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Article

Genesis of the Mengshan Granitoid Complex in an Early Mesozoic Intracontinental Subduction Tectonic Setting in South China: Evidence from Zircon U-Pb-Hf Isotopes and Geochemical Composition

by
Jin Wei
1,2,3,†,
Yongpeng Ouyang
2,3,4,5,†,
Jing Zou
2,3,
Runling Zeng
2,3,
Xinming Zhang
4,
Tao Zhang
4,
Shenao Sui
4,
Da Zhang
4,
Xiaolong He
1,* and
Yaoyao Zhang
6,*
1
School of Environment and Resources, Xiangtan University, Xiangtan 411105, China
2
The Tenth Geological Brigade of Jiangxi Geological Bureau, Yingtan 335001, China
3
Yingtan Key Laboratory of Exploration and Research of Scarce and Advantage Minerals, Yingtan 335001, China
4
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China
5
Jiangxi Province Key Laboratory of Exploration and Development of Critical Mineral Resources, Nanchang 330009, China
6
Chinese Academy of Geological Sciences, Beijing 100037, China
*
Authors to whom correspondence should be addressed.
†
These authors contributed equally to this work and should be considered co-first authors.
Minerals 2024, 14(9), 854; https://doi.org/10.3390/min14090854
Submission received: 6 July 2024 / Revised: 12 August 2024 / Accepted: 22 August 2024 / Published: 23 August 2024
(This article belongs to the Special Issue Rare Metal and Related Deposits: Geology, Geochemistry and Mineralization)
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Versions Notes

Abstract

:
The Mengshan granitoid complex is located in the central part of Jiangnan Orogen and belongs to the western part of Jiangxi Province, where several phases of granitic magmatism record the crustal evolution of the late-Indosinian. However, its petrogenesis remains uncertain, largely due to controversies over its origin, evolutionary process and tectonic setting during intrusion. In this study, the lithological features and contact relationships observed in the systematic field geological investigations indicate that the late magmatic phases of the Mengshan granitoid complex are mainly composed of medium–fine-grained biotite monzogranite and fine-grained monzogranite, both of which developed primary fine-grained muscovite. Petrological, petrographic, geochemical and zircon U-Pb-Hf isotopic studies were further carried out on these rocks. Zircon U-Pb isotopic analyses suggest that the medium–fine-grained biotite monzogranite mainly formed at 220.7 ± 1.0 Ma to 218.0 ± 0.8 Ma, and that the fine-grained monzogranite formed at 211.5 ± 2.9 Ma to 212.9 ± 1.0 Ma. Whole-rock geochemical analysis results suggest that these rocks are rich in Cs, Rb, and U, and deficient in Ba, Sr, and Ti, and that they have properties characteristic of rocks with high silica, low P content and high K calc-alkali. Mineralogical and geochemical analysis results suggest that they are S-type granites. The εHf(t) values of the early-stage medium–fine-grained biotite monzogranite and late-stage fine-grained monzogranite range from –4.7 to 0.3 and from –3.2 to 0.7, respectively. Geochemical and isotopic data suggest that these granitoids were derived from the partial melting of Proterozoic continent basement rocks, and that minor mantle materials were involved during their generation. The presence of the early Mesozoic Mengshan granitoid complex reflects a reduplicated far-field converge effect of the collision of the North China and South China blocks and the subduction of the Palaeo-Pacific plate into the South China block. The thickening of the Earth’s crust facilitated crustal delamination, underplating of mantle-derived magma, and crustal heating, triggering intense partial melting of the lithosphere and magma enrichment.

1. Introduction

Granite is widely distributed in continental areas and is mainly produced via the partial melting of the earth’s crust [1,2,3,4]. This process can be induced via the anatectic melting of crustal protolith, heat from the convective asthenospheric mantle, thickened crust delamination, and resultant lithospheric mantle upwelling [5,6,7,8]. Investigating the details of the petrogenesis of granites is of great significance to understanding the crustal evolution process and its connection with the related contemporaneous polymetallic mineralization [9,10,11,12,13,14,15]. The various geochemical signatures reflect the derivation of granite from different sources and differing degrees of melting and differentiation, and have shaped the evolution of orogeny [16,17,18,19]. According to the current plate tectonic paradigm, orogenesis occurs either during accretion at a subducting continental margin or due to continent–continent collision [20,21,22,23]. However, the process of collision orogenesis includes several unresolved questions, such as the duration, magmatism architecture, and relationship with non-metal and polymetallic mineralization.
The Mengshan granitoid complex is located in the western part of Jiangxi Province. This area is situated near the intersection of the Yangtze and Cathaysia blocks in the interior of the South China Plate and has undergone complex tectonic evolution since the Neoproterozoic [24,25]. This area is also the middle section of the Jiangnan Orogenic Belt and the Pingxiang–Leping Depression Belt, adjacent to the Jiuling Thrust Fault Belt in the north and the Wugongshan Granite Dome in the south [26,27,28,29]. It is a large-scale thrust structure that was developed on the Yangtze Block’s edge in the Late Paleozoic’s Middle Triassic (Figure 1). The recently discovered Shizhushan wollastonite deposit in the Mengshan district contains about 54 Mt, making it the world’s largest [30]. Several W-Au-Ag-Pb deposits are also located around the Mengshan granitoid complex. The results of many previous isotopic dating studies indicate that the Mengshan granitoid complex was formed mainly at ca. 230–220 Ma [28,31,32]. Some researchers further propose that some of the surrounding mineralization has also resulted from a combination of magmatism over a long period and multiple phases of evolution [26]. However, the petrogenesis of the Mengshan granitoid complex remains unclear, with much of the debate centered on the time of its formation, the period of magmatic intrusion, and whether it is an S-type or I-type granite [28,31,32]. In addition, field investigations have shown that some granites have intruded into the aforementioned granitoids formed at ca. 230–220 Ma. However, relevant geochronological and geochemical work has not yet been carried out on them, limiting the petrogenesis studies of the Mengshan granitoid complex. Their petrogenesis and relationship with mineralization also remain uncertain, largely due to controversy over their origin, evolutionary process and tectonic setting during intrusion.
In this study, we aim to investigate the mechanisms controlling the formation of the Mengshan granitoid complex through a careful study of the mineralogy, whole-rock geochemistry, zircon U-Pb geochronology, and zircon Lu-Hf isotopes of the late magmatic phases of the Mengshan granitoid complex. Our results and previous data provide essential insights into South China’s petrogenesis and tectonic setting during the early Mesozoic that may aid in developing conceptual models and exploration strategies.

