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Article

Petrogenesis of the Helong Granites in Southern Jiangxi Province, China: Constraints from Geochemistry and In Situ Analyses of Zircon U–Pb–Hf Isotopes

by
Xinxing Liu
1,
Weixin Shi
2,*,
Juan Zhang
1,*,
Xiaoyan Zhang
1,
Junfeng Yang
1 and
Wei Li
3
1
Hebei Key Laboratory of Strategic Critical Mineral Resources, Hebei GEO University, Shijiazhuang 050031, China
2
Cores and Samples Center of Natural Resources, China Geological Survey, Beijing 100192, China
3
The Seventh Geological Brigade of Jiangxi Bureau of Geology, Key Laboratory of Ionic Rare Earth Resources and Environment, Ganzhou 341000, China
*
Authors to whom correspondence should be addressed.
Minerals 2023, 13(1), 101; https://doi.org/10.3390/min13010101
Submission received: 24 November 2022 / Revised: 24 December 2022 / Accepted: 5 January 2023 / Published: 9 January 2023
(This article belongs to the Special Issue Petrology, Mineralogy, Geochemistry and Geochronology of Granites)
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Abstract

:
The Jinzhuping and Changkeng granites are related to the Helong W–Sn ore field in southern Jiangxi Province, China. Three different phases can be found in the Jinzhuping pluton, and their LA-ICP-MS zircon U–Pb ages are 155.2 ± 0.68 Ma, 154.0 ± 0.56 Ma, and 153.4 ± 0.99 Ma, respectively, indicating two types of granitic rocks. All granites in the Helong ore field have similar geochemical characteristics, they have high contents of SiO2 (73.99 wt.%–77.68 wt.%), and total alkali (7.56 wt.%–8.76 wt.%) and are weakly to strongly peraluminous. They are slightly enriched in HREE and depleted in Eu, Ba, Sr, P, and Ti. Zircon εHf(t) values of the Jinzhuping three granites are from −14.4 to −10.4, from −15.3 to −11.4, and from −18.1 to −10.5, and the Hf TDM model ages range from 1.83 to 2.06 Ga, from 1.89 to 2.14 Ga, and from 1.83 to 2.31 Ga, respectively. Whole-rock geochemistry and Hf isotope analysis indicate that the Helong granites experienced a high degree of differentiation and evolution derived by partial melting of the Late Paleoproterozoic crustal materials, and they formed in a backarc caused by low-angle subduction of the Paleopacific plate.

1. Introduction

The Nanling Range is one of the world’s largest W–Sn metallogenic provinces in the South China Block [1], which hosts the majority of the mineralization with about 9.943 million tons of WO3 and 6.561 million tons of Sn [2]. The eastern Nanling Range, (southern Jiangxi Province) presents a high density of W-dominant deposits with diverse metal associations (Sn, Mo, Bi, Cu, Ag, Sb, Hg, and rare earth elements), which are thought to be closely related to Mid-Late Mesozoic composite plutons (Figure 1) [2,3,4,5,6]. High-silica granites, associated with W-dominant and rare-metal deposits in southern Jiangxi, belong to high-K calc-alkaline and weakly peraluminous series, with pronounced negative Eu anomalies and are highly fractionated [7,8,9,10,11,12,13,14,15,16]. Previous studies have shown that the W–Sn-related granites in southern Jiangxi Province mostly resulted from partial melting of Mesoproterozoic to Paleoproterozoic crustal materials [1,17,18,19,20]. However, the dynamic background of the granitic plutons remains controversial, including two perspectives: (1) related to the syn-collision to post-collision stages after the closure of Paleotethys in the Early Yanshanian [21,22,23,24], (2) related to the back-arc extension associated with Paleopacific subduction in the Middle-Late Jurassic [25,26,27,28,29].
The Helong ore field, with W–Sn reserves of 15,000 tons and 9500 tons, respectively, is one of the W–Sn metallogenic prospects in southern Jiangxi Province (Figure 1) [29,30]. Many deposits in the Helong ore field formed during the Late Jurassic, as shown by recent wolframite and cassiterite U–Pb, molybdenite Re–Os, and mica Ar–Ar dating (ca. 160–150 Ma) [5,6,29,31]. The consistent isotope ages between the W–Sn deposits and the adjacent granites indicate a genetic link between them. However, the petrogenesis, chemical composition, and dynamic background of these Late Jurassic granites remain to be unclear.
In this paper, we present a detailed study on the petrology, mineralogy, whole-rock major and trace elements, and zircon U–Pb–Hf characteristics of the Jinzhuping and Changkeng granites in the Helong ore field. Combined with the corresponding published data, we constrain the petrogenesis of the Jinzhuping and Changkeng granites, and furthermore discuss the dynamic background of the plutonism in the southern Jiangxi Province.

2. Geological Setting of the Helong Ore Field and Petrology of the Granites

2.1. Geological Setting

The Helong orefield is located in Jiangxi Province, South China (Figure 1); geologically, the orefield is located in the Nanling tungsten belt [2,29]. The Nanling tungsten belt overlaps the EW-trending Nanling Range, which is composed of the Yuecheng, Doupang, Mengzhu, Qitian, and Dayu mountain belts that separate the Yangtze River and Zhujiang River systems [2]. Except for some scattered Late Triassic deposits, Late Jurassic deposits are the main W and Sn deposits in the Nanling tungsten belt [2,6,18,32,33,34,35,36]. Most granites in the region were formed coevally with the Late Jurassic W–Sn deposits, which occurred at a peak of ca. 160 to 150 Ma [5,6,28,33,34,35].
The Helong orefield is hosted in the junction of the E-W-trending complex structure belt of the middle and eastern Nanling region and the NNE-SSW-trending Wuyi uplifted zone [29]. Stratigraphic sequences exposed in the orefield include Chinese stage for the Sinian to Cambrian marine clastic rocks that are low-grade metamorphosed and extremely thick, Devonian to Permian marine to continental clastic and carbonate rocks, and Jurassic to Tertiary continental clastic rocks [29]. Mesozoic granites are dominant in the orefield, including the Dabu composite pluton, and many minor intrusions such as the Tieshanlong, Anqiantan, Jinzhuping, and Changkeng granites (Figure 2) [29,30]. These igneous rocks were mainly intruded during two periods, i.e., the Caledonian (ca. 423–430 Ma) and the Late Mesozoic (ca. 161–153 Ma) [29,37,38,39]. The W-polymetallic ore deposits associated with the Late Jurassic granites, which take the form of quartz vein, porphyry, skarn, and greisen type, are the Laikeng, Tongziping, Niushikeng, Changkeng, and Jinzhuping deposits, as shown in Figure 2. Importantly, the Jinzhuping and Changkeng granites have been associated with the W-dominant deposits in time, space, and genesis in the Helong orefield [5,6,29].
Drill cores show that the main phase of Jinzhuping granites is medium- to coarse-grained biotite granite, which intrudes into the Cambrian metamorphic clastic rocks and hosts most of the ore bodies of the Jinzhuping deposit [5]. The main-phase granite (Figure 3A–E) is replaced by porphyritic biotite granite in the top (Figure 3F–H) and cut through by aplite (Figure 3I–K). The Changkeng granite consists predominantly of the main-phase biotite granite (Figure 3L–N), and in this ore deposit, the quartz-wolframite veins occur directly within the Sinian metasandstone and slate [29]. Detailed petrological descriptions of the four granites are presented in the next section.

