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Article

Geochemistry and Zircon U–Pb Geochronology of the Wugongshan Granites in the Northwestern Jiangxi Area, China: Implications for the Paleozoic Tectonic Development of South China

by
Guangqin Yang
1,2,
Yaoyao Zhang
1,*,
Kai Liu
1,
Yi Zhou
2,
Shuxun Wang
1,2 and
Hailong Huo
2,*
1
Chinese Academy of Geological Sciences, Beijing 100037, China
2
School of Gemmology, China University of Geosciences, Beijing 100083, China
*
Authors to whom correspondence should be addressed.
Minerals 2023, 13(11), 1427; https://doi.org/10.3390/min13111427
Submission received: 18 September 2023 / Revised: 29 October 2023 / Accepted: 1 November 2023 / Published: 9 November 2023
(This article belongs to the Special Issue Petrogenesis, Magmatism and Geodynamics of Orogenic Belts)
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Abstract

:
The properties of the Caledonian orogeny along the transition belt of the Yangtze and Cathaysia blocks have received much attention in recent years. The widespread Early Paleozoic granites provide critical geological clues for unraveling the tectonic evolution and geodynamic processes of the South China Continent (SCC). Here we present new zircon U–Pb chronology, whole-rock major and trace elements, in situ Hf isotopes for Paleozoic granites, i.e., the Wugongshan granites in the northwest Jiangxi province, and aim to explore the magmatism and properties of the Caledonian orogeny involved in their formation. Our new data show that the Wugongshan granites were emplaced during the Early Silurian Period (442–438 Ma). The Paleozoic Wugongshan granites belong to S-type muscovite-bearing peraluminous granites (MPG) and show a single origin. The Wugongshan granites exhibit negative εHf(t) values (−11.56 to −6.19) and TDM2 model ages of 2148–1809 Ma, indicating their derivation from an ancient crustal source, through partial melting of ancient crustal material. The Wugongshan granitic magmatism is probably being generated in an extensional environment related to an intracontinental orogeny setting. It is inferred that the Paleozoic tectonic–magmatic event in the Wugongshan area was associated with the oceanic–continental convergence of the Paleo-Tethys Ocean. The Wugongshan granites highlight the intracontinental magmatism in the Early Paleozoic orogeny in the SCC.

