Yu Junzhen1,2
Junaid Khan- 1State Key Laboratory of Ni & Co Associated Minerals Resources Development and Comprehensive Utilization, Jinchang, Gansu, China
- 2Jinchuan Ni & Co Research and Engineering Institute, Jinchang, Gansu, China
- 3Faculty of Earth Resource, China University of Geosciences, Wuhan, China
- 4State Key Laboratory of Geological Processes and Mineral Resource, China University of Geosciences, Wuhan, China
- 5Geological Survey Institute, China University of Geosciences, Wuhan, China
The newly discovered Jiangjunmu Cu–Au deposits are hosted within granodiorite porphyry and K-feldspar granite of the East Kunlun metallogenic belt. Previous understanding of these deposits has been limited due to a lack of comprehensive isotopic data. To address this gap, we present new zircon U–Pb geochronology, whole-rock geochemistry, and Sr–Nd–Pb–Hf isotopic analyses of the Jiangjunmu intrusive rocks. Both intrusive rock samples exhibit nearly identical rare earth element patterns, suggesting they originated from the same source area. The K-feldspar granite (206Pb/238U age: 228 Ma) and the Jiangjunmu granodiorite porphyry intruded into the Jiangjunmu K-feldspar granite porphyry (206Pb/238U age: 234 Ma). They exhibit initial (87Sr/86Sr)ᵢ ratios of 0.70884–0.70944 and 0.70555–0.70913, εNd(t) values of −4.32 to −5.24 and −8.27 to −8.93, 207Pb/204Pb ratios of 15.615–15.677 and 15.664–15.682, and 208Pb/204Pb ratios of 38.443–38.544 and 38.526–38.650, respectively. The Jiangjunmu K-feldspar granite also has high Rb/Sr ratios (0.82), low MgO (0.66–1.19 wt%), Cr (6.6–13.6 ppm), Ni (4.4–6.4 ppm), and Co (55.9–97.2 ppm) contents, indicating an origin from a thickened lower continental crust (TLCC) magma source by partial melting (Sr/Y: 9.4–15.8; La/Yb: 25.6–35.5). Its lower Mg# values (36–39), relatively higher (87Sr/86Sr)ᵢ ratios, lower Sr concentrations (179.8–266.1 ppm), and εHf(t) values (−8.18 to −3.83) suggest that a more evolved upper continental crustal component (heterotypic sandstone) contributed to the formation of the K-feldspar granite during magmatic evolution. The presence of numerous mafic magmatic enclaves (MMEs) in the granodiorite porphyry suggests that the Cu (Au) contents of the Jiangjunmu deposit may have been derived from a mantle source. In association with the tectonic background and regional research, the Jiangjunmu granodiorite porphyry and K-feldspar granite (Th/Sm: 4.2–5.1; Th/Yb:11.5–14.8) formed in a post-collisional orogenic extensional setting after the closure of the Paleo-Tethys Ocean.
1 Introduction
Porphyry deposits are the world’s most important source of Cu, Mo, and Au, contributing over two-thirds of global Cu production, one-fifth of Au production, and one-half of total molybdenum production (Sillitoe, 2010; Junaid et al., 2022). Porphyry deposits mainly form in compressional settings like subduction zones (e.g., Luzon Arc, Andes) or strike-slip systems (e.g., Himalayas) (Zengqian et al., 2003; Sillitoe, 2010; Midea et al., 2021). A total of 97% of the giant to large porphyry Cu (Mo-Au) deposits are generated in island arc or continental margin settings (Richards, 2003; Cooke et al., 2005), while 3% occur in continental rift and extensional intracontinental settings (Hou et al., 2004; Hou and Cook, 2009; Hou et al., 2011).
Significant genetic relationships are well-documented between porphyry Cu and Cu-Mo deposits and the petrogenesis of their associated granitic intrusions. For instance, granitic bodies are known to be involved in the generation of magmas that evolve into porphyritic granites, which are linked with important mineral deposits (Zeng et al., 2017). Recent studies have emphasized the role of magma mixing in influencing the geochemistry of granodioritic intrusions, suggesting a complex interplay of magmatic processes that produce distinct geochemical signatures associated with mineralization (Qi et al., 2020). However, many geochemical characteristics of such intrusions, particularly in lesser-studied regions, are inadequately documented, highlighting a significant research gap in understanding the full scope of their petrogenesis (Qi et al., 2020).
The Qinghai–Tibet Plateau is a key region for the evolution of the Tethys and an important metallogenic domain in China, containing many porphyries and epithermal Cu–Mo–Au–Pb–Zn deposits (Hou and Cook, 2009). Based on deposit assemblages and location, there are several major porphyry metallogenic belts in this region, from south to north: 1) the Gangdese Cu–Mo–Au–Pb–Zn metallogenic belt (GDMB) (Zheng et al., 2002; Hou et al., 2004; Hou et al., 2009); 2) the Yu Long porphyry copper metallogenic belt (YLPMB) (e.g., Hou et al., 2003); and 3) the East Kunlun Mo–Cu–Au–Zn–Fe metallogenic belt (EKMB) (Feng et al., 2010; Li and Sun, 2010; Liu et al., 2013). In recent years, an increasing number of porphyry deposits have been discovered in the EKMB, such as the Aikengdesite porphyry Mo (Cu) deposit, Xiadeboli Cu–Mo deposit, Wulanwuzhuer porphyry Cu deposit, Jiangjunmu porphyry Cu–Au deposit, and Re Shui porphyry Mo deposit (Feng et al., 2010; Li and Sun, 2010; Wang et al., 2013), which show great potential for mineralization. The Jiangjunmu porphyry Cu–Au deposit, discovered in 2016 in the eastern part of the EKMB, is distinctive from other porphyry deposits in the region, which are dominated by Cu–Mo or Mo. It is marked by the presence of numerous mafic magmatic enclaves (MMEs) hosted in ore-bearing granodiorite porphyry. Despite the significance of the host rocks in the Jiangjunmu porphyry Cu-Au deposits, only preliminary geochemical and geochronological studies have been conducted (Yu et al., 2020). A more comprehensive understanding has been hindered by the lack of data on adjacent rock petrogenesis, tectonic setting, and magma-mineralization relationships. This study presents zircon U–Pb dating, whole-rock geochemistry, and Sr–Nd–Pb–Hf isotopes of the Jiangjunmu intrusive rocks, combined with regional analysis, to constrain the tectonic setting, magma source, and diagenetic processes, advancing the understanding of Jiangjunmu deposit formation.
2 Geological setting
The East Kunlun Orogenic Belt (EKOB) is a crucial part of the Central China Orogenic System (Chen et al., 2017). It is situated in the northern Qinghai-Tibet Plateau (Figure 1a) and lies within the Tethyan tectonic domain. The formation of the EKOB is intricately linked to the tectonic evolution of the Proto-Tethys and Paleo-Tethys Oceans. The tectonic setting of the EKOB is characterized by a series of geological events, including oceanic subduction, continental collision, and post-collisional processes, which have shaped its current structure and composition (Wang et al., 2023). The EKOB is bounded to the south by the Bayan Har Terrane, to the north by the Qaidam Basin, to the east by the West Qinling Orogen, and is truncated to the west by the Altyn Tagh Fault (Figure 1b). The belt extends approximately 1,500 km in an E–W direction and ranges in width from 90 to 240 km. From north to south, the EKOB is subdivided into three primary tectonic zones: the North Kunlun Belt (NKB), bounded by the North Kunlun Fault (NKF); the Central Kunlun Belt (CKB), delimited by the Middle Kunlun Fault (MKF); and the South Kunlun Belt (SKB) (Xu et al., 2014; Li et al., 2017).
Figure 1. (a) The geological map showing the location of the East Kunlun Orogenic Belt (EKOB) in Central China Orogenic System (modified after Lin et al., 2025); (b) Tectonic map of the EKOB (Mo et al., 2007; Xiong, 2014); (c) Age histogram of the main ore-forming rock masses in the Triassic, EKOB (modified after Xiong, 2014); and (d) Geological map of the EKOB showing the Jiangjunmu copper-gold deposit (modified after Song et al., 2016).
The EKOB hosts widespread intrusive and minor volcanic rocks, forming a major magmatic belt enriched with polymetallic deposits (Mo et al., 2007). Magmatic activity in the region spans from the Proterozoic to the Cenozoic, recording the belt’s tectonic evolution (Figure 1d). Four major magmatic episodes can be distinguished: the Jinningian episode (1990–824 Ma), dominated by acidic intrusions (e.g., diorite, granodiorite, monzonite, monzogranite, quartz diorite, and minor cordierite granite) (Chen and Li, 2002); the Caledonian episode (515–412 Ma), characterized by intermediate to felsic intrusions, including granodiorite, monzogranite, quartz diorite, and K-feldspar granite (Bai et al., 2001; Liu et al., 2004; Lu et al., 2005); the Hercynian episode (408–394 Ma), characterized by the emplacement of large granitic batholiths (Liu et al., 2012); and the Early Indosinian episode (248–240 Ma), dominated by monzogranite and granite intrusions along the South Kunlun Fault Belt. The Hercynian to Indosinian period represents a continuous tectono-magmatic evolution, with most polymetallic deposits in the eastern EKOB forming during the late Hercynian to early Indosinian period (Yuan and Mo, 2000a; Yuan and Mo, 2000b; Liu et al., 2004; Xiong et al., 2011).
The southern East Kunlun area is composed primarily of Pliocene sandstones, Late Triassic pyroclastic rocks, Middle Carboniferous carbonates, and Ordovician volcanic rocks. The main magmatic rocks consist of Late Triassic biotite granites and granodiorites, as well as Late Permian granodiorites, aligned along NW–SE and NE–SW trending structures. The ore-forming systems are associated primarily with Late Triassic granodiorites and are structurally controlled by NE–SW trends (Figures 1c, 2).