2.2. Petrology of the Ore-Hosting Granites

2.2.1. The Jinzhuping Granites

The main-phase granite occupies about 90% of the total pluton, while the porphyritic granite is mostly distributed in the top zone of the pluton, occupying about 6% of the total pluton (Figure 3A–F). The aplite that cuts through the main-phase granite (Figure 3I) is only visible in part of the drill cores, with a very small percentage. W–Sn mineralization occurs mainly in the main-phase granite (Figure 3D–E), followed by porphyritic granite, but no mineralization is found in aplite.
The main-phase granites are dominated by medium- to coarse-grained biotite granite (Figure 3A–C), and consist mainly of alkali feldspar (25–30 vol%), plagioclase (25–30 vol%), quartz (25–38 vol%), biotite (5–8 vol%), and muscovite (0–4 vol%) with accessory magnetite, zircon, apatite, ilmenite, titanite, hematite, and fergusonite. Hydrothermal minerals (mainly wolframite, cassiterite, chalcopyrite, pyrite, and scheelite) are widespread. Quartz is mainly present as anhedral grains (Figure 3B–C). K-feldspars are mainly subhedral granular perthite potassium feldspar, and they generally include fine-grained anhedral quartz (Figure 3B). Plagioclase is euhedral to subhedral (Figure 3C), and enclosed abundant tiny sericite. The biotite is euhedral to subhedral and coexists with K-feldspar and quartz (Figure 3C).
The texture varies into porphyritic in the top of the main-phase granite and the porphyritic granite is grayish white (Figure 3F). Abundant potassium feldspar megacrysts, usually euhedral to subhedral, are embedded in a moderately coarse groundmass of feldspars and quartz, and enclose abundant biotite and quartz (Figure 3G). The irregular or rounded quartz grains may reach 6 mm in diameter (Figure 3G). The flakes of muscovite, frequently clustered together, and enclose euhedral to subhedral garnet. The porphyritic biotite granite consists mainly of alkali feldspar (27–32 vol%), plagioclase (22–30 vol%), quartz (23–36 vol%), biotite (4–6 vol%), and varying muscovite (0–2 vol%) with accessory zircon, apatite, hematite, and fergusonite.
The aplite is mainly fine grained, light grey to light red (Figure 3I), and mainly comprises quartz (35–38 vol%), K-feldspar (40–45 vol%), plagioclase (15–18 vol%), biotite (3–5 vol%), and garnet (1–4 vol%), with accessory zircon, limonite, ilmenite, and cassiterite. Quartz is mainly present as subhedral to anhedral grains (Figure 3J–K). K-feldspar is mainly subhedral granular perthite, and it generally includes fine-grained euhedral plagioclase and tiny muscovite and is altered by clay minerals (Figure 3K). Plagioclase is euhedral to subhedral. The euhedral to subhedral garnets mostly occur interstitially between K-feldspar and quartz (Figure 3K). Muscovite is mostly present as subhedral fine- to medium-grained flakes.

2.2.2. The Changkeng Granite

The main-phase granite is dominated by medium- to coarse-grained biotite granite (Figure 3L) and consist mainly of K-feldspar (20–25 vol%), plagioclase (20–25 vol%), quartz (30–35 vol%), biotite (5–9 vol%), and muscovite (0–2 vol%) (Figure 3M–N) with accessory zircon, garnet (Figure 3N), titanite, and fluorite. Quartz is mainly present as anhedral grains (Figure 3M–N). K-feldspars are subhedral to anhedral, and generally, altered by chlorite and clay minerals (Figure 3M–N). Plagioclase is euhedral to subhedral (Figure 3M), and encloses abundant tiny sericite. The mainly subhedral biotite mostly occurs interstitially between K-feldspar and quartz (Figure 3M). Muscovite is mostly present, enclosed in K-feldspar as fine-grained flakes or occurs interstitially between biotite and quartz (Figure 3M). The subhedral to anhedral garnet mostly occurs interstitially between K-feldspar and quartz (Figure 3N).

3. Samples and Analytical Methods

3.1. Sampling

Samples of main-phase granite, porphyritic granite, and aplite in the Jinzhuping deposit, i.e., JZP-6, JZP-12, and JZP-33, for zircon U–Pb dating and Hf isotopes analyses were collected from drill core Zk4105 at depths of 525 m, 430 m, and Zk3305 at 610 m, respectively. Samples of the four granites, i.e., from JZP60-1 to JZP60-8, from JZP61-1 to JZP61-6, from JZP62-1 to JZP62-7, and from CK60-1 to CK60-7 for whole rock major and trace element analyses were collected from different depths of drill core Zk4105, Zk3305, Zk3301 in Jinzhuping, and Zk311 in Changkeng, respectively.

3.2. Whole Rock Major and Trace Element Analyses

The major and trace element analysis for the bulk rock samples was mainly carried out in the Yanduzhongshi Geological Analysis Laboratories Ltd. (103 Beiqing Road, Haidian District, Beijing). First, fresh samples were 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 1250 °C using a V8C automatic fusion machine produced by the Analymate Company in China. The bulk rock’s major elements were analyzed using X-ray fluorescence spectrometry techniques (Zetium, PANalytical, or XRF-1800, Shimadzu). The analytical errors for major elements were better than 1%. For trace element analysis, first, sample powders were dissolved using distilled HF + HNO3 in a screw-top Teflon beaker for 4 days at 100 °C. The 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 trace elements in the GSR-2 standard are all consistent with their recommended values.

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

The zircon U–Pb isotope analysis was carried out in situ by using a NWR193 laser-ablation microprobe (Elemental Scientific Lasers LLC), attached to a Analytikjena M90 at the Yanduzhongshi Geological Analysis Laboratories Ltd. In order to adjust sensitivity, helium was used as a carrier gas and argon gas was used as a compensation gas during the laser ablation process, and both were mixed by a Y-shaped junction before entering ICP. Every time-resolved analysis includes an approximately 20–30 s blank signal and a 40 s sample signal. Off-line processing of data was completed using the software ZSkits, including selection of samples and blank signals, drift correction of instrument sensitivity, calculations for elemental contents, and U–Th–Pb isotope ratios and ages.
Isotopic fractionation correction for U–Pb dating was carried out using zircon standard 91500 as an external standard. When 5–10 sample points were completed, 91500 was analyzed twice using one Plesovice analytical point as a monitor. The calculation of weighted average ages and plotting of the concordia diagram were completed with Isoplot/Ex_ver3 [40], and the common lead adjustment was conducted using the Andersen software [41]. According to the actual situation, the tested denuded diameter was selected as 30 μm. The standard sample 91500 and Plesovice both coincided with values recommended [42,43].

3.4. In Situ Zircon Hf Isotopic Analyses

Zircon Lu–Hf isotope analysis was carried out in situ by using a NWR193 laser-ablation microprobe (Elemental Scientific Lasers LLC), attached to a Neptune multicollector ICP-MS at the Yanduzhongshi Geological Analysis Laboratories Ltd. Instrumental conditions and data acquisition were comprehensively described by Wu et al. [44]. For the current analyses, a stationary spot with a beam diameter of 40 μm was used. Helium was used as carrier gas to transport the ablated sample from the laser-ablation cell to the ICP-MS torch via a mixing chamber mixed with argon. In order to correct the isobaric interferences of 176Lu and 176Yb on 176Hf, 176Lu/175Lu = 0.02658 and 176Yb/173Yb = 0.796218 ratios were determined (e.g., Chu et al. [45]). For instrumental mass bias correction, Yb isotope ratios were normalized to 172Yb/173Yb of 1.35274 (e.g., Chu et al. [45]) and Hf isotope ratios to 179Hf/177Hf of 0.7325 using an exponential law. The mass bias behavior of Lu was assumed to follow that of Yb, and mass bias correction protocol details were described by Wu et al. [44]. Zircon 91500 and Plesovice were used as the reference standards during our routine analyses. Initial 176Hf/177Hf ratios εHf (t) were calculated with reference to the chondritic reservoir (CHUR) of Blichert-Toft and Albarede [46] at the time of zircon growth from the magma. The single-stage Hf model age (TDM1) was calculated relative to the depleted mantle with present-day 176Hf/177Hf = 0.28325 and 176Lu/177Hf = 0.0384 (e.g., Griffin et al. [47]).

