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Article

Geochemical Characteristics, U-Pb Age, and Hf Isotope of Zircons from Muscovite Granite in Aotou Sn Deposit, Eastern Nanling Range, South China

by
Wei Li
1,2,3,
Na Guo
3,*,
Jie Lu
1,
Xinghai Lang
3,
Dunmei Lian
1,
Qiwen Yuan
1 and
Shuwen Chen
1
1
The Seventh Geological Brigade of Jiangxi Bureau of Geology, Key Laboratory of Ionic Rare Earth Resources and Environment, Ganzhou 341000, China
2
Jiangxi Province Key Laboratory of Exploration and Development of Critical Mineral Resources, Nanchang 330000, China
3
College of Earth and Planetary Sciences, Chengdu University of Technology, Chengdu 610059, China
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(12), 1331; https://doi.org/10.3390/min15121331
Submission received: 13 November 2025 / Revised: 12 December 2025 / Accepted: 17 December 2025 / Published: 18 December 2025
(This article belongs to the Special Issue Mineralogy, Geochemistry and Geochronology of W-Sn Polymetallic Deposits, 2nd Edition)
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Abstract

The Jiulongnao W–Sn ore field in the eastern Nanling Range is characterized by large-scale early Yanshanian magmatic activity and W–Sn mineralization. In recent years, increasing attention has been given to the close relationship between Indosinian magmatic activity and Sn mineralization. The Aotou quartz vein-type Sn deposit is unique for only Sn mineralization without W during the Indosinian period. Seventeen thin-to-thick cassiterite–quartz veins are densely distributed in Ordovician metasandstone and slate, and these veins extend down to the top of the concealed granite. However, both the diagenetic age and the petrological characteristics of the concealed granite remain unclear. This contribution shows that the Aotou muscovite intrusion is a highly fractionated S-type pluton, characterized by a peraluminous, high-K composition, enrichment in LREEs, and depletion of Ba, Sr, Ti, and Eu. In this study, LA–ICP–MS zircon U–Pb dating of the concealed muscovite granite yields emplacement ages of 238.7 ± 1.0 Ma and 225.4 ± 0.9 Ma, indicating that at least two stages of magmatic intrusion occurred in the Triassic, with the diagenetic environment transitioning from a compressional setting to an extensional setting. The εHf(t) values during the two stages are −0.98 to −0.95 and −0.98 to −0.96, and the TDM2 values are 1.78–2.08 Ga and 1.78–2.06 Ga, indicating that two-stage magma was derived from the late Paleoproterozoic lower crustal materials. Comprehensive analysis reveals that the second stage of Indosinian magma intrusion (232–225 Ma) in the Jiulongnao ore field is closely related to Sn mineralization, and the northern Wenying pluton has good prospecting potential for quartz vein-type Sn(–W) deposits.

1. Introduction

The Nanling metallogenic belt is a world-famous W–Sn metallogenic province, characterized by large-scale W–Sn deposits that are related to magmatic–hydrothermal processes, such as quartz vein-type, skarn-type, and altered granite-type deposits. Multiple types of mineralization often coexist in the same deposit and are spatially associated, for example, the Shizhuyuan, Limu, Xintianling, Maoping, and other W, Sn, and W–Sn deposits [1,2,3]. Previous studies have shown that the large-scale magmatic intrusion activities during the early Yanshanian period in the Nanling Range are particularly closely related to W–Sn mineralization, forming numerous super-large or large W, Sn, and W–Sn deposits, e.g., the Furong, Xianghualing, Shizhuyuan, Xihuashan, Piaotang, and Pangushan [4,5,6,7,8]. However, in recent years, through the application of U–Pb dating technology for wolframite, cassiterite, and other ore-forming minerals, the high-precision metallogenic ages of the Limu, Guguaichong, Xitian, Chuangkou, Xikeng, and Aotou deposits in the Nanling Range have been accurately obtained [9,10,11,12,13,14], revealing that large-scale W-Sn mineralization also occurred in the Nanling Range during the Indosinian period [15,16]. Nevertheless, most of the granites that are closely related to the metallogenic space, such as Miao’ershan, Dupangling, and Wangxianling, show the characteristics of multi-stage intrusion. Therefore, accurately identifying the ore-forming granite and determining its magma source is of great significance for a comprehensive understanding of W–Sn mineralization during this period.
The Early Yanshanian quartz vein-type W–Sn deposits are densely distributed in the eastern Nanling Range, such as Xihuashan, Dajishan, Pangushan, etc., and the W–Sn-bearing late Jurassic granites are mainly fractionated S-type granitoids and most are biotite granite [17,18]. In recent years, it has been newly discovered that the Xikeng W–Sn deposit in the Jiulongnao ore field was formed during the Indosinian period, contemporaneously with the Indosinian Keshuling intrusion in this area, and it is inferred that the Keshuling intrusion is closely related to Indosinian W–Sn mineralization [19,20,21,22]. However, recent reports show that the U–Pb ages of wolframite and cassiterite in the Keshuling deposit are 157.5 Ma and 150.3 Ma, respectively [23,24], indicating that the W–Sn mineralization in the Keshuling deposit occurred during the Yanshanian period and was not contemporaneous with the Indosinian Keshuling intrusion. Therefore, the ore-forming granite of Indosinian W–Sn mineralization in the Jiulongnao ore field has not yet been determined, and the research on the relationship between Indosinian magmatic activity and W–Sn mineralization in this area is still weak, which restricts the development of metallogenic theory and prospecting work.
The Aotou Sn deposit is a rare quartz vein-type Sn deposit in the eastern Nanling Range. Previous 40Ar–39Ar dating of muscovite and U–Pb dating of cassiterite have accurately constrained the Sn mineralization age to the Indosinian period [14,25]. Moreover, granitic intrusions that are closely symbiotic with Sn ore veins are developed in the Aotou Sn deposit, but the formation age and geochemical characteristics of this intrusion are not clear at present, which seriously hinders the correct understanding of W–Sn mineralization in the Aotou Sn deposit and even in the Jiulongnao ore field. Based on the previous research results on the metallogenic age of the Aotou Sn deposit, this paper carries out zircon U–Pb chronology, whole-rock major and trace elements, and Lu–Hf isotope studies on the Aotou concealed granite, aiming to discuss the petrogenesis, emplacement timing, and magma source of the Aotou granite, and promote comprehensive understanding of the relationship between the Indosinian magmatic activity and W–Sn mineralization in the Jiulongnao ore field.