Figure 2. Geological map of the Jiangjunmu porphyry copper-gold deposit, highlighting the study area (modified after Xiong, 2014).
The eastern part of the EKOB hosts the Jiangjunmu Cu-Au deposit. The deposit is hosted in granodiorite porphyry and K-feldspar granite, both of which exhibit a close temporal-spatial relationship with mineralization and intrude into the K-feldspar granite porphyry (Figure 3f). The ore body is NW-SE trending, structurally controlled, with a length of 800 m and a width of 8 m, and extends to a depth of 400 m. The ore is composed primarily of copper and gold, with smaller amounts of silver and cobalt, containing a total of more than 0.41 Mt of Cu resources. Average grades are 0.57% Cu, 1.48 g/t Au, 3–485 g/t Ag, and 0.01% Co. The ore minerals are dominated by chalcopyrite and pyrite (Figures 3a–c), with gangue minerals including quartz, plagioclase, K-feldspar, biotite, sericite, and hornblende. Mineralization styles include vein-type, disseminated, and stockwork deposits. The main alteration types are potassic alteration, chloritization, silicification, sericitization (phyllic alteration), and argillic (clay) alteration. Among these, silicification and sericitization show the strongest correlation with Cu–Au mineralization.
Figure 3. Photomicrographs of intrusive rocks hosting the Jiangjunmu porphyry Cu-Au deposit in the EKOB. (a–c) Granodiorite porphyry hosting the main ore minerals; (d) Hydrothermally-altered granodiorite porphyry with plagioclase replaced by sericite-quartz aggregates; (e) K-feldspar granite exhibiting minor kaolin alteration and plagioclase replaced by sericite; (f) K-feldspar granite porphyry hosting quartz, plagioclase, and Kfs; (g) Mafic magmatic enclaves (MME) hosted in granodiorite porphyry; (h) Photomicrograph of MME composed predominantly of amphibole and plagioclase; (i) Photomicrograph of amphibole containing abundant felsic porphyroclasts. Cpy, chalcopyrite; Rut, rutile; Py, pyrite; Cov, covellite; Mrc, marcasite; Hbl, hornblende; Bt, biotite; Pl, plagioclase; Kfs, K-feldspar; Ill, illite; Ms, muscovite; Qz, quartz.
3 Sampling and analytical methods
In the Jiangjunmu Cu-Au deposits of EKOB, a total of 12 samples from the ore-bearing granodiorite porphyry (Jjm 01–1, Jjm 01–2, Jjm 01–3, Jjm 01–4, Jjm 01–5, Jjm 01–6) and the K-feldspar granite (Jjm 02–1, Jjm 02–2, Jjm 02–3, Jjm 02–4, Jjm 02–5, Jjm 02–6) were collected for analysis. All fresh samples were selected from surface outcrops in the vicinity of Long: 98°16′50″E and Lat: 36°10′24″N. After petrographic study, elemental analyses were conducted on six K-feldspar granite samples. Six samples from the granodiorite porphyry and four samples from the K-feldspar granite were chosen for Sr–Nd–Pb.
For U-Pb dating, one fresh sample each of K-feldspar granite (Jjm 02–1) and intruded K-feldspar granite porphyry (Jjm 03) was selected. A total of sixteen zircon Lu–Hf isotope analyses were performed on the same U-Pb dating sample of K-feldspar granite.
3.1 Geochronology
In the Langfang Institute of Geological and Mineral Research Laboratory, zircon selection and crushing were performed on samples of the K-feldspar granite (Jjm 02–1) and K-feldspar granite porphyry (Jjm 03). U-Pb dating and trace element analysis of zircon were simultaneously conducted by LA-ICP-MS at the State Key Laboratory of Continental Dynamics (SKLCD), China University of Geosciences, Wuhan, China. The detailed operating conditions for the laser ablation system, the ICP-MS instrument, and data reduction are the same as described by Zong et al. (2017). Laser sampling was performed using a GeolasPro laser ablation system, which consists of a COMPexPro 102 ArF excimer laser (wavelength of 193 nm and maximum energy of 200 mJ) and a MicroLas optical system. An Agilent 7700e ICP-MS instrument was used to acquire ion-signal intensities. Helium was applied as the carrier gas, while argon was used as the make-up gas, mixed with the carrier gas via a T-connector before entering the ICP. A “wire” signal smoothing device is included in this laser ablation system (Hu et al., 2015). The laser spot size and frequency were set to 24 µm and 80 Hz, respectively, in this study. Zircon 91500 and glass NIST610 were used as external standards for U-Pb dating and trace element calibration, respectively. Each analysis included a background acquisition of approximately 20–30 s, followed by 50 s of data acquisition from the sample. An Excel-based software, ICPMSDataCal, was used for off-line selection and integration of the background and analyzed signals, time-drift correction, and quantitative calibration for trace element analysis and U-Pb dating (Liu et al., 2008). Concordia diagrams and weighted mean calculations were made using Isoplot/Ex_ver3 (Ludwig, 2003).
3.2 Whole-rock elemental geochemistry
Whole-rock major elements were analyzed using a PANalytical Axios Max X-ray fluorescence (XRF) spectrometer, and trace elements, including REEs, were determined with an Agilent 7700e inductively coupled plasma mass spectrometer (ICP-MS) at the State Key Laboratory of Continental Dynamics (SKLCD), China University of Geosciences, Wuhan, China. Major element compositions were obtained by fusing 500 mg of sample with anhydrous lithium tetraborate, ammonium nitrate (as an oxidant), and fluxes of lithium fluoride and lithium bromide in a 1:10 sample-to-flux ratio. The FeO content was determined by potassium dichromate titration, while the H2O content was measured by heating powdered samples at 1,000 °C in a tube furnace, followed by gravimetric absorption. For trace element analysis, the sample digestion procedure involved several steps. First, the powder sample (200 mesh) was placed in an oven at 105 °C and dried for 12 h. A 50 mg portion of the powder was then accurately weighed and placed in a Teflon bomb. To this, 1 mL of HNO3 and 1 mL of HF were slowly added. The Teflon bomb was then placed in a stainless-steel pressure jacket and heated to 190 °C in an oven for more than 24 h. After cooling, the Teflon bomb was opened and placed on a hotplate at 140 °C, where it was evaporated to incipient dryness. Following this, 1 mL of HNO3 was added and evaporated to dryness again. Next, 1 mL of HNO3, 1 mL of MQ water, and 1 mL of an internal standard solution (1 ppm In) were added. The Teflon bomb was resealed and placed back in the oven at 190 °C for more than 12 h. Finally, the solution was transferred to a polyethylene bottle and diluted to 100 g by adding 2% HNO3. After dilution, the solution was analyzed using the Agilent 7700e ICP-MS to quantify element concentrations. For further details, follow the procedures of Khan et al. (2023). The accuracy of the analyses was approximately 5%.
3.3 Sr–Nd–Pb isotopic geochemistry
The Sr–Nd–Pb isotopic ratios of the whole-rock samples were measured at the Geochemical Laboratory of the China Geological Survey (CGS) in Wuhan. The samples were first crushed and ground, then sieved through a 200-mesh screen, and dried in an oven at 80 °C for 3 h. A 100 mg portion of each sample was spiked with tracer solutions (85Rb + 84Sr and 149Sm + 145Nd), followed by dissolution in separate solutions of HF, HNO3, and HClO4 at 190 °C for 48 h. To isolate and purify Rb, Sr, Sm, and Nd, cation resin ion-exchange chromatography (Dowex508) and Di-(2-Ethylhexyl) phosphoric acid (HDEHP) methods were employed. The isotopic concentrations of Rb, Sr, Sm, and Nd were measured using a Thermo Triton Plus Thermal Ionization Mass Spectrometer (TIMS). The isotopic ratios of Sr and Nd were corrected based on the values of 86Sr/87Sr = 0.1194 and 146Nd/144Nd = 0.7219. Analysis of the standard NBS987 and GBW04411 resulted in average values of 87Sr/86Sr = 0.71031 ± 0.00003 (2σ) and 143Nd/144Nd = 0.512637 ± 0.000005 (2σ), both of which fall within the acceptable error limits of the approved values (Khan et al., 2023).
For Pb isotope analysis, approximately 100 mg of each powdered sample was dissolved in an equal-parts mixture of HF and HNO3 within a Teflon beaker. The separation and purification of Pb were carried out using an anion exchange resin (BIO-RAD AG1-X8), with HBr serving as the eluent in a Teflon column. Following purification, Pb was deposited onto a rhenium filament using a combination of H3PO4 and silica gel. Isotopic ratios of Pb were then determined using a MAT261 thermal ionization mass spectrometer (TIMS). To account for instrumental mass fractionation, the measured Pb ratios were adjusted based on repeated analyses of the NBS981 Pb standard, yielding a correction factor of 0.1% per atomic mass unit. The overall analytical precision was within 0.1% (2σ), and the total procedural blanks contained less than 60 pg of Pb.
3.4 Lu-Hf isotopic geochemistry
In situ Hf isotopic analyses were conducted using a neptune plus multi-collector (LA-MC-ICP-MS) at the State Key Laboratory of Continental Dynamics (SKLCD), China University of Geosciences, Wuhan, China. The analysis employed a laser repetition rate of 8 Hz at 100 mJ with spot sizes of 40 μm, and 91500-zircon was used as the standard. Instrument operating conditions and analytical procedure were adopted from Hu et al. (2015), and Hf-mode ages were calculated using the method of Griffin et al. (2002).
4 Analytical results
4.1 Petrographic study
The granodiorite porphyry exhibits porphyritic textures, with phenocrysts constituting approximately 10 vol%. These phenocrysts consist of subhedral plagioclase crystals (∼5 vol%), equant K-feldspar crystals (∼3 vol%), and medium-grained quartz crystals (∼2 vol%), set in a fine-grained groundmass (90 vol%) composed of subhedral biotite, plagioclase, quartz, hornblende, and accessory minerals such as zircon, apatite, and rutile (Figure 3d). The phenocrysts range from 0.3 to 2 mm in size, with plagioclase occurring as hypidiomorphic plates and polysynthetic twins (0.5–2 mm). Granodiorite is the main ore-bearing rock, having undergone moderate to strong silicification and sericitic alteration, with the ore occurring primarily as veins and disseminated deposits.
