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Article

Petrogenesis of Carboniferous-Permian Granitoids in the Kumishi Area of Tianshan, China: Insights into the Geodynamic Evolution Triggered by Subduction and Closure of the South Tianshan Ocean

by
Wenbin Kang
1,
Kai Weng
2,*,
Kai Cao
2,
Xiaojian Zhao
2 and
Yongwei Gao
2
1
School of Coal Engineering, Shanxi Datong University, Datong 037003, China
2
Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits MNR, Xi’an Center of Geological Survey, Western Cangtai Road, Xi’an 710119, China
*
Author to whom correspondence should be addressed.
Minerals 2024, 14(8), 811; https://doi.org/10.3390/min14080811 (registering DOI)
Submission received: 23 July 2024 / Revised: 8 August 2024 / Accepted: 9 August 2024 / Published: 11 August 2024
(This article belongs to the Special Issue Metallogenesis of the Central Asian Orogenic Belt)
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Abstract

:
Late Carboniferous–Early Permian granitoids are widespread in the Tianshan area and their tectonic setting is controversially discussed. Our research presents fresh whole-rock geochemical and Pb isotopic data, along with zircon U-Pb ages and Hf isotopic data for representative monzonitic and granitic intrusions in the Kumishi area. The aim is to decipher their magma sources and illuminate their geodynamic evolution. Zircon U-Pb dating results reveal that biotite monzonites in the Central Tianshan Belt were emplaced at 312.7 ± 2.9 Ma, while the quartz-monzonites and syenogranites in the South Tianshan Belt were formed at 284.5 ± 2.4 Ma and 283.4 ± 3.9 Ma, respectively. The biotite monzonites generally exhibit metaluminous and high-K calc-alkaline characteristics. They have a positive εHf(t) value (+4.9–+14.1), and are enriched in LREEs and LILEs but depleted in HREEs and HFSEs. These characteristics indicate that they were derived from a mixed magma source of the lower crust and the input of components derived from the mantle wedge above the subduction zone. The quartz-monzonites and syenogranites are high-K calc-alkaline to shoshonitic I-type granites, with εHf(t) values of +14.9–+15.5 and +6.6–+14.9, respectively. They are enriched in LREEs but depleted in HFSEs (e.g., Nb, Ta, and Ti), displaying relatively flat HREE patterns and negative Eu anomalies. The genesis of these rocks is attributed to a partial melting of the lower crust in which mantle-derived magmas participated, which was triggered by an upwelling asthenosphere in a post-collisional extensional geodynamic setting. These granitoids, together with regional analysis of other magmatism in the study area, suggest that the Kumishi area has experienced an evolution from subduction to post-collision from the Late Carboniferous to the Early Permian, which constrains the local closure of the Paleo-Asian Ocean.

1. Introduction

The Central Asian Orogenic Belt (CAOB) is a vast accretionary orogen that extends between the Siberian and Europe Cratons to the north and the Tarim and North China Cratons to the south (Figure 1a) [1,2,3,4,5,6,7,8,9,10]. The Tianshan Orogen, stretching over 2500 km through Uzbekistan, Tajikistan, Kyrgyzstan, and Kazakhstan to Xinjiang in northwestern China, occupies the southwestern part of the CAOB [1,2,5,11,12,13]. The Chinese portion of the Tianshan represents the final collision zone of the Paleo-Asian Ocean (PAO) between the Siberian and Tarim cratons [13,14]. It is dominated by Paleozoic subduction- and collision-related rocks along the Northern Central Tianshan and Southern Central Tianshan sutures [7,15,16,17,18,19,20,21,22,23,24,25,26,27,28], which separate the North Tianshan, Central Tianshan, and South Tianshan Belts from north to south (Figure 1a) [29]. The precise timing and nature of the CAOB’s final accretion-collision processes are important [6,7,27], yet there is an ongoing debate about the tectonic setting of the Chinese Tianshan Orogen during the Late Paleozoic and the timing of the South Tianshan Ocean’s closure, with proposed dates ranging from the Late Devonian [26,30,31,32,33], through to the Early Carboniferous [15,34], the end of the Early Carboniferous [22,35,36,37], the end of the Carboniferous to the Early Permian [8,26,38,39,40,41,42], and the Triassic [7,27,43,44].
Generally, the temporal and spatial distribution of granitic rocks and mafic-intermediate rocks is genetically related to geodynamic processes [45,46,47]. Hence, we present new whole-rock geochemical and Pb isotopic data, zircon U-Pb ages, and Hf isotopic data for selected monzonitic and granitic intrusions in the Kumishi area. The aim is to constrain their source and genetic relationship in order to unravel the Late Paleozoic geodynamic evolution of the Tianshan and the final formation of the southern CAOB.

2. Geological Setting of the Central Tianshan

The Chinese Tianshan is geographically subdivided into three sections: the western, middle, and eastern [29]. Our research concentrates on the Kumishi area located in the middle of the Chinese Tianshan, which is the narrowest part of the range. Tectonically, the middle of Tianshan range can be subdivided into the Northern, Central, and Southern Tianshan belts [7,26], which are separated by the Northern Central Tianshan suture (NCTS) and the Southern Central Tianshan suture (SCTS) (Figure 1b).
The Northern Tianshan Belt (NTB) is recognized as a continental magmatic arc that formed during the Late Paleozoic, related to the southward subduction of the northern Tianshan Ocean [6,7,22]. From the Early Devonian to Late Permian, the NTB mainly consists of sedimentary sequences, calc-alkaline volcanic, and intrusive rocks, which are unconformably overlain by Jurassic or Mesozoic clastic rocks [32,48]. The NTB is bordered to the south by the NCTS, characterized by Early Paleozoic ophiolites and related assemblages in Tangbale [49,50], Bingdaban [21], and the Gangou area [20]. Further east, the NCTS extends to the Kangguertage ophiolites [51,52], eventually intersected by the NE-trending Altyn Tagh strike-slip fault.
The Central Tianshan Belt (CTB) consists of the Western CTB and Eastern CTB. The Western CTB, which is the Yili area, predominantly comprises thick sedimentary cover strata from the Upper Proterozoic to Upper Paleozoic. In contrast, the Eastern CTB is characterized by the metamorphosed Meso-Proterozoic basement of the Baluntai Group in amphibolite facies [53] and the greenschist-facies metamorphosed Ordovician Kekenaike Formation, which is unconformably overlain by the Lowermost Carboniferous Maanqiao Formation. Notably, a large number of Paleozoic granitoids intruded into the Eastern CTB (Figure 1c).
The Southern Tianshan Belt (STB) is separated from the CTB by the southern boundary fault of the CTB, identified as a suture marked by ophiolites such as the Changawuzi, Guluogou [22], the Wuwamen [19], and the metamorphosed Yushugou ophiolite [18,54] from west to east. It comprises the deformed and metamorphosed basement of the Paleo-Proterozoic Xingditagh Group, which is covered by greenschist-facies metamorphic Mid-Proterozoic and nearly non-metamorphosed Upper Proterozoic to Paleozoic sedimentary sequences in the southern STB.

3. Sampling and Petrography

In our study, fifteen representative samples were selected from various monzonitic and granitic plutons in the Kumishi area (Figure 1c). Biotite monzonite samples were collected from the south margin of the CTB (18ZB-26-1, 2, and 3; 18ZB-44-1, 2, 3, and 4) and intruded into the Proterozoic Baluntai Group and Ordovician granite (Figure 1c). The biotite monzonite exhibits an equigranular texture and contains moderate grains of quartz, plagioclase, and K-feldspar, and is intruded by the granitic stocks. The monzonite predominantly consists of quartz (2–3 vol.%), weakly altered plagioclase (55–58 vol.%), biotite (8–10 vol.%), K-feldspar (28–30 vol.%), and calcite (1–2 vol.%). The accessory minerals include sphene, zircon, and apatite (Figure 2a,b).
The quartz-monzonitic and syenogranitic pluton is located in the northern margin of the STB and intrudes into the Lower Devonian Arbishimibulake Formation (Figure 1c), and the boundary between the two types of granitoids is gradual. The quartz-monzonitic pluton shows a typical porphyritic-like texture, with mineral grains mostly in medium and fine sizes. The phenocrysts (8–10 vol.%) mainly consist of plagioclase, while the matrix (90–92 vol.%) with a fine-grained granitic texture contains a mineral assemblage of quartz (8–10 vol.%), K-feldspar (45–50 vol.%), weakly altered plagioclase (20–25 vol.%), and a small amount of biotite (3–5 vol.%) (Figure 2b,c). The quartz-monzonitic pluton is represented by samples 18ZB-35-1, 2, 3, and 4.
The syenogranitic pluton is represented by samples 18ZB-24-1, 2, 3, and 4, which primarily consist of quartz (20–22 vol.%), weakly altered plagioclase (20–25 vol.%), and K-feldspar (50–55 vol.%), with small amounts of biotite (2–3 vol.%). The accessory minerals include magnetite and apatite. These granites mostly exhibit an equigranular texture and contain moderate grains of quartz, plagioclase, and K-feldspar (Figure 2e,f).

4. Analytical Methods

4.1. Zircon U-Pb Dating and Zircon Hf Isotope Analyses

Zircon grains were separated from crushed rocks using conventional heavy liquid and magnetic separation techniques, and subsequently handpicked under a binocular microscope. The zircon grains were mounted in an epoxy resin disk and polished to approximately half their thickness. Cathodoluminescence (CL) images of the zircons were obtained to examine their internal structures.
The U-Pb isotopic analyses of zircons were conducted at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, Xi’an Center of China Geological Survey, MNR. The analyses were performed using an Agilent 7700x ICP–MS instrument (Agilent, Middelburg, The Netherlands) equipped with a GeoLas Pro 193 nm ArF Excimer laser ablation system, with a beam diameter of 24 μm. Zircon standard 91500 was utilized for calibrating the U-Pb ages of the measured samples. Details of the instrumental conditions and data acquisition procedures were like those described by Li [55]. Isotopic ratios were calculated using GLITTER 4.0 [56], while age calculation and plotting of Concordia diagrams were conducted using Isoplot/Ex 3.0 [57].
Zircon Hf isotope analyses were carried out at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, MNR, Xi’an Center of Geological Survey, China Geological Survey. The analyses were performed using a GeoLas Pro laser ablation system coupled to a Neptune multiple-collector ICP-MS. Details of the instrumental conditions and data acquisition procedures are like those described by Meng [58] and Hou [59]. The analyses were conducted using a stationary laser ablation spot with a beam diameter of 30 μm. The ablated aerosol was transported by helium and subsequently mixed with argon in a mixing chamber before being introduced to the ICP-MS plasma. The Hf analyses were performed on the same spots used for U-Pb laser ablation. Zircon GJ-1 was utilized as the reference standard, resulting in a weighted mean 176Hf/177Hf ratio of 0.282030 ± 40 (2SE) during this study.

4.2. Whole-Rock Geochemical Analyses

The samples for whole-rock analyses were crushed to 200-mesh size using an agate mill. Whole-rock major element concentrations were measured on fused glass disks with a 1:8 sample to Li2B4O7 flux ratio using a Phillips PW 240 X-ray fluorescence (XRF) spectrometer (Philips, Australia). The measurements were conducted at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, Xi’an Center of China Geological Survey, MNR, with a precision better than 1%. Trace elements, including the rare earth elements (REEs), were determined by ICP–MS using an Agilent 7700×ICP–MS system at the same laboratory. The precision for minor element content was better than 5%. For a detailed analytical process, please refer to those described by Ma [60] and Gao [61].
Whole-rock Pb isotopic compositions were determined using an ISOPROBE-T thermal ionization mass spectrometer at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, Xi’an Center of China Geological Survey, MNR. Lead isotopic analyses were corrected using NBS981 as reference material. The uncorrected results were 208Pb/206Pb = 2.164940 ± 15, 207Pb/206Pb = 0.914338 ± 7, 204Pb/206Pb = 0.0591107 ± 2.

