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Article

Late Carboniferous Slab Rollback in the Southern Altaids: Evidence from a Slab-Derived Adakitic Granodiorite in the South Tianshan

by
Nijiati Abuduxun
1,*,
Wenjiao Xiao
2,3,*,
Wanghu Zhang
1,
He Yang
2,3,
Abidan Alimujiang
1,
Peng Huang
2,3 and
Jingmin Gan
2,3
1
Xinjiang Key Laboratory for Geodynamic Processes and Metallogenic Prognosis of the Central Asian Orogenic Belt, School of Geology and Mining Engineering, Xinjiang University, Urumqi 830046, China
2
National Key Laboratory of Ecological Safety and Sustainable Development in Arid Lands, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi 830011, China
3
Xinjiang Key Laboratory of Mineral Resources and Digital Geology, Xinjiang Research Centre for Mineral Resources, Chinese Academy of Sciences, Urumqi 830011, China
*
Authors to whom correspondence should be addressed.
Minerals 2025, 15(7), 674; https://doi.org/10.3390/min15070674
Submission received: 14 May 2025 / Revised: 12 June 2025 / Accepted: 20 June 2025 / Published: 24 June 2025
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

The South Tianshan records the latest accretionary and collisional events in the southwestern Altaids, but the internal subduction-related processes are controversial. This study provides an integrative analysis of a newly identified Late Carboniferous adakitic granodiorite from the South Tianshan, incorporating geochronological, zircon U-Pb and Lu-Hf isotopic, whole-rock geochemical, and Sr-Nd isotopic data. Zircon U-Pb analysis indicates that the granite was emplaced at 310 ± 2.5 Ma. Based on major element compositions, the granodiorite belongs to medium-K calc-alkaline weakly peraluminous series (A/CNK = 0.95–1.09). The samples exhibit typical high-silica adakitic affinity, as evidenced by the elevated contents of SiO2 (67.75–69.27 wt.%), Al2O3 (15.29–15.90 wt.%), Sr (479–530 ppm), and Ba (860–910 ppm); low concentrations of Yb (0.43–0.47 ppm) and Y (7.12–7.44 ppm); high Sr/Y ratios (67–72); and slight Eu anomalies (δEu = 0.89–1.03). The sodium-rich composition (K2O/Na2O = 0.48–0.71) is comparable to adakitic rocks from slab-derived melts. Elevated concentrations of Ni (22.12–24.25 ppm), Cr (33.20–37.86 ppm), Co (6.32–6.75 ppm), and V (30.33–32.48 ppm), along with high Mg# values (55–57), suggest melt–mantle interaction during magma ascent. The slightly enriched isotopic signatures, characterized by higher initial 87Sr/86Sr ratios (0.706086–0.706205) and lower εNd(t) (−3.09 to –2.47) and εHf(t) (−3.11 to +7.66) values, point to notable sedimentary contributions, potentially through source contamination and/or shallow-level crustal contamination. By integrating the new results with previously published data, we consider that the adakitic granodiorite was generated by partial melting of the subducted oceanic crust, triggered by asthenospheric upwelling associated with the southward rollback of the north-dipping South Tianshan oceanic lithosphere. Our data provide new insights into Late Carboniferous retreating subduction along the southern active margin of the Yili-Central Tianshan and the accretionary architecture of the southern Altaids.

1. Introduction

The Altaids [1], a tectonic collage situated between the Baltica and Siberian Cratons to the north and the Tarim and North China Cratons to the south (Figure 1a), constitute one of the largest accretionary orogenic systems during the Phanerozoic [1,2,3]. The Altaids evolved from the late Neoproterozoic to the Mesozoic through the prolonged accretion of multiple accretionary complexes, ophiolites, seamounts, oceanic arcs, and micro-continents [3,4,5,6,7,8], followed by the ultimate closure of the Paleo-Asian Ocean along the South Tianshan-Solonker suture [9]. The Carboniferous records one of the largest crustal growth and mineral resource formation stages in the southern Altaids, but their internal geodynamics have been long controversial. Some authors thought that the whole Altaids developed into a post-orogenic stage without any, or no large-scale, oceanic subduction [10,11,12], while others proposed that in the Late Carboniferous to Permian [13,14,15,16], Early Triassic [17], and even Late Triassic [18,19,20,21] the Altaids might have been controlled by oceanic subduction. Therefore, the Carboniferous internal geodynamics in the southern Altaids need systematical investigation.
The South Tianshan represents a critical part of the southern Altaids [23], preserving the record of the latest accretionary and collisional events involved in its tectonic evolution [15,24,25,26]. A prominent feature of the South Tianshan is that Late Carboniferous–Early Permian felsic intrusions are widely distributed along the strike of the orogen [27,28,29,30,31]. However, no consensus has yet been reached concerning the magmatic genesis and deep geodynamic processes responsible for the formation of these granitoids. Proposed models include (1) the Permian Tarim mantle plume-induced magmatism [32,33]; (2) post-collisional magmatism resulting from the interaction of upwelling asthenosphere with lithospheric mantle and crustal materials [30,34,35,36]; and (3) arc-related magmatism formed in an upper plate extensional regime that was likely triggered by southward retreat of the South Tianshan oceanic [27,31]. These divergent interpretations have hindered a comprehensive reconstruction of the Late Carboniferous and Early Permian tectonic framework of the southwestern Altaids.
In this study, we carry out a detailed petrological investigation of a newly identified Late Carboniferous adakitic granodiorite from the South Tianshan using petrographic, chronological, whole-rock geochemical, and Sr-Nd-Hf isotopic data. This work aims to elucidate the petrogenesis and geodynamic context of Late Carboniferous adakitic magmatism in the southern Altaids by integrating new results with previously published data. The present study yields novel insights into the accretionary architecture and evolution of the southern Altaids.