4. Results

4.1. Whole-Rock Major and Trace Element Compositions

The whole-rock major and trace elements were measured in 28 samples from Helong granites and the results are given in Table 1. All granites have very high SiO2 contents in the range 73.99%–77.68% (Figure 4A) and very similar geochemical characteristics. The Helong granite plots in the high-K field in terms of K2O vs. SiO2 (Figure 4B), and the granites are weakly to strongly peraluminous, with A/CNK values from 0.92 to 1.13 (Figure 4). In the Harker diagrams (Figure 5), they show similar geochemical trends. In the REE and trace element distribution patterns (Figure 6), they are most depleted in LREEs and Eu, but are enriched in HREEs, while the chondrite-normalized REE patterns of most porphyritic granite samples are nearly flat. Specifically, the Changkeng granite has lower Eu/Eu* ratios (0.03–0.05) relative to the Jinzhuping granites (the main-phase granite 0.01–0.09, the porphyritic granite 0.01–0.13, and the late-stage aplite 0.03–0.16), while the Jinzhuping porphyritic granite has higher (La/Yb)N values (from 0.14 to 1.04) relative to the Jinzhuping main-phase granite (from 0.08 to 0.48), the Jinzhuping late-stage aplite (from 0.13 to 0.21), and the Changkeng granite (from 0.16 to 0.47). In addition, the depletion in Eu in the Jinzhuping main-phase granite is stronger than that in the other granites, while the intensities of the depletions in Ba, Sr, P, and Ti were almost uniform in all granites.

4.2. LA-ICP-MS Zircon U–Pb Ages

Most of the zircon crystals selected from samples of JZP-6, JZP-12, and JZP-33 are short columnar, euhedral to subhedral, 60–180 μm long, and yield length/width ratios from 1:1 to 4:1. Most zircons are euhedral to subhedral, have well-developed oscillatory cathodoluminescence (CL) zoning (Figure 7), and are colorless to dark (most of samples JZP-6 and JZP-12) to dark and opaque (most of sample JZP-33). The age for each sample is given as the error-weighted mean of the common Pb-corrected 206Pb/ 238Pb ages of the selected grains at the 95% confidence level. The LA-ICP-MS U–Pb zircon geochronology results for two dated samples are presented in Table 2, and U–Pb concordia diagrams are given in Figure 8.
Twenty-two zircon grains from sample JZP-6 were examined, and their U and Th concentrations varied from 118.2 to 20583.2 ppm (mean 3985.5 ppm) and from 66.5 to 1801.3 ppm (736.3 ppm), respectively, and the U/Th ratios varied from 1.1 to 10.8 (Table 2). These characteristics indicate a magmatic origin for the zircon grains. Sixteen spots of the zircon grains (from JZP-6-6 to JZP-6-22) were used, because the other six analyses yielded very high-U contents that would result in inaccurate U–Pb age calibrations [51]. These analyses yielded a concordant age of 155.2 ± 0.68 Ma (MSWD = 0.8) (Figure 8A), which coincided well with the weighted mean 206Pb/238U age of 155.5 ± 1.3 Ma (MSWD = 0.96) (Figure 8B). This age represents the crystallization age of the main-phase biotite granite.
Twenty-two zircon grains from sample JZP-12 were examined, and their U and Th concentrations varied from 80.6 to 482.9 ppm (mean 246.1 ppm) and from 54.4 to 318.6 ppm (154.6 ppm), respectively, and the U/Th ratios varied from 0.9 to 2.4 (Table 2). These characteristics indicate a magmatic origin for the zircons. These analyses yielded a concordant age of 154.0 ± 0.56 Ma (MSWD = 4.3) (Figure 8C), which coincided well with the weighted mean 206Pb/238U age of 153.8 ± 1.1 Ma (MSWD = 0.6) (Figure 8D). This age represents the crystallization age of the porphyritic biotite granite.
Zircons from the fine-grained granite (JZP-33) typically have rugged surfaces, contain microfractures, and are characterized by strikingly high U (2954.8–35794.6 ppm) and Th (152.4–4008.8 ppm), with U/Th = 6.8–68.4 (Table 2). The high U and Th contents indicate that zircons of JZP-33 were magmatic in origin, but suffered metamictization after crystallization. Seventeen spots were selected for analysis (from JZP-33-17 to JZP-33-30), and most of them showed discordant ages due to the metamictization of zircons. The 17 discordant spots yielded a lower intercept age of 153.4 ± 0.99 Ma (MSWD = 0.43) (Figure 8E), which coincided well with the weighted mean 206Pb/238U age of 154.6 ± 1.3 Ma (MSWD = 0.27) (Figure 8F). This age represents the upper limit of the crystallization age.

4.3. Zircon Hf Isotopes

The zircon Hf isotope determination points were the same sites as the zircon U–Pb measurements. The data from the fifty measured spots of the Jinzhuping granite samples are shown in Table 3 and plotted on Figure 9. The Hf isotopic analyses for 15 zircon grains from the main-phase biotite granite (sample JZP-6), with initial 176Hf/177Hf ratios varying from 0.282292 to 0.282406, yield εHf(t) values from −14.2 to −10.4. The Hf isotopic analyses for 18 zircon grains from the porphyritic biotite granite (sample JZP-12), with initial 176Hf/177Hf ratios varying from 0.282257 to 0.282370, yield εHf(t) values from −15.3 to −11.4. There are 17 spots for the aplite (Sample JZP-33), providing initial 176Hf/177Hf ratios of 0.282190−0.282410, corresponding to an εHf(t) from −18.1 to −10.5. Their two-stage Hf model ages (TDM2) range from 1.83 to 2.06 Ga, from 1.89 to 2.14 Ga, and from 1.83 to 2.31 Ga, respectively.