5. Results

5.1. Zircon U-Pb Geochronology and Lu-Hf Isotopes

Zircons from the biotite monzonite sample (18ZB-44-4) are mostly prismatic in shape and show a well-developed magmatic oscillatory zoning in CL images (Figure 3a). They have moderate Th (105–425 ppm) and U (238–1398 ppm) content with moderate Th/U ratios (0.17–0.86) (Table 1). Twelve zircons were analyzed, yielding a weighted mean 206Pb/238U age of 312.7 ± 2.9 Ma (MSWN = 0.16) (Figure 3a), which represents the biotite monzonite formation age. Zircons from the biotite monzonite have variable Hf isotopic compositions, with 176Hf/177Hf ratios ranging from 0.282721 to 0.282992, and εHf(t) values ranging from +4.9 to +14.1. The Hf model ages of TDM1 and TDM2 range from 385 to 753 Ma and 469 to 1309 Ma, respectively (Table 2).
Zircons from sample 18ZB-35-4 of the quartz-monzonite exhibit stubby to weakly prismatic shape and well-developed magmatic oscillatory zoning in CL images (Figure 3b). The grains have moderate Th (83–709 ppm) and U (84–950 ppm) content with moderate Th/U ratios (0.48–1.18) (Table 1). Fifteen zircons were analyzed, yielding a weighted mean 206Pb/238U age of 284.5 ± 2.4 Ma (MSWN = 0.73) (Figure 3b), which represents the quartz-monzonite formation age. Zircons from the quartz-monzonite have variable Hf isotopic compositions, with 176Hf/177Hf ratios ranging from 0.283017 to 0.283032, and εHf(t) values ranging from +14.9 to +15.5. The Hf model ages of TDM1 and TDM2 range from 304 to 326 Ma and 326 to 375 Ma, respectively (Table 2).
Zircon grains from sample 18ZB-24-4 of the syenogranite exhibit stubby to weakly prismatic shapes and oscillatory zoning in CL images (Figure 3c). These grains have moderate Th (123–597 ppm) and U (161–1052 ppm) content with moderate Th/U ratios (0.29–0.76) (Table 1). These characteristics are consistent with those of igneous zircon. Twelve zircons were analyzed, yielding a weighted mean 206Pb/238U age of 283.4 ± 3.9 Ma (MSWN = 0.13) (Figure 3), which represents the syenogranite formation age. Zircons from the syenogranite have variable Hf isotopic compositions with 176Hf/177Hf ratios ranging from 0.282786 to 0.283025, and εHf(t) values ranging from +6.6 to +14.9. The Hf model ages of TDM1 and TDM2 range from 327 to 657 Ma and 381 to 1133 Ma, respectively (Table 2).

5.2. Whole-Rock Geochemistry

The major and trace element compositions of the representative samples of granitoids are provided in Table 3. The biotite monzonite samples are plotted in the monzonites field with high-K calc-alkaline affinities (Figure 4a,b). They have a SiO2 content of 55.25–59.50 wt.%, TiO2 of 0.72–1.06 wt.%, MgO of 2.25–2.46 wt.%, Al2O3 of 17.06–20.59 wt.%, Fe2O3 of 1.45–2.55 wt.%, FeO of 2.50–3.50 wt.%, CaO of 4.50–5.29 wt.%, K2O of 3.02–3.56 wt.%, Na2O of 4.07–4.97 wt.%, and Mg# of 50.2–51.8. These samples are characterized by enrichment of LREEs ((La/Yb)N = 33.23–41.57), significant depletion of HREEs ((Gd/Yb)N = 2.83–4.09), and negative Eu anomalies (δEu = 0.75–0.89) (Figure 5a). Meanwhile, they also show negative anomalies of Nb, Ta, P, and Ti, but positive anomalies of Rb, Ba, Th, U, K, Sr, Nd, and Pb (Figure 5b). The biotite monzonite has initial ratios of 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb at 18.168–18.320, 15.612–15.613, and 38.143–38.448, respectively (Table 4).
Table 3. Whole-rock major and trace element composition of the studied plutons in the Kumishi area.
Table 3. Whole-rock major and trace element composition of the studied plutons in the Kumishi area.
Sample18ZB-44-118ZB-44-218ZB-44-318ZB-26-118ZB-26-218ZB-26-318ZB-24-118ZB-24-218ZB-24-318ZB-35-118ZB-35-218ZB-35-3
LithologyBiotite MonzoniteBiotite MonzoniteBiotite MonzoniteBiotite MonzoniteBiotite MonzoniteBiotite MonzoniteSyenograniteSyenograniteSyenograniteQuartz-MonzoniteQuartz-MonzoniteQuartz-Monzonite
Major elements (wt.%)
SiO256.4556.1155.2558.2059.1259.5076.8777.0477.8261.5563.8271.38
Al2O320.2820.2820.5917.3617.0617.3712.0912.2711.7615.9516.2813.75
Fe2O31.451.451.562.282.372.550.550.360.001.902.010.99
FeO3.253.503.352.852.502.540.350.601.052.082.181.18
CaO4.764.834.725.295.084.500.590.560.544.942.351.47
MgO2.292.462.432.372.252.320.080.060.071.211.160.66
K2O3.063.023.563.143.063.114.794.674.525.215.845.81
Na2O4.974.904.904.074.074.133.633.843.613.323.292.98
TiO20.720.780.761.061.021.040.060.050.040.600.610.33
P2O50.560.600.580.460.430.440.01<0.01<0.010.190.190.09
MnO0.050.060.060.080.080.080.020.030.030.080.070.04
LOI1.671.491.662.502.672.080.950.510.652.741.981.14
A/CNK1.011.011.000.880.890.950.990.991.000.791.020.99
A/NK1.771.791.731.721.701.711.081.081.091.441.391.23
FeOt4.554.804.754.904.634.830.840.921.053.793.992.07
Mg#51.3051.8051.7050.3050.5050.2016.6012.0012.3040.1037.9040.10
Trace element (ppm)
Cu2.812.332.285.124.514.680.600.380.3936.607.769.34
Pb23.7022.3026.0017.8017.3017.3031.7039.6038.809.3114.5015.80
Zn63.3064.3070.6099.6090.7096.6022.3031.7032.1038.2044.8031.40
Ni9.228.439.106.906.527.171.210.901.065.725.113.08
Co11.2011.3012.009.989.9810.900.290.180.167.446.794.36
Li27.1027.8028.2035.2033.6033.3012.8054.5051.908.769.185.67
Rb128.00131.00149.00150.00148.00159.00343.00409.00397.00149.00191.00188.00
Cs7.548.029.403.343.093.197.0816.6015.203.894.794.46
W0.440.420.440.160.200.170.791.541.501.720.901.03
Mo0.260.240.200.740.890.820.530.570.631.180.630.93
Sr1700.001750.002000.001090.001030.001100.004.357.045.08493.00419.00289.00
Ba2310.002280.002530.001310.001140.001290.009.854.833.56999.001140.00928.00
V93.6093.9098.8081.3072.8079.201.330.630.4946.2048.6028.00
Sc14.1013.3013.8012.2012.1011.507.8410.308.3617.0015.4012.80
Nb11.6010.8011.0020.8020.4021.1015.3016.4018.0016.0017.0011.40
Ta0.830.790.701.341.431.361.552.022.051.130.961.14
Zr285.00298.00294.00304.00284.00300.0081.7096.50100.00236.00282.00165.00
Hf7.117.176.827.827.287.463.584.784.937.057.925.29
Ga21.8020.2021.8024.6023.8024.4018.4022.4018.8016.6016.8013.10
Sn2.411.981.692.952.863.043.375.495.120.840.910.63
U2.372.442.952.032.382.325.598.1110.003.082.584.31
Th31.0028.5024.2019.5017.3018.0041.4054.5048.6014.4013.1026.30
La109.00105.0097.3089.6085.2096.2016.9017.6014.8030.6038.1030.70
Ce189.00191.00178.00173.00174.00188.0044.1045.7040.4068.1079.1060.40
Pr21.0020.4019.2019.9019.8020.806.216.335.638.769.696.77
Nd70.6069.3067.5068.3065.5067.7026.2027.6022.3032.3034.3023.30
Sm11.3010.3010.3011.1010.9011.207.317.856.587.246.824.39
Eu2.692.522.712.422.362.530.080.060.041.841.691.18
Gd8.387.437.687.817.607.647.697.846.766.515.973.72
Tb1.101.011.020.961.031.001.381.441.301.020.920.57
Dy4.884.464.674.204.784.418.639.077.725.844.813.06
Ho0.890.850.880.740.790.761.701.831.621.130.950.62
Er2.412.342.351.861.981.934.515.154.443.192.561.76
Tm0.350.350.350.270.280.280.650.780.730.480.390.28
Yb2.262.172.101.581.621.664.065.194.583.182.581.89
Lu0.330.340.320.240.240.240.590.800.710.480.400.31
Y23.0020.6022.7018.9019.2019.3037.0048.4042.0028.0023.8016.70
(La/Yb)N34.6034.7133.2340.6837.7241.572.992.432.326.9010.5911.65
(Gd/Yb)N3.072.833.034.093.883.811.571.251.221.691.911.63
δEu0.810.840.890.750.750.790.030.020.020.800.790.87
Note: A/CNK = molar Al2O3/(CaO + Na2O + K2O); A/NK = molar Al2O3/(Na2O + K2O); Mg# = Mg2+/(Mg2+ + Fe2+) * 100; δEu = 2*EuN/(SmN + GdN); Chondrite-normalized values from Sun and McDonough [62].
Minerals 14 00811 g004
Figure 4. Major element diagrams for the granitoids in the Kumishi area. (a) Total alkali (wt.%) vs. silica diagram (wt.%) [63]; the alkaline and sub-alkaline division is after Irvine and Baragar [64]. (b) K2O (wt.%) vs. SiO2 (wt.%) (after Peccerillo and Taylor [65] and Calanchi [66]). (c) ANK vs. ACNK diagram [67] (data for compiled magmatic rocks are listed in Table S2).
Figure 4. Major element diagrams for the granitoids in the Kumishi area. (a) Total alkali (wt.%) vs. silica diagram (wt.%) [63]; the alkaline and sub-alkaline division is after Irvine and Baragar [64]. (b) K2O (wt.%) vs. SiO2 (wt.%) (after Peccerillo and Taylor [65] and Calanchi [66]). (c) ANK vs. ACNK diagram [67] (data for compiled magmatic rocks are listed in Table S2).
Minerals 14 00811 g004
Minerals 14 00811 g005
Figure 5. (a,c) Chondrite-normalized rare earth element (REE) patterns and (b,d) primitive mantle-normalized multielement variation diagrams for the granitoids in the Kumishi area. The chondrite values and primitive mantle values are after Taylor and McLennan [68] and Sun and McDonough [62], respectively (data for compiled magmatic rocks are listed in Table S2).
Figure 5. (a,c) Chondrite-normalized rare earth element (REE) patterns and (b,d) primitive mantle-normalized multielement variation diagrams for the granitoids in the Kumishi area. The chondrite values and primitive mantle values are after Taylor and McLennan [68] and Sun and McDonough [62], respectively (data for compiled magmatic rocks are listed in Table S2).
Minerals 14 00811 g005
Table 4. Whole-rock Pb isotope composition of the studied plutons in the Kumishi area.
Table 4. Whole-rock Pb isotope composition of the studied plutons in the Kumishi area.
SamplesLithologyUThPb206Pb/204Pb207Pb/204Pb208Pb/204Pbt(Ma)(206Pb/204Pb)i(207Pb/204Pb)i(208Pb/204Pb)i
18ZB-44-2Biotite monzonite2.4428.5022.3018.55415.63239.56831318.16815.61238.143
18ZB-26-32.3218.0017.3018.79315.63839.60831318.32015.61338.448
18ZB-24-2Syenogranite8.1154.5039.6019.25015.65139.26228318.59815.61737.876
18ZB-35-2Quartz-monzonite2.5813.1014.5018.76615.60839.08228518.19615.57838.166
18ZB-35-34.3126.3015.8019.42615.63339.75628518.55215.58838.068
The quartz-monzonites are plotted in the quartz-monzonite and granite fields in the TAS diagram with shoshonitic affinities (Figure 4a,b). They have a SiO2 content of 61.55–71.38 wt.%, TiO2 of 0.33–0.61 wt.%, MgO of 0.66–1.21 wt.%, Al2O3 of 13.75–16.28 wt.%, Fe2O3 of 0.99–2.01 wt.%, FeO of 1.18–2.18 wt.%, CaO of 1.47–4.94 wt.%, K2O of 5.21–5.84 wt.%, Na2O of 2.98–3.32 wt.%, and Mg# of 37.9–40.1. They can be classified as weakly metaluminous granite (A/CNK = 0.79–1.02 and A/NK = 1.23–1.44; Figure 4c). The quartz-monzonites exhibit remarkably enriched LREEs ((La/Yb)N = 6.9–11.7), relatively slightly depletion of HREEs ((Gd/Yb)N = 1.63–1.91), and negative Eu anomalies (δEu = 0.79–0.87) (Figure 5c), with strong negative Ba, Nb, Ta, Sr, P, and Ti anomalies, and enrichment in Rb, Th, U, K, and Pb (Figure 5d). The quartz-monzonites have initial ratios of 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ranging from 18.196–18.552, 15.578–15.588, and 38.068–38.166, respectively (Table 4).
The syenogranite samples are all plotted in the granite field with high-K calc-alkaline affinity (Figure 4a,b). These rocks have a SiO2 content of 76.87–77.82 wt.%, TiO2 of 0.04–0.06 wt.%, MgO of 0.06–0.08 wt.%, Al2O3 of 11.76–12.27 wt.%, Fe2O3 of 0.00–0.55 wt.%, FeO of 0.35–1.05 wt.%, CaO of 0.54–0.59 wt.%, K2O of 4.52–4.79 wt.%, Na2O of 3.61–3.84 wt.%, and Mg# of 12.0–16.6. They are metaluminous (A/CNK = 0.99–1 and A/NK = 1.08–1.09; Figure 4c). The syenogranite samples are characterized by weakly enriched LREEs ((La/Yb)N = 2.32–2.99), flat HREE patterns ((Gd/Yb)N = 1.22–1.57), and significant negative Eu anomalies (δEu = 0.02–0.03) (Figure 5c). Meanwhile, they are depleted in Ba, Sr, Nb, Ta, P, Eu, and Ti, and enriched in Rb, Th, U, K, and Pb (Figure 5d). The initial 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios of syenogranites are 18.598, 15.617, and 37.876, respectively (Table 4).
In the Harker diagrams (Figure 6), the content of Al2O3, TiO2, MgO, total FeO, CaO, MnO, Sr, and Ba decrease, while Rb content increases with increasing SiO2 for the quartz-monzonites and syenogranites.

