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Juvenile source nature of the North Tianshan turbidites and its tectonic implication

Published online by Cambridge University Press:  22 October 2024

Meng Wang Open the ORCID record for Meng Wang [Opens in a new window] ,
Ming Cao ,
Da Xu ,
Youxin Chen ,
Jinjiang Zhang ,
Bo Zhang ,
Xianzhi Pei ,
Zuochen Li ,
Hai Zhou  and
Zhian Bao
Meng Wang*
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi’an, China
Ming Cao
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Da Xu
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Youxin Chen
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Jinjiang Zhang
Affiliation:
Key Laboratory of Orogenic belts and Crustal Evolution, MOE, School of Earth and Space Sciences, Peking University, Beijing, China
Bo Zhang
Affiliation:
Key Laboratory of Orogenic belts and Crustal Evolution, MOE, School of Earth and Space Sciences, Peking University, Beijing, China
Xianzhi Pei
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Zuochen Li
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Hai Zhou
Affiliation:
Key Laboratory of Western Mineral Resources and Geological Engineering, MOE, School of Earth Science and Resources, Chang’an University, Xi’an, China
Zhian Bao
Affiliation:
State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi’an, China
*
Corresponding author: Meng Wang; Emails: [email protected]; [email protected]
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Abstract

Sediments within accretionary complexes, preserving key information on crust growth history of Central Asian Orogenic Belt, did not get enough attention previously. Here, we conduct comprehensive geochemical study on the turbidites from the North Tianshan Accretionary Complex (NTAC) in the Chinese West Tianshan orogen, which is a good example of sediments derived from juvenile materials. The turbidites, composed of sandstone, siltstone, and argillaceous siliceous rocks, are mainly Carboniferous. All the investigated samples have relatively low Chemical Index of Alteration values (35–63) and Plagioclase Index of Alteration values (34–68), indicating relatively weak weathering before erosion and deposition. The sandstone and siltstone, and slate samples display high Index of Compositional Variability values of 0.89–1.50 and 0.89–0.93, suggesting a relatively immature source. The sandstones and siltstones were mainly derived from intermediate igneous rocks, and the slates from felsic igneous rocks, formed in oceanic/continental arc settings. The investigated samples roughly display high positive εNd(t) values (mainly at +5.5 to +7.9, except one spot at +0.8), with corresponding Nd model ages at 672 Ma–522 Ma (except one at ∼1.1 Ga). Combined with the previous studies, we suggest that the turbidites in the NTAC were mainly derived from intermediate to felsic igneous rocks with juvenile arc signature, and thus the northern Chinese West Tianshan is a typical site with significant Phanerozoic crust growth.

Keywords

Turbiditesaccretionary complexgeochemistryCentral Asian Orogenic Beltcrustal growth
Type
Original Article
Information
Geological Magazine , Volume 161 , 2024 , e10
Creative Commons
Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (https://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
© The Author(s), 2024. Published by Cambridge University Press

1. Introduction

The Central Asian Orogenic Belt (CAOB), surrounded by the Siberia, Baltica, Tarim, and North China cratons, is a collage of microcontinents, oceanic-island arcs, seamounts, oceanic plateaus and accretionary complexes over ca. 800 million years (Sengör et al. Reference Şengör, Natal’in and Burtman1993; Jahn et al. Reference Jahn, Windley, Natal’in and Dobretsov2004; Kröner et al. Reference Kröner, Kovach, Belousova, Hegner, Armstrong, Dolgopolova, Seltmann, Alexeiev, Hofmann, Wong, Sun, Cai, Wang, Tong, Wilde, Degtyarev and Rytsk2014). It has been widely accepted that the CAOB, with the largest area of crustal growth in the Phanerozoic, is one of the largest accretionary orogens on Earth (Sengör et al. Reference Şengör, Natal’in and Burtman1993; Jahn et al. Reference Jahn, Wu and Chen2000, Reference Jahn, Windley, Natal’in and Dobretsov2004; Windley et al. Reference Windley, AlexeIev, Xiao, Kröner and Badarch2007; Xiao et al. Reference Xiao, Windley, Allen and Han2013; Safonova, Reference Safonova2017). The identification of many intro-oceanic arcs, accretionary complexes, oceanic plate strata, and MORB-OIB derived blueschist belts within the CAOB, and positive Nd-Hf isotope character of magmatic rocks are key evidence for its juvenile character (Jahn et al. Reference Jahn, Wu and Chen2000, Reference Jahn, Windley, Natal’in and Dobretsov2004; Safonova, Reference Safonova2017). However, some researchers stated that the volume of truly juvenile crustal material in the CAOB has been overestimated (Kröner et al. Reference Kröner, Kovach, Belousova, Hegner, Armstrong, Dolgopolova, Seltmann, Alexeiev, Hofmann, Wong, Sun, Cai, Wang, Tong, Wilde, Degtyarev and Rytsk2014, Reference Kröner, Kovach, Alexeiev, Wang, Wong, Degtyarev and Kozakov2017). One reason is that there are many microcontinents with Precambrian basement in the CAOB (Kröner et al. Reference Kröner, Kovach, Belousova, Hegner, Armstrong, Dolgopolova, Seltmann, Alexeiev, Hofmann, Wong, Sun, Cai, Wang, Tong, Wilde, Degtyarev and Rytsk2014; Long & Huang, Reference Long and Huang2017). Even in juvenile crustal regions such as the Chinese Altai, ancient crustal materials were identified (Xu et al. Reference Xu, Li, Jiang, Li, Qu, Yang, Zhou and Dong2015; Zhang et al. Reference Zhang, Wang, Tong, Zhang, Song, Zhang, Huang, Guo and Hou2017), and the Hf-in-zircon isotope data reveal recycled crust (Kröner et al. Reference Kröner, Kovach, Alexeiev, Wang, Wong, Degtyarev and Kozakov2017). Another reason might be whether the intra-oceanic arcs were correctly recognized (Kröner et al. Reference Kröner, Kovach, Alexeiev, Wang, Wong, Degtyarev and Kozakov2017). Therefore, the proportion of juvenile and recycled crust for crust growth during the late-stage evolution of the CAOB is still an open question.

