Zircon U-Pb Geochronology and Hf Isotopes of the Granitoids from Cahanwusu Cu Deposit in Awulale Mountain, Western Tianshan: Implication for Regional Mineralization

Abstract

Awulale Mountain is one of the most important Fe-Cu concentration areas situated in the eastern part of Western Tianshan. The Cu deposits in the belt are genetically associated with the Permian intermediate and felsic intrusions. However, the precise age and magma source of the causative intrusions are currently not confirmed, constraining our understanding of regional mineralization. The Cahanwusu porphyry Cu deposit is located in the western part of Awulale Mountain. Field investigations have shown that the mineralization in the deposit is genetically associated with granitic porphyry and diorite porphyry. In this paper, we provide detailed zircon U-Pb ages and in-situ Hf isotopic compositions of the granitic porphyry and diorite porphyry. The granitic porphyry and diorite porphyry have zircon U-Pb ages of 328.6 ± 2.6 Ma (MSWD = 0.52; n = 23) and 331 ± 2.8 Ma (MSWD = 0.95; n = 21), respectively. This indicates that the Cahanwusu deposit was formed in the Carboniferous in a subduction setting. This is distinguishable from other porphyry Cu deposits in the belt, which were generally formed in the Permian in the post-collision extensional setting. The granitic porphyry and diorite porphyry exhibit positive ε_Hf(t) values varying from +2.8 to +5.4 (average of +4.1) and +2.0 to +5.1 (average of +4.1), respectively. The magmas of these causative intrusions were interpreted to be derived from the partial melting of the juvenile lower crust which originated from cooling of mantle-derived magmas related to the subduction process. Our new results highlight that the Cahanwusu deposit represents a new episode of Cu mineralization in the belt and the Carboniferous granitoids in Awulale Mountain are potential candidates for Cu exploration.

1. Introduction

Awulale Mountain is located in the eastern segment of the Western Tianshan orogeny. It hosts numerous Fe and Cu (Au) polymetallic deposits, defining the so-called Awulale Fe-Cu Metallogenetic Belt [1,2,3,4,5,6]. Typical Fe deposits in the belt include the Zhibo, Dunde, Chagangnuoer, and Beizhan deposits. They are hosted by volcanic and volcanic-clastic rocks, especially the Carboniferous Dahalajunshan formation [1,5,7]. On the other hand, the Cu deposits, including the Nulasai, 109, Qunji, and Qunjisayi deposits, are generally genetically associated with the Permian intermediate and felsic intrusions [4,8,9]. Over the past decade, most research in the Awulale Fe-Cu metallogenetic belt has focused on Fe mineralization, and the genesis of these volcanic-related Fe deposits has been well established [6,10,11,12,13,14,15]. However, the Cu mineralization in the belt is rarely investigated. The precise age and magma source of the causative intrusions are currently not confirmed, constraining our understanding of regional mineralization.

The newly discovered Cahanwusu Cu deposit is located in the western part of Awulale Mountain. Filed investigations have shown that the mineralization in the deposit is genetically associated with granitic porphyry and diorite porphyry. However, the age and background of the mineralization is still ambiguous. In this paper, we provide detailed zircon U-Pb ages and in-situ Hf isotopic compositions of the granitic porphyry and diorite porphyry. Our new results not only well constrain the age and magma source of causative rocks in the Cahanwusu deposit, but also have important implications for the regional mineralization of the Awulale metallogenetic belt.

2. Geologic Background

The Tianshan orogenic belt is located in the southern part of the Central Asian Orogenic Belt (CAOB) (Figure 1a) and is divided into the Western and Eastern Tianshan belts. The Western Tianshan belt, which hosts Awulale Mountain, is sandwiched between the Junggar Block to the north and Tarim block to the south (Figure 1a). Tectonically, the Western Tianshan belt comprises four segments, including the North Tianshan arc accretionary complex in the north, the Yili block and the central Tianshan arc terrane in the middle and the northern margin of the Tarim block in the south [16,17,18,19]. The Western Tianshan belt has undergone a complex tectonic evolution [17,18,19]. The Paleozoic oceans, including the Terskey, North Tianshan, and South Tianshan Oceans, were closed in the Paleozoic, resulting in the amalgamations of a large amount of micro-continents in this period [17,18].

Awulale Mountain is located in the eastern part of the central Tianshan arc terrane in the Western Tianshan orogenic belt (Figure 1a). The Precambrian basement is located in the western part of Awulale Mountain and is composed of Meso- to Neo-Proterozoic gneisses, marble, migmatite and clastic rocks [20,21]. Volcanic sedimentary rocks and volcaniclastic sedimentary rocks with Silurian and Devonian ages are outcropped along the northern and southern margins of Awulale Mountain. Silurian and Devonian limestone are developed well, especially in the region around the Cahanwusu deposit. The carboniferous volcanic and volcaniclastic rocks, which are closely associated with Fe mineralization in the region, are widely distributed as a result of slab subduction. The Permian, Triassic and Jurassic strata consist mainly of conglomerate, sandstone, mudstone and shale and are locally present in the western part of Awulale Mountain.

3. Geology of the Cahanwusu Cu Deposit

The Cahanwusu Cu deposit is located in the eastern segment of Awulale Mountain (Figure 1b). The strata in the deposit are predominantly composed of Carboniferous volcano-sedimentary rocks and carbonate, which are locally overlain by the Quaternary alluvial and glacial–fluvial sediments (Figure 2). The volcano-sedimentary rocks are located in the northern part and are composed of andesites, tuffs and breccias. The intrusions include granitic porphyry and diorite porphyry, both of which are closely associated with mineralization (Figure 2). The granitic porphyry occurs as intrusions intruding both the volcano-sedimentary rocks and carbonate. It is composed of quartz, K-feldspar, plagioclase, and biotite with accessory minerals of apatite, zircon, allanite, and magnetite (Figure 3a). On the other hand, the diorite porphyry intrudes the volcano-sedimentary rocks and is composed dominantly of quartz, hornblende, plagioclase, and biotite, with minor zircon, apatite, titanite, and magnetite (Figure 3b).

The orebodies in the Cahanwusu deposit are typically lenticular in shape and are hosted in the volcano-sedimentary rocks (Figure 2). They have lengths of 100 to 500 m thickness of 10 to 50 m. The mineralization in the deposit occurs mainly as veins/veinlets. The veins (veinlets) have thicknesses ranging from one to several centimeters and are filled by granular quartz with abundant sulfides including bornite, chalcopyrite, molybdenite, pyrrhotite and pyrite (Figure 3c). Bornite is present as anhedral crystal and typically replaced by chalcopyrite. Chalcopyrite is widespread in the veins and occurs as subhedral to anhedral crystal or as disseminations (Figure 3c). The bornite and chalcopyrite at the surface are generally oxidized to malachite (Figure 3d). Molybdenite occurs in the form of flakes and small aggregates. In addition, disseminated molybdenite is also observed in the porphyries. Locally, the skarn-type mineralization, which consists of garnet, pyroxene, epidote, chlorite, quartz, calcite, chalcopyrite, bornite, molybdenite, and pyrite, is observed in the carbonate.

Propylitic alteration is intensive and pervasively developed in the volcano-sedimentary rocks and porphyries. It forms an alteration halo with a diameter of 2 km, enveloping the orebodies. The propylitic alteration is characterized by the development of widespread epidote and chlorite with minor sericite, actinolite, calcite, pyrite and chalcopyrite. In the volcano-sedimentary rocks and porphyries adjacent to the orebodies, the mafic minerals (e.g., biotite and hornblende) are almost completely replaced by the epidote and chlorite (Figure 3a). In addition to propylitic alteration, the quartz-sericite alteration, which is dominated by quartz, sericite, muscovite, pyrite, chlorite, bornite, chalcopyrite, pyrrhotite and molybdenite, is locally presented.

