is the most widely used; it can predict the exact time of the generation of geological bodies and events and is an important means to study geological evolution. Zircon is a common mineral used for U-Th-Pb isotope dating, as it is extremely stable. It is the most widely used mineral for U-Pb dating for its high contents of U and Th, low contents of common Pb, and particularly high closure temperature [23].
Monazite ((Ce,La,Th)PO4) is a phosphate mineral rich in LREEs. It is commonly found as an accessory mineral in peraluminous granites and Ca-poor metamorphic rocks [24] and sometimes forms in sedimentary rocks [25]. In recent years, it has become one of the more important dating minerals, because it contains a large amount of the highly radioactive elements of Th and U and very little common Pb [26,27,28,29].
The Baishi W-Cu deposit is located in the Xingguo–Ningdu ore concentration area of Jiangxi Province, and its metallogenic chronology and geodynamic setting are still unclear. Baishi granite is ore-forming rock, as it is ore bearing and has a close relationship with the ore veins. To clearly determine the forming ages of Baishi granite and of the Baishi W-Cu deposit, this study conducted LA-ICP-MS U-Pb dating using both zircon and monazite. This study summarized the metallogenic epoch of tungsten polymetallic deposits in the Nanling metallogenic belt and confirmed the important role of Indosinian mineralization in the Nanling region.

2. Geological Setting

The study area is located at the intersection of the eastern end of the EW tectonic-magmatic zone of Nanling and the Yushan depression zone of the western uplift zone of Wuyi Mountain (Figure 1A). In terms of metallogenic melt, the study area belongs to the eastern part of the Nanling metallogenic belt and is part of the Xingguo–Ningdu ore cluster (Figure 1B).
The oldest rocks in the study area are the Sinian (Edicaran) shallow marine facies strata that underwent lower greenschist-facies metamorphism. The lithologic assemblage is represented by metatuffs, metasandstones, phyllites, and siliceous rocks. Cambrian formation is represented by rhythmic sandstone-slate formation. Devonian and Carboniferous formations occur only sporadically; the former is mainly composed of continental clastic rocks with a few marine calc-argillaceous rocks, and the latter is represented by mud–sand detrital deposits in transition from continental to marine facies. A few outcrops are referred to have formed during the Permian–Jurassic interval. Permian formation is concerned with conglomerates, siltstones, sandstones, and tuffs. Jurassic formation contains calcareous shales and limestones. Cretaceous volcanic rocks, red sandstones, and conglomerates are widespread (Figure 1C).
There are mainly two NE-trending regional deep faults in the study area, namely, the Wan’an fault in the northwest and the Shefu fault in the southeast (Figure 1C). The fold deformation in the region is intense, and the fold hinges are mainly in the direction of nearly N-S or NW trending.
Magmatic rocks in the study area are well developed, and magmatic activities last for a long time, showing the characteristics of Caledonian (Silurian–Devonian), Indosinian, and Yanshanian multi-stage activities. The lithology is mainly acidic granites, showing a close relationship with tungsten, tin, molybdenum, copper, and other polymetallic mineralization (Figure 1C).

3. Petrology

Baishi granite, as the main igneous rock in this W-Cu deposit, occurs as grayish-white-to-grayish-yellow intermediate granite felsic stock (Figure 2A,B). The essential minerals of granite are plagioclase, K-feldspar, quartz, muscovite, and biotite (Figure 2C,D). The accessory minerals contain apatite, rutile, zircon, and monazite. Alterations are widespread, appearing in the form of reactions such as carbonatation and chloritization. Granite shows close spatial and genetic relations with W-Cu mineralization, including the following aspects: (1) Baishi granite contains ore vein and disseminated mineralization, as we could see in the field images (Figure 2A,B) and microphotographs (Figure 2E,F). (2) The average content of W in the three samples of Baishi granite was 38.17 ppm (unpublished data from Nanjing Center, China Geological Survey), which was much higher than the average contents of the continental crust (1.0 ppm), upper crust (1.4 ppm), and lower crust (0.6 ppm) [32]. Thus, Baishi granite and related ore bodies were considered to have formed simultaneously.

4. Ore Deposit Geology

The Baishi W-Cu deposit had been exploited since the founding of the People’s Republic of China. After that, exploration team No. 220 (now called Jiangxi Geological Survey and Exploration Institute), Gannan Brigade, and other units carried out general surveys and explored the Baishi W-Cu deposit until 1958. The Baishi W-Cu deposit is a medium-sized tungsten polymetallic deposit with Cu, Mo, Bi, and Zn.
The exposed strata of the mining area are lower Cambrian strata, composed of slate intercalated with sandstone and phyllite, and the stratigraphic trend is nearly north–south. The mining area is generally controlled by the north–south structure (Figure 3). The veins are filled in the fissures of WNW and NNE. The fissures of this group are mainly in the WNW direction, which have obvious tensile characteristics. However, the veins of the NEE fissures are small and dense, and belong to compressional and torsional fractures according to their mechanical properties. A massive ore body is found at the intersection of two groups of fractures in the WNW and the NNE fissures.
The formation of the Baishi W-Cu deposit is closely related to Baishi granite (Figure 2A,B). Granite and adjacent smaller intrusions with nodules are exposed in the mining area. The alterations closely related to mineralization include silication, sericitization, muscovitization, chloritization, and greisenization (Figure 2A,B).
This deposit belongs to a wolframite–chalcopyrite quartz vein type. The tungsten-bearing vein ore bodies are mainly in the WNW formation and occur secondarily in the NNE formation. In general, the veins are irregular, and the local variations are great. Along the vertical and horizontal directions, the pinching side appears and reappears. The main mineral in the ore vein is wolframite. A variety of sulfide minerals are associated, especially chalcopyrite (Figure 2E,F). Metal minerals include wolframite, chalcopyrite, marmatite, molybdenite, bismuth, and scheelite.
The mineralization in this mining area can be divided into the following stages: (1) The quartz–wolframite stage. This stage belongs to the pegmatic vaporization stage. The minerals generated are quartz, wolframite, molybdenite, muscovite, beryl, topaz, etc. In this stage, the metal and vapor-forming minerals are more common on both sides of the veins. There is an abundance of wolframite deposits in this stage. (2) The quartz sulfide stage. This stage is roughly in the middle-temperature stage. A large amount of chalcopyrite precipitate can be found in this period. Fluorite, sericite, and other minerals form in this stage. (3) The carbonate stage. This stage is a low-temperature hydrothermal stage in which calcite, sericite, and low-temperature silica dominate.