1. Introduction

The South China Continent (SCC) is formed by the Yangtze block to the north and the Cathaysia block to the south, and finally collision along the Jiangshan–Shaoxing fault zone during the Meso-Neoproterozoic, and accompanied by the NE-trending Jiangnan orogenic belt (also known as the Jiangnan archicontinent, ca. 850–820 Ma), respectively (Figure 1a) [1,2,3,4,5,6,7,8,9,10,11,12]. Since the Neoproterozoic, South China has long been located in the global supercontinental convergence tectonic background, and experienced Neoproterozoic rifting (ca. 810–760 Ma), Caledonian orogeny (ca. 450–420 Ma), Indosinian intracontinental reworking (ca. 240–220 Ma) and Yanshanian intracontinental orogeny (ca. 180–145 Ma), which have formed the unique geological geomorphology of South China today [7,8,12,13,14,15,16,17]. Therefore, the tectonic properties of South China and the tectonic processes at different stages are of crucial significance for the reconstruction of global supercontinents [14,15,17,18,19,20,21,22].
For decades, a variety of geological studies have been performed in the SCC to understand its tectonic and magmatic evolution [13,14,15,23,24,25,26]. However, the Caledonian orogenesis of the SCC remains enigmatic [10,14,17,19,20,25,26,27,28]. The types of Caledonian orogeny in South China are related to continental collision orogenies [10], or dominated by intracontinental orogenies [13,14,23,27,29], which need to be further studied [30,31]. The purpose of our study on the Wugongshan granites is to determine its petrogenesis and provide insights into the tectonic properties of the Caledonian orogeny in the SCC.
Minerals 13 01427 g001
Figure 1. Geological map of Wugongshan area of the SCC. (a) The inset shows the location of the SCC, modified from [22]. (b) Sketch tectonic map of the Wugongshan and adjacent areas, modified from [31]. (c) Intracontinental orogenic model, modified from [14]. (d) Continental collision orogenic model, modified from [10].
Figure 1. Geological map of Wugongshan area of the SCC. (a) The inset shows the location of the SCC, modified from [22]. (b) Sketch tectonic map of the Wugongshan and adjacent areas, modified from [31]. (c) Intracontinental orogenic model, modified from [14]. (d) Continental collision orogenic model, modified from [10].
Minerals 13 01427 g001
The Wugongshan area is located on the northern edge of the Cathaysia block, on the western part of the Jiangshan–Shaoxing fault zone (JSF)The Paleozoic magmatism is widely developed in the area and records complete information regarding the Paleozoic evolution of the SCC [16,20,24]. As an important junction of the Yangtze and Cathaysia blocks, the Wugongshan area provides a window to understanding the orogeny’s geological framework and the tectonic properties of the SCC during the Caledonian Period [3,13,14,19,32] (Figure 1b). For decades, previous studies have been made on the geological characteristics [33,34,35], petrology, geochemistry [36,37,38,39,40,41], and tectonic evolution [3,32] of the Early Paleozoic granite of the Wugongshan area. Although these studies provide insights into the Paleozoic granite’s evolution in the Wugongshan area, there has been no systematic analysis of the Caledonian tecto-magmatic evolutionary process of South China.
In this paper, we present zircon LA-ICP-MS U–Pb geochronological ages, in situ Hf isotopic data, and whole-rock major- and trace-element data for granites of the Wugongshan area. These new data, in conjunction with published data, help to constrain the relationships between Paleozoic orogeny and magmatic coupling process, and provide additional information concerning the Paleozoic tectonic evolution of South China.

2. Geological Setting

The basement strata in the Wugongshan area are Neoproterozoic–Cambrian weakly metamorphosed sandstone, uncomfortably overlain by the Devonian, Carboniferous-Triassic, and Quaternary strata [3,24,32,33,37,38] (Figure 2). The major lithologies of the Neoproterozoic–Cambrian are meta-greywackes, meta-volcanics, and phyllites, comprising a shallow-water, clastic-dominated meta-sedimentary environment [3,24,32].
The Anfu and Pingxiang basins have developed north and south of the Wugongshan granites (Figure 2). The granites are widely distributed in the Wugongshan area, with most being formed during the Early Paleozoic (Caledonian) and late Mesozoic (Yanshanian) [24,41]. The main rock types include porphyritic granite, gneissic granite, granodiorite biotite granite, two-mica granite, and muscovite granite. The Wugongshan pluton intruded into the Sinian and Cambrian meta-sedimentary strata, and the Yanshanian part consists of foliated gneiss granites in the Sanjiang and Qinglongshan, etc. [3,24,32,37,41].

3. Analytical Methods

In the present study, samples were collected from Xingqun, Qianshan, and Wanlongshan for detailed LA-ICP-MS U–Pb zircon age study, in situ Hf isotopic analyses, and geochemical analyses, with samples collected from different parts of the Wugongshan Paleozoic granites (Figure 2). The recent research shows that the geochemical elements change markedly along strong strain bands and siliceous veins in mylonitic granites, while the change in the geochemical characteristics away from strong strain bands can be ignored [42,43]. Therefore, in this study, to minimize the change in the geochemical characteristics of rocks by mylonitization, we selected samples far from the ductile shear zone, where mylonitization was weak and siliceous veins were absent.