Pacific-type convergent margins are major sits of continental growth and crustal recycling. The proportions of juvenile and recycled crust are generally estimated by the amount and geochemical signature of granitoids in the supra-subduction zone. However, the underestimation of crust growth caused by erosion of magmatic rocks during geological processes is generally ignored. These eroded materials were transported and deposited in the trench and adjacent for-arc and back-arc basins, forming characteristic clastic sedimentary rocks in accretionary complexes (Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a) These clastic rocks are compositionally similar to their source rocks and contain detrital zircons, recording crystallization ages and source characters information of their parental igneous rocks. If sediments were derived mainly from eroded intra-arc crust, then they can be regarded as contribution of continental growth. Therefore, the study of sediment recycling might be important in evaluating the proportion of continental growth. Despite a few recent studies (Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a, Reference Safonova, Perfilova, Obut, Kotler, Aoki, Komiya, Wang and Sunb), accretionary complexes, as major component of the CAOB, lack detailed study especially on assessing CAOB late-stage crustal growth.

The Chinese West Tianshan Orogen is located in the southwest part of the CAOB (Fig. 1a). The northern part of the Chinese West Tianshan Orogen is composed of late Paleozoic accretionary complex, including flysch type volcano-sedimentary rocks and some ophiolite fragments, in response to evolution of the North Tianshan Ocean. Previous studies mainly focus on the petrology, geochronology and geochemistry of the ophiolites (Xiao et al. Reference Xiao, Tang, Feng, Zhu, Li and Zhao1992; Xu et al. Reference Xu, Xia, Ma, Wang, Xia, Li and Wang2006a, Reference Xu, Li, Ma, Xia, Xia and Pengb; Li et al. Reference Li, Xiao, Han, Zhou, Zhang and Zhang2015; Feng & Zhu, Reference Feng and Zhu2018; Zheng et al. Reference Zheng, Zhong, Wang, Yang, Kapsiotis, Xiao and Wan2019), but studies on the sedimentary rocks are weak. Recently, our group reported detrital zircon U-Pb geochronology and Lu-Hf isotope characteristics of the turbidites, suggesting significant Carboniferous magmatism and continental growth (Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a). In this paper, we present whole rock geochemistry and Sr-Nd isotope for the turbidites in the North Tianshan Accretionary Complex (NTAC) (Fig. 2) to further constrain their provenance and tectonic setting of their parental igneous rocks and evaluate their contribution for continental growth.

Figure 1. (a) Tectonic framework of the Central Asian Orogenic Belt (modified after Şengör et al. Reference Şengör, Natal’in and Burtman1993 and Xiao et al. Reference Xiao, Windley, Allen and Han2013). (b) Geological map of the Chinese West Tianshan Orogen and adjacent regions (modified after Gao et al. Reference Gao, Long, Klemd, Qian, Liu, Xiong, Su, Liu, Wang and Yang2009). Numbers in circle refer to the tectonic boundaries: 1) North Tianshan Suture Zone; 2) Nikolaev line-North Nalati Suture Zone; 3) Southern Central Tianshan Suture Zone; and 4) North Tarim Thrust. Abbreviations for the tectonic unites are: NTAC = North Tianshan Accretionary Complex; YB = Yili Block; CTB = Central Tianshan Block; STB = South Tianshan Belt.

2. Geological background

The CAOB, also known as the modified Altaids, occupies an immense area in central Asia (Fig. 1a). The Tianshan orogenic belt, presently extending for more than 2500 km from west to east through Uzbekistan, via Tajikistan, Uzbekistan, and Kyrgyzstan to northwestern China, is an important constituent part of the CAOB. The Chinese Tianshan can be subdivided into the Western Tianshan and East Tianshan, which are different both in topography and evolutionary history, roughly along the longitude ∼90°E (Xiao et al. Reference Xiao, Windley, Allen and Han2013). The Chinese West Tianshan Orogen can be further subdivided into the North Tianshan Accretionary Complex (NTAC), the Yili Block (YB), the Central Tianshan Block, and the South Tianshan Belt, which are separated by the North Tianshan, North Narat, and South Tianshan faults (Fig. 1b).

The YB is a triangular shaped micro-continent which mainly Neoproterozoic basement rocks and extends over 1000 km across NW China, Kazakhstan, and Kyrgyzstan (Wang et al. Reference Wang, Faure, Cluzel, Shu, Charvet, Meffre and Ma2006). The center of the YB is covered by Cenozoic sediments. The basement rocks are exposed in the northern and southern side of the YB. Ordovican to Silurian intrusive rocks which might be related to the early stage subduction of the NTSO, are found in the Wenquan area of the northwestern YB (Wang et al. Reference Wang, Jahn, Shu, Li, Chung and Liu2012; Huang et al. Reference Huang, Long, Kröner, Yuan, Wang, Sun, Zhao and Wang2013). Late Paleozoic volcano-sedimentary rocks and intrusive rocks are widely distributed in both sides of the block and were suggested to be related to the subduction of the North Tianshan and South Tianshan oceans (Wang et al. Reference Wang, Zhang, Ren, Pei, Zhang, Chen, Li and Ge2022 and references therein).

The Central Tianshan Block is a strip-like arc terrane with Precambrian basement (Gao et al. Reference Gao, Long, Klemd, Qian, Liu, Xiong, Su, Liu, Wang and Yang2009). It approximately corresponds to the Narat Range in the west and extend from the Baluntai area to Xingxingxia area in the east. The basement rocks are mainly Meso- to Neo-proterozoic schists, paragneiss, and granitic gneisses (Hu et al. Reference Hu, Wei, Jahn, Zhang, Deng and Chen2010; Wang et al. Reference Wang, Liu, Shu, Jahn, Chung, Zhai and Liu2014; Gao et al. Reference Gao, Wang, Klemd, Jiang, Qian, Mu and Ma2015; Huang et al. Reference Huang, Cawood, Ni, Hou, Shi and Hu2017). Paleozoic volcanic and intrusive rocks are widely exposed and were formed due to subduction and closure of the Terskey and South Tianshan oceans (Xu et al. Reference Xu, Wang, Li, Chen, Ma, Zhu, Wang and Dong2013; Wang et al. Reference Wang, Zhang, Zhang, Liu and Ge2016a, Reference Wang, Zhang, Ren, Pei, Zhang, Chen, Li and Ge2022; Zhong et al. Reference Zhong, Wang, Alexeiev, Cao, Biske, Liu, Zhai and Xing2017).