2. Geological Background

The Jiulongnao ore field is located in the eastern Nanling Range (Figure 1a). More than twenty W, Sn, or W–Sn deposits, such as the Taoxikeng, Jiulongnao, Keshuling, and Aotou deposits, have been found around the Jiulongnao composite granite (Figure 1b). Multiple types of W–Sn mineralization have been identified, including quartz vein-, altered granite-, and skarn-type mineralization, and the quartz vein-type mineralization is the most developed. This field is composed of a Neoproterozoic–Silurian metamorphic folded basement, which is the main surrounding rock for quartz vein-type W–Sn ore veins. Devonian–Triassic sedimentary rocks are distributed in the east section. Fault structures are well developed in this ore field, including N–S-, E–W-, NE–SW-, and NW–SE-trending faults. The NE–SW-trending faults are the most developed and largest in scale, and NE–SW-, E–W-, and NW–SE-trending faults and their associated secondary fracture systems are the main ore-controlling structures for quartz vein-type tungsten in this field.
There were at least three epochs of magma intrusion in the Jiulongnao ore field [13]. Magmatic activity was most intense during the early Yanshanian period, resulting in the formation of the Jiulongnao and Baoshan granites, as well as the Taoxikeng and Dongfeng concealed granites, which are closely related to the W–Sn mineralization in this region [26]. Previous studies have suggested that Indosinian intrusions, for example, the Wenying granites, are closely related to U mineralization [27,28,29], whereas the Keshuling intrusion is closely associated with W–Sn mineralization [21,22]. The Caledonian magmatic activity in this region was relatively weak, with only the formation of the Guantian granodiorite and some basic dykes, which are not related to W–Sn mineralization.

3. Deposit Geology

The Aotou Sn deposit is the only quartz vein-type Sn deposit located in the central part of the Jiulongnao ore field. Nearly 90% of the Upper Ordovician Gaotan Formation is exposed in this deposit (Figure 2a), with metamorphic quartz sandstone and slate interbedded with carbonaceous slate. NE–SW- and NW–SE-trending faults are present in this area, and the former are the main ore-controlling structures, whereas the NW–SE-trending faults are post-mineralization structures.
The Caledonian Guantian granodiorite intrusion is exposed in the northwestern part of the deposit and is not spatially correlated with Sn mineralization. The granite that is concealed 45 m below the mineralization zone is medium- to fine-grained muscovite granite, with a grayish-white color, a medium to fine-grained texture, and a massive structure (Figure 3a). The granite is composed of 30–33 vol% quartz, 15–20 vol% microcline, 15–20 vol% plagioclase, 10–13 vol% muscovite, 7–10 vol% orthoclase, 2–3 vol% biotite (Figure 3a–c), and 1 vol% accessory minerals. The main mineral particle sizes range from 0.1 to 0.5 mm.
Seventeen thin-to-thick cassiterite–quartz veins densely distributed in an area of about 0.2 km2 are hosted in Ordovician metasandstone and slate. The ore veinlets are oriented mainly NE–SW and extend for approximately 50–700 m, with widths of 18–76 m. The vein density ranges from 0.7 to 1.3 veins/m, and the vein-bearing rate is 0.8% to 11%, with Sn @0.16% on average. The thin quartz veins are 0.05–0.10 m wide but gradually merge into 0.2–0.9 m ore veins in deep tunnels. The ore minerals are mainly cassiterite and minor wolframite chalcopyrite. The cassiterite is light brown in color and has an idiomorphic granular texture, which is often distributed at the edges of the ore veins.

4. Sampling and Methods

4.1. Sampling

All muscovite granite samples were collected from a mining tunnel at a level of 490 m. Samples of the five granites, i.e., from AT01 to AT05, with no or weak mineralization alteration, were collected for whole-rock major and trace element analyses. Sample AT-01 was also used for zircon U–Pb dating and Hf isotope analyses. Both hand specimen observation and microscopic identification confirmed that the samples were muscovite granite.