4. Analytical Methods

Representative granitic porphyry and diorite porphyry samples from the Cahanwusu deposit were collected for zircon LA-ICP-MS U-Pb dating and in-situ Hf isotopic analyses. The fresh porphyry samples were powdered into 80 meshes and deslimed in the purified water. This was followed by density separation and magnetic separation. After handpicking, the zircon grains were mounted in epoxy and polished to nearly a half section to expose internal structures. Prior to U-Pb and Hf isotopic analyses, all the zircon grains were investigated in optical microscopy and cathodoluminescent (CL) images to make sure that all the analyses were performed on the least fractured, inclusion-free zones.

4.1. Zircon U-Pb Dating

Zircon U-Pb analyses were performed using ELAN DRC-e ICP-MS equipped with a 193 nm Excimer laser at the State Key Laboratory of Ore Deposit Geochemistry (SKLODG), Institute of Geochemistry, Chinese Academy of Sciences. The measurement procedures and analytical conditions were similar to those described by Zhang et al. 2016 [22]. During the analyses, the spot sizes were 32 μm, whereas the laser repetition rates of the laser ablation system were 8 Hz. Helium and Argon were applied as carrier gas and make-up gas, respectively. The U-Pb fractionation and instrumental mass discrimination of zircon were normalized using the matrix-matched external zircon standard 91,500 (²⁰⁶Pb/²⁰⁸U age = 1062 Ma; Supplementary Materials Table S1) [23]. Two standard analyses were measured after every ten unknown spots. The data acquisition of each U-Pb analysis includes 20 s of gas blank, which is followed by 50 s of data acquisition. Off-line selection, integration of background and analytic signals, and mass bias calibrations were performed using ICPMSDataCal [24]. Age calculations and Concordia diagrams were conducted using the software Isoplot 3.0 [25].

4.2. Zircon Hf Isotope Analyses

In situ zircon Hf isotopic measurements were carried out using a Neptune MC-ICPMS equipped with a 193 nm ArF excimer laser ablation system at the SKLODG. The detailed operating conditions and analytical procedures are similar to those reported by Zhang et al. 2016 [22]. The analyses of zircon Lu-Hf isotopes were carried out on the same spots of U-Pb dating, using a laser beam diameter of 60 μm, a laser repetition rate of 10 Hz, and a laser beam energy density of 2.64–3.52 J/cm². Helium was used as a carrier gas to transport the ablated material from the laser-ablation cell to the ICPMS torch. Each measurement consisted of 20 s of background signal acquisition followed by 50 s of ablation signal acquisition. Zircon standard 91500 was used for external standard calibration to further optimize the analysis and test results. Two analyses of the standard were measured after every ten unknown spots. The standard zircons of 91500 yielded average ¹⁷⁶Hf/¹⁷⁷Hf values of 0.282298 ± 0.000012 (Supplementary Materials Table S2), in agreement with their recommended values (0.282297 ± 0.000044) [26,27]. Off-line selection and integration were also performed by using ICPMSDataCal.

5. Results

5.1. Zircon U-Pb Ages

Zircon grains from the granitic porphyry are generally colorless or transparent, euhedral to subhedral, and elongate to stubby in shape (Figure 4a). They have length varies from 100 to 200 μm with length-to-width ratios of 2:1 to 3:1. Most zircon grains exhibit typical magmatic oscillatory zonation and few contain inherited cores (Figure 4a). The detailed U-Pb results are reported in Table 1 and the U-Pb concordia diagram and weighted mean ²⁰⁶Pb/²³⁸U ages are shown in Figure 5. Zircon grains from the granitic porphyry have Th/U ratios varying between 0.35 and 0.93 (average 0.52; Table 1), which is consistent with a magmatic origin [28,29]. On the U-Pb Wetherill concordia diagram, the analyses yield a concordia age of 328.8 ± 3.5 Ma (Figure 5a). This age is consistent with the weighted mean ²⁰⁶Pb/²³⁸U ages of 328.6 ± 2.6 Ma (MSWD = 0.52; n = 23) (Figure 5b).

Zircon grains from the diorite porphyry have a morphology similar to that in the granitic porphyry (Figure 4b). They have Th/U ratios varying from 0.45 and 0.92 (average 0.58; Table 1), indicating they are magmatic in origin [28,29]. On the U-Pb Wetherill concordia diagram, the analyses yield a concordia age of 331.2 ± 1.4 Ma (Figure 5c). The weighted mean ²⁰⁶Pb/²³⁸U ages is 331.0 ± 2.8 Ma (MSWD = 0.95; n = 21) (Figure 5d). These ages are consistent with that of zircon grains in the granitic porphyry (Figure 5).

5.2. Zircon Hf Isotopes

Detailed in-situ Lu-Hf isotopic data of zircon from the granitic porphyry and diorite porphyry are presented in Table 2. Zircon grains from the granitic porphyry have ¹⁷⁶Hf/¹⁷⁷Hf ratios of 0.282659 to 0.282727 (average of 0.282692; Table 2). The calculated ε_Hf(t) values (age-corrected using the U-Pb age of individual grains) are similar, ranging from +2.83 to +5.42 with an average value of +4.09 (Table 2). All the analyses fall between the chondrite uniform reservoir reference line and the depleted mantle evolution line (Figure 6). The corresponding two-stage Hf model ages (T_DM2) vary from 992 to 1155 Ma (average of 1075 Ma) (Table 2). On the other hand, zircon grains from the diorite porphyry have ¹⁷⁶Hf/¹⁷⁷Hf ratios of 0.282637 to 0.282725 (average of 0.282690). The calculated ε_Hf(t) values (age-corrected using the U-Pb age of individual grains) are similar to that of zircon in the granitic porphyry, varying from +2.0 to +5.1 (average of +4.1; Figure 6). The T_DM2 ages vary from 1013 to 1208 Ma (average of 1079 Ma), also consistent with that of zircon grains in the granitic porphyry (Table 2).

6. Discussion

6.1. New Episode of Cu Mineralization in Awulale Mountain

The granitic porphyry and diorite porphyry are the exclusive intrusions in the Cahanwusu Cu deposit (Figure 2). The two pluses of porphyryies occur as plugs and host abundant quartz-chalcopyrite veins. In addition, they are strongly overprinted by propylitic alteration, where mafic minerals such as biotite and hornblende are mostly replaced by epidote and chlorite (Figure 3a). These features fit well with the causative intrusions in the porphyry Cu deposits [34,35]. This indicates that the mineralization is genetically associated with the granitic porphyry and diorite porphyry in the Cahanwusu deposit.

Previous studies have shown that the Cu mineralization in the Awulale Fe-Cu Metallogenetic Belt mostly occurred in the Permian. For example, the mineralization associated albite porphyry in the 109 deposit yields zircon U-Pb ages of 300 ± 4 Ma [8], the diabase, which hosts Cu mineralization in the Qunjsai deposit, has zircon U-Pb ages of 289.9 ± 1.4 Ma [9], and the granite porphyry in the Nulasai Cu deposit has zircon U-Pb ages of 288.3 ± 3.0 Ma. On the other hand, the sulfides in the deposit yield Re-Os ages of 283.5 ± 5.8 Ma [36]. However, our new results show that the mineralization-associated granitic porphyry and diorite porphyry in the Cahanwusu deposit have zircon U-Pb ages of 328.6 ± 2.6 Ma and 331 ± 2.8 Ma, respectively (Figure 5). This indicates that mineralization in the Cahanwusu deposit occurred at ca. 330 Ma, significantly older than that of other Cu deposits in Awulale Mountain. On this basis, we suggest that the Cahanwusu deposit represents an old episode of Cu mineralization in Awulale Mountain.