2. Geological Setting

The South Tianshan, a continuous tectonic belt marking the southwestern margin of the Altaids, stretches about 2500 km from western China to Central Asia (Figure 1) [24,26]. The belt is separated from the Paleozoic Yili-Central Tianshan arc by the Atbashi-Inylchek-South Nalati Fault to the north and from the Tarim Craton by the North Tarim Fault to the south (Figure 1b) [14,15,25]. Tectonically, the South Tianshan is a fossil accretionary complex formed by the northward subduction of the Paleo-South Tianshan Ocean [19,26,37]. It records the final suturing process between the Yili-Central Tianshan arc and the northern Tarim Craton, which is thought to have taken place in the late Paleozoic [13,32,38], or alternatively in the early Mesozoic [18,21,39,40].
The South Tianshan dominantly consists of Paleozoic continental terrigenous deposits and deep marine sedimentary rocks, which display diverse degrees of metamorphism [26,41,42]. Structurally, these rocks are commonly exposed as fault-bounded tectonic slices that dip northward [18,19,43]. Provenance analyses indicate that most of the sediments were sourced from the Yili-Central Tianshan arc [18,44,45,46,47]. Notably, recent detrital zircon geochronological data reveal that some greenschists and/or amphibolites, previously believed to be the Precambrian basement of the South Tianshan [48], actually date to the Paleozoic [46,49]. Moreover, accreted fragments of ocean plate stratigraphy (OPS), including MORB- and OIB-type basalts, ribbon cherts, siliciclastic turbidites, and limestones, have been identified within the Paleozoic strata [19,37,50]. These fragments typically form chaotic mélanges characterized by a block-in-matrix structure, resembling off-scraped and underplated basaltic–sedimentary sequences observed in modern convergent margins [51,52].
Exotic blocks of ophiolitic mélanges structurally crop out along the strike of the orogenic belt [53,54,55]. Ages of gabbros and conodont/radiolarian microfossils in associated siliceous rocks indicate a time span ranging from Cambrian to Late Carboniferous, indicating a long-lasting accretionary process [56,57,58,59,60]. A prominent high- and ultrahigh-pressure (HP/UHP) metamorphic belt, with peak metamorphism at ca. 319 Ma, is exposed in the Akyazi area of China and terminates westward in the Atbashi area in Kyrgyzstan (Figure 1b) [61,62,63]. Recent studies have suggested that the Yushugou ophiolitic mélange may represent an OIB-type metamorphic sole formed during the intra-oceanic subduction initiation, likely near a seamount or oceanic plateau [64].
Late Silurian to Early Devonian (430–380 Ma) granitoids and their volcanic equivalents with arc-related geochemical signatures are sporadically distributed along the South Tianshan [38,65,66,67]. By contrast, the Late Carboniferous to Permian (298–260 Ma) marks the primary phase of Paleozoic magmatism in the region, dominated by the widespread co-occurrence of A-, S-, and I-type granitoids, syenites, and minor mafic and felsic volcanic rocks [27,30,31,35,68].

3. Field Occurrence and Petrography

The study area is situated approximately 80 km northwest of Hejing county, where a Late Carboniferous–Early Permian granitoid is prominently exposed. The intrusion, referred to as Mangqisu pluton, represents one of the largest plutons in the South Tianshan, covering a surface area of approximately 940 km2. The pluton is a composite granitoid, consisting of a biotite granodiorite, two-mica granite, and granodiorite distributed from east to west (Figure 2). Previous geochronological investigations have demonstrated that the pluton formed in periods between ca. 304 and 292 Ma [31,36,69]. Geochemically, the eastern two-mica and biotite granites are characterized as peraluminous S-type granites [36,69], whereas the western Permian (ca. 296–297 Ma) biotite granodiorite exhibits a fractionated I-type granite affinity [36].
In this study, we collected five samples from a granodiorite for geochronological, Lu-Hf isotopic, bulk-rock Sr-Nd isotopic, and geochemical analysis. The sampling location is indicated in Figure 2. The granite has intruded a meta-sedimentary sequence consisting of meta-sandstones, schists, and biotite gneisses (Figure 3a,b). This metamorphosed sequence was previously attributed to the Middle Devonian Sa’arming Group [70]. Our earlier research determined the maximum depositional age of a meta-sandstone from this sequence to be ca. 421 Ma [18]. The granodiorite exhibits a fine-grained texture (Figure 3c) and is predominantly composed of quartz (20–30 vol.%), K-feldspar (20–30 vol.%), plagioclase (30–35 vol.%), and biotite (~15 vol.%) (Figure 3d,e).

4. Analytical Method

4.1. Zircon U-Pb Geochronology

Zircon grains were separated using standard magnetic separation and high-density liquid techniques, followed by handpicking and embedding in an epoxy mount. The mount was polished to EBSD standards using colloidal silica and coated with carbon [71]. The internal structures of individual zircon grains were analyzed through cathodoluminescence (CL) imaging, performed using a Tescan MIRA 3 field emission scanning electron microscope (SEM) at Beijing Zhongke Kuangyan Test Technology Co., Ltd. (Beijing, China).
Zircon U-Pb geochronology was conducted using an ESR NWR 193 laser-ablation system coupled with an Agilent 8900 quadrupole Inductively Coupled Plasma Mass Spectrometer (ICP-MS) from Beijing, China.
A 193 nm ArF excimer laser from Zhongke Kuangyan Test Technology Co., Ltd. (Guangzhou, China) homogenized through a beam delivery system was focused on individual zircon surfaces with an energy density of 4.5 J/cm2. Each analysis included a 20 s acquisition for background (gas blank), followed by a 40 s ablation with a spot diameter of 32 μm and a repetition rate of 6 Hz. Helium (~400 mL/min) was used as the carrier gas to efficiently transport the aerosol from the ablation cell and was mixed with argon (~1.15 L/min) via a T-connector before entering the ICP torch. The 91500-zircon served as an external standard to correct for instrumental mass discrimination and elemental fractionation, while GJ–1 and Plešovice zircons were employed as quality controls for geochronology [72]. Zircon trace element abundances were externally calibrated against NIST SRM 610 using Si as the internal standard. Raw data reduction was performed offline using ICPMSDataCal 12.2 software [73]. Age calculations and Concordia diagrams were generated using the ISOPLOT 4.15 toolkit for Microsoft Excel [74].

4.2. Zircon Lu-Hf Isotopes

In situ zircon Lutetium (Lu) and Hafnium (Hf) isotope analyses were conducted using a Resolution SE 193 laser ablation system coupled with a Thermo Fisher Scientific Neptune Plus Multi-Collector Inductively Coupled Plasma Mass Spectrometer (MC-ICP-MS) from Beijing Zhongke Kuangyan Test Technology Co., Ltd. (Beijing, China). The analyses were performed in single-spot ablation mode with a spot size of 44 μm. Each spot was superimposed on corresponding U-Pb spots. Helium was used as the carrier gas to transport ablated samples from the laser-ablation cell to the ICP-MS torch via a mixing chamber, where it was merged with argon. Instrumental conditions and data acquisition protocols followed those described by [75]. Corrections for isobaric interferences of 176Lu and 176Yb on 176Hf were made using 176Lu/175Lu = 0.02656 [76] and 176Yb/173Yb = 0.79639 [77]. Yb and Hf isotope ratios were normalized to 173Yb/171Yb = 1.132685 and 179Hf/177Hf = 0.7325 [77] using an exponential correction for mass bias. Zircon GJ–1 was employed as the reference standard. Data selection, signal integration, and mass bias calibrations were performed offline using ICPMSDataCal 12.2 software [73].
The εHf(t) values were calculated using chondritic reference values of 176Hf/177Hf = 0.0336 and 176Lu/177Hf = 0.282785 [78]. Single-stage model ages (TDM1) were determined relative to the depleted mantle, with present-day values of 176Hf/177Hf = 0.28325 and 176Lu/177Hf = 0.0384 [79]. Two-stage model ages (TDM2) were calculated using an average crustal 176Lu/177Hf value of 0.015 [80]. The εHf(t) values and Hf model ages were derived using the 206Pb/238U ages of individual zircon grains.