The South Tianshan Belt is a wide tectonic unit bounded by the southern Central Tianshan Fault and the northern Tairm Fault (Xiao et al. Reference Xiao, Windley, Allen and Han2013). It was formed as a result of the consumption of the South Tianshan ocean and subsequent collision between the Tarim Craton and Yili-Central Tianshan Block (Charvet et al. Reference Charvet, Shu, Laurent-Charvet, Wang, Faure, Cluzel, Chen and De Jong2011; Xiao et al. Reference Xiao, Windley, Allen and Han2013; Wang et al. Reference Wang, Zhai, Kapp, de Jong, Zhong, Liu, Ma, Gong and Geng2018b; Huang et al. Reference Huang, Wang, Tong, Qin, Ma and Yin2020). The South Tianshan Belt is composed of Cambrian to Carboniferous limestone, siliciclastic turbidites, cherts, and interlayered volcanics (Jiang et al. Reference Jiang, Gao, Klemd, Qian, Zhang, Xiong, Wang, Tan and Chen2014). Permian unconformably overlie the former strata (Wang et al. Reference Wang, Liu, Shu, Jahn, Chung, Zhai and Liu2014). Several ophiolite fragments with ages ranging from 590 to 320 Ma have been identified within the South Tianshan Belt (Jiang et al. Reference Jiang, Gao, Klemd, Qian, Zhang, Xiong, Wang, Tan and Chen2014; Wang et al. Reference Wang, Shu, Faure, Jahn, Cluzel, Charvet, Chung and Meffre2011, Reference Wang, Zhai, Kapp, de Jong, Zhong, Liu, Ma, Gong and Geng2018b and references therein). Ophiolites that experienced high pressure metamorphism were also reported in the Akeyazi, NW China (Gao et al. Reference Gao, He and Li1995), and Atbashi, Kyrgyzstan (Hegner et al. Reference Hegner, Klemd, Kröner, Corsini, Alexeiev, Iaccheri, Zack, Dulski, Xia and Windley2010).

The NTAC located between the Junggar terrane and the YB, extends over 300 km along the northern margin of the North Tianshan. It consists mainly of two of two different lithologies: 1) the ophiolitic remnants (Wang et al. Reference Wang, Faure, Cluzel, Shu, Charvet, Meffre and Ma2006; Xu et al. Reference Xu, Xia, Ma, Wang, Xia, Li and Wang2006a; Han et al. Reference Han, Guo, Zhang, Zheng, Chen and Song2010) and 2) the Carboniferous volcano-sedimentary rocks which were regarded as turbidites (Wang et al. Reference Wang, Faure, Cluzel, Shu, Charvet, Meffre and Ma2006). The ophiolites exposed discontinuously over an area of ∼250 km in length and 5–15 km in width (Fig. 1(b)), and the Bayingou ophiolite is one of the best outcrops (Xu et al. Reference Xu, Xia, Ma, Wang, Xia, Li and Wang2006a). Famennian-Visean conodonts and radiolarians had been found from the cherts within the NTAC (Xiao et al. Reference Xiao, Tang, Feng, Zhu, Li and Zhao1992). Gabbro and plagiogranite from the Bayingou ophiolite have SHRIMP U-Pb age of 344 Ma and 325 Ma (Xu et al. Reference Xu, Xia, Ma, Wang, Xia, Li and Wang2006a, b). Plagiogranite from the Kuitun River section were dated at 343 Ma (Li et al. Reference Li, Xiao, Han, Zhou, Zhang and Zhang2015). Layered and massive gabbros in the Jinghe ophiolite were dated to be 381 and 382 Ma (Zheng et al. Reference Zheng, Zhong, Wang, Yang, Kapsiotis, Xiao and Wan2019). There exist several different perspectives about the nature of the North Tianshan ophiolites, i.e. 1) remnant of a ‘Red Sea type’ oceanic basin (Xia et al. Reference Xia, Xu, Xia, Li, Ma and Wang2004; Xu et al. Reference Xu, Xia, Ma, Wang, Xia, Li and Wang2006a, b), 2) remnants of a long-lived wide ocean (Yang et al. Reference Yang, Li, Kerr and Tong2018), 3) products related to ridge subduction (Li et al. Reference Li, Xiao, Han, Zhou, Zhang and Zhang2015), and 4) ophiolite formed in forearc setting (Feng & Zhu, Reference Feng and Zhu2018).

The turbiditic sequence in the NTAC consist mainly of tuffaceous sandstone, siltstone, tuff, and black argillite alternations (Fig. 3). The tuffaceous sandstone ranges in thickness from a few centimeters to 50 centimeters, but mostly around 10–40 cm (Fig. 3a, b). Some deep-water ichnofossils, like Chondrites sp., Cosmorphaphe sp., Helminthopsis sp. et al., and deep-water microfossils were found in the turbidites (Jin et al. Reference Jin, Li and Li1989), indicating in a bathyal to deep-sea environment (Wang et al. Reference Wang, Faure, Cluzel, Shu, Charvet, Meffre and Ma2006). The turbiditic sequence near the North Tianshan Fault underwent low-grade metamorphism and display a subvertical slaty cleavage (Figs. 2 and 3c), and some siltstones had turned out to be andalusite schists (Wang et al. Reference Wang, Faure, Cluzel, Shu, Charvet, Meffre and Ma2006). Age of the turbidites were constrained to be Devonian to Carboniferous based on fossils discovered in the chert and limestone (XBGMR, 1993). However, our recent study shows that the turbidites have the youngest DZ ages of 312–303 Ma, constraining the maximum depositional time of the turbidites to the late Carboniferous (Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a; Bai et al. Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020).

Figure 2. Geological map of the study area (modified from XBGMR, 1993), showing sample locations. The sample locations for detrital zircon U-Pb dating are from Wang et al. (Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a).

Figure 3. Representative outcrop (a, b; from Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a) and microphotographs (c, d) of the turbidites from the NTAC.

