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Article

Chronology and Geochemistry of Intrusive Magmatic Rocks in the Shiquanhe Ophiolitic Mélange, Tibet: Constraints on the Tectonic Evolution of the Meso-Tethys Ocean

by
Kegang Dai
1,2,†,
Xu Zhang
1,3,†,
Ru-Xin Ding
4,*,
Harald Furnes
5,
Wei-Liang Liu
1,*,
Xiaobo Kang
2,
Hongfei Zhao
2,
Jing Li
2,
Qin Wang
6,
Yun Bai
7,
Chi Yan
1 and
Yutong Shi
1
1
Guangdong University Key Laboratory of Offshore Oil Exploration and Development/Guangdong Provincial Key Laboratory of Marine Resources and Coastal Engineering, School of Marine Sciences, Sun Yat-Sen University, Zhuhai 519082, China
2
The Fifth Geological Brigade, Tibet Bureau of Geology and Mineral Exploration and Development, Lhasa 850000, China
3
College of Engineering and Technology, Baoshan University, Baoshan 678000, China
4
Guangdong Provincial Key Lab of Geodynamics and Geohazards, School of Earth Sciences and Engineering, Sun Yat-Sen University, Zhuhai 519082, China
5
Department of Earth Science, University of Bergen, Allegt. 41, 5007 Bergen, Norway
6
College of Earth and Planetary Science, Chengdu University of Technology, Chengdu 610081, China
7
Sichuan Institute of Comprehensive Geological Survey, Chengdu 611231, China
*
Authors to whom correspondence should be addressed.
†
These authors have contributed equally to this work.
Minerals 2026, 16(2), 123; https://doi.org/10.3390/min16020123
Submission received: 16 November 2025 / Revised: 20 January 2026 / Accepted: 20 January 2026 / Published: 23 January 2026
(This article belongs to the Special Issue Petrological, Geochemical and Geodynamic Study of Ophiolites and Modern Oceanic Lithosphere)
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Abstract

Magmatic activity is crucial for identification of the tectonic framework of the ancient oceanic crust. In this study, systematic investigation, including a field survey, zircon LA-ICP-MS U-Pb dating, and whole-rock geochemical analysis, has been carried out on the intrusive quartz- and granodiorites within the Meso-Tethyan Shiquanhe Ophiolitic Mélange (SQM), Tibet. Zircon U-Pb dating yields the weighted mean ages of 174.7 ± 1.4 Ma (quartz diorite) and 178.9 ± 1.2 Ma (granodiorite), respectively, demonstrating the Early Jurassic formation age. The quartz diorite samples are metaluminous (A/NKC = 0.77–0.95) (molar/Al2O3/(CaO + Na2O + K2O)), while the granodiorite samples are weakly peraluminous (A/NKC = 0.95–1.21), and both of them exhibit tholeiitic to calc-alkaline geochemical characteristics and can be classified as I-type granites. The right-dipping rare-earth element (REE) patterns, enrichment in large ion lithophile elements (LILEs: Rb, Ba, Th), and depletion in high-field-strength elements (HFSEs: Nb, Ta, Ti), as well as relatively high (La/Yb)N ratios, are features compatible with an island arc setting. Combined with previous works, we suggest that the Shiquanhe ophiolitic mélange not only preserves records of mid-late Jurassic island arc magmatic activity but also contains evidence of island arc magmatism from the late Early Jurassic.

1. Introduction

As a global Paleo-ocean system between the Gondwana and Laurasia supercontinents during the Phanerozoic [1,2], the Tethyan tectonic domain serves as a natural laboratory for deciphering the mechanisms of ocean–continent transition, plate interaction, and continental growth and has been a focused and long-standing topic of research [3,4,5,6,7]. Suture zones and associated ophiolites in the Tibetan Plateau provide a record for over 500 million years of Tethyan tectonic evolution, which include the Proto-Tethyan West Kunlun suture, Paleo-Tethyan Kunlun, Jinsha and Shuanghu sutures, Meso-Tethyan Bangong suture, and Neo-Tethyan Yarlung-Zangbo suture [1,8]. This research provides crucial evidence for reconstructing the tectonic evolution of ancient oceans. Among them, the Shiquanhe-Namtso Ophiolitic Mélange Zone (SNMZ) and Bangong-Nujiang Suture Zone (BNSZ), which separate the Qiangtang terrane to the north and the Lhasa terrane to the south, represent the remnants of the Meso-Tethyan ocean [1,9]. The accurate definition of their tectonic attributes holds irreplaceable scientific value for clarifying the central tectonic framework of the Tibetan Plateau and reconstructing the evolutionary process of the Meso-Tethys Ocean.
In contrast to the extensive attention and research received by the Bangong-Nujiang Suture Zone [10,11,12,13,14,15,16], the Shiquanhe-Namtso Ophiolitic Mélange Zone has attracted relatively low research interest. However, several hypotheses have been proposed regarding its tectonic nature, such as (1) the southward tectonic nappe of the Bangong-Nujiang Suture Zone [17,18]; (2) the island arc and back-arc basin system formed by the subduction of the Bangong Meso-Tethys [19,20,21,22,23]; and (3) the remnants of an independent oceanic crust [24,25]. The intrusive magmatic rocks are important components of the SNMZ and provide important spatial and temporal information besides that of the volcanic rocks. The Shiquanhe Ophiolitic Mélange (SOM) is located at the west end of the SNMZ (Figure 1) and plays an important role in terms of the tectonic evolution of this mélange zone. During the investigation of the ophiolite and related rocks, it has been demonstrated that two stages of nascent intra-oceanic arcs developed during the Jurassic: the Early Jurassic (ca. 190–180 Ma) and the Middle-Late Jurassic nascent intra-oceanic arc (ca. 170–160 Ma) ([20,23,26,27,28,29] and references therein). Among these, research on the evolution of the Middle-Late Jurassic nascent intra-oceanic arc into a mature island arc has been widely reported and recognized ([20,23,27,29] and references therein). However, whether the Early Jurassic nascent intra-oceanic arc evolved into a mature island arc system over time remains unknown. In this contribution, we systematically collected representative intrusive rocks samples within the Shiquanhe Ophiolitic Mélange by detailed field surveys. Through analyses of spatial distribution and contact relation with country rocks, petrographic classification, whole-rock geochemical analysis, and zircon U-Pb chronological dating, this study report newly discovered Early Jurassic island arc granitic rocks from the Shiquanhe area in the west end of the SNMZ. This research has led to further discussions regarding its implications for the tectonic framework of the Shiquanhe Ophiolitic Mélange with Bangong Suture.