6.2. Tectonic Setting and Magma Sources

Detailed zircon U-Pb ages demonstrate that the Cahanwusu deposit was generated in the Carboniferous (Figure 5). The tectonic evolution of Awulale Mountain in the Late Paleozoic is still controversial. Two main models have been proposed, including (1) intra-continental rifting and post-collisional mantle plume activity in the extension setting [37,38,39], and (2) active continental arc setting related to the northward subduction of the South Tianshan Ocean [17,40,41,42,43,44]. The Carboniferous granitoids in Awulale Mountain are all calc-alkaline I-type granites with subduction-related features, e.g., enrichment in large ion lithophile elements (LILEs) relative to high field strength elements (HFSEs), and depletion of Nb and Ta [15,43,44,45]. In addition, the widely distributed Dahalajunshan Formation, which consisted of volcanic rocks with Early Devonian to Late Carboniferous ages (417 Ma to 304 Ma), also displays arc type signatures [1,40,46,47]. These observations indicate that the South Tianshan Ocean had been subducting northward under the Yili block during the Carboniferous (Figure 7a). Therefore, we suggest that the Cahanwusu deposit was formed in the continental arc setting related to the northward subduction of the South Tianshan Ocean. However, Permian shoshonitic rocks and underplating adakite with post-subduction signatures have widely been reported in Awulale Mountain [32,44,48,49,50]. This implies that the subduction of the South Tianshan Ocean had ceased and Awulale Mountains entered a post-collisional extensional setting since the Permian (Figure 7b).

The granitic porphyry and diorite porphyry in the Cahanwusu deposit have similar zircon U-Pb ages and Hf isotopic compositions (Figure 5 and Figure 6). This indicates that the two pluses of porphyries share similar magma sources. The granitic porphyry and diorite porphyry have positive ε_Hf(t) values varying from +2.83 to +5.42 (average of +4.09) and +2.0 to +5.1 (average of +4.1), respectively (Figure 6), which is inconsistent with granitoids derived from renewed melting or deep melting of ancient crust. However, this positive ε_Hf(t) value is similar to other Carboniferous intrusions in Awulale Mountain (Figure 6), such as the Wuling hornblende gabbro [31] and Zhongyangchang granitoids [30]. Actually, Paleozoic granitoids with positive ε_Nd(t) and/or ε_Hf(t) values have been widely reported in the CAOB [22,30,32,50,51,52,53,54,55]. This isotopic anomaly was interpreted to have resulted from the involvement of juvenile materials in their mantle source.

The juvenile crust has played an important role in the generation of the Phanerozoic granitoids in the CAOB [16,55,56,57,58]. During the Neoproterozoic to Mesozoic orogeny, large amounts of juvenile materials were incorporated into the crust, representing the most important crustal growth event in the Phanerozoic [16,57,58,59]. Most juvenile crusts in the CAOB were related to the accretion of arc complexes that were derived from the cooling of mantle-derived magmas in the course of the subduction process [58]. However, mantle underplating in post-collisional settings also played an important role in the crustal growth of juvenile crusts in the CAOB [55,57]. It is proposed that the voluminous A-type granites with positive ε_Nd(t) and ε_Hf(t) values in the post-collision setting were derived from the partial melting of the underplated basaltic magmas and subsequent extensive fractional crystallization [55]. However, A-type granites contemporary with the granitic porphyry and diorite porphyry in the Cahanwusu deposit have not been documented in Awulale Mountain. Therefore, the crustal growth model that involves mantle underplating in post-collisional settings can be excluded. As mentioned earlier, the Carboniferous granitoids in Awulale Mountain generally exhibit subduction-related features, i.e., enrichment in LILEs relative to HFSEs, and depletion of Nb and Ta [15,43,44,45]. On this basis, we suggest that the magmas of granitic porphyry and diorite porphyry could be derived from the partial melting of the juvenile lower crust which originated from cooling of mantle-derived magmas related to the subduction process.

6.3. Implication for Regional Mineralization

Our new results show that the Cahanwusu deposit represents a new episode of Cu mineralization in the Awulale metallogenetic belt formed in the subduction setting (Figure 7a). This has important implications for regional exploration of porphyry Cu deposits in the belt. Porphyry Cu deposits can be formed in both subduction and post-collision settings [60,61,62]. Most porphyry Cu deposits in the Awulale metallogenetic belt are clustered in the Permian [2,4,8,9,63,64]. Some causative intrusions in these deposits show an affinity of A-type granitic rocks which were generally related to extensional settings, such as the 109 and Qunjisayi deposits [8,65]. Therefore, these porphyry Cu deposits were interpreted to be formed in a post-collision extensional setting (Figure 7b). In contrast, the Cahanwusu deposit was formed in the Carboniferous during the subduction of the South Tianshan Ocean. Actually, the subduction of the South Tianshan Ocean in the Carboniferous has resulted in a variety of calc-alkaline I-type granitoids in Awulale Mountain [15,43,44,45]. The calc-alkaline I-type granitoids formed in the subduction setting are generally potential targets for porphyry-type Cu mining [35,66,67]. Therefore, although Cu mineralization associated with these Carboniferous granitoids has rarely been documented currently, our new results of the Cahanwusu deposit indicate that these Carboniferous granitoids are also potential candidates for Cu exploration in Awulale Mountain.

7. Conclusions

The granitic porphyry and diorite porphyry in the Cahanwusu deposit have zircon U-Pb ages of 328.6 ± 2.6 Ma and 331 ± 2.8 Ma, respectively. These ages are significantly older than that of other Cu deposits in the Awulale metallogenetic belt, indicating that the Cahanwusu deposit represents a new episode of Cu mineralization in the belt. The Cahanwusu deposit was formed in a subduction setting, distinguishable from other Cu deposits in the belt which were generally formed in the post-collision extensional setting. The granitic porphyry and diorite porphyry exhibit positive ε_Hf(t) values, and the magmas of these causative intrusions were derived from partial melting of the juvenile lower crust which originated from the cooling of mantle-derived magmas related to the subduction process. Our new results highlight that the Carboniferous granitoids in Awulale Mountain are potential candidates for Cu exploration.

Author Contributions

Conceptualization, W.Z. and X.-C.Z.; methodology, M.-X.C. and M.-L.Y.; software, W.-H.Y.; validation, W.Z. and X.-C.Z.; investigation, W.Z., W.-H.Y. and X.-C.Z.; data curation, M.-X.C. and M.-L.Y.; writing—original draft preparation, W.Z.; writing—review and editing, W.Z. and X.-C.Z.; supervision, X.-C.Z.; project administration, W.Z. and X.-C.Z.; funding acquisition, W.Z. and X.-C.Z. All authors have read and agreed to the published version of the manuscript.

Data Availability Statement

Data is contained within the article and Supplementary Materials.

Acknowledgments

We are grateful to Zhi-Hui Dai and Hong-Feng Tang for their help with the analyses. Ding-Jin Wu and Jing-Liang Cao are thanked for their assistance in the field.

Conflicts of Interest

The authors declare no conflicts of interest.

Footnotes

Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Figures and Tables

Figure 1 (a) Regional geological map of the Western Tianshan and the location of Awulale Mountain. Modified from Zhang et al. 2014 [5]. Inset map showing the location of the Western Tianshan within the Central Asian Orogenic Belt. (b) Simplified geological map of the Awulale Fe-Cu Metallogenetic Belt and the location of some Cu and Fe deposits. Modified from Hong et al. 2020 [11]. NTS = North Tianshan Suture, NL = Nikolaev Line, STS = South Tianshan Suture.