5. Sampling and Analytical Methods

Two samples were studied in this research study, and they are collected in the Baishi W-Cu deposit (Figure 3). One sample was chosen for obtaining the phase and compositional map using TESCAN Intergrated Mineral Analyzer (TIMA). The TIMA results were analyzed at Nanjing Hongchuang Geological Exploration Technology Service Co., Ltd. TIMA is a Mira-3 scanning electroscope equipped with four energy-dispersive X-ray spectroscopy devices (EDS; EDAX Element 30). For the experiment, we used an acceleration voltage of 25 kV and a probe current of 9 nA. The working distance was set to 15 mm. The pixel spacing was set to 3 μm, and the dot spacing was set to 9 μm. The sample was scanned using the liberation analysis module. The method is described in detail in [34].
Zircon grains for LA-ICP-MS U-Pb dating and monazite grains for LA-ICP-MS U-Pb dating and rare earth elements analyses were separated from Baishi granite using conventional heavy-liquid and magnetic separation methods. Representative zircon and monazite grains were hand-picked under a binocular microscope, mounted on an epoxy resin disk, and polished down to nearly half the section to expose their internal structures for LA-ICP-MS analyses. Zircon and monazite were documented with transmitted and reflected light micrographs as well as with cathodoluminescence (CL) images and back-scattered electron (BSE) images, respectively, to reveal their internal structures, and the mount was vacuum-coated with carbon. The CL and BSE images were taken with a scanning electron microscope at State Key Laboratory for Mineral Deposit Research (MiDeR), Nanjing University. U-Pb dating and rare earth elements were analyzed using LA-ICP-MS at Wuhan SampleSolution Analytical Technology Co., Ltd., Wuhan. Laser sampling was performed using an excimer laser ablation system (GeoLas Pro). An Agilent 7900 ICP-MS instrument was used to acquire ion-signal intensities. Helium was used as a carrier gas. Argon was used as the make-up gas and mixed with the carrier gas via a T-connector before entering the ICP. To decrease the detection limit and improve precision at spot sizes of 30 μm for zircon and 16 μm for monazite, nitrogen was added to the central gas flow (Ar + He) of the Ar plasma. The 91,500 and GJ-1 standard zircons were analyzed to correct isotopic fractionation and for zircon grains. The GJ-1 standard zircon analysis yielded an age of 604.2 ± 2.6 Ma (2σ, n = 8). The 44,069 and NIST 610 standards were used as external standards for monazite U-Pb dating and rare earth element calibration, respectively. The off-line selection and integration of background and quantitative calibration for rare earth element analyses and U-Pb dating were performed using in-house software ICPMSDataCal. Common Pb correction and the determination of the ages of the samples were carried out according to the method proposed by [35]. Data processing was carried out using the Isoplot programs of [36].

6. Results

6.1. TIMA Mineral Map

A section of Baishi granite was used to create the TIMA mineral map. The results are shown in Figure 4. The phase map was described using the backscattered electron (BSE) image and EDS data. Additionally, the percentage of minerals was calculated as the modal volume property. The potential reasons for unclassified minerals are as follows: (1) the energy spectra among different minerals are too close for the machine to identify, and (2) the grain size of the mineral is less than 3 μm, which is the pixel space. We could see that Baishi granite contained amounts of quartz (46.36%), albite (23.82%), and K-feldspar (10.28%). Muscovite (9.46%) and chlorite (3.56%) were ubiquitous. Most of the biotite was altered, and only little was reserved (0.59%). Baishi granite contained lots of accessory minerals, such as tourmaline (0.31%), apatite (0.25%), rutile (0.08%), zircon (0.02%), and monazite (0.01%). There were also some late carbonate minerals (0.15%) and clay minerals (0.02%).

6.2. LA-ICP-MS Zircon U-Pb Dating

The LA-ICP-MS analyses using zircon U-Pb isotopes were conducted on two granite samples. The results are summarized in Table 1. CL images of the representative zircon grains with 206Pb/238U ages are shown in Figure 5. The zircons were generally euhedral, short-to-long prismatic, colorless, and transparent. The crystal length ranged from 150 to 500 μm, with length-to-width ratios of 1:1 to 4:1. Most of the zircons showed clear oscillatory zoning in the CL images (Figure 5A,C), as is the case of magmatic zircon. The zircons showed variable U (151–2241 ppm) and Th (94–805 ppm) concentrations, with Th/U ratios ranging from 0.07 to 0.86 (Table 1). The Th/U ratios were consistent with the general magmatic zircons but were mostly higher than metamorphic zircons, which normally show lower Th/U ratios (<0.1) [37].
Twenty spot analyses on sample G001 yielded a weighted mean 206U/238Pb age of 223 ± 2 Ma (MSWD = 1.9) (Figure 5B). Twenty-one spot analyses on sample G003 yielded a weighted mean 206U/238Pb age of 226 ± 1 Ma (MSWD = 1.2) (Figure 5D). These ages were interpreted as the crystallization ages.