6. Discussion

6.1. Petrogenesis and Magma Source of the Late Carboniferous Biotite Monzonite

The biotite monzonite displays obvious enrichment in Rb, Th, and U, and depletion in Nb, Ta, P, and Ti in the primitive mantle-normalized trace element spider diagrams (Figure 5b). These features are commonly observed in the continental crust derived from the chemical differentiation of arc-derived magmas [69]. Additionally, the biotite monzonite exhibits high Y content (18.9–23 ppm) and a low Sr/Y ratio (53.6–88.1), resembling normal arc-related magmas [70,71]. These intermediate rocks have high and variable εHf(t) values (+4.9–+14.1, average +8.4). On the t-εHf(t) diagram, the samples fall between the chondritic uniform reservoir (CHUR) and the depleted mantle evolution line (Figure 7a). Hence, these rocks may be derived from the melting of juvenile lower crust, which can also be supported by the Th/La ratios (0.19–0.28, 0.2–0.5 for crustal origin) [62,72], and Pb isotope evidence that plot the biotite monzonite data in the area of the lower crust (Figure 7b). However, the involvement of mantle-derived magmas in the formation of this intermediate rock can be recognized by similar geochemical characteristics to mantle-derived magmas, including (1) Y/Nb ratios (0.91–2.06, ∼1.2) [73]; and (2) high Mg# values (50.2–51.8, >40) [74,75]. The coeval tholeiitic Luotuogou gabbros (312 Ma) near our research area also formed by mixing between the asthenospheric and metasomatized lithospheric mantle, which indicated the existence of contemporary mantle-derived magma [76]. Therefore, the melting of juvenile lower crust with the mantle-derived magma’s participation gives rise to the biotite monzonite in this study.
The significant depletion of HREEs, along with negative Eu anomalies, indicates the presence of both garnet and plagioclase in the residue within the source magma [77,78], corresponding to the lower crustal granulite facies environment.

6.2. Petrogenesis and Magma Source of the Early Permian Granitoids

6.2.1. Petrogenetic Type of Early Permian Granitoids

Field observations show that the quartz-monzonites and syenogranites in our study are spatially associated and gradually change in mineral compositions. Chronologically, they are formed at 285 Ma and 283 Ma, which are consistent within the error range. Geochemically, they exhibit a consistent trend in the Harker variation diagrams (Figure 6). These features suggest that the quartz-monzonites and syenogranites are the products of magmatic differentiation during a single magmatic event with the same source.
The quartz-monzonites and syenogranites contain a small amount of biotite and are not present in an interstitial form (Figure 3d,f). Furthermore, no typical alkaline dark minerals are found. The quartz-monzonites have geochemical characteristics of low HFSE (Zr, Nb, Ce, and Y) content and FeOT/MgO, (Na2O + K2O)/CaO, and 10,000 × Ga/Al ratios. These features are obviously similar to those of unfractionated I- and S-type granites (Figure 8). They possess a SiO2 content ranging from 61.55 to 71.38 wt.% and high K2O content (Figure 4b), with moderate A/CNK content (A/CNK ratio < 1.1; Figure 4c), suggesting affinities with shoshonitic I-type granites.
In contrast, the syenogranites plot in the A-type granite fields in Figure 8a–d, due to their high 10,000 × Ga/Al ratios. However, they have low content of Zr, Nb, Ce, and Y HFSEs, with a total content significantly below the lower limit for A-type granites (Zr + Nb + Ce + Y = 350 ppm). The samples plot in the fractionated I- or S-type granite fields in Figure 8e,f, indicating that the magma underwent a highly differentiated evolution. This is further supported by their high silicon content (76.87–77.82 wt%) and Rb/Sr ratios (58.1–78.9; >3), and low CaO, P2O5, Ba, Sr, Ti, and Zr/Hf ratios (20.2–22.8; <26) [80,81,82,83]. The highly differentiated evolution led to an increase in the 10,000 Ga/Al ratio, resulting in the syenogranites being plotted in the A-type granite fields in Figure 8a–d. For these Early Permian granites, P2O5 abundance decreases as the SiO2 content increases, and the concentrations of Th and Y rise along with the increasing Rb content, which is also characteristic of I-type granites (Figure 6g and Figure 9a,b). The syenogranites are weakly peraluminous and exhibit high K2O content (Figure 4b), suggesting affinities to high-K calc-alkaline I-type granites.
The K2O, Al2O3, and CaO content decreases with increasing SiO2 content for the quartz-monzonites and syenogranites (Figure 4b and Figure 6a,b) indicating that the K-feldspar fractionated from the magma. This is also supported by significant depletions in Sr, Ba, and Eu (Figure 5c,d), a negative correlation between Rb and Sr (Figure 9c), and a correlation between Ba and Sr (Figure 9d). Figure 6c–e shows negative correlations between SiO2 and total FeO, MgO, and MnO, and there is a negative correlation between Th and V (Figure 9f), indicating that biotite may have been a fractionation phase. The fractionation of apatite and sphene may cause the decrease in P2O5 and TiO2 content while SiO2 increases, respectively (Figure 6f,g). In the (La/Yb)N vs. La diagram (Figure 9e), the variations in REE content seem to be mainly related to fractionation of apatite and sphene. Therefore, during the formation of syenogranites, K-feldspar, biotite, apatite, and sphene likely fractionated from the quartz-monzonites. The less evolved geochemical affinities of quartz-monzonites indicate that they are more similar to the primary magmas.

6.2.2. Magma Source of the Early Permian Granitoids

The quartz-monzonites and syenogranites have arc-affinity trace element compositions, characterized by the enrichment of LILEs and LREEs relative to HFSEs, consistent with normal arc-related magmas, which have high Y content (16.7–48.4 ppm) and low Sr/Y ratios (0.12–17.61). The high SiO2 (61.55–71.38 wt%) and low MgO (0.66–1.21 wt%) content, along with low ratios of FeOT/MgO and (K2O + Na2O)/CaO, suggest that the quartz-monzonites were crystallized from crust-derived magmas. This is also supported by their Th/La ratios (0.34–0.85; 0.2–0.5 for crustal origin) [62,72] and Th/U ratios (4.68–6.10; ~6 for lower crustal origin) [86]. The Pb isotope compositions of the syenogranite and quartz-monzonite plot in the field of lower crust in Figure 7b. Moreover, zircons in the quartz-monzonites and syenogranites have highly positive εHf(t) values of +14.9 to +15.5 and +6.6 to +14.9, respectively, indicating a juvenile lower crustal source. Furthermore, the Nb/Ta ratios (10–17.78; 11–12 for crustal origin) [87] and Y/Nb ratios (1.4–1.75; >2 for crustal origin) [73] for these granitoids also indicate a crustal-dominated origin with minor mantle material input. The mafic enclaves found in the quartz-monzonite plutons also indicate a binary magma genesis (Figure 2c). The depletion of HREEs and the presence of negative Eu anomalies in the quartz-monzonite indicate that both garnet and plagioclase exist in the residue within the source magma (Figure 5c) [77,78], corresponding to the lower crustal granulite facies environment. Therefore, the granitoids may be the products of partial melting of mixing between lower crustal metabasaltic materials and minor mantle-derived magmas.

6.3. Tectonic Setting

The tectonic setting of the granitoids remains unclear, including models for an intra-continental rift or mantle plume [88,89,90,91], an arc-related setting [27,43,44,92,93,94], or a post-collisional setting [36,95,96]. Therefore, we assess tectonic and crustal evolution from the Late Carboniferous to the Early Permian by utilizing the granitic rocks studied here, in combination with already published whole-rock geochemistry and zircon Hf isotopic data of the Carboniferous to Early Permian magmatic rocks in the Kumishi area (Figure 4, Figure 5, and Figure 7a; Tables S1–S3).

6.3.1. Carboniferous Arc

The biotite monzonites are metaluminous and belong to high-K calc-alkaline series (Figure 4b,c) with the characteristics of enrichment in LREEs and LILEs and depletion in Nb, Ta, and Ti (Figure 5a,b), which implies that they may be related to subduction of the oceanic crust. Considering the petrographical, petrological, and geochemical discussion above, the biotite monzonites are interpreted as derived from a mixed origin that involves both crustal and mantle-derived components. In the major element discrimination diagram (Figure 10), the samples plot within the volcanic arc granite (VAG) field.
The compiled Carboniferous I-type granitoids in the Kumishi area, mainly distributed in the northern margin of the CTB (Figure 1c), belong to low-K to medium-K calc-alkaline series (Figure 4b) and exhibit metaluminous to peraluminous composition (Figure 4c). They show negative HFSE anomalies and LILE enrichment with strongly depleted Nb-Ta-Ti (Figure 5a,b), indicating their arc-related setting. According to Figure 10, the Carboniferous granitic rocks are plotted in the VAG field. Accordingly, the Carboniferous granitic rocks were formed in a volcanic arc tectonic setting.
Combining the geochemical characteristics of the magma source, petrology, and geochronology, we propose the biotite monzonites were formed in the CTB and were derived from a mixed magma source between the lower crust and the input of components derived from the mantle wedge above the subduction zone of the South Tianshan oceanic crust during the Carboniferous [97].
Minerals 14 00811 g010
Figure 10. Tectonic discrimination diagrams of the igneous rocks in the Kumishi area of (a) Y v. Nb, (b) Y + Nb v. Rb, (c) Yb v. Ta, and (d) Yb + Ta v. Rb [98] (data for compiled magmatic rocks are listed in Table S2). syn-COLG, syn-collisional granites; ORG, ocean ridge granites; VAG, volcanic arc granite; WPG, within-plate granite.
Figure 10. Tectonic discrimination diagrams of the igneous rocks in the Kumishi area of (a) Y v. Nb, (b) Y + Nb v. Rb, (c) Yb v. Ta, and (d) Yb + Ta v. Rb [98] (data for compiled magmatic rocks are listed in Table S2). syn-COLG, syn-collisional granites; ORG, ocean ridge granites; VAG, volcanic arc granite; WPG, within-plate granite.
Minerals 14 00811 g010