Figure 2 Simplified geological map of the Cahanwusu Cu deposit (after Central South Geo-Exploration Institute, unpublished internal report).

Figure 3 (a) Photograph of the granitic porphyry. Note that the biotite and hornblende are intensively replaced by epidote. (b) Photograph of the diorite porphyry. (c) Quartz-chalcopyrite vein crosscut the volcanic rock. (d) Chalcopyrite is oxidized to malachite at the surface.

Figure 4 Representative cathodoluminescence images of zircon grains in the granitic porphyry (a) and diorite porphyry (b). The U-Pb dating spots are denoted by white circles and the Lu-Hf isotopic spots are denoted by yellow circles.

Figure 5 LA-ICP-MS U-Pb ages of zircon from the granitic porphyry and diorite porphyry in the Cahanwusu deposit. (a) Wetherill concordia diagram and (b) weighted average ²⁰⁶Pb/²³⁸U ages of zircon from the granitic porphyry. (c) Wetherill concordia diagram and (d) weighted average ²⁰⁶Pb/²³⁸U ages of zircon from the diorite porphyry.

Figure 6 The ε_Hf(t) vs. U-Pb age (Ma) diagram of the granitic porphyry and diorite porphyry in the Cahanwusu deposit. The area of other Carboniferous intrusions in Awulale Mountain is plotted by Tang et al. (2014) [30], Yan et al. (2015) [31], and Sun et al. (2021, 2022) [32,33].

Figure 7 Sketch model showing the tectonic evolution of Awulale Mountain and the corresponding Cu mineralization in the Late Paleozoic. (a) In the Carboniferous, the South Tianshan Oceanic Crust subducted beneath the Yili-central Tianshan, resulting in the formation of Cahanwusu Cu deposit. (b) In the Permian, break-off of the subducted slab in the post-collisional setting triggered the upwelling of the depleted asthenospheric mantle and produced the Nalusai and 109 deposits. SCLM = subcontinental lithospheric mantle.

Table 1

Zircon LA-ICP-MS U-Pb ages of granitic porphyry and diorite porphyry in the Cahanwusu deposit.

Spots	Th (ppm)	U (ppm)	Th/U	207Pb/206Pb		207Pb/235U		206Pb/238U		207Pb/206Pb		207Pb/235U		206Pb/238U		Concordance
				Ratio	1sigma	Ratio	1sigma	Ratio	1sigma	Age	1sigma	Age	1sigma	Age	1sigma
Granitic Porphyry
CH12-01	325	693	0.47	0.0597	0.0036	0.4496	0.0251	0.0532	0.0011	594	131	377	17.5	334	6.83	97%
CH12-02	355	611	0.58	0.0570	0.0034	0.4218	0.0228	0.0531	0.0011	500	131	357	16.3	334	6.47	95%
CH12-03	350	751	0.47	0.0528	0.0028	0.3832	0.0178	0.0522	0.0009	320	122	329	13.1	328	5.77	99%
CH12-04	244	518	0.47	0.0555	0.0032	0.4116	0.0247	0.0524	0.0010	435	134	350	17.8	330	6.16	98%
CH12-05	234	673	0.35	0.0540	0.0026	0.3957	0.0187	0.0521	0.0009	369	109	339	13.6	327	5.66	96%
CH12-06	179	321	0.56	0.0531	0.0036	0.3920	0.0252	0.0537	0.0013	332	154	336	18.4	337	7.73	99%
CH12-07	560	916	0.61	0.0569	0.0027	0.4080	0.0179	0.0514	0.0008	487	99.1	347	12.9	323	5.15	96%
CH12-09	283	634	0.45	0.0551	0.0032	0.4059	0.0239	0.0520	0.0009	417	128	346	17.3	327	5.71	94%
CH12-10	562	914	0.61	0.0546	0.0025	0.4003	0.0180	0.0521	0.0008	394	97.2	342	13.1	328	5.15	95%
CH12-11	125	257	0.48	0.0589	0.0056	0.4146	0.0328	0.0535	0.0014	565	208	352	23.5	336	8.37	95%
CH12-12	381	722	0.53	0.0577	0.0027	0.4175	0.0185	0.0519	0.0010	517	102	354	13.3	326	6.09	97%
CH12-14	264	504	0.52	0.0647	0.0043	0.4583	0.0293	0.0512	0.0012	765	142	383	20.4	322	7.10	96%
CH12-15	168	382	0.44	0.0601	0.0037	0.4503	0.0282	0.0530	0.0013	606	140	377	19.7	333	7.77	97%
CH12-16	208	470	0.44	0.0538	0.0033	0.3864	0.0217	0.0515	0.0010	365	141	332	15.9	323	6.40	97%
CH12-17	279	593	0.47	0.0564	0.0029	0.4108	0.0197	0.0519	0.0010	465	113	349	14.2	326	5.90	93%
CH12-18	292	648	0.45	0.0537	0.0026	0.4058	0.0191	0.0532	0.0009	367	105	346	13.8	334	5.62	96%
CH12-19	349	641	0.55	0.0531	0.0029	0.4017	0.0205	0.0537	0.0011	332	121	343	14.9	337	6.81	98%
CH12-20	104	272	0.38	0.0518	0.0038	0.3886	0.0281	0.0530	0.0014	280	167	333	20.6	333	8.56	99%
CH12-22	427	555	0.77	0.0565	0.0032	0.4103	0.0227	0.0512	0.0011	472	124	349	16.3	322	6.46	93%
CH12-23	367	554	0.66	0.0583	0.0031	0.4340	0.0222	0.0525	0.0010	543	110	366	15.7	330	5.91	98%
CH12-24	685	734	0.93	0.0546	0.0027	0.4066	0.0185	0.0527	0.0010	394	109	346	13.4	331	5.94	95%
CH12-25	374	763	0.49	0.0536	0.0026	0.3915	0.0177	0.0517	0.0009	354	107	335	12.9	325	5.82	96%
CH12-26	135	362	0.37	0.0624	0.0038	0.4533	0.0267	0.0517	0.0013	687	130	380	18.7	325	7.70	95%
Diorite porphyry
CH15-01	180	278	0.6467	0.0541	0.0031	0.3928	0.0209	0.0514	0.0010	376	128	336	15.2	323	6.3	97%
CH15-02	313	422	0.7413	0.0543	0.0026	0.3916	0.0182	0.0524	0.0009	383	107	336	13.3	329	5.5	98%
CH15-03	157	318	0.4950	0.0568	0.0032	0.4050	0.0217	0.0523	0.0010	483	129	345	15.7	329	6.2	96%
CH15-04	364	490	0.7425	0.0513	0.0022	0.3702	0.0155	0.0522	0.0009	254	100	320	11.5	328	5.3	97%
CH15-05	116	181	0.6377	0.0556	0.0036	0.3949	0.0247	0.0517	0.0011	435	146	338	18.0	325	6.6	96%
CH15-06	97.3	195	0.4984	0.0541	0.0032	0.3825	0.0218	0.0511	0.0012	376	135	329	16.0	321	7.2	97%
CH15-08	600	644	0.9308	0.0513	0.0022	0.3795	0.0158	0.0520	0.0009	254	98.1	327	11.6	327	5.3	99%
CH15-09	151	240	0.6264	0.0533	0.0036	0.3836	0.0236	0.0519	0.0010	339	147	330	17.3	326	6.2	98%
CH15-10	190	318	0.5965	0.0553	0.0028	0.4041	0.0198	0.0525	0.0011	433	147	345	14.3	330	6.7	95%
CH15-11	57.2	125	0.4573	0.0573	0.0049	0.4066	0.0287	0.0537	0.0014	502	189	346	20.7	337	8.8	97%
CH15-13	406	510	0.7964	0.0533	0.0023	0.3941	0.0159	0.0529	0.0008	339	98.1	337	11.6	332	4.9	98%
CH15-14	87.8	174	0.5054	0.0550	0.0036	0.4185	0.0267	0.0545	0.0012	413	146	355	19.1	342	7.4	96%
CH15-15	142	255	0.5559	0.0577	0.0036	0.4273	0.0239	0.0545	0.0011	520	137	361	17.0	342	6.8	94%
CH15-16	130	235	0.5544	0.0557	0.0037	0.4079	0.0248	0.0533	0.0012	443	148	347	17.9	335	7.1	96%
CH15-17	94.4	183	0.5165	0.0593	0.0041	0.4371	0.0272	0.0541	0.0014	589	145	368	19.2	340	8.4	98%
CH15-19	177	285	0.6213	0.0590	0.0034	0.4206	0.0216	0.0527	0.0010	565	126	356	15.4	331	6.1	97%
CH15-20	76.1	146	0.5193	0.0578	0.0045	0.4238	0.0301	0.0550	0.0014	524	174	359	21.5	345	8.6	96%
CH15-21	67.3	127	0.5303	0.0657	0.0054	0.4391	0.0296	0.0523	0.0013	798	174	370	20.9	329	7.8	98%
CH15-22	119	182	0.6542	0.0531	0.0037	0.3948	0.0261	0.0540	0.0012	345	157	338	19.0	339	7.1	99%
CH15-23	237	488	0.4860	0.0555	0.0025	0.3978	0.0167	0.0518	0.0009	432	98.1	340	12.1	326	5.6	95%
CH15-24	193	360	0.5366	0.0540	0.0028	0.4038	0.0201	0.0540	0.0011	372	119	344	14.6	339	6.7	98%