3.1. LA-ICP-MS U–Pb and Hf Zircon Isotopic Analyses

Three representative fresh samples from the surface outcrop of the Wugongshan Paleozoic granites were selected for zircon LA-ICP-MS U–Pb analyses and in situ Hf isotopic dating. Zircon grains were extracted from the samples labeled CJK06–2, WGS06022, and WGS06022, using standard density and magnetic separation techniques, at the Hebei Institute of the Regional Geological Survey, Langfang City, Hebei Province, China. Zircons were photographed in reflected and transmitted light. Cathodoluminescence (CL) photographs of the zircons, LA-ICP-MS U–Pb zircon analyses, and in situ Hf isotopic dating were produced at Gaonian Linghang Technology LLC., Beijing, China, and the sites for zircon U–Pb and Hf analysis were based on these. The zircon U–Pb data and in situ Hf isotopic analyses were carried out using a Finnigan Neptune type LA-ICP-MS instrument with a New Wave UP213 lase, using laser-ablation spots of 20–30 μm diameter. 91,500 zircon and NIST 610 glass standards were used for calibration. Data processing was undertaken using Ludwig SQUID 1.03 and ISOPLOT 3.0 software [44,45,46,47]. Standard zircon Plešovice (337 ± 0.37 Ma) was used for quality control purposes during the in situ Hf isotopic analyses, and a weighted mean 176Hf/177Hf ratio of 0.282480 ± 0.000050 (2σ, n = 18), consistent with a published value of 0.282008 ± 0.000012 was used [48,49,50]. The results are listed in Supplementary Table S1.

3.2. Major- and Trace-Element Analyses

The major- and trace-element composition analyses were determined at the Hebei Institute of the Regional Geological Survey, Langfang City, Hebei Province, China. Major elements were identified using a Philips X-ray fluorescence spectrometer (XRF; Axiosmax). Analytical precision was better than ±5%. Trace elements were analyzed using a Thermofisher X Series 2 (ICP-MS), using procedures similar to the [51]. The results are listed in Supplementary Tables S2 and S3.

4. Results

4.1. Petrography

We collected and analyzed the Early Paleozoic granites from different locations in Wugongshan granites. The representative lithologies included biotite monzonitic granite, two-mica monzonitic granite, and porphyritic two-mica monzonitic granite (Figure 3), which had different degrees of mylonitic characteristics, which are described as follows:
Biotite monzonitic granite (CJK06–2): It is grey in color, has a granitic texture and a mineral plagioclase (0.4~3.0 mm; 45%), K-feldspar (2~5 mm; 15%~20%), quartz (0.05~1.0 mm; 20%~25%), biotite (5%~10%), and minor muscovite (1%) content.
Two-mica monzonite granite (WGS06022): It is grey and composed of plagioclase (0.05~2.0 mm; 30%~45%), K-feldspar (0.05~2.0 mm; 30%~35%), quartz (0.1~3.0 mm; 25%), biotite and muscovite (total 10%). It has a granitic texture and displays a foliation defined by oriented biotite and muscovite.
Porphyritic two-mica monzonite granite (WGS06028): It is grey, has a granitic texture, and is composed of plagioclase (0.2~1.8 mm; 35%~40%), K-feldspar (2~9 mm; 30%~35%), quartz (0.1~0.7 mm; 20%~25%), biotite and muscovite (total 5%~10%).

4.2. Geochronology and Hf Isotopic Compositions

Representative biotite monzonitic granite (CJK06–2), two-mica monzonite granite (WGS06022), and porphyritic two-mica monzonite granite (WGS06028) samples were collected for zircon U–Pb dating. Separated zircons are transparent, mostly euhedral or sub-rounded, and exhibit strong oscillatory zoning and high Th/U ratios (0.19–1.08), typical of a magmatic origin [52,53]. The analytical results for U–Pb and in situ Lu–Hf compositions are listed in Supplementary Tables S1 and S4.
Zircons with oscillatory zoning from samples CJK06–2, WGS06022, and WGS06028 were selected for 206Pb/238U dating (Figure 4). For sample CJK06–2, 26 zircon grains produced concordant results (within error), with a weighted-mean age of 438.9 ± 1.2 Ma (MSWD = 0.33) (Figure 4a). There were 27 analyses of WGS06022, which yielded a weighted-mean age of 439.4 ± 1.9 Ma (MSWD = 0.34) (Figure 4b). There were 31 analyses of WGS06028, which yielded a weighted-mean age of 441.9 ± 1.6 Ma (MSWD = 0.85) (Figure 4c).
For sample CJK06–2, 15 Hf isotopic analyses resulted in εHf(t) values of −9.34 to −6.19 and two-stage model (TDM2) ages of 1809–2006 Ma, with initial 176Hf/177Hf ratios of 0.282250–0.282337, and initial 176Lu/177Hf ratios varying from 0.000889 to 0.002222. There were 16 analyses of WGS06022, which produced εHf(t) values of −10.60 to −8.13 and TDM2 ages of 1930–2086 Ma, with initial 176Hf/177Hf ratios of 0.282219–0.282300, and 176Lu/177Hf ratios of 0.000715–0.002144. There were 18 analyses of WGS06028, which yielded εHf(t) values of −11.56 to −8.25 and TDM2 ages of 1940–2148 Ma, with initial 176Hf/177Hf ratios of 0.282202–0.282286, and 176Lu/177Hf ratios of 0.000934–0.002952 [54].

