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Article

Chronological and Geochemical Characteristics of a Newly Discovered Biotite Granite Porphyry in the Zhuxi W-Cu Polymetallic Deposit, Jiangxi Province, South China: Implications for Cu Mineralization

by
Yongpeng Ouyang
1,2,3,*,
Qi Chen
2,3,
Runling Zeng
2,3 and
Tongfei Li
3,4
1
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China
2
The Tenth Geological Brigade of Jiangxi Geological Bureau, Jiangxi Geological Bureau, Yingtan 335001, China
3
Yingtan Key Laboratory of Exploration and Research of Scarce and Advantage Minerals, The Tenth Geological Brigade of Jiangxi Geological Bureau, Yingtan 335001, China
4
College of Environment and Tourism, West Anhui University, Lu’an 237012, China
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(6), 624; https://doi.org/10.3390/min15060624 (registering DOI)
Submission received: 24 February 2025 / Revised: 14 May 2025 / Accepted: 6 June 2025 / Published: 9 June 2025
(This article belongs to the Special Issue Using Mineral Chemistry to Characterize Ore-Forming Processes)
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Abstract

:
Multiple occurrences of adakitic rocks, with crystallization ages clustering around ~160 Ma, have been documented in the Zhuxi district, northeast Jiangxi Province, South China. This research identifies a new adakitic biotite granite porphyry within the Zhuxi W-Cu polymetallic deposit. Zircon U-Pb geochronology of this porphyry yields a crystallization age of 161.6 ± 2.1 Ma. Integrated with previously published data, the adakitic rocks in the study area—comprising diorite porphyrite, biotite quartz monzonite porphyry, and the newly identified biotite granite porphyry—are predominantly calc-alkaline and peraluminous. They exhibit enrichment in light rare-earth elements (LREEs) and depletion in heavy rare-earth elements (HREEs), with slight negative Eu anomalies. The trace element patterns are characterized by enrichment in Ba, U, K, Pb, and Sr, alongside negative Nb, Ta, P, and Ti anomalies, indicative of arc-like magmatic signatures. Comparative analysis of geological and geochemical characteristics suggests that these three rock types are not comagmatic. Petrogenesis of the Zhuxi adakitic suite is linked to a dynamic tectonic regime involving Mesozoic crustal thickening, subsequent delamination, and lithospheric extension. Asthenospheric upwelling likely triggered partial melting of the overlying metasomatized lithospheric mantle, generating primary mantle-derived magmas. Underplating and advection of heat by these magmas induced partial melting of the thickened lower crust, forming the biotite granite porphyry. Partial melting of delaminated lower crustal material, interacting with the asthenosphere or asthenosphere-derived melts, likely generated the diorite porphyrite. The biotite quartz monzonite porphyry is interpreted to have formed from mantle-derived magmas that underwent assimilation of, or mixing with, silicic crustal melts during ascent. The ~160 Ma crystallization ages of these adakitic rocks are broadly contemporaneous with W-Mo mineralization in the Taqian mining area of the Zhuxi district. Furthermore, their geochemical signatures imply a prospective metallogenic setting for Cu-Mo mineralization around this period in the Taqian area.

1. Introduction

Adakites were initially defined as calc-alkaline dacitic and andesitic volcanic rocks characterized by distinctive geochemical signatures: high Al2O3 (>15 wt%), elevated Na2O (typically 3.5–7.5 wt%), high Sr concentrations (>400 ppm), low Yb (<1.9 ppm) and Y (<18 ppm) contents, and the absence of significant negative Eu anomalies relative to typical island-arc calc-alkaline magmas [1,2]. Subsequent research has demonstrated that adakitic rocks can also form in non-plate-subduction tectonic settings, for instance, through partial melting of low-potassium tholeiitic basalt that has undergone granulite-facies metamorphism under high confining pressures [3]. In recent years, numerous intermediate-to-acidic volcanic and intrusive rocks exhibiting adakite-like geochemical characteristics have been identified across China [4,5,6,7,8]. These are frequently associated with significant porphyry-type Cu-Mo-Au deposits [9,10,11,12,13,14,15,16,17], including prominent examples such as the Dexing porphyry Cu deposit in Jiangxi Province and the Gangdese porphyry Cu belt in Tibet [18,19,20,21].
The Zhuxi district in northeast Jiangxi Province represents one of South China’s most significant W-Cu polymetallic metallogenic provinces. Key deposits within this district include the Zhuxi W-Cu polymetallic deposit, the Taqian porphyry W-Mo deposit, and the Yuexing vein-type Cu-Pb-Zn polymetallic deposit. The Zhuxi W-Cu polymetallic deposit alone hosts estimated WO3 resources of approximately 3.634 million tons (at an average grade of 0.537 wt%) and ~361,000 tons of Cu metal, ranking it as the largest known W-polymetallic deposit globally [22]. While extensive research has elucidated many geological features, petrogenetic aspects, and metallogenic controls of this deposit [23,24,25,26,27,28,29,30,31,32,33,34,35,36], the “W-Cu coexistence” phenomenon observed here remains inadequately explained. Tungsten mineralization is conventionally linked to crustally derived magmas [37,38], whereas copper mineralization is typically associated with mantle-derived magmas and processes related to oceanic crust subduction [39,40,41]. Given these disparate magmatic origins, W and Cu mineralizations are generally not expected to coexist within the same mineral system. However, drilling at the Zhuxi W-Cu polymetallic deposit has revealed widespread spatial association and paragenetic complexity of W and Cu ore bodies.
Recent investigations in the Zhuxi district have identified multiple intermediate-to-acidic intrusions with adakitic affinities that appear closely related to Cu-Mo mineralization, with crystallization ages ranging from 157 to 160 Ma [23,24,25]. Notably, a diorite porphyrite displaying adakitic geochemical signatures, with a crystallization age of 162.7 ± 1.4 Ma, was discovered within altered granite from borehole ZK4212 in the Zhuxi mining area [42]. Furthermore, this study reports a newly discovered biotite granite porphyry in borehole ZK2105 within the same mining area. Field geological observations suggest that this intrusive body may have been tectonically emplaced to its current position by regional thrusting. Considering the recognized metallogenic potential of adakitic magmas, particularly for porphyry Cu systems, this study aims to (1) determine the precise emplacement age of the newly identified biotite granite porphyry, (2) analyze its detailed geochemical characteristics, (3) investigate its petrogenesis and explore its genetic relationship with other adakitic rocks in the vicinity, and (4) elucidate its implications for W-Cu mineralization. These objectives are pursued to refine petrogenetic and metallogenic models for the Zhuxi district, and to provide robust geological constraints for future mineral exploration endeavors in the region.