2. Geological Background and Sample Locations

From north to south, the Tibetan Plateau is divided into several major parts by the Jinsha suture zone (JSSZ), Longmu-Shuanghu suture zone (LSSZ), BNSZ, SNMZ, and Indus-Yarlung Tsangpo suture zones (IYTSZ), including the Songpan-Ganzi, Northern Qiangtang (NQ), Southern Qiangtang (SQ), Lhasa, and Himalaya terranes (Figure 1a) [30,31,32,34,35,36,37]. The BNSZ starts at the Bangong Lake (at the western end), passing through the Gerze, Dongqiao, Amdo, and Dingqing, and terminates at the Nujiang ophiolite to the east. The SNMZ begins in the Shiquanhe (at the western end), passing through the Asa, Yongzhu, Namu Tso, and Jiali and extends to the east (Figure 1b) [27,31,36].
The selected study area is located near Shiquanhe Town (Figure 1b). As the largest exposed ophiolitic section in the west part of SNMZ, the ophiolitic mélanges in this region generally extend in a northwest direction, spanning over 60 km [20,26,27,33]. The diorite intrusions studied for this work are exposed in the Banglongchamu and Qionggaleniao areas of the Shiquanhe region and mainly intrude into the Shianne Ophiolitic Mélange as stocks and bosses (Figure 1c and Figure 2a,c). They extend in an east–west direction and have a total outcrop area of approximately 6.5 km2. The primary rock types include quartz diorite, tonalite, and granodiorite.

3. Field Relations and Petrography

The granodiorite bodies occur primarily as lenses intruding serpentinized harzburgite (Figure 2a). It shows a gray to white color and exhibits a fine-grained, granitic texture and a massive structure. Under the microscope, it is composed of plagioclase, K-feldspar, quartz, amphibole, and biotite. Plagioclase constitutes about 4–50 vol. %, occurring as hypidiomorphic tabular crystals, with grain sizes generally 0.2–2 mm, and shows well-developed zoning structures, as well as polysynthetic twinning. The crystals are randomly distributed and have suffered kaolinization and sericitization alteration. K-feldspar is about 5–10 vol. % and occurs as anhedral granular crystals, mainly microcline, with grain sizes typically 0.5–3.5 mm. They are distributed interstitially, with slight kaolinization, and perthitic twinning is visible. Quartz is about 20–25 vol. % and occurs as anhedral granular crystals, with grain sizes usually 2–6 mm. They are distributed interstitially, with obvious recrystallization and local grain refinement at the edges. Distinct undulatory extinction is present within grains. Amphibole is approximately 5 vol. % and occurs as hypidiomorphic-anhedral prismatic or prism-granular crystals, with grain sizes 0.2–2 mm, and some grains form pseudomorphs. They are distributed randomly, with alterations such as uralitization and chloritization. Biotite is about 5–10 vol. % and occurs as flaky crystals, with flake diameters about 0.2–2 mm. They are distributed randomly, and most grains are replaced by chlorite, muscovite, or epidote to form pseudomorphs, with titanium minerals precipitated. The accessory minerals mainly include zircon and apatite (Figure 2b).
The quartz diorite is primarily gray to light-gray in color. It occurs as lenses intruding into gabbroic complex (Figure 2c) and exhibits a medium- to fine-grained, subhedral granular texture and a massive structure. Under the microscope, it is composed of plagioclase, quartz, amphibole, and pyroxene. Plagioclase dominates and accounts for about 50–60 vol. %, occurring as hypidiomorphic tabular crystals, with a visible zoning structure, and polysynthetic twinning is common. The grain size ranges from 0.2 to 2 mm with a slight directional arrangement of long axes, which are randomly distributed with alterations to parts of sericitization, kaolinization, and epidotization. Quartz defines approximately 10 vol. %, occurring as anhedral granular crystals, with grain sizes typically 1–5.5 mm. The crystals are distributed interstitially, with undulatory extinction observed within grains. Amphibole is about 20 vol. % and occurs as hypidiomorphic prismatic or prism-granular crystals, with grain sizes mostly 0.2–2 mm (a few 3.5 mm). They are distributed randomly, and aggregates exhibit a slight orientation of banded or striped appearance. A small number of grains are replaced by uralite, chlorite, or epidote. The accessory minerals mainly include magnetite and epidote (Figure 2d).