2. Geological Setting

The Mengshan granitoid complex is in the western part of Jiangxi Province. Regarding geotectonic position, the Mengshan granitoid complex is located in the interior of the South China Plate, at the junction of the Cathaysia Block and the Yangtze Block. This area is also the middle section of the Jiangnan Orogenic Belt and the Pingle Depression, adjacent to the Jiuling Thrust Fault Belt in the north and the Wugongshan Granite Dome in the south [26,27,28,29]. The Pingle Depression is bounded by the Pingxiang–Guangfeng–Yifeng–Jingdezhen Fault. It is a large-scale thrust structure that was developed on the Yangtze Block’s edge in the Late Paleozoic’s Middle Triassic [30]. In general, the distribution of the Mengshan granitoid complex and related rare metal deposits in the Pingle Depression is controlled by the northeast-trending structure.
The mineralization conditions in the Mengshan area are favorable, and the mineralization potential is considerable. The abundance values of mineralization elements such as tungsten, copper, lead, zinc, and molybdenum in the strata are higher than those in the crust of eastern China [31,34,35]. The area where the Mengshan granitoid complex is located exposes strata from the late Paleozoic to the Cenozoic, mainly including Carboniferous, Permian, Triassic, Jurassic, Cretaceous, and Quaternary (Figure 2). The Carboniferous strata are mainly siltstone, silty mudstone, dolomite, and limestone. The Permian strata include carbonate rocks such as limestone and dolomite, and siliceous rock. The Triassic strata are mainly sedimentary rocks such as conglomerate, sandstone, mudstone, and siltstone. The Cretaceous strata include mudstone, gravel-bearing siltstone, and conglomerate. The Quaternary strata are distributed in modern river depressions and comprise sand, gravel, and sub-clay layers.
The Mengshan granitoid complex is elliptical and has an exposed area of 39 square kilometers. Surrounding the complex is a metamorphic halo formed via obvious hydrothermal replacement and thermal metamorphism, in which skarn-type deposits are distributed [26,31,36]. Previous studies have postulated that two phases of magmatic intrusion formed it, the first phase being Triassic granite (~217 to ~236 Ma) and the second phase being Jurassic–Cretaceous dykes (~135 Ma to ~142 Ma) [27]. The first phase of magmatic intrusion can be divided into three stages. The first stage is white medium–coarse-grained porphyritic biotite granite, with an age of 236–223 Ma [27,32]; the second stage is flesh-red biotite granite, with an age of 222–220 Ma [31,32,37]; the third stage is gray-white fine-grained granite, with an age of 218–217 Ma [31,32]. In the present study, systematic field geological investigations and the observed cross-cutting relationships have shown that the first phase of magmatism of the Mengshan granitoid complex can be divided into three stages, the first stage being medium–coarse-grained biotite granite, the second stage being medium–fine-grained biotite monzogranite, and the third stage being fine-grained monzogranite (Figure 3). Medium–coarse-grained biotite granite was observed to have been introduced via an intrusion of the second and third stages of granitoids (Figure 2), for example, by medium–fine-grained biotite monzogranite (Figure 3a). In addition, the contact zone between the Mengshan granitoid complex and the Permian carbonate sequences is generally strongly transformed into skarn, and is where the largest wollastonite deposit (Shizhushan deposit) in Asia has been discovered [30].
Affected by the thrust-nappe structure of the South China Orogenic Belt in the Early Paleozoic and the thrust-slip structure since the Indosinian period, the structural deformation in the area mainly includes NE-trending, near-EW-trending, NE–NEE-trending, NNE-trending, and thrust-nappe (-slip) structures [38,39,40,41,42,43]. The NE-trending structure mainly manifests as a series of tight linear folds and derived faults. The near-EW structure is manifested as strong folds and normal faults in the south and strong folds and thrust faults in the north. The thrust-nappe structure is an external system overthrown on the local strata to form the klippe structure. Folds dominate the NE–NEE-trending structure. The north–northeast-trending structure is dominated by faults, mainly distributed in the western and central parts of the area.

3. Sample Collection and Analytical Methods

3.1. Sample Characteristics

The first stage of the medium–coarse-grained biotite granite is grayish in color, with a granite texture and massive structure (Figure 3a,b). It has the widest distribution in the district, and is generally observed to have been introduced via an intrusion of the later two stages of granitoids (Figure 3a). It is also the most studied granitoid in the region [30,31,32], so this phase was not investigated in this study. Representative samples of the medium–fine-grained biotite monzogranite and fine-grained monzogranite were selected for analysis. The sampling locations are shown in Figure 2.
Medium–fine-grained biotite monzogranite is grayish white, with a granite texture and massive structure (Figure 3a,c). The rock comprises plagioclase, potassium feldspar, quartz, biotite, and muscovite, with a 7–10 mm mineral size (Figure 3d–g). The plagioclase is hypidiomorphic and plate-shaped, undergoing sericitization, carbonation, and chloritization, makes up about 30% of the rock (Figure 3d). The potassium feldspar is hypidiomorphic and plate-shaped, with sericitization and carbonation, and makes up about 30% of the rock (Figure 3d–g). The quartz is xenomorphic granular, making up about 20% of the rock (Figure 3d–g). The biotite is flaky and has mostly transformed into chlorite (Figure 3e,g), making up 10%–15% of the rock. The muscovite is poikilitic in the feldspar, with obvious pleochroism, and makes up <5% of the rock (Figure 3e–g).
The fine-grained monzogranite has a light grayish-white granite texture and massive structure (Figure 3h). The rock comprises plagioclase, potassium feldspar, quartz, and muscovite, with a 3–5 mm mineral size (Figure 3i–l). The plagioclase is hypidiomorphic and plate-shaped, with sericitization and carbonate, and makes up 30–35% of the rock (Figure 3i–l). The potassium feldspar is also hypidiomorphic and plate-shaped, with sericitization; it makes up about 30%–35% of the rock (Figure 3i–l). The quartz is xenomorphic and granular, making up 25%–30% of the rock (Figure 3i–l). The muscovite is poikilitic in the feldspar, has obvious pleochroism, and makes up 1%–3% of the rock (Figure 3i–k).