6.3.2. Permian Post-Collision

The quartz-monzonites and syenogranites exhibit I-type granite affinity with metaluminous trends. They are interpreted as derived from a mixed origin that involves both crustal and mantle-derived components. According to Figure 10, the Permian quartz-monzonites are plotted in the VAG field, while the syenogranites are plotted in the within-plate granite (WPG) and syn-collisional granite (syn-COLG) fields, indicating a transitional tectonic setting.
The compiled Permian granitoids in the Kumishi area are distributed in both the CTB and STB (Figure 1c). Most of these granitoids belong to high-K calc-alkaline to shoshonite series (Figure 4b) and exhibit metaluminous to peraluminous composition (Figure 4c). These granitoids, which are A-, S-, or I-type granites, also show negative HFSE anomalies and LILE enrichment with strongly depleted Nb-Ta-Ti (Figure 5a,b). However, from the Carboniferous to Early Permian, the magmatism displays a compositional variation trend from calc-alkaline to alkaline (Figure 4a,b), a feature often observed in a post-collisional setting during a gradual transition to post-orogenic intra-continental extension. According to Figure 10, the Early Permian granitic rocks are plotted in the volcanic arc granite (VAG), syn-collisional granite (syn-COLG), and within-plate granite (WPG) fields, indicating a transitional tectonic setting. In such a setting, the previously metasomatized mantle wedge, underplated mafic material, and uplifted asthenosphere are possible sources for magmas in a high regional heat flow [99,100]. The arc geochemical characteristics of the Early Permian granitic rocks may be inherited from a magma source metasomatized by subduction-derived fluids. Therefore, the Early Permian granitic rocks were formed in a post-collision tectonic setting. In summary, the tectonic setting of our granitoids, along with previously published data, indicates that the collisional regime in the Kumishi area had ceased by the Early Permian [14,29,101].
However, there are diverse types of evidence indicating the Early Permian arc-related setting for the Western Tianshan, including the following: (1) The existence of ~300 Ma glaucophane-bearing greenschist facies meta-volcanoclastic units in the Akeyazi HP/UHP complex suggests the subduction of the South Tianshan Ocean was probably still active during the Late Carboniferous [102]; (2) MORB- and OIB-type igneous rocks from Wuwamen ophiolite with ages of 334–309 Ma and enriched MORB-type gabbro of the Atbashi ophiolitic mélange in STB with age of 248 ± 5 Ma indicate that oceanic crust was still in existence [103,104]; (3) Upper Permian turbidites were unconformably overlain by the Middle to Upper Triassic red-beds in the Aiweigou area, Central Tianshan, suggesting that final tectonic accretion took place between the latest Permian and the Triassic [27]; (4) Late Silurian to Early Permian arc-type magmatic rocks are found on the southern margin of the Yili-CTB [15,22,29,36,39,92,93,94,96,105,106,107,108,109]; (5) The latest Permian–Triassic syn-collisional thrusts and Jurassic–Cretaceous post-collisional normal faults have been recognized in the northern Tarim Basin [110]; (6) Middle Devonian to Middle Triassic samples sourced from the South Tianshan accretionary complex or from isolated seamounts or oceanic plateaus carry no input from the Tarim Craton, whereas an Upper Triassic sample demonstrates a mixed provenance from both the Tarim Craton and the Yili-CTB [111]. Therefore, the Western Tianshan could have been amalgamated later than the eastern part of the Chinese Tianshan [29].

6.4. Tectonic Implications

The Kumishi area is located in the southern limb of the Kazakhstan orocline and near the eastern promontory of the Tarim Craton. The Kazakhstan orocline in the western CAOB was first formed as a nearly straight accretionary orogen in the Early–Middle Devonian and later buckled by compressing due to the rotation of the Siberian Craton [112,113,114] during the assembly of the Siberian and Tarim Cratons [115]. Along the huge length of the STB, the initial collisional times between the Tarim Craton and the northern accretionary systems could have been different and diachronous, but generally became younger westwards for the clockwise rotation of Tarim Craton during amalgamation [43].
The new zircon U-Pb ages of granitoids in the Kumishi area allow them to be correlated with the Paleozoic evolution of the Tianshan Orogenic Belt. Our present geochemical studies on the biotite monzonite show a mixed magma source derived from the crust and mantle-derived materials which may be related to the subduction of the South Tianshan oceanic crust. The latest arc magmatism is represented by the ca. 313 Ma biotite monzonites in the study area, suggesting that the South Tianshan Oceanic lithosphere was still subducting northward at this time (Figure 11a). There is a magmatic lull at 310–295 Ma in the Kumishi area. This is distinctly different from widely distributed Carboniferous arc-related volcanic rocks or Early Permian post-collisional granitic intrusions [14,29,100,101,116,117]. In addition, the conglomerates and limestones of the lowermost Lower Carboniferous Maanqiao Formation represent the deposits in an intermontane basin after collision [29]. Therefore, we propose that the collisional stage occurred mainly during the magmatic lull.
According to our geochemical study of the quartz-monzonites and syenogranites in the Kumishi area, which show I-type granite geochemical affinity and were formed in a transitional tectonic setting, this suggests that these granitic intrusions were formed in a post-collisional tectonic setting. The formation of these granitoids, together with regional Early Permian magmatism, requires a significant amount of heat energy, which induces extensive partial melting of lower crustal materials. This heat is commonly thought to be provided by the underplating of mantle-derived mafic magmas at lower crustal levels or the upwelling of the asthenosphere in an extension setting [118]. Our and complied geochemical and Hf isotope data clearly show a remarkable increase in εHf(t) values and K2O content from Carboniferous to Early Permian magmatic rocks (Figure 4b and Figure 7a), providing evidence of involvement of mantle-derived magmas under an extensional regime. Lithospheric extension likely induced upwelling of the asthenosphere.
A geodynamic model of slab breakoff has been proposed for the Early Permian extension in the research area, explaining the zonal distribution of magmatic activity in a roughly E–W direction (Figure 1c and Figure 11b)) [14,119,120,121]. Slab breakoff can cause continued crustal extension, large-scale upwelling of the asthenosphere, partial melting of crustal materials, or materials that are a mixture of lower crustal materials and mantle-derived magmas. This process resulted in the formation of the Early Permian I-type granitoids, as well as A-, S-type granitoids [14,29,101].

7. Conclusions

  • Zircon U-Pb dating indicates that the emplacement of biotite monzonite in the Kumishi area occurred during 312.7 ± 2.9 Ma, while the quartz-monzonites and syenogranites were emplaced during 284.5 ± 2.4 Ma and 283.4 ± 3.9 Ma, respectively;
  • The Late Carboniferous biotite monzonites were derived from a mixed magma source of the lower crust and the input of components derived from the mantle wedge above the subduction zone of the South Tianshan oceanic crust during the Carboniferous;
  • The Early Permian syenogranites and quartz-monzonites exhibit geochemical affinity with I-type granite and originated from partial melting of a mixture of lower crustal metabasaltic materials and minor mantle-derived magmas. The formation of these granitic rocks was triggered by an upwelling asthenosphere in a post-collisional extensional geodynamic setting;
  • These granitoids, along with the analysis of other magmatism in the study area, suggest that the Kumishi area experienced an evolution from subduction to post-collision from the Late Carboniferous to the Early Permian, which constrains the local closure of the PAO.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min14080811/s1, Table S1: Compilations of the Carboniferous–Permian plutons in the Kumishi area.xlsx; Table S2: Whole-rock Major and trace element composition of the studied plutons in the Kumishi area; Table S3. Compilations of the Zircon Lu-Hf isotopic compositions of the granitoids from the compiled Carboniferous–Permian plutons in the Kumishi area.

Author Contributions

Investigation, W.K., K.W., K.C., X.Z. and Y.G.; Software, W.K.; Supervision, K.W.; Writing—original draft, W.K.; Writing—review and editing, W.K. All authors have read and agreed to the published version of the manuscript.

Funding

This study was jointly supported by the Key R & D Program of Shaanxi Province (No. 2024GH-ZDXM-26), Free Exploration Youth Scientific Research Project in Shanxi Province (202203021212488), and Key R & D Program of Xinjiang Province (No. 2022A03010-2).

