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Article

Genesis of the Wuzhutang Granite and Associated W–Sn–Be Mineralization in the Xuebaoding Mining Area, Sichuan Province, China

by
Hongzhang Dai
1,*,
Denghong Wang
1,
Xin Li
2,
Shanbao Liu
1,
Chenghui Wang
1 and
Yan Sun
1
1
MNR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resource, CAGS, Beijing 100037, China
2
School of Earth Science and Resources, China University of Geoscience (Beijing), Beijing 100083, China
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(8), 993; https://doi.org/10.3390/min12080993
Submission received: 27 June 2022 / Revised: 27 July 2022 / Accepted: 30 July 2022 / Published: 5 August 2022
(This article belongs to the Special Issue Rare Metal Ore Formations and Rare Metal Metallogeny)
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Abstract

:
The Xuebaoding W–Sn–Be mining area, located in the Songpan–Garze orogenic belt in western China, is known for producing large, colorful, euhedral crystals of scheelite, cassiterite, and tabular beryl. Zircon LA-ICP-MS U–Pb dating of the Wuzhutang granite yields a concordia age of 218.96 ± 2.1 Ma, and a weighted mean 206Pb/238U age of 218.98 ± 1.12 Ma. Cassiterite LA-MC-ICPMS dating of the quartz vein bearing beryl, cassiterite, and scheelite, yields a concordant age of 213.5 ± 1.7 Ma. These observations indicate that magmatic activities and mineralization on the western side of the Zibaishan dome occurred during the late Indosinian, prior to their occurrence on the eastern side of the dome, reflecting the fact that the granite may have undergone two epochs of magmatic evolution and metallogenic processes. Geochemical analysis revealed that the Wuzhutang granite has relatively high A/CNK (average: 1.05) and differentiation index (DI; 81.16~85.88) values, and that they are enriched in W, Sn, Be, Li, and Cs. Unlike the Pukouling and Pankou granites, the Wuzhutang granite contains a certain amount of plagioclase and relatively high contents of Ba (633~1007 ppm) and Sr (334~411 ppm). Sr–Nd–Pb isotope values (87Sr/86Sr(t) = 0.70747–0.70865, εNd(t) = −6.35 to –4.34, 206Pb/204Pb = 18.186–18.3, 207Pb/204Pb = 15.556–15.592, and 208Pb/204Pb = 38.268–38.432) indicate a Mesoproterozoic basement origin for the Wuzhutang granite. We suggest the three granites belong to a peraluminous magma system and were derived by partial melting of the upper crust, the magma of the Wuzhutang granite originated from a deeper source and exhibits a lower degree of differentiation than that of the Pankou and Pukouling granites.

1. Introduction

The Songpan–Garze orogenic belt (SGOB) is an area well-known for its Li, Be, Nb, and Ta concentrations in China. Large and super-large granitic pegmatite-type rare metal deposits, represented by the Jiajika and Ke’eryin deposits, mainly occur along the eastern margin of the SGOB. In recent years, several high-temperature hydrothermal W–(Sn–Be) deposits have been identified in the Yidun island arc belt of the SGOB and the adjacent Qinling orogenic belt [1,2]. The Xuebaoding mining area in the northeastern part of the SGOB is known for producing large, colorful, euhedral, ornamental- to gem-grade crystals of scheelite, cassiterite, and tabular beryl [3,4,5,6,7,8,9,10,11]. Chronological data (216~182 Ma) of these rare metal deposits, including the Jiajika, Ke’eryin, and Xuebaoding deposits, show that a large-scale rare-metal metallogenic event occurred in the SGOB from the late Indosinian to the early Yanshanian; such large-scale rare-metal metallogenic events are closely related to the peraluminous granitic magma activities during this period [1,12,13,14,15,16,17,18,19].
The Xuebaoding mining area is located along the northern margin of the Longmen Mountains, at the intersection of the Yangtze Plate, Songpan–Garze orogenic belt, and Qinling orogenic belt [20]. Previous studies have primarily focused on the mineralogy [21,22,23,24,25,26,27,28,29,30], magmatic ore-forming epoch [20,26,31,32,33], elemental and isotopic characteristics of the Pukouling and Pankou granites [34,35,36,37,38,39], and characteristics of the ore-forming fluids [40,41] in the region. In particular, the granite group, which is composed of four exposed granites in the Xuebaoding area, belongs to leucogranite. Moreover, weak alteration has been found in the contact zone between these granites and country rocks [24,34]. Although the W–Sn–Be mineralization in the Xuebaoding area is thought to be closely related to the evolution of the highly fractionated Pukouling and Pankou granites [32,39,42,43,44], the magmatic and metallogenic processes of the Wuzhutang granite and nearby ore bodies on the western side of the dome have not been studied. Therefore, it is not clear whether the Wuzhutang granite has the same geochemical and evolutionary characteristics as the Pukouling and Pankou granites, which impedes a comprehensive understanding of the magmatic and metallogenic processes of the granite in the Zibaishan dome, as a whole.
In this work, we performed systematic adit logging and sampling on the Wuzhutang granite and ore bodies in the western part of the Zibaishan dome. Zircon and cassiterite U–Pb dating were used to constrain the magmatic and metallogenic age of the Wuzhutang area. Complementary geochemical studies were conducted to reveal the relationship between magmatic evolution and rare metal enrichment. Moreover, a comparative study between the Pukouling and Pankou granites in the eastern part, and the Wuzhutang granite and ore bodies in the western part, was carried out so as to elucidate the W–Sn–Be mineralization in the Zibaishan dome. The results of this study are expected to provide a reference for further evaluation of the rare metal metallogenic potential in the area.

2. Geological Background

2.1. Regional Geology

The SGOB, which occupies an area in excess of 2 × 105 km2, formed due to the closure of the Paleo-Tethys Ocean during the late Indosinian; it was also affected by the joint action of the Indian Plate, Pacific Plate, and Eurasian Plate [45,46]. Granitoids in the SGOB show a wide range of compositions, and include calc–alkaline, alkaline, peralkaline, and peraluminous rocks that formed at different stages during the evolution of the SGOB (Figure 1) [1,47,48,49]. Rare metals such as Li, Be, Nb, and Ta are abundant in the region. The currently known large and super-large rare metal deposits are mainly located along the eastern margin of the SGOB, and granitic pegmatite-type deposits are the most important type of rare metal deposits. At present, the Xuebaoding mining area is the only high-temperature hydrothermal deposit in the orogenic belt [38].