3.2. Analytical Methods

The laboratory of Hebei Provincial Regional Survey Institute was used to conduct the geochemical analysis. The rocks were crushed into centimeter-sized blocks, and fresh samples without alterations or interspersed veins were selected, rinsed with purified water, dried, and crushed into a 200 mesh for testing. For the significant element test, the powder sample was weighed and mixed with Li2B4O7 (1:8) flux and heated to 1150 °C using a melting machine to melt it into a uniform glass sheet in a gold–platinum crucible. Then, it was tested using an Axios max X-ray fluorescence spectrometer. The 200-mesh powder sample was weighed and placed in a polytetrafluoroethylene dissolving tank for the trace element test, and HF+HNO3 was added. The high-pressure digestion tank was kept at 190 °C in a drying oven for 72 h, and then taken out; acid was driven out, and the solution was fixed to a dilute solution for testing. The test was completed using an ICAPQ inductively coupled plasma mass spectrometer. The measured data showed an error of less than 5% according to the monitoring standard GSR-2, and the analysis error of some volatile and extremely-low-content elements was less than 10%. The experimental temperature was 20 °C–25 °C, and the relative humidity was 10%–30%.
Zircon target preparation and cathodoluminescence (CL) were completed in the Hebei Provincial Institute of Regional Survey laboratory, and Beijing Zhongke Mining Research Testing Technology Co., Ltd. (Beijing, China) completed age testing. The age test analysis instruments used were the laser ablation multi-receiver inductively coupled plasma mass spectrometer (LA-ICP-MS; Agilent 7500, Agilent, Tokyo, Japan). The zircon dating method used was LA-ICP-MS, with a beam spot diameter of 30 μm, a laser energy density of 13–14 J·cm−2, and a frequency of 8–10 Hz. Plešovice (age of 337 ± 0.37 Ma) was used as an external standard for matrix correction, and the common lead correction method was performed using the ComPbCorr#3.17 correction program. The data were processed using the ICP-Ms DataCal 10.2 software, and the concordance diagram and other figures were drawn with a confidence level of 95%. Detailed instrument operating conditions and data processing methods are shown in [44,45].
The zircon Hf isotope test was conducted at Beijing Zhongke Mining Research Testing Technology Co., Ltd. The analytical instrument was a New Wave-213 nm ArF-excimer laser-ablation system linked to a Neptune multiple- collector inductively coupled plasma mass spectrometer (NEPTUNE plus, Thermo Fisher Scientific, Waltham, MA, USA). The ablation protocol employed a spot diameter of 55 μm at a 10 Hz repetition rate and a fluence of 7–8 J/cm2 for zircon, and He was used as the carrier gas for the ablation material. Zircon standard 91,500 (176Hf/177Hf = 0.282308 ± 12 (2σ)) was used as an external standard for matrix correction [45]. In calculating the mantle model age of Hf, the present value of 176Hf/177Hf of the depleted mantle was 0.28325, and that of 176Lu/177Hf was 0.0384 [46]. When calculating the crustal model age, the average crustal value of 176Lu/177Hf = 0.015 was used [47].