2. Regional Geology and Sample Description

2.1. Geological Background

The Zhuxi district is located at the eastern margin of the Pingle Depression, within the northern segment of the Jiangnan Orogen, marking a transition zone between the Yangtze Block to the northwest and the Cathaysia Block to the southeast [43,44] (Figure 1a). The district lies northwest of the Northeast Jiangxi Deep Fault system and is geographically adjacent to the major Dexing Cu-Au-Ag and Jiurui Cu-Au mining areas. Since the Neoproterozoic (Jingningian period), the region has experienced multiple protracted tectonothermal cycles involving sedimentation, deformation, metamorphism, and magmatism. This complex geological evolution generated conditions highly favorable for polymetallic mineralization, leading to the formation of significant W, Cu, Mo, and Au deposits, among which the Zhuxi W-Cu polymetallic deposit is the largest discovered to date.
The regional stratigraphy comprises a metamorphic basement unconformably overlain by a sedimentary cover sequence (Figure 1b). The most extensively exposed basement units belong to the Neoproterozoic Wannian and Shuangqiaoshan groups, predominantly consisting of low-grade metavolcanic and metasedimentary rocks. These are overlain by Carboniferous, Permian, Triassic, Jurassic, Cretaceous, Neogene, and Quaternary strata [23].
Recurrent magmatism accompanied the region’s prolonged and complex tectonic evolution. Magmatic activity, ranging from mafic–ultramafic to felsic (granitic), occurred episodically from the Neoproterozoic (Jingningian) to the Cenozoic (Himalayan). Mafic-to-intermediate rocks primarily comprise lamprophyre, diorite porphyrite, and quartz diorite porphyrite, which typically occur as dikes emplaced at relatively shallow crustal levels within the mining district. Intermediate-to-acidic intrusions include granodiorite porphyry, biotite granite, altered granite, two-mica granite, muscovite granite, and granite porphyry. Among these, the acidic granites generally form dike swarms or larger plutons at deeper levels, whereas granodiorite porphyries occur predominantly as small stocks or dykes at shallower levels. Metallogenesis in the district is closely linked to the emplacement of Yanshanian (Jurassic–Cretaceous) intermediate-to-acidic intrusions, particularly granites and the biotite granite porphyry relevant to this study [45].
The basement rocks are interpreted as metamorphosed marine volcano-sedimentary sequences, largely derived from Neoproterozoic volcanic-arc and back-arc basin systems. Structurally, the study area lies within a zone of intense deformation resulting from the Paleozoic collision and amalgamation between the Yangtze and Cathaysia blocks, followed by significant Mesozoic intracontinental deformation. Key tectonic events include (1) strong Neoproterozoic (Jingningian) folding and metamorphism; (2) Caledonian folding and thrusting; (3) Variscan–Indosinian intracontinental deformation, including northeast-trending ductile shearing and orogeny; and (4) Yanshanian–Himalayan intracontinental reactivation, characterized by further orogeny, basin formation, and significant lithospheric extension. Consequently, regional structures are complex, featuring prominent folds, extensive fault systems (including major thrusts and strike-slip faults), and localized ductile shear zones.
Minerals 15 00624 g001
Figure 1. Geological sketched map of the study area: (a) Tectonic sketched map of the study area (NCB denotes the North China Block, QDO denotes the Qinling–Dabie Orogen, YB denotes the Yangtze Block, JNO denotes the Jiangnan Orogen, CB denotes the Cathaysian Block, and SECMZ denotes the Southeast China Magmatic Zone) (modified from [22]). (b) Simplified geological map of the Zhuxi district (modified from [46]).
Figure 1. Geological sketched map of the study area: (a) Tectonic sketched map of the study area (NCB denotes the North China Block, QDO denotes the Qinling–Dabie Orogen, YB denotes the Yangtze Block, JNO denotes the Jiangnan Orogen, CB denotes the Cathaysian Block, and SECMZ denotes the Southeast China Magmatic Zone) (modified from [22]). (b) Simplified geological map of the Zhuxi district (modified from [46]).
Minerals 15 00624 g001
The study area hosts abundant and diverse mineral resources, encompassing metallic, nonmetallic, and energy minerals. Metallic deposits, including W-Cu polymetallic, W-Mo polymetallic, and Cu polymetallic systems, are concentrated within the Taqian–Fuchun metallogenic belt. These are primarily hosted within late Paleozoic carbonate strata and at or near the contact zones with Yanshanian intermediate-to-acidic intrusions [47]. Nonmetallic mineral occurrences are largely stratabound or associated with dikes. For instance, limestone deposits are developed in the Carboniferous Huanglong Formation (northeastern area) and the Permian Qixia and Changxing formations. Dolomite is exploited from the dolomite member of the Carboniferous Huanglong Formation in the northeastern region, while clay minerals are found in shale units within the Permian Xiaojiangbian Formation (northeastern area). Coal deposits are hosted by the Permian Leping Formation and the Triassic Anyuan Formation.
Based on ore genesis and style of mineralization, three primary deposit types are recognized in the district (Figure 1b). Skarn-type W-Cu polymetallic deposits, including major occurrences such as the Zhuxi, Taqian, Zhangjiawu, and Tanling deposits, are predominantly developed within late Paleozoic carbonate strata, typically concentrated at the contacts between Yanshanian intermediate-to-acidic intrusions and the carbonate host rocks. Intrusion-hosted disseminated/stockwork W-Cu-Mo-Pb-Zn deposits, exemplified by the Yangcaojian and Xiyuanwu deposits, encompass mineralization found primarily within Yanshanian intermediate-to-acidic intrusions (e.g., biotite granite, altered granite, granodiorite, and granite porphyry) or their immediate endo-/exo-contact zones; this category is sometimes referred to locally as “altered granite (porphyry) type”. Additionally, vein-type (fracture-controlled) Cu-W-Pb-Zn polymetallic deposits, represented by the Yuexing deposits, are predominantly structurally controlled, localized within faults, fracture zones, and detachment structures, and can occur in a variety of country rock types [22].

2.2. Sample Description

This study investigates several intrusive rocks from the Zhuxi W-Cu polymetallic deposit. While incorporating previously published data for a biotite quartz monzonite porphyry from the Zaolin ore block (Figure 2a) and a diorite porphyrite hosted within altered granite [42], the primary focus involves new analyses of a biotite granite porphyry intersected between −1285.2 m and −1317.4 m depth in drill hole ZK2105 (indicated in Figure 2b).
Samples of the biotite granite porphyry collected for this study are grayish-white and exhibit a blocky structure in hand specimen, with a distinct porphyritic texture (Figure 3a). Petrographic analysis reveals phenocrysts set in a finer-grained matrix. Phenocrysts constitute approximately 35% of the rock volume and primarily consist of feldspar (~20%) and biotite (~15%). Biotite occurs as subhedral-to-euhedral flakes or laths, ranging from 0.1 to 1.8 mm in diameter, typically exhibiting well-defined cleavage; some grains show partial alteration to chlorite (Figure 3b). Feldspar phenocrysts are subhedral to anhedral, tabular to prismatic in shape, with grain sizes ranging from 0.2 to 4 mm. Some larger feldspar crystals show evidence of partial alteration (e.g., sericitization), resulting in slightly clouded surfaces (Figure 3b). The matrix (~65% volume) is microcrystalline and composed predominantly of quartz, feldspar, and mica.