2.2. Mining Geology

The Xuebaoding W–Sn–Be mining area in Sichuan Province is located at the northwest margin of the Longmen Mountains at the intersection of the Yangtze Plate, Songpan–Garze orogenic belt and Qinling orogenic belt. The mining area is located within the Zibaishan dome, which is at the core of the Moziping–Shangnami inverted compound syncline. It is one part of the E–W-trending Motianling complex structural belt. Four granites (Wuzhutang, Huahuashui, Pukouling, and Pankou granites), each with exposures measuring less than 1 km2 occur at the core of the dome [34], intruding into the lower member of the Triassic Zagu’nao Formation (T2z). The regional Triassic strata are primarily composed of the Lower Triassic Bocigou Formation (T1b), Middle Triassic Zagu’nao Formation (T2z), and the Upper Triassic Zhuwo Formation (T3zh), of which the Zagu’nao Formation is the main ore-bearing formation, with W–Sn–W deposits in the Xuebaoding area. The lower member of the Zagu’nao Formation mainly consists of phyllite and marble; tensional joints are well developed in this member, and giant crystals of minerals are commonly observed therein.
The ore bodies occur in and around the Wuzhutang granite in the western portion of the Zibaishan dome (Figure 2). These ore veins obliquely cut through the granite and the Zagu’nao Formation. The joints, fissures, and quartz veins are well developed in the strata. Tungsten–beryllium mineralized bodies form in greisenized quartz veins. The ore bodies dip to the southwest (215°~260°) with dip angles of 55°~65°, lengths of 70~260 m, and thicknesses of 1.06~2.07 m. The grades of WO3, SnO2, and BeO are 0.06%~2.74%, 0.19%~3.09%, and 0.26%~3.87%, respectively. A certain degree of greisenization is observed at the contact zone between the granite body and ore veins (Figure 3c,d,e). Field and hand specimens of the Wuzhutang granite are massive and have a granitic structure; they are white to gray in color (Figure 3a,b,d). The minerals in the granite mainly consist of muscovite (10~15 vol%), potassium feldspars (20~25 vol%), plagioclase (20~30 vol%), and quartz (40~45 vol%) (Figure 3g). In contrast with the Pukouling and Pankou granites, the Wuzhutang granite contains a certain amount of plagioclase (Figure 3g). Taken together, field and microscopic observation results indicate that beryl, cassiterite, and scheelite formed during the same metallogenic period and occur as single crystals or aggregates (Figure 3e,f). The characteristics of muscovite and other accessory minerals (Figure 3g–i) from the granite and the vein indicate the occurrence of fluid metasomatism and the fact that the processes of element enrichment and mineral precipitation were not completely synchronous.
Overall, the metallogenic characteristics of the western part of the dome are similar to those of the eastern part [38]. However, several differences between them have been identified during our field observations: (1) In the western part of the dome, the W-enriched ore veins extend from the interior of the Wuzhutang granite to the marble, which is similar to that in the eastern (the Pankou and Pukouling granites) part of the dome [24,32]. However, the distance over which these veins extend is smaller in the western part of the dome. Notably, we observed that W–Sn–Be ore veins still occur in the Zhuwo Formation (T3zw) which is nearly 2 km away from the eastern side of the Pukouling granite (Figure 2a); (2) Tourmaline is almost absent in the granites and ore veins in the western part; and (3) The scale and intensity of mineralization in the western part are smaller and lower, respectively, than those in the eastern part of the dome.

3. Sampling and Analytical Methods

All samples were collected from the Wuzhutang granite and nearby Triassic strata. The samples for zircon U–Pb dating (pwWZTG-1) of granite and those for chemical analysis were taken from adits PD01 and PD03. The sample for cassiterite U–Pb dating was taken from the No. 4 ore vein in adit PD03 (PD03-#4) of the Wuzhutang granite.
Major and rare earth elements concentrations were analyzed at the National Geological Experiment Test Center, CAGS, Beijing. Major elements were analysed using a Rigaku 3080E X-ray fluorescence (XRF), with analytical uncertainties were less than 5%. Rare earth elements were determined by a PE300D inductively coupled plasma mass spectrometer (ICP-MS), with analytical uncertainties were less than 3%. Trace elements other than rare earth elements were analyzed at the Southwest Metallurgical Geological Testing Institute, Sichuan Province, using a XSeries Ⅱ inductively coupled plasma mass spectrometer (ICP-MS), with analytical precisions were better than 5%.
Zircon U–Pb isotope analyses were conducted using LA–MC–ICP–MS at the MNR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, CAGS. A Neptune MC-ICP-MS (Thermo Fisher Scientific, Waltham, MA, USA) in combination with a matched New wave UP 213 Nd:YAG laser ablation system, was used. Samples were ablated with a spot size of 24 μm, laser frequency of 10 Hz, and beam energy density of 2.5J/cm2. Calibration was performed externally using one NIST SRM 610 and two GJ1 for every 10 samples, with Ca as the internal standard to correct for instrument drift. Data reduction was carried out using the commercial software ICPMSDataCal 10.8 [50]. The U–Pb concordia diagrams were plotted using IsoplotR [51].
Cassiterite U–Pb isotope analyses were performed for the PD03-#4 samples using an Agilent 7900 ICP-MS in combination with a RESOlution LR 193 nm ArF excimer laser ablation system (Australian Scientific Instruments Pty Ltd., Canberra, Australia) at the Tianjin Center of China Geological Survey. Samples were ablated with a spot size of 30 μm, laser frequency of 8 Hz, and beam energy density of 10J/cm2. Calibration was performed externally using NIST SRM 610 and with 117Sn as the internal standard to correct for instrument drift. Data reduction was carried out using the commercial software ICPMSDataCal 10.9. The mass spectrometer utilized a novel orthogonal detector system (ODS) that could provide dynamic ranges of up to 11 orders of magnitude, for concentrations ranging from sub-ppm to percentage levels, with >109 CPS/PPM at <2% CeO conditions.
Whole rock Sr–Nd–Pb isotope analysis was performed using a thermal ionization mass spectrometry (TIMS; ISOPROBE-T, and Phoenix) and Phoenix Thermal Ionization Mass Spectrometer (PIMS) at the Analytical Laboratory, Beijing Research Institute of Uranium Geology, China National Nuclear Corporation. The mass fractionation corrections for Sr and Nd isotopic ratios were based on 86Sr/88Sr = 0.1194 and 146Nd/144Nd = 0.7219. During the analysis, the 87Sr/86Sr isotopic ratio and 143Nd/144Nd isotopic ratio were adjusted using the Sr standard NBS-987 and the Nd standard La Jolla. The measured values for the two standards were 0.910215 ± 11 (2σ, for 22 analyses) and 0.511852 ± 4 (2σ, for 24 analyses), respectively [52]. In the Pb isotope analytical process, Tl was added as an internal standard for correcting mass-dependent isotopic fractionation at a temperature of 1100–1300 °C. The exponential correction value of 205Tl/203Tl was 2.3871. The Pb isotopic ratios were corrected using average values of the NBS981 standard measured under the same conditions. The analytical procedures for the determination of these isotopes have been described in detail by [53].

4. Results

4.1. U–Pb Ages of Zircon

Zircon crystals from the Wuzhutang granite (sample pwWZT-G) are elongated, prismatic, and transparent. They range in size from ~50 to 155 μm, with aspect ratios of ~3:1 to 1:1, and typically exhibit magmatic oscillatory zoning (Figure 4a). The Th/U ratios in the zircons in all pwWZTG-33 samples are greater than 0.1, indicating that they have a magmatic origin. Isotope analysis was conducted on a total of 34 zircon spots (Table 1). One spot (pwWZTG-3) was excluded owing to its extremely low concordance (53%). The obtained concordant 206Pb/238U ages were in the range of 191.27–247.40 Ma. To accurately constrain the crystallization age of the Wuzhutang granite, 15 spots with concordances less than 95% were excluded from the calculations, although these data were used for the estimation of the magmatic age. The concordant ages of the remaining 18 zircons were in the range of 198.96–247.40 Ma. Two of these 18 spots (pwWZTG-25 and pwWZTG-34) deviated significantly from the concordia age (218.96 ± 2.10 Ma, MSWD = 1.9); spot pwWZTG-25 (198.96 Ma) was attributed to radiogenic Pb loss, and spot pwWZTG-34 (247.40 Ma) was interpreted as captured zircon. The weighted mean age of the remaining 16 spots was 218.98 ± 1.12 Ma (MSWD = 0.63), which can be taken to represent the crystallization age of the Wuzhutang granite (Figure 4b,c).