4. Analytical Methods

4.1. Zircon U-Pb Geochronological Analysis

Two diorite samples (PM204TW1, quartz diorite and PM207TW1, granodiorite) were collected for separation, target preparation, morphological observation, imaging, and U-Pb analysis conducted at Beijing ZKKY GeoAnalysis Laboratory Co., Ltd. (Beijing, China). The procedures were as follows: rock samples were first crushed to 50–80 mesh, followed by separation of zircon, titanite, and rutile via heavy liquid and magnetic separation techniques. Selected zircons were mounted in epoxy resin, initially polished with 7000-grit silicon carbide paper, then finely polished with 0.05 μm alumina powder and cleaned to ensure clear visualization of external features before target preparation. Cathodoluminescence (CL) imaging was performed using a MIRA3 field emission scanning electron microscope (TESCAN ORSAY HOLDING, a.s., Brno, Czech Republic) with an acceleration voltage of 7 kV and 120 s exposure time to obtain clear oscillatory zoning patterns. Based on transmitted, reflected, and CL images, zircon grains with intact surfaces and host-rock characteristics were selected for U-Pb isotopic analyses. Subsequent zircon U-Pb isotopic analyses were conducted at the same laboratory using an Agilent 7500 ICP-MS (Agilent, San Clara, CA, USA) equipped with a 193 nm laser ablation system (ESI NWR). Helium was used as the carrier gas, mixed with argon (as balance gas) via a Y-shaped mixer prior to ICP introduction to optimize detection sensitivity. Each analytical spot included a 15–20 s blank signal acquisition followed by 45 s of sample signal collection, and the detailed procedures follow the description of [38]. Zircon 91500 (1062 Ma) was employed as the external standard to correct for instrumental mass discrimination and elemental fractionation, with GJ-1 (600 Ma) and Plešovice (337 Ma) serving as quality control standards for geochronology. Raw data were processed offline using ICPMSDataCal 11.8 software [39], and weighted mean age calculations and concordia diagrams were generated using Isoplot/Ex_ver3 4.15 [40].

4.2. Major and Trace Element Analyses

The determination of major element contents in the samples of this study was conducted at ALS Minerals (Guangzhou) Co., Ltd. (Guangzhou, China). The specific measurement procedure was as follows: first, the powder samples, sieved through a 200-mesh sieve, were fused using lithium borate-lithium nitrate as the flux. After the melt cooled, it was dissolved with diluted nitric acid and hydrochloric acid. Following dissolution, the samples were analyzed by X-ray fluorescence spectrometry, with the minimum detectable concentration of each major element being 0.01%. For the determination of loss on ignition (LOI), the high-temperature ignition method was employed. The analytical process was roughly as follows: the prepared samples to be tested were placed in a muffle furnace and heated at a high temperature (1000 °C) for 1 h. After cooling, the samples were weighed. The ratio represented by the weight difference before and after heating the samples was the percentage of loss on ignition. The FeO concentration was measured using a volumetric procedure.
The analysis of trace element contents was carried out at Nanjing FocuMS Technology Co., Ltd. (Nanjing, China), The digestion procedure was as follows: (1) An accurately weighed 40 mg portion of the powder sample to be tested was placed in a polytetrafluoroethylene (PTFE) digestion bomb, followed by the addition of a digestion solution consisting of 0.5 mL concentrated nitric acid and 1.0 mL concentrated hydrofluoric acid. The digestion bomb containing the powder sample and digestion solution was then sealed with a steel jacket and placed in an oven set at 195 °C for 72 h to ensure complete digestion of the sample. The digested solution was evaporated to a wet salt state on a hot plate, after which 1 mL of internal standard Rh and 5 mL of nitric acid with a mass fraction of 40% were added. The digestion bomb was resealed and returned to the same temperature oven overnight. (2) Approximately 6 mL of the digested solution was transferred to a centrifuge tube and weighed on a balance. An appropriate amount of the solution was then taken and diluted appropriately (at a dilution ratio of 2000 times relative to the solid weight). The solution was subsequently heated to an aerosol state and introduced into an Agilent 7700x ICP-MS (Agilent, San Clara, CA, USA) (inductively coupled plasma mass spectrometer) for the determination of trace element contents in the samples. The precision for the major element analysis is better than ±1%–2% for a concentration of 0.5 wt.% and for the trace elements precisions is better than ±5%.

5. Results

5.1. Zircon U-Pb Geochronology

The results of zircon U-Pb dating analysis on the granodiorite and quartz diorite are shown in Supplementary Table S1. In the cathodoluminescence (CL) images (Figure 3a), the analyzed zircon grains from the quartz diorite sample (PM204TW1) range in length from sixty to a few hundred microns and have sharp and clear edges. In addition, all of them exhibit oscillatory zoning, a characteristic feature of zircons that crystallized from magmas [41]. For the granodiorite sample (PM207TW1), the zircon grains are mainly acicular and prismatic with clear edges and corners (Figure 3b). Moreover, these zircons exhibit distinct oscillatory zoning (Figure 3b), which is consistent with the characteristic features of zircons crystallized from acidic magma [41]. Their Th/U ratios (0.27–0.59, PM204TW1; 0.36–0.58, PM207TW1, respectively) are higher than those of metamorphic zircons (Supplementary Table S1) and are consistent with characteristic features of magmatic zircons [42].
For quartz diorite sample PM204TW1, 18 spots were analyzed on 18 zircons, all of which yielded relatively concordant ages. The 236Pb/238U ages of the concordant spots are continuously distributed between 171 ± 4 Ma and 179 ± 4 Ma, yielding a weighted mean age of 174.7 ± 1.4 (Mean Square of Weighted Deviates, MSWD = 0.39) and a concordia age of 174.3 ± 1.7 Ma (MSWD = 0.45) (Figure 3a). A total of 31 measurement points were analyzed on 31 zircon grains, and 31 concordant ages were obtained for granodiorite sample PM207TW1. The zircon 236Pb/238U ages of these 31 concordant spots range from 172 ± 6 Ma to 193 ± 7 Ma, yielding a weighted mean age of 178.9 ± 1.2 Ma (MSWD = 2.6) and a concordia age of 180.1 ± 1.6 Ma (MSWD =0.97) (Figure 3b).