5. Discussion

5.1. Geochronology of the Helong Granites

The “high-U effect” of zircon grains has been known for many years, and may lead to uncertainties in age results and greater discordance in the concordia diagram than normal zircons using the U–Pb method [52,53,54]. It is likely to be caused by radiogenic damage to the crystal lattice and subsequent alteration of zircon grains [55]. Many works have been done on the metamict effect of zircon grains with high U and Th. The physical properties of zircon grains, such as an increase in solubility and becoming opaque, could be affected by radioactive damage [56,57]. The “high-U effect” attributed to enhanced ionization of Pb results in a positive correlation between the apparent ages and the U or U/Th contents of zircon grains [54,58,59], but not all high-U zircon grains yield anomalously old U–Pb dates [60], in some cases the positive correlation may be slight or in existence [54].
More than half of zircon grains from the Jinzhuping main-phase granite have high uranium and thorium concentrations (more than 2500 μg/g and 1100 μg/g) that may lead to uncertainties in age. All the grains show no correlation between U and apparent age. Except for some zircon grains with high-U contents that have weakly older ages (ca. 160 Ma), the other grains show very close ages (ca.152–158 Ma), and yield a well weighted mean 206Pb/238U age (155.5 ± 1.3 Ma) (Figure 8B). Therefore, the main-phase granite of the Jinzhuping pluton was crystallized at ca. 152 to 160 Ma. The porphyritic biotite granite, formed by the structural change of the main-phase granite, has low uranium and thorium concentrations, and then their close ages of zircon grains from ca. 151 to 157 Ma present their crystallization ages. Zircon grains from the late-stage Jinzhuping aplite are characterized by high uranium and thorium concentrations, but there is no correlation between U and apparent age. Most of the zircon crystals are altered by hydrotherm (as shown in Figure 7), and thus, the lower intercept age of 153.4 ± 0.99 Ma should be the upper limit of the crystallization age. The 17 discordant spots used to yield weighted mean age for the aplite show an age range from ca. 150 Ma to 157 Ma, and are considered to be the age of hydrothermal activities after the emplacement of this igneous rock.
Previously published age data for the Helong granites have been zircon U–Pb isotope ages, which are ca. 159 Ma for the Jinzhuping porphyritic biotite granite and ca. 157 Ma for the Changkeng biotite granite [29,31]. In our study, precise LA-ICP-MS zircon U–Pb dates, within the error, obtained for the main-phase biotite granite, porphyritic biotite granite, and the aplite of the Jinzhuping deposit, are consistent, suggesting that the Helong granites were emplaced within a very short period, i.e., from ca. 150 Ma to 159 Ma.

5.2. Granite Sources

According to the studies of Sylvester [61], peraluminous granite formed by partial melting of source materials with different compositions will result in different CaO/Na2O ratios. The CaO/Na2O ratio of granites formed from mudstone (<0.3) is lower than that of granites formed from clastic rocks. In the Rb/Sr-Rb/Ba diagram (Figure 10A), the Helong granites in southern Jiangxi Province mainly fall into the clay-rich source area, and in the Rb/Sr-CaO/Na2O diagram (Figure 10B), they fall into the argillite source region. Su et al. [28] suggested that the granitoids related to W–Sn deposits in the southern Jiangxi Province mainly formed from argillaceous rock rich in clay. This conclusion also supports the interpretation that the Helong granites were derived from the fertile crustal source.
The variations of composition and the correlation of elements in Harker diagrams (Figure 5) indicate that the Helong granites probably derived from homogeneous sources. The 176Hf/177Hf values of the Jinzhuping granites fall around the line of the lower crust (Figure 9A,B), which is same with the Changkeng granite [29], indicating that the Helong magma was derived from the lower crust. Hf two-stage model TDM ages (1.83–2.31 Ga) indicate that the Jinzhuping granites may have resulted from the Paleoproterozoic crustal materials, which is consistent with the source of Changkeng granite [29]. Therefore, the Helong granites derived from partial melting of the Late Paleoproterozoic crustal materials. Low εHf(t) values from −18.1 to −10.1 with an average value of −12.8 for Jinzhuping granites, and from −14.1 to −11.1 with an average value of −12.9 for Changkeng granite [29] (Figure 9) indicate that possibly there was no involvement of mantle-derived materials.

5.3. Degrees of Fractional Crystallization of Helong Granites

The Helong granites are rich in Rb, Th, U, Nb, Ta, Nd, and Sm. Strong depletions in Eu, Ba, Sr, P, and Ti prove that crystallization of plagioclase, apatite, and Ti–Fe oxides occurred during their formation (Figure 6).
The Jinzhuping main-phase granite has the strongest depletions in Eu, P, Ti, and Sr in the four granites (Figure 6). The average Sr contents of Changkeng and Jinzuping granites (from the main-phase, porphyritic to aplite) increase from 11.1 to 11.2 to 15.9 to 17.5 μg/g. The average Ba contents of the four granites are 19.6, 10.1, 30.8, and 18.0 μg/g, respectively. The K/Rb ratio can reflect the degree of magma differentiation evolution, and a low K/Rb ratio is usually one of the important characteristics of highly evolved magmatic systems [62,63,64]. The K/Rb ratios of the Helong ore-hosting granites are all low, with average values of 84.15, 63.43, 60.76, and 64.84, respectively. The Zr/Hf ratio of rocks indicates the evolution degree of magmatic system and whether fluid metasomatism has occurred. The Zr/Hf ratio of granites decreases with increasing degree of evolution or fluid metasomatism [62,63]. The average Zr/Hf ratios of the four granites are 13.14, 12.02, 15.05, and 11.28, respectively, which are significantly lower than those of ordinary granites (39) [28]. This result indicates that the Helong granites have undergone large-scale fluid metasomatism, in a similar way to what happened with granites from the granites in Southern Jiangxi Province [28]. On the basis of above evidences, the Helong granites experienced a high degree of differentiation and evolution, while the degree of the main-phase Jinzhuping granite is much higher than other granites.

5.4. Geodynamic Setting of the Helong Granites

There are close temporal, spatial, and genetic relationships between granitic rocks and intensive metallic mineralization in southern Jiangxi Province, Nanling Region in Mesozoic [2,4,5,6,29,65]. Research has shown that the Nanling area was in a lithospheric extensional environment in the early Yanshanian [35,65,66]. For example, Mao et al. [67] proposed that the magmatism and mineralization in East China dated at ca. 180–135 Ma formed within a continental magmatic arc, with widespread magmatism and back-arc extension caused by low-angle subduction of the Paleopacific plate. By comparing two sets of different metallogenic series and their related granites in Jurassic of Qinhang belt (Middle Jurassic porphyry-skarn-hydrothermal vein copper-gold polymetallic deposit and late Jurassic greisen-quartz vein-skarn W–Sn polymetallic deposit), Guo et al. [26] and Mao et al. [67] suggested that the large-scale diagenetic and metallogenic events in this belt were formed in the back-arc extensional environment related to the Pacific subduction.
Many Jurassic W–Sn granitic plutons including Helong, Baxiannao, Pangushan, Xihuashan, Taoxikeng, Jiulongnao, Baoshan, and Zhangdoukeng are located in the southern Jiangxi Province [5,9,10,11,13,29,68,69]. Su et al. [28] has recognized that, compositionally, these ore-hosting granites are high-K calc-alkaline; peraluminous; highly differentiated; enriched in Rb, U, and Th; depleted in Nd, Zr, Ti, Eu, Ba, Sr, and P; with low Al2O3, TiO2, MgO, P2O5 values; and probably formed during lithospheric thinning and crustal extension. For example, Fang et al. [38,69] suggested that the Pangushan granite crystallized from high-K calc-alkaline, from metaluminous to peraluminous and highly differentiated magmas, and formed in an intraplate extension environment. Many researchers believe that the Nanling area was in a lithospheric extensional environment in the early Yanshanian [27,33,35,65,66,70]. In conclusion, few W–Sn-related granites including Jinzhuping and Changkeng in the Helong orefield occurred within an extensional environment caused by Paleopacific subduction in the middle to late Jurassic.

6. Conclusions

(1)
The Helong granites include three different phases in the Jinzhuping ore deposit, i.e., main-phase biotite granite, porphyritic biotite granite, and aplite, as well as the Changkeng main-phase biotite granite.
(2)
LA-ICP-MS zircon U–Pb ages confirm that the Jinzhuping granites were emplaced in the Late Jurassic. The ages of main-phase biotite granite, porphyritic biotite granite, and aplite are 155.2 ± 0.68 Ma, 154.0 ± 0.56 Ma, and 153.4 ± 0.99 Ma, respectively.
(3)
Four granites were derived by partial melting of the Paleoproterozoic crustal materials, and they underwent high degrees of fractional crystallization.
(4)
Helong granites hosting W–Sn deposits in the Nanling W–Sn polymetallic metallogenic belt occurred within a backarc setting with significant lithosphere thinning, probably caused by low-angle subduction of the Paleopacific plate.