4.3. Geochemistry

Major- and trace-element compositions of 16 granites are listed in Supplementary Tables S2 and S3. The Wugongshan granite samples are characterized by 65.77–75.82 wt.% SiO2, 2.24–4.46 wt.% Na2O, 2.64–4.95 wt% K2O, 0.08–1.40 wt% MgO, 0.40–5.90 wt% CaO, 12.16–15.46 wt% Al2O3 and 0.02–0.59 wt% TiO2, respectively. A total-alkali-silica (TAS) diagram shows that most samples plot in the granite fields (Figure 5a). Most have high K2O/SiO2 ratios and plot in the potassium field in the K2O–SiO2 diagram (Figure 5b). The samples are peraluminous, with A/CNK values of 0.68–1.31, ALK (total alkali (Na2O+K2O)) contents 5.18–8.62 wt.%, and A/NK values of 1.22–2.15 (Figure 5c). In the AFM diagram, the samples plot in the Calc-alkali field (Figure 5d).
The Wugongshan Paleozoic granite samples are characterized by relatively uniform trace-element compositions. The granite samples have total rare earth element (ΣREE) contents of 13.29–334.05 ppm, and all granite samples show light REE (LREE) enrichment and heavy REE (HREE) depletion in the chondrite-normalized REE diagram (Figure 6a; Table S3). The granites show (La/Yb)N values greater than 7.91 (except for samples XQZK11–1 and WGS06027), and have strongly negative Eu anomalies (Eu/Eu* = 0.51–1.00) (except for samples WGS06027). In the N-MORB-normalized spider diagram (Figure 6b), the Wugongshan granites exhibit positive K, U, and Pb anomalies and negative Ba, Nb, Ce, Sr, P, and Ti anomalies.

5. Discussion

5.1. Ages

The age results of the representative Wugongshan granites show that the zircon U–Pb age is 438.9 ± 1.2 Ma~441.2 ± 1.6 Ma, indicating that the Wugongshan granite was formed in the Early Silurian Period. The previous research results show that the Early Paleozoic granite age in the Wugongshan area is roughly concentrated in three periods: 455 Ma, 440 Ma, and 425 Ma and the granites under investigation represent the age range of the second periods (438~442 Ma), respectively.
Early Paleozoic igneous rocks were widespread in the SCC, with most having formed during the Caledonian stage (460–410 Ma) [14,17,19,24]. The classification of the Wugongshan granites in northwestern Jiangxi is still under discussion. The Wugongshan granites have peraluminous characteristics, as indicated by their A/NK ratios (1.22–2.15), and A/CNK ratios (0.68–1.31). In the A/NK-A/CNK diagram, all points are placed on the I–S granite boundary area (Figure 5c).
In summary, Wugongshan granites are S-type rather than I-type, as indicated by an A/CNK > 1.1 and widespread Al-rich minerals (e.g., muscovite), together with alkaline minerals (e.g., iron-rich biotite), which indicate that the Wugongshan granites belong to muscovite-bearing peraluminous granites (MPG) [62,63,64,65,66,67,68,69].