The K-feldspar granite is in close contact with the granodiorite porphyry (Figure 3e) and displays a granitic texture consisting of coarse-grained euhedral K-feldspar (∼65 vol%), medium-grained quartz (∼30 vol%), and minor accessory minerals (∼5 vol%), including hornblende, magnetite, zircon, and apatite. This rock has undergone slight potassic silicification and sericitic alteration. The ore occurs as stockwork, suggesting post-mineralization of the granite. Additionally, numerous mafic magmatic enclaves (MMEs) hosted within the granodiorite porphyry are approximately 3–5 cm in diameter at the outcrop. These enclaves exhibit porphyritic texture (Figures 3g–i) and are mainly composed of medium-grained subhedral plagioclase (∼60 vol%), with a fine-grained groundmass consisting of hornblende (∼20 vol%), K-feldspar (∼10 vol%), and quartz (∼7 vol%), along with ∼3 vol% accessory minerals such as biotite, magnetite, and minor zircon, calcite, epidote, and titanite. These rocks have experienced strong serpentine alteration.
4.2 Zircon U–Pb dating
The detailed zircon U-Pb analytical results for the K-feldspar granite (Jjm 02–1) and K-feldspar granite porphyry (Jjm03) are presented in Supplementary Table S1. Concordia diagrams with cathodoluminescence (CL) images and weighted mean age plots are shown in Figure 4. Most of the zircons from Jiangjunmu rock samples are hypidiomorphic laths or short and columnar in shape, with wide concentric oscillatory zoning. These zircons have crystal lengths of 80–120 μm and length-to-width ratios ranging from 2:1 to 1.5:1, respectively. Zircons from both samples exhibit high Th/U ratios (averaging 0.7), consistent with a magmatic origin (Wu and Zheng, 2004; Yu et al., 2025). A total of 16 zircon analyses from Jjm 02–1 yielded a weighted mean 206Pb/238U age of 228.7 ± 1.8 Ma (MSWD = 0.1) (Figure 4a') and 16 zircon analyses from Jjm03 yielded a weighted mean 206Pb/238U age of 234.7 ± 1.0 Ma (MSWD = 0.25) (Figure 4b'). The ages of both rock units are consistent with their intrusive contact relationships.
Figure 4. Zircon U–Pb Concordia diagrams with cathodoluminescence (CL) images of zircons and weighted mean ages of: (a,a') K-feldspar granite and (b,b') K-feldspar granite porphyry.
4.3 Major and trace elements analysis
The major and trace element analysis results are presented in Supplementary Table S2. Most samples exhibit LOI values ranging from 0.2 to 2.1 wt%, indicating slight hydrothermal alteration, consistent with petrographic observations. LOI values are less than 3 wt% for relatively fresh or little altered rock samples (Tatsumi and Eggins, 1995; Kraus, 2005; Wang et al., 2009; Junaid et al., 2024).
The K-feldspar granite varies slightly, exhibiting overall characteristics of high SiO2 (69.44–75.04 wt%), Al2O3 (12.19–15.17 wt%), K2O (3.07–4.64 wt%) with K2O/Na2O (0.87–1.62), and low MgO (0.66–1.19 wt%) with Mg# (36–39). Based on their chemical compositions, they mainly plot in the quartz monzonite and granite areas on the SiO2 vs. K2O + Na2O diagram (Figure 5a) and show a high-K calc-alkaline series on the SiO2 vs. K2O diagram (Figure 5b). However, in the P2O5/Al2O3 vs. K2O/Al2O3 diagram (Figure 5c), which can be used to eliminate the effects of alteration (Crawford et al., 2007), the K-feldspar granite plots in the low-K field. This suggests that the high-K content of the K-feldspar granite is likely a result of later potassic alteration or contamination from the upper crust. Additionally, as shown in Figure 5d, the K-feldspar granite shows a transition from meta-aluminous to peraluminous and from I-type granites to S-type granites, which may be attributed to upper crustal contamination (McDonough et al., 1992).
Figure 5. TAS classification diagrams for the Jiangjunmu K-feldspar granite: (a) SiO2 vs. (Na2O + K2O) classification diagram (after Middlemost, 1994); (b) K2O vs. SiO2 variation diagram (Peccerillo and Taylor, 1976); (c) P2O5/Al2O3 vs. K2O/Al2O3 discrimination diagram (after Crawford et al., 2007); (d) A/CNK vs. A/NK diagram (after Maniar and Piccoli, 1989).
The K-feldspar granite has relatively high ∑REE (162.12–205.88 ppm) and experienced significant fractionation with high (La/Yb) N (18.38–20.19; Figure 6). They are characterized by a right-inclined shape with high LREE/HREE ratios (13.61–15.87), weak negative Eu anomalies (Eu/Eu* = 0.55–0.68), and a relative enrichment of large ion lithophile elements (LILE), such as Th, U, Rb, and K, along with depletion of high field strength elements (HFSE) like Nb, P, Ba, Ti, Zr, and Eu, indicating arc geochemical affinities (Figure 8a; Kelemen et al., 2003). A positive Sr anomaly and weak negative Eu anomalies suggest that plagioclase underwent slight fractional crystallization. The depletion of P and Ti further indicates that the magma experienced fractional crystallization of apatite, titanite, and Ti-rich minerals.
Figure 6. Geochemical discrimination diagrams for the Jiangjunmu K-feldspar granite: (a) Sr/Y vs. Y (after Defant and Drummond, 1990). and (b) (La/Yb)N vs. Sr/Y (after Sun et al., 2018; Liu et al., 2010).
4.4 Sr–Nd–Pb isotopic analysis
The whole-rock Sr-Nd-Pb isotope results for the granodiorite porphyry and K-feldspar granite are presented in Supplementary Tables S3, S4, respectively. The Sr and Nd isotopic compositions of the granodiorite porphyry show initial 87Sr/86Sr ratios ranging from 0.70555 to 0.70913 and εNd(t) values from −8.27 to −8.93, with two-stage Nd model mean age is 1,698 Ma. The K-feldspar granite samples have initial 87Sr/86Sr ratios from 0.70884 to 0.70944, except for one sample (Jjm02-4, which has a ratio of 0.7015), and εNd(t) values from −4.32 to −5.24, with two-stage Nd model mean age is 1,398 Ma. The Pb isotopic compositions of the granodiorite porphyry and K-feldspar granite show 206Pb/204Pb ratios from 18.349 to 18.388 (mean = 18.371) and 18.368 to 18.579 (mean = 18.466), 207Pb/204Pb ratios from 15.664 to 15.682 (mean = 15.674) and 15.615 to 15.677 (mean = 15.647), 208Pb/204Pb ratios from 38.526 to 38.650 (mean = 38.5785) and 38.443 to 38.544 (mean = 38.494), μ (238U/204Pb) values ranging from 9.60 to 9.63 (mean = 9.61) and 9.50 to 9.61 (mean = 9.55), and ω (232Th/204Pb) values ranging from 39.51 to 40.01 (mean = 39.69) and 37.31 to 38.53 (mean = 37.8), respectively.
4.5 Lu-Hf isotopic analysis
The zircon U-Pb spots were used to analyze the in situ Hf isotopic compositions. Sixteen dated zircon grains from K-feldspar granite (Jjm 02–1) were selected for Hf isotopic composition analysis, and the result is presented in Supplementary Table S5. The Hf isotopic data show that the zircons from the K-feldspar granite have εHf(t) values ranging from −8.18 to −3.83, with corresponding two-stage Hf model ages ranging from 1,342 to 1,582 Ma (mean = 1,500 Ma).
5 Discussion
5.1 Petrogenesis
5.1.1 Origin and source of the Jiangjunmu intrusion
The Jiangjunmu K-feldspar granite has high SiO2, Al2O3, and K2O contents, with K2O/Na2O > 1, and low Sr, Y, and Yb contents. All the samples in the SiO2 vs. Na2O, MgO, TiO2, Cr, P2O5, Ni, Al2O3, and Mg# variation diagrams are almost trending in the lower continental crust (LCC) field (Figures 7a–h). Moreover, the Jiangjunmu K-feldspar granite and the adjacent granodiorite porphyry exhibit rare earth element (REE) patterns consistent with lower continental crust (LCC) signatures (Figure 8; Rudnick and Gao, 2003; Yu et al., 2020), supporting their origin through partial melting of the LCC during Late Triassic magmatism in the Mo Getong and Xiang Rede areas (Xiong, 2014; Figure 8). Although there are some differences in petrologic characteristics and major-trace element contents, these suggest that both rocks originated from the same source area. The contents and ratios of La and Yb, Sr, and Y are important parameters for studying the source area of the rocks (Sun and McDonough, 1989; Rudnick and Gao, 2003; Sun et al., 2008). The K-feldspar granite has high Sr/Y and La/Yb values, consistent with the adjacent Jiangjunmu granodiorite porphyry, the barren adakites from the Dabie Mountains and ore-bearing granodiorite porphyry from the GDMB, which were related to the partial melting of the lower continental crust (Supplementary Table S6; Wang et al., 2007; Huang et al., 2008; Ling et al., 2011; Yu et al., 2020). This is significantly different from the Lower Yangtze River Belt (LYRB), which is related to the partial melting of the subducted oceanic slab represented by N-MORB (Supplementary Table S6; Xu et al., 2002; Ling et al., 2011). Moreover, the argument is also supported by the results from the Sr, Nd, and Pb isotopes (Figures 9a,b). In the εNd(t) vs. (87Sr/86Sr)i diagram, all samples of the granodiorite porphyry and K-feldspar granite plot in the LCC fields, consistent with I-type granite derived from the LCC in the Late Triassic East Kunlun (Figure 9a). In the 207Pb/204Pb vs. 208Pb/204Pb diagram, all samples plot in the LCC fields (Figure 9b), consistent with the GDMB, which are characterized by (87Sr/86Sr)i (0.705252–0.706708), 206Pb/204Pb (18.106–18.752), 207Pb/204Pb (18.106–18.752), and 208Pb/204Pb (37.394–39.058) (Xiaoming et al., 2007; Chen et al., 2019), different from the LYRB (Xu et al., 2002; Ling et al., 2011) and Cook Islands (Stern and Kilian, 1996; Hou et al., 2004). These results collectively indicate that both Jiangjunmu intrusions were derived from a LCC magma source through partial melting. (Figure 10d).