3. Methodology

3.1. LA-ICP-MS Zircon U-Pb Dating

The selection of biotite granite porphyry zircons for this study was accomplished via Guangzhou Tuoyan Testing Technology Co., Ltd. (Guangzhou, China) The selection criteria were euhedral zircons with a good crystal shapes, no cracks, and transparency and cleanliness. After selection, they were polished to the zircon centers and secured with epoxy glue. Subsequently, micrographs were obtained using transmitted light, reflected light, and cathodoluminescene (CL) techniques with a scanner with an analytical electron microscope (JSM-IT300) from JEOL (Tokyo, Japan) linked to a Delmic Sparc system. The imaging was conducted under an electric field with voltages ranging from 0.5 to 30 kV and a tungsten filament current of 72 μA. Zircon laser ablation–inductively coupled plasma mass spectrometry (LA-ICP-MS) U-Pb isotope dating was performed at the State Key Laboratory of Geological Processes and Mineral Resources (GPMR) at the China University of Geosciences (Wuhan, China). For this purpose, a UP193FX 193 nm ArF excimer laser ablation system from Newwave Company (San Diego, CA, USA) was utilized. The laser that was used was from ATL Company (Wermelskirchen, Germany) and the ICP-MS instrument was Agilent 7500a (Santa Clara, CA, USA). The beam spot diameter used in this study was 32 μm. Both samples were subjected to external standard calibration using the zircon Standard 91500 [48]. The analytical method and process can be found in the literature [48]. The material’s elemental composition and isotope ratio were computed via the GLITER_Ver4.0 program. The final zircon 207Pb/206Pb and 238U/206Pb diagrams of the Tera–Wasserburg concordia, along with the 206Pb/238U weighted average ages, were plotted via Isoplot 3.0 software [49].

3.2. Whole-Rock Geochemical Analysis

The testing of major, trace, and rare-earth samples was carried out by ALS Minerals-ALS Chemex (Guangzhou) Co., Ltd. (Guangzhou, China) The major element analysis was carried out via a PANalytical PW2424 X-ray fluorescence spectrometer (Almelo, The Netherlands) and analyzed using the ME-XRF26F method. The samples were prepared by mixing 0.5 g of the powdered sample with 5 g of Li2B4O7 and LiBO2 and then forming wafers. The range of study inaccuracies was 0.1~1% relative standard deviation (RSD).
Trace element analysis was carried out via an Agilent 5110 ICP emission spectrometer and an Agilent 7900 ICP mass spectrometer (Santa Clara, CA, USA), and the ME-MS61r method was used for analysis. Forty milligrams of sample powder was dissolved in a mixture of HF, HNO3, and H2SO4 and then evaporated twice at temperatures between 150 and 200 °C. After evaporation, the residue was redissolved in 49 mL of 1% HNO3 for analysis. As an internal standard, 1 mL of 500 ppb indium was inserted into the sample and used as an external standard.
The Agilent 7900 inductively coupled plasma mass spectrometer (Santa Clara, CA, USA) was used to analyze the rare-earth elements, employing the ME-MS81 analytical method. Next, 50 mg of lithium metaborate (LiBO2/Li2B4O7) flux was added to the sample, which was mixed thoroughly and fused in a furnace at 1025 °C. After cooling, the fused material was dissolved and diluted with nitric acid, hydrochloric acid, and hydrofluoric acid. The rare-earth element contents were subsequently analyzed with an inductively coupled plasma mass spectrometer. This method ensures analytical precision, with a relative deviation of less than 10%, and accuracy, with a relative error of less than 10%.

4. Results

4.1. Zircon U-Pb Dating

Zircons from the biotite granite porphyry sample ZK2105-1 were analyzed for U-Pb isotopes via LA-ICP-MS; the results for 14 analysis spots are presented in Table 1. Cathodoluminescence (CL) images reveal that the analyzed zircons are mostly euhedral to subhedral, with long-axis dimensions ranging from 55 μm to 185 μm and aspect ratios between 1:1 and 3:1 (Figure 4). The grains typically exhibit distinct internal structures, including oscillatory zoning and growth bands, characteristic of magmatic crystallization [50]. The uranium concentrations vary from 205 ppm to 2343 ppm, and the Th concentrations range from 55 ppm to 449 ppm. The resulting Th/U ratios span from 0.04 to 1.16, with an average of 0.34, consistent with a magmatic origin for most grains.
All 14 analytical spots yielded concordant or near-concordant U-Pb ages, plotting cohesively on the Tera–Wasserburg concordia diagram (Figure 5). Nine relatively concentrated isotopic ages provided a weighted mean 206Pb/238U age of 161.6 ± 2.1 Ma (MSWD = 1.5, n = 9). This age was interpreted as the crystallization age of the biotite granite porphyry. The other measurement points were relatively scattered, ranging from 606 to 879 Ma, which may indicate the age of captured Neoproterozoic zircons (e.g., ~847 Ma [51]).

4.2. Characteristics of Major Elements

Whole-rock major element compositions for the newly analyzed biotite granite porphyry (ZK2105 samples) and previously published data for diorite porphyrite (ZX15-01-06 [42]) and biotite quartz monzonite porphyry (ZL-YQ11-15 [52]) are listed in Table 2. The three rock types show increasing SiO2 contents, corresponding to increasing acidity, from the diorite porphyrite (avg. 59.13 wt%) to the biotite quartz monzonite porphyry (avg. 64.91 wt%) to the biotite granite porphyry (avg. 68.46 wt%). The TiO2 content is highest in the diorite porphyrite (avg. 0.62 wt%), lowest in the biotite quartz monzonite porphyry (avg. 0.33 wt%), and intermediate in the biotite granite porphyry (avg. 0.41 wt%). The Al2O3 contents are relatively high and comparable across the three types (avg. 15.46 wt%, 15.28 wt%, and 14.94 wt%, respectively). With increasing SiO2, the MgO (avg. 4.22, 1.90, and 0.96 wt%) and TFe2O3 (total iron as Fe2O3; avg. 4.49, 2.50, and 2.38 wt%) contents decrease, while the total alkali content (Na2O + K2O; avg. 4.76, 5.35, and 6.48 wt%) increases. Notably, the biotite quartz monzonite porphyry exhibits a significantly higher K2O content compared to the other two rock types at similar SiO2 levels.
The Rittman index values (σ = (Na2O + K2O)2/(SiO2 − 43)) for all three rock types are less than 3.3, indicating a calc-alkaline affinity. On the SiO2 vs. K2O classification diagram (Figure 6a), the samples plot within the calc-alkaline and high-K calc-alkaline fields. In the A/NK vs. A/CNK diagram (Figure 6b; A/NK = molar Al2O3/(Na2O + K2O), A/CNK = molar Al2O3/(CaO + Na2O + K2O)), all samples plot in the peraluminous field (A/CNK > 1). Thus, all three intrusive types are classified as peraluminous, calc-alkaline to high-K calc-alkaline rocks. The Harker diagrams (Figure 7) show that inter-element correlations with SiO2 do not define simple linear trends across the three rock types, and apparent compositional gaps or discontinuities exist. This suggests that they are unlikely to be related solely by fractional crystallization from a single parental magma.