4.3. Bulk-Rock Major and Trace Element Geochemistry

Fresh rock chips were isolated from crushed Bulk-rock samples to prepare for geochemical analysis. Bulk-rock major element concentrations were measured at Beijing Zhongke Kuangyan Test Technology Co., Ltd. using X-ray Fluorescence (XRF-1800) on fused glass beads. Loss on ignition was determined by heating the samples to 1000 °C for 3 h in a muffle furnace. The analytical precision was within ±2% for oxides greater than 0.5 wt.% and within ±5% for oxides greater than 0.1 wt.%.
Bulk-rock trace element concentrations were analyzed at Nanjing FocuMS Technology Co., Ltd. using an Agilent Technologies 7700× quadrupole ICP-MS (Tokyo, Japan). Approximately 30 mg of powdered sample was mixed with a lithium metaborate flux, fused in a furnace at 650 °C, and subsequently cooled. The resulting melt was dissolved in 100 mL of 4% HNO3 solution. The United States Geological Survey (USGS) granodiorite standard GPS–2 was used as an external standard [81]. The analytical uncertainty for trace element measurements was better than 5%.

4.4. Bulk-Rock Sr and Nd Isotopes

Bulk-rock Sr and Nd isotopic compositions were measured at Nanjing FocuMS Technology Co., Ltd., following the analytical procedures outlined in [82]. Raw isotopic ratio data were internally corrected for mass fractionation using an exponential law and normalized to 86Sr/88Sr = 0.1194 for Sr and 146Nd/144Nd = 0.7219 for Nd. Isotopic standards (NIST SRM 987 for Sr and JNdi-QC and CAGS-Nd for Nd) were utilized to assess instrument stability during data acquisition. Geological reference materials BHVO–2 (143Nd/144Nd = 0.512982 ± 0.000002 and 87Sr/86Sr = 0.703488 ± 0.000003) and BCR–2 (143Nd/144Nd = 0.512639 ± 0.000002 and 87Sr/86Sr = 0.7050004 ± 0.000003) were analyzed to monitor the accuracy of the procedures. The isotopic results were consistent with previous published values within analytical uncertainties [83]. Two-stage Nd model ages were calculated relative to the average continental crust, using a 147Sm/144Nd ratio of 0.118 [84].

5. Results

5.1. Zircon U-Pb Ages

The results of zircon U-Pb dating for the granodiorite are presented in Table 1. Cathodoluminescence (CL) images of the analyzed zircons are shown in Figure 4.
The zircon grains, ranging in size from 150 μm to 300 μm with length-to-width ratios of 2:1 to 3:1, are predominantly transparent, prismatic, and euhedral. Clear oscillatory zoning observed in the CL images (Figure 4) suggests a magmatic origin, which is further indicated by their high Th/U ratios of 0.27 to 1.00 [85]. Twenty zircon grains from the granodiorite were analyzed, of which fifteen yield concordant 206Pb/238U ages of 307–314 Ma (Figure 5a). These results provide a weighted mean 206Pb/238U age of 310 ± 2.5 Ma (MSWD = 0.19) (Figure 5b), representing the formation age of the granodiorite. Five grains define older ages of 329 Ma, 425 Ma, 435 Ma, 445 Ma, and 466 Ma, likely representing xenocrysts or inherited zircons.

5.2. Bulk-Rock Geochemistry

The results of whole-rock major and trace element geochemical analyses for the granodiorite are listed in Table 2. The samples show low loss on ignition (LOI) values (0.55–0.68 wt.%), indicating that post-magmatic alteration is limited.
The granodiorite samples exhibit SiO2 contents ranging from 67.75 to 69.27 wt.% and K2O + Na2O contents between 5.95 and 6.91 wt.%, plotting within the granodiorite field in the total alkalis (K2O + Na2O) wt.% vs. SiO2 (wt.%) classification diagram (Figure 6a) [86]. The samples display limited compositional variation, with low to moderate concentrations of Al2O3 (15.29–15.90 wt.%), TiO2 (0.49–0.51 wt.%), MgO (1.48–1.59 wt.%), and P2O5 (0.15–0.17 wt.%), along with elevated CaO (3.15–3.17 wt.%) contents and Mg# values (55–57). In the K2O (wt.%) vs. SiO2 (wt.%) diagram (Figure 6b) [87], all samples plot in the medium-K calc-alkaline series, characterized by lower K2O contents ranging from 1.93 to 2.88 wt.% and K2O/Na2O ratios of 0.48 to 0.71 (Figure 6c). The A/CNK ratios of the samples are between 0.99 and 1.09 and plot in to the weakly peraluminous field on the A/NK vs. A/CNK diagram (Figure 6d) [88].
The granodiorite samples exhibit chondrite-normalized rare earth element (REE) patterns characterized by pronounced enrichment in light rare earth elements (LREEs) relative to heavy rare earth elements (HREEs), as reflected in their high LaN/YbN ratios, ranging from 54 to 61 (Figure 7a and Table 2). These samples display strongly fractionated REE patterns, indicated by elevated LaN/SmN ratios of 4.95 to 5.52, and show negligible Eu anomalies (δEu = 0.89–1.03) (Figure 7a) [89]. In the primitive mantle-normalized multi-element diagram (Figure 7b), the granodiorite samples show enrichment in large-ion lithophile elements (LILEs; Rb, Ba, Th and U) and light REEs, alongside pronounced depletion in Nb and Ta.

5.3. Zircon Hf and Bulk-Rock Sr and Nd Isotopes

Excluding the five inherited or captured zircons with older ages, the remaining 15 dated grains were analyzed for their Lu-Hf isotopic compositions. The results of in situ Lu-Hf isotopes for the granodiorite are listed in Table 3 and illustrated in Figure 8a. Most of the grains display εHf(t) values between –3.11 and +1.14, with crustal model ages (TDM2) ranging between 1237 and 1527 Ma. An exception is spot 22ST18-04, which exhibits a distinctly positive εHf(t) value of +7.66, corresponding to a younger crustal model age of 840 Ma.
The initial Sr and Nd isotope ratios of five granodiorite samples were calculated based on the weighted mean age (ca. 310 Ma) obtained from zircon U-Pb dating. The results are provided in Table 4 and depicted in Figure 8b. The samples display restricted isotopic variability, characterized by initial 87Sr/86Sr ratios spanning a limited range of 0.706086 to 0.706205. The Nd isotopic compositions are relatively consistent and slightly negative, with εNd(t) values from −3.09 to −2.47. The two-stage Nd model ages fall between 1276 and 1326 Ma.