4. Results

4.1. Geochemistry

The make-up of SiO2 in the medium–fine-grained biotite monzogranite amounts to 72.51%–75.68%, suggesting it is an acidic rock. The make-up of Al2O3amounts to 14.37%–15.50%, that of K2O amounts to 4.45%–5.19%, that of Na2O amounts to 0.91%–2.96%, and the total alkali contents (K2O+Na2O) make up 5.36%–8.15% of the monzogranite. The amount of TiO2 is 0.16%–0.39%, that of TFe2O3 is 0.91%–1.82%, that of MnO is 0.01%–0.05%, that of CaO is 0.19%–0.32%, that of MgO content is 0.49%–0.87%, and that of P2O5 is 0.04–0.07% (Table S1). After deducting the volatile matter and the loss on ignition, the samples were recalculated to 100%. The TAS diagram (Figure 4a) plots the samples in the granite range with sub-alkaline characteristics. The samples are plotted in the monzogranite area in the QAP diagram (Figure 4b). In the K2O–SiO2 diagram (Figure 4c), the samples are mainly plotted in the high-potassium calc-alkaline area, and some are plotted near the high-potassium calc-alkaline area and the boundary of potassium shoshonite, with characteristics of high potassium content. The rock differentiation index (DI) values are 87.07–89.77, indicating a high degree of differentiation. The aluminum saturation index A/CNK ratios are 1.38–2.19, indicating it belongs to the category of peraluminous rock (Figure 4d).
The amounts of SiO2 in fine-grained monzogranite are 74.96%–83.73%, suggesting it is an acidic rock. The Al2O3 amounts have a variation range of 9.52%–13.25%. The K2O amounts are 3.00%–5.13%, and the Na2O amounts are 0.32%–2.82%, with an extensive variation range. The total alkali content (K2O+Na2O) amounts to 3.32%–7.98%, the TiO2 content amounts to 0.10%–0.20%, the TFe2O3 content amounts to 1.17%–1.49%, the MnO content amounts to 0.01%–0.03%, the CaO content amounts to 0.19%–0.78%, the MgO content amounts to 0.43%–0.47%, and the P2O5 content amounts to 0.05–0.07% (Table S1). After deducting volatiles and loss on ignition, the samples were plotted and recalculated to 100%. The TAS diagram (Figure 4a) plots the samples in the granite range. Some points near the boundary between granite and quartzite show sub-alkaline characteristics. The samples are plotted in the monzogranite area in the QAP diagram (Figure 4b). The K2O–SiO2 diagram (Figure 4c) shows that the samples are plotted in the high-potassium calc-alkaline area and near the boundary of potassium shosphorite, showing characteristics of high potassium content. The differentiation index (DI) values are 90.14–90.91, indicating a high degree of differentiation. The aluminum saturation index A/CNK ratios are 1.15–2.38, also indicating that it belongs to the category of peraluminous rock (Figure 4d).
The rare earth content of the medium–fine-grained biotite monzogranite samples is low, with ΣREE ranging from 97.72 × 10−6 to 290.89 × 10−6, the light rare earth LREE content ranges from 84.86 × 10−6 to 271.98 × 10−6, and the heavy rare earth HREE content ranges from 12.86 × 10−6 to 25.02 × 10−6 (Table S1). The light/heavy rare earth ratio is 3.19–14.38, (La/Yb)N is 2.15–19.69, and the degree of differentiation between light and heavy rare earth is low; the value of δEu is 0.17–0.36, with a strong negative anomaly, and that of δCe is 0.74–3.36, with a weak anomaly. The rare earth distribution curve is seagull-shaped, with a relative abundance of light rare earths and relative scarcity of heavy rare earths (Figure 5a). The rare earth content in fine-grained monzogranite samples is low, with ΣREE ranging from 24.04 × 10−6 to 309.70 × 10−6, the light rare earth LREE content ranges from 10.03 × 10−6 to 264.61 × 10−6, and the heavy rare earth HREE content ranges from 14.01 × 10−6 to 45.09 × 10−6 (Table S1). The light/heavy rare earth ratio is 0.72–5.87, that of (La/Yb)N is 0.37–6.96, and the degree of differentiation between light and heavy rare earth is low; the value of δEu is 0.13–0.22, with a strong negative anomaly, and the value of δCe is 0.67–0.91, with a negative anomaly. The rare earth distribution curve is seagull-shaped, with a relative abundance of light rare earths and a relative scarcity of heavy rare earths (Figure 5a). In the N-MORB-normalized spider diagram (Figure 5b), the Mengshan granites exhibit positive Rb, K, Th, and U anomalies and negative Ba, Sr, P, and Ti anomalies.

4.2. Geochronology

The zircons used in this age test had good idiomorphism, mainly existing a long columnar shape, and were relatively complete overall. Age tests were conducted at zircon locations where cracks and inclusions were not developed. The locations tested were mostly in magmatic zircons with developed oscillation rings [50,51,52] (Figure 6). The ages measured according to the zircons are all less than 1.0 Ga, as suggested by the zircon 206Pb/238U age [53], and the test method is ICP-MS. Zircon test data are shown in Table S2.
The zircon Pb content in the medium–fine-grained biotite monzogranite (23MS-AFT-03) is 50.30 × 10−6–366.17 × 10−6, the Th content is 653.87 × 10−6–3004.36 × 10−6, the U content is 975.78 × 10−6–8013.64 × 10−6, and the Th/U ratio is 0.37–0.76. The zircon age of the sample is from 214.69 ± 1.95 Ma to 225.68 ± 3.20 Ma, with a weighted average age of 220.7 ± 1.0 Ma and a MSWD value of 0.83 (Figure 7a). The zircon Pb content of sample 23MS-AFT-09 is 49.42 × 10−6–429.63 × 10−6, the Th content is 721.51 × 10−6–3100.52 × 10−6, the U content is 914.49 × 10−6–9460.35 × 10−6, and the Th/U ratio is 0.33–0.81. The zircon age of the sample is from 215.21 ± 2.09 Ma to 220.89 ± 2.13 Ma, with a weighted average age of 217.98 ± 0.76 Ma and a MSWD value of 0.76 (Figure 7b).
The zircon Pb content of fine-grained monzogranite (23MS-AFT-05) is 30.92 × 10−6–150.48 × 10−6, the Th content is 379.99 × 10−6–1220.79 × 10−6, the U content is 429.48 × 10−6–3063.13 × 10−6, and the Th/U ratio is 0.25–0.91. The zircon age of the sample is from 205.40 ± 3.13 Ma to 218.41 ± 2.44 Ma, with a weighted average age of 211.5 ±2.9 Ma (MSWD = 4.3, Figure 7c). The zircon Pb content of sample 23MS-AFT-08 is 52.06 × 10−6–222.29 × 10−6, the Th content is 785.98 × 10−6–5085.20 × 10−6, the U content is 1114.67 × 10−6–5293.28 × 10−6, and the Th/U ratio is 0.40–1.70. The zircon age of the sample is from 209.27 ± 3.10 Ma to 218.86 ± 1.98 Ma, with a weighted average age of 212.9 ± 1.0 Ma and a MSWD value 1.6 (Figure 7d). All the granites tested were formed in the Triassic.