4.3. Characteristics of Rare-Earth Elements

Rare-earth element (REE) and trace element data for the three rock types are presented in Table 2. Chondrite-normalized REE patterns (Figure 8a) are characterized by enrichment in light REEs (LREEs) relative to heavy REEs (HREEs), resulting in moderately to steeply right-dipping patterns. The LREE segments are steeper than the relatively flat HREE segments. The total REE contents (ΣREEs) are similar for the diorite porphyrite (avg. 202.8 ppm) and the biotite quartz monzonite porphyry (avg. 208.8 ppm) but lower in the more evolved biotite granite porphyry (avg. 173.0 ppm). The ΣREEs contents follow the same trend (avg. 191.2, 199.0, and 166.2 ppm, respectively). The ΣREEs contents decrease systematically with increasing SiO2, from the diorite porphyrite (avg. 11.6 ppm) through the biotite quartz monzonite porphyry (avg. 9.8 ppm) to the biotite granite porphyry (avg. 6.8 ppm). Consequently, the degree of LREE/HREE fractionation, indicated by ratios such as (La/Yb)N, increases with differentiation (the average (La/Yb)N values are approximately 16.5, 20.4, and 24.4 for the three rock types, respectively). All samples exhibit slight negative Eu anomalies, with δEu (Eu/Eu*) values ranging from 0.83 to 0.90 for the diorite porphyrite, from 0.74 to 0.81 for the biotite quartz monzonite porphyry, and from 0.77 to 0.81 for the biotite granite porphyry.
The primitive mantle-normalized trace element patterns (Figure 8b) for all three rock types display enrichment in large-ion lithophile elements (LILEs, e.g., Ba, U, K, Pb, Sr) and depletion in high-field-strength elements (HFSEs, e.g., Nb, Ta, Ti), as well as P. These features, particularly the pronounced negative Nb-Ta-Ti anomalies, are characteristic of arc-related magmas. Crucially, all samples exhibit low Y contents (range 6.97–14.9 ppm, avg. 9.95 ppm) and low Yb contents (range 0.53–1.26 ppm, avg. 0.81 ppm). Combined with high Sr contents, this results in high Sr/Y ratios (range 29.9–83.7, avg. 58.1). On the (La/Yb)N-YbN and Sr/Y vs. Y discrimination diagrams (Figure 9a,b), the samples plot predominantly within the adakite field. Combined with their high Al2O3 contents (Table 2), these geochemical features (high Al2O3, high Sr/Y, low Y, low Yb) confirm that all three intrusive rock types possess adakitic affinities.

5. Discussions

5.1. Sources of Diorite Porphyrite, Biotite Quartz Monzonite Porphyry, and Biotite Granite Porphyry

Petrographic observations indicate that samples from all three intrusive types investigated (biotite granite porphyry, diorite porphyrite, and biotite quartz monzonite porphyry) have experienced variable degrees of post-emplacement alteration (e.g., chloritization of biotite, sericitization of feldspar; Figure 3). This is consistent with their relatively high Loss-on-Ignition (LOI) values, which generally exceed 3 wt% (Table 2), suggesting interactions with hydrothermal fluids or weathering processes. To evaluate the potential influence of alteration on whole-rock geochemistry and ensure the robustness of subsequent petrogenetic interpretations, the behavior of elements considered to be relatively immobile during low–moderate-temperature alteration, such as high-field-strength elements (HFSEs, e.g., Th, Zr, Hf, Ti, Nb, Ta) and rare-earth elements (REEs), was assessed.
Correlation diagrams for pairs of geochemically coherent, relatively immobile elements, such as Th vs. La and Zr vs. Hf (Figure 10), show strong positive linear correlations for samples from all three intrusive suites. This coherence suggests that these elements, and likely other HFSEs and REEs, largely preserved their primary magmatic ratios and were not significantly mobilized or fractionated relative to each other by the observed alteration. Furthermore, the overall consistency and systematic variations observed in the chondrite-normalized REE patterns (Figure 8a) and primitive mantle-normalized trace element patterns (Figure 8b), particularly for the HFSEs, lend further support to their relative immobility and utility in reflecting primary magma characteristics [57].
Therefore, while acknowledging the presence of alterations, the HFSE and REE geochemical data are considered to be reliable indicators of primary magmatic processes and source characteristics for these intrusive rocks. These elements will be utilized preferentially in the following sections to discuss the petrogenesis of the diorite porphyrite, biotite quartz monzonite porphyry, and biotite granite porphyry, and to constrain their tectonic setting.
Three distinct types of adakitic intrusions have been identified within the Zhuxi district: the diorite porphyrite identified within altered granite (borehole ZK4212 [42]), the biotite quartz monzonite porphyry from the Zaolin ore block [52], and the biotite granite porphyry newly characterized in this study (borehole ZK2105). These rocks display a compositional range from intermediate (diorite porphyrite) to intermediate–acidic (biotite quartz monzonite porphyry) to acidic (biotite granite porphyry). Although their zircon U-Pb crystallization ages are broadly contemporaneous, clustering within the late Jurassic (diorite porphyrite at 162.7 ± 1.4 Ma [42], biotite quartz monzonite porphyry at 157 ± 1 Ma [52], and biotite granite porphyry at 161.6 ± 2.1 Ma; this study), several lines of evidence argue against a simple comagmatic relationship linking them through fractional crystallization.
Geochemically, the three rock types fail to define linear trends on Harker diagrams (Figure 7). Instead, distinct compositional gaps and non-linear variations are observed, particularly for elements like TiO2, MgO, and K2O. Furthermore, they exhibit distinct REE fractionation patterns (Figure 8a); the diorite porphyrite shows relatively flatter HREE patterns (lower (La/Yb)N), whereas the biotite granite porphyry displays the most fractionated HREE patterns (highest (La/Yb)N). While sharing overall trace element characteristics typical of adakitic rocks (Figure 8b), subtle but significant differences exist—notably, the biotite quartz monzonite porphyry belonging distinctly to the high-K calc-alkaline series, whereas the others are predominantly medium-K calc-alkaline (Figure 6a).
Spatially, the three rock types also exhibit distinct distributions. Both the diorite porphyrite and the biotite granite porphyry were intersected by drilling within the main Zhuxi W-Cu deposit area, whereas the biotite quartz monzonite porphyry occurs in the separate Zaolin ore block. Geological interpretations based on drill cores suggest that the biotite granite porphyry may have been tectonically emplaced via thrust faults or nappe structures, obscuring its original intrusive relationships. The diorite porphyrite was intersected nearby, hosted within altered granite [42], further complicating the interpretation of primary spatial relationships. Crucially, no direct field evidence (e.g., observed cross-cutting relationships, gradational contacts) linking the three distinct intrusive types as part of a single zoned pluton or evolutionary sequence has been documented.
Considering the combined geochemical discrepancies (non-linear major element trends, differing REE fractionation patterns, varying K contents) and the lack of clear spatial or temporal field relationships indicative of a shared, evolving magmatic system, we conclude that these three adakitic intrusions are unlikely to be comagmatic. They likely represent discrete magma batches, potentially derived from different source materials, under varying physical conditions (e.g., pressure, temperature, water content), or involving different petrogenetic processes.