6. Discussion

6.1. Petrogenesis and Magma Source

Geochemically, the granodiorite samples exhibit high SiO2 (67.75–69.27 wt.% ≥ 56 wt.%), Al2O3 (15.29–15.90 wt.% ≥ 15 wt.%), Na2O (4.02–4.26 wt.%), Sr (479–530 ppm > 400 ppm), Ba (860–910 ppm), and Sr/Y ratios (67–72 > 40), along with low MgO (1.48–1.59 wt.% < 3 wt.%), Yb (0.43–0.47 ppm < 1.9 ppm), Y (7.12–7.44 ppm < 18 ppm), and K2O/Na2O ratios (0.48–0.71). The samples display highly fractionated REE patterns (LaN/YbN = 54–61 > 20), with low HREE contents and negligible Eu anomalies (δEu = 0.89–1.03). These characteristics are typical of adakites [90,94,95]. As confirmed by Sr/Y vs. Yb and (La/Yb)N vs. YbN diagrams (Figure 9a,b) [96], all samples are classified as adakites. Originally, the term “adakite” referred to subduction-related intermediate to felsic magmatic rocks generated by partial melting of young (<25 Ma) oceanic lithosphere under eclogite-facies conditions [90]. However, more recent models suggest that adakitic signatures can arise in diverse geodynamic settings, including (1) high-pressure fractionation of subduction-modified mantle magma [97,98]; (2) melting of thickened lower crust beneath magmatic arcs [99,100]; (3) delamination of thickened continental crust in collisional zones followed by melt–mantle interaction [101]; (4) fluid-fluxed melting at normal crustal pressures [102]; (5) magma mixing between crustal felsic and metasomatized mantle melts [103,104]; and (6) partial melting of subducted slabs induced by asthenospheric upwelling triggered by slab rollback, slab tear-off, or ridge subduction [105,106,107].
Adakites derived from thickened or delaminated crust typically show elevated K2O (≥3 wt.%) and lower Al2O3 contents [93,108], which contrasts with the sodic signature (K2O = 1.93–2.88 wt.%; K2O/Na2O = 0.48–0.71) and high Al2O3 (15.29–15.90 wt.%) contents of the studied granodiorite. Additionally, the high Mg# values (55–57) are inconsistent with a thickened crust origin, which typically produces magma with lower Mg# values (<50) [109]. Restricted Th/U ratios (~5), lower than those of the lower continental crust [97], further support this hypothesis. The low HREE, Y, and Yb contents, as well as high Sr/Y and LaN/YbN ratios, suggest garnet as a residual phase in the source [90,95]. Garnet stabilization requires crustal thickness ≥ 30 km [95,109,110]. However, the South Tianshan, being an accretionary complex dominated by structurally accreted materials [18,19,26], likely lacked the lithospheric thickness required for garnet stabilization, rendering a thickened crust origin unlikely. Furthermore, ongoing northward subduction of the South Tianshan ocean during the Late Carboniferous, evidenced by widespread subduction-related magmatism (ca. 310–320 Ma), mélanges, ophiolites, and HP/UHP metamorphic rocks [18,21,22,39,111,112], implies that collision-related delaminated crust is not a viable genesis for the granodiorite.
The granodiorite’s high Mg# values (55–57), coupled with high SiO2 (67.75–69.27 wt.%), Al2O3 (15.29–15.90 wt.%), and Na2O (4.02–4.26 wt.%), along with low MgO (1.48–1.59 wt.%), are inconsistent with features of the low-silica adakites generated by partial melting of a subduction-modified mantle wedge [94,98]. Instead, its sodium-rich composition (Na2O > 3.5 wt.%; K2O/Na2O = 0.48–0.71), high Al2O3 contents, and CaO/Al2O3 ratios align with potassium-depleted high-silica adakites formed through partial melting of subducted oceanic slabs [94] (Figure 10). As shown in Figure 11, higher Ni (22.12–24.25 ppm), Cr (33.20–37.86 ppm), Co (6.32–6.75 ppm), and V (30.33–32.48 ppm) concentrations, as well as Mg# values (55–57 > 40), suggest proportional melt–mantle interaction during magma ascent [113] (Figure 12a).
The granodiorite samples display relatively enriched isotopic signatures, characterized by higher initial 87Sr86Sr ratios (0.706086–0.706205), lower εNd(t) (−3.09 to −2.47), and εHf(t) (−3.11 to +7.66). These values distinguish the samples from typical slab-derived adakites, while remaining less enriched than crustal-derived granitoids in the South Tianshan (Figure 8a,b). One possible explanation for this isotopic signature is magma mixing between melts derived from mantle and crust [103,104]. However, there is currently no supporting geological or petrological evidence, such as the absence of isochronous mafic magmatic rocks and mafic microgranular enclaves (MMEs), to substantiate a hybrid magma origin for the granodiorite. Moreover, adakite-like geochemical features are mainly acquired from the felsic member in hybrid magmas, which is often associated with a thickened crust origin [104]. As previously discussed, this is tectonically not the case for the adakitic granodiorite in the South Tianshan.
Alternatively, sediment involvement in the source during slab melting is a well-documented process at subduction zones [105,114,115]. This process produces relatively enriched isotopic compositions, as overlying flysch sediments resemble crustal materials in composition [116,117]. As shown in Figure 8b, the Sr-Nd isotopic data for these samples show displacement toward the EM-2 end member, closely resembling sediment-contaminated slab-derived adakites from the Lower Yangtze River Belt (LYRB). This suggests an origin involving oceanic slab-derived melts significantly contaminated by sedimentary melts [91,93]. Further evidence for sediment involvement is provided by the high Th/La ratios (0.33–0.37) of the samples (Figure 12b). These values reflect a mixture of basalt oceanic crust and continental sediments, as Th/La ratios are typically low (<0.2) in oceanic basalts, elevated in (>0.25) continental crust, and intermediate (0.09–0.34) in arc basalts and marine sediments [117,118]. This feature aligns with the Sr-Nd-Hf isotopic data. Consistently, the samples plot along trends indicating crustal contamination or magma mixing in the Nb/La vs. Nb/Th diagram (Figure 12c) and fall between basalt and greywacke in the Rb/Sr vs. Rb/Ba diagram (Figure 12d), further supporting sediment incorporation during the formation of the adakitic granodiorite. The potential contribution of anatectic melt during upper crustal extension and/or of a felsic melting-assimilation-storage-homogenization (MASH) process is another possible mechanism of sediment involvement [119,120]. Additional geochemical evidence bolsters this interpretation. The sample display low Nb/U (3.0–4.2), high Ba/Th (72.5–73.8), and high Th/Yb (26–28) ratios, which imply a significant contribution from crustal materials [121]. Furthermore, the consistent presence of inherited or captured zircons (Figure 5a) within the granodiorite suggest sediment involvement, either through source contamination or shallow-level crustal contamination [122]. Collectively, these observations indicate that the granodiorite was produced by partial melting of a subducted oceanic slab, with substantial contributions from crustal materials.
Minerals 15 00674 g011
Figure 11. Discrimination diagrams of adakites showing the oceanic slab-derived origin of the studied adakitic granodiorite, which is distinct from those of crustal-derived adakites from the Yili-Central Tianshan arc [22]. (a) SiO2 (wt.%) vs. Mg# diagram, reference fields are from [108]; (b–d) SiO2 (wt.%) vs. MgO (wt.%), Ni (ppm), and Cr (ppm) diagrams, reference fields are from [22] and references therein. Symbols and data source are as in Figure 6.
Figure 11. Discrimination diagrams of adakites showing the oceanic slab-derived origin of the studied adakitic granodiorite, which is distinct from those of crustal-derived adakites from the Yili-Central Tianshan arc [22]. (a) SiO2 (wt.%) vs. Mg# diagram, reference fields are from [108]; (b–d) SiO2 (wt.%) vs. MgO (wt.%), Ni (ppm), and Cr (ppm) diagrams, reference fields are from [22] and references therein. Symbols and data source are as in Figure 6.
Minerals 15 00674 g011
Minerals 15 00674 g012
Figure 12. (a) Cr (ppm) vs. Ni (ppm) diagram showing that the samples are characterized by higher Ni and Cr contents than the expected range of slab-derived melt, e.g., adakites in Kitakami, SW Japan [113]. Slab and mantle melt mixing line is based on [113]; (b) Th (ppm) vs. Th/La [117] diagram shows higher Th contents and Th/La ratios, which is indicative of a possible contribution from marine sediments. Data for upper crust and marine sediments are from [117], and for MORB are from [118]; (c,d) Nb/La vs. Nb/Th and Rb/Sr vs. Ra/Ba diagrams indicating a significant sediment involvement during the formation of the adakitic granodiorite. Data for the sediment-incorporated slab-derived adakites from the North Qilian orogen are from [107].
Figure 12. (a) Cr (ppm) vs. Ni (ppm) diagram showing that the samples are characterized by higher Ni and Cr contents than the expected range of slab-derived melt, e.g., adakites in Kitakami, SW Japan [113]. Slab and mantle melt mixing line is based on [113]; (b) Th (ppm) vs. Th/La [117] diagram shows higher Th contents and Th/La ratios, which is indicative of a possible contribution from marine sediments. Data for upper crust and marine sediments are from [117], and for MORB are from [118]; (c,d) Nb/La vs. Nb/Th and Rb/Sr vs. Ra/Ba diagrams indicating a significant sediment involvement during the formation of the adakitic granodiorite. Data for the sediment-incorporated slab-derived adakites from the North Qilian orogen are from [107].
Minerals 15 00674 g012