4.3. Hf Isotopic Compositions

The 176Lu/177Hf ratios of the medium–fine-grained biotite monzogranite (23MS-AFT-03) are 0.000819–0.001644, and the 176Lu/177Hf ratio is less than 0.002, indicating that the zircon only had a tiny amount of radiogenic Hf accumulation after its formation. Therefore, the initial 176Hf/177Hf ratio can represent the Hf isotope composition at the time of formation [54]. The zircon Hf isotope ratios of 176Yb/177Hf are 0.022454–0.044441, the 176Hf/177Hf ratios are 0.282524–0.282640, the fLu/Hf values are from –0.95 to –0.98, the zircon εHf(t) values are from –4.1 to 0, the zircon Hf single-stage model ages (TDM) are from 866 Ma to 1049 Ma, and the two-stage model ages (TDMC) are from 1682 Ma to 2058 Ma (Table S3; Figure 8).
The 176Lu/177Hf ratios of medium–fine-grained biotite monzogranite (23MS-AFT-09) are 0.000785–0.003383. Except for a few points, the 176Lu/177Hf ratios are less than 0.002, indicating that the zircons only had a small amount of radiogenic Hf accumulation after formation. Therefore, the initial 176Hf/177Hf ratio can represent the Hf isotope composition at the time of formation [54]. The zircon Hf isotope ratios of 176Yb/177Hf are 0.021857–0.095409, the 176Hf/177Hf ratios are 0.282518–0.282649, the fLu/Hf values are from –0.90 to –0.98, the zircon εHf(t) values are from –4.7 to 0.3, the zircon Hf single-stage model ages (TDM) are 850–1110 Ma, and the two-stage model ages (TDMC) are 1653–2103 Ma (Table S3; Figure 8).
The 176Lu/177Hf ratios of the fine-grained monzogranite (23MS-AFT-08) are between 0.000704 and 0.002538. Except for a few points, the 176Lu/177Hf ratios are less than 0.002, indicating that zircons only had a tiny amount of radiogenic Hf accumulation after formation. Therefore, the initial 176Hf/177Hf ratio can represent the Hf isotope composition at the time of formation [54]. The zircon Hf isotope ratios of 176Yb/177Hf are 0.019312–0.069183, the 176Hf/177Hf ratios are 0.282559–0.282662, the fLu/Hf values are from –0.92 to –0.98, the zircon εHf(t) values are from –3.2 to 0.7, the zircon Hf single-stage model ages (TDM) are 835–1023 Ma, and the two-stage model ages (TDMC) are 1619–1970 Ma (Table S3; Figure 8).

5. Discussion

5.1. Chronological Significance

The Mengshan granitoid complex is a multi-stage composite rock mass, and the age of the rock mass was tested to varying degrees. The isotopic age determined using the biotite K-Ar method is 174 Ma, and it is believed that the rock mass was formed in the Jurassic [55]. Since the Mengshan granitoid complex was formed via multiple magmatic intrusions and the biotite K-Ar system has a low closure temperature, it is easily affected by later thermal events, resulting in a K-Ar age younger than the actual formation age of the rock mass. The zircon U-Pb system has the characteristics of a high closure temperature and strong anti-interference ability. The zircon U-Pb age measured using the in situ technology can accurately reflect the formation time of the rock mass. In recent years, a large number of new zircon SHRIMP and LA-ICP-MS U-Pb age data have shown that the formation time of the Indosinian granite in South China is mainly 210–240 Ma [26,27,31,32,56,57]. It can be seen that the time during which Mengshan granite magma activity occurred is consistent with the intrusion time of other Indosinian granites in South China. The Indosinian peraluminous granites mainly include garnet-bearing granites, cordierite-bearing granites, biotite/two-mica granites, and muscovite-granites, which are closely related to mineralization, such as that of tungsten, tin, niobium, and tantalum [58,59,60,61].
According to previous research results, the first phase of the Mengshan granitoid complex is currently divided into three stages, namely 236–223 Ma (white medium–coarse-grained porphyritic biotite granite in the first stage), 222–220 Ma (flesh-red biotite granite in the second stage), and 218–217 Ma (gray-white fine-grained granite in the third stage). Because of the complexity of the magmatic activity of the Mengshan granitoid complex, this work selected representative samples for zircon LA-ICP-MS age testing and obtained four isotopic ages, which are 220.7 ± 1.0 Ma, 217 ± 0.76 Ma, 212.9 ± 1.76 Ma, and 211.5 ± 2.9 Ma (Figure 7). This work also obtained granite from three stages. Based on a combination of the field geological characteristics and the latest age data, the first phase of magmatism in the Mengshan granitoid complex is suggested to be divided into three stages. The first stage is the medium–coarse-grained porphyritic biotite granite with an age of ca. 236–223 Ma; the second stage is the medium–fine-grained biotite monzogranite, with an age of ca. 222–217 Ma; and the third stage is the fine-grained monzogranite, with an age of ca. 212–211 Ma.