Data Availability Statement

All data generated or analyses during this study are included in this published article and its Supplementary Information Files.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Jahn, B.; Wu, F.; Chen, B. Massive Granitoid Generation in Central Asia: Nd Isotope Evidence and Implication for Continental Growth in the Phanerozoic. Epis. J. Int. Geosci. 2000, 23, 82–92. [Google Scholar] [CrossRef] [PubMed]
  2. Jahn, B. The Central Asian Orogenic Belt and Growth of the Continental Crust in the Phanerozoic. Geol. Soc. Lond. Spec. Publ. 2004, 226, 73–100. [Google Scholar] [CrossRef]
  3. Kröner, A.; Windley, B.; Badarch, G.; Tomurtogoo, O.; Hegner, E.; Jahn, B.; Gruschka, S.; Khain, E.; Demoux, A.; Wingate, M.; et al. Accretionary Growth and Crustformation in the Central Asian Orogenic Belt and Comparison with the Arabian-Nubian Shield. Mem. Geol. Soc. Am. 2007, 200, 181–209. [Google Scholar]
  4. Kröner, A.; Alexeiev, D.V.; Rojas-Agramonte, Y.; Hegner, E.; Wong, J.; Xia, X.; Belousova, E.; Mikolaichuk, A.V.; Seltmann, R.; Liu, D. Mesoproterozoic (Grenville-Age) Terranes in the Kyrgyz North Tianshan: Zircon Ages and Nd–Hf Isotopic Constraints on the Origin and Evolution of Basement Blocks in the Southern Central Asian Orogen. Gondwana Res. 2013, 23, 272–295. [Google Scholar] [CrossRef]
  5. Windley, B.F.; Alexeiev, D.; Xiao, W.; Kröner, A.; Badarch, G. Tectonic Models for Accretion of the Central Asian Orogenic Belt. J. Geol. Soc. 2007, 164, 31–47. [Google Scholar] [CrossRef]
  6. Xiao, W.J.; Windley, B.F.; Yuan, C.; Sun, M.; Han, C.M.; Lin, S.F.; Chen, H.L.; Yan, Q.R.; Liu, D.Y.; Qin, K.Z. Paleozoic Multiple Subduction-Accretion Processes of the Southern Altaids. Am. J. Sci. 2009, 309, 221–270. [Google Scholar] [CrossRef]
  7. Xiao, W.J.; Windley, B.F.; Huang, B.C.; Han, C.M.; Yuan, C.; Chen, H.L.; Sun, M.; Sun, S.; Li, J.L. End-Permian to Mid-Triassic Termination of the Accretionary Processes of the Southern Altaids: Implications for the Geodynamic Evolution, Phanerozoic Continental Growth, and Metallogeny of Central Asia. Int. J. Earth Sci. 2009, 98, 1189–1217. [Google Scholar] [CrossRef]
  8. Zonenshain, L.P.; Kuzmin, M.I.; Natapov, L.M. Geology of the USSR: A Plate-Tectonic Synthesis. Am. Geophys. Union Geodyn. Ser. 1990, 21, 120. [Google Scholar]
  9. Weng, K.; Dong, Y.; Ma, Z.; Cao, K.; Gao, Y. Petrogenesis of the Bastielieke W-Mineralized Granitic Pluton in the Altai Orogen, NW China. J. Asian Earth Sci. 2024, 268, 106175. [Google Scholar] [CrossRef]
  10. Weng, K.; Kang, W.; Zhao, X.; Ma, Z.; Cao, J.; Sui, Q. Petrogenesis, Tectonic Setting and Geodynamic Implications of Keziergayin Granites in the Kelan Basin (Chinese Altai): Constraints from Geochemistry, Zircon U-Pb Geochronology and Nd–Hf–Pb–O Isotopes. Front. Earth Sci. 2023, 11, 1203157. [Google Scholar] [CrossRef]
  11. Klemd, R.; Gao, J.; Li, J.; Meyer, M. Metamorphic Evolution of (Ultra)-High-Pressure Subduction-Related Transient Crust in the South Tianshan Orogen (Central Asian Orogenic Belt): Geodynamic Implications. Gondwana Res. 2015, 28, 1–25. [Google Scholar] [CrossRef]
  12. Scheltens, M.; Zhang, L.; Xiao, W.; Zhang, J. Northward Subduction-Related Orogenesis of the Southern Altaids: Constraints from Structural and Metamorphic Analysis of the HP/UHP Accretionary Complex in Chinese Southwestern Tianshan, NW China. Geosci. Front. 2015, 6, 191–209. [Google Scholar] [CrossRef]
  13. Şengör, A.M.C.; Natal’In, B.A.; Burtman, V.S. Evolution of the Altaid Tectonic Collage and Palaeozoic Crustal Growth in Eurasia. Nature 1993, 364, 299–307. [Google Scholar] [CrossRef]
  14. Ma, X.; Shu, L.; Meert, J.G. Early Permian Slab Breakoff in the Chinese Tianshan Belt Inferred from the Post-Collisional Granitoids. Gondwana Res. 2015, 27, 228–243. [Google Scholar] [CrossRef]
  15. Allan, M.B.; Windley, B.F.; Zang, C. Paleozoic Collisional Tectonics and Magmatism of the Chinese Tien Shan, Central Asia. Tectonophysics 1992, 220, 89–115. [Google Scholar] [CrossRef]
  16. Ao, S.J.; Xiao, W.J.; Han, C.M.; Mao, Q.G.; Zhang, J.E. Geochronology and Geochemistry of Early Permian Mafic–Ultramafic Complexes in the Beishan Area, Xinjiang, NW China: Implications for Late Paleozoic Tectonic Evolution of the Southern Altaids. Gondwana Res. 2010, 18, 466–478. [Google Scholar] [CrossRef]
  17. Coleman, R.G. Continental Growth of Northwest China. Tectonics 1989, 8, 621–635. [Google Scholar] [CrossRef]
  18. Dong, Y.; Wang, R.; Zhou, D. Geochemistry and Genesis of Meta-Mafic-Ultramafic Rocks from Yushugou Region, North Margin of the South Tianshan Tectonic Belt, Western China. Geochimica 2001, 30, 559–568. [Google Scholar]
  19. Dong, Y.P.; Zhou, D.W.; Zhang, G.W.; Zhang, C.L.; Li, X.M. Tectonic Setting of the Wuwamen Ophiolite at the Southern Margin of Middle Tianshan Belt. Acta Petrol. Sin. 2005, 21, 37–44. [Google Scholar]
  20. Dong, Y.P.; Zhou, D.W.; Zhang, G.W.; Zhao, X.; Luo, J.H.; Xu, J.G. Geology and Geochemistry of the Gangou Ophiolitic Melange at the Northern Margin of the Middle Tianshan Belt. Acta Petrol. Sin. 2006, 22, 49–56. [Google Scholar]
  21. Dong, Y.; Zhang, G.; Zhou, D.; Luo, J.; Zhang, C.; Xia, L.; Xu, X.; Li, X. Geology and Geochemistry of the Bingdaban Ophiolitic Mélange in the Boundary Fault Zone on the Northern Central Tianshan Belt, and Its Tectonic Implications. Sci. China Ser. D Earth Sci. 2007, 50, 17–24. [Google Scholar] [CrossRef]
  22. Gao, J.; Li, M.; Xiao, X.; Tang, Y.; He, G. Paleozoic Tectonic Evolution of the Tianshan Orogen, Northwestern China. Tectonophysics 1998, 287, 213–231. [Google Scholar] [CrossRef]
  23. Qian, Q.; Gao, J.; Klemd, R.; He, G.; Song, B.; Liu, D.; Xu, R. Early Paleozoic Tectonic Evolution of the Chinese South Tianshan Orogen: Constraints from SHRIMP Zircon U–Pb Geochronology and Geochemistry of Basaltic and Dioritic Rocks from Xiate, NW China. Int. J. Earth Sci. 2009, 98, 551–569. [Google Scholar] [CrossRef]
  24. Ren, R.; Han, B.-F.; Ji, J.-Q.; Zhang, L.; Xu, Z.; Su, L. U–Pb Age of Detrital Zircons from the Tekes River, Xinjiang, China, and Implications for Tectonomagmatic Evolution of the South Tian Shan Orogen. Gondwana Res. 2011, 19, 460–470. [Google Scholar] [CrossRef]
  25. Windley, B.F.; Allen, M.B.; Zhang, C.; Zhao, Z.Y.; Wang, G.R. Paleozoic Accretion and Cenozoic Redeformation of the Chinese Tien Shan Range, Central Asia. Geology 1990, 18, 128–131. [Google Scholar] [CrossRef]
  26. Xiao, W.; Zhang, L.; Qin, K.; Sun, S.H.U.; Li, J. Paleozoic Accretionary and Collisional Tectonics of the Eastern Tianshan (China): Implications for the Continental Growth of Central Asia. Am. J. Sci. 2004, 304, 370–395. [Google Scholar] [CrossRef]
  27. Xiao, W.; Han, C.; Yuan, C.; Sun, M.; Lin, S.; Chen, H.; Li, Z.; Li, J.; Sun, S. Middle Cambrian to Permian Subduction-Related Accretionary Orogenesis of Northern Xinjiang, NW China: Implications for the Tectonic Evolution of Central Asia. J. Asian Earth Sci. 2008, 32, 102–117. [Google Scholar] [CrossRef]
  28. Zhang, J.; Xiao, W.; Han, C.; Ao, S.; Yuan, C.; Sun, M.; Geng, H.; Zhao, G.; Guo, Q.; Ma, C. Kinematics and Age Constraints of Deformation in a Late Carboniferous Accretionary Complex in Western Junggar, NW China. Gondwana Res. 2011, 19, 958–974. [Google Scholar] [CrossRef]
  29. Dong, Y.; Zhang, G.; Neubauer, F.; Liu, X.; Hauzenberger, C.; Zhou, D.; Li, W. Syn- and Post-Collisional Granitoids in the Central Tianshan Orogen: Geochemistry, Geochronology and Implications for Tectonic Evolution. Gondwana Res. 2011, 20, 568–581. [Google Scholar] [CrossRef]
  30. Charvet, J.; Shu, L.; Laurent-Charvet, S.; Wang, B.; Faure, M.; Cluzel, D.; Chen, Y.; De Jong, K. Palaeozoic Tectonic Evolution of the Tianshan Belt, NW China. Sci. China Earth Sci. 2011, 54, 166–184. [Google Scholar] [CrossRef]
  31. Wang, B.Y.; Lang, Z.J.; Li, X.D. Study on the Geological Sections across the Western Segment of Tianshan Mountains, China; Science Press: Beijing, China, 1994. [Google Scholar]
  32. Xia, L.Q.; Xu, X.Y.; Xia, Z.C.; Li, X.M.; Ma, Z.P.; Wang, L.S. Petrogenesis of Carboniferous Rift-Related Volcanic Rocks in the Tianshan, Northwestern China. Geol. Soc. Am. Bull. 2004, 116, 419–433. [Google Scholar] [CrossRef]
  33. Xiao, X.C.; Tang, Y.Q.; Feng, Y.M. Tectonic Evolutionofthe Northern XinjiangandIts Adjacent Regions; GeologicalPublishing House: Beijing, China, 1992. [Google Scholar]
  34. Wang, B.; Shu, L.; Faure, M.; Jahn, B.; Cluzel, D.; Charvet, J.; Chung, S.; Meffre, S. Paleozoic Tectonics of the Southern Chinese Tianshan: Insights from Structural, Chronological and Geochemical Studies of the Heiyingshan Ophiolitic Mélange (NW China). Tectonophysics 2011, 497, 85–104. [Google Scholar] [CrossRef]
  35. Biske, Y.S.; Seltmann, R. Paleozoic Tian-Shan as a Transitional Region between the Rheic and Urals-Turkestan Oceans. Gondwana Res. 2010, 17, 602–613. [Google Scholar] [CrossRef]
  36. Gao, J.; Long, L.; Klemd, R.; Qian, Q.; Liu, D.; Xiong, X.; Su, W.; Liu, W.; Wang, Y.; Yang, F. Tectonic Evolution of the South Tianshan Orogen and Adjacent Regions, NW China: Geochemical and Age Constraints of Granitoid Rocks. Int. J. Earth Sci. (Geol. Rundsch.) 2009, 98, 1221–1238. [Google Scholar] [CrossRef]
  37. Su, W.; Gao, J.; Klemd, R.; Li, J.-L.; Zhang, X.; Li, X.-H.; Chen, N.-S.; Zhang, L. U–Pb Zircon Geochronology of Tianshan Eclogites in NW China: Implication for the Collision between the Yili and Tarim Blocks of the Southwestern Altaids. Eur. J. Mineral. 2010, 22, 473–478. [Google Scholar] [CrossRef]
  38. Bazhenov, M.L.; Collins, A.Q.; Degtyarev, K.E.; Levashova, N.M.; Mikolaichuk, A.V.; Pavlov, V.E.; Van der Voo, R. Paleozoic Northward Drift of the North Tien Shan (Central Asia) as Revealed by Ordovician and Carboniferous Paleomagnetism. Tectonophysics 2003, 366, 113–141. [Google Scholar] [CrossRef]
  39. Chen, C.; Lu, H.; Jia, D.; Cai, D.; Wu, S. Closing History of the Southern Tianshan Oceanic Basin, Western China: An Oblique Collisional Orogeny. Tectonophysics 1999, 302, 23–40. [Google Scholar] [CrossRef]
  40. Klemd, R.; Bröcker, M.; Hacker, B.R.; Gao, J.; Gans, P.; Wemmer, K. New Age Constraints on the Metamorphic Evolution of the High-Pressure/Low-Temperature Belt in the Western Tianshan Mountains, NW China. J. Geol. 2005, 113, 157–168. [Google Scholar] [CrossRef]
  41. Konopelko, D.; Biske, G.; Seltmann, R.; Eklund, O.; Belyatsky, B. Hercynian Post-Collisional A-Type Granites of the Kokshaal Range, Southern Tien Shan, Kyrgyzstan. Lithos 2007, 97, 140–160. [Google Scholar] [CrossRef]
  42. Seltmann, R.; Konopelko, D.; Biske, G.; Divaev, F.; Sergeev, S. Hercynian Post-Collisional Magmatism in the Context of Paleozoic Magmatic Evolution of the Tien Shan Orogenic Belt. J. Asian Earth Sci. 2011, 42, 821–838. [Google Scholar] [CrossRef]