6.3. LA-ICP-MS Monazite U-Pb Dating and Rare Earth Elements Analysis

The LA-ICP-MS analyses using monazite U-Pb isotopes were conducted on two granite samples. The results are summarized in Table 2.
BSE images of the representative monazite grains with 206Pb/238U ages are shown in Figure 6. The monazites were generally euhedral–subhedral, short-to-long prismatic, colorless, and transparent. The crystal length ranged from 100 to 500 μm, with length-to-width ratios of 1:1 to 3:1. The structure of most monazites was uniform without zonation, and the edge of the monazite grain was round (Figure 6A,C). The monazites showed variable U (445–7363 ppm) and Th (51,037–74,816 ppm) concentrations, with Th/U ratios ranging from 10.2 to 120.6 (Table 2).
Twenty-five spot analyses of sample G001 yielded a weighted mean 206U/238Pb age of 224 ± 2 Ma (MSWD = 2.9) (Figure 6B). Twenty-three spot analyses of sample G003 yielded a weighted mean 206U/238Pb age of 223 ± 1 Ma (MSWD = 5.2) (Figure 6D). The ages were interpreted as the crystallization ages.
In addition, the analysis of rare earth elements was conducted simultaneously, and the results are shown in Table 3. The samples display negative Eu anomalies (Figure 7).

7. Discussion

7.1. Origin of Monazite

In terms of genetic mineralogy, monazites can be divided into magmatic monazite, metamorphic monazite, and hydrothermal monazite. It is very important to identify the monazite genetic types for the reasonable explanation of U-Pb ages. The types of monazites can be distinguished according to paragenetic minerals, BSE characteristics, and rare earth element characteristics [38].
Magmatic monazite often exhibits oscillating bands [39], fan-shaped zones [40], and homogeneous internal structures [41] in BSE images, with few inclusions. The common internal structures of hydrothermal monazite in BSE images are concentric oscillating bands and fan-shaped zonings, and a large number of fluid inclusions are developed inside [42]. In this study, a single monazite particle selected from Baishi pluton showed a homogeneous structure in the BSE image (Figure 5A,C), with very few internal inclusions, so it was presumed to be magmatic monazite.
From the perspective of the rare earth element characteristics of monazite, magmatic monazite usually has obvious negative Eu anomalies, while hydrothermal monazite has no Eu anomalies or no obvious negative Eu anomalies [38]. The chondrite-normalized rare earth elements of monazite in this study were compared with data of typical magmatic monazite and hydrothermal monazite (Table 3, Figure 7), further confirming that the monazite in this study was of the magmatic type because of the similar patterns between the monazite in this study and magmatic monazite. Therefore, the age of monazite obtained in this paper could represent the age of formation of Baishi granite, which intruded in the late Triassic.
Minerals 12 01387 g007 550
Figure 7. Normalized REE pattern of Baishi granite monazite. Chondrite data are from [43]. The red filled area represents the data of this study. The blue transparent area represents hydrothermal monazite (data from [44]). The orange transparent area represents hydrothermal monazite (data from [41]).
Figure 7. Normalized REE pattern of Baishi granite monazite. Chondrite data are from [43]. The red filled area represents the data of this study. The blue transparent area represents hydrothermal monazite (data from [44]). The orange transparent area represents hydrothermal monazite (data from [41]).
Minerals 12 01387 g007

7.2. Age of the Baishi W-Cu Deposit and Geodynamic Setting

There is much debate about the geodynamic setting of magmatism and mineralization during the Indosinian in South China. Compared with previous models of continental collision involving the westward subduction of the Pacific Plate [45,46,47] and the flat-slab subduction of the Paleo-Pacific plate [48], recently, researchers have tended toward the perspective of intracontinental orogeny [17,49,50]. Unfortunately, the absence of island arc granites [49,51] suggests that the early Mesozoic magmatic event is not directly related to plate subduction. However, there is much evidence to support the occurrence of an intracontinental tectonic event: (1) the large area distribution of bimodal vocanics generated in the setting of lithosphere extension and thinning [52], such as gabbro dating to 225 Ma in Daoxian in Hunan province and plagioclase amphibolite dating to 252 Ma in Jingning in Zhejiang province [53]; (2) the absence of early Mesozoic ophiolite, a subduction complex, related volcanic rocks, arc magmatism, and high-pressure metamorphism in South China [49,51,54,55,56]; (3) the existence of quite a few mylonitized granites that formed later than the regional deformation action, suggesting that there was a process of extrusion and extension in the Triassic [57,58].
During the Indosinian, the South China plate was located between the North China plate and the Indo-China peninsula, and the Indosinian movement probably began in the middle Permian (267~262 Ma) [59]. The collision peak between the Indo-China peninsula and the South China block generated the Song Ma suture zone dated at 258~243 Ma [60]. Moreover, the metamorphic peak age of the Qinling–Dabie suture is 230~226 Ma, which represents the collision between the South China block and the North China block [61]. The collision force was transmitted from south to north, which may have been related to the sequential collision of the Indo-China peninsula, the South China block, and the North China block [60,61,62]. Indosinian orogeny completed the integration of the South China and North China blocks and formed a unified Chinese mainland. A series of collisions resulted in intense magmatism and mineralization in the domain. Although the Nanling region is located in the hinterland of South China, it is still affected by the remote effect of multiple block collisions [20].
Furthermore, research shows that the intense extension and deformation led to the crust thickness being increased by 50 km [60]. Additionally, the crust thickening caused crust extension and decompression melting, forming granite magma [63,64]. Many early–middle-Triassic syncollisional granites and late-Triassic post-collisional granites were generated in this area [65]. Against the extensional tectonic background, a series of tungsten–polymetallic mineralizations related to granites occurred [19,21,22].
The LA-ICP-MS zircon U-Pb ages of the ore-related Baishi granite of the Baishi W-Cu deposit were determined to be 223 ± 2 Ma and 226 ± 1 Ma, and the LA-ICP-MS U-Pb ages of the magmatic monazite were determined to be 224.6 ± 2.0 Ma and 223.7 ± 1.6 Ma. In consideration of the reliability of the dating methods and Baishi granite’s tendency toward mineralization, it could be inferred that the Baishi W-Cu deposit was formed in the Triassic. On account of the age of formation of the rock, which is 226~223 Ma, it was inferred that the Baishi W-Cu deposit was formed in the extensional stage after intracontinental orogeny (Figure 8).