5.2. Whole-Rock Major and Trace Elements

5.2.1. Quartz Diorite

The SiO2 content of the quartz diorite samples ranges from 55.49 wt. % to 61.66 wt. %, with an average of 58.49 wt. %, belonging to intermediate rocks. Their abundant quartz justifies classification as quartz diorite, consistent with granitic rock compositions. Their contents of K2O and P2O5 are 0.42–0.80 wt. % and 0.06–0.08 wt. %, respectively. Moreover, they have high MgO and Fe2O3t content (3.45–5.68 wt. % and 7.08–10.24 wt. %) (Supplementary Table S2). Their differentiation index (DI) (Normative Minerals Q + Ab + Or + Ne + Kp + Lc (wt. %)) [43] ranges from 39.18 to 48.96 (average: 42.93), and the solidification index (SI) (100 × MgO/(MgO + FeO + Fe2O3 + Na2O + K2O)) [44] ranges from 26.15 to 30.32 (average: 28.82), indicating a low degree of magma differentiation. The Rittmann index (σ) ((Na2O + K2O)2/(SiO2-43)) [45] ranges from 0.44 to 0.95 (average: 0.64), indicating the calcic series. The aluminum saturation index (A/NKC) (A/CNK = molar Al2O3/(CaO + Na2O + K2O)) [46] ranges from 0.77 to 0.95 (average: 0.87), and the A/NK (A/NK = molar/Al2O3/(Na2O + K2O)) [46] ratio ranges from 2.72 to 3.69 (average: 3.22), thus classifying them as belonging to the metaluminous rocks.
In the total alkali-silica (TAS) diagram [47], the samples plot in the field of the subalkaline series (Figure 4a). In the normative mineral An-Ab-Or diagram [48] (Figure 4b), the samples plot in the tonalite field, which is consistent with the microscopic identification as quartz diorite. When further plotted in the F-A-M classification diagram [49] (Figure 4c), the samples fall into the field of the calc-alkaline series. In the K2O-SiO2 variation diagram [50] (Figure 4d), two samples fall into the low-K (tholeiitic) series field and other samples fall into the calc-alkaline series field, indicating low-potassium characteristics.
The total REE content (ΣREE) of the quartz diorite samples ranges from 25.53 to 29.66 ppm, with an average of 27.43 ppm, indicating a low total REE content (Supplementary Table S2). The ratio of ΣLREE/ΣHREE ranges from 2.29 to 3.42, with an average of 2.99, indicating insignificant LREE-HREE fractionation. The Eu anomaly (δEu) (δEu = EuN/(SmN × GdN)1/2) ranges from 1.15 to 1.34, with an average of 1.26, showing weak Eu enrichment, indicating the mantle-derived magma source. The Ce anomaly (δCe) (δCe = 2 × CeN/(La+Pr)N) (“N” refers to chondritie normalized value by [52]) ranges from 0.96 to 1.02, with an average of 0.99, showing without obvious Ce depletion or enrichment. The chondrite-normalized ratios are as follows: (La/Yb)N = 1.34–2.58 (average: 2.14), (Ce/Yb)N = 1.23–2.07 (average: 1.73), and (Gd/Yb)N = 0.64–0.78 (average: 0.72). All these values indicate a weak LREE enrichment and insignificant REE fractionation. The REE distribution pattern curve is a nearly horizontal smooth curve (Figure 5a).
Among the quartz diorite samples, the contents of Cs, Sc, and V are 1.24–4.05 ppm, 19.8–249 ppm, and 185–287 ppm, respectively. The Rb/Sr ratio of the quartz diorite samples ranges from 0.03 to 0.12 (average: 0.09). The other trace element ratios are as follows: Rb/Ba = 0.07–0.14 (average: 0.10), K/Rb = 189.54–273.52 (average: 228.81), Zr/Hf = 37.63–41.87 (average: 39.85), and Nb/Ta = 3.98–15.74 (average: 8.6). In the trace element spider diagram (Figure 5b), large ion lithophile elements (LILEs) such as K, Rb, Sr, and Ba are relatively enriched, while high-field-strength elements (HFSEs) are relatively depleted, with obvious Nb depletion, indicating that the samples show normal arc granite characteristics.

5.2.2. Granodiorite

The SiO2 content of the granodiorite ranges from 68.72 wt. % to 70.02 wt. %, with an average of 69.25%, thus belonging to the composition of acid rocks. Meanwhile, based on their microscopic features (such as the presence of abundant quartz and amphibole), they can be classified as granodiorite. Compared to the quartz diorite, the granodiorite samples have lower MgO (1.65–2.45 wt. %) and Fe2O3t (3.20–4.70 wt. %) content and higher content of K2O and P2O5 (2.36–2.75 wt.% and 0.08–0.10 wt. %, respectively) (Supplementary Table S2). Their differentiation index (DI) ranges from 65.56 to 75.43 (average: 71.43), and the solidification index (SI) ranges from 16.65 to 21.38 (average: 19.1), indicating a moderate degree of magmatic differentiation. The Rittmann index (σ) ranges from 0.7 to 1.25 (average: 1.0), belonging to the calcic series. The aluminum saturation index (A/NKC) ranges from 0.95 to 1.21 (average: 1.06), and the A/NK ratio ranges from 1.77 to 2.28 (average: 1.96), indicating weakly peraluminous rocks. In the CIPW normative minerals, the corundum (C) content ranges from 0 to 2.55 wt. %, but the mineral was not observed under the microscope. In the normative mineral An-Ab-Or diagram (Figure 4), most samples plot in the granodiorite field, which is consistent with the microscopic identification. In the total alkali-silica (TAS) diagram (Figure 4a), the samples are classified as belonging to the subalkaline series. When further discriminated by the F-A-M classification diagram (Figure 4c), the granodiorite samples also fall into the calc-alkaline series field, which is consistent with the calc-alkaline characteristics as they are also displayed in the K2O-SiO2 diagram (Figure 4d).
The total REE content (ΣREE) is relatively low and ranges from 104.35 to 122.65 ppm, with an average of 113.16 ppm. The ΣLREE/ΣHREE ratio ranges from 6.41 to 9.97, with an average of 8.27, showing significant LREE-HREE fractionation. The Eu anomaly (δEu) ranges from 0.706 to 1.036, with an average of 0.84, and the Ce anomaly (δCe) ranges from 0.88 to 0.98, with an average of 0.93, indicating the depletion of Eu and Ce. The chondrite-normalized ratios are as follows: (La/Yb)N = 6.20–12.40 (average: 9.03), (Ce/Yb)N = 4.8–8.49 (average: 6.78), and (Gd/Yb)N = 1.37–1.89 (average: 1.58). These values indicate LREE enrichment and significant REE fractionation, which is also displayed in the right-dipping distribution patterns, as shown in Figure 5.