  43. Xiao, W.; Windley, B.F.; Allen, M.B.; Han, C. Paleozoic Multiple Accretionary and Collisional Tectonics of the Chinese Tianshan Orogenic Collage. Gondwana Res. 2013, 23, 1316–1341. [Google Scholar] [CrossRef]
  44. Zhang, L.; Ai, Y.; Li, X.; Rubatto, D.; Song, B.; Williams, S.; Song, S.; Ellis, D.; Liou, J.G. Triassic Collision of Western Tianshan Orogenic Belt, China: Evidence from SHRIMP U–Pb Dating of Zircon from HP/UHP Eclogitic Rocks. Lithos 2007, 96, 266–280. [Google Scholar] [CrossRef]
  45. Tang, G.; Chung, S.; Wang, Q.; Wyman, D.A.; Dan, W.; Chen, H.; Zhao, Z. Petrogenesis of a Late Carboniferous Mafic Dike–Granitoid Association in the Western Tianshan: Response to the Geodynamics of Oceanic Subduction. Lithos 2014, 202–203, 85–99. [Google Scholar] [CrossRef]
  46. Wang, B.; Cluzel, D.; Jahn, B.; Shu, L.; Chen, Y.; Zhai, Y.; Branquet, Y.; Barbanson, L.; Sizaret, S. Late Paleozoic Pre-and Syn-Kinematic Plutons of the Kangguer–Huangshan Shear Zone: Inference on the Tectonic Evolution of the Eastern Chinese North Tianshan. Am. J. Sci. 2014, 314, 43–79. [Google Scholar] [CrossRef] [PubMed]
  47. Yuan, C.; Sun, M.; Wilde, S.; Xiao, W.; Xu, Y.; Long, X.; Zhao, G. Post-Collisional Plutons in the Balikun Area, East Chinese Tianshan: Evolving Magmatism in Response to Extension and Slab Break-Off. Lithos 2010, 119, 269–288. [Google Scholar] [CrossRef]
  48. Charvet, J.; Shu, L.; Laurent-Charvet, S. Paleozoic Structural and Geodynamic Evolution of Eastern Tianshan (NW China): Welding of the Tarim and Junggar Plates. Episodes 2007, 30, 162. [Google Scholar]
  49. Feng, Y.M. Genetic Environments and Original Types of Ophiolites in West Junggar. Bulletion Xi’an Inst. Geol. Miner. Resour. Chin. Acad. Geol. Sci. 1986, 13, 37–45. [Google Scholar]
  50. Zhu, B.Q.; Wang, L.S.; Wang, L.X. Paleozoic era ophiolite of southwest part in western Junggar, Xinjiang, China. Chin. Acad. Geol. Sci. Bull. Xi’an Inst. Geol. Miner. Resour. 1987, 17, 3–64. [Google Scholar]
  51. Li, W.Q.; Xia, B.; Wu, G.G.; Wang, H.; Wang, R. Kangguertage Ophiolite and Tectornic Significance, Shanshan, Xinjiang China. Acta Petrol. Sin. 2005, 21, 1617–1632. [Google Scholar]
  52. Li, W.; Ma, H.; Wang, R.; Wang, H.; Xia, B. SHRIMP Dating and Nd-Sr Isotopic Tracing of Kangguertage Ophiolite in Eastern Tianshan, Xinjiang. Acta Petrol. Sin. 2008, 24, 773–780. [Google Scholar]
  53. Che, Z.C.; Liu, H.F.; Liu, L. Formation and Evolution of the Middle Tianshan Orogenic Belt; Geological Publish House: Beijing, China, 1994. [Google Scholar]
  54. Shu, L.; Yu, J.; Charvet, J.; Laurent-Charvet, S.; Sang, H.; Zhang, R. Geological, Geochronological and Geochemical Features of Granulites in the Eastern Tianshan, NW China. J. Asian Earth Sci. 2004, 24, 25–41. [Google Scholar] [CrossRef]
  55. Li, Y.G.; Wang, S.S.; Liu, M.W.; Meng, E.; Wei, X.Y.; Zhao, H.B.; Jin, M.Q. U-Pb Dating Study of Baddeleyite by LA-ICP-MS: Technique and Application. Acta Geol. Sin. 2015, 89, 2400–2418. [Google Scholar]
  56. Griffin, W.L. GLITTER: Data Reduction Software for Laser Ablation ICP-MS. Laser Ablation ICP-MS Earth Sci. Curr. Pract. Outst. Issues 2008, 40, 308–311. [Google Scholar]
  57. Ludwig, K.R. Isoplot 3.00: A Geochronological Toolkit for Microsoft Excel. Berkeley Geochronol. Cent. Spec. Publ. 2003, 4, 70. [Google Scholar]
  58. Meng, E.; Liu, F.; Liu, P.; Liu, C.; Yang, H.; Wang, F.; Shi, J.; Cai, J. Petrogenesis and Tectonic Significance of Paleoproterozoic Meta-Mafic Rocks from Central Liaodong Peninsula, Northeast China: Evidence from Zircon U–Pb Dating and in Situ Lu–Hf Isotopes, and Whole-Rock Geochemistry. Precambrian Res. 2014, 247, 92–109. [Google Scholar] [CrossRef]
  59. Hou, K.J. Laser Ablation-MC-ICP-MS Technique for Hf Isotope Microanalysis of Zircon and Its Geological Applications. Acta Petrol. Sin. 2007, 23, 2595–2604. [Google Scholar]
  60. Ma, Q.; Zheng, J.; Griffin, W.L.; Zhang, M.; Tang, H.; Su, Y.; Ping, X. Triassic “Adakitic” Rocks in an Extensional Setting (North China): Melts from the Cratonic Lower Crust. Lithos 2012, 149, 159–173. [Google Scholar] [CrossRef]
  61. Gao, S.; Rudnick, R.L.; Xu, W.; Yuan, H.; Liu, Y.; Walker, R.J.; Puchtel, I.S.; Liu, X.; Huang, H.; Wang, X.-R. Recycling Deep Cratonic Lithosphere and Generation of Intraplate Magmatism in the North China Craton. Earth Planet. Sci. Lett. 2008, 270, 41–53. [Google Scholar] [CrossRef]
  62. Sun, S.S.; McDonough, W.F. Chemical and Isotopic Systematics of Oceanic Basalts: Implications for Mantle Composition and Processes. Geol. Soc. Lond. Spec. Publ. 1989, 42, 313–345. [Google Scholar] [CrossRef]
  63. Middlemost, E.A. Naming Materials in the Magma/Igneous Rock System. Earth-Sci. Rev. 1994, 37, 215–224. [Google Scholar] [CrossRef]
  64. Irvine, T.N.; Baragar, W.R.A. A Guide to the Chemical Classification of the Common Volcanic Rocks. Can. J. Earth Sci. 1971, 8, 523–548. [Google Scholar] [CrossRef]
  65. Peccerillo, A.; Taylor, S.R. Geochemistry of Eocene Calc-Alkaline Volcanic Rocks from the Kastamonu Area, Northern Turkey. Contrib. Mineral. Petrol. 1976, 58, 63–81. [Google Scholar] [CrossRef]
  66. Calanchi, N.; Peccerillo, A.; Tranne, C.A.; Lucchini, F.; Rossi, P.L.; Kempton, P.; Barbieri, M.; Wu, T.W. Petrology and Geochemistry of Volcanic Rocks from the Island of Panarea: Implications for Mantle Evolution beneath the Aeolian Island Arc (Southern Tyrrhenian Sea). J. Volcanol. Geotherm. Res. 2002, 115, 367–395. [Google Scholar] [CrossRef]
  67. Maniar, P.D.; Piccoli, P.M. Tectonic Discrimination of Granitoids. Geol. Soc. Am. Bull. 1989, 101, 635–643. [Google Scholar] [CrossRef]
  68. Taylor, S.R.; McLennan, S.M. The Chemical Composition of the Archaean Crust. Geol. Soc. Lond. Spec. Publ. 1986, 24, 173–178. [Google Scholar] [CrossRef]
  69. Taylor, S.R.; McLennan, S.M. The Geochemical Evolution of the Continental Crust. Rev. Geophys. 1995, 33, 241–265. [Google Scholar] [CrossRef]
  70. McCulloch, M.T.; Gamble, J.A. Geochemical and Geodynamical Constraints on Subduction Zone Magmatism. Earth Planet. Sci. Lett. 1991, 102, 358–374. [Google Scholar] [CrossRef]
  71. Pearce, J.A. Role of the Sub-Continental Lithosphere in Magma Genesis at Active Continental Margins; Hawkesworth, C.J., Norry, M.J., Eds.; Shiva Publications: Nantwich, UK, 1983; pp. 230–249. ISBN 978-0-906812-34-1. [Google Scholar]
  72. Hofmann, A.W. Chemical Differentiation of the Earth: The Relationship between Mantle, Continental Crust, and Oceanic Crust. Earth Planet. Sci. Lett. 1988, 90, 297–314. [Google Scholar] [CrossRef]
  73. Eby, G.N. Chemical Subdivision of the A-Type Granitoids:Petrogenetic and Tectonic Implications. Geology 1992, 20, 641–644. [Google Scholar] [CrossRef]
  74. Rapp, R.P.; Watson, E.B. Dehydration Melting of Metabasalt at 8–32 Kbar: Implications for Continental Growth and Crust-Mantle Recycling. J. Petrol. 1995, 36, 891–931. [Google Scholar] [CrossRef]
  75. Smithies, R.H.; Champion, D.C. The Archaean High-Mg Diorite Suite: Links to Tonalite–Trondhjemite–Granodiorite Magmatism and Implications for Early Archaean Crustal Growth. J. Petrol. 2000, 41, 1653–1671. [Google Scholar] [CrossRef]
  76. Tang, G.-J.; Wang, Q.; Wyman, D.A.; Li, Z.-X.; Xu, Y.-G.; Zhao, Z.-H. Metasomatized Lithosphere–Asthenosphere Interaction during Slab Roll-Back: Evidence from Late Carboniferous Gabbros in the Luotuogou Area, Central Tianshan. Lithos 2012, 155, 67–80. [Google Scholar] [CrossRef]
  77. Douce, A.E.P. Effects of Pressure and H2O Content on the Compositions of Primary Crustal Melts. Earth Environ. Sci. Trans. R. Soc. Edinb. 1996, 87, 11–21. [Google Scholar] [CrossRef]
  78. Yuan, C.; Sun, M.; Xiao, W.; Li, X.; Chen, H.; Lin, S.; Xia, X.; Long, X. Accretionary Orogenesis of the Chinese Altai: Insights from Paleozoic Granitoids. Chem. Geol. 2007, 242, 22–39. [Google Scholar] [CrossRef]
  79. Whalen, J.B.; Currie, K.L.; Chappell, B.W. A-Type Granites: Geochemical Characteristics, Discrimination and Petrogenesis. Contrib. Mineral. Petrol. 1987, 95, 407–419. [Google Scholar] [CrossRef]
  80. Halliday, A.N.; Davidson, J.P.; Hildreth, W.; Holden, P. Modelling the Petrogenesis of High Rb/Sr Silicic Magmas. Chem. Geol. 1991, 92, 107–114. [Google Scholar] [CrossRef]
  81. Bau, M. Controls on the Fractionation of Isovalent Trace Elements in Magmatic and Aqueous Systems: Evidence from Y/Ho, Zr/Hf, and Lanthanide Tetrad Effect. Contrib. Mineral. Petrol. 1996, 123, 323–333. [Google Scholar] [CrossRef]
  82. Pérez-Soba, C.; Villaseca, C. Petrogenesis of Highly Fractionated I-Type Peraluminous Granites: La Pedriza Pluton (Spanish Central System). Geol. Acta: Int. Earth Sci. J. 2010, 8, 131–149. [Google Scholar]
  83. Ballouard, C.; Poujol, M.; Boulvais, P.; Branquet, Y.; Tartèse, R.; Vigneresse, J.-L. Nb-Ta Fractionation in Peraluminous Granites: A Marker of the Magmatic-Hydrothermal Transition. Geology 2016, 44, 231–234. [Google Scholar] [CrossRef]
  84. Chappell, B.W.; White, A.J.R. I-and S-Type Granites in the Lachlan Fold Belt. Earth Environ. Sci. Trans. R. Soc. Edinb. 1992, 83, 1–26. [Google Scholar]
  85. Wu, F.; Jahn, B.; Wilde, S.A.; Lo, C.-H.; Yui, T.-F.; Lin, Q.; Ge, W.; Sun, D. Highly Fractionated I-Type Granites in NE China (I): Geochronology and Petrogenesis. Lithos 2003, 66, 241–273. [Google Scholar] [CrossRef]
  86. Rudnick, R.L.; Gao, S. 4.1—Composition of the Continental Crust. In Treatise on Geochemistry, 2nd ed.; Holland, H.D., Turekian, K.K., Eds.; Elsevier: Oxford, UK, 2003; pp. 1–51. ISBN 978-0-08-098300-4. [Google Scholar]
  87. Green, T.H. Significance of Nb/Ta as an Indicator of Geochemical Processes in the Crust-Mantle System. Chem. Geol. 1995, 120, 347–359. [Google Scholar] [CrossRef]
  88. Han, Y.; Zhao, G. Final Amalgamation of the Tianshan and Junggar Orogenic Collage in the Southwestern Central Asian Orogenic Belt: Constraints on the Closure of the Paleo-Asian Ocean. Earth-Sci. Rev. 2018, 186, 129–152. [Google Scholar] [CrossRef]
  89. Han, Y.; Zhao, G.; Cawood, P.A.; Sun, M.; Liu, Q.; Yao, J. Plume-Modified Collision Orogeny: The Tarim–Western Tianshan Example in Central Asia. Geology 2019, 47, 1001–1005. [Google Scholar] [CrossRef]
  90. He, P.-L.; Huang, X.-L.; Xu, Y.-G.; Li, H.-Y.; Wang, X.; Li, W.-X. Plume-orogenic Lithosphere Interaction Recorded in the Haladala Layered Intrusion in the Southwest Tianshan Orogen, NW China. J. Geophys. Res. Solid Earth 2016, 121, 1525–1545. [Google Scholar] [CrossRef]
  91. Zhang, C.-L.; Zou, H.-B. Permian A-Type Granites in Tarim and Western Part of Central Asian Orogenic Belt (CAOB): Genetically Related to a Common Permian Mantle Plume? Lithos 2013, 172, 47–60. [Google Scholar] [CrossRef]