4.2. Whole-Rock Major and Trace Element Analyses

Whole-rock major and trace element testing was carried out at the Yanduzhongshi Geological Analysis Laboratories Ltd., Beijing, China. Fresh samples were first broken to centimeter sizes; only the fresh pieces were selected, washed with deionized water, dried, and then ground to less than 200 mesh (0.5200 ± 0.0001 g) for geochemical analyses. Sample powders were fluxed with Li2B4O7 (1:8) to make homogeneous glass disks at 1150 °C using a V8C automatic fusion machine produced by the Analymate Company in Guangzhou, China. The major bulk rock major elements were analyzed using X-ray fluorescence spectrometry techniques (Zetium, PANalytical from Almolo, Netherlands or XRF-1800, Shimadzu from Kyoto, Japan). The analytical errors for major elements were better than 1%. For trace element analysis, sample powders were first dissolved using distilled HF + HNO3 in a screw-top Teflon beaker for 72 h at 190 °C. Trace elements of those samples were analyzed by inductively coupled mass spectrometry (ICP–MS) at the Yanduzhongshi Geological Analysis Laboratories Ltd. The analytical uncertainty of the elements examined here was better than 5% for ICP–MS analysis, except for a few samples with low contents of trace elements for which the uncertainty was about 10%. The obtained values of the trace elements in the GSR-2 standard are all consistent with their recommended values.

4.3. Zircon LA–ICP–MS In Situ U–Pb Dating Method

Zircon U–Pb isotope analysis was carried out in situ by using an NWR193 laser ablation microprobe (Elemental Scientific Lasers LLC, Portland, Oregon, USA), attached to an Analytikjena PlasmaQuant MS (Jena, Germany) quadrupole ICP-MS at Yanduzhongshi Geological Analysis Laboratories Ltd. Helium was used as the carrier gas, and argon gas was mixed as the compensation gas during the laser ablation process, with both passed through a Y-shaped junction before entering ICP. Laser pulses (9 Hz) with a spot size of 26 μm were used to ablate the surfaces of the zircon grains. Every time-resolved analysis includes an approximately 20–30 s blank signal and a 40 s sample signal. Offline processing of data was completed using ZSkits v. 1.0 [30]. Standard Plesovice and NIST 610 were used as external calibrations for the U–Pb ages and trace element content calculations, respectively. Zircon standards 91500, Tanz, and ZS were analyzed between every 10 unknown samples for quality control. Weighted average ages were calculated, and a concordia diagram was constructed with Isoplot 4.15 [31]. The standard samples 91500, Plesovice, Tanz, and ZS had values that coincide with those recommended [32,33,34,35].

4.4. In Situ Zircon Hf Isotope Analyses

Zircon Lu–Hf isotope analysis was carried out in situ by using an NWR193 laser ablation microprobe (Elemental Scientific Lasers LLC, Portland, Oregon, USA), attached to a Neptune multicollector ICP–MS at Yanduzhongshi Geological Analysis Laboratories Ltd., Beijing, China. Instrumental conditions and data acquisition were comprehensively described by Wu et al. [36]. A “wire” signal smoothing device was included in this laser ablation system (e.g., [37]), and helium was used as the carrier gas. All the data were acquired on zircons in single-spot ablation mode with a spot size of 44 μm. The energy density of the laser ablation used in this study was ~7.0 J cm−2. The ratios 176Yb/173Yb = 0.79622 and 176Lu/175Lu = 0.02658 (e.g., [38]) were used to calculate 176Yb/177Hf and 176Lu/177Hf, and 172Yb/173Yb = 1.35274 (e.g., [38]) and 179Hf/177Hf = 0.7325 were used to correct instrumental mass bias, respectively. The details of the mass bias correction protocol are described in Wu et al. [36]. Zircon 91500 and Plesovice were used as the reference standards during our routine analyses. The single-stage Hf model age (TDM1) is calculated relative to the depleted mantle with present-day 176Hf/177Hf = 0.28325 and 176Lu/177Hf = 0.0384 (e.g., [39]).

5. Results

5.1. Whole-Rock Major and Trace Element Compositions

Five muscovite granite samples were collected for whole-rock major and trace element analysis, and the results are given in Table 1. The Aotou granites have very similar geochemical characteristics, with high SiO2 contents ranging from 71.56% to 73.17% and high K2O contents ranging from 5.29% to 5.46%, and plot in the high-K to shoshonitic field in terms of K2O vs. SiO2 (Figure 4a), with strongly peraluminous compositions and A/CNK values ranging from 1.16 to 1.33 (Figure 4b). The contents of TiO2, MnO, and P2O5 in the granite are very low. Five samples show similar trace element characteristics. The total REE contents range from 83.43 to 101.96 ppm; the LREE/HREE ratios range from 9.37 to 10.86; the δEu values range from 0.32 to 0.40; and the δCe values range from 1.01 to 1.03. In the chondrite-normalized REE patterns (Figure 4c), the Aotou granites are enriched in LREEs, have large negative Eu anomalies, and exhibit a right-dipping “seagull” distribution, suggesting that large-scale plagioclase fractional crystallization occurred. The Aotou granites contain relatively high contents of mineralization-related elements such as W, Sn, and Li, which are closely related to Sn mineralization. In the primitive mantle-normalized trace element diagram (Figure 4d), the samples show a consistent overall trend of right dipping, with significant depletion of Ba, Nb, Sr, and Ti, which suggests that plagioclase or Fe–Ti oxides underwent fractional crystallization during magma crystallization, indicating that the magma was derived from the crust [40].