Author Contributions

Conceptualisation, W.S. and J.Z.; field investigation, X.Z., J.Y. and W.L.; methodology, X.L.; data curation, X.L. and J.Z.; writing—original draft preparation, X.L.; writing—review and editing, J.Z.; supervision, W.S. and J.Z.; funding acquisition, X.L. and J.Z.; All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by the National Key Research and Development Program of China (2021YFC2900100), the National Science Foundation of China (41702352), National Pre-research Funds of Hebei GEO University in 2023 (Grant 008), metallogenic regularities and prediction evaluation of strategic metal mineral resources such as lithium and beryllium in eastern China (2019YFC0605202), and mineral geology survey and prospecting prediction in an integrated exploration area (No. DD29190166-2020-08).

Data Availability Statement

All the data are presented in the paper.

Acknowledgments

The authors would like to acknowledge the three anonymous reviewers for their constructive comments, which helped to significantly improve the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Distribution map of granitoids and major Mesozoic W–Sn deposits in Nanling region (modified from [4]).
Figure 1. Distribution map of granitoids and major Mesozoic W–Sn deposits in Nanling region (modified from [4]).
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Figure 2. Geological map of the Helong ore field (modified from [5]).
Figure 2. Geological map of the Helong ore field (modified from [5]).
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Figure 3. Photographs showing mineral composition of granites associated with the Jinzhuping (A–K) and Changkeng (L–N) ore deposits. (A–C) Medium- to coarse-grained biotite granite; (D–E) potash feldspathization, greisenization, and wolframite-quartz vein in the main-phase granite; (F–H) porphyritic biotite granite; (I–K) aplite; (L–N) mineral composition of biotite granite, and the K-feldspar replaced by chlorite. Q—quartz; Pl—plagioclase; Kfs—potassium feldspar; Bt—biotite; Ms—muscovite; Grt—garmet; Chl—chlorite.
Figure 3. Photographs showing mineral composition of granites associated with the Jinzhuping (A–K) and Changkeng (L–N) ore deposits. (A–C) Medium- to coarse-grained biotite granite; (D–E) potash feldspathization, greisenization, and wolframite-quartz vein in the main-phase granite; (F–H) porphyritic biotite granite; (I–K) aplite; (L–N) mineral composition of biotite granite, and the K-feldspar replaced by chlorite. Q—quartz; Pl—plagioclase; Kfs—potassium feldspar; Bt—biotite; Ms—muscovite; Grt—garmet; Chl—chlorite.
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Figure 4. Pl SiO2 vs. K2O diagram (A) and A/NK vs. A/CNK diagrams (B) of the Helong granities (the compositional fields are from Rollinson [48] and Streckeisen and Le Maitre [49], respectively).
Figure 4. Pl SiO2 vs. K2O diagram (A) and A/NK vs. A/CNK diagrams (B) of the Helong granities (the compositional fields are from Rollinson [48] and Streckeisen and Le Maitre [49], respectively).
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Figure 5. Harker diagrams for the Helong granites. Symbols as in Figure 4.
Figure 5. Harker diagrams for the Helong granites. Symbols as in Figure 4.
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Figure 6. Chondrite-normalized REE patterns and element diagrams for the Jinzhuping granites (A–C), and the Changkeng granite (D). Normalization values are from Sun and McDonough [50].
Figure 6. Chondrite-normalized REE patterns and element diagrams for the Jinzhuping granites (A–C), and the Changkeng granite (D). Normalization values are from Sun and McDonough [50].
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Figure 7. Cathodoluminescence (CL) images of zircon crystals from the Jinzhuping pluton.
Figure 7. Cathodoluminescence (CL) images of zircon crystals from the Jinzhuping pluton.
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Figure 8. LA-ICP-MS U–Pb concordia diagrams and weighted mean 206Pb/238U ages of zircon in the Jinzhuping medium to coarse-grained biotite granite (A,B), porphyritic biotite granite (C,D) and aplite (E,F).
Figure 8. LA-ICP-MS U–Pb concordia diagrams and weighted mean 206Pb/238U ages of zircon in the Jinzhuping medium to coarse-grained biotite granite (A,B), porphyritic biotite granite (C,D) and aplite (E,F).
Minerals 13 00101 g008
Minerals 13 00101 g009 550
Figure 9. εHf(t) vs. age plots (A) and 176Hf/177Hf vs. age plots (B) for the Jinzhuping zircons.
Figure 9. εHf(t) vs. age plots (A) and 176Hf/177Hf vs. age plots (B) for the Jinzhuping zircons.
Minerals 13 00101 g009
Minerals 13 00101 g010 550
Figure 10. The Rb/Sr-Rb/Ba diagram (A) and the Rb/Sr-CaO/Na2O diagram (B) of the Helong granites. Symbols as in Figure 4.
Figure 10. The Rb/Sr-Rb/Ba diagram (A) and the Rb/Sr-CaO/Na2O diagram (B) of the Helong granites. Symbols as in Figure 4.
Minerals 13 00101 g010
Table
Table 1. Major and trace element compositions of the Helong granites.
Table 1. Major and trace element compositions of the Helong granites.
Sample NumbersJZP-60-1JZP-60-2JZP-60-3JZP-60-5JZP-60-6JZP-60-7JZP-60-8JZP-60-9JZP-61-1JZP-61-2JZP-61-3JZP-61-5JZP-61-6JZP-61-8JZP-62-1JZP-62-2JZP-62-3JZP-62-5JZP-62-6JZP-62-7JZP-62-8CK-60-1CK-60-3CK-60-4CK-60-5CK-60-6CK-60-7CK-60-8
SiO276.3375.9673.9975.6875.9275.7276.3375.5776.876.4575.0276.5876.5675.5177.0176.9277.1575.375.3376.4776.3677.6876.3776.0776.1976.4676.476.07
TiO20.010.020.020.010.020.020.020.010.020.030.010.010.020.010.020.020.010.010.020.010.010.020.0100.01000
Al2O313.0313.0712.2612.7312.9113.1612.7713.112.8712.6412.8213.2613.2813.0312.612.512.8612.912.8613.0212.9312.0812.5912.7612.6912.4712.1912.64
TFe2O30.990.841.070.751.290.820.660.630.980.960.870.750.740.860.820.80.670.620.630.690.690.370.920.830.460.771.140.87
MnO0.060.160.270.140.10.360.220.090.080.080.10.190.190.10.620.620.240.10.10.220.220.150.280.10.160.090.180.13