  92. Tao, Z.; Yin, J.; Sun, M.; Wang, T.; Yuan, C.; Chen, W.; Huang, H.; Seltmann, R.; Thomson, S.N.; Chen, Y. Spatial and Temporal Variations of Geochemical and Isotopic Compositions of Paleozoic Magmatic Rocks in the Western Tianshan, NW China: A Magmatic Response of the Advancing and Retreating Subduction. J. Asian Earth Sci. 2022, 232, 105112. [Google Scholar] [CrossRef]
  93. Tao, Z.; Yin, J.; Xiao, W.; Seltmann, R.; Chen, W.; Sun, M.; Wang, T.; Yuan, C.; Thomson, S.N.; Chen, Y. Contrasting Styles of Peraluminous S-Type and I-Type Granitic Magmatism: Identification and Implications for the Accretionary History of the Chinese South Tianshan. Am. J. Sci. 2022, 322, 280–312. [Google Scholar] [CrossRef]
  94. Tao, Z.; Yin, J.; Chen, W.; Li, D.; Cai, K.; Xu, Z.; Du, Q. New Zircon U-Pb Ages of Mylonitic Granite in the Baluntai Area of the Central Tianshan Block and Their Geological Implications. Acta Geol. Sin. 2019, 93, 1149. [Google Scholar] [CrossRef]
  95. Han, B.; He, G.; Wang, X.; Guo, Z. Late Carboniferous Collision between the Tarim and Kazakhstan–Yili Terranes in the Western Segment of the South Tian Shan Orogen, Central Asia, and Implications for the Northern Xinjiang, Western China. Earth-Sci. Rev. 2011, 109, 74–93. [Google Scholar] [CrossRef]
  96. Long, L.; Gao, J.; Klemd, R.; Beier, C.; Qian, Q.; Zhang, X.; Wang, J.; Jiang, T. Geochemical and Geochronological Studies of Granitoid Rocks from the Western Tianshan Orogen: Implications for Continental Growth in the Southwestern Central Asian Orogenic Belt. Lithos 2011, 126, 321–340. [Google Scholar] [CrossRef]
  97. Barbarin, B. A Review of the Relationships between Granitoid Types, Their Origins and Their Geodynamic Environments. Lithos 1999, 46, 605–626. [Google Scholar] [CrossRef]
  98. Pearce, J.A.; Harris, N.B.; Tindle, A.G. Trace Element Discrimination Diagrams for the Tectonic Interpretation of Granitic Rocks. J. Petrol. 1984, 25, 956–983. [Google Scholar] [CrossRef]
  99. Oyhantçabal, P.; Siegesmund, S.; Wemmer, K.; Frei, R.; Layer, P. Post-Collisional Transition from Calc-Alkaline to Alkaline Magmatism during Transcurrent Deformation in the Southernmost Dom Feliciano Belt (Braziliano–Pan-African, Uruguay). Lithos 2007, 98, 141–159. [Google Scholar] [CrossRef]
  100. Wang, B.; Cluzel, D.; Shu, L.; Faure, M.; Charvet, J.; Chen, Y.; Meffre, S.; De Jong, K. Evolution of Calc-Alkaline to Alkaline Magmatism through Carboniferous Convergence to Permian Transcurrent Tectonics, Western Chinese Tianshan. Int. J. Earth Sci. 2009, 98, 1275–1298. [Google Scholar] [CrossRef]
  101. Huang, G.; Wang, X.; Zhang, W.; Li, H.; Hu, J. Zircon LA-ICP-MS U-Pb Age and Geochemistry of Two-Mica Granite in Kumishen Area in Eastern Part of the Southern Tianshan Mountains. Xinjiang Geol. 2011, 29, 263–269. [Google Scholar]
  102. Tan, Z.; Agard, P.; Monie, P.; Gao, J.; John, T.; Bayet, L.; Jiang, T.; Wang, X.-S.; Hong, T.; Wan, B. Architecture and PT-Deformation-Time Evolution of the Chinese SW-Tianshan HP/UHP Complex: Implications for Subduction Dynamics. Earth-Sci. Rev. 2019, 197, 102894. [Google Scholar] [CrossRef]
  103. Sang, M.; Xiao, W.; Orozbaev, R.; Bakirov, A.; Sakiev, K.; Pak, N.; Ivleva, E.; Zhou, K.; Ao, S.; Qiao, Q. Structural Styles and Zircon Ages of the South Tianshan Accretionary Complex, Atbashi Ridge, Kyrgyzstan: Insights for the Anatomy of Ocean Plate Stratigraphy and Accretionary Processes. J. Asian Earth Sci. 2018, 153, 9–41. [Google Scholar] [CrossRef]
  104. Wang, B.; Zhai, Y.; Kapp, P.; de Jong, K.; Zhong, L.; Liu, H.; Ma, Y.; Gong, H.; Geng, H. Accretionary Tectonics of Back-Arc Oceanic Basins in the South Tianshan: Insights from Structural, Geochronological, and Geochemical Studies of the Wuwamen Ophiolite Mélange. Bulletin 2018, 130, 284–306. [Google Scholar] [CrossRef]
  105. Ma, Z.; Xia, L.; Xu, X.; Xia, Z.; Li, X.; Wang, L. Geochemical Characteristics and Petrogenesis of the Early Paleozoic Igneous Rocks from Bayinbuluke, Southern Tianshan. Acta Petrol. Sin. 2008, 24, 2289–2300. [Google Scholar]
  106. Yang, T.; Wang, X. Geochronology, Petrochemistry and Tectonic Implications of Early Devonian Plutons in Kumux Area, Xinjiang. Acta Petrol. Et Mineral. 2006, 25, 401–411. [Google Scholar]
  107. Yang, T.; Li, J.; Sun, G.; Wang, Y. Earlier Devonian Active Continental Arc in Central Tianshan: Evidence of Geochemical Analyses and Zircon SHRIMP Dating on Mylonitized Granitic Rock. Acta Petrol. Sin. 2006, 22, 41–48. [Google Scholar]
  108. Zhou, D.; Graham, S.A.; Chang, E.Z.; Wang, B.; Hacker, B.; Hendrix, M.S.; Davis, G.A. Paleozoic Tectonic Amalgamation of the Chinese Tian Shan: Evidence from a Transect along the Dushanzi-Kuqa Highway. In Paleozoic and Mesozoic Tectonic Evolution of Central and Eastern Asia: From Continental Assembly to Intracontinental Deformation; Geological Society of America: Washington, DC, USA, 2001; Volume 194. [Google Scholar]
  109. Zhu, Y.-F.; Zeng, Y.; Gu, L. Geochemistry of the Rare Metal-Bearing Pegmatite No. 3 Vein and Related Granites in the Keketuohai Region, Altay Mountains, Northwest China. J. Asian Earth Sci. 2006, 27, 61–77. [Google Scholar] [CrossRef]
  110. Wen, D.; He, Z. Late Carboniferous Crustal Evolution of the Chinese Central Tianshan Microcontinent: Insights from Zircon U–Pb and Hf Isotopes of Granites. Geol. J. 2019, 55, 1947–1963. [Google Scholar] [CrossRef]
  111. Abuduxun, N.; Xiao, W.; Windley, B.F.; Chen, Y.; Huang, P.; Sang, M.; Li, L.; Liu, X. Terminal Suturing Between the Tarim Craton and the Yili-Central Tianshan Arc: Insights From Mélange-Ocean Plate Stratigraphy, Detrital Zircon Ages, and Provenance of the South Tianshan Accretionary Complex. Tectonics 2021, 40, e2021TC006705. [Google Scholar] [CrossRef]
  112. Xiao, W.; Windley, B.F.; Sun, S.; Li, J.; Huang, B.; Han, C.; Yuan, C.; Sun, M.; Chen, H. A Tale of Amalgamation of Three Permo-Triassic Collage Systems in Central Asia: Oroclines, Sutures, and Terminal Accretion. Annu. Rev. Earth Planet. Sci. 2015, 43, 477–507. [Google Scholar] [CrossRef]
  113. Xiao, W.; Windley, B.F.; Han, C.; Liu, W.; Wan, B.; Zhang, J.; Ao, S.; Zhang, Z.; Song, D. Late Paleozoic to Early Triassic Multiple Roll-Back and Oroclinal Bending of the Mongolia Collage in Central Asia. Earth-Sci. Rev. 2018, 186, 94–128. [Google Scholar] [CrossRef]
  114. Abrajevitch, A.; Van der Voo, R.; Bazhenov, M.L.; Levashova, N.M.; McCausland, P.J.A. The Role of the Kazakhstan Orocline in the Late Paleozoic Amalgamation of Eurasia. Tectonophysics 2008, 455, 61–76. [Google Scholar] [CrossRef]
  115. Li, P.; Sun, M.; Rosenbaum, G.; Yuan, C.; Safonova, I.; Cai, K.; Jiang, Y.; Zhang, Y. Geometry, Kinematics and Tectonic Models of the Kazakhstan Orocline, Central Asian Orogenic Belt. J. Asian Earth Sci. 2018, 153, 42–56. [Google Scholar] [CrossRef]
  116. Ma, X.; Shu, L.; Meert, J.G.; Li, J. The Paleozoic Evolution of Central Tianshan: Geochemical and Geochronological Evidence. Gondwana Res. 2014, 25, 797–819. [Google Scholar] [CrossRef]
  117. Xu, X.; Ma, Z.; Xia, Z.; Xia, L.; Li, X.; Wang, L. TIMS U-Pb Isotopic Dating and Geochemical Characteristics of Paleozoic Granitic Rocks from the Middle-Western Section of Tianshan. Northwestern Geol. 2006, 39, 50–75. [Google Scholar]
  118. Collins, W.J.; Beams, S.D.; White, A.J.R.; Chappell, B.W. Nature and Origin of A-Type Granites with Particular Reference to Southeastern Australia. Contrib. Mineral. Petrol. 1982, 80, 189–200. [Google Scholar] [CrossRef]
  119. Du, L.; Long, X.; Yuan, C.; Zhang, Y.; Huang, Z.; Sun, M.; Xiao, W. Petrogenesis of Late Paleozoic Diorites and A-Type Granites in the Central Eastern Tianshan, NW China: Response to Post-Collisional Extension Triggered by Slab Breakoff. Lithos 2018, 318, 47–59. [Google Scholar] [CrossRef]
  120. Huw Davies, J.; von Blanckenburg, F. Slab Breakoff: A Model of Lithosphere Detachment and Its Test in the Magmatism and Deformation of Collisional Orogens. Earth Planet. Sci. Lett. 1995, 129, 85–102. [Google Scholar] [CrossRef]
  121. Coulon, C.; Megartsi, M.; Fourcade, S.; Maury, R.C.; Bellon, H.; Louni-Hacini, A.; Cotten, J.; Coutelle, A.; Hermitte, D. Post-Collisional Transition from Calc-Alkaline to Alkaline Volcanism during the Neogene in Oranie (Algeria): Magmatic Expression of a Slab Breakoff. Lithos 2002, 62, 87–110. [Google Scholar] [CrossRef]
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Figure 1. (a) Simplified tectonic map of the Central Asian Orogenic Belt (modified after Wang [34]). (b) Tectonic sketch map of the North Xinjiang (after Xiao [26]). (c) Geological map of the Kumishi area with the sampling locations and distribution of Carboniferous–Permian magmatic rocks, see Table S1 for details (modified after Dong [29]). AQK Fm.—Lower Permian Aqikebulake Formation, DKE Fm.—Middle Carboniferous Dikaner Formation, YMS Fm.—Lower Carboniferous Yamansu Formation, MAQ Fm.—Lowermost Carboniferous Maanqiao Formation, AEB Fm.—Lower Devonian Arbishimibulake Formation, MSG Fm.—Silurian Mishigou Formation, AHB Fm.—Silurian Ahabulake Formation, KKN Fm.—Ordovician Kekenaike Formation, BLT Gr.—Proterozoic Baluntai Group.
Figure 1. (a) Simplified tectonic map of the Central Asian Orogenic Belt (modified after Wang [34]). (b) Tectonic sketch map of the North Xinjiang (after Xiao [26]). (c) Geological map of the Kumishi area with the sampling locations and distribution of Carboniferous–Permian magmatic rocks, see Table S1 for details (modified after Dong [29]). AQK Fm.—Lower Permian Aqikebulake Formation, DKE Fm.—Middle Carboniferous Dikaner Formation, YMS Fm.—Lower Carboniferous Yamansu Formation, MAQ Fm.—Lowermost Carboniferous Maanqiao Formation, AEB Fm.—Lower Devonian Arbishimibulake Formation, MSG Fm.—Silurian Mishigou Formation, AHB Fm.—Silurian Ahabulake Formation, KKN Fm.—Ordovician Kekenaike Formation, BLT Gr.—Proterozoic Baluntai Group.
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Figure 2. (a–e) Field and microscopic photos of the monzonitic and granitic intrusions in the Kumishi area. (a,b) The biotite monzonite; (c,d) the quartz-monzonitic pluton; (e,f) the syenogranitic pluton. Mineral abbreviations: Qtz = quartz, Pl = plagioclase, Bt = biotite, Kfs = K-feldspar. Cross-polarized light.
Figure 2. (a–e) Field and microscopic photos of the monzonitic and granitic intrusions in the Kumishi area. (a,b) The biotite monzonite; (c,d) the quartz-monzonitic pluton; (e,f) the syenogranitic pluton. Mineral abbreviations: Qtz = quartz, Pl = plagioclase, Bt = biotite, Kfs = K-feldspar. Cross-polarized light.
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Figure 3. U-Pb concordia diagrams and CL images of zircon grains for the granitoids in the Kumishi area. (a)18ZB–44 for biotite monzonite; (b) 18ZB–35 for quartz-monzonite; (c) 18ZB–24 for syenogranite.