4.2. U–Pb Ages of Cassiterite

Cassiterite was analyzed using LA-MC-ICPMS, and the corresponding U–Pb data are listed in Table 2. The 238U/206Pb and 206Pb/207Pb ratios of the PD03-#4 samples were in the ranges of 20.41–30.72 and 2.63–19.43, respectively. The characteristics of 206Pb/207Pb ratios indicate that the contents of common lead in cassiterite in the PD03-#4 samples are relatively low; thus, more accurate ages can be obtained using the T-W diagram [54]. LA-MC-ICPMS dating of cassiterite yields an age of 213.5 ± 1.7 Ma for the PD03-#4 samples (Figure 5).

4.3. Geochemistry of the Wuzhutang Granite

Major and trace element compositions of 12 samples from the Wuzhutang mining area are provided in Table 3. The loss-on-ignition (LOI) values were in the range of 0.36–1.46 wt.%. All Wuzhutang granite samples possessed high SiO2 contents of 69.81–72.05 wt.%; alkali contents (Na2O + K2O) of 7.57–7.97 wt.% with K2O contents (3.29–3.56 wt.%) are less than Na2O contents (4.28–4.57 wt.%); low concentrations of MgO (0.66–0.89 wt.%), CaO (1.87–3.15 wt.%), and TiO2 (0.25–0.3 wt.%); and LOI values (0.36~1.46). In the (Na2O + K2O) vs. SiO2 diagram (Figure 6a), the samples plot in the granite field and further in the monzogranite field (Figure 6b), which is consistent with the observation that the Wuzhutang granite contains a certain amount of plagioclase (Figure 3g). Typically, the Wuzhutang granite is peraluminous, with alumina saturation index (A/CNK) values of 0.91–1.07 (only one data point was less than 1). The differentiation index (DI), solidification index (SI) and the Rittman index (σ) were in the ranges of 81.16~85.88, 6.59~11.85 and 2.09 to 2.28, respectively. Petrochemical analyses indicated that the Wuzhutang granite belongs to the quasi-aluminous and high-K calc–alkaline series (Figure 6c,d) and that it is a highly differentiated granite (Figure 6c). CaO, TFe2O3, MgO, TiO2, P2O5, and MnO contents were in the ranges of 1.87–3.15, 1.5–2, 0.66–1.29, 0.25–0.3, 0.09–0.1, and 0.03–0.04 wt.%, respectively. High field-strength elements, such as Nb, Ta, Zr, Hf, and Th, were present in relatively low concentrations. The volatile element F (0.04–0.20 wt.%, with average of 0.06 wt.%) in the Wuzhutang granite, was significantly lower than that in the Pankou and Pukouling granites.
REE, LREE, and HREE concentrations of the samples of the Wuzhutang granite were in the ranges of 78.3–122.14, 66.38–115.87, and 5.61–6.45, respectively. Whole rock chondrite-normalized REE plots exhibited weak negative Eu anomalies (0.81–0.91), light REE enrichment with (La/Yb)N = 18.09–26.13, and nearly flat heavy REE patterns (Figure 7a). The spider diagram of trace element ratios shows that the rare metal concentrations of the Wuzhutang granite samples were significantly high (Figure 7b), with Li, Be, W, Sn, Cs, and Rb concentrations being 61.6–80 ppm, 4.03–33.3 ppm, 3.49–45.6 ppm, 4.33–75.7 ppm, 9.93–27.8 ppm, and 111–133 ppm, respectively. In addition, these samples contained low contents of siderophile elements, e.g., Sc, V, Cr, and Co concentrations were 3.22–5.32 ppm, 21.5–33.5 ppm, 12.7–33.7 ppm, 2.75–5.45 ppm, respectively. Moreover, the volatile element B (7.21–14.7 ppm) was significantly lower than that in Pankou and Pukouling granites.

4.4. Sr–Nd–Pb Isotope Ratios of the Wuzhutang Granite

Sr–Nd–Pb isotope ratios of the granite samples are listed in Table 4 and Table 5. The granite samples possessed 87Sr/86Sr(t) = 0.70747–0.70865, and 143Nd/144Nd = 0.511175–0.511966, with εNd(t) values of −6.35 to −4.34. Owing to the low εNd(t) values, the calculated two-stage model ages were reliable. Lead isotope ratios of the granite samples were 206Pb/204Pb = 18.186–18.3, 207Pb/204Pb = 15.556–15.592, and 208Pb/204Pb = 38.268–38.432.

5. Discussion

5.1. Age of the Xuebaoding Mining Area

The magmatic age of the Wuzhutang granite in this study was 218.98 ± 1.12 Ma, which means that it predates the Pukouling and Pankou granites (200.6 ± 1.2 Ma and 193.7 ± 1.1 Ma, respectively) [32]. The W–Sn–Be mineralization age (213.5 ± 1.7 Ma) of the ore vein in the Wuzhutang granite indicates that it predates the ore veins on the eastern side of the Zibaishan dome. Metallogenic ages obtained from the eastern Zibaishan dome were: (1) a quartz 40Ar/39Ar age of 191.8 ± 0.7 Ma [31]; (2) a muscovite 40Ar/39Ar plateau age of 189.9 ± 1.8 Ma [20]; (3) a scheelite Sm–Nd isochron age of 182.0 ± 9.2 Ma [25]; (4) cassiterite U–Pb ages of 194.8 ± 6.2 Ma and 194.8 ± 6.4 Ma [59]; (5) a muscovite 40Ar/39Ar age of 193.6 ± 6 Ma and a cassiterite U–Pb age of 194.53 ± 1.0 Ma [33]; and (6) a muscovite 40Ar/39Ar age of 195.7 ± 2.5 Ma [24]. In addition, a biotite K–Ar age of 244 Ma was obtained for the biotite granite at the periphery of the Xuebaoding mining area [60], and a muscovite K–Ar age of 164 Ma was obtained for the early Yanshanian granite group exposed in the Zibaishan–Wuzhutang area [61]. All these ages reflect that rare metal mineralization mainly occurred during the late stage of the Indosinian, and that two epochs of diagenesis and mineralization events have occurred in the Xuebaoding mining area. Such ages are coupled with those of pegmatite-type rare metal deposits in other areas of the SGOB, implying a widespread tectono–magmatic event. The characteristics of diagenesis and mineralization on the eastern and western sides of the dome differ primarily in terms of two aspects: (1) the diagenesis and mineralization ages of the Wuzhutang granite indicate that it is older than the Pukouling and Pankou granites; (2) in contrast with the eastern side of the Zibaishan dome, beryllium mineralization mainly occurred in the interior of the Wuzhutang granite body (Figure 2). In addition, unlike the Wuzhutang granite, ideal SHRIMP U–Pb results for zircons from the Pankou and Pukouling granites have not been obtained, which may be attributable to the fact that these zircons contain U-bearing mineral inclusions and have experienced radiation damage [38]. These differences may be closely related to the petrogeochemical characteristics of the granites on the eastern and western sides of the Zibaishan dome.