7.3. Indosinian Tungsten Mineralization in the Nanling Region

For a long time, the chronology of granites and related tungsten mineralization in the Nanling region has widely drawn the attention of geologists [9,10,11,17,65,66,67,68,69,70]. According to our statistics, more than 50 tungsten-related deposits in the Nanling metallogenic belt have been studied in detail, and many papers have been published [13,15,16,68,71,72] (Table 4, Figure 9). Most studies show that the majority of tungsten deposits in the Nanling region are related to granite intrusions in the Yanshanian [5,6,7,8,9,10,11]. However, Huang and Chen [73] put forward that although tungsten deposits in the Nanling region were mainly formed in the Yanshanian, they may have experienced multi-stage mineralization, especially during the Indosinian.
In recent years, increasing numbers of researchers have discovered Indosinian tungsten deposits in the Nanling region based on the quick development of dating technology ([12,13,14,15,16,17], this study). In addition, more scholars have realized that the tungsten mineralization in the Nanling region is characterized by multiple stages [4,18]. Mao et al. [4] systematically summarize the high-precision isotopic chronology data published in recent years and divide the Mesozoic tungsten polymetallic mineralization in the Nanling region into three stages, finding the Yanshanian to be the peak stage of mineralization. Meanwhile, the Indosinian has become increasingly important when discussing tungsten mineralization in the Nanling metallogenic belt. However, insufficient attention has been paid to the exploration of tungsten mineralization in the Indosinian.
This study provides new data relating to Indosinian mineralization in the Nanling metallogenic belt, further proving that the Indosinian has prospecting potential. Geologists should pay more attention to strengthening Indosinian tungsten prospecting in the Nanling region.

8. Conclusions

  • The zircon and monazite LA-ICP-MS U-Pb dating results can confirm the chronology of the ore-related Baishi granite, which formed in late Triassic, ranging from 226 to 223 Ma;
  • The Baishi W-Cu deposit was formed in an extensional environment after intracontinental orogeny;
  • Indosinian tungsten mineralization in the Nanling region has great exploration potential.

Author Contributions

Conceptualization, L.L. and H.-L.L.; methodology, L.L. and H.-L.L.; formal analysis, H.-L.L.; investigation, H.-L.L. and J.-D.S.; writing—original draft, L.L. and H.-L.L.; writing—review and editing, L.L. and G.-G.W.; founding acquisition, L.L. and J.-D.S. All authors have read and agreed to the published version of the manuscript.

Funding

This work was financially supported by the open fund of State Key Laboratory for Mineral Deposits Research, Nanjing University (grant No. 2022-LAMD-K09); National Science Foundation of the Jiangsu Higher Education Institutions of China (grant No. 22KJD170001); China Geological Survey Program (grant No. DD20221688); Engineering Research Center Program of Development & Reform Commission of Jiangsu Province (grant No. [2021] 1368); and Nature Science Research Project of Jiangsu Urban and Rural Construction College (grant No. XJZK21013).

Data Availability Statement

Not Applicable.