5.2. Petrogenesis and Magmatic Source

Granite can be divided into the I type, S type, M type, and A type, according to the differences in source area and tectonic environment. S-type granite is produced via the partial melting and crystallization of crustal sediments [1,62,63]. Mineralogical signs are reliable signs for distinguishing between granite types. For example, magmatic muscovite, cordierite, garnet, corundum, and tourmaline are essential signs of S-type granite [62,64,65,66]. In the medium–fine-grained biotite monzogranite, panidiomorphic lamellar muscovite in sizes of 200–500 μm is generally present in the form of poikilitic with quartz, plagioclase, and potassium feldspar (Figure 3e–g). In the fine-grained monzogranite, there is hypidiomorphic lamellar muscovite (Figure 3i,k) in the form of poikilitic with quartz, plagioclase, and potassium feldspar, or panidiomorphic lamellar muscovite wrapped in plagioclase (Figure 3l), indicating that there is a large amount of primary muscovite of magmatic origin in these acidic rocks in the Mengshan area. In addition, previous researchers have also proposed that the color of primary biotite of magmatic origin is also related to the origin of granite. Biotite in S-type granite is usually rich in Fe2+ and presents a reddish-brown color, while biotite in I-type granite is richer in Fe3+ and Mg and presents a brownish-green color [2,62,63]. The primary biotite in the medium–fine-grained biotite monzogranite and the fine-grained monzogranite is of a significant reddish-brown color (Figure 3c,h). The above mineralogical evidence shows that the granites of the Mengshan granitoid complex have the typical characteristics of S-type granite. The 10,000 Ga/Al ratio of the granite is less than the lower limit of 2.6 for A-type granite [1,67], indicating that it does not have the characteristics of A-type granite. In the K2O+Na2O and w(FeO*)/w(MgO) versus 10,000 Ga/Al diagrams, almost all of the sample spots fall into the I- or S-type granite range (Figure 9a,b). However, the P2O5 content of the rock mass is 0.04%–0.07% (Table S1), which is different from the typical content in I-type granite. The standard mineral calculation (CIPW) of the rock mass contains a large number of standard corundum molecules (1.76–8.37), and the A/CNK is 1.15–2.38, showing its strong peraluminous characteristics, similar to those of S-type granite (Figure 4d). The samples in the ACF diagram (Figure 9c) are projected to the side of S-type granite. Therefore, the geochemical analysis of the granite in this study also shows that the granites of the Mengshan granitoid complex belong to S-type granite.
S-type granite is a type of granite that is produced via the partial melting and crystallization of crustal sediments. S-type granite is closely associated with W, Sn, and light rare earth element (LREE) deposits regarding genesis. W-rich granite’s ideal magma source area is usually rich in significant ion lithophile and ore-forming elements [68,69,70,71]. Biotite and muscovite in crustal rocks are the main minerals that host highly incompatible significant ion lithophile elements such as W, Cs, and U. Partial melting of metamorphic sedimentary rocks will form melts with high U content and low Th/U ratios [5,72]. Therefore, the W-rich initial magma produced via the partial melting of enriched crustal materials will also be rich in U and Cs and show characteristics of high U and a low Th/U ratio. The granites of the Mengshan granitoid complex are rich in Cs, Rb, U, Sn, and Li to varying degrees, and the Th/U ratio is low (Table S2; Figure 5b), indicating that the magma of the Mengshan granitoid complex comes from the partial melting of enriched crustal materials. “Nb/Ta = 5” is considered to be the geochemical distinguishing mark for normal crystallization differentiation and magma–hydrothermal interaction, and “Zr/Hf = 26” is considered to be the geochemical boundary-distinguishing mark for highly differentiated and ultra-differentiated granites [3]. In the diagram of Nb/Ta vs. Zr/Hf that characterizes the origin of granite (Figure 9d), both types of granitoid complexes show a high degree of differentiation and strong melt–fluid interaction close to granite areas associated with mineralization, such as that in W-Sn rare metals, suggesting that the Mengshan granitoid complex has the potential for W-Sn rare metal mineralization; for example, it may be related to W mineralization (Taizibi W deposit; Figure 2) around the granitoid complex.
Minerals 14 00854 g009
Figure 9. (a) K2O+Na2O vs. 10,000 Ga/Al diagram; (b) w(FeO*)/w(MgO) vs. 10,000 Ga/Al diagram; (c) ACF diagram [73]; (d) Nb/Ta vs. Zr/Hf diagram [1,2].
Figure 9. (a) K2O+Na2O vs. 10,000 Ga/Al diagram; (b) w(FeO*)/w(MgO) vs. 10,000 Ga/Al diagram; (c) ACF diagram [73]; (d) Nb/Ta vs. Zr/Hf diagram [1,2].
Minerals 14 00854 g009
In this study, zircon Hf isotope tests were conducted on representative samples, and the fLu/Hf values of the samples were all less than –0.90. The zircon εHf(t) values of the medium–fine-grained biotite monzogranite samples 23MS-AFT-03 and 23MS-AFT-09 were from –4.1 to 0 and –4.7 to 0.3, and the zircon εHf(t) values of fine-grained monzogranite sample 23MS-AFT-08 were from –3.2 to 0.7 (Figure 8). The zircon εHf(t) values of the magmatic rocks of these two periods were mainly negative, and there was also a small number of positive points, indicating that the source of these magmas is mainly ancient crustal materials and that a small amount of mantle materials are mixed in. The two-stage model ages (TDMC) of the zircons from the biotite monzogranite samples 23MS-AFT-03 and 23MS-AFT-09 were 1682–2058 Ma and 1653–2103 Ma, and the two-stage model ages (TDMC) of the zircons from monzogranite sample 23MS-AFT-08 were 1619–1970 Ma. The results show that ancient crustal material in the magma source area was formed in the early Mesoproterozoic period. Combined with the previous research results, it is believed that the Mengshan granite is an S-type granite, and the magma source area is mainly composed of Early Mesoproterozoic crustal materials [27,31,32].