Volcanic rocks, represented by the Arbasay Formation, also exist within the NTAC. The Arbasay Formation, which is mainly composed of volcanic rocks in the lower part and volcaniclastic rocks in the upper part, exposes to the north of the Bayingou ophiolite (Wang et al. Reference Wang, Zhang, Zhang, Liu and Ge2016a). The Arbasay Formation was previously regarded as early Permian in age, because it unconformably overlies the upper Carboniferous Qianxia Formation and is covered by the upper Permian Quanzijie Formation (XBGMR, 1993). However, zircons from the volcanic rocks and tuff of the Arbasay Formation were dated at 315–305 Ma, indicating a Late Carboniferous age (Liu et al. Reference Liu, Cheng, Guo, Jolivet and Song2015; Wang et al. Reference Wang, Wu, Li, Zhu, Chen, Li, Wu, Deng and Chen2017; Bai et al. Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020). The volcanic rocks from the Arbasay Formation include basalt, andesite, dacite, and rhyolite, dominated by andesites (Liu et al. Reference Liu, Cheng, Guo, Jolivet and Song2015; Bai et al. Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020). The volcanic rocks display arc-like geochemical signatures, indicating that they are subduction related and might have formed during the tectonic transition from compression to extension (Wang et al., Reference Wang, Wu, Li, Zhu, Chen, Li, Wu, Deng and Chen2017; Bai et al. Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020).

3. Sampling and analytical methods

Fifteen clastic rock samples, mainly fine-grained sandstones and siltstones, and 4 slate samples were collected from the NTAC for geochemical studies. We also selected 6 sandstones to determine their Rb-Sr and Sm-Nd isotope compositions. The detailed sampling locations are illustrated in Fig. 2. Representative petrographic characteristics of the studied samples are shown in Fig. 3c-d.

Whole-rock major and trace element analyses were conducted at the SKLCD, Norwest University, China. The rock samples were first crushed into small fragment and cleaned in distilled water, dried, and then ground into powder. Major elements were determined by XRF method, while trace and rare earth elements were analyzed using an ICP-MS (PE 6100 DRC). Analytical precision and accuracy are better than 5% for major elements, 2%for most trace elements and 10% for transition metals. Detailed procedures and working conditions are described in Dong et al. (Reference Dong, Zhang, Neubauer, Liu, Hauzenberger, Zhou and Li2011).

The Rb-Sr and Sm-Nd isotopes of the samples were analyzed at the Wuhan SampleSolution Analytical Technology Co., Ltd., Wuhan, China. All chemical preparations were performed on class 100 work benches within a class 1000 over-pressured clean laboratory. Whole rock Sr-Nd isotope analyses were performed on a Neptune Plus MC-ICP-MS (Thermo Fisher Scientific, Dreieich, Germany). Analyses of the NIST SRM 987 standard solution yielded 87Sr/86Sr ratio of 0.710243 ± 4 (2 SD, n = 7), which is the same with published value of0.710241±12within error (Zhang et al. Reference Zhang, Hu and Liu2020). The USGS reference materials BCR-2 (basalt) and RGM-2 (rhyolite) yielded 87Sr/86Sr ratios of 0.704990 ± 6 and 0.703960 ± 6, respectively, consistent with the published values (Zhang et al. Reference Zhang, Hu and Liu2020; Li et al. Reference Li, Li, Li, Guo and Yang2012). Analyses of the GSB 04-3258-2015 standard yielded 143Nd /144Nd ratio of 0.512441 ±2 (2SD, n = 7), which is identical within error to the published values (0.512439 ± 10 (2SD), Li et al. Reference Li, Tang, Zhu and Pan2017). In addition, the USGS reference materials BCR-2 (basalt) and RGM-2 (rhyolite) yielded 143Nd/144Nd ratios of 0.512644 ± 7 and 0.512802 ± 6, respectively, which are within error to their published values (Zhang et al. Reference Zhang, Hu and Liu2020).

4. Analytical results

4.a. Major element

Analytical results of whole-rock major and trace elements are listed in Table 1. The sandstone/siltstones display a wide range of SiO2 contents varying from 49.73 wt %–71.25 wt %, but mostly lower than 65 wt % (average 60.28 wt %), which are below or slightly higher than that of average upper continental crust (UCC; 66.6 wt %) (Taylor et al. Reference Taylor, McLennan, Armstrong and Tarney1981) and post-Archaean Australian shales (PAAS; 62.4 wt %) (Taylor and McLennan, Reference Taylor and McLennan1985). They also have variable Na2O (2.30–5.58 wt %) and K2O (0.52–4.85), with Na2O/K2O ratios between 0.6 and 9.2. The samples have high Fe2O3T (av. 5.31 wt %), Al2O3(av. 16.05 wt %) and MgO (av. 2.15 wt %) contents, suggesting a more mafic to intermediate source. The slates show higher SiO2 contents of 66.78 wt %–73.21 wt %, higher than those in UCC and PAAS. They also have lower Fe2O3T (av. 3.57 wt %), MgO (1.44 wt %), and Al2O3 (av. 13.56 wt %) than the sandstones, suggesting more quartz and less mafic minerals in the source of the slates. Although the sandstones and the slates have different major element compositions, they all plot in the greywacke field in the rock type discrimination diagram (Fig. 4). The Na2O/Al2O3 ratios of 0.17–0.36 for the studied samples are also typical of greywackes. Negative correlations can be observed for all the samples between SiO2 and TiO2, Al2O3, Fe2O3, and MgO (Figures not shown), indicating weak major element fractionation during sedimentation, i.e., they are first cycle sediments (Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a).

Table 1. Whole rock geochemical composition of the Carboniferous turbidites in the NTAC

Note: CIA=[Al2O3/(Al2O3+CaO*+Na2O+K2O)]×100 and PIA=[(Al2O3–K2O)/(Al2O3+CaO*+Na2O–K2O)]×100, where CaO* represents Ca in silicate-bearing minerals only and all in molecular proportions; ICV= (Fe2O3+K2O+Na2O+CaO+MgO+TiO2)/Al2O3.

Table 2. Sr-Nd isotopic composition of the Carboniferous turbidites in the NTAC

Unit of model age ( ${\rm{T}}_{{\rm{DM}}}^1$ and ${\rm{T}}_{{\rm{DM}}}^2$ ) is Ma.

εNd(t)=[(143Nd/144Nd)S/(143Nd/144Nd)CHUR-1]×10,000.