MgO0.070.140.080.140.140.080.080.140.140.130.120.060.070.110.110.10.070.150.130.070.070.080.090.10.080.080.080.09
CaO0.580.851.640.850.620.550.580.830.790.770.850.630.620.850.750.760.611.091.10.560.560.420.590.70.570.660.580.67
Na2O3.583.693.193.843.474.53.62.923.713.72.994.384.3734.094.14.143.33.283.953.93.613.673.793.883.712.863.77
K2O5.184.434.763.994.923.824.884.94.44.395.523.993.995.543.713.74.014.264.294.544.524.824.554.464.794.554.854.53
P2O50.030.030.030.030.030.030.030.030.040.030.030.030.030.030.030.030.030.030.030.030.030.030.030.030.030.030.030.03
LOI0.651.092.011.580.710.691.021.540.630.671.220.590.631.270.660.680.631.891.970.690.720.730.821.0311.111.30.9
TOTAL100.5100.2899.3199.73100.1499.74100.1999.76100.4599.8499.55100.47100.5100.31100.42100.22100.4399.6699.73100.2599.9999.9899.9499.8899.8699.9499.6199.68
A/CNK1.041.050.921.051.061.051.041.131.051.031.031.051.051.041.041.031.051.071.071.051.051.011.051.041.011.021.111.03
Rb525 500 699 523 530 604 608 656 503 499 675 619 615 670 461 468 521 552 559 577 583 440 428 488 447 486 479 434
Ba16.6418.348.8912.224.912.135.4511.8447.5645.6636.334.964.837.7141.8849.778.1311.5212.26.466.3128.3612.8919.928.1718.3715.7913.52
Th17.1826.4613.8915.3420.2312.0210.9513.522.3824.219.2814.4919.9318.1712.4612.7925.6414.7812.3321.5618.9514.1817.9619.8320.3923.8713.2620.27
U24.833028.2632.828.2834.4230.3227.6815.5219.514.8730.6534.6814.7131.3830.4237.6325.324.0932.9629.7927.628.9523.228.0126.7120.3628.74
Nb13.3512.6720.1810.9112.216.3416.449.9415.9515.7611.6511.7312.8111.438.689.1220.8214.9912.5216.1714.016.8911.7414.169.6311.6511.0412.65
Ta7.119.341.510.316.2312.2111.9810.038.356.866.6414.0617.446.635.35.1119.418.779.0210.8510.229.9311.159.19.867.8710.2510.56
K171.93 147.01 158.04 132.54 163.5 126.69 162.06 162.55 146.07145.65 183.31 132.39 132.5 183.83 123.28 122.99 133.05 141.55 142.39 150.67 150.11 159.95 151.24 148.2 159.09 151.11 161.11 150.43
La6.246.485.114.493.324.26.544.961010.176.494.454.96.316.356.696.473.953.55.626.143.25.277.394.45.785.125.14
Ce17.0817.2318.1712.0210.051019.3912.0724.2324.3416.6512.0213.0616.1914.4915.7820.6611.4610.2416.4517.237.7914.4619.110.7615.313.2613.24
Sr9.1623.216.4116.717.044.025.4211.4128.2427.3716.033.984.1615.6927.8128.18.3921.7522.37.197.0110.9810.9513.2910.113.458.9510.02
P117 130 142 126 122 129 120 143 156 147 137 131 136 133 116 126 138 121 122 131 121
Nd13.3512.6720.1810.9112.216.3416.449.9415.9515.7611.6511.7312.8111.438.689.1220.8214.9912.5216.1714.016.8911.7414.169.6311.6511.0412.65
Zr81.48114.1153.4482.478.0786.2867.7374.7364.6880.3774.21132.67142.3170.3774.0175.84112.4279.445.17113.8890.6575.2985.2676.6186.5872.2775.9270.6
Hf5.68.24.637.167.467.546.115.894.655.254.5410.7311.784.549.099.449.116.253.769.076.896.146.575.46.215.645.815.54
Sm5.594.6712.25.417.212.938.315.224.894.724.116.747.364.163.123.3514.6111.058.039.57.634.035.326.284.625.074.636.8
Eu0.070.150.040.040.050.020.020.050.230.20.160.030.030.170.210.190.030.050.050.030.020.060.060.10.060.080.060.08
Ti65.3397.0998.8985.71113.28104.2998.8982.11122.27150.4477.3288.789.972.52148.04116.2755.1464.7391.767.1384.5198.2941.369.5967.7310.1917.9815.58
Gd6.285.913.947.18.895.9710.387.235.545.215.239.179.645.075.335.3416.8313.719.9812.249.566.17.027.326.386.75.838.48
Dy13.5414.0327.5317.8719.326.2925.215.1210.359.4110.5522.9125.7610.4523.4323.5334.3824.321926.7121.7913.8419.4714.5715.313.5812.9317.82
Er8.4812.6317.5912.3612.2724.4717.549.346.345.876.3416.8918.876.4221.4321.7819.6712.2710.6217.8115.838.9916.38.9710.738.849.1411.13
Yb9.3421.4823.0815.0415.313723.159.437.277.027.4121.8324.577.436.0336.3626.3713.8112.923.2621.911.8923.211.3213.2110.0812.6113.73
Lu1.584.083.982.792.966.964.021.571.281.241.273.924.311.316.676.824.72.42.224.133.882.094.131.922.431.682.242.39
Y92.42130.56216.72142.01156.3262.24200.71116.5774.3572.1674.21179.87197.3771.09247.88254.37260.87135.6121.28207.22181.32110.51176.19109.58120.05107.27108.64131.81
Pr2.672.563.152.0621.393.041.963.193.182.372.122.312.311.982.123.462.362.032.832.671.252.232.861.862.262.142.3
Tb1.81.793.692.292.652.623.152.211.421.291.362.883.211.372.32.284.883.432.813.42.871.912.32.091.981.931.72.48
Ho2.893.546.014.014.076.825.633.382.1822.185.325.952.26.256.316.754.543.715.794.913.34.893.283.513.183.13.76
Tm1.442.913.22.382.435.123.311.51.111.051.113.163.51.134.714.743.622.191.983.293.171.793.171.712.091.561.832.1
∑REE183 241 375 241 259 402 347 201 168 164 151 303 334 147 389 399 444 256 221 354 313 184 296 211 207 195 194 234
Eu/Eu*0.040.090.010.020.020.010.010.020.130.120.110.010.010.110.160.140.010.010.020.010.010.040.030.050.030.040.040.03
(La/Yb)N0.480.220.160.210.160.080.20.380.991.040.630.150.140.610.130.130.180.210.190.170.20.190.160.470.240.410.290.27
Th/U0.690.880.490.470.720.350.360.491.441.241.30.470.571.240.40.420.680.580.510.650.640.510.620.850.730.890.650.71
Ba/Rb0.030.040.010.020.0100.010.020.090.090.050.010.010.060.090.110.020.020.020.010.010.060.030.040.060.040.030.03
Rb/Sr57.3121.5742.6231.2975.27150.29112.0557.4917.8218.2242.1155.72147.9542.6916.5816.6462.0525.3825.0880.2183.1340.0639.0636.6944.2736.1653.5143.29
Sm/Nd0.420.370.60.50.590.460.510.530.310.30.350.570.570.360.360.370.70.740.640.590.540.580.450.440.480.440.420.54
Nd/Ta1.881.3613.481.060.750.521.370.991.912.31.760.830.731.721.641.791.071.711.391.491.370.691.051.560.981.481.081.2
Zr/Hf14.5613.9111.5311.510.4711.4411.0912.6913.915.316.3512.3712.0815.58.148.0412.3412.712.0212.5513.1512.2612.9714.1713.9312.8213.0612.75
K/Rb81.8573.4456.4963.3777.1552.4166.6961.9672.5872.9967.9153.4353.8568.6366.8465.7363.8664.163.6465.2964.3990.9386.6581.5684.4682.878.55
K/Ba2584 2003 4447 2712 8327 14867 7433 3431 768 797 1261 6677 6899 1219 736 618 4094 3072 2917 5831 5946 1410 2874 1998 1341 2192 2382
Table
Table 2. LA-ICP-MS zircon U–Pb dating results of the Jinzhuping granites.
Table 2. LA-ICP-MS zircon U–Pb dating results of the Jinzhuping granites.
Sample238U232Th238U/232Th207Pb/206Pb1sigma207Pb/235U1sigma206Pb/238U1sigma208Pb/232Th1sigma207Pb/Pb2061sigma207Pb/235U1sigma206Pb/238U1sigma208Pb/232Th1sigma