5.2. Nature of Sources

The Wugongshan granite’s characteristics indicate that the magma is mainly formed by the partial melting of upper crust material, and there are no obvious mantle-source materials in the magma formation process. The δEu of Wugongshan granites is 0.51~1.00 (except WGS06027), indicating that plagioclase separation and crystallization occurred during the magmatic evolution, which mainly comes from the partial remelting of upper crustal materials [62,65,66]. The moderate negative δEu anomaly, a relatively flat distribution pattern of heavy rare earth elements (HREE), and negative Ba and Sr anomalies, may indicate that residual minerals in the source contain a certain amount of feldspar [62]. The zircons from different sources often have different Hf isotopic characteristics, so the magma source characteristics can be traced with the Hf isotopes [49,70,71,72]. The single-stage mode age (tDM) of Wugongshan granite zircon Hf was 1305~1540 Ma, and the two-stage mode age (tDM2) was 1809~2148 Ma. The (Lu/Hf)f of Wugongshan granite is −0.98~−0.91, which is significantly lower than that of the continental crust (−0.72, Vervoort et al., 1996). All the zircon εHf(t) is negative (−11.56~−6.19), except for some points near the 1.8Ga trend evolution line. Other points are projected between the 1.8 Ga and 2.5 Ga trend evolution lines, indicating that the Wugongshan granites were derived from the partial melting of ancient crust and significant crustal reworking (Figure 7).
The Wugongshan granites have relatively low Rb/Sr and Rb/Ba ratios, implying an affinity with pelite-derived and psammite-derived melt, and all samples plot in the clay-poor field in the Rb/Ba-Rb/Sr diagram (Figure 8a; [73]). In the CaO/Na2O–Al2O3/TiO2 diagram (Figure 8b), the Wugongshan granites display varied CaO/Na2O ratios, and the spots plot in the pelite-derived field, indicating the magma was derived from partial melting of the pelite rocks from the Paleoproterozoic continental crust [73].
Recent studies have shown that the content and ratio of Sr and Y elements in granites are closely related to the residual facies in the magmatic source [74]. During the partial melting of magmatic rocks, Nb and Ta often remain in hornblende, while Ti remains in rutile [75]. The obvious loss of Sr, Ba, and Ti from the Wugongshan granite suggests that plagioclase and Ti-containing minerals (such as biotite) have undergone obvious separation and magma crystallization. When the content of garnet in the residual phase of the magma source reaches 10%, the magma has the characteristics of high Sr and low Y [76]. If the residual facies in the magma source are dominated by hornblende, Y/Yb is close to 10. If the residual facies in the magma source are dominated by garnet, the ratio is significantly greater than 10 [77]. The composition of the Wugongshan granites showed that the Y/Yb ratio was 7.15~12.65 and close to 10, and the rock mass did not have the characteristics of adakite (high Sr and low Y), indicating that the magma source was dominated by hornblende residues. The Wugongshan granites have δEu anomalies (0.51~1.00, except WGS06027), indicating that there are plagioclase residues in the magmatic source [65].
Based on the above discussion of the analysis, we infer that the residual facies of the Wugongshan granites in the magma source are amphibolite facies, and the residual mineral assemblage is hornblende + plagioclase.