5.2. Characteristics of the Magmatic Source

Several petrogenetic models have been proposed for the formation of adakitic rocks, including (1) partial melting of subducted oceanic crust [1], (2) mixing between felsic crustal melts and mantle-derived mafic magmas [58], (3) assimilation and fractional crystallization (AFC) processes involving mantle-derived basaltic magmas interacting with crustal materials [59,60,61], (4) partial melting of delaminated lower crust [62,63], and (5) partial melting of thickened lower crust [8,62,63,64].
The Nb/Ta ratios for the three Zhuxi intrusive types range from 6.94 to 17.09 (avg. 12.81), generally approaching typical continental crustal values (~11–13 [65,66]). Their Zr/Hf ratios (range 35.87–42.02, avg. 38.81) are slightly greater than that of crustal magma (~33 [67]). Crucially, the Nb/U ratios (range 1.71–3.42, avg. 2.62) are significantly lower than the primitive mantle values (~30–47), strongly indicating substantial crustal input or modification during magma genesis. Collectively, these ratios suggest significant crustal involvement in the petrogenesis of all three rock types.
Derivation solely through fractional crystallization of parental basaltic magma appears unlikely. Such a process typically requires voluminous associated mafic intrusions [68], and although mafic rocks occur regionally, no voluminous, coeval (~160 Ma) mafic intrusions have been documented in direct association with the Zhuxi adakitic rocks.
Magma mixing processes often leave characteristic petrographic evidence, such as mafic microgranular enclaves (MMEs) or mineral disequilibrium textures [69,70]. While MMEs were not observed in the studied samples of the three rock types, microscopic examination revealed the presence of resorbed or rounded quartz phenocrysts within the biotite quartz monzonite porphyry (Figure 11). This texture can be interpreted as mineralogical evidence of disequilibrium, potentially resulting from magma mixing. In contrast, such direct petrographic evidence for magma mixing is absent in the diorite porphyrite and the biotite granite porphyry. This suggests that magma mixing may have played a specific role in the petrogenesis of the biotite quartz monzonite porphyry. However, considering that its overall geochemical signature (e.g., low Nb/U, Nb/Ta ratios) still points towards a dominantly crustal character, we can infer that the mixing likely involved a predominantly crust-derived felsic melt incorporating a relatively minor component of mantle-derived mafic magma, rather than being a 50:50 mixture or mafic-dominated hybrid.
The magma formed by the partial melting of delaminated crust often exhibits a relatively high contents of MgO, Cr, and Ni due to its interaction with upwelling mafic magma [61,71]. However, the observed low MgO, Cr, and Ni contents of the biotite granite porphyry (Table 2), appear inconsistent with melting of a mafic-dominated source associated with delamination. Conversely, these geochemical characteristics are more consistent with the magma originating from partial melting of a thickened crust [62,63,64].
The diorite porphyrite exhibits relatively higher MgO, Cr, and Ni contents [42]. This composition could be consistent with partial melting of delaminated lower crust. Petrogenetic models involving delamination and subsequent melting are often linked to intraplate extensional tectonic settings [15]. At the same time, a key feature of all three intrusive types is their prominent arc-like geochemical signature, including negative Nb-Ta-Ti anomalies (Figure 8b) [72] and their plotting within volcanic-arc fields on tectonic discrimination diagrams (e.g., Rb vs. Y + Nb, Figure 12a; Rb-Hf-Ta ternary diagram, Figure 12b). Since the diagenetic age of these three rock types is ~160 Ma, extensive research indicates that South China experienced significant lithospheric extension and intraplate deformation during the Jurassic–Cretaceous period, following earlier collisional orogenies. This establishes a post-orogenic extensional setting, which is conducive to lithospheric thinning, asthenospheric upwelling, and potentially lower crustal delamination—processes that can trigger the melting of both metasomatized lithospheric mantle and lower crust. Therefore, we believed that the diorite porphyrite originated from partial melting involving delaminated lower crustal materials within this extensional regime. The required heat could be supplied by the upwelling asthenosphere following delamination. The arc-like geochemical signature can be interpreted as an inherited feature, reflecting pervasive metasomatism of the South China lithosphere (both mantle and lower crust) during earlier Paleozoic subduction events, rather than indicating active arc magmatism at ~160 Ma. This interpretation aligns the geochemical data with the inferred post-orogenic extensional tectonic setting conducive to delamination-related magmatism.
In summary, the petrogenesis of the ~160 Ma adakitic suite in the Zhuxi district appears to be intrinsically linked to a dynamic late Jurassic tectonic regime characterized by post-orogenic lithospheric extension following earlier crustal thickening. This setting likely facilitated complex crust–mantle interactions, potentially involving delamination of the thickened lithosphere. According to this study, we propose a scenario initiated by asthenospheric upwelling, possibly triggered by extension and/or delamination, which induced partial melting of the overlying metasomatized subcontinental lithospheric mantle (SCLM), generating primary mantle-derived magmas. Underplating and/or advection of heat by these mantle magmas likely induced partial melting of the pre-existing thickened lower crust, generating the silicic melts parental to the low-MgO biotite granite porphyry. Concurrently, influenced by mantle-derived magmas, the delaminated lower crustal material underwent partial melting, ultimately resulting in the formation of diorite porphyrite. Finally, the biotite quartz monzonite porphyry likely represents a hybrid product, formed through mixing or assimilation processes involving ascending mantle-derived magmas (or melts derived from metasomatized SCLM) and a significant component of crust-derived silicic melt, consistent with its intermediate composition, high-K character, and subtle petrographic evidence of disequilibrium.