5.2. Petrogenesis of the Wuzhutang Granite

The Wuzhutang granite contained abundant muscovite and exhibited SiO2 concentrations in excess of 67%, an aluminum saturation index greater than 1, a C value (corundum content) greater than 1 (based on of CIPW calculations), 87Sr/86Sr(t) > 0.706, and εNd < −2%, indicating peraluminous properties [62,63,64], which were similar to the properties of the Pankou and Pukouling granites [39]. In the Harker diagram (Figure 8), the CaO, Fe2O3T, and MgO contents of the Wuzhutang granite displays an obvious negative linear correlation with SiO2 content, and the Na2O/CaO vs. Al2O3/CaO, Na2O/CaO vs. SiO2/CaO, and SiO2/MgO vs. Al2O3/MgO plots display an obvious positive linear correlation. Although samples of the Pankou and Pukouling granites display similar trends, their data points are relatively scattered, which indicates that the Wuzhutang granite originated from a relatively more homogeneous magma source [65].
Compared with typical S- and I-type granites [66], the Wuzhutang granite was enriched in Sr (333.62–441.3 ppm), which imparts partially adakitic properties to the samples (Sr/Y > 20, Y < 20 ppm; e.g., [67]), but with slightly lower Sr contents, significantly lower Cr contents, higher Rb/Sr and CaO/Na2O ratios, higher K2O contents, and a higher A/CNK ratio than those of typical adakites. The Ba contents in samples of the Wuzhutang granite were also high, but they did not reach the levels seen in typical high Ba–Sr granites (Ba + Sr > 2000 ppm; e.g., [68,69]). The granites in the Xuebaoding mining area were once considered to have the characteristics of A-type granite [25]. Based on elemental geochemistry and Sr–Nd and B isotopic data, the Pankou and Pukouling granites were reclassified as highly differentiated S-type granites, derived from the partial melting of metasedimentary rocks [25]. The Wuzhutang granite contained higher SiO2, CaO, FeO, MgO, TiO2, and ∑REE contents, and relatively lower Al2O3, K2O, Na2O, Rb, and Cs contents than the Pankou and Pukouling granites. The Pankou and Pukouling granites displayed a depletion in Nb, strong negative Eu anomaly, and slight depletion in Ta. By contrast, the Wuzhutang granite was characterized by significantly high Ba and Sr contents, weak negative Eu anomalies, and weak decoupling between Nb and Ta. In the Harker, chondrite-normalized REE, and primitive mantle-normalized trace element distribution diagrams, almost no similarity was discovered between the Wuzhutang granite and the other two granites, reflecting the occurrence of different magmatic processes.
The La/Yb and (La/Yb)N values of the Wuzhutang granite samples were much higher than those of the Pankou and Pukouling granites, suggesting that the source of the Wuzhutang granite magma was deeper than that of the Pankou and Pukouling granites [70]. The εNd(t) values of the Wuzhutang, Pankou, and Pukouling granites were −6.35 to −4.34, −11.65 to −23.19, and −11.49 to −12.39, and the 87Sr/86Sr(t) ratios were 0.70747–0.70865, 0.711569–0.732583, and 0.673054–0.712731, respectively, indicating that the three granites have a crustal source, which is consistent with the results of the Pb isotope analysis. Notably, the Wuzhutang granite has significantly higher εNd(t) values and lower 87Sr/86Sr(t) values than the Pankou and Pukouling granites.
In the AMF vs. CMF diagram (Figure 9a), the Pankou and Pukouling granite samples plot mainly in the field of metagraywackes, and a few samples plot in the field of metapelites. Although all data points of the Wuzhutang granite plot in the field of metagraywackes, they are very close to the field of metabasaltic to metatonalitic sources, implying they originated from a deeper source. In the 87Sr/86Sr(t) vs. εNd(t) diagram (Figure 9b), samples of the Wuzhutang, Pankou, and Pukouling granites plot in two completely different fields. The data points of the Pankou and Pukouling samples plot in and near the field of the Songpan–Garze metasediments, but they are extremely scattered, indicating an inhomogeneous and shallow crustal source, which is consistent with the insights revealed by the Harker (Figure 8) and 206Pb/204Pb vs. 208Pb/204Pb diagrams (Figure 10). In contrast, the data points of the Wuzhutang granite samples are relatively concentrated, and plot in and near the field of the western Yangtze craton, overlapping with the area defined by the Songpan–Garze Indosinian high-K calc–alkaline I-type granite (Figure 9). The Sr–Nd isotope composition (Table 4) indicates that the Wuzhutang granite originated from a deeper source than the Pankou and Pukouling granites, which could be a Mesoproterozoic basement (TDM = 1327~1604 Ma). In addition, most Wuzhutang granite samples had higher 87Sr/86Sr(t) values than those of the western Yangtze craton (the data points of samples plot in the area between the western Yangtze craton and the Songpan–Garze metasediments), implying that the protoliths of the Wuzhutang magma contain sedimentary components with high Isr values, which could be the reason for the high Sr/Y ratio of the magma [71]. Taken together, we believe that the elemental geochemistry and Sr–Nd–Pb isotope analyses indicate that although the three granites are in close geographical proximity and all belong to a peraluminous magma system (Figure 11b), the magma of the Wuzhutang granite exhibits a lower differentiation degree (Figure 11a), and may originate from a deeper source than that of the Pankou and Pukouling granites.

5.3. Magmatic and Metallogenic Processes in the Xuebaoding Mining Area

Although the SGOB was strongly reformed during the Cenozoic [77,78], its deformation process mainly occurred during the Late Triassic or Indosinian [46,79]. The Indosinian orogeny in the SGOB is characterized by the formation of a thick accretionary flysch orogenic wedge and the intrusion of a large number of orogenic and post-orogenic granitic magmas [80,81,82]. The strong compressional regime caused the formation of nappes in the South Qinling area during the late Indosinian, forming a series of N–S-trending longitudinal bending folds and E–W-trending brittle ductile fault zones, accompanied by the intrusion of medium and acidic magmas, which provided favorable geological conditions for large-scale rare metal mineralization (Figure 12a). Under a regime of extension and decompression, these granitic magmas intruded into the Triassic metamorphic flysch, forming magmatic diapiric domes [78,83,84]. Pegmatite-type and magmatic hydrothermal deposits with rare metal (Li, Be, Nb, Ta, W, Sn, etc.) mineralization often occur in these domes [49,85,86], and these deposits have a close genetic relationship with the highly differentiated, peraluminous granites in the cores of the domes [85,86]. It is generally believed that these granites are derived from the remelting of Triassic metamorphic flysch in the upper crust (e.g., [1,14,38,87]). The generation of these magmas may be ascribed to shear heating along the detachment zone [49,85,86,88], or the upwelling of heat triggered by continental delamination during the late stage of the orogeny [89,90]. The magmatic activity and rare metal mineralization in the Xuebaoding mining area occurred during the same stage of tectonic evolution as other pegmatite-type deposits in western Sichuan, and differences in their protoliths may be one of the factors affecting the properties of granitoids and mineralization types during the remelting of sedimentary strata [91].
In this study, we found that the Wuzhutang granite (~218 Ma) in the western Zibaishan dome is an important ore-forming rock for rare metal mineralization, as are the highly differentiated and peraluminous Pukouling and Pankou granites (201~194 Ma; [38]). Although all three granites are peraluminous granites, a lower degree of differentiation and a deeper origin have been confirmed for the Wuzhutang granite, indicating that these granites experienced different evolutionary paths. Chronological data indicate that these granites may have undergone two epochs of magmatic evolution and metallogenic processes (Figure 12b). The phenomenon whereby magmatic rocks of different origins are mixed with sedimentary rocks in different proportions in different homologous areas is common in Songpan–Garze granitoids [91]. Although the degree of differentiation of the Wuzhutang granite is lower and the magma source is deeper than that of the Pukouling and Pankou granites, they are all highly differentiated granites. The source areas of the three granites may be mixed with some W–Sn–Be rich materials, e.g., a W–Sn–Be-bearing metasedimentary strata comparable to the Shuangqiaoshan Formation in southern China [92,93,94].
The magmatic and metallogenetic processes in the Xuebaoding area can be summarized as follows (Figure 12b): During the Late Triassic, intense compression and thickening caused the partial melting of the Mesoproterozoic metamorphic basement in the lower part of the Triassic flysch deposits, forming the magma chamber of the Wuzhutang granite; this underwent upwelling during the late Indosinian. The existence of a large amount of volatile F, B, and P lowered the solidus temperature and promoted the crystallization and differentiation of the magma melt [95]; it also improved the solubility of alkali metals and large ion lithophile elements such as W, Sn, Be, Li, Rb, and Cs [96,97,98,99]. In the western part of the Zibaishan dome, owing to local tectonic movements, the monzogranite melt differentiated from the deep magma chamber and intruded upward into the Zagunao Formation at approximately 218 Ma. During the late stage of magmatic evolution (213 Ma), the exsolution of F-rich fluid further enriched the ore-forming elements. The cooling of the granite body produced radial tensile fractures in the overlying marble. During its upward migration along the fractures, the addition of Ca2+ from the marble caused the formation of coarse scheelite and beryl crystals via chemical precipitation. During 201~194 Ma, the albite granite melts in the eastern part of the Zibaishan dome intruded into the strata and subsequently underwent the same mineralization process (195.6~182 Ma). As the Pukouling and Pankou granites underwent a higher degree of crystallization differentiation, both the scale and extension of mineralization and the particle size of the rare metal minerals in the eastern part of the dome are larger than those in the western part.