Acknowledgments

We express our thanks to anonymous reviewers for their constructive comments, which significantly improved the manuscript. The authors thank X.H.L. and C.L.Z. from Nanjing Center, China Geological Survey, and C.B.F. and Z.X.W. from Gannan Geological Brigade for their help during fieldwork. The authors thank State Key Laboratory for Mineral Deposits Research, Nanjing University, Nanjing Hongchuang Geological Exploration Technology Service Co., Ltd., and Wuhan SampleSolution Analytical Technology Co., Ltd., for their assistance in the experiment.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 12 01387 g001 550
Figure 1. (A) Simplified map showing the distribution of Yanshanian granites in South China (modified from [30]). (B) Schematic distribution map of tungsten ore cluster and typical W-Sn deposits in South Jiangxi Province (modified from [18]). (C) Regional geological map of Baishi W-Cu deposit (modified from [31]).
Figure 1. (A) Simplified map showing the distribution of Yanshanian granites in South China (modified from [30]). (B) Schematic distribution map of tungsten ore cluster and typical W-Sn deposits in South Jiangxi Province (modified from [18]). (C) Regional geological map of Baishi W-Cu deposit (modified from [31]).
Minerals 12 01387 g001
Minerals 12 01387 g002 550
Figure 2. Photographs of Baishi granite. (A) Field photo of Baishi granite that contained wolframite quartz veins. (B) Hand specimen picture of Baishi granite that contained disseminated wolframite and chalcopyrite. (C,D) Cross-polarized light microphotographs of Baishi granite. (E,F) Reflected light microphotographs of Baishi granite that contained wolframite and chalcopyrite. Abbreviations: Wol, wolframite; Ccp, chalcopyrite; Q, quartz; Kfs, k-feldspar; Pl, plagioclase; Bt, biotite; Mu, muscovite.
Figure 2. Photographs of Baishi granite. (A) Field photo of Baishi granite that contained wolframite quartz veins. (B) Hand specimen picture of Baishi granite that contained disseminated wolframite and chalcopyrite. (C,D) Cross-polarized light microphotographs of Baishi granite. (E,F) Reflected light microphotographs of Baishi granite that contained wolframite and chalcopyrite. Abbreviations: Wol, wolframite; Ccp, chalcopyrite; Q, quartz; Kfs, k-feldspar; Pl, plagioclase; Bt, biotite; Mu, muscovite.
Minerals 12 01387 g002
Minerals 12 01387 g003 550
Figure 3. Geological deposit map of Baishi W-Cu deposit region (modified from [33]).
Figure 3. Geological deposit map of Baishi W-Cu deposit region (modified from [33]).
Minerals 12 01387 g003
Minerals 12 01387 g004 550
Figure 4. (A) BSE photo of Baishi granite. (B) Phase map and composition of Baishi granite.
Figure 4. (A) BSE photo of Baishi granite. (B) Phase map and composition of Baishi granite.
Minerals 12 01387 g004
Minerals 12 01387 g005 550
Figure 5. Typical CL images (A,C) and LA-ICP-MS zircon U-Pb concordant curves (B,D) of zircon of Baishi granite. The yellow, solid-line circles represent the locations of zircon U-Pb.
Figure 5. Typical CL images (A,C) and LA-ICP-MS zircon U-Pb concordant curves (B,D) of zircon of Baishi granite. The yellow, solid-line circles represent the locations of zircon U-Pb.
Minerals 12 01387 g005
Minerals 12 01387 g006 550
Figure 6. Typical BSE images (A,C) and LA-ICP-MS monazite U-Pb concordant curves (B,D) of monazite of Baishi granite. The yellow, solid-line circle represents the locations for monazite U-Pb.
Figure 6. Typical BSE images (A,C) and LA-ICP-MS monazite U-Pb concordant curves (B,D) of monazite of Baishi granite. The yellow, solid-line circle represents the locations for monazite U-Pb.
Minerals 12 01387 g006
Minerals 12 01387 g008 550
Figure 8. Geodynamic model for the forming of Baishi granite and the Baishi W-Cu deposit.
Figure 8. Geodynamic model for the forming of Baishi granite and the Baishi W-Cu deposit.
Minerals 12 01387 g008
Minerals 12 01387 g009 550
Figure 9. The metallogenic age of the tungsten polymetallic deposits in the Nanling region (detailed reference in Table 4).
Figure 9. The metallogenic age of the tungsten polymetallic deposits in the Nanling region (detailed reference in Table 4).
Minerals 12 01387 g009
Table
Table 1. LA-ICP-MS zircon U-Pb dating data of Baishi granite.
Table 1. LA-ICP-MS zircon U-Pb dating data of Baishi granite.
Analysis SpotThUTh/UIsotope RatiosIsotope Ages (Ma)
(ppm)(ppm)207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ207Pb/206Pb2σ207Pb/235U2σ206Pb/238U2σ
G001-ZR1-01995930.170.05270.00150.25050.00790.03410.0005322120227122166
G001-ZR1-022083950.530.05790.00270.28620.01360.03590.00105282082562222812
G001-ZR1-031291510.860.05010.00340.24520.01680.03570.00112113142232822614
G001-ZR1-042873950.730.05070.00170.24680.00720.03550.0004228156224122256
G001-ZR1-051203800.320.04860.00150.24240.00740.03610.0004128144220122284
G001-ZR1-061866470.290.05050.00160.24450.00790.03510.0005217148222122226