5.3. Implications for Copper Mineralization in the Zhuxi District

Yanshanian magmatism and associated mineralization in the Zhuxi district occurred in several pulses, with significant activity recognized around ~160 Ma, possibly followed by events around ~150 Ma and ~130 Ma. The ~160 Ma event involved the emplacement of I-type granitoids and related porphyries exhibiting adakitic affinities, as documented in this study and previous work [42,52]. Mineralization associated with this stage includes significant W-Mo systems, exemplified by the Taqian deposit where molybdenite yields Re-Os ages of 162 ± 2 Ma [75]. This timing highlights the potential for broadly contemporaneous Cu-Mo mineralization during this period.
A strong spatial and temporal association between adakitic magmatism and porphyry Cu(-Mo-Au) deposits is widely recognized globally and within South China, such as those documented in the Middle–Lower Yangtze River Metallogenic Belt e.g., [9,10,11,12,13,14,15,16,17]. The giant Dexing porphyry Cu deposit, situated adjacent to the Zhuxi district, is a prominent regional example linked to adakitic intrusions [18,19,20,21]. While the specific adakitic intrusions studied here (particularly the biotite granite porphyry from ZK2105) may be tectonically displaced and are not observed in direct intrusive contact with the main Taqian ore zones, their ~160 Ma crystallization ages are essentially contemporaneous with the ~162 Ma mineralization event documented at Taqian [75]. This temporal coincidence strongly suggests a genetic link between the ~160 Ma adakitic magmatism and associated polymetallic (including Cu-Mo) mineralization potential in the district.
Classic models often associate the fertility of subduction-related adakites for porphyry Cu deposits with high water contents, high oxygen fugacity (fO2), and efficient transport of sulfur and metals derived from the subducting slab or overlying mantle wedge [11,76]. However, it is increasingly recognized that adakitic magmas generated in non-subduction settings (e.g., post-collisional, intraplate extension) can also be fertile, potentially involving different mechanisms for metal enrichment or volatile behavior. Processes such as crust–mantle mixing (inferred for the biotite quartz monzonite porphyry) or partial melting involving metasomatized delaminated lower crust (inferred for the diorite porphyrite), as proposed for the Zhuxi adakites, can influence melt oxidation states, volatile contents, and metal budgets in ways that are potentially favorable for Cu-Mo-Au mineralization [77].
As discussed previously (Section 5.2), the inferred tectonic setting for the Zhuxi district at ~160 Ma is likely one of post-orogenic/intraplate extension. The specific petrogenetic processes inferred here—including partial melting involving delaminated lower crust and mixing between crust- and mantle-derived components—occurred within this dynamic setting. These processes, associated with the ~160 Ma adakitic magmatism, likely established favorable physicochemical conditions for the formation of associated porphyry-type Cu-Mo mineralization during this important metallogenic episode in the Zhuxi district.

6. Conclusions

(1) Zircon U-Pb geochronology indicates a crystallization age of 161.6 ± 2.1 Ma for the newly identified biotite granite porphyry within the Zhuxi W-Cu polymetallic deposit.
(2) The three investigated intrusive types (diorite porphyrite, biotite quartz monzonite porphyry, and biotite granite porphyry) display a compositional progression from intermediate to acidic. All are peraluminous and belong to the calc-alkaline to high-K calc-alkaline series, with the biotite quartz monzonite porphyry being distinctly potassic. They share adakitic geochemical affinities, characterized by LREE enrichment relative to depleted HREEs ((LREE/HREE)N increases with SiO2), slight negative Eu anomalies, enrichment in LILEs (e.g., Ba, K, Sr), depletion in HFSEs (e.g., Nb, Ta, Ti) and P, high Sr/Y ratios, and low Y and Yb contents.
(3) Despite their broadly contemporaneous emplacement ages (~160 Ma), geochemical data (e.g., non-linear Harker trends, distinct REE fractionation patterns) and spatial distributions suggest that the three adakitic intrusive types are not comagmatic. Their petrogenesis is linked to complex crust–mantle interactions within a post-orogenic setting: The biotite granite porphyry likely originated from partial melting of thickened felsic lower crust, induced by heat from underplated mantle-derived magmas. The diorite porphyrite was interpreted to result from partial melting involving delaminated lower crustal material, potentially reflecting a more mafic or metasomatized source component compared to the granite porphyry source. The biotite quartz monzonite porphyry likely formed through mixing between crust-derived silicic melt and a minor component of ascending mantle-derived magma (or melt from metasomatized SCLM).
(4) The formation of these ~160 Ma adakitic rocks occurred within a dynamic tectonic regime involving post-orogenic lithospheric extension, potentially accompanied by delamination following earlier crustal thickening. The associated petrogenetic processes, including partial melting of diverse crustal sources (thickened and delaminated lower crust) and crust–mantle mixing, likely established favorable physicochemical conditions for contemporaneous porphyry-type Cu-Mo mineralization in the Zhuxi district.

Author Contributions

Writing—Original Draft, Y.O.; Methodology, Q.C.; Visualization, R.Z.; Writing—Review and Editing, T.L. All authors have read and agreed to the published version of the manuscript.

Funding

This study was jointly supported by the “Deep Earth Probe and Mineral Resources Exploration-National Science and Technology Major Project, grant number 2024ZD1002204”, “Geological Exploration Project funded by Jiangxi Provincial Finance, grant number 20250020”, “Key R&D Plan Project of Science and Technology Department of Jiangxi Province, grant number 20212BBG73045”, “Jiangxi Natural Science Foundation General Program, grant number 20224BAB203037”, “The Youth Science and Technology Leaders Training Program Project of Jiangxi Geological Bureau, grant numbers 2022JXDZKJRC02 and 2023JXDZKJRC05”, and the “Science and Technology Plan Project of Yingtan City, grant numbers 20233-185656, 202412-28880 and 2024SYD017”.

Data Availability Statement

The data presented in this study are available upon request from the corresponding author.