Nameμg/gμg/g Age (Ma) Age (Ma) Age (Ma) Age (Ma)
Main-phase granite
JZP-6-1673 257 2.70020.09310.00260.3210.00810.02510.00030.01660.00051490282836160233210
JZP-6-27718 1801 4.19530.06340.00140.22080.00860.02480.00060.01390.001722452037158427919
JZP-6-36097 823 4.03910.06040.0010.2090.00760.02520.0010.0120.0005618381936160624110
JZP-6-45591 1627 3.48590.05890.00280.20050.0090.02470.00040.00760.0001563108186815731543
JZP-6-57178 1573 5.19050.05420.00260.17810.00820.02380.00030.00740.0001381111166715221502
JZP-6-65241 901 5.89810.05270.00090.18020.00350.02470.00030.00970.000331721168315721947
JZP-6-720,583 1654 10.82750.04940.0020.16250.00590.02380.00040.00750.000116992153515221523
JZP-6-8293 238 1.29830.04880.00150.16070.00490.0240.00040.00820.000314040151415331656
JZP-6-9353 335 1.12470.05190.00210.17260.00780.02410.00060.00830.000228162162715431675
JZP-6-107375 886 8.62690.05050.00210.16790.0060.02410.00050.00760.000121896158515431533
JZP-6-11315 217 1.48280.05040.00270.1690.00940.02420.00060.00870.000321586159815441767
JZP-6-125164 1109 4.66790.04990.0020.16630.00570.02420.00050.00760.000119094156515431543
JZP-6-13172 94 1.80370.04980.00170.16430.00570.02420.00040.00750.000318652154515421526
JZP-6-14118 76 1.6380.04950.00310.16170.00930.02420.00050.00810.000417096152815431648
JZP-6-15231 132 1.80460.0490.00180.16370.00620.02420.00040.00850.000414956154515431729
JZP-6-167831 1346 5.92220.04820.00170.16110.00470.02420.00050.00770.000111180152415431553
JZP-6-173589 470 7.90020.05050.00240.17120.00740.02460.00040.00780.0002219110160615731564
JZP-6-18394 173 2.32040.04940.00160.16730.00520.02470.00040.00810.000316646157515721646
JZP-6-195691 702 8.24960.04960.00130.16980.00370.02480.00040.00790.000117464159315821582
JZP-6-20135 66 2.11320.04890.00260.16790.00920.02490.00050.00790.000414487158815831598
JZP-6-212644 1604 1.94770.04820.00370.16520.01140.02480.00080.00790.00021101721551015851594
JZP-6-22293 113 2.75140.05040.00180.17380.00610.02510.00040.00890.0005213541635160217910
Porphyritic granite
JZP-12-1423 277 1.52730.050.00130.16630.0050.0240.00040.00750.000219761156415321504
JZP-12-283 54 1.53010.04920.0030.16460.010.02460.00050.00740.0004156142155915631508
JZP-12-3151 123 1.22330.04940.00220.16190.00710.02390.00040.00740.0003167105152615221507
JZP-12-4203 88 2.30130.05010.00190.16880.00660.02450.00030.00870.000419890158615621757
JZP-12-5113 64 1.75320.05130.00220.16820.00720.02410.00050.00760.0005254991586153315411
JZP-12-6190 96 1.9810.05030.00190.16530.00620.0240.00040.00820.000420886155515321648
JZP-12-7110 56 1.9640.05180.00280.17330.00840.02460.00050.00760.00052761251627156315310
JZP-12-881 65 1.24270.050.00250.16050.00780.02370.00050.00780.0004196115151715131578
JZP-12-9227 183 1.24260.05110.00230.16910.00740.02420.00060.00760.00052431051596154415310
JZP-12-10291 123 2.36430.05030.00210.1690.00680.02440.00030.00790.000320798159615621597
JZP-12-11118 67 1.76850.050.00220.16540.00690.02420.00040.00820.00061941011556154316511
JZP-12-12311 192 1.62350.05030.00180.16720.00590.02410.00040.00830.000320782157515431685
JZP-12-13152 116 1.30380.04890.00240.16590.00830.02460.00040.00740.00051421131567157314911
JZP-12-14140 97 1.44280.05110.00250.17030.00850.02430.00050.00780.0004246114160715531578
JZP-12-15750 434 1.73040.04940.0010.16220.0040.02380.00030.00750.000316950153315221515
JZP-12-16104 101 1.03250.05030.00320.16180.01070.02360.00050.00710.0004210149152915131449
JZP-12-17293 148 1.98040.05130.00160.17230.00570.02440.00040.00760.000325374161515531536
JZP-12-18483 295 1.6390.05070.00120.16540.00420.02380.00030.00710.000322653155415121435
JZP-12-19414 319 1.29990.04880.00140.16510.00510.02460.00040.00750.000213667155415731515
JZP-12-20356 158 2.26040.04960.00250.16160.00760.02380.00060.00740.0004175118152715241498
JZP-12-21182 215 0.8470.050.00190.1670.00690.02460.00050.00780.000319689157615731566
JZP-12-22239 131 1.81960.05030.00220.16370.0070.02370.00040.00790.00052081011546151316010
Aplite
JZP-33-13926 255 15.40110.05440.0020.17930.00620.02390.00030.00750.000238785167515221504
JZP-33-211,616 905 12.83390.05270.00280.17790.00720.02450.00090.00770.0003317124166615651545
JZP-33-34525 235 19.23070.05250.00380.170.01110.02350.00070.00740.00043071651591015041487
JZP-33-45364 489 10.96790.05250.00070.17530.00250.02410.00030.00660.000330814164215421346
JZP-33-55856 338 17.33190.05870.00330.19110.01020.02360.00050.00730.0003556127178915031475
JZP-33-64296 427 10.0520.05590.00130.18740.00370.02430.00020.00760.000144751174315521532
JZP-33-75927 877 6.75980.0550.00350.180.01070.02370.00050.00740.0002412145168915131493
JZP-33-88268 931 8.87960.05480.00460.18280.01370.02420.00090.00760.00034041911701215461525
JZP-33-916,324 806 20.24140.05270.00060.17730.00560.02450.00080.01420.0006315331665156528511
JZP-33-1031,531 3344 9.42850.05370.00120.18050.00470.02460.00060.01280.0006357271684156425711
JZP-33-113897 497 7.84370.05650.00350.18770.01120.02410.00040.00750.00034711421751015431515
JZP-33-1215,528 1627 9.54360.05190.00220.17480.00610.02440.00060.00770.000228099164515641554
JZP-33-138352 632 13.20720.05330.00190.17730.00550.02410.00040.00760.000234383166515431523
JZP-33-1411,340 713 15.9160.05060.00140.16880.00350.02420.00040.00760.000222164158315431543
JZP-33-155043 406 12.42230.05090.00060.1720.00370.02440.00050.0070.000423422161315531408
JZP-33-167647 492 15.53150.05020.00260.16830.00790.02430.00050.00770.0003205121158715531545
JZP-33-174391 249 17.62630.04950.00140.16570.00350.02430.00040.00770.000117165156315531553
JZP-33-184715 479 9.84340.05130.00250.17350.00670.02450.00070.00770.0002254116162615651555
JZP-33-194496 210 21.43660.05060.00180.17110.0050.02460.00050.00770.000222086160415631564
JZP-33-205662 282 20.0550.05130.0020.17080.00530.02410.00060.00760.000225593160515441534
JZP-33-213820 152 25.05910.0510.00180.16930.00540.02410.00040.00760.000223984159515321534