G001-ZR1-071976060.330.05020.00140.23990.00660.03460.0004206194218102196
G001-ZR1-082587690.340.04940.00120.23740.00540.03480.000416511221682216
G001-ZR1-092255780.390.04900.00140.23030.00710.03410.0004150140210122166
G001-ZR1-101545050.300.05360.00170.26330.00800.03450.0005354154237122196
G001-ZR1-113584380.820.05010.00300.24240.01370.03530.00081982902202222410
G001-ZR1-121477930.190.05100.00130.24910.00620.03510.0003243114226102224
G001-ZR1-131403950.350.04880.00170.24060.00810.03560.0005200160219142266
G001-ZR1-141748090.210.04880.00160.24340.00800.03610.0007139160221142298
G001-ZR1-151803290.550.05250.00210.24970.00890.03480.0006306178226142216
G001-ZR1-162699910.270.05100.00130.24940.00600.03530.0004239110226102246
G001-ZR1-172556560.390.05170.00140.25710.00640.03610.0005272122232102296
G001-ZR1-181386340.220.05040.00140.24680.00660.03540.0004213130224102244
G001-ZR1-191704870.350.05400.00140.25630.00630.03430.0005372110232102186
G001-ZR1-201777990.220.04890.00130.24470.00680.03610.0005143126222122286
G003-ZR1-01945540.170.05290.00320.26080.01400.03540.0007324278235222248
G003-ZR1-021767540.230.05240.00200.26670.01170.03640.00073061702401823010
G003-ZR1-0344922380.200.04990.00140.24930.00750.03580.0006191134226122278
G003-ZR1-0410814080.080.05010.00180.25250.01120.03640.00122111662291823014
G003-ZR1-0515710350.150.05120.00120.25470.00550.03590.000425011223082286
G003-ZR1-0619311690.170.04690.00130.23530.00620.03620.000543134215102296
G003-ZR1-071104980.220.04980.00160.24650.00760.03580.0005187152224122276
G003-ZR1-0854113890.390.05070.00120.25170.00550.03580.000423310822882264
G003-ZR1-092816700.420.04960.00140.24760.00700.03600.0004176130225122286
G003-ZR1-1015022410.070.04850.00090.24300.00450.03600.00031248822182284
G003-ZR1-1125623530.110.05120.00110.24990.00500.03520.00032569622782234
G003-ZR1-121809250.190.05280.00150.25680.00730.03510.0004320134232122224
G003-ZR1-132279370.240.05070.00130.25080.00650.03570.0004233118227102266
G003-ZR1-141549210.170.05180.00160.25360.00780.03540.0005276136230122246
G003-ZR1-1511415030.080.05030.00120.24670.00580.03530.0004209112224102244
G003-ZR1-1616919280.090.05200.00120.26430.00600.03670.0004283112238102326
G003-ZR1-1767518540.360.04920.00100.24970.00520.03650.00041678822682316
G003-ZR1-182043890.520.04690.00230.23680.01240.03640.000756222216202308
G003-ZR1-191696010.280.04780.00140.22980.00550.03500.0004100146210102226
G003-ZR1-2080515950.500.04750.00100.23350.00520.03540.00047210421382244
G003-ZR1-211527970.190.05100.00170.25660.00800.03630.0006243152232122308
Table
Table 2. LA-ICP-MS monazite U-Pb dating data of Baishi granite.
Table 2. LA-ICP-MS monazite U-Pb dating data of Baishi granite.
Analysis SpotThUTh/UIsotope RatiosIsotope Ages (Ma)
(ppm)(ppm)207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ207Pb/206Pb2σ207Pb/235U2σ206Pb/238U2σ
G001-TW1-0158,25269983.40.05660.00370.28180.01640.03700.0006476288252262348
G001-TW1-0257,15978872.50.05240.00300.25180.01500.03520.0005302262228242236
G001-TW1-0359,48878276.00.05020.00320.24000.01500.03520.0005211294218242236
G001-TW1-0458,98769584.90.05070.00320.23920.01460.03490.0005233290218242216
G001-TW1-0560,587550110.30.05270.00370.25700.01730.03600.0007322332232282288
G001-TW1-0664,042231827.60.04920.00170.24560.00860.03630.0004167162223142304
G001-TW1-0756,57765885.90.04920.00350.23410.01540.03560.0006167300214262268
G001-TW1-0865,142155641.90.04740.00200.22980.00980.03530.000478182210162244
G001-TW1-0953,620445120.60.05590.00430.27630.02020.03680.00114502802483223314
G001-TW1-1055,868476117.40.05650.00480.27740.02190.03660.0007472316249342328
G001-TW1-1174,521694510.70.05090.00120.24540.00580.03500.0003235112223102224
G001-TW1-1266,46476686.80.05280.00280.27030.01440.03740.0005320244243242376
G001-TW1-1358,121532109.20.05800.00380.28420.01660.03630.0007532344254262308
G001-TW1-1466,003156742.10.05460.00220.26220.01040.03500.0004394178236162224
G001-TW1-1566,78584978.70.05680.00300.27530.01380.03550.0005483234247222256
G001-TW1-1665,960127651.70.05110.00330.24160.01530.03460.0005243284220262196
G001-TW1-1760,35973682.00.05670.00400.26430.01690.03470.0005480310238282206
G001-TW1-1869,072428316.10.05270.00150.25060.00720.03450.0003317138227122194
G001-TW1-1959,06672881.10.05600.00340.27120.01630.03510.0005454262244262236
G001-TW1-2060,60481574.30.05410.00340.25710.01500.03490.0005376278232242216
G001-TW1-2168,974156944.00.05420.00220.26820.01150.03590.0004376194241182276
G001-TW1-2266,618135149.30.05160.00280.24890.01240.03550.0005333248226202256
G001-TW1-2365,277141446.20.05190.00230.25020.01100.03520.0004283212227182234
G001-TW1-2461,789136245.40.05040.00240.25430.01140.03710.0007217218230182358
G001-TW1-2574,816736310.20.05070.00110.24970.00550.03580.000322810422682274
G003-TW1-0158,890125946.80.04980.00270.24230.01250.03580.0005183260220202276
G003-TW1-0262,629134846.50.05490.00260.27400.01200.03660.0005409220246202326