6. Conclusions

(1)
The magma emplacement and mineralization of the Wuzhutang granite occurred during the late Indosinian, and predate those of the granites in the eastern part of the Zibaishan dome. The Xuebaoding mining area may have undergone two epochs of magmatic evolution and metallogenic processes;
(2)
The Wuzhutang granite contains a certain amount of plagioclase and relatively high contents of Ba and Sr. Although the Wuzhutang granite belongs to a peraluminous magma system, as do the Pukouling and Pankou granites, the magma of the Wuzhutang granite originated from a deeper source and exhibits a lower differentiation degree;
(3)
The W–Sn–Be mineralization within the Zibaishan dome has a close genetic relationship with these highly fractionated granites.

Author Contributions

Conceptualization, H.D. and D.W.; data curation, H.D.; writing—original draft preparation, H.D.; writing—review and editing, H.D., X.L., S.L., C.W. and Y.S. All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by the National Key Research and Development Program of China (2021YFC2901900 and 2021YFC2901905), and the China Geological Survey’s projects (DD20221684, DD20190173 and DD20190379).

Acknowledgments

We acknowledge support for field work undertaken by W. Li and former miners at the Xuebaoding mining area, and experimental support from Q. Wang at MNR Key Laboratory of Metallogeny and Mineral Assessment and J.R. Tu at Tianjin Center of China Geological. We also appreciate four anonymous reviewers for their valuable revision suggestions.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Sketch of regional tectonics and distribution of rare metal deposits in Western Sichuan, China (after [48]).
Figure 1. Sketch of regional tectonics and distribution of rare metal deposits in Western Sichuan, China (after [48]).
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Figure 2. (a) Simplified regional geological map of the Xuebaoding W–Be–Sn mining area. (b) Geological map of the Wuzhutang granite. The age of the Pukouling and Pankou granite follows [38].
Figure 2. (a) Simplified regional geological map of the Xuebaoding W–Be–Sn mining area. (b) Geological map of the Wuzhutang granite. The age of the Pukouling and Pankou granite follows [38].
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Figure 3. (a) Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (b) Wuzhutang granite and marble from the Middle Triassic Zagunao Formation (T and W–Sn–Be quartz vein in adit PD03 from the Xuebaoding mining area). (c) Greisenization zone of the Wuzhutang granite in adit PD03 from the Xuebaoding mining area. (d) Monzogranite and quartz vein bearing beryl, cassiterite, and scheelite from the Wuzhutang granite. (e) Planar greisenization in the ore-bearing quartz vein in the crystal cave structure in adit PD03. (f) Beryl and cassiterite ores with coarse euhedral crystals. (g) Microscopic characteristics of monzogranite. (h) Microscopic characteristics of the quartz vein bearing beryl, cassiterite, and scheelite. (i) Backscattered electron image of the quartz vein beryl, cassiterite, and scheelite. Abbreviation: Ab—Albite, Brl—Beryl, Cas—Cassiterite, Sch—Scheelite, Mus—Muscovite, Pl—Plagioclase, Kfs—K-feldspar, Qtz—Quartz.
Figure 3. (a) Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (b) Wuzhutang granite and marble from the Middle Triassic Zagunao Formation (T and W–Sn–Be quartz vein in adit PD03 from the Xuebaoding mining area). (c) Greisenization zone of the Wuzhutang granite in adit PD03 from the Xuebaoding mining area. (d) Monzogranite and quartz vein bearing beryl, cassiterite, and scheelite from the Wuzhutang granite. (e) Planar greisenization in the ore-bearing quartz vein in the crystal cave structure in adit PD03. (f) Beryl and cassiterite ores with coarse euhedral crystals. (g) Microscopic characteristics of monzogranite. (h) Microscopic characteristics of the quartz vein bearing beryl, cassiterite, and scheelite. (i) Backscattered electron image of the quartz vein beryl, cassiterite, and scheelite. Abbreviation: Ab—Albite, Brl—Beryl, Cas—Cassiterite, Sch—Scheelite, Mus—Muscovite, Pl—Plagioclase, Kfs—K-feldspar, Qtz—Quartz.
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Figure 4. Cathodoluminescence images and ages of zircons in the monzogranite from the Wuzhutang granite in the Xuebaoding mining area, Sichuan Province, China. (a) Characteristics and dating results of zircon. (b) Concord age of zircon. (c) Weighted mean age of zircon.
Figure 4. Cathodoluminescence images and ages of zircons in the monzogranite from the Wuzhutang granite in the Xuebaoding mining area, Sichuan Province, China. (a) Characteristics and dating results of zircon. (b) Concord age of zircon. (c) Weighted mean age of zircon.
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Figure 5. LA-MC-ICPMS cassiterite U–Pb age of the beryl-, cassiterite-, and scheelite-bearing quartz vein in the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China.
Figure 5. LA-MC-ICPMS cassiterite U–Pb age of the beryl-, cassiterite-, and scheelite-bearing quartz vein in the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China.
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Figure 6. (a) TAS diagram (after [55]) of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (b) ANOR vs. Q’ diagram (after [56]) of the Wuzhutang granite. (c) A/CNK vs. A/NK diagram (after [57]) of the Wuzhutang granite. Data of A-type granite and highly fractionated granites are from [44]. (d) SiO2 vs. K2O diagram (after [57]) of the Wuzhutang granite. Data of the Pankou and Pukouling granites are from [38,39].
Figure 6. (a) TAS diagram (after [55]) of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (b) ANOR vs. Q’ diagram (after [56]) of the Wuzhutang granite. (c) A/CNK vs. A/NK diagram (after [57]) of the Wuzhutang granite. Data of A-type granite and highly fractionated granites are from [44]. (d) SiO2 vs. K2O diagram (after [57]) of the Wuzhutang granite. Data of the Pankou and Pukouling granites are from [38,39].