JZP-33-2216,291 1343 12.12740.05060.00220.17190.00560.02460.00070.00780.0002225102161515741564
JZP-33-2330,986 4009 7.72950.05130.00060.17390.00370.02450.00050.00580.000325522163315631187
JZP-33-248695 696 12.49780.05080.00120.17140.00330.02450.00040.00770.000123357161315621552
JZP-33-2535,795 523 68.40890.05080.00060.16830.00410.02440.00060.01550.001232271584156431119
JZP-33-264079 224 18.2320.05160.00210.17450.0060.02450.00050.00770.000226696163515631555
JZP-33-274586 313 14.67070.05120.00150.17010.00420.02410.00030.00760.000224967160415421533
JZP-33-282955 282 10.49130.0490.00310.16390.00950.02430.00060.00770.0003146143154815541556
JZP-33-297740 456 16.98020.05090.00140.16750.0040.02390.00040.00750.000123667157315221512
JZP-33-3019,129 1464 13.06720.05080.00160.17010.00450.02430.00040.00770.000123173159415521543
Table
Table 3. In situ zircon Hf isotopic results of the Helong granites.
Table 3. In situ zircon Hf isotopic results of the Helong granites.
Samplet(Ma)176Yb/177Hf(corr)2σ176Lu/177Hf(corr)2σ176Hf/177Hf(corr)2σεHf(t)ErrorTDM (Ma)T2DM (Ma)
JK-6-001153.60.0518770.0004620.0014880.0000180.2823000.000016−13.90.613612046
JK-6-002157.20.0375880.0005740.0010980.0000160.2823420.000017−12.30.612891950
JK-6-0031540.0694770.0023470.0018400.0000510.2823230.000021−13.10.713421998
JK-6-004158.70.0677140.0010520.0020590.0000290.2823430.000015−12.30.513201951
JK-6-005154.70.1281230.0040760.0038600.0000600.2824060.000015−10.40.512931827
JK-6-006152.60.0482250.0008120.0013660.0000200.2823490.000027−12.21.012871937
JK-6-007153.80.0535230.0029420.0013880.0000730.2822920.000021−14.20.713692063
JK-6-008159.30.3674160.0114190.0095880.0002930.2823680.000024−12.20.816161947
JK-6-009154.30.0579020.0007350.0016110.0000270.2823710.000016−11.40.612641889
JK-6-010153.80.0260430.0003790.0007000.0000060.2823140.000016−13.30.613142011
JK-6-011161.30.1989310.0134310.0047770.0002970.2823320.000015−13.00.514431993
JK-6-012159.70.0447050.0019730.0011970.0000540.2823040.000018−13.60.613442031
JK-6-013155.10.0206400.0001350.0005860.0000050.2823110.000015−13.40.513142016
JK-6-0141550.0981740.0020050.0029400.0000440.2823080.000017−13.70.614052038
JK-6-015153.80.1484830.0047200.0042740.0001030.2823910.000015−11.00.513321863
JK-12-001153.10.0726490.0008670.0020160.0000140.2823670.000017−11.60.612851903
JK-12-002156.50.0262960.0010650.0007600.0000230.2823030.000017−13.60.613302032
JK-12-003152.40.0289960.0006110.0007870.0000140.2822970.000019−14.00.713402049
JK-12-004155.90.0336720.0003960.0010210.0000160.2823620.000017−11.60.612581906
JK-12-005153.40.0323920.0008270.0009070.0000290.2822930.000016−14.10.613502057
JK-12-006152.70.0259600.0002190.0007540.0000090.2823370.000019−12.50.712841961
JK-12-007156.50.0311220.0001580.0009060.0000090.2822750.000017−14.70.613752096
JK-12-008150.90.0272960.0007240.0008150.0000280.2823700.000019−11.40.712401889
JK-12-009156.50.0268850.0001880.0007620.0000030.2823140.000016−13.20.613152008
JK-12-010154.10.0287580.0000930.0008300.0000070.2823380.000016−12.50.612851959
JK-12-011153.50.0302140.0010680.0008600.0000260.2823250.000014−13.00.513041988
JK-12-012156.70.0372580.0006340.0010590.0000250.2823190.000016−13.10.613192000
JK-12-013154.80.0338400.0007630.0009260.0000140.2822570.000017−15.30.614012137
JK-12-014151.80.0325560.0002900.0009380.0000070.2823070.000015−13.60.513322029
JK-12-015150.70.0349990.0004460.0010060.0000060.2823230.000017−13.10.613111994
JK-12-016155.40.0366070.0003530.0010400.0000040.2822890.000017−14.20.613612067
JK-12-017151.40.0509250.0023970.0015730.0000800.2823160.000015−13.40.513412012
JK-12-018156.70.0438640.0007430.0012530.0000150.2823090.000018−13.50.613412024
JK-33-001158.20.0499460.0010580.0014960.0000410.2823130.000008−13.30.313432015
JK-33-002106.90.1090990.0038310.0030740.0000700.2823480.000010−13.30.413501973
JK-33-003155.30.4142760.0075000.0110050.0001450.2823740.000028−12.21.016871944
JK-33-0041570.0910550.0031380.0026970.0000750.2823370.000013−12.70.413531971
JK-33-005155.50.0501480.0007540.0014910.0000230.2823280.000012−12.90.413211983
JK-33-006155.70.1678920.0037110.0047750.0000940.2823690.000012−11.70.413851913
JK-33-007152.90.1829330.0035730.0048880.0000730.2821900.000145−18.15.116682310
JK-33-008155.90.2318050.0122910.0064600.0003010.2824100.000019−10.50.713911835
JK-33-009156.40.0665680.0025300.0018970.0000740.2823590.000014−11.80.512911916
JK-33-0101560.4089610.0119390.0102150.0002700.2824040.000021−11.00.815831870
JK-33-011155.50.0883310.0011850.0024040.0000210.2823010.000014−13.90.513942049
JK-33-012158.40.2326780.0081360.0060270.0002040.2823770.000019−11.60.714261904
JK-33-013158.70.1358850.0016370.0038550.0000420.2823180.000018−13.40.614262019
JK-33-0141550.0263200.0011760.0006940.0000320.2823200.000012−13.10.413051996
JK-33-015157.60.0772320.0028390.0020530.0000660.2823650.000015−11.60.512881903
JK-33-016156.90.0802540.0010980.0022690.0000270.2823370.000013−12.60.513371968
JK-33-017155.20.0881090.0030250.0022870.0000710.2823460.000015−12.30.513241949
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MDPI and ACS Style

Liu, X.; Shi, W.; Zhang, J.; Zhang, X.; Yang, J.; Li, W. Petrogenesis of the Helong Granites in Southern Jiangxi Province, China: Constraints from Geochemistry and In Situ Analyses of Zircon U–Pb–Hf Isotopes. Minerals 2023, 13, 101. https://doi.org/10.3390/min13010101

AMA Style

Liu X, Shi W, Zhang J, Zhang X, Yang J, Li W. Petrogenesis of the Helong Granites in Southern Jiangxi Province, China: Constraints from Geochemistry and In Situ Analyses of Zircon U–Pb–Hf Isotopes. Minerals. 2023; 13(1):101. https://doi.org/10.3390/min13010101

Chicago/Turabian Style

Liu, Xinxing, Weixin Shi, Juan Zhang, Xiaoyan Zhang, Junfeng Yang, and Wei Li. 2023. "Petrogenesis of the Helong Granites in Southern Jiangxi Province, China: Constraints from Geochemistry and In Situ Analyses of Zircon U–Pb–Hf Isotopes" Minerals 13, no. 1: 101. https://doi.org/10.3390/min13010101

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