Table 2

Hf isotopes of zircons from the granitic porphyry and diorite porphyry in the Cahanwusu deposit.

Spots	176Lu/177Hf	1σ	176Hf/177Hf	1σ	εHf(t)	1σ	TDM1	1σ	TDM2	1σ
Granitic Porphyry
CH12-01	0.001403	0.000010	0.282669	0.000018	3.26	0.64	835	25.7	1128	40.4
CH12-02	0.001606	0.000087	0.282680	0.000017	3.60	0.60	824	24.5	1106	38.2
CH12-03	0.001168	0.000016	0.282682	0.000018	3.77	0.64	812	25.5	1096	40.4
CH12-04	0.001018	0.000010	0.282694	0.000016	4.23	0.57	792	22.6	1067	35.9
CH12-05	0.001135	0.000003	0.282699	0.000016	4.38	0.57	787	22.7	1057	35.9
CH12-06	0.001293	0.000034	0.282660	0.000011	2.96	0.39	846	15.7	1147	24.7
CH12-07	0.001359	0.000013	0.282678	0.000018	3.59	0.64	822	25.7	1107	40.4
CH12-09	0.001334	0.000022	0.282689	0.000017	3.98	0.60	805	24.2	1082	38.2
CH12-10	0.001491	0.000018	0.282679	0.000019	3.59	0.67	823	27.2	1107	42.6
CH12-11	0.001388	0.000011	0.282688	0.000018	3.94	0.64	808	25.7	1085	40.4
CH12-12	0.001535	0.000025	0.282720	0.000021	5.04	0.74	765	30.1	1015	47.2
CH12-14	0.001058	0.000017	0.282686	0.000019	3.94	0.67	804	26.9	1085	42.7
CH12-15	0.001384	0.000056	0.282696	0.000018	4.22	0.64	797	25.7	1067	40.4
CH12-16	0.000990	0.000026	0.282695	0.000012	4.27	0.42	790	17.0	1064	27.0
CH12-17	0.001237	0.000009	0.282687	0.000022	3.95	0.78	806	31.3	1085	49.4
CH12-18	0.001832	0.000035	0.282659	0.000018	2.83	0.64	860	26.0	1156	40.4
CH12-19	0.001041	0.000002	0.282713	0.000019	4.92	0.67	765	26.9	1024	42.7
CH12-20	0.001347	0.000075	0.282700	0.000015	4.39	0.53	790	21.4	1057	33.7
CH12-22	0.001003	0.000038	0.282727	0.000014	5.42	0.50	745	19.8	992	31.5
CH12-23	0.001152	0.000012	0.282705	0.000018	4.61	0.64	779	25.5	1043	40.5
CH12-24	0.001255	0.000012	0.282697	0.000016	4.30	0.57	792	22.8	1063	35.9
CH12-25	0.001733	0.000030	0.282712	0.000017	4.73	0.60	781	24.5	1036	38.2
CH12-26	0.001641	0.000063	0.282696	0.000019	4.18	0.67	802	27.3	1070	42.7
Diorite Porphyry
CH15-01	0.001253	0.000005	0.282707	0.000019	4.70	0.67	778	27.0	1039	42.7
CH15-02	0.002497	0.000180	0.282725	0.000016	5.07	0.57	778	23.9	1016	36.1
CH15-03	0.001476	0.000026	0.282692	0.000018	4.12	0.64	804	25.8	1076	40.4
CH15-04	0.001392	0.000006	0.282695	0.000020	4.25	0.71	798	28.5	1068	44.9
CH15-05	0.001217	0.000004	0.282718	0.000014	5.10	0.50	762	19.9	1014	31.5
CH15-06	0.001352	0.000043	0.282656	0.000016	2.87	0.57	853	22.8	1155	35.9
CH15-08	0.002171	0.000140	0.282699	0.000016	4.22	0.57	809	23.5	1070	36.0
CH15-09	0.001465	0.000020	0.282706	0.000012	4.62	0.42	784	17.2	1044	27.0
CH15-10	0.001126	0.000003	0.282697	0.000020	4.37	0.71	790	28.3	1060	44.9
CH15-11	0.001149	0.000004	0.282683	0.000014	3.87	0.50	810	19.8	1092	31.4
CH15-13	0.001150	0.000004	0.282699	0.000013	4.44	0.46	787	18.4	1056	29.2
CH15-14	0.001118	0.000006	0.282661	0.000019	3.10	0.67	840	26.9	1140	42.6
CH15-15	0.001203	0.000018	0.282688	0.000015	4.04	0.53	804	21.3	1081	33.7
CH15-16	0.002177	0.000065	0.282637	0.000018	2.02	0.64	900	26.3	1209	40.3
CH15-17	0.001253	0.000012	0.282696	0.000018	4.31	0.64	794	25.6	1064	40.4
CH15-19	0.000946	0.000006	0.282701	0.000019	4.56	0.67	780	26.8	1048	42.7
CH15-20	0.000825	0.000010	0.282662	0.000017	3.20	0.60	833	23.9	1134	38.1
CH15-21	0.001016	0.000013	0.282705	0.000024	4.68	0.85	776	33.9	1040	53.9
CH15-22	0.001241	0.000006	0.282677	0.000014	3.64	0.50	821	19.9	1106	31.4
CH15-23	0.001360	0.000021	0.282695	0.000013	4.25	0.46	797	18.5	1068	29.2
CH15-24	0.001603	0.000030	0.282685	0.000016	3.85	0.57	817	23.0	1093	35.9

ε_Hf (t) = ((¹⁷⁶Hf/¹⁷⁷Hf)_S − (¹⁷⁶Lu/¹⁷⁷Hf)_S × (e^λt −1))/((¹⁷⁶Hf/¹⁷⁷Hf)_CHUR,0 − (¹⁷⁶Lu/¹⁷⁷Hf)_CHUR × (e^λt − 1) − 1) × 10,000; T_DM1 = 1/λ × In (1 + ((¹⁷⁶Hf/¹⁷⁷Hf)_S − (¹⁷⁶Hf/¹⁷⁷Hf)_DM)/((¹⁷⁶Lu/¹⁷⁷Hf)_S − (¹⁷⁶Lu/¹⁷⁷Hf)_DM)); T_DM2 = T_Hf1 − (T_Hf1 − t)((f_cc − f_s)/(f_cc − f_DM)). Note: the ε_Hf(t) ratios were calculated with the age in Table 1.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min15040380/s1, Table S1: LA-ICP-MS U-Pb results of zircon standard 91500; Table S2: LA-MC-ICP-MS Hf isotopes of zircon standard 91500.