6. Discussion

6.1. Formation Ages of the Quartz Diorite and Granodiorite

Through detailed field geological surveys, it can be established that the granodiorite of this study intrudes the Jurassic ophiolitic harzburgite and that the quartz diorite intrudes the Jurassic ophiolitic gabbro complexes. These observations thus constrain the intrusion ages to be contemporary with the formation of the Jurassic ophiolite or later. The zircon U-Pb dating of this study yields the weighted mean ages of 174.7 ± 1.4 Ma and 178.9 ± 1.2 Ma for quartz diorite and granodiorite samples, respectively (Figure 3a,b). We thus conclude that these intrusive rocks formed in Early Jurassic time. Furthermore, these ages are contemporary with that of the newly obtained forearc setting of the ophiolitic gabbros north of Lameila [23], and the two samples of granodiorite and quartz diorite are both derived from the Shiquanhe ophiolitic mélange. Therefore, we propose that they might preserve evidence of magmatic activity linked to the Early Jurassic evolution of the oceanic crust in the Shiquanhe area.

6.2. Petrogenesis

6.2.1. Influence of Alteration

To investigate the petrogenesis of the intrusive rocks from the Shiquanhe ophiolitic mélange, we need to estimate alteration effect on the samples. As shown in Supplementary Table S2, the quartz diorite and granodiorite samples exhibit relatively low loss on ignition (LOI) values (1.68–2.82 wt. %), indicating that they have not been significantly affected by alteration or metamorphism. This is also consistent with the microscopic observations (Figure 2b,d). Consequently, we find it justifiable to use the elemental compositions and their ratios as proxies for the original composition of these rocks and to discuss the petrogenesis and tectonic environment of these samples.

6.2.2. Petrogenesis of Quartz Diorite

In the A/CNK-A/NK diagram [46] (Figure 6a), the quartz diorites plot in the metaluminous field, which is consistent with the late Early Jurassic granitic rocks in the Lhaguotso area within the BNSZ [29]. This suggests that the quartz diorite samples in this study may have I-type granite features, i.e., formed by partial melting of an unweathered igneous source rock, which is further supported by the (Zr + Nb + Y + Ce) vs. FeOt/MgO [53] and SiO2 vs. P2O5 [29] diagrams (Figure 6b,c). Further, the high MgO and Fe2O3t contents of the quartz diorites are comparable with those of the Lhaguotso plagiogranites, Shiquanhe High-Mg andesites [20] within the SNMZ and Archean Sanukitic rocks, post-Archean High-Mg adakites, and boninites [54,55,56,57]. These intermediate-acid rocks enriched in mafic components are interpreted as a significant contribution of mantle-derived components to their source [29]. In addition, the low Rb/Sr and Rb/Ba ratios, lower Th contents, and relatively weak light rare-earth element (LREE) enrichments of the quartz diorites also suggest that these rocks were formed from a mantle-derived magma source. This implies that the magma of the quartz diorite samples probably contained a significant mafic component. In the C/MF vs. A/MF diagram (A/MF = Al2O3/(MgO + FeOt), C/MF = CaO/(MgO + FeOt)) [58] (Figure 6d), the quartz diorite samples plot within the field of partial melting of mafic rocks, implying an origin represented by partial melting of a mafic rock component.
In the CaO/(FeOt + MgO + TiO2) vs. (FeOt + MgO + TiO2 + CaO) [59], Rb/Ba vs. Rb/Sr [60], and Th/La vs. Th [61] diagrams, the quartz diorite samples, similar to the Lhaguotso high-Mg granites within the SNMZ [29], all plot in fields close to amphibolite, metabasalt, or mid-ocean ridge basalt (MORB) (Figure 7a–c). This supports the inference of a mantle-derived source without obvious crust material input. Additionally, the quartz diorite samples in this study, analogous to the Laguocuo high-Mg granites, are characterized by low Th content and high U/Th ratios, and they both fall into the field of sediment-free island arc volcanic rocks in the U/Th vs. Th diagram [20,62] (Figure 7d). Hence, we conclude that the magma of the quartz diorite was derived from the melting of mantle-derived mafic rocks, without any obvious addition of crustal material.