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Figure 7. (a) Chondrite-normalized REE distribution patterns and (b)primitive mantle-normalized trace element spider diagrams of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data for the chondrite and primitive mantle are computed from [58], and data of the Pankou and Pukouling granites are from [38,39].
Figure 7. (a) Chondrite-normalized REE distribution patterns and (b)primitive mantle-normalized trace element spider diagrams of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data for the chondrite and primitive mantle are computed from [58], and data of the Pankou and Pukouling granites are from [38,39].
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Figure 8. Harker diagram of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data of the Pankou and Pukouling granites are from [38,39].
Figure 8. Harker diagram of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data of the Pankou and Pukouling granites are from [38,39].
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Figure 9. Binary diagrams showing the source of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (a) Plot of CMF vs. AMF (CMF-CaO/(MgO + FeOT); AMF-Al2O3/(MgO + FeOT) (after [72]) of the Wuzhutang granite. (b) Plot of 87Sr/86Sr(t) vs. Nd(t) of the Wuzhutang granite. Sr–Nd isotopic data of the SGOB high-K calc–alkaline I-type granite is from [73,74], that of the SGOB peraluminous S-type granite is from [47,74,75], that of the SGOB metasediments is from [47,74], that of the western Yangtze craton is from [74]; geochemical data of the Pankou and Pukouling granites are from [38,39].
Figure 9. Binary diagrams showing the source of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (a) Plot of CMF vs. AMF (CMF-CaO/(MgO + FeOT); AMF-Al2O3/(MgO + FeOT) (after [72]) of the Wuzhutang granite. (b) Plot of 87Sr/86Sr(t) vs. Nd(t) of the Wuzhutang granite. Sr–Nd isotopic data of the SGOB high-K calc–alkaline I-type granite is from [73,74], that of the SGOB peraluminous S-type granite is from [47,74,75], that of the SGOB metasediments is from [47,74], that of the western Yangtze craton is from [74]; geochemical data of the Pankou and Pukouling granites are from [38,39].
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Figure 10. Plot of 206Pb/204Pb vs. 208Pb/204Pb (after [76]) of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data of the Pankou and Pukouling granites are from [39].
Figure 10. Plot of 206Pb/204Pb vs. 208Pb/204Pb (after [76]) of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. Data of the Pankou and Pukouling granites are from [39].
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Figure 11. Binary diagrams showing the degree of differentiation of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (a) Plot of SI vs. DI of the Wuzhutang granite. (b) Plot of Zr/Hf vs. Nb/Ta of the Wuzhutang granite. Data of highly fractionated granites are from [44], data of the Pankou and Pukouling granites are from [38,39].
Figure 11. Binary diagrams showing the degree of differentiation of the Wuzhutang granite from the Xuebaoding mining area, Sichuan Province, China. (a) Plot of SI vs. DI of the Wuzhutang granite. (b) Plot of Zr/Hf vs. Nb/Ta of the Wuzhutang granite. Data of highly fractionated granites are from [44], data of the Pankou and Pukouling granites are from [38,39].
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Figure 12. (a) Schematic model explaining the geodynamic setting of the rare metal mineralization in the Songpan–Garze orogenic belt (modified after [90]). (b) Schematic model illustrating the formation of granitoids and ore veins in the Xuebaoding mining area, Sichuan Province, China.
Figure 12. (a) Schematic model explaining the geodynamic setting of the rare metal mineralization in the Songpan–Garze orogenic belt (modified after [90]). (b) Schematic model illustrating the formation of granitoids and ore veins in the Xuebaoding mining area, Sichuan Province, China.
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Table
Table 1. LA-ICP-MS U–Pb isotopic data for zircon in the Wuzhutang granite from the Xuebaoding mining area.
Table 1. LA-ICP-MS U–Pb isotopic data for zircon in the Wuzhutang granite from the Xuebaoding mining area.
Sample
Spot		WB/10−6Common Pb Isotope Ratio (±1σ)Common Pb Isotope Age (Ma) (±1σ)
PbThUTh/U207Pb/206Pb207Pb/235U206Pb/238U207Pb/206Pb207Pb/235U206Pb/238U
Ratio±1σRatio±1σRatio±1σAge±1σAge±1σAge±1σ
pwWZTG-199.84407.202867.990.140.061740.002540.287310.011800.033650.00078664.8387.02256.449.31213.384.90
pwWZTG-243.72180.841190.970.150.053000.002250.246020.010200.033560.00069327.8496.29223.348.32212.804.32
pwWZTG-390.79463.302240.630.210.085630.003440.414850.020550.034770.000771331.4877.78352.3614.75220.314.78
pwWZTG-433.48282.47811.460.350.059210.002560.281260.011820.034460.00093575.9692.58251.659.37218.415.82
pwWZTG-527.30218.09667.030.330.064820.003860.304910.018480.034000.00080768.52130.55270.2314.38215.554.96
pwWZTG-665.26791.521630.900.490.054480.001720.262270.008720.034830.00080390.7972.22236.497.01220.714.98
pwWZTG-787.21269.372569.530.100.051000.001810.243380.009650.034690.00099242.6676.84221.197.88219.836.16
pwWZTG-8107.69573.923005.740.190.056270.001950.265620.008850.034360.00099461.1677.77239.197.10217.766.17
pwWZTG-999.18424.262773.950.150.055460.002820.253700.012750.034330.00104431.53108.32229.5710.33217.626.48
pwWZTG-1046.12248.021255.660.200.050670.002930.237220.012590.034020.00062233.40133.32216.1410.33215.683.89
pwWZTG-11119.32545.993538.420.150.053860.001770.223700.007260.030110.00056364.8769.44204.986.03191.273.48
pwWZTG-1266.60433.301744.150.250.057640.002600.273910.011950.034500.00071516.7199.99245.819.53218.644.40
pwWZTG-1348.71575.081230.140.470.051670.001710.244130.008610.034210.00059333.3975.91221.807.03216.853.70
pwWZTG-1439.59318.671001.790.320.051560.001960.248630.010740.034850.00071264.8887.02225.468.74220.834.45
pwWZTG-1566.24216.801856.360.120.052670.001820.247830.008750.034170.00077322.2877.77224.817.12216.574.82
pwWZTG-1685.87472.882367.310.200.053670.001620.244500.010020.032840.00080366.7273.14222.108.18208.315.01