References

1. Ge, S.; Zhai, M.; Safonova, I.; Li, D.; Zhu, X.; Zuo, P.; Shan, H. Whole-rock geochemistry and Sr–Nd–Pb isotope systematics of the Late Carboniferous volcanic rocks of the Awulale metallogenic belt in the western Tianshan Mountains (NW China): Petrogenesis and geodynamical implications. Lithos; 2015; 228–229, pp. 62-77. [DOI: https://dx.doi.org/10.1016/j.lithos.2015.04.019]

2. Liu, R.; Chen, G. Characteristics of rare earth elements, Zr, and Hf in ore-bearing porphyries from the Western Awulale Metallogenic Belt, Northwestern China and their application in determining metal fertility of granitic magma. Resour. Geol.; 2018; 69, pp. 193-210.

3. Shan, Q.; Zhang, B.; Luo, Y.; Zhou, C.P.; Yu, X.Y.; Zeng, Q.S.; Yang, W.B.; Niu, H.C. Characteristics and trace element geochemistry of pyrite from the Songhu iron deposit, Nilek County, Xinjiang, China. Acta Petrol. Sinica; 2009; 25, pp. 1456-1464.

4. Wang, R.; Zhao, X.; Xue, C.; Chu, H.; Zhao, Y.; Sun, Q.; Zhu, W. Fluid evolution of the Nulasai Cu deposit, Xinjiang, NW China: Evidence from fluid inclusions and O-H-C isotopes. Ore Geol. Rev.; 2024; 173, 106220.

5. Zhang, Z.; Hong, W.; Jiang, Z.; Duan, S.; Li, F.; Shi, F. Geological characteristics and metallogenesis of iron deposits in western Tianshan, China. Ore Geol. Rev.; 2014; 57, pp. 425-440.

6. Sun, W.; Niu, Y.; Ma, Y.; Liu, Y.; Zhang, G.; Hu, Z.; Zhang, Z.; Chen, S.; Li, J.; Wang, X. . Petrogenesis of the Chagangnuoer deposit, NW China: A general model for submarine volcanic-hosted skarn iron deposits. Sci. Bull.; 2015; 60, pp. 363-379.

7. Feng, J.X.; Shi, F.P.; Wang, B.Y.; Hu, J.M.; Wang, J.T.; Tian, J.Q. The Syngenetic Volcanogenic Iron ore Deposits in Awulale Metallogenetic Belt, Western Tianshan Mountains; Geological Publishing House: Beijing, China, 2010; 132.(In Chinese)

8. Liu, R.; Chen, G. The 109 porphyry Cu deposit in the western Tianshan orogenic belt, NW China: An example of Cu mineralization in a reduced magmatichydrothermal system in an extensional setting. Ore Geol. Rev.; 2019; 112, 102989.

9. Zhao, X.; Xue, C.; Chi, G.; Zhao, J.; Yan, Y. Diabase-hosted copper mineralization in the Qunjsai deposit, West Tianshan, NW China: Geological, geochemical and geochronological characteristics and mineralization mechanism. Ore Geol. Rev.; 2018; 92, pp. 430-448.

10. Duan, S.; Zhang, Z.; Jiang, Z.; Zhao, J.; Zhang, Y.; Li, F.; Tian, J. Geology, geochemistry, and geochronology of the Dunde iron-zinc ore deposit in western Tianshan, China. Ore Geol. Rev.; 2014; 57, pp. 441-446. [DOI: https://dx.doi.org/10.1016/j.oregeorev.2013.08.019]

11. Hong, W.; Zhang, Z.; Baker, M.J.; Jiang, Z.; Duan, S. Zircon U-Pb dating and stable isotopic compositions for constraining the genesis of the Chagangnuoer magnetite deposit in western Tianshan, NW China. Ore Geol. Rev.; 2020; 121, 103478.

12. Jiang, Z.; Zhang, Z.; Wang, Z.; Duan, S.; Li, F.; Tian, J. Geology, geochemistry, and geochronology of the Zhibo iron deposit in the Western Tianshan, NW China: Constraints on metallogenesis and tectonic setting. Ore Geol. Rev.; 2014; 57, pp. 406-424.

13. Wang, X.S.; Zhang, X.; Gao, J.; Li, J.L.; Jiang, T.; Xue, S.C. A slab break-off model for the submarine volcanic-hosted iron mineralization in the Chinese Western Tianshan: Insights from Paleozoic subduction-related to post-collisional magmatism. Ore Geol. Rev.; 2018; 92, pp. 144-160.

14. Zhang, X.; Klemd, R.; Gao, J.; Dong, L.H.; Wang, X.S.; Haase, K.; Jiang, T.; Qian, Q. Metallogenesis of the Zhibo and Chagangnuoer volcanic iron oxide deposits in the Awulale Iron Metallogenic Belt, Western Tianshan orogen, China. J. Asian Earth Sci.; 2015; 113, pp. 151-172. [DOI: https://dx.doi.org/10.1016/j.jseaes.2014.06.004]

15. Zhang, X.; Tian, J.Q.; Gao, J.; Klemd, R.; Dong, L.H.; Fan, J.J.; Jiang, T.; Hu, C.J.; Qian, Q. Geochronology and geochemistry of granitoid rocks from the Zhibo syngenetic volcanogenic iron ore deposit in the Western Tianshan Mountains (NW-China): Constraints on the age of mineralization and tectonic setting. Gondwana Res.; 2012; 22, pp. 585-596.

16. Windley, B.F.; Alexeiev, D.; Xiao, W.J.; Kröner, A.; Badarch, G. Tectonicmodels for accretion of the Central Asian Orogenic Belt. J. Geol. Soc.; 2007; 164, pp. 31-47.

17. Gao, J.; Long, L.L.; Klemd, R.; Qian, Q.; Liu, D.Y.; Xiong, X.M.; Sun, W.; Liu, W.; Wang, Y.T.; Wang, F.Y. Tectonic evolution of the South Tianshan orogen and adjacent regions, NW China: Geochemical and age constraints of granitoid rocks. Int. J. Earth Sci.; 2009; 98, pp. 1221-1238.

18. Charvet, J.; Shu, L.S.; 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, pp. 166-184.

19. Xiao, W.J.; Windley, B.F.; Allen, M.B.; Han, C.M. Paleozoic multiple accretionary and collisional tectonics of the Chinese Tianshan orogenic collage. Gondwana Res.; 2013; 23, pp. 1316-1341.

20. Gao, J.; Li, M.S.; Xiao, X.C.; Tang, Y.Q.; He, G.Q. Paleozoic tectonic evolution of the Tianshan Orogen northwestern China. Tectonophysics; 1998; 287, pp. 212-231.