${\rm{T}}_{{\rm{DM}}}^1$ =1/λSm×ln{[(143Nd/144Nd)S-0.51315]/[(147Sm/144Nd)S-0.2137]}.

${\rm{T}}_{{\rm{DM}}}^2$ = ${\rm{T}}_{{\rm{DM}}}^1$ -( ${\rm{T}}_{{\rm{DM}}}^1$ -t)×[(fCC-fS)/ (fCC-fDM)].

where S= sample, (143Nd/144Nd)CHUR=0.512638 and (147Sm/144Nd)CHUR=0.1967. The fCC, fS and fDM are fSm/Nd values of the continental crust, the sample and the depleted mantle, respectively.

Figure 4. Geochemical classification diagram of the turbidites in the NTAC (after Herron, Reference Herron1988).

4.b. Trace and rare earth element

Most of the studied samples have lower rare earth and other incompatible element concentrations than PAAS (Fig. 5). Most of the sandstone/siltstone samples have low rare earth element (REE) contents of from 60 ppm to 99 ppm, except for one sample TS17-70 which has total REE values of 133 ppm. The slates have relatively higher ΣREE values of 110 ppm–121 ppm, with one exception (TS17-44) of 76 ppm. Both the sandstone/siltstone and slate samples display are enriched in LREE and depleted in HREE (Fig. 5c, d), with (La/Yb)N ratios of 2.09–6.58 and 4.88–7.00, respectively (Table 1). Most sandstone/siltstone samples display weak positive Eu anomalies ((Eu/Eu*) = 1.01–1.3), and two samples show weak negative Eu anomalies ((Eu/Eu*) = 0.98 and 0.88), similar to that of the Late Carboniferous basaltic rocks in the NTAC (Fig. 5c). In comparison, the slate samples have moderate negative Eu anomalies ((Eu/Eu*) = 0.77–0.87, with one exception of 1.02), which is a feature of intermediate to felsic magmatic rocks that undergone fractional crystallization of plagioclase.

Figure 5. Chondrite-normalized REE patterns and upper crust-normalized spider diagrams for the Paleozoic graywackes. Symbols are the same as in Fig. 4. Chondrite and PM normalizing values are from Sun and McDonough (Reference Sun and McDonough1989) and upper crust-normalizing data are from Taylor and McLennan (Reference Taylor and McLennan1985). Geochemical data for volcanic rocks in the NTAC are from Liu et al. (Reference Liu, Guo, Zhang and Wu2012), Wang et al. (Reference Wang, Wu, Li, Zhu, Chen, Li, Wu, Deng and Chen2017) and Bai et al. (Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020).

In the primitive mantle normalized multielement spectra (Fig. 5a, b), all the samples show clear Nb depletion compared to La (Nb/Lapm = 0.2-0.8) and Th (Nb/Thpm = 0.1-0.2), suggesting their derivation from supra-subduction/arc volcanic rocks (Briqueu et al. Reference Briqueu, Bougault and Joron1984; Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a)

4.c. Sr-Nd isotope

We conducted Rb-Sr and Sm-Nd isotope analyses for six sandstone samples from the NTAC. The samples display 147Sm/144Nd ratios between 0.129367 and 0.163533, and 143Nd/144Nd ratios between 0.512543 and 0.512975 (Table 2). Most samples have high positive εNd(t) values (+5.5 to +7.9), with only one exception(εNd(t) = +0.8) (Fig. 6), and the TDM2 values are mainly from 0.63 to 0.45 Ga (with one exception at ∼1.0 Ga) (Table 2).

Figure 6. εNd(t) versus age diagram for the Paleozoic igneous rocks and sediments in the northern Chinese West Tianshan. Nd isotopic Data for the igneous rocks can be found in Supplementary Table S1.

5. Discussion

5.a. Influence of chemical weathering and recycling

The geochemical compositions of clastic rocks are dominated controlled by, and thus can used to constrain weathering conditions and recycling of, their source rocks (Nesbitt and Young, Reference Nesbitt and Young1984; Mclennan et al. Reference McLennan, Hemming, Mcdaniel and Hanson1993; Fedo et al. Reference Fedo, Nesbitt and Young1995). Some parameters, such as the chemical index of alteration (CIA), the plagioclase index of alteration (PIA), and index of compositional variability (ICV), are frequently used to quantify the degree of chemical weathering and composition maturity of the source rocks (Nesbitt and Young, Reference Nesbitt and Young1984; Cox & Lowe, Reference Cox and Lowe1995).

The CIA values of the sandstone/siltstone samples are 35–56 (average 52) and slate samples are 56–63 (average 59). However, the CIA values could be influenced by potassium metasomatism during diagenesis, so it is necessary to use the A-CN-K triangle diagram to identify it and make corrections. In the A-CN-K diagram (Fig. 7a), the sandstone/siltstone samples define a weathering trend line that does not parrel to the A-CN line, and reflect potassium metasomatism. The point of intersection between the weathering trend line and the Pl-Kfs line is near the plot of the tonalite (Fig. 7a). This means that the average composition of the source rocks is equal to intermediate rocks. The corrected initial CIA values of the sandstones and siltstones were slightly higher than the calculated CIA, but still lower than 60 (Fig. 7a). The slates plot near the granite field with limited weathering towards illite (Fig. 7a), reflecting a dominate felsic rock source. The corrected CIA values of the sandstone/siltstones are close to the CIA values of NASC and Archean greywacke sandstones (58; Condie, Reference Condie1993), but much lower than that of PAAS (70; Taylor and McLennan, Reference Taylor and McLennan1985). This suggests that the source rocks of the turbidites experienced low to moderate weathering before erosion and deposition. In addition, the PIA values of sandstone/siltstone (34–67, average 51) and slate samples (58–68, average 63) are both lower than that of the PAAS (Fedo et al. Reference Fedo, Nesbitt and Young1995), also indicating a relatively low degree of chemical weathering.