pwWZTG-1739.58259.051037.320.250.051820.002260.253720.010230.035660.00087275.9999.99229.598.28225.905.39
pwWZTG-1851.92213.271384.270.150.051510.002240.252060.012990.035270.00072264.8899.99228.2510.54223.454.49
pwWZTG-1980.18154.342243.420.070.054090.001940.261960.012140.035020.00105375.9876.85236.249.77221.916.57
pwWZTG-2032.28382.12808.350.470.050100.002140.238930.010590.034510.00055198.2398.13217.548.68218.713.42
pwWZTG-2162.77570.561707.320.330.051660.001450.243300.006880.034170.00059333.3966.66221.125.61216.613.68
pwWZTG-2227.86184.31741.430.250.049940.002140.239640.010350.034850.00066190.8293.51218.138.48220.814.13
pwWZTG-23117.73401.163405.310.120.053390.001350.261240.009330.035450.00091346.3589.81235.667.51224.565.68
pwWZTG-2418.57120.40318.440.380.052440.003470.244530.014780.034170.00145305.62151.83222.1212.06216.579.02
pwWZTG-25116.271163.263330.850.350.051940.001620.224130.007520.031340.00073283.4072.22205.346.24198.964.55
pwWZTG-2640.44383.531054.140.360.057050.002440.279280.012200.035640.00075494.4994.43250.099.68225.744.66
pwWZTG-2730.33191.77842.750.230.054370.002440.258600.012000.034540.00081387.0999.99233.549.68218.905.04
pwWZTG-2882.33286.922491.560.120.049850.001600.234730.008380.034260.00089187.1269.43214.106.89217.155.53
pwWZTG-2931.11283.61832.240.340.055950.003030.264320.013740.034470.00078450.05120.36238.1411.04218.474.84
pwWZTG-3064.62756.731582.620.480.053200.002300.259400.011410.035500.00084344.5098.14234.189.20224.885.22
pwWZTG-3173.931037.951905.510.540.055030.001790.257230.008550.034000.00061413.0172.22232.436.91215.533.83
pwWZTG-3237.11510.55966.480.530.058580.002730.265210.011920.033010.00085550.0497.21238.859.57209.335.34
pwWZTG-33102.85168.432901.050.060.053060.001370.252270.008010.034420.00064331.5457.40228.426.49218.144.01
pwWZTG-3476.65347.651881.260.180.054150.002000.291670.010660.039120.00089375.9878.70259.878.38247.405.49
Table
Table 2. LA-ICP-MS U–Pb isotopic data for cassiterite in the Wuzhutang granite from the Xuebaoding mining area.
Table 2. LA-ICP-MS U–Pb isotopic data for cassiterite in the Wuzhutang granite from the Xuebaoding mining area.
Sample
Spot		WB/10−6T-W ConcordantSample
Spot		WB/10−6T-W Concordant
PbThU238U/206PbErr% × 2207Pb/206PbErr% × 2PbThU238U/206PbErr% × 2207Pb/206PbErr% × 2
PD03-#4-10.00.11.627.996.50.139624.6PD03-#4-460.10.03.229.274.60.080416.7
PD03-#4-20.10.01.828.815.60.118560.5PD03-#4-470.00.01.728.626.30.105525.8
PD03-#4-30.10.02.028.655.70.103319.2PD03-#4-480.10.12.227.285.00.130016.0
PD03-#4-40.10.02.129.895.60.090225.1PD03-#4-490.00.01.328.206.80.122323.5
PD03-#4-50.00.00.730.0410.90.1009121.5PD03-#4-500.00.01.130.627.00.104429.9
PD03-#4-60.00.01.227.038.00.167120.5PD03-#4-510.00.01.829.016.50.094027.2
PD03-#4-70.10.03.029.495.00.072122.3PD03-#4-520.10.01.928.675.80.086422.7
PD03-#4-80.10.11.629.875.70.097725.6PD03-#4-530.10.02.927.354.70.142215.5
PD03-#4-90.00.00.928.097.10.153422.8PD03-#4-540.10.11.725.506.00.221916.1
PD03-#4-100.10.01.528.436.00.154722.3PD03-#4-550.10.02.127.845.50.099823.2
PD03-#4-110.00.01.226.016.60.183322.1PD03-#4-560.10.12.028.505.20.088319.0
PD03-#4-120.00.01.227.626.60.178120.5PD03-#4-570.10.01.927.845.90.071240.3
PD03-#4-130.10.13.427.144.20.089915.8PD03-#4-580.10.12.828.524.20.073718.7
PD03-#4-140.10.02.428.035.00.073521.8PD03-#4-590.10.12.928.434.30.064816.2
PD03-#4-150.10.05.228.993.20.067515.0PD03-#4-600.00.01.528.826.40.123322.5
PD03-#4-160.00.11.327.366.10.111826.3PD03-#4-610.10.11.928.035.80.087725.9
PD03-#4-170.10.03.329.064.40.064918.4PD03-#4-620.00.11.627.705.80.090423.0
PD03-#4-180.00.01.227.996.90.181823.6PD03-#4-630.00.01.427.797.50.167222.9
PD03-#4-190.00.01.329.277.60.104224.8PD03-#4-640.10.04.929.854.00.059015.0
PD03-#4-200.10.02.128.385.80.109420.8PD03-#4-650.00.01.528.936.20.086027.7
PD03-#4-210.10.15.328.433.40.075619.5PD03-#4-660.10.03.429.304.60.060618.3
PD03-#4-220.10.04.027.804.10.106220.8PD03-#4-670.10.14.128.414.10.062317.8
PD03-#4-230.10.04.328.183.70.069516.4PD03-#4-680.10.01.827.985.60.093123.1
PD03-#4-240.10.05.028.723.90.075217.0PD03-#4-690.10.00.720.709.30.381028.4
PD03-#4-250.00.11.828.486.60.110224.5PD03-#4-700.10.02.025.935.00.145816.4
PD03-#4-260.00.01.225.088.20.199434.3PD03-#4-710.10.02.127.746.30.095820.2
PD03-#4-270.00.11.127.409.80.175722.0PD03-#4-720.10.04.329.493.70.072414.1
PD03-#4-280.10.01.928.806.50.096226.0PD03-#4-730.00.01.127.778.10.093125.7
PD03-#4-290.10.02.226.805.20.138917.1PD03-#4-740.00.00.425.2411.40.286138.3
PD03-#4-300.00.11.730.106.30.114720.1PD03-#4-750.10.02.126.1720.90.084419.9
PD03-#4-310.10.02.527.334.90.128315.7PD03-#4-760.00.01.529.655.60.088522.4
PD03-#4-320.10.13.829.013.70.068717.2PD03-#4-770.10.02.330.095.00.076318.2
PD03-#4-330.10.02.128.015.30.093221.7PD03-#4-780.20.06.628.732.90.053613.7
PD03-#4-340.00.01.029.568.60.141537.2PD03-#4-790.10.02.029.065.30.080919.3
PD03-#4-350.00.01.227.847.70.129334.8PD03-#4-800.20.06.529.563.20.051516.1
PD03-#4-360.00.00.827.678.90.132534.6PD03-#4-810.00.00.628.7310.90.247634.5
PD03-#4-370.00.01.729.175.60.065524.8PD03-#4-820.10.02.229.915.60.088420.0
PD03-#4-380.10.12.127.924.90.094119.8PD03-#4-830.00.01.427.726.70.092523.8
PD03-#4-390.10.13.627.134.00.129812.1PD03-#4-840.10.02.725.145.30.203814.7
PD03-#4-400.10.03.629.804.20.077517.9PD03-#4-850.10.01.826.085.60.182418.2
PD03-#4-410.10.03.128.204.50.079518.4PD03-#4-860.00.01.128.767.00.121927.3
PD03-#4-420.10.11.820.415.50.29299.5PD03-#4-870.00.01.628.366.40.081226.3
PD03-#4-430.00.00.826.1610.00.228329.7PD03-#4-880.20.02.622.084.90.28499.4
PD03-#4-440.10.03.030.724.40.063717.3PD03-#4-890.00.00.524.939.70.170833.0
PD03-#4-450.20.05.827.778.10.060412.9PD03-#4-900.10.02.429.004.80.077419.2
Table
Table 3. Analysis results of the major (wt.%) and trace (ppm) elements of the Wuzhutang granite from the Xuebaoding mining area.
Table 3. Analysis results of the major (wt.%) and trace (ppm) elements of the Wuzhutang granite from the Xuebaoding mining area.
SampleH1H3H4H6H7H1H3H4H6H7H11H13
PD01PD03
SiO272.0271.3471.5670.3869.8171.0671.3170.7570.8372.0571.6171.04
TiO20.250.250.260.260.30.270.250.260.270.250.250.26