6.2. Tectonic Setting

Late Carboniferous–Early Permian felsic magmatism is well-documented across the South Tianshan by previous geochronological studies [27,28,29,30,31,34,92,123]. However, the proposed geodynamic processes controlling the generation of these granitoids remain controversial. Proposed models include mantle plume activity [32], post-collisional processes [29,30,34,35,36,92], and retreat subduction [27,31]. This persistent controversy has led to significantly divergent interpretations concerning the terminal closure timing of the South Tianshan Ocean [13,14,15,18,25,26].
The formation age of the adakitic granodiorite determined in this study is 310 ± 2.5 Ma, which predates the main eruption phases of the Permian Tarim Large Igneous Province, occurring primarily at ~290 and ~280 Ma [124]. Furthermore, our previous investigation has highlighted significant contrasts between the plume-related A1-type granites in the western Tarim Craton and the orogen-related A2-type granites in the South Tianshan in terms of the rock assemblages, magma conditions, and geochemical and Lu-Hf isotopic compositions [27]. These differences indicate that the petrogenetic mechanism controlling granitoid generation in the South Tianshan was distinct from that driving the plume-induced granitoids in the Tarim Craton. Therefore, the Late Carboniferous South Tianshan granitoids were likely unrelated to the Permian Tarim mantle plume.
The post-collision model implies a pre-Late Carboniferous [13,14,25], or even as early as pre-Early Carboniferous [10,12], collision between the Tarim Craton and the Yili-Central Tianshan. However, geochronological, sedimentological, and structural evidence from imbricated trench-filled turbidites, ophiolites, tectonic mélanges, and HP-UHP metamorphic rocks at various locations in the South Tianshan demonstrates that the northward subduction of the South Tianshan Ocean persisted until the Late Permian to Triassic [17,18,39,40,111]. The presence of fragmented OPS is widely recognized as a hallmark of subduction-accretion processes at convergent margins [52,125]. Structural and geochronological analyses of oceanic plate stratigraphy (OPS) fragments at Yangbulak confirm that the maximum depositional age of the sedimentary matrix within the mélange is ca. 311 Ma [18], providing direct evidence for ongoing subduction-related accretion during the Late Carboniferous. Thus, the post-collision model is inconsistent with the available evidence and is therefore implausible.
This evidence is further corroborated by the newly identified Late Carboniferous adakitic granodiorite in this study. Geochemically, the granodiorite is classified as belonging to the medium-K calc-alkaline series (Figure 6b). As discussed earlier, the granodiorite is thought as a slab-derived high-silica adakite subtype, characterized by elevated SiO2 (67.75–69.27 wt.%), Al2O3 (15.29–15.90 wt.%), and N2O (4.02–4.26 wt.%) contents, as well as Mg# values of 55–57. The samples also exhibit lower MgO (1.48–1.59 wt.%) contents and K2O/Na2O ratios (0.48–0.71) (Figure 10). They are enriched in LREEs, U, Th, Rb, and Ba, but show pronounced depletion in Nb and Ta (Figure 7b), consistent with diagnostic subduction-related trace element signatures. On trace element discrimination diagrams, the samples plot within the magmatic arc field (Figure 13) [126], aligning with the geochemical features of previously documented arc-related granitoids in the South Tianshan [27,30,31,92]. Overall, these geochemical characteristics are diagnostic of subduction-related petrogenesis for the granodiorite.

6.3. Tectonic Implications

While the original conceptualization of adakites invoked melting of hot, young subducted slabs [90], subsequent studies have demonstrated that slab-melted rocks can also form through slab windows created by the direct contact of the subducting plate edge with the upwelling asthenosphere [105,127]. Slab windows are associated with specific geological processes, such as ridge subduction or slab rearing in subduction zones [127,128,129]. Furthermore, laboratory experiments by Kincaid and Griffiths [130] revealed that the increased corner flow velocities within the mantle wedge during slab rollback can generate thermal conditions conducive to slab melting.
At a regional scale, a Late Carboniferous–Early Permian (315–270 Ma) magmatic “flare-up” characterized by diverse magmatic activity has been widely recognized in both the South Tianshan and Yili-Central Tianshan, forming a broad orogen-parallel magmatic arc in the southwestern Altaids [27,131,132]. Notably, the presence of adakites, bimodal volcanic rocks, A2-types granites, and alkaline rocks indicates a regional extensional setting along the Yili-Central Tianshan during the Late Carboniferous to Early Permian [22,27,132,133,134]. Further evidence for extension is provided by Early Permian rifted basins and high-temperature metamorphism observed in these regions [135,136,137]. Given that extension-related magmatic rocks are tectonically constrained within a narrow linear zone along the upper plate of the convergent margin in the southern Yili-Central Tianshan [27], it is likely that the thermal anomaly was induced by slab-rollback. This interpretation is reinforced by the oceanward migration of magmatism, as indicated by their temporal and spatial distributions, which were extensively discussed in prior geochronological studies by [132].
Integrating these observations leads to the conclusion that the newly identified adakitic granodiorite in this study provides further evidence supporting our previously proposed tectonic model [27]. As illustrated in Figure 14, the prolonged southward rollback of the South Tianshan oceanic slab and the resultant asthenospheric upwelling created favorable conditions for melt generation, including a thermal anomaly arising from the direct interaction between the oceanic slab and the asthenosphere. Similar processes have been documented not only in modern Pacific-type accretionary orogens, such as the Kinki district in SW Japan [105], but also in fossil accretionary orogens, such as the Tethyan Gangdese and North Qilian [106,138], and the Central Orogenic Belt in North China [139]. In addition to slab melting, magma underplating and elevated geothermal gradients led to extensive crustal anatexis. This anomalous thermal event, while prominent in the South Tianshan, was also widespread across the Yili-Central Tianshan, driving the Late Carboniferous–Early Permian magmatic “flare-up” observed across the region.