Figure 7. Discrimination diagrams illustrating weathering and sediment recycling. (a) Th/Sc versus Zr/Sc diagram (after McLennan et al. Reference McLennan, Hemming, Mcdaniel and Hanson1993); (b) A-CN-K diagram (after Fedo et al. Reference Fedo, Nesbitt and Young1995), Data for basalt (Ba) tonalite (To), granodiorite (Gd), granite (Gr), and average post-Archean upper crust are from Condie (Reference Condie1993) and Nesbitt and Young (Reference Nesbitt and Young1984); (c) Th/U versus Th (after McLennan et al. Reference McLennan, Hemming, Mcdaniel and Hanson1993); (d) ICV versus CIA diagram (after Nesbitt and Young, Reference Nesbitt and Young1984).

The ICV values are used to reflect the maturity of the source rocks of clastic rocks (Cox & Lowe, Reference Cox and Lowe1995). Sedimentary rocks which were derived from a source dominated by clay minerals generally have low ICV values, while those sourced from an immature source with high percentage of nonclay minerals commonly possess high IVC values (Van de & Leake, Reference Van de and Leake1985). Both the sandstone/siltstone and slate samples display high ICV values of 0.89–1.50 and 0.89–0.93 (Fig. 7b), higher than the PAAS, suggesting a relatively immature source. In the Th/Sc–Zr/Sc plot (Fig. 7c), the samples show a trend of compositional variation instead of sedimentary recycling. The sandstone/siltstone samples have Th/U ratios lower than that of the UCC (3.8; Taylor and McLennan, Reference Taylor and McLennan1985), while the slate samples have higher Th/U ratios than the UCC (Fig. 7d), suggesting that the sandstones/siltstones were derived from source rocks with less weathering than that of the slates.

The SiO2/Al2O3 ratio is also an index for sedimentary maturity because quartz has stronger weathering resistance than feldspars, mafic minerals, and lithic grains (Roser et al. Reference Roser, Cooper, Nathan and Tulloch1996; Zhang, Reference Zhang2004). The average values range from ∼3.0 to ∼5.0 for unaltered basic and felsic igneous rocks, while values >5.0–6.0 in sediments are an indication of progressive maturity (Zhang, Reference Zhang2004). The sandstone/siltstones have SiO2/Al2O3 ratios of 3.3–5.5, indicating low degree and sorting and deposition close to sources. The slates have slightly higher SiO2/Al2O3 ratios of 4.4–5.8, suggesting possibly stronger weathering.

To conclude, the turbidites from the NTAC were first cycle sediments and derived from immature materials with low degree of chemical weathering. The slates might contain hither contents of materials which experience slightly stronger weathering than the sandstone/siltstone samples.

5.b. Source rocks and tectonic setting

The turbidites from the NTAC are characterized by large proportions of angular volcanic lithic fragments and immature geochemical signatures, suggesting that they were derived from a nearby magmatic arc. The sandstone/siltstone samples have more mafic to andesitic volcanic clasts than the slates, indicating a more mafic source. This is consistent with the geochemical data. Geochemical characteristics of sedimentary rocks derived from different source rocks have been studied for a long time (Bhatia and Taylor, Reference Bhatia and Taylor1981; Bhatia and Crook, Reference Bhatia and Crook1986; McLennan and Taylor, Reference McLennan and Taylor1991; Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a, b). According to the source rock discrimination diagrams using major elements (Fig. 8a), the sandstone/siltstone from the NTAC were mainly derived from intermediate and felsic igneous rocks, while the slates were mainly from felsic igneous rocks and quartz-rich sedimentary rocks. In the La/Th versus Hf diagram (Fig. 8b), most sandstone/siltstone samples plot in the mixed felsic/basic source area, while the slates plot in the acid arc source area. Potassium and Rb are relatively mobile elements during low grade metamorphism and diagenesis, but their covariant relation is generally considered as a standard for determining the source rocks of clastic rocks (Floyd et al. Reference Floyd, Winchester and Park1989). Although the samples from the NTAC show a wide range of K/Rb ratios, their high Rb and K2O contents indicate the derivation from acidic to intermediate igneous rocks (Fig. 8c). Some trace element ratios, such as Th/Sc, Co/Th, La/Sc, and Ti/Zr are also good indicators for provenance study, as silicic rocks trends to have more contents of Th and Zr, whereas basic rocks hold more contents of Sc, Co, and Ti (Cullers, Reference Cullers1994). Th/Sc and Zr/Sc ratios increase with supply of felsic detritus, whereas Ti/Zr and Co/Th ratios decrease. Most of the sandstone/siltstones have higher Ti/Zr ratios (12.4–83.3, av. = 39.5) compared to the UCC (19.9), indicating dominantly basic-intermediate igneous rocks in the source area. In comparation, the slates exhibit relatively low Ti/Zr ratios (15.6–35.1, av. = 20.2), suggesting a dominantly felsic igneous source. In the Co/Th versus La/Sc diagrams (Fig. 8d), the sandstone/siltstone samples plot in a mixing source from basalt to andesite and felsic volcanic rocks. As a contrast, the slates mainly distribute around the felsic rocks (Fig. 8d). These features indicate a provenance of basaltic to felsic rocks for the sandstone/siltstones and mainly felsic rocks for the slates.

Figure 8. Source rock discrimination diagrams. (a) discriminant function diagram using major elements after Roser and Korsch (Reference Roser and Korsch1988); (b) La/Th versus Hf diagram (after Floyd and Leveridge, Reference Floyd and Leveridge1987); (c) K2O versus Rb diagram (after Folyd et al. Reference Floyd, Winchester and Park1989); (d) Co/Th versus La/Sc diagram (after Gu et al. Reference Gu, Liu, Zheng, Tang and Qi2002).