G003-TW1-0352,470107548.80.05130.00380.24700.01670.03570.00082543402242822610
G003-TW1-0453,820114247.10.05640.00270.27720.01320.03610.0005478206248202296
G003-TW1-0560,059183232.80.05070.00220.24300.01050.03480.0004228200221182216
G003-TW1-0666,584338219.70.05070.00170.24880.00780.03570.0003233152226122264
G003-TW1-0757,282108252.90.05380.00290.25960.01390.03530.0005361248234222236
G003-TW1-0860,678198730.50.05390.00220.25730.01040.03480.0004369186232162206
G003-TW1-0961,815164237.60.04980.00240.23720.01130.03470.0004187216216182206
G003-TW1-1072,610289825.10.04860.00190.23540.00930.03500.0003128182215162224
G003-TW1-1161,572191532.20.05500.00280.25920.01280.03440.0004413230234202186
G003-TW1-1265,090234527.80.05350.00210.25880.00940.03530.0004350174234162234
G003-TW1-1355,483116547.60.05450.00280.26690.01300.03600.0005391168240202286
G003-TW1-1459,880205229.20.05440.00270.27980.01360.03760.0006387218250222386
G003-TW1-1556,294135841.50.05200.00270.25470.01310.03570.0005287306230222266
G003-TW1-1658,402168334.70.05080.00250.24170.01120.03500.0004228230220182224
G003-TW1-1762,968150541.80.05120.00300.25130.01440.03550.0005250280228242256
G003-TW1-1851,037114844.40.05140.00270.24410.01250.03470.0005261176222202206
G003-TW1-1960,907163637.20.05020.00240.24200.01120.03500.0003206222220182224
G003-TW1-2053,50392258.00.05520.00300.26530.01450.03500.0005420244239242226
G003-TW1-2158,839144040.90.05850.00290.27450.01280.03450.0004546218246202194
G003-TW1-2263,637155740.90.05830.00300.28080.01430.03490.0004543216251222216
G003-TW1-2354,987108550.70.07700.00350.38500.01710.03660.00051122180331262326
Table
Table 3. LA-ICP-MS monazite rare earth elements data of Baishi granite (×10−6).
Table 3. LA-ICP-MS monazite rare earth elements data of Baishi granite (×10−6).
Analysis SpotLaCePrNdSmEuGdTbDyHoErTmYbLu
G001-TW1-01148,861244,56224,17583,66694991644643437159021134427.796.49.28
G001-TW1-02146,503243,98924,67584,13799751805073475176423539231.711311.0
G001-TW1-03144,860245,41824,79386,51010,2371715209498187824340733.012611.0
G001-TW1-04139,383243,50224,80789,31511,0671965882566212629348036.814412.3
G001-TW1-05149,388243,37424,35085,08896551984904449169222436627.910410.1
G001-TW1-06128,564232,03924,87491,00413,1442407703840350648884871.628124.2
G001-TW1-07143,731245,90924,64486,33299171914968458169022536927.71038.75
G001-TW1-08133,537238,18525,21391,75612,0952446633657260135560349.617917.0
G001-TW1-09153,041248,23324,40682,78490341764304373138618029322.787.47.95
G001-TW1-10155,670249,76324,11281,66385581524107362133617328122.382.47.76
G001-TW1-11107,969215,82724,47694,57516,55221910,35111954858648112795.639633.3
G001-TW1-12151,851243,41523,96682,29288271654358401151320733626.51119.45
G001-TW1-13155,636246,92223,85181,30085801574059352130316827921.783.66.77
G001-TW1-14128,634235,84725,16890,91012,8241717030703266735859047.117815.9
G001-TW1-15137,995239,09424,73388,74611,5012345873546187922934324.589.67.24
G001-TW1-16130,740238,04925,30690,71312,3661596777686270137561849.318815.0
G001-TW1-17142,305242,84224,33885,15999941555034484182024139430.51149.86
G001-TW1-18120,567225,26424,42991,03014,69019888191015402254892479.531030.4
G001-TW1-19142,168245,85325,12789,91410,8942085524522189425241932.412111.7
G001-TW1-20138,813237,52224,55590,38411,2042376198607232331552041.615514.3
G001-TW1-21131,306237,58224,52588,91011,8781446435653259635559748.918916.6
G001-TW1-22136,087240,44924,62889,30111,4731536124615235231553643.717115.6
G001-TW1-23131,769235,41824,59689,53811,9671896372650257035059548.417916.6
G001-TW1-24134,133235,54023,82787,17110,9371925976595231331653344.417115.4
G001-TW1-25105,849210,06823,78290,39416,34519710,64313445755810147713356751.7
G003-TW1-01136,336239,77925,10690,19311,7101696048600231831652541.215413.9
G003-TW1-02135,854241,23725,08590,58611,9781636127595223130149440.315112.8
G003-TW1-03140,653244,07225,15489,34511,7762036125602225730348039.914312.9
G003-TW1-04143,307244,39025,06289,22211,3941915857568217528346737.014212.4
G003-TW1-05127,852239,37125,39292,53313,2081407192750299941270557.422119.6
G003-TW1-06111,582224,16525,75898,88316,2492699137977396954392776.729126.4
G003-TW1-07137,815242,73925,08388,59911,5181696044582224130449540.115213.4
G003-TW1-08126,539230,63025,07892,44413,6802507712803317643572457.723019.6
G003-TW1-09129,026235,44825,31592,91113,3212057413750296439364349.719016.2
G003-TW1-10115,329228,96325,47494,12615,1821938529907363450285871.028223.9
G003-TW1-11136,153239,31024,75584,79311,4931795864535182019723214.542.13.16
G003-TW1-12125,219233,75924,90890,14213,3571787460791320344475462.925322.3
G003-TW1-13138,522241,73224,99890,84611,8151866314611233830249537.614412.5
G003-TW1-14127,032232,87225,09492,67813,3031737244755297241070658.222320.3
G003-TW1-15133,141238,99425,18792,33412,4332106705665255434456644.517314.2
G003-TW1-16133,987241,30925,25690,33512,7441536921713279838264651.920716.7