5.2. Zircon U–Pb Ages

Most zircons from Sample AT01 are euhedral to subhedral and 90–180 µm long, and yield length/width ratios ranging from 1:1 to 4:1. These zircons have well-developed oscillatory cathodoluminescence (CL) zoning and clear internal structures and rhythmic zoning patterns (Figure 3c), which are characteristic of magmatic zircons. LA–ICP–MS U–Pb dating results for eighteen points on 20 grains from the Aotou intrusion are shown in Table 2. The Th/U ratios vary from 0.09 to 1.00, with an average of 0.32, and most grains have Th/U ratios between 0.1 and 0.4, which are lower than those of zircons from general magmatic rocks and Yanshanian metallogenic granites in the Nanling Range [2,42]. The ages of twenty zircons are concentrated in the range of 221.7–240.4 Ma and can be divided into two age ranges. The ages of the twelve grains range from 221.7 Ma to 229.2 Ma and yield a lower intercept age of 225.4 ± 0.9 Ma (MSDW = 0.1), which coincides well with the weighted mean 206Pb/238U age of 225.4 ± 1.8 Ma (MSDW = 0.5) (Figure 5a). Eight grains are 237.4–240.4 Ma in age, and the concordant age and weighted mean age are 238.7 ± 1.0 Ma (MSDW = 0.6) and 238.8 ± 2.1 Ma (MSDW = 0.1), respectively (Figure 5b).

5.3. Zircon Hf Isotopes

In situ zircon Hf isotope determination points are the same as those used for the zircon U–Pb measurements, and the data from twenty measured spots in the AT01 sample are listed in Table 3 and plotted in Figure 4c,d. The initial 176Hf/177Hf ratios during the two stages vary from 0.282272 to 0.282405 and 0.282282 to 0.282399; the 176Lu/177Hf ratios vary from 0.000684 to 0.001756 and 0.000684 to 0.001329; and the fLu/Hf values are −0.98 to −0.95 and −0.98 to −0.96, respectively. The corresponding εHf(t) values range from −12.6 to −8.2 and 12.5 to −8.1; the two-stage model ages (TDM2) are 1.78–2.08 Ga and 1.78–2.06 Ga, indicating that the two-stage magma may have the same material source.

6. Discussion

6.1. Timing of Granite Emplacement in the Aotou Deposit

The Guantian granodiorite intrusion is exposed in the northeastern part of the Aotou deposit, with a crystallization age of 417.1 ± 3.2 Ma [43], and formed during the Caledonian period. The Wenying composite pluton intruded mainly from 247 to 231 Ma, with the age of the first-stage granite concentrated at ~236 Ma, which is significantly earlier than the later highly evolved granite (~227 Ma; [27,28]), indicating that there are at least two intrusive phases that occurred during the Indosinian period in the Jiulongnao ore field. The muscovite granite is concealed in the lower part of the cassiterite–quartz veins and is closely related to Sn mineralization in the Aotou deposit. Unlike those of the Guantian intrusion, the lithology characteristics of the Aotou concealed granite are similar to those of the third-stage intrusion of the Jiulongnao granitic complex. This is why the Aotou granitic deposit was classified as a Jurassic granite, and the Aotou Sn deposit formed during the early Yanshanian period [44,45,46].
In recent years, cassiterite U–Pb dating of the Aotou deposit has yielded ages of 227.4 ± 6.9 Ma and 228.0 ± 1.5 Ma [14,21], which are essentially consistent with the 40Ar-39Ar age of muscovite (228.7 ± 1.5 Ma) [14,25]. These metallogenic ages reveal that Sn mineralization in the Aotou deposit occurred during the Indosinian period. Considering the close association between the cassiterite–quartz veins and the concealed granite in this deposit, we presume that the granites formed during the Indosinian period rather than the early Yanshanian period. In this study, the crystallization ages of the muscovite granite are determined to be 238.7 ± 1.0 Ma and 225.4 ± 0.9 Ma, indicating two stages of magmatic intrusion during the Indosinian period. The second magmatic episode is consistent with the Sn mineralization within the error range of the Aotou deposit, suggesting that diagenetic and mineralization processes occurred in the Late Triassic. In addition to the widely exposed Wenying intrusion related to U mineralization in the Jiulongnao ore field, the Indosinian Keshuling, Xikeng, and Aotou granites are closely associated with W–Sn mineralization in this area [19,20,21,22,23,25]. These findings suggest that large-scale Indosinian magmatic activity and W–Sn mineralization occurred in the Jiulongnao ore field.