6.2.3. Petrogenesis of Granodiorite

As discussed in Section 5.2, the granodiorites have higher SiO2, K2O, and P2O5 and lower MgO and Fe2O3t than the quartz diorites. This implies that the magma properties of the granodiorites were different from those of the quartz diorites. Meanwhile, the granodiorites have higher A/CNK values than the quartz diorites, as shown in Figure 6a. They plot within the field of previously identified coeval granodiorites and tonalites from the Shiquanhe area [29] and share similar characteristics with them, with some samples also exhibiting peraluminous signatures (Figure 6a). This suggests that the granodiorites exhibit transitional characteristics towards S-type granites (i.e., formed by the partial melting of sedimentary rock). This conclusion is further supported by their relatively uniform FeOt/MgO ratios and variable (Zr + Nb + Y + Ce) contents (Figure 6b). The granodiorites plot across a wide range in the C/MF vs. A/MF diagram (Figure 6d), overlapping the partial melting fields for metamorphic mudstone, metamorphic greywackes, and mafic rocks. This distribution emphasizes their transitional character towards S-type granites and indicates the input of sedimentary-derived material into the magma.
The granodiorite samples exhibit uniform FeOt + MgO + TiO2 + CaO contents and variable CaO/(FeOt + MgO + TiO2) ratios, and they plot analogously to coeval granitic rocks from the Shiquanhe area in the CaO/(FeOt + MgO + TiO2) vs. (FeOt + MgO + TiO2 + CaO) diagram (Figure 7a), distributing in the mafic and amphibolite fields. This suggests the mafic rock origin of their magma. Meanwhile, the granodiorite samples plot in or close to the field of the Shiquanhe coeval granitic rocks in the Rb/Ba vs. Rb/Sr, Th/La vs. Th diagrams (Figure 7b,c). Moreover, the granodiorite in this study, along with coeval granitic rocks from the Basu and Amdo areas of the BNSZ, all plot within a field with sediments contribution in the Rb/Ba vs. Rb/Sr, and Th/La vs. Th diagrams (Figure 7b,c). All these geochemical features indicate melting of a mantle-derived source, together with input of a sedimentary component. Furthermore, analogous to the coeval granitic rocks from the Amdo and Shiquanhe areas [14,29], the granodiorites in this study also plot within the field of island arc volcanic rocks with sediment components, as demonstrated in the U/Th vs. Th diagram (Figure 7d). Therefore, we conclude that the granodiorite magma originated from a mantle-derived mafic source with sediment input in an island arc-type environment.

6.3. Tectonic Setting and Its Implications

Multiple analyses of tectonic setting discrimination and trace element characteristics have defined our intrusive rocks as having been formed in a subduction-related island arc setting [26,63,64]. In the Rb versus Y+Nb diagram [65] (Figure 8a), all our samples, as well as other intrusive rock samples along the SNMZ, including Amdo diorites and Basu granite, all plot within in the volcanic arc granite (VAG) field, indicating formation within an arc environment. In the R1-R2 diagram [66] (Figure 8b), the samples all fall in the mantle trondhjemite field. In the Rb/30-Hf-3Ta diagram (Figure 8c), the samples also plot in the volcanic arc granite field. Furthermore, the REE and trace element pattern of our samples are highly consistent with the standard arc granite pattern and coeval arc setting granites developed in BNSZ (Figure 5) [14,29,51]. Additionally, the enrichment in large ion lithophile elements (LILEs) and depletion of high-field-strength elements (HFSEs) provide further evidence of the island arc setting.
The studied intrusive rock suites belong to the low-K tholeiitic to calc-alkaline series, with a prominent metaluminous attribution, which are similar to the slab subduction-derived trondhjemite-tonalite-dacite in a modern oceanic tectonic setting [69], specially formed in the island arc tectonic environment. Combined with the island arc setting discussed above, we suggest our Early Jurassic intrusive samples formed in an island arc environment during the Meso-Tethys subduction stage [23,28,70]. By considering the new discovery of the nearby Early Jurassic north Lameila forarc ophiolite, which represents the early-stage subduction of the Bangong Meso-Tethys ([23] and references therein), it is reasonable to conclude that the Shiquanhe opiolitic mélange preserves records of Early Jurassic intra-oceanic subduction and corresponding island arc magmatism in the Meso-Tethys Ocean (Figure 9). During oceanic crust subduction, the products of partial melting of the subducting slab or the mantle partial melts induced by dehydration of the subducting slab serve as crucial sources of ore-forming parental magmas for large porphyry copper deposits [68,71,72]. Concurrently, intra-oceanic subduction triggers back-arc spreading or mantle plume activity, generating tholeiitic basaltic magmas. During their ascent, these magmas may react with sulfur-rich country rocks (e.g., carbonates, black shales), leading to the formation of sulfide deposits [73,74,75,76,77,78,79]. Thus, we propose that this Early Jurassic island arc magmatism initiated a new era of Mesozoic mineralization in the Shiquanhe area, which appears to be supported by the discovery of the Jurassic Xiongcun Cu-Au ore concentration area in the middle segment of the SNMZ [80,81].

7. Conclusions

(1) The obtained zircon LA-ICP-MS U-Pb dating of quartz diorite and granodiorite within the Shiquanhe Ophiolitic mélange yielded weighted mean ages of 174.7 ± 1.4 Ma and 178.9 ± 1.2 Ma, respectively, demonstrating formation in the Early Jurassic.
(2) The geochemistry of these Early Jurassic intermediate intrusive rocks indicates a subduction-induced island arc magmatism.
(3) The Shiquanhe ophiolitic mélange represents an island arc and back-arc assemblage rather than an independent ocean basin.

Supplementary Materials

The analytical results of major and trace elements, and zircon U-Pb geochronology for the granitic rock samples in this study. The following supporting information can be downloaded at https://www.mdpi.com/article/10.3390/min16020123/s1, Table S1. Results of zircon U-Pb dating of Shiquanhe granodiorite and quartz diorite. Table S2. Major and trace elements abundances of Shiquanhe granodiorite and quartz diorite.