5.3. Tectonic Implications

The tectonic setting of South China in the Early Paleozoic orogeny has been controversial. Some scholars have ascribed the Paleozoic orogeny to an oceanic subduction and collision setting, with the ocean basin situated between the Yangtze and Cathaysia blocks [25,26,78,79]. Others proposed that it was an intracontinental orogeny with no ocean basin separation between the two blocks [13,14,17,24,78,79]. As an important part of the continental crust, granites can be formed in different tectonic settings, such as active continental margins, continental crust-thickening stages of collision, and post-orogenic extensional tectonic settings [57,80,81]. There are no records of oceanic crust remnants or fragments along the boundary between the Yangtze and Cathaysia blocks in the Early Paleozoic period, and no ophiolite or arc-related magmatic rock development during that time [8,9,12,13,15,19]. The widely developed S-type granites and the absence of high-pressure, low-temperature metamorphism in the Caledonian orogenic belt in the SCC is inconsistent with an oceanic subduction setting [13,17,78]. Therefore, it does not belong to the Andean-type orogeny formed by the subduction of the oceanic plate under the continental plate in the Caledonian orogenic belt in the SCC.
The Early Paleozoic magmatic rocks are widely distributed in the Yangtze and Cathaysia blocks and their ages were construed to be ca. 460–410 Ma, without developing along the subduction zone [13,17,78]. The palaeogeographic studies of South China show that there is a lack of active continental margin sedimentation, or similar sedimentary environment facies, along the boundary between the Yangtze and Cathaysia blocks [13,17,78]. The paleontological strata and paleoecological evolution between the Yangtze block and the Cathaysia block are related and continuous and belong to the unified continental basin’s paleogeographical environment in the Early Paleozoic [13,17,78]. The Early Paleozoic–Caledonian orogeny in South China is an intracontinental orogenic event that developed from the Middle Ordovician (>460 Ma) to the Early Devonian (about 415 Ma), while the Wugongshan granite was formed in the intracontinental setting rather than the continental collision setting [14,23].
In the Hf–(Rb/10)–(3Ta) discrimination diagram (Figure 9a; [82]), the Wugongshan samples plot in the collisional granites field (COLG), while in the Hf–(Rb/30)–(3Ta) diagram (Figure 9b) the samples plot in the overlapping field of post-collisional granites (P-COLG) and syn–collisional granites (S-COLG). In the Rb–(Yb+Ta) diagram, Rb–(Y+Nb) diagram, Nb–Y diagram, and Ta–Yb diagram, all the samples plot in the overlapping field of S-COLG and volcanic arc granites (VAG) (Figure 10; [83]). Given the intracontinental orogenic characteristic, S-type granite, and relatively uniform negative Lu-Hf isotopic compositions, Wugongshan granites were formed in the process of the collision or post-collision extensional tectonic setting [23,24,80,82]. These studies of granulites from Yiyang, Yunkai, and Taoxi indicate that the rocks have a clockwise P-T-t path, and the zircon indicates that the time of subduction and exhumation was ca. 440 Ma [78]. The Early Paleozoic granites and the granulites in Wugongshan have the same U–Pb age, which indicates that the Wugongshan pluton developed in the post-collision extensional tectonic background [24,80].
With the continental collision of the Yangtze block and Cathaysia block, the Paleo- Tethys Ocean closed along the Jiangshan-Shaoxing fault zone during the Neoproterozoic (ca. 850–820 Ma) (Figure 1b) [14,28]. The later bimodal magmatism, diabasic dykes, and the depression basin, probably represent the Neoproterozoic rifting (ca. 840–760 Ma) (Figure 11a) [14,28]. From the Ediacaran to the Early Paleozoic (760–460 Ma), the SCC sediments were deposited in a stable neritic-slope environment, which was not obviously affected by the Pan-African movement (Figure 11b) [13,17,28,78]. From the late Ordovician (ca. 460 Ma), the intracontinental granitic magmatism widespread in the SCC was the tectonic response to the closure of the Proto-Tethys Ocean (Figure 11) [14,24,78]. Finally, magma intrusion occurred during the post-orogenic stage, which is consistent with the occurrence of the Wugongshan granitic intrusions (Figure 11). Here, we invoke a model similar to that proposed by [28] and [14] to account for the tectonic evolution of the SCC (Figure 11).
Considering that the Indochina block in Vietnam’s subduction north to south China occurred along with the subduction of the Proto-Tethys Ocean during the Paleozoic [16,17], given the combined effects of oceanic–continental subduction the intracontinental subduction of the Yangtze block and Cathaysia block resulted in the superposition of two continental crust slabs and the thickening of the continental crust (Figure 11c). Thereafter, the Wugongshan granites intruded under the intracontinental tectonic plates in response to the distant stresses of the convergence of the Proto-Tethys Ocean.