21. Li, J.L.; Su, W.; Zhang, X. Zircon Cameca U–Pb dating and its significance for granulite-facies granitic gneisses from the west Awulale Mountains, West Tianshan. Geol. Bull Chin.; 2009; 28, pp. 1852-1862. (In Chinese with English Abstract)

22. Zhang, W.; Leng, C.B.; Zhang, X.C.; Su, W.C.; Tang, H.F.; Yan, J.H.; Cao, J.L. Petrogenesis of the Seleteguole granitoids from Jinhe county in Xinjiang (West China): Implications for the tectonic transformation of Northwest Tianshan. Lithos; 2016; 256–257, pp. 148-164. [DOI: https://dx.doi.org/10.1016/j.lithos.2016.04.002]

23. Wiedenbeck, M.; Allé, P.; Corfu, F.; Griffin, W.L.; Meier, M.; Oberli, F.; Quadt, A.V.; Roddick, J.C.; Spiegel, W. Three natural zircon standards for U-Th-Pb, Lu-Hf, trace element and REE analyses. Geostand. Geoanal. Res.; 1995; 19, pp. 1-23. [DOI: https://dx.doi.org/10.1111/j.1751-908X.1995.tb00147.x]

24. Liu, Y.S.; Gao, S.; Hu, Z.C.; Gao, C.G.; Zong, K.Q.; Wang, D.B. Continental and oceanic crust recycling-induced melt-peridotite interactions in the Trans-North China orogen: U-Pb dating, Hf isotopes and trace elements in zircons of mantle xenoliths. J. Petrol.; 2010; 51, pp. 537-571. [DOI: https://dx.doi.org/10.1093/petrology/egp082]

25. Ludwig, K.R. User’s Manual for Isoplot 3.0: A Geochronological Toolkit for Microsoft Excel; Special Publication No 4 Berkeley Geochronology Center: Berkeley, CA, USA, 2003.

26. Griffin, W.L.; Pearson, N.J.; Belousova, E.; Jackson, S.E.; van Achterbergh, E.; O’Reilly, S.Y.; Shee, S.R. The Hf isotope composition of cratonic mantle: LAM-MC-ICPMS analysis of zircon megacrysts in kimberlites. Geochim. Cosmochim. Acta; 2000; 64, pp. 133-147. [DOI: https://dx.doi.org/10.1016/S0016-7037(99)00343-9]

27. Griffin, W.L.; Wang, X.; Jackson, S.E.; Pearson, N.J.; O’Reilly, S.Y.; Xu, X.; Zhou, X. Zircon chemistry and magma mixing, SE China: In-situ analysis of Hf isotopes. Tonglu and Pingtan igneous complexes. Lithos; 2002; 61, pp. 237-269. [DOI: https://dx.doi.org/10.1016/S0024-4937(02)00082-8]

28. Belousova, E.A.; Griffin, W.L.; O’Reilly, S.Y.; Fisher, N.I. Igneous zircon, trace element composition as an indicator of source rock type. Contrib. Mineral. Petr.; 2002; 143, pp. 602-622. [DOI: https://dx.doi.org/10.1007/s00410-002-0364-7]

29. Rubatto, D. Zircon trace element geochemistry: Partitioning with garnet and the link between U-Pb ages and metamorphism. Chem. Geol.; 2002; 184, pp. 123-138. [DOI: https://dx.doi.org/10.1016/S0009-2541(01)00355-2]

30. Tang, G.J.; Chung, S.L.; Wang, Q.; Wyman, D.A.; Dan, W.; Chen, H.Y.; Zhao, Z.H. Petrogenesis of a Late Carboniferous mafic dike-granitoid association in the western Tianshan: Response to the geodynamics of oceanic subduction. Lithos; 2014; 202–203, pp. 85-99. [DOI: https://dx.doi.org/10.1016/j.lithos.2014.04.010]

31. Yan, S.; Shan, Q.; Niu, H.C.; Yang, W.B.; Li, N.B.; Zeng, L.J.; Jiang, Y.H. Petrology and geochemistry of late Carboniferous hornblende gabbro from the Awulale Mountains, western Tianshan (NW China): Implication for an arc–nascent back-arc environment. J. Asian Earth Sci.; 2015; 113, pp. 218-237. [DOI: https://dx.doi.org/10.1016/j.jseaes.2015.01.016]

32. Sun, Q.; Zhao, X.; Xue, C.; Seltmann, R.; Symons, D.T. Late Carboniferous –Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting. Lithos; 2021; 400–401, 106417. [DOI: https://dx.doi.org/10.1016/j.lithos.2021.106417]

33. Sun, Q.; Zhao, X.; Xue, C.; Seltmann, R.; McClenaghan, S.H.; Chu, H.; Wang, M. Two episodes of Late Paleozoic mafic magmatism in the western Tianshan Orogen: From Carboniferous subduction to Permian post-collisional extension. Gondwana Res.; 2022; 109, pp. 518-535.

34. Seedorff, E.; Dilles, J.H.; Proffett, J.M., Jr.; Einaudi, M.T.; Zurcher, L.; Stavast, W.J.A.; Johnson, D.A.; Barton, M.D. Porphyry Deposits: Characteristics and Origin of Hypogene Features; Society of Economic Geologists: Littleton, CO, USA, 2005; pp. 251-298.

35. Sillitoe, R.H. Porphyry copper systems. Econ. Geol.; 2010; 105, pp. 3-41.

36. Luo, H. Geological, Geochemical Characteristics of the Nulasai Copper Deposit, Western Tian Shan, Xinjiang. Master’s Thesis; China University of Geosciences (Beijing): Beijing, China, 2016; 63p. (In Chinese with English Abstract)

37. Che, Z.C.; Liu, L.; Liu, H.F.; Luo, J.H. Review on the ancient Yili rift, Xinjiang, China. Acta Petrol. Sinica; 1996; 12, pp. 478-490. (In Chinese with English Abstract)

38. Gu, L.X.; Hu, S.X.; Yu, C.S.; Wu, C.Z.; Yan, Z.F. Initiation and evolution of the Bogda subduction-tore-type rift. Acta Petrologica Sinica; 2001; 17, pp. 585-597. (In Chinese with English Abstract)

39. Xia, L.Q.; Xu, X.Y.; Xia, Z.C.; Li, X.; Ma, Z.P.; Wang, L.S. Petrogenesis of Carboniferous rift-related volcanic rocks in the Tianshan, northwestern China. Geol. Soc Am. Bull.; 2004; 116, pp. 419-433.

40. An, F.; Zhu, Y.F.; Wei, S.N.; Lai, S.C. An Early Devonian to Early Carboniferous volcanic arc in North Tianshan, NW China: Geochronological and geochemical evidence from volcanic rocks. J. Asian Earth Sci.; 2013; 78, pp. 100-113.

41. Feng, W.; Zhu, Y. Petrogenesis and tectonic implications of the late Carboniferous calc-alkaline and shoshonitic magmatic rocks in the Awulale mountain, western Tianshan. Gondwana Res.; 2019; 76, pp. 44-61.

42. Gao, J.; Klemd, R. Formation of HP-LT rocks and their tectonic implications in the western Tianshan Orogen, NW China: Geochemical and age constraints. Lithos; 2003; 66, pp. 1-22.

43. 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, pp. 321-340.

44. Yang, W.B.; Niu, H.C.; Shan, Q.; Luo, Y.; Sun, W.D.; Li, C.Y.; Li, N.B.; Yu, X.Y. Late Paleozoic calc-alkaline to shoshonitic magmatism and its geodynamic implications, Yuximolegai area, western Tianshan, Xinjiang. Gondwana Res.; 2012; 22, pp. 325-340.