Author Contributions

Data curation: K.D., W.-L.L., X.Z. and R.-X.D.; formal analysis: C.Y., Y.S., H.Z. and J.L.; funding acquisition, K.D. and W.-L.L.; investigation: X.K., H.Z. and Y.B.; project administration: X.K., H.Z. and Q.W.; Methodology: K.D., R.-X.D., W.-L.L. and Q.W.; supervision: X.Z., R.-X.D., W.-L.L. and Q.W.; visualization: W.-L.L., X.Z., K.D. and C.Y.; writing—original draft: K.D. and X.Z.; writing—review and editing: X.Z., R.-X.D., W.-L.L., H.F. and Q.W. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by Guangdong Basic and Applied Basic Research Foundation, China [grant number 2024A1515010439]; the Deep Earth Probe and Mineral Resources Exploration—National Science and Technology Major Project (2024ZD1001003); the Scientific Research Fund Project of Yunnan Education Department [2026J1058]; National Natural Science Foundation of China [no. 41972049, 41472054, 42072229, 41977231, 42595550, 42595554]; National Key R&D Program of China (2025YFF0811600); China State Scholarship Fund for Visiting Scholars [Grant No. 202506380223, 20170638507]; and National Key Research and Development Program of China: Demonstration of Responsible Exploration and Resources Expansion of Copper Polymetallic Resource Bases in Tibet (2022YFC2905001).

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The data set is presented directly in the present study.

Acknowledgments

We are grateful to Guo-Chao Gao and Wei Li for assistance related to regional geological fieldwork and Liang Li, Li Liu, and He Xiao for analytical assistance.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (a) Tectonic map of the Tibetan Plateau. Main sutures and faults: wK, west Kunlun suture; A, Altyan fault zone; K, Kunlun suture; J, Jinsa suture; S, Shuanghu suture; B, Bangong suture; Bo, Bangong-Nujiang ophiolite sub-belt; So, Shiquanhe-Jiali ophiolite sub-belt; Y, Yarlung Zangbo suture. After Zhang et al. [30,31] and Jin et al. [32]. (b) Simplified geological map showing the distinct geological constitute of middle to western Bangong suture and adjacent terrane. Bo: the Bangong Lake-Nujinag ophiolite sub-belt (BNO sub-belt) in the north (the BNSZ in a strict sense); So, the Shiquanhe-Jiali ophiolite sub-belt (SJO sub-belt) in the south (the SNMZ in a strict sense), after [20]. (c) Geological map of the Bangong Lake-Shiquanhe area, western BSZ (after Zheng et al. [33] and our field work). Age data source: 161 Ma [20], 185–180 Ma [23,28], 167 Ma [27], 185 Ma and 191–187 Ma [28], 193.1 ± 3.2 Ma and 165.8 Ma [33].
Figure 1. (a) Tectonic map of the Tibetan Plateau. Main sutures and faults: wK, west Kunlun suture; A, Altyan fault zone; K, Kunlun suture; J, Jinsa suture; S, Shuanghu suture; B, Bangong suture; Bo, Bangong-Nujiang ophiolite sub-belt; So, Shiquanhe-Jiali ophiolite sub-belt; Y, Yarlung Zangbo suture. After Zhang et al. [30,31] and Jin et al. [32]. (b) Simplified geological map showing the distinct geological constitute of middle to western Bangong suture and adjacent terrane. Bo: the Bangong Lake-Nujinag ophiolite sub-belt (BNO sub-belt) in the north (the BNSZ in a strict sense); So, the Shiquanhe-Jiali ophiolite sub-belt (SJO sub-belt) in the south (the SNMZ in a strict sense), after [20]. (c) Geological map of the Bangong Lake-Shiquanhe area, western BSZ (after Zheng et al. [33] and our field work). Age data source: 161 Ma [20], 185–180 Ma [23,28], 167 Ma [27], 185 Ma and 191–187 Ma [28], 193.1 ± 3.2 Ma and 165.8 Ma [33].
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Figure 2. Field occurrences of the quartz diorite (a) and granodiorite (c), photomicrographs showing quartz diorite (b) and granodiorite (d). Amp = amphibole; Pl = plagioclase; Kfs = K-feldspar.
Figure 2. Field occurrences of the quartz diorite (a) and granodiorite (c), photomicrographs showing quartz diorite (b) and granodiorite (d). Amp = amphibole; Pl = plagioclase; Kfs = K-feldspar.
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Figure 3. Concordia plots and weighed average age of LA-ICP-MS U–Pb data of quartz diorite (a) and granodiorite (b), analyzed zircon CL images in the quartz diorite and granodiorite.
Figure 3. Concordia plots and weighed average age of LA-ICP-MS U–Pb data of quartz diorite (a) and granodiorite (b), analyzed zircon CL images in the quartz diorite and granodiorite.
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Figure 4. (a) K2O+Na2O vs. SiO2 (modified after [47]), (b) An-Ab-Or (modified after [48]), (c) F-A-M (modified after [49]), and (d) SiO2 vs. K2O diagrams (modified after [50]) for the Shiquanhe granodiorite and quartz diorite. Data sources for comparison: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29]. Ab = albite, An = anorthite, Or = orthoclase, F = Fe2O3t =1.113 × FeO + Fe2O3, A = Na2O + K2O, M = MgO.
Figure 4. (a) K2O+Na2O vs. SiO2 (modified after [47]), (b) An-Ab-Or (modified after [48]), (c) F-A-M (modified after [49]), and (d) SiO2 vs. K2O diagrams (modified after [50]) for the Shiquanhe granodiorite and quartz diorite. Data sources for comparison: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29]. Ab = albite, An = anorthite, Or = orthoclase, F = Fe2O3t =1.113 × FeO + Fe2O3, A = Na2O + K2O, M = MgO.
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Figure 5. Chondrite-normalized REE patterns (a,c) and primitive-mantle-normalized spider diagrams (b,d) for the Shiquanhe granodiorite and quartz diorite. Values of chondrite, primitive mantle, and N-MORB (normal mid-ocean ridge basalt) are from [52]. Data sources: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29].
Figure 5. Chondrite-normalized REE patterns (a,c) and primitive-mantle-normalized spider diagrams (b,d) for the Shiquanhe granodiorite and quartz diorite. Values of chondrite, primitive mantle, and N-MORB (normal mid-ocean ridge basalt) are from [52]. Data sources: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29].
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Figure 6. (a) A/CNK vs. A/NK (modified after Maniar and Piccoli [44]) (b) Zr + Nb + Y + Ce vs. FeOt/MgO [53], (c) SiO2 vs. P2O5 [29], and (d) C/MF vs. A/MF diagrams (modified after [58]) for the Shiquanhe granodiorite and quartz diorite. Data sources for comparison: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29]. A/NK = molar/Al2O3/(Na2O + K2O), A/CNK = molar Al2O3/(CaO + Na2O + K2O), A/MF = Al2O3/(MgO + FeOt), C/MF = CaO/(MgO + FeOt).
Figure 6. (a) A/CNK vs. A/NK (modified after Maniar and Piccoli [44]) (b) Zr + Nb + Y + Ce vs. FeOt/MgO [53], (c) SiO2 vs. P2O5 [29], and (d) C/MF vs. A/MF diagrams (modified after [58]) for the Shiquanhe granodiorite and quartz diorite. Data sources for comparison: Amdo granite and diorite [14], Basu granite [51], Shiquanhe granodiorite and tonalite [29], and Lhaguotso granite [29]. A/NK = molar/Al2O3/(Na2O + K2O), A/CNK = molar Al2O3/(CaO + Na2O + K2O), A/MF = Al2O3/(MgO + FeOt), C/MF = CaO/(MgO + FeOt).
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Figure 7. (a) Plots of CaO/(FeOt + MgO + TiO2) vs. FeOt + MgO + TiO2 + CaO (after [59]), (b) plots of Rb/Ba vs. Rb/Sr (after [60]), (c) plots of Th/La-Th (after [61]), (d) plots of U/Th-Th (after [62]). Data sources for comparison are detailed in Figure 6.
Figure 7. (a) Plots of CaO/(FeOt + MgO + TiO2) vs. FeOt + MgO + TiO2 + CaO (after [59]), (b) plots of Rb/Ba vs. Rb/Sr (after [60]), (c) plots of Th/La-Th (after [61]), (d) plots of U/Th-Th (after [62]). Data sources for comparison are detailed in Figure 6.
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Figure 8. Geochemical data of Shiquanhe granodiorite and quartz diorite, plotted on the (a) Y + Nb vs. Rb [65], (b) R1 vs. R2 [66], (c) Rb/30-Hf-3Ta [67]. Data sources for comparison are detailed in Figure 6. R1 = molar/4 × SiO2 − 22 × (Na2O + K2O) − 2 × (FeOt + TiO2); R2 = molar/2 × Al2O3 + 2 × MgO + 6 × CaO [68].
Figure 8. Geochemical data of Shiquanhe granodiorite and quartz diorite, plotted on the (a) Y + Nb vs. Rb [65], (b) R1 vs. R2 [66], (c) Rb/30-Hf-3Ta [67]. Data sources for comparison are detailed in Figure 6. R1 = molar/4 × SiO2 − 22 × (Na2O + K2O) − 2 × (FeOt + TiO2); R2 = molar/2 × Al2O3 + 2 × MgO + 6 × CaO [68].
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Figure 9. Cartoon showing the petrogenesis of the Shiquanhe intrusive rocks in this study. Not drawn to scale. For the specific explanation, please refer to the text.
Figure 9. Cartoon showing the petrogenesis of the Shiquanhe intrusive rocks in this study. Not drawn to scale. For the specific explanation, please refer to the text.
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MDPI and ACS Style