7. Conclusions

Zircon U-Pb geochronology indicates that the adakitic granodiorite in the South Tianshan formed at 310 ± 2.5 Ma.
The sodium-rich composition of the granodiorite, coupled with its high-silica adakite characteristics, suggests that it was likely generated through initial partial melting of oceanic slab, with subsequent melt–peridotite interaction during magma ascent. The slightly enriched zircon Hf-Sr-Nd isotopes are interpreted as evidence of substantial sedimentary material involvement in the magma process.
By integrating the new results with existing magmatic, sedimentological, metamorphic, and structural data from the South Tianshan and Yili-Central Tianshan, it can be concluded that the formation of the slab-derived adakitic granitoid was influenced by the upwelling of asthenospheric mantle, driven by the retreating subduction of the north-dipping South Tianshan oceanic slab. Slab rollback emerges as the most plausible geodynamic process controlling the Late Carboniferous magmatic “flare-up” observed along the accretionary southern Altaids, which may have generated massive continental growth.

Author Contributions

Conceptualization, N.A. and W.X.; methodology, N.A.; software, W.Z. and A.A.; validation, N.A., H.Y. and W.X.; formal analysis, H.Y.; investigation, N.A., P.H. and J.G.; resources, N.A.; data curation, H.Y.; writing—original draft preparation, N.A.; writing—review and editing, N.A. and W.X.; visualization, A.A. and W.Z.; supervision, W.X.; project administration, N.A.; funding acquisition, N.A. All authors have read and agreed to the published version of the manuscript.

Funding

This study was financially supported by the Key Research and Development Program of Xinjiang Uygur Autonomous Region, China (No. 2022B03015-2), the Third Xinjiang Comprehensive Scientific Expedition (Nos. 2022xjkkl1301 and 2023xjkk0100), the Science and Technology Major Project of Xinjiang Uygur Autonomous Region of China (No. 2021A03001-1), and by funds from the National Natural Science Foundation of China (Nos. 42472279 and 41962013).

Data Availability Statement

The data for this study are available in this manuscript.