Acknowledgments

We are grateful to the editors and the anonymous reviewers for handling our manuscript and providing valuable suggestions for improving it.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 2. Simplified map of the deployment of the exploration project of the Zhuxi W-Cu polymetallic deposit: (a) Simplified geological map of the Zhuxi mining area (1—Quaternary strata; 2—Triassic strata; 3—Permian strata; 4—Upper Carboniferous Series Huanglong Formation; 5—Upper Carboniferous Series Huanglong Formation; 6—Upper Proterozoic Wannian Group; 7—aplite; 8—granite porphyry; 9—diorite porphyrite; 10—lamprophyre; 11—tremolite actinization zone; 12—green alteration zone; 13—thrust nappe fault; 14—measured (presumed) fault; 15—locations and the number of drill holes; 16—exploration line and the number of exploration lines) (revised from [29]). (b) Profile map of the 21st exploration line in the Zaolin ore section in the Zhuxi mining area.
Figure 2. Simplified map of the deployment of the exploration project of the Zhuxi W-Cu polymetallic deposit: (a) Simplified geological map of the Zhuxi mining area (1—Quaternary strata; 2—Triassic strata; 3—Permian strata; 4—Upper Carboniferous Series Huanglong Formation; 5—Upper Carboniferous Series Huanglong Formation; 6—Upper Proterozoic Wannian Group; 7—aplite; 8—granite porphyry; 9—diorite porphyrite; 10—lamprophyre; 11—tremolite actinization zone; 12—green alteration zone; 13—thrust nappe fault; 14—measured (presumed) fault; 15—locations and the number of drill holes; 16—exploration line and the number of exploration lines) (revised from [29]). (b) Profile map of the 21st exploration line in the Zaolin ore section in the Zhuxi mining area.
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Figure 3. Hand samples and microscopic characteristics of the biotite granite porphyry in the Zhuxi district: (a) hand samples; (b) porphyritic texture of the sample (Pl—plagioclase; Afs—alkaline feldspar; Bt—biotite); (c) chloritized biotite (under a single polarizer); (d) chloritized biotite (under an orthogonal polarizer).
Figure 3. Hand samples and microscopic characteristics of the biotite granite porphyry in the Zhuxi district: (a) hand samples; (b) porphyritic texture of the sample (Pl—plagioclase; Afs—alkaline feldspar; Bt—biotite); (c) chloritized biotite (under a single polarizer); (d) chloritized biotite (under an orthogonal polarizer).
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Figure 4. Zircon cathodoluminescence (CL) images of the biotite granite porphyry in the Zhuxi district.
Figure 4. Zircon cathodoluminescence (CL) images of the biotite granite porphyry in the Zhuxi district.
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Figure 5. Zircon U-Pb isotope concordia diagram of the biotite granite porphyry in the Zhuxi district: (a) concordia diagram of the 14 LA-ICP-MS U-Pb ages; (b) weighted mean age plot of the 9 LA-ICP-MS U-Pb ages.
Figure 5. Zircon U-Pb isotope concordia diagram of the biotite granite porphyry in the Zhuxi district: (a) concordia diagram of the 14 LA-ICP-MS U-Pb ages; (b) weighted mean age plot of the 9 LA-ICP-MS U-Pb ages.
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Figure 6. Petrological diagrams of the adakitic rocks in the Zhuxi district: (a) Relationships between K2O and SiO2 (the base map is from [53]). (b) A/NK vs. A/CNK diagram (the base map is from [54]).
Figure 6. Petrological diagrams of the adakitic rocks in the Zhuxi district: (a) Relationships between K2O and SiO2 (the base map is from [53]). (b) A/NK vs. A/CNK diagram (the base map is from [54]).
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Figure 7. Diagram of SiO2 and major oxides in the adakitic rocks in the Zhuxi district.
Figure 7. Diagram of SiO2 and major oxides in the adakitic rocks in the Zhuxi district.
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Figure 8. Distribution patterns of REEs and trace elements in adakitic rocks in the Zhuxi district: (a) chondrite-normalized REE patterns; (b) primitive mantle-normalized trace element patterns (the standard values can be founded in the related paper [55]).
Figure 8. Distribution patterns of REEs and trace elements in adakitic rocks in the Zhuxi district: (a) chondrite-normalized REE patterns; (b) primitive mantle-normalized trace element patterns (the standard values can be founded in the related paper [55]).
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Figure 9. Discrimination diagram of the adakitic rocks in the Zhuxi district: (a) (LaN)/(YbN) vs. YbN diagram; (b) (Sr/Y) vs. Y diagram (the base map is from [56]).
Figure 9. Discrimination diagram of the adakitic rocks in the Zhuxi district: (a) (LaN)/(YbN) vs. YbN diagram; (b) (Sr/Y) vs. Y diagram (the base map is from [56]).
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Figure 10. La vs. Th and Hf vs. Zr diagrams of the adakitic rocks in the Zhuxi district: (a). La vs. Th diagram; (b). Hf vs. Zr diagram.
Figure 10. La vs. Th and Hf vs. Zr diagrams of the adakitic rocks in the Zhuxi district: (a). La vs. Th diagram; (b). Hf vs. Zr diagram.
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Figure 11. Rounded quartz in the biotite quartz monzonite porphyry (Bt—biotite; Pl—plagioclase; Qz—quartz) (revised from [52]).
Figure 11. Rounded quartz in the biotite quartz monzonite porphyry (Bt—biotite; Pl—plagioclase; Qz—quartz) (revised from [52]).
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Figure 12. Tectonic discrimination diagram of the adakitic rocks in the Zhuxi district: (a) Rb vs. (Y + Nb) tectonic discrimination diagram (the base map is from [73]); (b) Rb-Hf-Ta tectonic discrimination diagram (the base map is from [74]).
Figure 12. Tectonic discrimination diagram of the adakitic rocks in the Zhuxi district: (a) Rb vs. (Y + Nb) tectonic discrimination diagram (the base map is from [73]); (b) Rb-Hf-Ta tectonic discrimination diagram (the base map is from [74]).
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Table 1. LA-ICP-MS zircon U-Pb isotope dating results of the biotite granite porphyry in the Zhuxi district.
Table 1. LA-ICP-MS zircon U-Pb isotope dating results of the biotite granite porphyry in the Zhuxi district.
No.Content (ppm)Th/UIsotope RatioIsotope Age (Ma)
206Pb232Th238U207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ206Pb/238U1σ
122.777.48060.100.05250.00160.18010.00560.02480.00031582
277.11526470.230.06690.00160.92710.02850.10010.002261513
327.052.79490.060.05320.00190.19010.00670.02590.00041652
47.561522230.680.04980.00370.17690.01290.02590.00051653