6. Conclusions

(1)
The U–Pb ages of the granites indicated that the Wugongshan granites were emplaced in 442–438 Ma.
(2)
Their strongly peraluminous nature, combined with the presence of muscovite, indicates that Wugongshan granites are S–type granites. The Hf isotopic compositions and the geochemical characteristics of the Wugongshan granites indicate that the magmas were derived from partial melting of the upper crust of the SCC.
(3)
The Caledonian granites in the Wugongshan area are being generated in an intracontinental orogenic setting, which is a far–field effects response to the convergence of the Paleo-Tethys Ocean.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min13111427/s1, Supplementary Table S1. LA–ICP–MS U–Pb zircon ages of Wugongshan granite samples CJK06–2, WGS06022, and WGS06022; Supplementary Table S2. Whole-rock major–oxide (wt.%) compositions of the Wugongshan granites; Supplementary Table S3. Whole-rock trace–element (ppm) compositions of the Wugongshan granites; Supplementary Table S4. Zircon Hf isotopic compositions of the Wugongshan granites.

Author Contributions

Conceptualization, G.Y., Y.Z. (Yaoyao Zhang) and H.H.; methodology, G.Y.; software, H.H.; validation, K.L. and Y.Z. (Yi Zhou); formal analysis, G.Y.; investigation, G.Y., Y.Z. (Yi Zhou) and H.H.; resources, G.Y. and S.W.; data curation, H.H. and G.Y.; writing—original draft preparation, G.Y.; writing—review and editing, Y.Z. (Yi Zhou) and G.Y.; visualization, G.Y.; supervision, G.Y. and Y.Z. (Yi Zhou); project administration, Y.Z. (Yi Zhou); funding acquisition, G.Y. and H.H. All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by the fundamental research funds of CGS Research (JKYQN202307), the National Natural Science Foundation of China (grant Nos. U2244205), the Joint Innovation Fund of China National Uranium Co., Ltd. and State Key Laboratory of Nuclear Resources and Environment (No. NRE2021–01), and the China Geological Survey Bureau (DD20221677–2).

Data Availability Statement

Not applicable.