5.3. Tectonic Setting

High-field-strength elements (HFSE), such as Nb, Ta, Th, Zr, Hf, HREE, etc., can effectively indicate the tectonic environment of rocks [74]. In the Rb–Y+Nb diagram of granite (Figure 10a), the samples are plotted in the syn-collision area, close to the boundary with the plate. In the Rb–Yb+Ta diagram (Figure 10b), all the samples are plotted in the syn-collision area. The above structural discrimination diagrams show that the samples are projected in the intra-plate tectonic and syn-collision tectonic environments, indicating that the granite has the geochemical characteristics of intracontinental and syn-collision granite.
The South China Plate is located at the intersection of multiple tectonic domains of the North China Plate, the Indosinian Plate, and the Paleo-Pacific Plate in the Triassic. Tectonic deformation events and magmatic activities are widely distributed in the South China Plate. The collision and convergence of the north and south margins of the South China Plate led to the thickening of the crust in South China, forming a large-scale Early Mesozoic fold-nappe system, a large ductile shear zone, and a series of S-type granites [76,77]. Studies have shown that the initial collision between the South China Plate and the North China Plate occurred in the Early Triassic [78]. The subduction–accretion and collision orogeny of the North China Plate and the South China Plate along the Mianlue suture in the Middle Triassic led to the development of the NW/NWW-trending fold-thrust tectonic belt in the Qinling–Dabie orogenic belt and its foreland [77,79,80]. The related deformation is not limited to the Qinling–Dabie orogenic belt and its foreland but affects the Jiangnan orogenic belt and the interior of the Cathaysia block [81,82,83], resulting in strong intracontinental compression deformation in Jiangxi, and the development of NE-trending fold-nappe structures in the strata before the Early Triassic period. Ref. [84] pointed out through the study of A-type granites in South China that the South China plate completed its final collision and amalgamation with the Indian and North China plates around 230 Ma. Some scholars also believe that 240–220 Ma was the main collision period between the Yangtze block and the North China plate [85,86]. Ref. [56] proposed that the formation time of the Indosinian granite in South China has excellent temporal coupling with the Indosinian movement the Dabie orogenic belt in the north, indicating that the formation of the Indosinian granite in South China is related to the strong subduction/collision orogeny around the South China plate. Ref. [6] proposed the flat-slab subduction model of the Pacific plate to explain the tectonic evolution of South China since the early Mesozoic. From the early Mesozoic period (about 265 Ma), the ancient Pacific plate began to subduct gently under the Eurasian continent along the NW direction, resulting in large-scale magmatic activity in South China. Refs. [87,88] suggested that there is a lack of conclusive evidence of collision between the South China plate and the Indosinian plate in the Triassic period and that the tectonic-magmatic thermal event in South China during the Indosinian period was related to the NW subduction of the ancient Pacific Plate.
In summary, the driving force of the Indosinian tectonic–magmatic thermal event in South China should have come from the reduplicated remote effects of the collision between the North China Plate and the South China Plate in the north and of the subduction of the Paleo-Pacific Plate to the South China Plate (Figure 11). The collision of the North China Plate with the South China Plate and the subduction of the Pacific Plate caused the compression of the South China Plate, forming a series of NE-trending thrust structures. The thickening of the Earth’s crust facilitated crustal delamination, underplating of mantle-derived magma, and crustal heating, triggering intense partial melting of the lithosphere and magma enrichment. As a result, peraluminous S-type granite was formed in the Mengshan area, and its formation environment was an intracontinental subduction environment under the convergent tectonic system.

6. Conclusions

(1)
The medium–fine-grained biotite monzogranite and the fine-grained monzogranite in the Mengshan granitoid complex mainly formed at 220.7 ± 1.0 Ma to 218.0 ± 0.8 Ma and 211.5 ± 2.9 Ma to 212.9 ± 1.0 Ma, respectively. They are the products of the magmatic evolution of the Mengshan complex up to a late stage. They belong to the category of S-type granites and are characterized by strongly peraluminous, high K calc-alkaline content, high silica content, high Cs and U concentrations, and low Th/U ratios. They were derived from the partial melting of Proterozoic continent basement rocks, and minor mantle materials were involved during their generation.
(2)
Combined with the systematic field investigation in this study and previous data, three stages of magmatism are proposed for the formation of the Mengshan granitoid complex, comprising medium–coarse-grained porphyritic biotite granite formed at ca. 236–223 Ma, medium–fine-grained biotite monzogranite formed at ca. 222–217 Ma, and fine-grained monzogranite formed at ca. 212–211 Ma.
(3)
The presence of the Early Mesozoic Mengshan granitoid complex reflects a reduplicated far-field converge effect of the collision of the North China and South China blocks and the subduction of the Palaeo-Pacific plate into the South China block. The thickening of the Earth’s crust facilitated crustal delamination, the underplating of mantle-derived magma, and crustal heating, triggering the intense partial melting of the lithosphere and magma enrichment.

Supplementary Materials

The following supporting information can be downloaded at https://www.mdpi.com/article/10.3390/min14090854/s1. Table S1: Major element (wt%), REE element (ppm), and trace element (ppm) compositions of the Mengshan granitoid complex; Table S2: LA-ICP-MS zircon U-Pb data for the Mengshan granitoid complex; Table S3: LA-ICP-MS Lu-Hf analysis results of the Mengshan granitoid complex zircons [89,90,91].

Author Contributions

Conceptualization, J.W., Y.O., X.H. and Y.Z.; methodology, J.W., J.Z., R.Z. and Y.O.; software, R.Z.; validation, J.Z. and D.Z.; formal analysis, J.W., Y.Z. and X.H.; investigation, J.W., X.Z., X.H., T.Z., S.S. and D.Z.; resources, S.S., T.Z. and X.Z.; data curation, J.W. and Y.Z.; writing—original draft preparation, J.W. and Y.O.; writing—review and editing, X.H. and Y.Z.; visualization, S.S.; supervision, T.Z.; project administration, X.H., J.W., D.Z. and Y.O.; funding acquisition, X.H. and Y.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by a Jiangxi Geological Bureau Young Science and Technology Leader Training Programme Project (2023JXDZKJRC05 and 2022JXDZKJRC02), a National Natural Science Foundation of China (42302099), a project of Science and Technology Department of Hunan Province (2023JJ40624), a Natural Science Foundation of Jiangxi Province (20224BAB203037), a Geological survey project funded by the Provincial Department of Finance of Jiangxi Province (20240022), a Key R&D Project of Science and Technology Department of Jiangxi Province (20212BBG73045), and a Science and Technology Programme Project of Yingtan City (20233-185656 and 2024SYD017).

Data Availability Statement

The data are contained within the article and Supplementary Materials.