511.12283250.700.04980.00290.17550.01010.02560.00031632
629.51929960.190.05180.00170.18270.00620.02550.00041622
761.399.922070.050.04930.00120.17150.00440.02500.00021591
865.71325040.260.06590.00150.99620.02720.10930.002266913
920.482.86890.120.05260.00200.18610.00760.02550.00041623
101543118580.360.06690.00141.35580.03190.14600.001787910
1172.73714710.790.06570.00160.99710.03010.10930.002166912
1214.44443851.150.04990.00190.17530.00660.02570.00041632
131031338750.150.06540.00130.89580.02640.09850.002160612
1475.035124560.140.05120.00130.18430.00570.02590.00051653
Table 2. Major element and trace element contents of biotite granite porphyry (ZK2105-1-5), diorite porphyrite (ZK15-01-06) [42], and biotite quartz monzonite porphyry (ZL-YQ11-15) [52].
Table 2. Major element and trace element contents of biotite granite porphyry (ZK2105-1-5), diorite porphyrite (ZK15-01-06) [42], and biotite quartz monzonite porphyry (ZL-YQ11-15) [52].
ElementsZK2105-2-1ZK2105-2-2ZK2105-1-5ZK2105-2-4ZK2105-2-5ZX15-01ZX15-02ZX15-03ZX15-04ZX15-06ZL-YQ11ZL-YQ12ZL-YQ13ZL-YQ14ZL-YQ15
SiO268.5869.6667.7267.8368.558.6658.0860.359.8958.7365.265.0464.765.1264.48
Al2O314.7714.7714.8615.1615.1115.4615.2515.8315.2515.5214.8515.6715.1115.3715.39
TiO20.40.410.410.410.410.630.620.650.590.630.350.350.330.320.31
TFe2O32.332.352.462.382.44.514.524.564.264.62.52.522.532.492.45
MgO0.950.940.960.990.964.194.344.323.974.291.811.951.971.941.85
MnO0.030.030.030.030.030.080.070.080.080.080.030.030.030.030.03
CaO2.552.182.842.582.435.685.884.935.316.133.893.663.843.733.87
Na2O3.593.593.73.383.643.371.633.623.252.211.841.751.771.741.7
K2O2.882.912.673.162.860.92.911.361.752.783.473.593.653.653.61
P2O50.120.120.120.120.120.20.20.210.190.20.10.10.10.120.08
LOI3.422.753.943.573.484.864.912.894.053.433.112.483.082.643.4
Li88.569.384.579.769.420216511613792.410.929.799.4511.539.68
Be2.852.822.782.862.862.83.082.472.732.44.632.752.694.193.27
Sc5.585.735.835.325.32171821816.117.65.275.975.775.685.71
V45.845.548.84444.313613514012113654.9856.3657.0255.5853.01
Cr17.415.716.716.113.318218419818018814.9216.9818.3718.712.28
Co5.955.816.645.755.5921.821.321.319.320.56.777.096.686.555.97
Ni8.235.615.45.884.8773.874.77837175.87.097.086.556.244.71
Cu6.978.0913.94.7910.12220.325.225.421.74.785.796.742.471.98
Zn13743.762.659.259.974.579.169.590.580.366.3770.464.557.0150.43
Ga23.122.824.421.922.322.623.123.823.322.922.8723.5723.3823.5122.4
As22.14.7440.329.918422935491.91591382.612.63.016.97.54
Rb13913414114413074.3238104121185129.9138.6142.3143.8133.6
Sr51340146846448311644371238856630474.16366.05437.88408.94383.67
Y7.687.578.126.977.4214.914.614.813.91428.897.467.557.268
Zr194200186187184182183184179178306314303317278
Nb7.157.077.57.627.129.69.789.919.595312.1511.4211.4211.049.55
Cs36.533.24941.433.893.125495.311216717.3219.1118.4318.5918.02
Ba71962857289668037839865865959199985511509741099
Hf4.894.764.614.614.535.034.994.964.9957.917.77.887.767.19
Ta0.6620.6560.6390.6280.6220.60.590.580.580.591.751.591.950.690.56
Pb4216.838.337.632.52017.722239232335.5732.9834.0131.8527.02
Th18.71818.417.717.417.717.218.117.717.417.8618.1219.0219.2417.89
U4.174.093.933.753.832.942.863.012.952.9144.174.214.174
Mo--0.225--0.230.50.190.220.120.758.460.780.420.37
Sb2.522.092.912.261.913.6815.44.515.911.30.531.140.920.820.7
W0.2130.370.5160.8470.121.452.241.430.850.61.551.741.741.891.25
Bi0.1740.0850.0510.04190.2040.140.240.120.540.160.450.380.460.090.06
La42.538.345.141.838.85047.249.249.146.850.1650.148.6849.3352.03
Ce83.484.187.181.778.591.6869289.186.593.2494.3895.2493.2595.7
Pr7.887.418.247.457.3310.19.629.959.799.469.839.8810.219.710.2
Nd28.728.331.427.127.837.635.137.436.434.737.237.537.8936.4737.93
Sm4.544.544.764.534.316.315.876.46.26.065.685.636.015.585.9
Eu1.051.021.11.031.011.531.551.51.561.491.481.41.391.381.5
Gd3.193.243.3333.084.324.324.244.344315.395.175.325.135.33
Tb0.4020.4020.4250.3850.3870.570.550.590.560.560.570.530.540.530.54
Dy1.561.591.541.541.553.12.873.183.013.072.211.9421.982.01
Ho0.260.2470.2590.2450.2410.520.480.510.490.50.350.30.30.30.32
Er0.7930.7170.7110.6950.6971.571.561.641.561.650.880.740.750.740.78
Tm0.08590.0870.08570.07920.08030.20.190.190.190.20.1110.0930.090.0940.099
Yb0.5620.5680.5820.5260.5361.211.21.261.191.20.730.640.620.650.68
Lu0.08420.08090.08250.07940.07640.190.180.190.170.180.1070.0910.0910.0870.097
ΣREE175.01170.60184.72170.16164.40208.82196.69208.25203.66196.68207.94208.39209.13205.22213.12
ΣLREE168.07163.67177.70163.61157.75197.14185.34196.45192.15185.01197.59198.89199.42195.71203.26
ΣHREE6.946.937.026.556.6511.6811.3511.8011.5111.6710.359.509.719.519.86
ΣLREE/ΣHREE24.2323.6125.3324.9823.7316.8816.3316.6516.6915.8519.0920.9320.5420.5820.62
δEu0.800.770.800.800.810.850.900.830.870.850.810.780.740.770.80
Sr/Y66.8052.9757.6466.5765.0978.1229.9383.6561.584.4453.3449.0758.0056.3347.96
Rb/Sr0.270.330.300.310.270.060.540.080.140.290.270.380.320.350.35
Nb/Ta10.8010.7811.7412.1311.4516.0016.5817.0916.3816.156.947.185.8616.0017.05
Zr/Hf39.6742.0240.3540.5640.6236.1836.6737.1035.8735.6038.6940.7838.4540.8538.66
Nb/U1.711.731.912.031.863.273.423.293.223.273.042.742.712.652.39
Data sourcesData analyzed in this paperData from paper [42]Data from paper [52]
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Ouyang, Y.; Chen, Q.; Zeng, R.; Li, T. Chronological and Geochemical Characteristics of a Newly Discovered Biotite Granite Porphyry in the Zhuxi W-Cu Polymetallic Deposit, Jiangxi Province, South China: Implications for Cu Mineralization. Minerals 2025, 15, 624. https://doi.org/10.3390/min15060624

AMA Style

Ouyang Y, Chen Q, Zeng R, Li T. Chronological and Geochemical Characteristics of a Newly Discovered Biotite Granite Porphyry in the Zhuxi W-Cu Polymetallic Deposit, Jiangxi Province, South China: Implications for Cu Mineralization. Minerals. 2025; 15(6):624. https://doi.org/10.3390/min15060624

Chicago/Turabian Style

Ouyang, Yongpeng, Qi Chen, Runling Zeng, and Tongfei Li. 2025. "Chronological and Geochemical Characteristics of a Newly Discovered Biotite Granite Porphyry in the Zhuxi W-Cu Polymetallic Deposit, Jiangxi Province, South China: Implications for Cu Mineralization" Minerals 15, no. 6: 624. https://doi.org/10.3390/min15060624

APA Style

Ouyang, Y., Chen, Q., Zeng, R., & Li, T. (2025). Chronological and Geochemical Characteristics of a Newly Discovered Biotite Granite Porphyry in the Zhuxi W-Cu Polymetallic Deposit, Jiangxi Province, South China: Implications for Cu Mineralization. Minerals, 15(6), 624. https://doi.org/10.3390/min15060624

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