Acknowledgments

The manuscript benefited from careful reviews and constructive comments from anonymous reviewers.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (a) Simplified tectonic map of the Altaids showing the position of the South Tianshan in (b) (modified after [1]). (b) Simplified geological map of the South Tianshan and adjacent tectonic units (modified after [16]). The position of Figure 2 is marked. The position of the terminal suture between the Yili-Central Tianshan arc and the Tarim Craton is based on [18]. The adakitic granodiorite from the Yili-Central Tianshan arc is from [22]. Abbreviation: NTAC, North Tianshan Accretionary Complex; KYB, Kazakhstan-Yili Block; CCTA, Chinese Central Tianshan Arc; KNT, Kazakhstan North Tianshan; KMTA, Kyrgyz Middle Tianshan Arc; STAC, South Tianshan Accretionary Complex.
Figure 1. (a) Simplified tectonic map of the Altaids showing the position of the South Tianshan in (b) (modified after [1]). (b) Simplified geological map of the South Tianshan and adjacent tectonic units (modified after [16]). The position of Figure 2 is marked. The position of the terminal suture between the Yili-Central Tianshan arc and the Tarim Craton is based on [18]. The adakitic granodiorite from the Yili-Central Tianshan arc is from [22]. Abbreviation: NTAC, North Tianshan Accretionary Complex; KYB, Kazakhstan-Yili Block; CCTA, Chinese Central Tianshan Arc; KNT, Kazakhstan North Tianshan; KMTA, Kyrgyz Middle Tianshan Arc; STAC, South Tianshan Accretionary Complex.
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Figure 2. Geological map of the Mangqisu area showing main lithologies of the Mangqisu pluton [70]. The sampling location of the studied granodiorite is marked. Literature data are from [36,69]. CTA, Central Tianshan Arc; STAC, South Tianshan Accretionary Complex.
Figure 2. Geological map of the Mangqisu area showing main lithologies of the Mangqisu pluton [70]. The sampling location of the studied granodiorite is marked. Literature data are from [36,69]. CTA, Central Tianshan Arc; STAC, South Tianshan Accretionary Complex.
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Figure 3. (a) A field photo showing that the granodiorite intruded Devonian metasedimentary rocks in the Mangqisu area; geologist for scale. (b) A field photo showing the contact zone of the granodiorite and its sedimentary wall rock; ruler for scale. (c) A hand sample showing the fine-grained texture of the granite; ruler for scale. (d,e) Photomicrographs showing the main mineral compositions and textures of the granodiorite; scale is marked. Abbreviations: Bt, biotite; Kfs, K-feldspar; Pl, plagioclase; Qtz, quartz.
Figure 3. (a) A field photo showing that the granodiorite intruded Devonian metasedimentary rocks in the Mangqisu area; geologist for scale. (b) A field photo showing the contact zone of the granodiorite and its sedimentary wall rock; ruler for scale. (c) A hand sample showing the fine-grained texture of the granite; ruler for scale. (d,e) Photomicrographs showing the main mineral compositions and textures of the granodiorite; scale is marked. Abbreviations: Bt, biotite; Kfs, K-feldspar; Pl, plagioclase; Qtz, quartz.
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Figure 4. Cathodoluminescence (CL) images of zircons from the granodiorite in this study. Red circles indicate positions of dated laser spots; yellow dashed circles indicate positions of Lu-Hf isotopic analyses. Spot numbers with corresponding U-Pb ages and εHf(t) values are marked.
Figure 4. Cathodoluminescence (CL) images of zircons from the granodiorite in this study. Red circles indicate positions of dated laser spots; yellow dashed circles indicate positions of Lu-Hf isotopic analyses. Spot numbers with corresponding U-Pb ages and εHf(t) values are marked.
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Figure 5. (a) U-Pb Concordia diagram of dated zircons from the granodiorite in this study. (b) The calculated weighted mean age of the granodiorite. Ages are in Ma, and ellipses show 1σ errors. Red ellipses are used to calculate the formation age of the granodiorite. Brown dashed ellipses represent ages of inherited/captured zircons.
Figure 5. (a) U-Pb Concordia diagram of dated zircons from the granodiorite in this study. (b) The calculated weighted mean age of the granodiorite. Ages are in Ma, and ellipses show 1σ errors. Red ellipses are used to calculate the formation age of the granodiorite. Brown dashed ellipses represent ages of inherited/captured zircons.
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Figure 6. Petrochemical classification diagrams of the granodiorite. (a) SiO2 wt.% vs. (Na2O + K2O) wt.% diagram [86]; (b) SiO2 (wt.%) vs. K2O (wt.%) diagram showing the low- to middle-K calc-alkaline affinity of the granodiorite [87]; (c) SiO2 wt.% vs. K2O/Na2O diagram showing the sodium-rich signature of the granodiorite; (d) plot of A/CNK (Al2O3/CaO + Na2O + K2O) molar vs. A/NK (Al2O3/Na2O + K2O) molar [88] showing the weakly peraluminous nature of the granodiorite. Data of a ca. 314 Ma crust-derived adakitic granodiorite from the Yili-Central Tianshan arc [22] are plotted for comparison.
Figure 6. Petrochemical classification diagrams of the granodiorite. (a) SiO2 wt.% vs. (Na2O + K2O) wt.% diagram [86]; (b) SiO2 (wt.%) vs. K2O (wt.%) diagram showing the low- to middle-K calc-alkaline affinity of the granodiorite [87]; (c) SiO2 wt.% vs. K2O/Na2O diagram showing the sodium-rich signature of the granodiorite; (d) plot of A/CNK (Al2O3/CaO + Na2O + K2O) molar vs. A/NK (Al2O3/Na2O + K2O) molar [88] showing the weakly peraluminous nature of the granodiorite. Data of a ca. 314 Ma crust-derived adakitic granodiorite from the Yili-Central Tianshan arc [22] are plotted for comparison.
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Figure 7. Chondrite-normalized REE patterns (a) and primitive mantle-normalized multi-element distributions (b) of the studied granodiorite. Chondrite and primitive mantle values are after [89]. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
Figure 7. Chondrite-normalized REE patterns (a) and primitive mantle-normalized multi-element distributions (b) of the studied granodiorite. Chondrite and primitive mantle values are after [89]. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
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Figure 8. (a) Temporal variations of zircon Hf isotopes showing that the εHf(t) values of the studied granodiorite are higher than those of crustal-derived Permian granitoids in the South Tianshan; (b) (87Sr/86Sr)initial vs. εNd(t) diagram showing the slightly enriched Sr-Nd compositions of the studied granodiorite. Cenozoic slab-derived adakites [90], MORB and marine sediments [91], Permian granitoids in the South Tianshan [30,36,92], slab-derived adakites from the LYRB [93], and references therein are shown for comparison. LYRB, Lower Yangtze River Belt.
Figure 8. (a) Temporal variations of zircon Hf isotopes showing that the εHf(t) values of the studied granodiorite are higher than those of crustal-derived Permian granitoids in the South Tianshan; (b) (87Sr/86Sr)initial vs. εNd(t) diagram showing the slightly enriched Sr-Nd compositions of the studied granodiorite. Cenozoic slab-derived adakites [90], MORB and marine sediments [91], Permian granitoids in the South Tianshan [30,36,92], slab-derived adakites from the LYRB [93], and references therein are shown for comparison. LYRB, Lower Yangtze River Belt.
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Figure 9. (a) Y vs. Sr/Y [90], and (b) YbN vs. (La/Yb)N [96] diagrams showing the typical adakitic affinity of the granodiorite. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
Figure 9. (a) Y vs. Sr/Y [90], and (b) YbN vs. (La/Yb)N [96] diagrams showing the typical adakitic affinity of the granodiorite. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
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Figure 10. Discrimination diagrams showing the high-Si adakite affinity of the studied granodiorite. (a) Al2O3 (wt.%) vs. K2O/Na2O diagram; reference fields are based on [93] and references therein; (b) TiO2 (wt.%) vs. Cr/Ni diagram [94]; (c,d) SiO2 (wt.%) vs. MgO (wt.%), Nb (ppm) diagrams [94]. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
Figure 10. Discrimination diagrams showing the high-Si adakite affinity of the studied granodiorite. (a) Al2O3 (wt.%) vs. K2O/Na2O diagram; reference fields are based on [93] and references therein; (b) TiO2 (wt.%) vs. Cr/Ni diagram [94]; (c,d) SiO2 (wt.%) vs. MgO (wt.%), Nb (ppm) diagrams [94]. Data source for the ca. 314 Ma adakitic granodiorite is as in Figure 6.