6.2. Origin of Magmatism

Many researchers have suggested that the granites closely related to W–Sn mineralization in South China are mainly S-type [2,47,48,49], but Wu et al. [50] reported that ore-forming granites with peraluminous and muscovite-rich characteristics are highly differentiated I-type intrusions. The Aotou granites are characterized by high-silica, peraluminous, and high-K compositions, and are enriched in LREEs, as well as negative for Ba, Sr, Ti, and Eu, indicating highly fractionated granite. The REE contents of the Aotou granites (average 90 ppm) are significantly lower than those of the Jiulongnao pluton (e.g., [46]), the Taoxikeng ore-forming granite (e.g., [51]), and the Baoshan granite (e.g., [52]) in this ore field, indicating that it underwent a higher degree of fractional evolution [3]. In the (Zr + Nb + Ce + Y) vs. (Na2O + K2O)/(CaO) diagram (Figure 6a), the Aotou granites mainly plot in the highly differentiated granite area, and they plot in the S-type granite area in the SiO2 vs. P2O5. diagram (Figure 6b) and Rb vs. Th diagram (Figure 6c).
The Zr/Hf ratios (30.7–33.2) and Nb/Ta ratios (5.5–9.2) of the Aotou granites are lower than those of mantle-derived rocks (e.g., [40,53]) and are close to the average values for the continental crust (e.g., [54]), indicating that the granites may have been derived from crustal materials. Hf isotopes of zircon can be used to effectively trace magmatic sources [55]. The n(176Lu)/n(177Hf) ratios (0.000480 to 0.001159) and fLu/Hf values (−0.99 to −0.97) are significantly lower than those of the upper crust (Figure 5c,d) [56]. The low εHf(t) values range from −12.7 to −8.0, and the Hf two-stage model ages (TDM2) range from 1.57 Ga to 1.90 Ga, indicating that the Aotou intrusion was most likely derived from the partial melting of late Paleoproterozoic lower crustal materials. As discussed above, the Aotou intrusion is a highly fractionated S-type granite. According to previous research results, the Aotou intrusion shares petrological characteristics, geochemical characteristics, zircon U–Pb geochronology, and Hf isotopes similar to those of the Keshuling granite in the Jiulongnao ore field [13,20,21,22], suggesting that the Indosinian W–Sn ore-forming granites share similar magmatic source material and magmatic evolution processes.
Minerals 15 01331 g006
Figure 6. The (Zr + Nb + Ce + Y) vs. (Na2O + K2O)/CaO diagrams (a), SiO2 vs. P2O5 (b), Rb vs. Th diagrams (c) and R1 vs. R2 diagram (d) for the Aotou granites, eastern Nanling Range. (a–d) are modified from [57,58,59], and the sources of the Keshuling granite data are from [22].
Figure 6. The (Zr + Nb + Ce + Y) vs. (Na2O + K2O)/CaO diagrams (a), SiO2 vs. P2O5 (b), Rb vs. Th diagrams (c) and R1 vs. R2 diagram (d) for the Aotou granites, eastern Nanling Range. (a–d) are modified from [57,58,59], and the sources of the Keshuling granite data are from [22].
Minerals 15 01331 g006

6.3. Geodynamic Setting of the Aotou Granite

The Indo-China movement in South China may have begun in the middle Permian (~260 Ma; [60]). Intense compressional collision between the North China, South China, and Indo-China blocks may have occurred in the late Permian or Early Triassic [61,62,63], and this tectonic setting may have persisted until the formation of the Pangea continent in the Late Triassic (~220 Ma, [64,65,66]). The Jiulongnao ore field is located in the eastern part of the South China Block, far from the compressional uplift center of collision and extrusion. Since the Middle Triassic sedimentary strata are absent in southern Jiangxi, it is inferred that the Indo-China movement in the Jiulongnao ore field may have started in the late Early Triassic or Middle Triassic, initiating Indosinian magmatic intrusion and associated mineralization in the region. The Aotou granites plot in the syn-collisional granite and post-orogenic granite fields in the R1–R2 discrimination diagram (Figure 6d), indicating that the diagenetic environment transitioned from a compressional setting to an extensional setting during the late stage of the Indo-China movement.
The two-stage crystallization ages of the Aotou concealed granite are consistent with those of the Wenying granite complex, indicating that at least two intrusive phases have occurred in the Jiulongnao ore field. This is consistent with the two-stage crystallization age of the Aotou concealed granite in this study. The Keshuling and Xikeng granites in this field formed at 232–225 Ma, which is consistent with the second stage of the Aotou and Wenying granites. Since the Sn or W–Sn quartz veins in the Xikeng and Aotou deposits are divergent from the concealed granite, and the cassiterite and wolframite U–Pb ages are concentrated in 228–227 Ma [13,25], it is inferred that the Indosinian W–Sn mineralization was associated with the second-stage intrusive activity during the Indosinian period. On the basis of the distribution of Indosinian granites and stream sediment anomaly in the Jiulongnao ore field [67], we propose that the second-stage intrusions distributed around the northern Wenying granite have good prospecting potential for quartz vein-type Sn(–W) deposits, which is a new direction for future exploration in this area.