Figure 7. SiO2variation diagrams of the Jiangjunmu K-feldspar granite. (a)Na2O vs. SiO2diagram; (b)MgO vs. SiO2diagram; (c)TiO2vs. SiO2diagram; (d)SiO2vs. Cr diagram; (e)SiO2vs. P2O5diagram; (f)SiO2vs. Ni diagram; (g)SiO2vs. Al2O3diagram; (h)SiO2vs. Mg#diagram. Adakites related to subducted oceanic crust (Wang et al., 2006a; Eyuboglu et al., 2011), Adakites related to thickened lower (Zhao et al., 2020), Adakites related to delaminated lower crust (Xu et al., 2002; Gao et al., 2004; Wang et al., 2004), Metabasaltic and eclogitic melts (Rapp et al., 1999; Rapp et al., 2002; Eyuboglu et al., 2011), Pure slab melt (Stern and Kilian, 1996; Eyuboglu et al., 2011), Mantle melt (Eyuboglu et al., 2011), Fractional crystallization of basaltic magmas (FCBM) (Castillo et al., 1999; Macpherson et al., 2006; Jiang et al., 2007; Wang et al., 2005; Xu et al., 2002; Xu et al., 2017); Partial melting of the lower crust (PMLC) (Xu et al., 2002; Wang et al., 2006; Jiang et al., 2007); The I-type and S-type trends from Hieu et al. (2020).
Figure 8. (a) Chondrite-normalized rare earth elements (REE) spider diagram for the Jiangjunmu K-feldspar granite; (b) Primitive mantle-normalized incompatible elements spider diagram for the Jiangjunmu K-feldspar granite. Chondrite and primitive mantle reference values are from Sun and McDonough (1989); upper and lower continental crust data are from Rudnick and Gao (2003). Data for Late Triassic granite, diorite, and granodiorite porphyry are from Xiong (2014).
Figure 9. (a) εNd(t) vs. (87Sr/86Sr)i diagram (after Winter 2001); (b) (208Pb/204Pb)i vs. (206Pb/204Pb)i diagram (after Zindler and Hart, 1986); (c) Histogram of zircon εHf(t) values; (d) Zircon εHf(t) vs. zircon U–Pb ages (after Bodet and Schärer, 2000). Mafic magmatic enclaves (MME), Andean Volcanic Zone (AVZ), assimilation and fractional crystallization (AFC), depleted mantle (DM), Eastern Pacific Rise basalts (EPRB), Mid-Atlantic Ridge basalts (MARB), mid-ocean ridge basalts (MORB), North Andean Volcanic Zone (NAVC), and lower continental crust (LCC).
Figure 10. Tectonic discrimination diagrams for the Jiangjunmu intrusions: (a) Y + Nb versus Rb (ppm); (b) Nb versus Y (ppm) (after Pearce et al., 1984; Pearce, 1996); (c) Th/Yb versus Th/Sm (after Zhu et al., 2009); (d) La/Yb vs. La (Furman and Graham, 1999). Within-plate granites (WPG), volcanic-arc granites (VAG), collision-related granites (COLG), ocean-ridge granites (ORG), post-collisional adakites (PCA).
Previous research work (Green, 1994; Wu et al., 2002; Rollinson, 2003; Davidson et al., 2007) indicates that the residue of garnet and amphibole in the magma source significantly affects the distribution pattern of HREEs and the Y/Yb ratio of the derived melts. When the source is dominated by garnet as the residue the derived melts are strongly enriched in HREEs, with Y/Yb > 10 and (Ho/Yb)N > 1.2 (Green, 1994). In contrast, amphibole-bearing sources generate melts with near-chondritic Y/Yb (∼10) and (Ho/Yb)N (∼1.2) ratios along with flatter HREE patterns, reflecting amphibole’s greater affinity for MREEs (Green, 1994; Wu et al., 2002; Rollinson, 2003; Davidson et al., 2007). The K-feldspar granite has high Y/Yb (9.2–11.9) and (Ho/Yb) N (2.7–3.2), with a relatively flat HREE distribution pattern. The Jiangjunmu granodiorite porphyry adjacent to the K-feldspar granite is directly related to amphibole melt, combined with the high contents of SiO2 and Al2O3, the enrichment of Sr, and low Y and Yb values, along with a slightly negative Eu anomaly (Yu et al., 2020). These characteristics indicate that the granodiorite porphyry-related magma may have originated from an amphibole-garnet source with the suppression of plagioclase crystallization within the lower crust (Defant and Drummond, 1990). This is similar to the melt composition produced by the melting of meta-basalt or eclogite under conditions of 1–4.0 GPa (Figures 7b,h; Rapp, 1995; Rapp and Watson, 1995) because experimental petrology studies concluded that under high-pressure conditions (>1 GPa), rocks such as basalt, eclogite, and amphibolite will form a melt with garnet as the main remnant mineral phase (Xiao and Clemens, 2007). The K-feldspar granite samples trend in the diagram from the amphibolite melt to the metasandstone zone (Figure 11), indicating that their source area enrichment is similar to that of the granodiorite porphyry, with some differences.
Figure 11. (a) Plots of CaO + MgO + FeOT + TiO2 vs. CaO/MgO + FeOT + TiO2; (b) plots of Al2O3+MgO + FeOT + TiO2 vs. Al2O3/MgO + FeOT + TiO2 (after Altherr and Siebel, 2002; Kaygusuz et al., 2008).
5.1.2 Mantle and LCC contributions to Jiangjunmu intrusion formation
The contribution from the mantle and the interaction between the mantle and LCC in the magmatic chamber play an important role in the formation of porphyry deposits and ore-bearing porphyries (Richards and Kerrich, 2007; Hou et al., 2011). The granodiorite porphyry has relatively low Mg# values and Sr concentrations (Yu et al., 2020), which lie between those of the enriched mantle (Sr = 1,100 ppm) and LCC (Sr = 290 ppm) (Chen and Zhai, 2003). Furthermore, few MMEs are hosted in the Jiangjunmu granodiorite porphyry (Figure 3g), indicating that there is material exchange between the mantle and LCC in the magma chamber. This argument is further supported by the Sr, and Nd isotopic compositions (Figures 9a,c,d). The granodiorite porphyry has initial 87Sr/86Sr ratios (0.70555–0.70913) that lie between those of the modern primitive mantle (average value: 0.7045; DePaolo and Wasserburg, 1976) and the continental crust (average value: 0.719; Sun, 2001). On the 87Sr/86Sr vs. εNd(t) diagram (Figure 9a), all granodiorite porphyry samples plot within the fields of LCC or a mixture of LCC and mantle, consistent with Xiang rede area granodiorites and the Mo Getong area diorite porphyry, both formed by the mixing of LCC and mantle. In addition, the granodiorite porphyry has εHf(t) values ranging from −1.7 to +1.01 (Yu et al., 2020). These results suggest that there was a mantle contribution to the formation of the Jiangjunmu granodiorite porphyry, with mantle-enclave grains (Mg# > 40; Rapp and Watson, 1995). Furthermore, previous experimental petrological research has suggested that basaltic melts, which are high in elements like S, Cu (Au), and Co (Hofmann, 1997; Rudnick and Gao, 2003), underplate felsic magmas and interact with each other, elevating the Cu (Au) content of the magma. While crust-derived felsic magmas typically have low solubility for S and Cu (Au), but high contents of Pb, Zn, Ag, etc. (Wallace and Carmichael, 1992; Mungall, 2002; Hou et al., 2013). These findings indicate that the Cu (Au) contents of the Jiangjunmu deposit may have originated from the mantle. In contrast, the K-feldspar granite shows lower Mg# values (36–39) and relatively higher 87Sr/86Sr ratios (0.70884–0.70944), with Sr concentrations (179.8–266.1ppm) that are lower than the Sr content of both the LCC (Sr = 290 ppm) and the enriched mantle (Sr = 1,100 ppm). The εHf(t) values of the K-feldspar granite (−8.18 to −3.83) are also more negative than those of the granodiorite porphyry (Figure 9d). These results, combined with data from Figure 11, indicate that an upper continental crust composition (heterotypic sandstone) contributed to the formation of the K-feldspar granite during magmatic evolution, as reflected by its high 87Sr/86Sr ratios (0.70884–0.70944; Supplementary Table S3), TDM2 values (1,342–1,582 Ma; Supplementary Table S5), and decreased εHf(t) values (−8.18 to −3.83; Supplementary Table S5).