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Figure 13. Discrimination diagrams of (a) Y (ppm) vs. Nb (ppm) and (b) (Y + Nb) ppm vs. Rb (ppm) [126] showing the magmatic arc nature of the studied adakitic granodiorite, which is consistent with those of arc-related granitoids in the South Tianshan (Data are from [27,30,36]).
Figure 13. Discrimination diagrams of (a) Y (ppm) vs. Nb (ppm) and (b) (Y + Nb) ppm vs. Rb (ppm) [126] showing the magmatic arc nature of the studied adakitic granodiorite, which is consistent with those of arc-related granitoids in the South Tianshan (Data are from [27,30,36]).
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Figure 14. Conceptual model depicting upwelling of the asthenosphere induced by southward rollback of the South Tianshan oceanic slab and the resulting slab-derived magmatism that formed the Late Carboniferous adakitic granodiorite in the South Tianshan. STAC, South Tianshan Accretionary Complex.
Figure 14. Conceptual model depicting upwelling of the asthenosphere induced by southward rollback of the South Tianshan oceanic slab and the resulting slab-derived magmatism that formed the Late Carboniferous adakitic granodiorite in the South Tianshan. STAC, South Tianshan Accretionary Complex.
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Table 1. Results of LA-ICP-MS U-Pb dating of the Late Carboniferous adakitic granodiorite in the South Tianshan.
Table 1. Results of LA-ICP-MS U-Pb dating of the Late Carboniferous adakitic granodiorite in the South Tianshan.
SpotTh/U207Pb/206Pb±1σ207Pb/235U±1σ206Pb/238U±1σ207Pb/206Pb (Ma)±1σ207Pb/235U (Ma)±1σ206Pb/238U (Ma)±1σ
22ST18-010.37 0.052430.001730.378240.013220.052360.00090306743269.73295.5
22ST18-020.62 0.053670.003160.363600.019920.049480.0007936713331514.83114.8
22ST18-030.48 0.049460.002340.336000.015410.049510.0006516911129411.73124.0
22ST18-040.59 0.057750.002510.394600.017260.049620.000745209633812.63124.5
22ST18-050.81 0.057370.004360.395260.034840.049270.0012550616833825.43107.7
22ST18-060.84 0.056100.001880.555240.020710.071540.000894576944813.54455.4
22ST18-070.27 0.052530.001960.359900.012950.049830.00085309853129.73145.2
22ST18-080.48 0.051730.002280.352450.016160.049410.0007527210230712.13114.6
22ST18-090.57 0.059220.004250.567800.041240.069770.0013257615745726.74358.0
22ST18-100.84 0.059120.003290.607370.031970.074990.0010657211648220.24666.4
22ST18-110.53 0.054380.002660.375410.021440.049770.0010338711132415.83136.3
22ST18-121.00 0.056300.003890.521690.030150.068140.0013546515442620.14258.2
22ST18-130.55 0.050860.003190.343450.021950.048940.0007823514430016.63084.8
22ST18-140.40 0.049620.001990.335560.014100.049190.0008617612729410.73105.3
22ST18-150.58 0.054400.002000.365680.012340.048950.00069387883169.23084.2
22ST18-160.42 0.058160.002320.395640.016480.049400.000676008233812.03114.1
22ST18-170.51 0.053760.001830.362090.013710.048840.000763617631410.23074.7
22ST18-180.56 0.057890.002430.394360.019910.049260.001185249333814.53107.2
22ST18-190.54 0.058640.002590.395760.018840.048850.0007155410133913.73074.4
22ST18-200.50 0.055250.002140.369880.014850.048780.000774338732011.03074.7
Table 2. Major (%) and trace element (ppm) compositions of the Late Carboniferous adakitic granodiorite from the South Tianshan.
Table 2. Major (%) and trace element (ppm) compositions of the Late Carboniferous adakitic granodiorite from the South Tianshan.
Sample22ST18-122ST18-222ST18-322ST18-422ST18-5
SiO268.7968.3969.2767.7567.94
TiO20.510.510.500.520.49
Al2O315.7215.6815.7415.9015.29
TFe2O32.902.812.812.842.71
MnO0.040.030.040.040.03
MgO1.541.541.541.591.48
CaO3.203.193.153.373.15
K2O2.122.081.932.342.88
Na2O4.034.204.024.264.03
P2O50.160.160.160.170.15
LOI 10000.580.590.550.620.86
Mg#55 56 56 57 56
K2O + Na2O6.156.285.956.606.91
K2O/Na2O0.530.500.480.550.71
A/CNK1.071.051.091.010.99
Li22.2923.8218.1627.0132.88
Be2.051.801.861.971.74
Sc3.283.323.413.754.76
V31.3231.4830.7832.4830.33
Cr36.6733.2033.3135.4337.86
Co6.586.756.466.756.32
Ni23.8224.2522.1824.1323.03
Cu8.4815.937.675.307.55
Zn60.9660.3455.2459.0655.15
Ga20.9220.7519.4621.2821.96
Rb80.0479.9878.6286.4894.35
Sr504 509 479 530 512
Y7.397.357.127.357.44
Zr172 172 167 171 173.97
Nb9.947.826.838.427.33
Sn2.192.061.952.281.97
Sb0.290.140.050.050.10
Cs5.214.484.784.313.84
Ba 900 910 866 874 861
La36.1036.8032.5034.9036.30
Ce62.9962.7151.3664.0264.28
Pr7.387.536.797.217.39
Nd25.5425.3921.0926.6326.81
Sm4.654.573.804.524.73
Eu1.111.141.061.251.20
Gd3.163.022.723.073.10
Tb0.380.380.360.350.34
Dy1.631.611.561.661.66
Ho0.260.260.260.260.25
Er0.580.620.630.630.60
Tm0.070.080.070.070.06
Yb0.450.470.430.450.43
Lu0.070.060.060.060.06
Hf4.234.214.364.134.21
Ta0.610.490.480.510.47
W0.690.570.760.550.50
Tl0.430.410.420.460.47
Th12.2012.4011.9511.9511.85
U2.382.362.242.502.41
Sr/Y6869677269
∑REE144.4144.6122.7145.1147.2
(La/Yb)N5856545661
(La/Sm)N5.05.25.55.05.0
δEu0.890.941.011.030.96
Mg#: 100 × (MgO/40.3044)/(MgO/40.3044 + ((Fe2O3T × 0.8998)/71.844) × 0.85); δEu = EuN/SQRT (SmN × GdN).
Table 3. Results of Hf isotopes for zircons from the Late Carboniferous adakitic granodiorite in the South Tianshan.
Table 3. Results of Hf isotopes for zircons from the Late Carboniferous adakitic granodiorite in the South Tianshan.
SpotAge (Ma)176Yb/177Hf176Lu/177Hf176Hf/177Hf1σεHf(t) 1σTDM1TDM2
22ST18-02311 0.0023530.0006670.2826200.000020 1.45 0.86876 1237
22ST18-03312 0.0095890.0002950.2825980.000023 0.63 0.95913 1290
22ST18-04312 0.0157470.0005250.2827980.000038 7.66 1.45638 840
22ST18-05310 0.0080130.0002490.2825880.000025 0.25 1.01925 1313
22ST18-07314 0.0107290.0003650.2826000.000024 0.75 1.00911 1284
22ST18-08311 0.0091270.0002980.2825850.000022 0.16 0.93930 1319
22ST18-11313 0.0153410.0005230.2825950.000028 0.52 1.11922 1298
22ST18-13308 0.0101970.0003420.2825900.000017 0.27 0.79924 1310
22ST18-14310 0.0120330.0004250.2825900.000019 0.29 0.86927 1311
22ST18-15308 0.0124690.0004090.2825440.000026 −1.36 1.06989 1414
22ST18-16311 0.0091310.0003230.2825450.000022 −1.24 0.93986 1409
22ST18-17307 0.0101640.0003400.2825780.000026 −0.20 1.04942 1339
22ST18-18310 0.0100970.0003370.2824930.000034 −3.11 1.311058 1527
22ST18-19307 0.0098960.0003320.2825770.000031 −0.20 1.20942 1340
22ST18-20307 0.0110240.0003700.2825150.000023 −2.42 0.951029 1481
Table 4. Results of Bulk-rock Sr-Nd isotopes for the Late Carboniferous adakitic granodiorite in the South Tianshan.
Table 4. Results of Bulk-rock Sr-Nd isotopes for the Late Carboniferous adakitic granodiorite in the South Tianshan.
SamplesRb (ppm)Sr (ppm)87Rb/86Sr87Sr/86Sr87Sr/86Sr (i)Sm (ppm)Nd (ppm)147Sm/
144Nd		143Nd/
144Nd 		TDM1 (Ma)TDM2
(Ma)		143Nd/
144Nd(i)		εNd(t)
22ST18-182.3 515 0.460.708170 0.706161 4.56 26.07 0.105725 0.512322 1174 1285 0.512107 −2.58
22ST18-280.0 509 0.450.708094 0.706120 4.57 25.39 0.108735 0.512333 1190 1276 0.512113 −2.47
22ST18-378.6 479 0.480.708172 0.706110 3.80 21.09 0.108917 0.512303 1237 1325 0.512082 −3.08
22ST18-486.5 530 0.47 0.708255 0.706205 4.52 26.63 0.102542 0.512309 1158 1295 0.512101 −2.71
22ST18-594.3 512 0.530.708401 0.706086 4.73 26.81 0.106592 0.512298 1218 1326 0.512082 −3.09
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Abuduxun, N.; Xiao, W.; Zhang, W.; Yang, H.; Alimujiang, A.; Huang, P.; Gan, J. Late Carboniferous Slab Rollback in the Southern Altaids: Evidence from a Slab-Derived Adakitic Granodiorite in the South Tianshan. Minerals 2025, 15, 674. https://doi.org/10.3390/min15070674

AMA Style

Abuduxun N, Xiao W, Zhang W, Yang H, Alimujiang A, Huang P, Gan J. Late Carboniferous Slab Rollback in the Southern Altaids: Evidence from a Slab-Derived Adakitic Granodiorite in the South Tianshan. Minerals. 2025; 15(7):674. https://doi.org/10.3390/min15070674

Chicago/Turabian Style

Abuduxun, Nijiati, Wenjiao Xiao, Wanghu Zhang, He Yang, Abidan Alimujiang, Peng Huang, and Jingmin Gan. 2025. "Late Carboniferous Slab Rollback in the Southern Altaids: Evidence from a Slab-Derived Adakitic Granodiorite in the South Tianshan" Minerals 15, no. 7: 674. https://doi.org/10.3390/min15070674

APA Style

Abuduxun, N., Xiao, W., Zhang, W., Yang, H., Alimujiang, A., Huang, P., & Gan, J. (2025). Late Carboniferous Slab Rollback in the Southern Altaids: Evidence from a Slab-Derived Adakitic Granodiorite in the South Tianshan. Minerals, 15(7), 674. https://doi.org/10.3390/min15070674

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