7. Conclusions

  • LA–ICP–MS zircon U–Pb dating of the Aotou concealed granite yields lower intercept ages of 238.7 ± 1.0 Ma and 225.4 ± 0.9 Ma, indicating that the pluton experienced two intrusive phases during the Indosinian period.
  • The geochemical characteristics and Hf isotopes indicate that the Aotou granite was highly differentiated and derived from the late Paleoproterozoic lower crustal materials.
  • The Jiulongnao W–Sn ore field experienced two intrusive stages during the Indosinian period, and the second-stage granites are closely related to Sn(–W) mineralization.

Author Contributions

Conceptualization, N.G. and X.L.; field investigation, J.L., S.C., Q.Y., and W.L.; data curation, D.L. and W.L.; writing—original draft preparation, W.L.; writing—review and editing, N.G.; supervision, X.L.; funding acquisition, W.L. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by the project from Jiangxi Province Key Laboratory of Exploration and Development of Critical Mineral Resources (Grant No. GJKC2025ZZ03), the Young Science and Technology Leader Training Plan Project of Jiangxi Bureau of Geology (Grant No. 2024JXDZKJRC01) and the National Science and Technology Major Project (Grant No. 2025ZD1009707).

Data Availability Statement

All the data are presented in the paper.

Acknowledgments

The authors would like to acknowledge Shiwei Song and four anonymous reviewers for their constructive comments, which helped to significantly improve the manuscript. We thank senior engineer Huan Wang for their great effort in sample testing and data processing.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. The location (a) and geological map (b) of the Jiulongnao ore field in the eastern Nanling Range, South China (modified from [22]).
Figure 1. The location (a) and geological map (b) of the Jiulongnao ore field in the eastern Nanling Range, South China (modified from [22]).
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Figure 2. Geological map (a) and cross-section through the A–A’ exploration line (b) of the Aotou quartz vein-type Sn deposit, eastern Nanling Range (modified from [14]).
Figure 2. Geological map (a) and cross-section through the A–A’ exploration line (b) of the Aotou quartz vein-type Sn deposit, eastern Nanling Range (modified from [14]).
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Figure 3. Photographs showing features of muscovite granite samples (a–c) and cathodoluminescence (CL) images of zircons (d) from the Xikeng W–Sn deposit, eastern Nanling region. Qtz: quartz; Pl: plagioclase; Or: orthoclase; Bt: biotite; Ms: muscovite; Mc: microcline.
Figure 3. Photographs showing features of muscovite granite samples (a–c) and cathodoluminescence (CL) images of zircons (d) from the Xikeng W–Sn deposit, eastern Nanling region. Qtz: quartz; Pl: plagioclase; Or: orthoclase; Bt: biotite; Ms: muscovite; Mc: microcline.
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Figure 4. SiO2 vs. K2O diagram (a), A/CNK vs. A/NK diagrams (b), chondrite-normalized REE patterns (c), and element diagrams (d) for the Aotou granites, eastern Nanling Range. Normalization values are from Sun and McDonough [41].
Figure 4. SiO2 vs. K2O diagram (a), A/CNK vs. A/NK diagrams (b), chondrite-normalized REE patterns (c), and element diagrams (d) for the Aotou granites, eastern Nanling Range. Normalization values are from Sun and McDonough [41].
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Figure 5. U–Pb ages of zircon (a,b) and εHf(t) vs. age plots (c,d) for the Aotou granites, eastern Nanling Range.
Figure 5. U–Pb ages of zircon (a,b) and εHf(t) vs. age plots (c,d) for the Aotou granites, eastern Nanling Range.