5.2 Tectonic implications
5.2.1 Tectonic setting of Jiangjunmu intrusions
A variety of tectonic models have been proposed for most of the porphyry deposits in the world, which mainly occur in continental margins (e.g., Richards et al., 2001) and island-arc settings related to the subduction of the ocean (Kerrich et al., 2000; Richards et al., 2001), as well as continental rifting and extensional intracontinental settings (Wang et al., 2006; Hou and Cook, 2009). The Jiangjunmu porphyry deposit is located in the northern part of the Qinghai-Tibet Plateau, an important area in the evolution of the Tethys Ocean. In the Y + Nb vs. Rb diagram, all samples plot in the volcanic-arc granites (VAG) field (Figure 10a). In the Nb vs. Y diagram (Figure 10b), all samples plot in the VAG + collision-related granites (COLG) fields. In the Th/Sm vs. Th/Yb diagram (Figure 10c), all samples plot in the post-collisional adakites (PCA) field, indicating that the Jiangjunmu intrusions formed during the transition stage from the COLG to PCA tectonic setting. Moreover, Li et al. (2013), Cao et al. (2015), Bai et al. (2016), and Xia et al. (2015) studied diorite (zircon U-Pb: 225.8 ± 1.5 Ma) in Gerizhuotuo, granite (zircon U-Pb: 225 ± 1.7 Ma) in Gouli, diorite (zircon U-Pb: 228 ± 2 Ma) in Galinge, and plagiogranite (zircon U-Pb: 227.2 ± 10 Ma) in Shuangqing, and their results show that these rock masses formed in a post-collision extensional setting of east Kunlun. Wu et al. (2011) reported the formation of a suite of granite (zircon U-Pb: 218 ± 2 Ma) by mixing of crustal and mantle materials in Maxingdaban, suggesting that the granite formed in the post-orogenic extensional setting after the Tethys Ocean closed in the EKOB region. In this study, we determined the ages of the K-feldspar granite porphyry and K-feldspar granite to be 234 Ma and 228 Ma, respectively (Figures 4a’,b’). Additionally, the granodiorite porphyry age, as determined by Yu et al. (2020), is 218 Ma. When compared to the ages of East Kunlun, these results suggest that the Jiangjunmu intrusions formed in a post-orogenic extensional setting. However, all samples show arc geochemical affinities (Figures 8a, 10a,b), consistent with the arc-like magma source described by Kelemen et al. (2003), which may be inherited from the juvenile crust produced during the Mesoproterozoic oceanic subduction between the Bayan Har Block and East Kunlun Crust.
5.2.2 Magmatic genesis of the Jiangjunmu porphyry deposits
The recognition of the physical and chemical features of porphyry systems could lead to the discovery of concealed ore deposits (Wilkinson, 2013). A better understanding of the genesis of ore-bearing rocks not only provides comprehensive insight into the evolution of magmatic-hydrothermal systems but also facilitates mineral exploration. The Jiangjunmu porphyry deposit formed in a post-collisional tectonic setting, with the ore-bearing rocks forming in the Late Triassic when the Paleo-Tethyan Ocean closed (Yu et al., 2020). This suggests that oceanic subduction is not responsible for the formation of the deposit. Thus, two main diagenesis models have been proposed for the formation of ore-bearing porphyry rocks:
1. Partial melting of the delaminated lower continental crust and interaction with the upwelling hot mantle (Xu et al., 2002; Chung et al., 2003; Wang et al., 2007).
2. Direct partial melting of the thickened lower continental crust (TLCC) or TLCC interaction with the upwelling hot mantle (Chung et al., 2003; Zhao and Zhou, 2008).
The Jiangjunmu granodiorite porphyry (Yu et al., 2020) and K-feldspar granite exhibit relatively high Rb/Sr ratios and Mg# values, consistent with adakites (Figure 7h) formed by the melting of thickened lower continental crust (TLCC) or delaminated lower continental crust (DLCC). Adakites typically have a Rb/Sr ratios >0.05 ppm and Mg# values between 27 and 54 (Drummond et al., 1996; Hou et al., 2004; Alirezaei et al., 2017). Additionally, in the SiO2 variation diagram (Figures 7a–h), all samples of the granodiorite porphyry fall within the overlapping fields of DLCC and TLCC. However, the partial melting of the DLCC would cause the lower continental crust (LCC) to subduct into the deep mantle, with a significantly elevated magma content of MgO, Mg#, Cr, Ni, and Co during magma-mantle interaction. In contrast, the Jiangjunmu granodiorite porphyry (Yu et al., 2020) and K-feldspar granite exhibit relatively low values of MgO, Mg#, Cr, Ni, and Co. Furthermore, the granodiorite porphyry (Yu et al., 2020) and K-feldspar granite have Rb/Sr ratios (0.4–0.44, 0.63–1.02) that distinguish them from newly formed basaltic melts resulting from the partial melting of the DLCC, which typically have Rb/Sr ratios of 0.01–0.05 (Huang et al., 2009). These results suggest that the formation of the Jiangjunmu intrusions is related to the partial melting of TLCC rather than DLCC.
In conclusion, based on the tectonic background and regional research, the Jiangjunmu intrusions (granodiorite porphyry and K-feldspar granite) formed in a post-collisional orogenic extensional setting after the closure of the Paleo-Tethys Ocean. The detachment of the subducted slab, accompanied by extensional forces, led to the thickening of the lower continental crust, which underwent partial melting and interacted with upwelling deep mantle materials. This process resulted in the formation of magma associated with metallogenesis. The magma was subsequently transported along faults and ascended to the near-surface, where it experienced diagenetic alteration and mineralization (Figure 12).
Figure 12. Conceptual model for the Jiangjunmu Au-Cu deposit associated with intrusions (after Xiong, 2014).
6 Conclusion
K-feldspar granite porphyry (234 Ma) intruded by K-feldspar granite (228 Ma) that host the Jiangjunmu Cu–Au deposits in the East Kunlun Orogenic Belt (EKOB), exhibits the following petrogenetic and tectonic implications:
1. The K-feldspar granite magma, with contributions from upper continental crustal material (heterotypic sandstone), likely originated through partial melting of an amphibole–garnet-bearing source within the TLCC. The adjacent granodiorite porphyry may also have originated from a similar amphibole–garnet source, with suppressed plagioclase crystallization during partial melting within the TLCC. The porphyry-hosed MMEs indicate that the Cu (Au) content of the Jiangjunmu deposit may have a mantle-derived origin.
2. The Jiangjunmu porphyry deposit rocks formed in a post-collisional extensional setting during the Late Triassic epoch after the Paleo-Tethyan Ocean closed.
Data availability statement
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding author.
Author contributions
YJ: Writing – original draft, Project administration, Investigation. LD: Writing – original draft, Methodology, Formal Analysis. GY: Methodology, Writing – original draft, Investigation. MB: Writing – original draft, Software, Data curation. ZY: Supervision, Funding acquisition, Writing – original draft. JK: Writing – review and editing, Writing – original draft, Supervision. AT: Writing – review and editing, Software.
Funding
The author(s) declare that financial support was received for the research and/or publication of this article. This work was supported by the following funding sources: Project of State Key Laboratory of Ni & Co associated minerals resources development and comprehensive utilization (No. JKDGNZ26Z202406); Natural Science Foundation project of Gansu Province (No. 24JRC001); Commonwealth project from the Ministry of Land and Resources (No. 1015); Changjiang Scholars and Innovative Research Team in Universities (No. RT14R54); China Geological Survey (Nos 1212011121204, 12120113032800, 21201011000150004).
Acknowledgments
We gratefully acknowledge all project members and sincerely thank Professor Nanshi Zeng from the College of Earth Sciences, Guilin University of Technology, for his valuable suggestions and insightful discussions. We also extend our appreciation to the supporting laboratories for their assistance.
Conflict of interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Generative AI statement
The author(s) declare that no Generative AI was used in the creation of this manuscript.
Any alternative text (alt text) provided alongside figures in this article has been generated by Frontiers with the support of artificial intelligence and reasonable efforts have been made to ensure accuracy, including review by the authors wherever possible. If you identify any issues, please contact us.
Publisher’s note
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.
Supplementary material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2025.1616423/full#supplementary-material
References
Alirezaei, A., Arvin, M., and Dargahi, S. (2017). Adakite-like signature of porphyry granitoid stocks in the meiduk and parkam porphyry copper deposits, NE of Shahr-e-Babak, Kerman, Iran: constrains on geochemistry. Ore Geol. Rev. 88, 370–383. doi:10.1016/j.oregeorev.2017.04.023
Altherr, R., and Siebel, W. (2002). I-type plutonism in a Continental back-arc setting: miocene granitoids and monzonites from the central aegean sea, Greece. Contributions Mineralogy Petrology 143, 397–415. doi:10.1007/s00410-002-0352-y
Bai, Y., Chang, G., and Tan, S. (2001). Study on the characteristics of the Caledonian orogen intrusion in the eastern part of the eastern kunlun. Qinghai Geol. S1, 28–35.
Bai, Y., Sun, F., Qian, Y., Liu, H., and Zhang, D. (2016). Zircon U-Pb geochronology and geochemistry of pyroxene diorite in galinge iron-polymetallic deposit,east kunlun. Glob. Geol. 35 (1), 17–27.
Bodet, F., and Schärer, U. (2000). Evolution of the SE-Asian continent from U-Pb and Hf isotopes in single grains of zircon and baddeleyite from large Rivers. Geochimica Cosmochimica Acta 64, 2067–2091. doi:10.1016/s0016-7037(00)00352-5
Cao, J., Yuan, W., Hao, N., Feng, Y., Chen, X., Duan, H., et al. (2015). Geochronology, geochemistry and geodynamic implications of the gouli area granites in east kunlun Mountains. Geol. Sci. Technol. Inf. 34 (2), 42–51.
Castillo, P. R., Janney, P. E., and Solidum, R. U. (1999). Petrology and geochemistry of Camiguin island, southern Philippines: insights to the source of adakites and other lavas in a complex arc setting. Contributions Mineralogy Petrology 134, 33–51. doi:10.1007/s004100050467
Chen, N., and Li, H. (2002). The polygonal criterion for the treatment of inconsistent age data of granular zircon U-Pb determined by thermal ionization mass spectrometry: a case study for metamorphic rocks from the dabie Mountains and the eastern kunlun deformed. Geol. Sci. Technol. Inf. 21, 24–29.