The major and trace element compositions of sediments are also widely used to constrain the tectonic setting of their source rocks (Bhatia and Taylor, Reference Bhatia and Taylor1981; Roser and Korsch, Reference Roser and Korsch1986; Bhatia and Crook, Reference Bhatia and Crook1986). Generally, sandstones sourced from oceanic island arcs the have higher Fe2O3T+MgO, Al2O3, and TiO2, and lower SiO2, K2O/Na2O, and Al2O3/(Na2O+CaO) than those sourced from passive margins (Bhatia, Reference Bhatia1983). In the K2O/Na2O versus Fe2O3T+MgO, Al2O3/(Na2O+CaO) versus Fe2O3T+MgO, TiO2 versus Fe2O3T+MgO, and Al2O3/SiO2 versus Fe2O3T+MgO diagrams (Fig. 9a-d), the sandstone/siltstones all plot within or near the oceanic island arc and continental island arc fields, while the slates mainly distribute within or around the active continental margin field. When plotting on the Df1 versus Df2 diagram which considers the role of multiple variables (Fig. 9e), it shows that the sandstone/siltstones illustrate an oceanic island and active continental margin setting, while the slates reflect an active continental margin setting. In the (Fe2O3T + MgO)/(SiO2 + Na2O + K2O) versus Al2O3/SiO2 diagram (Fig. 9f), most of the sandstone/siltstone samples fall within the immature island arc (IIA) field and evolved island arc (EIA) field, while the slates mainly fall within the mature magmatic arc (MMA) field. Similar results are observed in the tectonic setting discrimination diagrams using trace elements (Fig. 10).

Figure 9. Tectonic setting discrimination diagrams using major elements for turbidites in the NTAC (after Bhatia, Reference Bhatia1983; Kumon and Kiminami, Reference Kumon and Kiminami1994). (a) K2O/Na2O versus (Fe2O3+ MgO) diagram; (b) Al2O3/(Na2O + CaO) versus (Fe2O3+ MgO) diagram; (c) TiO2 versus (Fe2O3+ MgO) diagram; (d) Al2O3/SiO2 versus (Fe2O3+ MgO) diagram; (e) Df1 versus Df2 diagram; (f) Al2O3/SiO2 versus (Fe2O3+ MgO)/(SiO2+ Na2O + K2O) diagram. The discriminant functions are: Df1 = −0.0447 × SiO2 − 0.972 × TiO2 + 0.008 × Al2O3- 0.267 × Fe2O3 + 0.208 × FeO − 3.082 × MnO + 0.14 + MgO + 0.195 × CaO + 0.719 × Na2O − 0.032 × K2O + 7.510 × P2O5 + 0.303; Df2 = −0.421 × SiO2 + 1.988 × TiO2 − 0.526 × Al2O3 − 0.551 × Fe2O3 − 1.61 × FeO + 2.72 × MnO + 0.881 × MgO − 0.907 × CaO − 0.177 × Na2O − 1.84 × K2O + 7.244 × P2O5 + 43.57. Abbreviations for tectonic settings: A, oceanic island arc; B, continental arc; C, active continental margin; D, passive continental margin; IIA, immature island arc; EIA, evolved island arc; MMA, mature magmatic arc.

Figure 10. Tectonic setting discrimination diagrams using trace elements for turbidites in the NTAC (after Bhatia and Crook, Reference Bhatia and Crook1986). (a) Ti/Zr versus La/Sc diagram; (b) La/Y versus Sc/Cr; (c) Th-Sc-Zr/10 diagram; (d) Th-Co-Zr/10 diagram; (e) La-Th-Sc diagram. Abbreviations for tectonic settings are the same as in Fig. 9.

In the northern YB and the NTAC, there are massive Paleozoic volcanic and intrusive rocks which exhibit distinguishable Nd isotope characteristics (Fig. 6). The sandstone/siltstone samples have comparable Sr-Nd isotope compositions with the Late Paleozoic mafic igneous rocks in the northern YB and Carboniferous volcanic rocks in the NTAC (Fig. 6). If they were mainly sourced from the northern YB, their source rocks were supposed to contain the felsic volcanic rocks as these rocks make up a larger proportion in the northern YB (Fig. 1b). This is inconsistent with the above suggestion that the source rocks of the sandstone/siltstones are mainly basic-intermediate igneous rocks. In addition, the U-Pb ages of the turbidites are unimodal with major peaks at 323 Ma (Fig. 11a; Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a). It is completely different from the detrital zircon age spectrum of Early Carboniferous sandstone just to the south of the North Tianshan Fault, which contain many Early Paleozoic and Precambrian detrital zircons (Wang et al. Reference Wang, Zhang, Pei, Zhang, Chen, Xiao and Zheng2018c). What is more, the sandstone/siltstones from the NTAC have depleted whole-rock Nd isotope and detrital zircon Hf isotope composition (Fig. 6 and Fig. 11b), indicating a juvenile mantle source for their parental rocks, which might be part of an intra-oceanic arc. These features indicate the sandstone/siltstone were sourced from a Carboniferous intra-oceanic arc and deposited in a fore-arc/trench. The source rocks of the slate are more felsic and might be part of a continental arc. Therefore, the turbidites from the NTAC were likely deposited between an intra-oceanic arc (the North Tianshan arc) and a continental arc (the northern YB).

Figure 11. (a) Relative probability plot for detrital zircons from turbidites in the NTAC (after Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a); (b) Plot of εHf(t) versus U-Pb age for detrital zircons from turbidites in the NTAC (after Wang et al. Reference Wang, Zhang, Pei, Liu, Zhang and Chen2018a).

5.c. Implication for crustal growth in the CAOB

Juvenile continental growth can be recorded by trondhjemite-granodiorite (TTG) and mafic magmatism at supra-subduciton zone and intra-plate settings (Safonova, Reference Safonova2017). However, the oceanic crust was mostly subducted into deep mantle and the intra-oceanic arcs could have been eroded or buried deeply in the lower crust, which might lead to the underestimation of proportion of juvenile crust. Turbidites and greywackes deposited at convergent margin are sourced from upper crust of the adjacent plates and thus recorded the nature of these upper crust rocks. If these sediments were sourced from the juvenile materials, then it represents continental growth (Kröner et al. Reference Kröner, Kovach, Alexeiev, Wang, Wong, Degtyarev and Kozakov2017). Recent geochemical, detrital zircon geochronological and Hf-Nd isotopic studies on sandstones from central and eastern Kazakhstan had implied several pre-existed intra-oceanic arcs (Safonova et al. Reference Safonova, Perfilova, Savinskiy, Kotler, Sun and Wang2022a, b).