Acknowledgments

The authors thank Qiuye Yu of the Changchun Institute of Technology and Lele Han of China University of Geosciences (Beijing) for the computer mapping work.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 2. Simplified structural map of the Wugongshan area (modified from [3,32]).
Figure 2. Simplified structural map of the Wugongshan area (modified from [3,32]).
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Figure 3. Field photographs and photomicrographs (crossed polar) of granites in the Wugongshan area: (a,b) biotite monzonitic granite; (c,d) two-mica monzonite granite; (e,f) porphyritic two-mica monzonite granite. Abbreviations: Q—quartz; Bt—biotite; Pl—plagioclase; Kfs—K-feldspar.
Figure 3. Field photographs and photomicrographs (crossed polar) of granites in the Wugongshan area: (a,b) biotite monzonitic granite; (c,d) two-mica monzonite granite; (e,f) porphyritic two-mica monzonite granite. Abbreviations: Q—quartz; Bt—biotite; Pl—plagioclase; Kfs—K-feldspar.
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Figure 4. U–Pb concordia diagram for Wugongshan granites: (a) CJZK06–2, (b) WGS06022, and (c) WGS06028.
Figure 4. U–Pb concordia diagram for Wugongshan granites: (a) CJZK06–2, (b) WGS06022, and (c) WGS06028.
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Figure 5. (a) Total-alkali-silica (TAS) diagram; (b) K2O–SiO2 diagram (after [55,56]); (c) the A/NK–A/CNK diagram (from [57]); and (d) AFM diagram (from [58,59]) for the Wugongshan granites. The triangle denotes published data for the Wugongshan granites ([24]; and reference data; the same below).
Figure 5. (a) Total-alkali-silica (TAS) diagram; (b) K2O–SiO2 diagram (after [55,56]); (c) the A/NK–A/CNK diagram (from [57]); and (d) AFM diagram (from [58,59]) for the Wugongshan granites. The triangle denotes published data for the Wugongshan granites ([24]; and reference data; the same below).
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Figure 6. (a) Chondrite-normalized REE and (b) N-MORB-normalized spider patterns of the Wugongshan granites (normalizing factors are from [60,61]; N-MORB compositions are from [60]). The black lines indicate published data for the Wugongshan granites ([24]; and reference data).
Figure 6. (a) Chondrite-normalized REE and (b) N-MORB-normalized spider patterns of the Wugongshan granites (normalizing factors are from [60,61]; N-MORB compositions are from [60]). The black lines indicate published data for the Wugongshan granites ([24]; and reference data).
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Figure 7. The data of zircon εHf(t) vs. 206Pb/238U ages for Wugongshan granites (a,b), indicating that the magma was formed by the reworking of the upper-middle crust. The corresponding lines are from [49].
Figure 7. The data of zircon εHf(t) vs. 206Pb/238U ages for Wugongshan granites (a,b), indicating that the magma was formed by the reworking of the upper-middle crust. The corresponding lines are from [49].
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Figure 8. Rb/Ba–Rb/Sr (after [73]) (a) and CaO/Na2O–Al2O3/TiO2 (b) (from [73]) diagrams for the Wugongshan granites.
Figure 8. Rb/Ba–Rb/Sr (after [73]) (a) and CaO/Na2O–Al2O3/TiO2 (b) (from [73]) diagrams for the Wugongshan granites.
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Figure 9. Tectonic discrimination diagrams for Wugongshan granites. (a) Rb/10–Hf–(3Ta); (b) Rb/30–Hf–(3Ta) (after [82]). COLG—collisional granite; VAG—volcanic arc granite; WPG—within–plate granite; S-COLG—syn–collisional granite; ORG—oceanic ridge granite; P-COLG—post–collisional granite.
Figure 9. Tectonic discrimination diagrams for Wugongshan granites. (a) Rb/10–Hf–(3Ta); (b) Rb/30–Hf–(3Ta) (after [82]). COLG—collisional granite; VAG—volcanic arc granite; WPG—within–plate granite; S-COLG—syn–collisional granite; ORG—oceanic ridge granite; P-COLG—post–collisional granite.
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Figure 10. Tectonic discrimination diagrams for Wugongshan granites: (a) Rb–(Yb+Ta) diagrams; (b) Rb–(Y+Nb) diagrams; (c) Nb–Y diagrams; (d) Ta–Yb diagrams (from [83]).
Figure 10. Tectonic discrimination diagrams for Wugongshan granites: (a) Rb–(Yb+Ta) diagrams; (b) Rb–(Y+Nb) diagrams; (c) Nb–Y diagrams; (d) Ta–Yb diagrams (from [83]).
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Figure 11. The dynamic model of the Neoproterozoic to the Paleozoic tectonic evolution of South China (non-scale for crust and lithosphere) (modified from [14,28,62].
Figure 11. The dynamic model of the Neoproterozoic to the Paleozoic tectonic evolution of South China (non-scale for crust and lithosphere) (modified from [14,28,62].
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Yang, G.; Zhang, Y.; Liu, K.; Zhou, Y.; Wang, S.; Huo, H. Geochemistry and Zircon U–Pb Geochronology of the Wugongshan Granites in the Northwestern Jiangxi Area, China: Implications for the Paleozoic Tectonic Development of South China. Minerals 2023, 13, 1427. https://doi.org/10.3390/min13111427

AMA Style

Yang G, Zhang Y, Liu K, Zhou Y, Wang S, Huo H. Geochemistry and Zircon U–Pb Geochronology of the Wugongshan Granites in the Northwestern Jiangxi Area, China: Implications for the Paleozoic Tectonic Development of South China. Minerals. 2023; 13(11):1427. https://doi.org/10.3390/min13111427

Chicago/Turabian Style

Yang, Guangqin, Yaoyao Zhang, Kai Liu, Yi Zhou, Shuxun Wang, and Hailong Huo. 2023. "Geochemistry and Zircon U–Pb Geochronology of the Wugongshan Granites in the Northwestern Jiangxi Area, China: Implications for the Paleozoic Tectonic Development of South China" Minerals 13, no. 11: 1427. https://doi.org/10.3390/min13111427

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