Acknowledgments

We are grateful to Youguo Deng, Lin He, Xianghui, Zeng and Qi Chen of the Tenth Geological Brigade of Jiangxi Geological Bureau, and Shuxun Wang, Mingjian Yang, and Mengying Cai of the China University of Geosciences (Beijing) for their help with fieldwork and indoor mapping. Special thanks go to the reviewers for their constructive comments on this paper.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (a) Simplified tectonic map of China showing major terranes around the South China Block; (b) simplified geological map showing the distribution of Mesozoic granites and volcanic rocks (modified from [14,33]).
Figure 1. (a) Simplified tectonic map of China showing major terranes around the South China Block; (b) simplified geological map showing the distribution of Mesozoic granites and volcanic rocks (modified from [14,33]).
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Figure 2. Simplified regional geological map showing the sampling locations in this study and the relative position of the three stages of granitic magmatism of the Mengshan granitoid complex (modified from [27,35]).
Figure 2. Simplified regional geological map showing the sampling locations in this study and the relative position of the three stages of granitic magmatism of the Mengshan granitoid complex (modified from [27,35]).
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Figure 3. Graph and micrograph of the Mengshan granitoid complex. (a) Grayish medium–coarse-grained biotite granite in stage I introduced via an intrusion by the grayish-white medium–fine-grained biotite monzogranite in stage II; (b) photograph of medium–coarse-grained biotite granite (stage I); (c–g) photographs and micrographs of the medium–fine-grained biotite monzogranite in stage II (sampling number 23MS-AFT-03); (h–l) photographs and micrographs of the fine-grained monzogranite in stage III (23MS-AFT-05). Bt—biotite; Kfs—K-feldspar; Ms—muscovite; Pl—plagioclase; Qz—quartz.
Figure 3. Graph and micrograph of the Mengshan granitoid complex. (a) Grayish medium–coarse-grained biotite granite in stage I introduced via an intrusion by the grayish-white medium–fine-grained biotite monzogranite in stage II; (b) photograph of medium–coarse-grained biotite granite (stage I); (c–g) photographs and micrographs of the medium–fine-grained biotite monzogranite in stage II (sampling number 23MS-AFT-03); (h–l) photographs and micrographs of the fine-grained monzogranite in stage III (23MS-AFT-05). Bt—biotite; Kfs—K-feldspar; Ms—muscovite; Pl—plagioclase; Qz—quartz.
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Figure 4. Classification and discriminant diagrams of magmatic rocks. (a) K2O+Na2O vs. SiO2 diagram [48]; (b) QAP (quartz–akali-feldspar–plagioclase) diagram; (c) K2O vs. SiO2 diagram [48]; (d) A/NK vs. A/CNK diagram [48].
Figure 4. Classification and discriminant diagrams of magmatic rocks. (a) K2O+Na2O vs. SiO2 diagram [48]; (b) QAP (quartz–akali-feldspar–plagioclase) diagram; (c) K2O vs. SiO2 diagram [48]; (d) A/NK vs. A/CNK diagram [48].
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Figure 5. (a) Chondrite-normalized REE and (b) N-MORB-normalized spider patterns of the Rizhao granites (normalizing factors are from [49]; N-MORB compositions are from [49]).
Figure 5. (a) Chondrite-normalized REE and (b) N-MORB-normalized spider patterns of the Rizhao granites (normalizing factors are from [49]; N-MORB compositions are from [49]).
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Figure 6. Cathodoluminescence (CL) images of zircons for the Mengshan granitoid complex.
Figure 6. Cathodoluminescence (CL) images of zircons for the Mengshan granitoid complex.
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Figure 7. U–Pb concordia diagram for the Mengshan granitoid complex: (a) 23MS-AFT-03, (b) 23MS-AFT-09, (c) 23MS-AFT-05, and (d) 23MS-AFT-08.
Figure 7. U–Pb concordia diagram for the Mengshan granitoid complex: (a) 23MS-AFT-03, (b) 23MS-AFT-09, (c) 23MS-AFT-05, and (d) 23MS-AFT-08.
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Figure 8. εHf(t) versus age diagram (a,b) (base image based on [54]).
Figure 8. εHf(t) versus age diagram (a,b) (base image based on [54]).
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Figure 10. Tectonic discrimination diagrams for magmatic rocks (base image according t [75]). (a) Rb vs. (Y+Nb) diagram; (b) Rb vs. (Yb+Ta) diagram. Syn-COLG, syn-collision granite; VAG, volcanic arc granite; WPG, within plate granite; ORG, ocean ridge granite; post-COLG, post-collision granite.
Figure 10. Tectonic discrimination diagrams for magmatic rocks (base image according t [75]). (a) Rb vs. (Y+Nb) diagram; (b) Rb vs. (Yb+Ta) diagram. Syn-COLG, syn-collision granite; VAG, volcanic arc granite; WPG, within plate granite; ORG, ocean ridge granite; post-COLG, post-collision granite.
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Figure 11. A dynamic model of the Mesozoic intracontinental subduction of the South China Plate (non-scaled for crust and lithosphere).
Figure 11. A dynamic model of the Mesozoic intracontinental subduction of the South China Plate (non-scaled for crust and lithosphere).
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Wei, J.; Ouyang, Y.; Zou, J.; Zeng, R.; Zhang, X.; Zhang, T.; Sui, S.; Zhang, D.; He, X.; Zhang, Y. Genesis of the Mengshan Granitoid Complex in an Early Mesozoic Intracontinental Subduction Tectonic Setting in South China: Evidence from Zircon U-Pb-Hf Isotopes and Geochemical Composition. Minerals 2024, 14, 854. https://doi.org/10.3390/min14090854

AMA Style

Wei J, Ouyang Y, Zou J, Zeng R, Zhang X, Zhang T, Sui S, Zhang D, He X, Zhang Y. Genesis of the Mengshan Granitoid Complex in an Early Mesozoic Intracontinental Subduction Tectonic Setting in South China: Evidence from Zircon U-Pb-Hf Isotopes and Geochemical Composition. Minerals. 2024; 14(9):854. https://doi.org/10.3390/min14090854

Chicago/Turabian Style

Wei, Jin, Yongpeng Ouyang, Jing Zou, Runling Zeng, Xinming Zhang, Tao Zhang, Shenao Sui, Da Zhang, Xiaolong He, and Yaoyao Zhang. 2024. "Genesis of the Mengshan Granitoid Complex in an Early Mesozoic Intracontinental Subduction Tectonic Setting in South China: Evidence from Zircon U-Pb-Hf Isotopes and Geochemical Composition" Minerals 14, no. 9: 854. https://doi.org/10.3390/min14090854

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