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Table 1. Major and trace element compositions for the Aotou muscovite granites, eastern Nanling Range.
Table 1. Major and trace element compositions for the Aotou muscovite granites, eastern Nanling Range.
Sample
Numbers		SiO2TiO2Al2O3TFe2O3FeOMnOMgOCaONa2OK2OP2O5LOIA/CNK
AT-H173.170.16514.191.431.130.0320.4920.8232.955.290.2331.191.23
AT-H271.560.17015.601.431.030.0340.5030.7683.015.460.2351.181.33
AT-H371.580.16915.411.451.130.0340.4620.8373.295.360.2361.121.26
AT-H472.090.16415.131.391.030.0350.4220.8333.245.330.2361.091.25
AT-H572.150.16914.671.451.130.0350.4070.9113.395.460.2331.081.16
Sample
Numbers		ARσ43R1R2LaCePrNdSmEuGdTbDy
AT-H12.32.26252738817.334.73.9716.83.270.3102.700.4301.97
AT-H22.172.53236441017.535.04.0116.93.300.3822.800.4582.12
AT-H32.362.63228641218.336.84.3217.53.500.4222.990.4702.21
AT-H42.362.53235140421.142.64.9719.04.080.4103.760.5602.84
AT-H52.542.7226640219.539.04.5717.43.780.4133.550.5292.52
Sample
Numbers		HoErTmYbLuYΣREE(La/Yb)NδEuδCeLiBeRb
AT-H10.2980.7350.1060.6980.0979.3483.4 17.8 0.32 1.03 57.8 13.0 344
AT-H20.3170.8030.1170.7360.10910.284.6 17.1 0.38 1.02 62.1 12.3 375
AT-H30.3250.8510.1220.7310.11610.688.6 18.0 0.40 1.01 62.7 9.67 373
AT-H40.4141.030.1570.9270.14512.810216.3 0.32 1.02 76.1 14.6 424
AT-H50.3790.9250.1440.8360.12912.193.7 16.7 0.34 1.01 78.9 10.8 422
Sample
Numbers		BaThUNbSrZrHfScTaCrCoNiCs
AT-H1179 9.35 12.1 13.8 37.9 70.6 2.13 2.83 1.63 7.90 1.33 4.72 27.0
AT-H2249 10.1 11.1 14.8 46.2 73.3 2.23 3.11 1.66 6.89 1.33 3.40 29.1
AT-H3271 9.86 8.01 14.9 50.9 113 3.49 2.99 1.65 8.43 1.49 3.07 29.4
AT-H4224 12.63 10.6 16.5 52.2 86.9 2.83 3.35 1.79 8.62 1.72 6.28 34.8
AT-H5238 11.33 18.0 17.0 57.7 97.9 3.15 3.45 1.94 8.83 1.65 3.67 33.4
Sample
Numbers		VGaAsBiSbWSnCuPbZnRb/SrZr/HfNb/Ta
AT-H17.57 17.6 0.679 0.4530.117 3.34 20.1 3.70 33.8 53.4 9.06 33.198.47
AT-H28.44 19.5 0.747 0.5190.074 3.47 20.7 3.01 35.0 46.3 8.13 32.858.96
AT-H38.53 19.8 0.826 0.9260.113 3.17 21.5 3.82 35.4 45.6 7.33 32.299.03
AT-H49.28 22.5 0.956 0.5800.126 4.01 25.1 4.48 39.4 58.0 8.16 30.739.21
AT-H59.21 23.1 1.62 0.5220.091 3.44 24.6 4.77 40.0 52.3 7.30 31.068.77
Table 2. LA-ICP-MS zircon U–Pb dating results for the Aotou muscovite granites, eastern Nanling Range.
Table 2. LA-ICP-MS zircon U–Pb dating results for the Aotou muscovite granites, eastern Nanling Range.
Sample
(Spot)		U
μg/g		Th
μg/g		U/Th
Ratio 		207Pb/206Pb1 Sigma207Pb/235U1 Sigma206Pb/238U1 Sigma206Pb/238U
Age (Ma)		1 SigmaCor.
%
Mean = 225.4 ± 1.8 Ma, MSWD = 0.5, n = 12
AT01-018151660.20 0.0504 0.0006 0.2491 0.0038 0.0359 0.0004 227.2 2.5 99.4
AT01-0210201430.14 0.0503 0.0009 0.2469 0.0058 0.0358 0.0008 226.5 4.7 98.9
AT01-045551290.23 0.0505 0.0007 0.2482 0.0052 0.0356 0.0006 225.5 3.5 99.8
AT01-054601710.37 0.0504 0.0006 0.2459 0.0036 0.0354 0.0004 224.2 2.4 99.6
AT01-064361060.24 0.0503 0.0007 0.2444 0.0052 0.0352 0.0005 223.2 3.4 99.5
AT01-1225602420.09 0.0512 0.0006 0.2473 0.0037 0.0350 0.0004 221.7 2.6 98.8
AT01-136881770.26 0.0503 0.0007 0.2471 0.0046 0.0356 0.0005 225.3 3.2 99.5
AT01-1613202070.16 0.0507 0.0008 0.2509 0.0038 0.0360 0.0005 227.7 3.1 99.8
AT01-175341380.26 0.0507 0.0009 0.2520 0.0055 0.0360 0.0006 227.9 3.6 99.9
AT01-187751740.22 0.0513 0.0009 0.2505 0.0050 0.0355 0.0006 224.6 3.7 99.0
AT01-233732210.59 0.0506 0.0010 0.2470 0.0053 0.0355 0.0005 225.1 2.8 99.6
AT01-244061990.49 0.0504 0.0012 0.2506 0.0077 0.0362 0.0006 229.2 4.0 99.1
Mean = 238.7 ± 1.0 Ma, MSWD = 0.6, n = 8
AT01-093691870.51 0.0510 0.0008 0.2670 0.0056 0.0380 0.0006 240.4 3.6 100
AT01-109133310.36 0.0513 0.0009 0.2659 0.0049 0.0376 0.0004 237.9 2.8 99.4
AT01-1113502030.15 0.0505 0.0005 0.2636 0.0043 0.0378 0.0005 239.0 3.1 99.4