Chen, B., and Zhai, M. (2003). Geochemistry of late Mesozoic lamprophyre dykes from the taihang Mountains, north China, and implications for the sub-continental lithospheric mantle. Geol. Mag. 140 (1), 87–93. doi:10.1017/s0016756802007124
Chen, G., Pei, X., Li, R., Li, Z., Liu, C., Chen, Y., et al. (2017). Paleo-tethyan Oceanic crust subduction in the eastern section of the east kunlun orogenic belt:geochronology and petrogenesis of the qushi’ang granodiorite. Acta Geol. Sin. Engl. Ed. 91 (2), 565–580. doi:10.1111/1755-6724.13118
Chen, X., Richards, J. P., Liang, H., Zou, Y., Zhang, J., Huang, W., et al. (2019). Contrasting arc magma fertilities in the Gangdese belt, southern Tibet: evidence from geochemical variations of Jurassic volcanic rocks. Lithos 324, 789–802. doi:10.1016/j.lithos.2018.12.008
Chung, S. L., Liu, D., Ji, J., Chu, M. F., Lee, H. Y., Wen, D. J., et al. (2003). Adakites from Continental collision zones: melting of thickened lower crust beneath southern Tibet. Geology 31 (11), 1021–1024. doi:10.1130/g19796.1
Cooke, D. R., Hollings, P., and Walshe, J. L. (2005). Giant porphyry deposits: characteristics, distribution, and tectonic controls. Econ. Geol. 100, 801–818. doi:10.2113/100.5.801
Crawford, A. J., Meffre, S., Squire, R. J., Barron, L. M., and Falloon, T. J. (2007). Middle and late Ordovician magmatic evolution of the macquarie arc, lachlan orogen, New South Wales. J. Earth Sci. 54, 181–214. doi:10.1080/08120090701227471
Davidson, J., Turner, S., Handley, H., Macpherson, C., and Dosseto, A. (2007). Amphibole “sponge” in arc crust? Geology 35, 787–790. doi:10.1130/g23637a.1
Defant, M. J., and Drummond, M. S. (1990). Derivation of some modern arc magmas by melting of young subducted lithosphere. Nature 347, 662–665. doi:10.1038/347662a0
DePaolo, D. J., and Wasserburg, G. J. (1976). Inferences about magma sources and mantle structure from variations of143Nd/144Nd. Geophys. Res. Lett. 3 (12), 743–746. doi:10.1029/gl003i012p00743
Drummond, M. S., Defant, M. J., and Kepezhinskas, P. K. (1996). Petrogenesis of slab-derived trondhjemite–tonalite–dacite/adakite magmas. Earth and Environmental Science Transactions of the Royal Society of Edinburgh 87 (1-2), 205–215. doi:10.1017/s0263593300006611
Eyuboglu, Y., Santosh, M., Dudas, F. O., Chung, S. L., and Akaryalı, E. (2011). Migrating magmatism in a Continental arc: geodynamics of the eastern mediterranean revisited. J. Geodyn. 52 (1), 2–15. doi:10.1016/j.jog.2010.11.006
Feng, C., Li, D., and Wu, Z. (2010). Major types, time-space distribution and metallogeneses of polymetallic deposits in the qimantage metallogenic belt, eastern kunlun area. Northwest Geol. 43, 10–17.
Furman, T., and Graham, D. (1999). “Erosion of lithospheric mantle beneath the East African rift system: geochemical evidence from the Kivu volcanic province,”. Editors R. D. Hilst, and W. F. McDonough, 24, 237–262. doi:10.1016/s0419-0254(99)80014-7Dev. Geotect.
Gao, S., Rudnick, R. L., Yuan, H. L., Liu, X. M., Liu, Y. S., Xu, W. L., et al. (2004). Recycling lower Continental crust in the north China craton. Nature 432, 892–897. doi:10.1038/nature03162
Green, T. H. (1994). Experimental studies of trace-element partitioning applicable to igneous petrogenesis — sedona 16 years later. Chem. Geol. 117, 1–36. doi:10.1016/0009-2541(94)90119-8
Griffin, W. L., Wang, X., Jackson, S. E., Pearson, N. J., O'Reilly, S. Y., Xu, X., et al. (2002). Zircon chemistry and magma mixing, SE China: in-situ analysis of Hf isotopes, tonglu and pingtan igneous complexes. Lithos 61, 237–269. doi:10.1016/s0024-4937(02)00082-8
Hieu, P. T., Anh, N. T., Minh, P., and Thuy, N. T. (2020). Geochemistry, zircon U–PB ages and HF isotopes of the muong luan granitoid pluton, northwest Vietnam and its petrogenetic significance. Isl. Arc 29 (1), e12330. doi:10.1111/iar.12330
Hofmann, A. W. (1997). Mantle geochemistry: the message from Oceanic volcanism. Nature 385, 219–229. doi:10.1038/385219a0
Hou, Z., and Cook, N. J. (2009). Metallogenesis of the Tibetan collisional orogen: a review and introduction to the special issue. Ore Geol. Rev. 36, 2–24. doi:10.1016/j.oregeorev.2009.05.001
Hou, Z. Q., Ma, H. W., Khin, Z., Zhang, Y. Q., Wang, M. J., Wang, Z., et al. (2003). The himalayan yulong porphyry copper belt: product of large-scale strike-slip faulting in eastern Tibet. Econ. Geol. 98, 125–145. doi:10.2113/98.1.125
Hou, Z. Q., Gao, Y. F., Qu, X. M., Rui, Z. Y., and Mo, X. X. (2004). Origin of adakitic intrusives generated during mid-Miocene east–west extension in southern Tibet. Earth Planet. Sci. Lett. 220 (1-2), 139–155. doi:10.1016/s0012-821x(04)00007-x
Hou, Z., Yang, Z., Qu, X., Meng, X., Li, Z., Beaudoin, G., et al. (2009). The Miocene gangdese porphyry copper belt generated during post-collisional extension in the Tibetan orogen. Ore Geol. Rev. 36 (1-3), 25–51. doi:10.1016/j.oregeorev.2008.09.006
Hou, Z., Zhang, H., Pan, X., and Yang, Z. (2011). Porphyry Cu (Mo–Au) deposits related to melting of thickened mafic lower crust: examples from the eastern tethyan metallogenic domain. Ore Geol. Rev. 39, 21–45. doi:10.1016/j.oregeorev.2010.09.002
Hou, Z., Zheng, Y., Yang, Z., Rui, Z., Zhao, Z., Jiang, S., et al. (2013). Contribution of mantle components within juvenile lower-crust to collisional zone porphyry Cu systems in Tibet. Miner. Deposita 48 (2), 173–192. doi:10.1007/s00126-012-0415-6
Hu, Z., Zhang, W., Liu, Y., Gao, S., Li, M., Zong, K., et al. (2015). “wave” signal-smoothing and mercury-removing device for laser ablation Quadrupole and multiple collector icpms analysis: application to lead isotope analysis. Anal. Chem. 87, 1152–1157. doi:10.1021/ac503749k
Huang, F., Li, S., Dong, F., He, Y., and Chen, F. (2008). High-Mg adakitic rocks in the dabie orogen, central China: implications for foundering mechanism of lower Continental crust. Chem. Geol. 255, 1–13. doi:10.1016/j.chemgeo.2008.02.014
Huang, X., Xu, Y., Lan, J., Yang, Q., and Luo, Z. (2009). Neoproterozoic adakitic rocks from mopanshan in the Western yangtze craton: partial melts of a thickened lower crust. Lithos 112, 367–381. doi:10.1016/j.lithos.2009.03.028
Jiang, N., Liu, Y., Zhou, W., Yang, J., and Zhang, S. (2007). Derivation of Mesozoic adakitic magmas from ancient lower crust in the north China craton. Geochim. Cosmochim. Acta 71, 2591–2608. doi:10.1016/j.gca.2007.02.018
Junaid, K., Yao, H. Z., Zhao, J. H., Tahir, A., Chen, K. X., Wang, J. X., et al. (2024). Geochronology, geochemistry, and tectonic setting of the Neoproterozoic magmatic rocks in Pan-African basement, west Ethiopia. Ore Geol. Rev. 164, 105858. doi:10.1016/j.oregeorev.2023.105858
Junaid, K., Yao, H. Z., Chen, K. X., Xu, J. Y., Wang, J. X., Sun, W. G., et al. (2022). Geochemical prospecting of polymetallic mineralization in Gimbi-Nejo area, West Ethiopia. Ore Geol. Rev. 149, 105117.
Kaygusuz, A., Siebel, W., Şen, C., and Satir, M. (2008). Petrochemistry and petrology of I-type granitoids in an arc setting: the composite torul pluton, eastern pontides, NE Turkey. Int. J. Earth Sci. 97, 739–764. doi:10.1007/s00531-007-0188-9
Kelemen, P., Hanghøj, K., and Greene, A. (2003). “One view of the geochemistry of subduction-related magmatic arcs, with an emphasis on primitive andesite and lower crust,” in Treatise on geochemistry. Editors H. D. Holland, and K. K. Turekian (Amsterdam: Elsevier), 593–659.
Kerrich, R., Goldfarb, R., Groves, D., Garwin, S., and Jia, Y. (2000). The characteristics, origins, and geodynamic settings of supergiant gold metallogenic provinces. Earth Sci. 43, 1–68. doi:10.1007/bf02911933
Khan, J., Yao, H., Zhao, J., Li, Q., Xiang, W., Jiang, J., et al. (2023). Petrogenesis and tectonic implications of the tertiary choke shield basalt and Continental flood basalt from the central ethiopian Plateau. J. Earth Sci. 34 (1), 86–100. doi:10.1007/s12583-022-1729-7
Kraus, S. (2005). Magmatic dyke systems of the south shetland islands volcanic arc (west Antarctica): reflections of the geodynamic history. Als Diss., 1–160.