Al2O315.3115.4115.4814.8815.4415.3815.4615.315.4415.4815.3915.31
FeO1.120.971.061.241.311.071.131.051.091.021.141.15
Fe2O30.360.530.540.20.540.550.360.430.50.370.310.36
MnO0.030.030.040.030.040.040.030.030.030.030.030.03
MgO0.820.840.830.81.290.860.810.790.890.660.690.78
CaO1.8921.913.152.6221.872.422.091.931.921.96
Na2O4.454.44.54.284.54.54.434.434.574.474.514.39
K2O3.453.563.463.293.243.313.453.293.43.53.393.47
P2O50.10.10.10.10.10.090.10.10.10.090.090.1
F0.040.040.040.20.10.040.040.070.040.040.040.04
LOI0.360.530.461.460.870.570.670.780.520.370.460.49
Total100.2100100.24100.27100.1699.7499.9199.799.77100.2599.8399.38
Na2O + K2O7.97.967.967.577.747.817.887.727.977.977.97.86
A/NK1.381.391.391.41.421.41.41.411.381.391.391.39
A/CNK1.071.061.080.9211.071.091.021.051.071.071.07
DI85.5285.1785.3281.9581.1684.7685.3183.6584.685.8885.6185.12
SI8.048.157.998.1511.858.367.957.918.526.596.877.68
Li73.4667.1670.9166.4468.8261.5779.9668.2362.8973.3374.1975.96
W3.4945.612.96127.730.8916.9634.4211.3225.648.645.3110.94
Sn4.3310.444.685.374.415.3411.8411.1575.7414.6821.8314.56
Be8.2133.266.475.164.036.696.074.09105.35.5826.39
B9.168.059.678.768.9914.514.6811.4311.069.9314.247.21
Rb127.7132.8130.1127.9114.4112.4117.5127.8123.1119.7111.33132.7
Sr350.48366.93361.46349.44411.3374.98333.62387.55376.16383.01361.22359.35
Rb127.7132.8130.1127.9114.4112.4117.5127.8123.1119.7111.33132.7
Sr350.48366.93361.46349.44411.3374.98333.62387.55376.16383.01361.22359.35
Ba711.41007701704.85884.2647.8742.65633737.9725653.35704.3
Co3.563.343.713.455.453.93.683.864.652.753.293.92
Cr16.551715.8917.5633.6519.414.521.416.4712.718.5924.27
Cs16.0416.3410.8611.2611.4316.4613.6427.8312.139.9311.7315.19
Zn52.4141.4540.9442.0244.7341.8544.7441.5140.2842.3739.4344.13
Nb5.987.447.187.026.466.557.646.156.326.176.856.2
Ta0.70.660.840.760.620.760.920.650.970.860.810.76
Th8.496.316.996.357.027.196.926.556.296.086.67.72
U2.883.161.892.222.242.172.883.122.31.92.012.17
Zr102.69122.12110.82108.53122.43109.91117.06115.28119.26123.01115.09115.21
Hf3.123.683.313.293.553.433.573.443.553.613.453.4
Sc4.193.984.024.085.324.33.993.824.063.223.643.82
Ti16501725.2416221762.931875.991768.381579.521727.181754.91592.111699.241671.8
V24.5921.6325.725.3833.4926.4624.7827.127.3221.5423.7626.04
Bi0.740.911.490.830.520.830.710.810.490.390.50.29
Cd0.070.090.090.060.050.130.080.080.050.030.060.05
Ga23.2721.2620.3521.1222.423.321.8524.3121.0819.3624.1420.73
Y7.627.437.958.668.438.17.947.697.617.966.898.72
Cl48.6695.1832.7947.7855.5929.1940.3155.4583.8635.56120.4135.55
La16.417.61719.517.416.915.623.717.118.520.418.3
Ce33.235.634.83934.635.231.364.534.237.141.537.5
Pr3.774.013.864.363.943.793.555.283.854.084.474
Nd13.314.213.514.913.913.512.618.41414.215.813.9
Sm2.752.822.782.942.82.682.623.222.692.742.982.76
Eu0.690.710.690.750.750.740.710.770.720.710.70.72
Gd2.292.32.382.412.382.292.292.652.232.272.322.41
Tb0.320.310.330.340.330.320.320.340.310.310.320.35
Dy1.521.541.651.591.641.531.531.551.491.511.421.74
Ho0.260.250.270.280.280.260.260.260.260.260.230.3
Er0.670.640.720.730.750.710.690.690.660.70.60.77
Tm0.090.090.10.10.110.10.090.090.090.10.090.11
Yb0.610.570.630.680.690.670.60.60.610.620.560.68
Lu0.090.080.090.10.10.10.090.080.090.090.080.09
ΣREE75.9680.7278.8087.6879.6778.7972.25122.1478.3083.1891.4683.63
LREE/HREE11.9812.9611.7713.0811.6912.1811.3118.4912.6513.2115.3011.96
LaN/YbN19.2822.1519.3620.5718.0918.0918.6528.3320.1121.4026.1319.30
δEu0.820.830.800.840.870.890.870.780.870.850.780.83
δCe1.001.001.010.990.981.030.991.350.991.001.021.03
Table
Table 4. Sr–Nd isotopic composition of the Wuzhutang granite in the Xuebaoding mining area.
Table 4. Sr–Nd isotopic composition of the Wuzhutang granite in the Xuebaoding mining area.
SampleAgeRbSr87Rb/86Sr87Sr/86SrIsrεSr(t)
Maμg/g
PD03-H12181123750.86480.7101560.7074745.8
PD03-H32181183341.0230.7118220.7086562.6
PD03-H62181233760.94730.7104460.7075146.4
PD03-H112181113610.89040.7102820.7075246.5
PD03-H132181333591.07280.7110550.7077349.5
SampleSmNd147Sm/144Nd143Nd/144NdINdT2DMεNd(t)
μg/g
PD03-H12.6813.50.120.5122370.5120661458−5.69
PD03-H32.6212.60.12570.5122230.5120441492−6.12
PD03-H62.69140.11620.5123010.5121351348−4.34
PD03-H112.9815.80.1140.5121950.5120321511−6.35
PD03-H132.7613.90.120.5122380.5120671457−5.67
Table
Table 5. Pb isotopic composition of the Wuzhutang granite in the Xuebaoding mining area.
Table 5. Pb isotopic composition of the Wuzhutang granite in the Xuebaoding mining area.
SamplePbThUIsotope Ratio (±2σ)(208Pb/204Pb)i(207Pb/204Pb)i(206Pb/204Pb)i
μg/g208Pb/204Pb±2σ207Pb/204Pb±2σ206Pb/204Pb±2σt = 219Ma
PD03-H1298.492.8838.3960.00715.5760.00218.240.00318.02315.56538.188
PD03-H332.16.313.1638.4320.00315.5920.00118.30.00118.08515.58138.292
PD03-H628.56.352.2238.4230.00515.5890.00218.2080.00218.03815.58038.264
PD03-H11286.62.0138.2680.00715.5560.00318.1860.00318.03015.54838.101
PD03-H1328.27.722.1738.3480.00315.5720.00118.2250.00218.05715.56438.153
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Dai, H.; Wang, D.; Li, X.; Liu, S.; Wang, C.; Sun, Y. Genesis of the Wuzhutang Granite and Associated W–Sn–Be Mineralization in the Xuebaoding Mining Area, Sichuan Province, China. Minerals 2022, 12, 993. https://doi.org/10.3390/min12080993

AMA Style

Dai H, Wang D, Li X, Liu S, Wang C, Sun Y. Genesis of the Wuzhutang Granite and Associated W–Sn–Be Mineralization in the Xuebaoding Mining Area, Sichuan Province, China. Minerals. 2022; 12(8):993. https://doi.org/10.3390/min12080993

Chicago/Turabian Style

Dai, Hongzhang, Denghong Wang, Xin Li, Shanbao Liu, Chenghui Wang, and Yan Sun. 2022. "Genesis of the Wuzhutang Granite and Associated W–Sn–Be Mineralization in the Xuebaoding Mining Area, Sichuan Province, China" Minerals 12, no. 8: 993. https://doi.org/10.3390/min12080993

APA Style

Dai, H., Wang, D., Li, X., Liu, S., Wang, C., & Sun, Y. (2022). Genesis of the Wuzhutang Granite and Associated W–Sn–Be Mineralization in the Xuebaoding Mining Area, Sichuan Province, China. Minerals, 12(8), 993. https://doi.org/10.3390/min12080993

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