Dai, K.; Zhang, X.; Ding, R.-X.; Furnes, H.; Liu, W.-L.; Kang, X.; Zhao, H.; Li, J.; Wang, Q.; Bai, Y.; et al. Chronology and Geochemistry of Intrusive Magmatic Rocks in the Shiquanhe Ophiolitic Mélange, Tibet: Constraints on the Tectonic Evolution of the Meso-Tethys Ocean. Minerals 2026, 16, 123. https://doi.org/10.3390/min16020123

AMA Style

Dai K, Zhang X, Ding R-X, Furnes H, Liu W-L, Kang X, Zhao H, Li J, Wang Q, Bai Y, et al. Chronology and Geochemistry of Intrusive Magmatic Rocks in the Shiquanhe Ophiolitic Mélange, Tibet: Constraints on the Tectonic Evolution of the Meso-Tethys Ocean. Minerals. 2026; 16(2):123. https://doi.org/10.3390/min16020123

Chicago/Turabian Style

Dai, Kegang, Xu Zhang, Ru-Xin Ding, Harald Furnes, Wei-Liang Liu, Xiaobo Kang, Hongfei Zhao, Jing Li, Qin Wang, Yun Bai, and et al. 2026. "Chronology and Geochemistry of Intrusive Magmatic Rocks in the Shiquanhe Ophiolitic Mélange, Tibet: Constraints on the Tectonic Evolution of the Meso-Tethys Ocean" Minerals 16, no. 2: 123. https://doi.org/10.3390/min16020123

APA Style

Dai, K., Zhang, X., Ding, R.-X., Furnes, H., Liu, W.-L., Kang, X., Zhao, H., Li, J., Wang, Q., Bai, Y., Yan, C., & Shi, Y. (2026). Chronology and Geochemistry of Intrusive Magmatic Rocks in the Shiquanhe Ophiolitic Mélange, Tibet: Constraints on the Tectonic Evolution of the Meso-Tethys Ocean. Minerals, 16(2), 123. https://doi.org/10.3390/min16020123

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