Li, B., and Sun, F. (2010). Genesis and ore-forming mechanism of the yerasai copper deposit in the calcutka region, eastern kunlun, Qinghai province. Acta Petrol. Sina, 3696–3708.
Li, Z., Pei, X., Liu, Z., Li, R., Pei, L., Chen, G., et al. (2013). Geochronology and geochemistry of the Gerizhuotuo diorites from the buqingshan tectonic mélange belt in the southern Margin of East Kunlun and their geologic implications. Acta Geol. Sin. 87 (8), 1089–1103.
Li, R., Pei, X., Li, Z., Pei, L., Chen, G., Chen, Y., et al. (2017). Late Cambrian SSZ-type ophiolites in acite zone, east kunlun orogen of northern Tibet Plateau: insights from zircon U-Pb isotopes and geochemistry of Oceanic crust rocks. Acta Geol. Sin. Engl. Ed. 91 (1), 66–67. doi:10.1111/1755-6724.13189
Lin, Y., Yu, C., Chen, S., Shi, S., Luo, S., and Khan, J. (2025). Paleozoic multi-stage magmatism in the yuka terrane, north qaidam orogenic belt: Mantle modification, tectonic evolution, and geodynamic processes. Front. Earth Sci. 13, 1545127. doi:10.3389/feart.2025.1545127
Ling, M., Wang, F., Ding, X., Zhou, J., and Sun, W. (2011). Different origins of adakites from the dabie Mountains and the lower yangtze river belt, eastern China: geochemical constraints. Int. Geol. Rev. 53, 727–740. doi:10.1080/00206814.2010.482349
Liu, C., Mo, X., and Luo, Z. (2004). The crust-ceramic magmatic mixing in east kunlun: evidence from zircon SHRIMP geochronology. China Sci. Bull. 49, 596–602.
Liu, Y., Hu, Z., Gao, S., Günther, D., Xu, J., Gao, C., et al. (2008). In situ analysis of major and trace elements of anhydrous minerals by LA-ICP-MS without applying an internal standard. Chem. Geol. 257, 34–43. doi:10.1016/j.chemgeo.2008.08.004
Liu, S., Li, S., He, Y., and Huang, F. (2010). Geochemical contrasts between Early Cretaceous ore-bearing and ore-barren high-Mg adakites in central-eastern China: implications for petrogenesis and Cu–Au mineralization. Geochimica Cosmochimica Acta 74, 7160–7178. doi:10.1016/j.gca.2010.09.003
Liu, B., Ma, C., and Zhang, J. (2012). Origin of early Devonian intrusive rocks in the eastern segment of the East Kunlun orogenic belt and its indications for early paleozoic orogenicity. Acta Petrol. Sina 28, 1785–1807.
Liu, J., Feng, C., Zhao, Y., Li, D., Xiao, Y., Zhou, J. H., et al. (2013). Characteristics of intrusive rock, metasomatites, mineralization and alteration in Yemaquan skarn Fe-Zn polymetallic deposit, Qinghai province. Mineral. Deposits 32, 77–93.
Lu, P., Li, J., and Qin, X. (2005). The characteristics and tectonic significance of the lumen tagaqakegan Granitic in the East Kunlun Mountains. Sediment. Tethyan Geol. 25 (4), 46–54.
Ludwig, K. R. (2003). Isoplot 3.00: a geochronological toolkit for microsoft excel. California: Berkeley Geochronology Center.
Macpherson, C. G., Dreher, S. T., and Thirlwall, M. F. (2006). Adakites without slab melting: high pressure differentiation of island arc magma, mindanao, the Philippines. Earth Planet. Sci. Lett. 243, 581–593. doi:10.1016/j.epsl.2005.12.034
Maniar, P. D., and Piccoli, P. M. (1989). Tectonic discrimination of granitoids. Geol. Soc. Am. Bull. 101, 635–643. doi:10.1130/0016-7606(1989)101<0635:tdog>2.3.co;2
McDonough, W. F., Sun, S. S., Ringwood, A. E., Jagoutz, E., and Hofmann, A. W. (1992). Potassium, rubidium, and cesium in the Earth and moon and the evolution of the mantle of the Earth. Geochimica Cosmochimica Acta 56, 1001–1012. doi:10.1016/0016-7037(92)90043-i
Middlemost, E. A. K. (1994). Naming materials in the magma/igneous rock system. Earth Sci. Rev. 37, 215–224. doi:10.1016/0012-8252(94)90029-9
Midea, W. P., Hattori, K., and Valera, G. T. V. (2021). Igneous rocks related to porphyry cu-au mineralization at the dizon mine, Philippines. Resour. Geol. 71 (4), 392–408. doi:10.1111/rge.12273
Mo, X., Luo, Z., Deng, J., Yu, X., Liu, C., Chen, H., et al. (2007). Granitoids and crustal growth in the east-kunlun orogenic belt. Geol. J. China Univiversity 13, 403–414.
Mungall, J. E. (2002). Roasting the mantle: slab melting and the genesis of major Au and Au-rich Cu deposits. Geology 30, 915–918. doi:10.1130/0091-7613(2002)030<0915:rtmsma>2.0.co;2
Pearce, J. A. (1996). Sources and settings of granitic rocks. Episodes 19, 120–125. doi:10.18814/epiiugs/1996/v19i4/005
Pearce, J. A., Harris, N. B. W., and Tindle, A. G. (1984). Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. J. Petrology 25, 956–983. doi:10.1093/petrology/25.4.956
Peccerillo, A., and Taylor, S. R. (1976). Geochemistry of Eocene calc-alkaline volcanic rocks from the Kastamonu area, northern Turkey. Contributions Mineralogy Petrology 58, 63–81. doi:10.1007/bf00384745
Qi, H., Lu, S., Yang, X., Deng, J., Zhou, Y., Zhao, L., et al. (2020). The role of magma mixing in generating granodioritic intrusions related to Cu–W mineralization: a case study from qiaomaishan deposit, eastern China. Minerals 10 (2), 171. doi:10.3390/min10020171
Rapp, R. P. (1995). Amphibole-out phase boundary in partially melted metabasalt, its control over liquid fraction and composition, and source permeability. J. Geophys. Res. Solid Earth 100 (B8), 15601–15610. doi:10.1029/95jb00913
Rapp, R. P., and Watson, E. B. (1995). Dehydration melting of metabasalt at 8-32 kbar: implications for Continental growth and crust-mantle recycling. J. Petrology 36, 891–931. doi:10.1093/petrology/36.4.891
Rapp, R. P., Shimizu, N., Norman, M. D., and Applegate, G. S. (1999). Reaction between slab derived melts and peridotite in the mantle wedge: experimental constraints at 3.8GPa. Chem. Geol. 160, 335–356. doi:10.1016/s0009-2541(99)00106-0
Rapp, R. P., Xiao, L., and Shimizu, N. (2002). Experimental constraints on the origin of potassium-rich adakites in east China. Acta Petrol. Sin. 18, 293–311.
Richards, J. P. (2003). Tectono-magmatic precursors for porphyry Cu-(Mo-Au) deposit formation. Econ. Geol. 98, 1515–1533. doi:10.2113/98.8.1515
Richards, J. P., and Kerrich, R. (2007). Special paper: adakite-Like rocks: their diverse origins and questionable role in metallogenesis. Econ. Geol. 102, 537–576. doi:10.2113/gsecongeo.102.4.537
Richards, J. P., Boyce, A. J., and Pringle, M. S. (2001). Geologic evolution of the escondida area, Northern Chile: a model for spatial and temporal localization of Porphyry Cu mineralization. Econ. Geol. 96, 271–305. doi:10.2113/gsecongeo.96.2.271
Rollinson, H. (2003). Metamorphic history suggested by garnet-growth chronologies in the Isua Greenstone belt, West Greenland. Precambrian Res. 126, 181–196. doi:10.1016/s0301-9268(03)00094-9
Rudnick, R. L., and Gao, S. (2003). “Composition of the continental crust,” in Treatise on geochemistry. Editors H. D. Holland, and K. K. E. Turekian (Oxford: Elsevier–Pergamon), 1–64.
Sillitoe, R. H. (2010). Porphyry copper systems. Econ. Geol. 105 (1), 3–41. doi:10.2113/gsecongeo.105.1.3
Song, X., Yi, J., Chen, L., She, Y., Liu, C., Dang, X., et al. (2016). The giant xiarihamu Ni-Co sulfide deposit in the East Kunlun orogenic belt, northern Tibet Plateau, China. Econ. Geol. 111, 29–55. doi:10.2113/econgeo.111.1.29
Stern, C. R., and Kilian, R. (1996). Role of the subducted slab, mantle wedge and Continental crust in the generation of adakites from the andean Austral volcanic zone. Contributions Mineralogy Petrology 123, 263–281. doi:10.1007/s004100050155
Sun, S. L. (2001). The study on metallogenic series of hydrocarbon alkali fluids in Devonian in Xicheng concentrated mineralization area, west Qinling, Gansu Province. (Ph.D. thesis). Chengdu University of Technology, Chengdu, China.
Sun, S. S., and McDonough, W. F. (1989). Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes. London: Geological Society, London, Special Publications 42 (1), 313–345.