45. Wang, M.; Zhang, J.; Zhang, B.; Liu, K.; Chen, Y.; Zheng, Y. Geochronology and geochemistry of the Borohoro pluton in the northern Yili Block, NW China: Implication for the tectonic evolution of the northern West Tianshan orogen. J. Asian Earth Sci.; 2018; 153, pp. 154-169. [DOI: https://dx.doi.org/10.1016/j.jseaes.2017.03.024]

46. Zhu, Y.F.; Zhang, L.F.; Gu, L.B.; Guo, X.; Zhou, J. The zircon SHRIMP chronology and trace element geochemistry of the Carboniferous volcanic rocks in western Tianshan Mountains. Chin. Sci. Bull.; 2005; 50, pp. 2201-2212. [DOI: https://dx.doi.org/10.1007/BF03182672]

47. Zhu, Y.F.; Guo, X.; Song, B.; Zhang, L.F.; Gu, L. Petrology, Sr-Nd-Hf isotopic geochemistry and zircon chronology of the Late Palaeozoic volcanic rocks in the southwestern Tianshan Mountains, Xinjiang, NW China. J. Geol. Soc.; 2009; 166, pp. 1085-1099. [DOI: https://dx.doi.org/10.1144/0016-76492008-130]

48. Xiong, X.L.; Zhao, Z.H.; Bai, Z.H.; Mei, H.J.; Xu, J.F.; Wang, Q. Origin of Awulale adakitic sodium-rich rocks in western Tianshan: Constraints for Nd and Sr isotopic compositions. Acta Petrol. Sinica; 2001; 17, pp. 514-522.

49. Zhao, Z.H.; Guo, Z.J.; Han, B.F.; Wang, Y. The geochemical characteristics and tectonic-magmatic implications of the latest-Paleozoic volcanic rocks from Santanghu basin, eastern Xinjiang, northwest China. Acta Petrol. Sinica; 2006; 22, pp. 199-214.

50. Zhao, Z.; Xiong, X.; Wang, Q.; Bai, Z.; Qiao, Y. Late Paleozoic underplating in North Xinjiang: Evidence from shoshonites and adakites. Gondwana Res.; 2009; 16, pp. 216-226. [DOI: https://dx.doi.org/10.1016/j.gr.2009.03.001]

51. Cao, R.; Bagas, L.; Chen, B.; Wang, Z.; Gao, Y. Geochronology and petrogenesis of the composite Zuluhong Granite, North Xinjiang Province of China: Implications for the crust-mantle interaction and continental crustal growth in Western Tianshan Orogen. Lithos; 2021; 380–381, 105837. [DOI: https://dx.doi.org/10.1016/j.lithos.2020.105837]

52. Chen, J.; Zhou, T.; Xie, Z.; Zhang, X.; Guo, X. Formation of positive 1 Nd(T) granitoids from the Alataw Mountains, Xinjiang, China, by mixing and fractional crystallization: Implication for Phanerozoic crustal growth. Tectonophysics; 2000; 328, pp. 53-67. [DOI: https://dx.doi.org/10.1016/S0040-1951(00)00177-3]

53. Feng, W.; Zheng, J.; Shen, P. Petrology, mineralogy, and geochemistry of the Carboniferous Katbasu Au-Cu deposit, western Tianshan, Northwest China: Implications for petrogenesis, ore genesis, and tectonic setting. Ore Geol. Rev.; 2023; 161, 105659. [DOI: https://dx.doi.org/10.1016/j.oregeorev.2023.105659]

54. Han, B.; Wang, S.; Jahn, B.; Hong, D.; Kagami, H.; Sun, Y. Depleted-mantle source for the Ulungur River A-type granites from North Xinjiang, China: Geochemistry and Nd–Sr isotopic evidence, and implications for Phanerozoic crustal growth. Chem. Geol.; 1997; 138, pp. 135-159. [DOI: https://dx.doi.org/10.1016/S0009-2541(97)00003-X]

55. Jahn, B.M.; Wu, F.Y.; Hong, D.W. Important crustal growth in the Phanerozoic: Isotopic evidence of granitoids from east-central Asia. Acad. Proc. Earth Planet. Sci.; 2000; 109, pp. 5-20. [DOI: https://dx.doi.org/10.1007/BF02719146]

56. Hu, A.Q.; Jahn, B.M.; Zhang, G.X.; Zhang, Q.F. Crustal evolution and Phanerozoic crustal growth in northern Xinjiang: Nd–Sr isotopic evidence. Part I: Isotopic characterisation of basement rock. Tectonophysics; 2000; 328, pp. 15-51.

57. Jahn, B.M.; Windley, B.; Natal’in, B.; Dobretsov, N. Phanerozoic continental growth in Central Asia. J. Asian Earth Sci.; 2004; 23, pp. 599-603.

58. Sengör, 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, pp. 298-307.

59. Kröner, A.; Kovach, V.; Belousova, E.; Hegner, E.; Armstrong, R.; Dolgopolova, A.; Seltmann, R.; Alexeiev, D.V.; Hoffmann, J.E.; Wong, J. . Reassessment of continental growth during the accretionary history of the Central Asian Orogenic Belt. Gondwana Res.; 2014; 25, pp. 103-125. [DOI: https://dx.doi.org/10.1016/j.gr.2012.12.023]

60. Hou, Z.; Yang, Z.; Qu, X.; Meng, X.; Li, Z.; Beaudoin, G.; Rui, Z.; Gao, Y.; Zaw, K. The Miocene Gangdese porphyry copper belt generated during post-collisional extension in the Tibetan Orogen. Ore Geol. Rev.; 2009; 36, pp. 25-51. [DOI: https://dx.doi.org/10.1016/j.oregeorev.2008.09.006]

61. Hou, Z.Q.; Yang, Z.M.; Lu, Y.J.; Kemp, A.; Zheng, Y.C.; Li, Q.Y.; Tang, J.X.; Yang, Z.S.; Duan, L.F. A genetic linkage between subduction-continental collision-related porphyry Cu deposits in Tibet. Geology; 2015; 43, pp. 247-250.

62. Richards, J.P. Magmatic to hydrothermal metal fluxes in convergent and collided margins. Ore Geol. Rev.; 2011; 40, pp. 1-26. [DOI: https://dx.doi.org/10.1016/j.oregeorev.2011.05.006]

63. Liu, R.; Wang, L.X.; Chen, G.W. Genesis, geological significance and metallogentic potentiality of A-type granites in the Awulale area of the western Tianshan, Xinjiang. Acta Petrol. Sinica; 2017; 33, pp. 1741-1751. (In Chinese with English Abstract)

64. Zhao, Z.H.; Xiong, X.L.; Wang, Q.; Bai, Z.H.; Mei, H.J. A case study on porphyry Cu deposit related with adakitic quartz albite porphyry in Mosizaote, Western Tianshan, Xinjiang, China. Acta Petrol. Sinica; 2004; 20, pp. 249-258. (In Chinese with English Abstract)

65. Li, N.B.; Niu, H.C.; Shan, Q.; Yang, W.B. Two episodes of Late Paleozoic A-type magmatism in the Qunjisayi area, western Tianshan: Petrogenesis and tectonic implications. J. Asian Earth Sci.; 2015; 113, pp. 238-253. [DOI: https://dx.doi.org/10.1016/j.jseaes.2014.12.015]

66. Cooke, D.R.; Hollings, P.; Walshe, J.L. Giant porphyry deposits: Characteristics, distribution, and tectonic Controls. Econ. Geol.; 2005; 100, pp. 801-818. [DOI: https://dx.doi.org/10.2113/gsecongeo.100.5.801]

67. Candela, P.A.; Piccoli, P.M. Magmatic Processes in the Development of Porphyry-Type Ore Systems; Society of Economic Geologists: Littleton, CO, USA, 2005; pp. 25-37.