AT01-1410601570.15 0.0507 0.0005 0.2623 0.0043 0.0375 0.0005 237.4 3.1 99.6
AT01-154132320.56 0.0509 0.0007 0.2647 0.0038 0.0377 0.0004 238.4 2.4 100
AT01-197821580.20 0.0504 0.0006 0.2617 0.0042 0.0377 0.0006 238.4 3.6 99.0
AT01-208482170.26 0.0512 0.0008 0.2681 0.0052 0.0380 0.0006 240.3 3.7 99.7
AT01-212182171.00 0.0509 0.0009 0.2663 0.0057 0.0379 0.0005 240.0 3.1 99.9
Table 3. In situ zircon Hf isotope results for the Aotou muscovite granites, eastern Nanling Range.
Table 3. In situ zircon Hf isotope results for the Aotou muscovite granites, eastern Nanling Range.
Sample
(Spot)		t (Ma)176Yb/177Hf
(Corr.)		2 Sigma176Lu/177Hf
(Corr.)		2 Sigma176Hf/177Hf
(Corr.)		2 SigmaεHf(t)TDM1
(Ma)		TDM2
(Ma)		fLu/Hf
the first stage
AT01-01227.2 0.03164 0.00068 0.001186 0.000027 0.282321 0.000015 −11.1 1321 1966 −0.96
AT01-02226.5 0.03995 0.00167 0.001608 0.000065 0.282339 0.000016 −10.6 1310 1930 −0.95
AT01-04225.5 0.02102 0.00022 0.000831 0.000010 0.282353 0.000014 −10.0 1264 1893 −0.97
AT01-05224.2 0.02151 0.00013 0.000846 0.000006 0.282405 0.000015 −8.2 1191 1777 −0.97
AT01-06223.2 0.02092 0.00040 0.000829 0.000015 0.282353 0.000017 −10.1 1264 1895 −0.98
AT01-12227.9 0.04517 0.00103 0.001756 0.000036 0.282346 0.000014 −10.3 1305 1914 −0.95
AT01-13224.6 0.01852 0.00019 0.000722 0.000010 0.282340 0.000014 −10.5 1279 1922 −0.98
AT01-16240.4 0.03705 0.00061 0.001400 0.000026 0.282272 0.000014 −12.6 1398 2071 −0.96
AT01-17237.9 0.02783 0.00037 0.001077 0.000014 0.282348 0.000013 −10.0 1280 1900 −0.97
AT01-18239.0 0.02616 0.00071 0.001038 0.000028 0.282369 0.000015 −9.2 1248 1850 −0.97
AT01-23240.3 0.02606 0.00030 0.001038 0.000013 0.282305 0.000014 −11.4 1338 1994 −0.97
AT01-24240.0 0.02203 0.00050.000868 0.000018 0.282359 0.000018 −9.5 1257 1870 −0.97
the second stage
AT01-09221.7 0.01743 0.00024 0.000684 0.000008 0.282346 0.000015 −10.3 1269 1909 −0.98
AT01-10225.3 0.03029 0.00063 0.001197 0.000022 0.282375 0.000015 −9.3 1245 1847 −0.96
AT01-11227.7 0.03459 0.00097 0.001328 0.000024 0.282282 0.000014 −12.5 1381 2055 −0.96
AT01-14225.1 0.03407 0.00071 0.001329 0.000023 0.282377 0.000012 −9.2 1246 1843 −0.96
AT01-15229.2 0.02026 0.00012 0.000784 0.000002 0.282349 0.000016 −10.0 1267 1898 −0.98
AT01-19237.4 0.02417 0.00046 0.000952 0.000012 0.282327 0.000013 −10.7 1305 1945 −0.97
AT01-20238.4 0.02820 0.00040 0.001126 0.000018 0.282380 0.000016 −8.8 1236 1828 −0.97
AT01-21238.4 0.01987 0.00016 0.000770 0.000007 0.282399 0.000014 −8.1 1197 1780 −0.98
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Li, W.; Guo, N.; Lu, J.; Lang, X.; Lian, D.; Yuan, Q.; Chen, S. Geochemical Characteristics, U-Pb Age, and Hf Isotope of Zircons from Muscovite Granite in Aotou Sn Deposit, Eastern Nanling Range, South China. Minerals 2025, 15, 1331. https://doi.org/10.3390/min15121331

AMA Style

Li W, Guo N, Lu J, Lang X, Lian D, Yuan Q, Chen S. Geochemical Characteristics, U-Pb Age, and Hf Isotope of Zircons from Muscovite Granite in Aotou Sn Deposit, Eastern Nanling Range, South China. Minerals. 2025; 15(12):1331. https://doi.org/10.3390/min15121331

Chicago/Turabian Style

Li, Wei, Na Guo, Jie Lu, Xinghai Lang, Dunmei Lian, Qiwen Yuan, and Shuwen Chen. 2025. "Geochemical Characteristics, U-Pb Age, and Hf Isotope of Zircons from Muscovite Granite in Aotou Sn Deposit, Eastern Nanling Range, South China" Minerals 15, no. 12: 1331. https://doi.org/10.3390/min15121331

APA Style

Li, W., Guo, N., Lu, J., Lang, X., Lian, D., Yuan, Q., & Chen, S. (2025). Geochemical Characteristics, U-Pb Age, and Hf Isotope of Zircons from Muscovite Granite in Aotou Sn Deposit, Eastern Nanling Range, South China. Minerals, 15(12), 1331. https://doi.org/10.3390/min15121331

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