G003-TW1-17131,910240,21825,48392,35312,6061786513627244132855143.316515.3
G003-TW1-18140,758244,11325,36392,04011,8961936230603231330450739.114613.1
G003-TW1-19131,353236,41225,12692,75412,8441867073719286439266353.919818.9
G003-TW1-20146,753248,21924,92286,45010,5431985358500189724940131.611910.0
G003-TW1-21136,580243,32125,21588,71212,2362006586625219226739628.51038.66
G003-TW1-22130,692237,20224,83089,34012,4491526735668268035360848.117216.3
G003-TW1-23140,700244,16924,77688,51711,2161745790556212528546837.413713.3
Table
Table 4. Summary of chronological data on the major typical W polymetallic deposits in the Nanling region.
Table 4. Summary of chronological data on the major typical W polymetallic deposits in the Nanling region.
No.DepositMineralizationAge/MaMethod of DatingReference
1Dajishan, Southern JiangxiW-Nb-Ta144Mica Ar-Ar[74]
2Dajishan, Southern JiangxiW-Nb-Ta147Mica Ar-Ar[75]
3Yaoling, Northern GuangdongW149Mica Ar-Ar[75]
4Niutangjie, Northern GuangxiW418Apatite U-Pb[76]
5Hongshuizhai, Jiulongnao orefield, Southern JiangxiW156Molybdenite Re-Os[77]
6Jiulongnao, Jiulongnao orefield, Southern JiangxiW151Molybdenite Re-Os[77]
7Zhangdongkeng, Jiulongnao orefield, Southern JiangxiW151Molybdenite Re-Os[77]
8Taoxikeng, Southern JiangxiW152Muscovite Ar-Ar[78]
9Taoxikeng, Southern JiangxiW155Muscovite Ar-Ar[78]
10Meiziwo, Northern GuangdongW156Muscovite Ar-Ar[79]
11Zhangdongkeng, Southern JiangxiW154Molybdenite Re-Os[80]
12Jiaoli, Southern JiangxiW polymetallic170Molybdenite Re-Os[81]
13Baoshan, Southern JiangxiW161Molybdenite Re-Os[81]
14Dengfuxian, HunanW152Molybdenite Re-Os[82]
15Qingshiling, Southern HunanW-Mo157Quartz Rb-Sr[83]
16Dalingbei, Southern HunanW150Zinnwaldite Ar-Ar[83]
17Xihuashan, Southern JiangxiW139Quartz Rb-Sr[84]
Wolframite Sm-Nd[84]
18Xihuashan, Southern JiangxiW137Fluorite Sm-Nd[84]
19Niuling, Southern JiangxiW-Sn154Molybdenite Re-Os[85]
20Yaolanzhai, Southern JiangxiW155Molybdenite Re-Os[8]
21Jiangjunzhai, Southeast HunanW169Molybdenite Re-Os[86]
22Miao’ershan, Northern GuangxiW212Scheelite Sm-Nd[14]
23Helong, Southern JiangxiW157Molybdenite Re-Os[87]
24Helong, Southern JiangxiW159Molybdenite Re-Os[87]
25Yanqian, Southern JiangxiW159Molybdenite Re-Os[88]
26Hongling, GuangdongW159Molybdenite Re-Os[89]
27Yaogangxian, HunanW-Mo156Quartz Rb-Sr[90]
28Yaogangxian, HunanW-Mo175Quartz Rb-Sr[90]
29Yaogangxian, HunanW-Mo170Molybdenite Re-Os[90]
30Gao’aobei, HunanW157Molybdenite Re-Os[90]
31Yaogangxian, HunanW-Mo158Cassiterite U-Pb[91]
32Jianlong, Southern JiangxiCu-W155Molybdenite Re-Os[92]
33ChuankouW212Molybdenite Re-Os[17]
Wolframite U-Pb[17]
34Zhangjiadi, Southern JiangxiW158Molybdenite Re-Os[18]
35Zhangjiadi, Southern JiangxiW161Molybdenite Re-Os[18]
36Shizhuyuan, HunanW-Mo-Bi153Muscovite Ar-Ar[93]
37Shizhuyuan, HunanW-Mo-Bi152Quartz Ar-Ar[93]
38Da’ao, Southern HunanW-Sn151Molybdenite Re-Os[94]
39Xintianling, Southern HunanW-Mo161Molybdenite Re-Os[95]
40Zhazixi, HunanW-Sb227Scheelite Sm-Nd[96]
41Anjiatan, Southern JiangxiW-Bi-Mo156Molybdenite Re-Os[97]
42Yuanlingzhai, Southern JiangxiW-Bi-Mo160Molybdenite Re-Os[97]
43Zhangdou, Southern JiangxiW-Sn149Molybdenite Re-Os[95]
44Huangsha, Southern JiangxiW153Molybdenite Re-Os[98]
45Piaotang, GannanW-Sn158Muscovite Ar-Ar[12]
46Keshuling, GannanW-Sn158Muscovite Ar-Ar[12]
47Xian’etang, GannanSn-W231Muscovite Ar-Ar[12]
48Qingshan, JiangxiW228Muscovite Ar-Ar[16]
49Qingshan, JiangxiW229[16]
50Baxiannao, Southern JiangxiW-Sn-Mo-Bi158Cassiterite U-Pb[99]
51Bikeng, Southern JiangxiW-Sn-Mo-Bi159Cassiterite U-Pb[99]
52Jinzhuping, Southern JiangxiW-Sn-Mo-Bi156Cassiterite U-Pb[99]
53Jinzhuping, Southern JiangxiW-Sn-Mo-Bi157Molybdenite Re-Os[99]
54Changkeng, Southern JiangxiW-Sn156Cassiterite U-Pb[55]
55Maoping, Southern JiangxiW-Sn156Cassiterite U-Pb[11]
56Xiangdong, HunanW-Sn151Cassiterite U-Pb[71]
57Xiangdong, HunanW-Sn141Cassiterite U-Pb[71]
58Xiangdong, HunanW-Sn136Cassiterite U-Pb[71]
59Sanjiaotan, HunanW225Molybdenite Re-Os[15]
60Baishi, JiangxiW-Cu223Zircon U-Pb
Monazite U-Pb		This study
224Monazite U-Pb
226Zircon U-Pb
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Li, L.; Li, H.-L.; Wang, G.-G.; Sun, J.-D. Geochronology of the Baishi W-Cu Deposit in Jiangxi Province and Its Geological Significance. Minerals 2022, 12, 1387. https://0-doi-org.brum.beds.ac.uk/10.3390/min12111387

AMA Style

Li L, Li H-L, Wang G-G, Sun J-D. Geochronology of the Baishi W-Cu Deposit in Jiangxi Province and Its Geological Significance. Minerals. 2022; 12(11):1387. https://0-doi-org.brum.beds.ac.uk/10.3390/min12111387

Chicago/Turabian Style

Li, Li, Hai-Li Li, Guo-Guang Wang, and Jian-Dong Sun. 2022. "Geochronology of the Baishi W-Cu Deposit in Jiangxi Province and Its Geological Significance" Minerals 12, no. 11: 1387. https://0-doi-org.brum.beds.ac.uk/10.3390/min12111387

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