Figure 3. U-Pb concordia diagrams and CL images of zircon grains for the granitoids in the Kumishi area. (a)18ZB–44 for biotite monzonite; (b) 18ZB–35 for quartz-monzonite; (c) 18ZB–24 for syenogranite.
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Figure 6. Harker diagrams of selected elements vs. SiO2 for granitic rocks in the Kumishi area. (a) Al2O3, (b) CaO, (c) FeOt, (d) MgO, (e) MnO, (f) TiO2, (g) P2O5, (h) Rb, and (i) Sr.
Figure 6. Harker diagrams of selected elements vs. SiO2 for granitic rocks in the Kumishi area. (a) Al2O3, (b) CaO, (c) FeOt, (d) MgO, (e) MnO, (f) TiO2, (g) P2O5, (h) Rb, and (i) Sr.
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Figure 7. (a) Age versus εHf(t) diagram (data for compiled magmatic rocks are listed in Table S3), and (b) 206Pb/204Pb versus 207Pb/204Pb diagram.
Figure 7. (a) Age versus εHf(t) diagram (data for compiled magmatic rocks are listed in Table S3), and (b) 206Pb/204Pb versus 207Pb/204Pb diagram.
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Figure 8. Discrimination diagrams of A-type granites from I- and S-type granites (data for compiled magmatic rocks are listed in Table S2) [79]. FG, fractionated granites; OGT, unfractionated granites. (a–d) FeOT/MgO, Zr, Ce and Y vs. 10,000*Ga/Al; (e–f) FeOT/MgO and (Na2O+K2O)/CaO vs. Zr+Nb+Ce+Y.
Figure 8. Discrimination diagrams of A-type granites from I- and S-type granites (data for compiled magmatic rocks are listed in Table S2) [79]. FG, fractionated granites; OGT, unfractionated granites. (a–d) FeOT/MgO, Zr, Ce and Y vs. 10,000*Ga/Al; (e–f) FeOT/MgO and (Na2O+K2O)/CaO vs. Zr+Nb+Ce+Y.
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Figure 9. Trace element variation diagrams for the granitic rocks in the Kumishi area. (a,b) Variations of Th and Y vs. Rb, respectively, from Chappell and White [84], (c,d) variations of Sr vs. Ba and Rb, respectively, (e) variations of La vs. (La/Yb)N (modified after Wu [85]), and (f) variations of Th vs. V.
Figure 9. Trace element variation diagrams for the granitic rocks in the Kumishi area. (a,b) Variations of Th and Y vs. Rb, respectively, from Chappell and White [84], (c,d) variations of Sr vs. Ba and Rb, respectively, (e) variations of La vs. (La/Yb)N (modified after Wu [85]), and (f) variations of Th vs. V.
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Figure 11. Schematic tectonic evolution of subduction of the South Tianshan Ocean beneath the CTB.
Figure 11. Schematic tectonic evolution of subduction of the South Tianshan Ocean beneath the CTB.
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Table 1. Zircon U-Pb geochronological data for the studied plutons in the Kumishi area.
Table 1. Zircon U-Pb geochronological data for the studied plutons in the Kumishi area.
SampleTh (ppm)U (ppm)Th/URatiosAge (Ma)
207Pb/206Pb±1s207Pb/235U±1 s206Pb/238U±1 s207Pb/206Pb±1 s207Pb/235U±1 s206Pb/238U±1 s
Biotite monzonite
18ZB44011488520.170.055480.002100.380830.014230.049800.0007243182328103134
18ZB44021893530.540.053070.002870.364030.019370.049760.00084332118315143135
18ZB44051862700.690.053450.004810.368630.032480.050030.00118348191319243157
18ZB44101913620.530.052920.003840.364820.025940.050010.00100325156316193156
18ZB44111662380.700.055320.005090.378630.034110.049650.00118425193326253127
18ZB44124254970.860.054480.003050.372080.020460.049540.00085391121321153125
18ZB441329213980.210.053520.002080.370990.014220.050280.0007335185320113164
18ZB44142554210.610.053450.003430.368660.023200.050030.00092348138319173156
18ZB44151054820.220.053870.002550.366730.017080.049380.00077366103317133115
18ZB44163484240.820.052730.002510.360700.016890.049620.00078317104313133125
18ZB44172593690.700.052900.002550.360430.017140.049420.00078325106313133115
18ZB44183935220.750.054200.002390.367490.015980.049180.0007537996318123105
Syenogranite
18ZB24033829360.410.050800.001880.319410.011690.045560.000642328328192874
18ZB24041964700.420.053870.003620.347340.022840.046710.00090365144303172946
18ZB24051773400.520.052680.003130.326760.019060.044930.00079315130287152835
18ZB24062905320.550.050310.002360.319310.014730.045980.00071209105281112904
18ZB24073637980.450.056830.002050.358710.012800.045720.0006548479311102884
18ZB24082328100.290.051850.001970.313150.011750.043740.000622798527792764
18ZB24091533360.450.047090.004310.277800.024900.042730.0009753205249202706
18ZB241059710520.570.053930.001700.332710.010400.044680.000603686929282824
18ZB24111231610.760.048600.005620.288020.032620.042920.00118129251257262717
18ZB24122404810.500.053450.002440.335160.015070.045410.00070348100294112864
18ZB24133627570.480.050930.001900.313510.011540.044570.000622388427792814
18ZB24142294660.490.052150.002300.323850.014080.044970.0006829298285112844
Quartz-monzonite
18ZB35011913350.570.054460.003060.347310.019190.046290.00082390121303142925
18ZB35034669440.490.052250.001450.319970.008990.044450.000612966228272804
18ZB35043987060.560.051370.002030.321440.012630.045430.0006825788283102864
18ZB35063525620.630.053160.002340.331980.014450.045340.0007133697291112864
18ZB35073917030.560.051850.002090.327420.013090.045850.0006927990288102894
18ZB35081281380.930.057740.005480.359200.033340.045170.00113520196312252857
18ZB35097096261.130.055780.003310.353960.020620.046080.00085444127308152905
18ZB35102182970.730.055780.003340.343720.020230.044750.00082443128300152825
18ZB35115668230.690.053890.001960.332730.012020.044840.000663678029292834
18ZB35145687300.780.052820.002650.330610.016360.045470.00075321110290122875
18ZB35152695620.480.052390.002280.321190.013840.044540.0006930296283112814
18ZB35161901611.180.054070.005320.328130.031610.044090.00112374208288242787
18ZB351782.683.70.990.053570.005770.331100.034930.044910.00121353227290272837
18ZB35181631900.860.054930.003910.346530.024190.045840.00093410152302182896
18ZB35196929500.730.054070.002110.329880.012760.044330.0006637485290102804
Table 2. Zircon Lu-Hf isotopic data for the studied plutons in the Kumishi area.
Table 2. Zircon Lu-Hf isotopic data for the studied plutons in the Kumishi area.
SampleAge (Ma)176Hf/177Hf2σ176Lu/177Hf2σ176Yb/177Hf2σ176Hf/177HfiεHf(0)εHf(t)2σTDM (Ma)2σTDMC (Ma)2σfLu/Hf
Biotite monzonite
18ZB-44-13130.2827840.0000190.0016200.0000200.0751030.0007030.2827740.47.00.767555111886−0.95
18ZB-44-23130.2829020.0000230.0021330.0000180.0949690.0007160.2828904.611.00.851267749103−0.94
18ZB-44-33130.2827430.0000290.0011900.0000400.0505520.0018250.282736−1.05.61.0725821240130−0.96
18ZB-44-43130.2828360.0000220.0016650.0000430.0737250.0022700.2828272.38.80.86006495199−0.95
18ZB-44-53130.2828350.0000220.0015400.0000530.0702210.0022770.2828262.28.80.86016295397−0.95
18ZB-44-63130.2827280.0000240.0013350.0000390.0558140.0009390.282721-1.55.10.9749701290110−0.96
18ZB-44-73130.2829920.0000260.0025830.0001060.1229010.0057120.2829777.814.10.938578469119−0.92
18ZB-44-83130.2828840.0000220.0020450.0000180.0934060.0004360.2828723.910.40.85386380798−0.94
18ZB-44-93130.2827960.0000210.0011200.0000100.0450860.0006270.2827890.87.50.864961107097−0.97
18ZB-44-103130.2828960.0000220.0021250.0000130.0973770.0010400.2828834.410.80.85216476999−0.94
18ZB-44-113130.2827210.0000220.0009870.0000220.0437750.0011490.282715-1.84.90.875362130999−0.97
18ZB-44-123130.2827880.0000220.0014460.0000250.0650920.0015120.2827800.67.20.8666641101100−0.96
Syenogranite
18ZB-24-12830.2827860.0000210.0007760.0000130.0342670.0006820.2827820.56.60.765758113393−0.98
18ZB-24-1-12830.2828700.0000190.0011370.0000030.0562750.0002180.2828643.59.50.75445487185−0.97
18ZB-24-1-22830.2830000.0000310.0019560.0001120.0954530.0051040.2829898.113.91.136791468141−0.94
18ZB-24-1-32830.2828520.0000190.0010150.0000080.0497670.0005410.2828472.88.90.75675392585−0.97
18ZB-24-1-52830.2828120.0000190.0009540.0000160.0455050.0010070.2828071.47.40.762455105488−0.97
18ZB-24-1-62830.2828600.0000250.0011120.0000680.0547820.0037960.2828543.19.10.955870903111−0.97
18ZB-24-1-72830.2828990.0000290.0015510.0000930.0759890.0046010.2828914.510.41.050982785129−0.95
18ZB-24-1-82830.2828820.0000220.0013520.0000600.0646730.0031840.2828753.99.90.853064836101−0.96
18ZB-24-1-92830.2828190.0000230.0009390.0000330.0421160.0014780.2828151.77.70.8613661029106−0.97
18ZB-24-1-102830.2830250.0000220.0016880.0000270.0931600.0018070.2830169.014.90.832765381101−0.95
18ZB-24-1-112830.2828320.0000230.0009640.0000050.0465860.0002110.2828272.18.20.859666990105−0.97
18ZB-24-1-122830.2829910.0000310.0012820.0000810.0710970.0048480.2829847.713.71.137390485141−0.96
18ZB-24-22830.2828600.0000190.0011380.0000050.0570180.0005490.2828543.19.10.75595490485−0.97
18ZB-24-32830.2830200.0000260.0016590.0000320.0925250.0026690.2830118.814.70.933577398120−0.95
18ZB-24-42830.2828480.0000180.0009570.0000130.0474560.0005040.2828432.78.70.75725293882−0.97
18ZB-24-52830.2828310.0000190.0009650.0000050.0480670.0004070.2828262.18.10.75975499386−0.97
18ZB-24-62830.2829150.0000260.0012220.0000180.0616100.0010610.2829095.111.10.948174727117−0.96
18ZB-24-72830.2828410.0000400.0013130.0001660.0544370.0062260.2828342.48.41.4588115967181−0.96
18ZB-24-82830.2828760.0000180.0014370.0000200.0739040.0010780.2828683.79.60.75405385884−0.96
18ZB-24-92830.2828330.0000260.0009560.0000470.0410240.0014880.2828282.28.20.959473986116−0.97
18ZB-24-102830.2829660.0000330.0021570.0000770.1012890.0026760.2829546.912.71.241998581151−0.94
18ZB-24-112830.2829970.0000190.0009470.0000080.0480340.0005540.2829927.914.00.73615546088−0.97
Quartz-monzonite
18ZB-35-82850.2830410.0000220.0015660.0000110.0725770.0006320.2830329.515.50.83046332699−0.95
18ZB-35-102850.2830260.0000220.0016500.0000160.0747390.0003900.2830179.014.90.83266337599−0.95
18ZB-35-112850.2830270.0000230.0013040.0000160.0577100.0005950.2830209.015.00.832266368104−0.96
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Kang, W.; Weng, K.; Cao, K.; Zhao, X.; Gao, Y. Petrogenesis of Carboniferous-Permian Granitoids in the Kumishi Area of Tianshan, China: Insights into the Geodynamic Evolution Triggered by Subduction and Closure of the South Tianshan Ocean. Minerals 2024, 14, 811. https://doi.org/10.3390/min14080811

AMA Style

Kang W, Weng K, Cao K, Zhao X, Gao Y. Petrogenesis of Carboniferous-Permian Granitoids in the Kumishi Area of Tianshan, China: Insights into the Geodynamic Evolution Triggered by Subduction and Closure of the South Tianshan Ocean. Minerals. 2024; 14(8):811. https://doi.org/10.3390/min14080811

Chicago/Turabian Style

Kang, Wenbin, Kai Weng, Kai Cao, Xiaojian Zhao, and Yongwei Gao. 2024. "Petrogenesis of Carboniferous-Permian Granitoids in the Kumishi Area of Tianshan, China: Insights into the Geodynamic Evolution Triggered by Subduction and Closure of the South Tianshan Ocean" Minerals 14, no. 8: 811. https://doi.org/10.3390/min14080811

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