Sun, W., Hu, Y., Kamenetsky, V. S., Eggins, S. M., Chen, M., and Arculus, R. J. (2008). Constancy of Nb/U in the mantle revisited. Geochimica Cosmochimica Acta 72, 3542–3549. doi:10.1016/j.gca.2008.04.029
Sun, W. D., Liu, L. J., Hu, Y. B., Ding, W., Liu, J. Q., Ling, M. X., et al. (2018). Post-ridge-subduction acceleration of the Indian plate induced by slab rollback. Solid Earth Sci. 3 (1), 1–7. doi:10.1016/j.sesci.2017.12.003
Wallace, P., and Carmichael, I. S. E. (1992). Sulfur in basaltic magmas. Geochimica Cosmochimica Acta 56, 1863–1874. doi:10.1016/0016-7037(92)90316-b
Wang, Q., Xu, J. F., Zhao, Z. H., Bao, Z. W., Xu, W., and Xiong, X. L. (2004). Cretaceous high potassiumintrusiverocksintheYueshan-HongzhenareaofeastChina:adakites in an extensional tectonic regime within a continent. Geochem. J. 38, 417–434. doi:10.2343/geochemj.38.417
Wang, Q., McDermott, F., Xu, J., Bellon, H., and Zhu, Y. (2005). Cenozoic K-rich adakitic volcanic rocks in the hohxil area, northern Tibet: lower-crustal melting in an intracontinental setting. Geology 33, 465–468. doi:10.1130/g21522.1
Wang, Q., Xu, J. F., Jian, P., Bao, Z. W., Zhao, Z. H., Li, C. F., et al. (2006). Petrogenesis of adakitic porphyries in an extensional tectonic setting, dexing, south China: implications for the genesis of porphyry copper mineralization. J. Petrology 47 (1), 119–144. doi:10.1093/petrology/egi070
Wang, J., Hattori, K. H., Kilian, R., and Stern, C. R. (2007). Metasomatism of sub-arc mantle peridotites below southernmost South America: reduction of fO2 by slab-melt. Contribution Mineralogy Petrology 153, 607–624. doi:10.1007/s00410-006-0166-4
Wang, F., Zheng, X. S., Lee, J. I., Choe, W. H., Evans, N., and Zhu, R. (2009). An 40Ar/39Ar geochronology on a mid- Eocene igneous event on the barton and weaver peninsulas: implications for the dynamic setting of the antarctic peninsula. Geochem. Geophys. Geosyst. 10 (12). doi:10.1029/2009gc002874
Wang, F., Chen, J., Xie, Z., Li, S., Tan, S., Zhang, Y., et al. (2013). Geological features and Re-Os isotopic dating of the lalingzaohuo molybdenum polymetallic deposit in East Kunlun. Geol. China 40, 1209–1217.
Wang, X., Pei, X., Li, R., Liu, C., Pei, L., Li, Z., et al. (2023). Tectonic background of Carboniferous to early Permian sedimentary rocks in the east kunlun Orogen: constraints from geochemistry and geochronology. Minerals 13 (3), 312. doi:10.3390/min13030312
Wilkinson, J. J. (2013). Triggers for the formation of porphyry ore deposits in magmatic arcs. Nat. Geosci. 6, 917–925. doi:10.1038/ngeo1940
Wu, Y., and Zheng, Y. (2004). Genesis of zircon and its constraints on interpretation of U-Pb age. Chinia Sci. Bull. 49, 1554–1569. doi:10.1007/bf03184122
Wu, F. Y., Sun, D. Y., Li, H., Jahn, B. M., and Wilde, S. (2002). A-type granites in northeastern China: age and geochemical constraints on their petrogenesis. Chem. Geol. 187 (1-2), 143–173. doi:10.1016/s0009-2541(02)00018-9
Wu, X., Meng, F., Xu, H., and Cui, M. (2011). Zircon U- Pb dating, geochemistry and Nd- Hf isotopic compositions of the Maxingdaban Late Triassic granitic pluton from Qimantag in the eastern kunlun. Acta Petrol. Sin. 27 (11), 3380–3394. (in Chinese with English abstract).
Xia, R., Wang, C., Qing, M., Deng, J., Carranza, E. J. M., Li, W., et al. (2015). Molybdenite re–os, zircon U–Pb dating and Hf isotopic analysis of the shuangqing fe–pb–zn–cu skarn deposit, east kunlun Mountains, Qinghai province, China. Ore Geol. Rev. 66, 114–131. doi:10.1016/j.oregeorev.2014.10.024
Xiao, L., and Clemens, J. D. (2007). Origin of potassic (C-type) adakite magmas: experimental and field constraints. Lithos 95, 399–414. doi:10.1016/j.lithos.2006.09.002
Xiong, F. (2014). Temporal and spatial distribution, petrology and geological significance of paleo-tethys granites in the eastern part of eastern kunlun orogenic belt. Wuhan: China University of Geosciences.
Xiong, F., Ma, C., and Zhang, J. (2011). The zircon U-Pb ages and geological significance of the LA-ICP-MS in the bailiqili gabbro in the East kunlun orogenic belt. Geol. Bull. 31, 1196–1202.
Xu, J., Shinjo, R., Defant, M. J., Wang, Q., and Rapp, R. P. (2002). Origin of Mesozoic adakitic intrusive rocks in the ningzhen area of east China: partial melting of delaminated lower Continental crust? Geology 30, 1111–1114. doi:10.1130/0091-7613(2002)030<1111:oomair>2.0.co;2
Xu, Q., Sun, F., and Li, B. (2014). Geochronology, geochemical characteristics, and tectonic setting of granite porphyry in the mohe xiala silver polymetallic deposit, east kunlun. Geotect. metallogenia 38 (02), 421–433.
Xu, X., Li, H., Peters, S. G., Qin, K., Mao, Q., Wu, Q., et al. (2017). Cu-rich porphyry magmas produced by fractional crystallization of oxidized fertile basaltic magmas (sangnan, east junggar, PR China). Ore Geol. Rev. 91, 296–315. doi:10.1016/j.oregeorev.2017.09.020
Yu, J. Z., Zheng, Y. Y., Xu, R. K., Hou, W. D., and Cai, P. J. (2020). Zircon U-Pb chronology, geochemistry of jiangjunmu ore-bearing pluton, eastern part of east kunlun and their geological significance. Earth Sci. 45 (4), 1151–1167.
Yu, J., Li, D., Zheng, Y., Ma, B., Wang, J., Shi, G., et al. (2025). Syn-to post-orogenic mineralization in the Shuangkoushan Au–Ag–Pb deposit, North Qaidam: insights from H–O–S isotopes and U–Pb geochronology. Front. Earth Sci. 13, 1609741. doi:10.3389/feart.2025.1609741
Yuan, W., and Mo, X. (2000a). Granite records of regional tectonic of east kunlun in indosinian. Geol. Rev. 46, 203–211.
Yuan, W., and Mo, X. (2000b). The record of Granite in the back of the Indosinian regional structure in Kunlun. Geol. Rev. 46, 203–211.
Zeng, Y., Chen, J., Xu, J., Lei, M., and Xiong, Q. (2017). Origin of miocene cu-bearing porphyries in the zhunuo region of the southern lhasa subterrane: constraints from geochronology and geochemistry. Gondwana Res. 41, 51–64. doi:10.1016/j.gr.2015.06.011
Zengqian, H., Ma, H., Zaw, K., Zhang, Y., Mingjie, W., Zeng, W., et al. (2003). The himalayan yulong porphyry copper belt: product of large-scalestrike-slip faulting in eastern Tibet. Econ. Geol. 98 (1), 125–145. doi:10.2113/gsecongeo.98.1.125
Zhao, J., and Zhou, M. (2008). Neoproterozoic adakitic plutons in the northern margin of the yangtze block, China: partial melting of a thickened lower crust and implications for secular crustal evolution. Lithos 104, 231–248. doi:10.1016/j.lithos.2007.12.009
Zhao, Y., Ao, W., Zhang, H., and Wang, Q. (2020). Possible imprints of late Paleoproterozoic orogeny in the Dunhuang terrane, NW China: constraints from igneous and metapelitic rocks. Precambrian Res. 350, 105918. doi:10.1016/j.precamres.2020.105918
Zheng, Y. Y., Wang, B., Fan, Z. H., and Zhang, H. P. (2002). Analysis of tectonic evolution in the eastern section of the Gangdese mountains, Tibet and the metallogenic potentialities of copper gold polymetal. Geol. Sci. Technol. Inf. 21, 55–60.
Zhu, D. C., Zhao, Z. D., Pan, G. T., Lee, H. Y., Kang, Z. Q., Liao, Z. L., et al. (2009). Early Cretaceous subduction-related adakite-like rocks of the gangdese belt, southern Tibet: products of slab melting and subsequent melt–peridotite interaction? J. Asian Earth Sci. 34 (3), 298–309. doi:10.1016/j.jseaes.2008.05.003
Zindler, A., and Hart, S. R. (1986). Chemical geodynamics. Annu. Rev. Earth Planet. Sci. 14, 493–571. doi:10.1146/annurev.ea.14.050186.002425
Zong, K., Klemd, R., Yuan, Y., He, Z., Guo, J., Shi, X., et al. (2017). The assembly of rodinia: the correlation of early Neoproterozoic (Ca. 900 ma) high-grade metamorphism and Continental arc formation in the southern beishan orogen, southern central asian orogenic belt (CAOB). Precambrian Res. 290, 32–48. doi:10.1016/j.precamres.2016.12.010
Keywords: Jiangjunmu granodiorite porphyry, Jiangjunmu K-feldspar granite, East Kunlun metallogenic belt, mafic magmatic enclaves, thickened lower continental crust
Citation: Junzhen Y, Dexian L, Yalin G, Bo M, Youye Z, Khan J and Tahir A (2025) Petrogenesis and tectonic implications of intrusive rocks in the Jiangjunmu porphyry deposit, East Kunlun orogeny, NW China. Front. Earth Sci. 13:1616423. doi: 10.3389/feart.2025.1616423
Received: 22 April 2025; Accepted: 08 September 2025;
Published: 03 October 2025.
Edited by:
Daniel Kwayisi, University of Ghana, GhanaReviewed by:
Patrick Asamoah Sakyi, University of Ghana, GhanaZayyanu Usman Magawata, Kebbi State University of Science and Technology Aliero, Nigeria
Minh Pham, Ho Chi Minh City University of Science, Vietnam
Copyright © 2025 Junzhen, Dexian, Yalin, Bo, Youye, Khan and Tahir. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Junaid Khan, SnVuYWlka2hhbjU2MTVAeWFob28uY29t