Though the outcrop is limited, the occurrence of Carboniferous arc type volcanic rocks in the NTAC, and juvenile source nature of the turbidites allow us to infer that there was a Late Devonian to Carboniferous intra-oceanic arc to the north of the YB, which was partly eroded and/or covered later. Here, we term this intra-oceanic arc as the North Tianshan arc, also mentioned by Bai et al. (Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020). However, the extent of the North Tianshan arc was unknown, maybe equivalently to the NTAC, because most of this arc was overlain by the Carboniferous turbidites. Another evidence for the arc nature of the NTAC basement is the magnetic anomaly data in the northern Xinjiang (He et al. Reference He, Li, Fan and Yang2013). To the east of Urumqi, the Bogda Range contains massive Carboniferous magmatic rocks with geochemical signatures of oceanic island arc and was called the Bogda arc (Xie et al. Reference Xie, Luo, Xu, Chen, Hong, Ma and Ma2016; Memtimin et al. Reference Memtimin, Pe-Piper, Piper, Guo and Zhang2020). According to the magnetic anomaly data, the Bogda arc is characterized by a medium–low magnetic anomaly, and this anomaly extends westward to the North Tianshan area (He et al. Reference He, Li, Fan and Yang2013). This similarity suggests that the basement of the NTAC (the North Tianshan arc) might be linked with the Bogda arc. The Late Carboniferous Arbasay Formation may represent limited outcrop of the North Tianshan arc (Bai et al. Reference Bai, Chen, Song, Xiao, Windley, Ao, Li and Xiang2020).

In summary, our study indicates the possibly pre-existence of a Devonian to Carboniferous intra-oceanic arc, i.e., the North Tianshan arc, to the north or the YB. This arc was then partly eroded and transferred to form the Carboniferous turbidites with overlain sequences. This study further proves the validity of using sedimentary record to reveal neglected juvenile crustal growth in accretionary orogens. The contribution of the eroded or covered intra-oceanic arc should be considered when calculating the net crustal growth in the CAOB.

6. Conclusions

  1. (1) The turbidites in the North Tianshan Accretionary Complex are mainly composed of sandstone, siltstone and slate, and belong to greywackes.

  2. (2) The sandstone and siltstone are characterized by immature geochemical features suggesting derivation from mafic to intermediate volcanic rocks, while the slates from a felsic magmatic source.

  3. (3) The sandstone and siltstone display high positive εNd(t) values (+5.5 to +7.9) with only one exception of +0.8, implying derivation from juvenile crust rocks. Combining with previous studies, we suggest that the basement of the North Tianshan might be a Devonian to Carboniferous intra-oceanic arc.

Supplementary material

To view supplementary material for this article, please visit https://doi.org/10.1017/S0016756824000207

Acknowledgements

This research was supported by the National Natural Science Foundation of China (42072267, 41602229), the West light Foundation of the Chinese Academy of Sciences (XAB2020YW03), the Natural Science Fountain of Shaan’xi Province, China (2023-JC-YB-237), Opening Foundation of State Key Laboratory of Continental Dynamics, Northwest University (19LCD06), and the Youth Innovation Team of Shaanxi Universities.

References

Bai, XY, Chen, YC, Song, DF, Xiao, WJ, Windley, BF, Ao, SJ, Li, L and Xiang, DF (2020). A new Carboniferous–Permian intra-oceanic subduction system in the North Tianshan (NW China): implications for multiple accretionary tectonics of the southern Altaids. Geological Journal 55, 2232–53.CrossRefGoogle Scholar
Bhatia, MR (1983) Plate-tectonics and geochemical composition of sandstones. Journal of Geology 91, 611–627.CrossRefGoogle Scholar
Bhatia, MR and Crook, KAW (1986) Trace element characteristics of graywackes and tectonic setting discrimination of sedimentary basins. Contributions to Mineralogy and Petrology 92, 181–193.CrossRefGoogle Scholar
Bhatia, MR and Taylor, SR (1981) Trace-element geochemistry and sedimentary provinces: a study from the Tasman geosyncline, Australia. Chemical Geology 33, 115–125.CrossRefGoogle Scholar
Briqueu, L, Bougault, H and Joron, JL (1984) Quantification of Nb, Ta, Ti and V anomalies in magmas associated with subduction zones: petrogenetic implications. Earth and Planetary Science Letters 68, 297–308.CrossRefGoogle Scholar
Charvet, J, Shu, LS, Laurent-Charvet, S, Wang, B, Faure, M, Cluzel, D, Chen, Y and De Jong, K (2011) Palaeozoic tectonic evolution of the Tianshan Belt, NW China. Science China: Earth Sciences 54, 166–184.CrossRefGoogle Scholar
Condie, KC (1993) Chemical composition and evolution of the upper continental crust: contrasting results from surface samples and shales. Chemical Geology 104, 1–37.CrossRefGoogle Scholar
Cox, R and Lowe, DR (1995) A conceptual review of regional-scale controls on the composition of clastic sediment and the co-evolution of continental blocks and their sedimentary cover. Journal of Sedimentary Research 1, 1–12.Google Scholar
Cullers, RL (1994) The chemical signature of source rocks in size fractions of Holocene stream sediment derived from metamorphic rocks in the Wet Mountains region, Colorado, U.S.A. Chemical Geology 113, 327–343.CrossRefGoogle Scholar
Dong, YP, Zhang, GW, Neubauer, F, Liu, XM, Hauzenberger, C, Zhou, DW and Li, W (2011) Syn- and post-collisional granitoids in the Central Tianshan orogen: geochemistry, geochronology and implications for tectonic evolution. Gondwana Research 20, 568–581.CrossRefGoogle Scholar
Fedo, CM, Nesbitt, HW and Young, GM (1995). Unraveling the effects of potassium metasomatism in sedimentary rocks and paleosoils, with implications for paleoweathering conditions and provenance. Geology 23, 921–924 2.3.CO;2>CrossRefGoogle Scholar
Feng, WY and Zhu, YF (2018) Petrology and geochemistry of mafic and ultramafic rocks in the north Tianshan ophiolite: implications for petrogenesis and tectonic setting. Lithos 318–319, 124–142.CrossRefGoogle Scholar
Floyd, PA and Leveridge, BE (1987) Tectonic environment of the Devonian Gramscatho basin, south Cornwall: framework mode and geochemical evidence from turbiditic sandstones. Journal of the Geological Society 144, 531–542.CrossRefGoogle Scholar
Floyd, PA, Winchester, JA and Park, RG (1989) Geochemistry and tectonic setting of Lewisian clastic metasediments from the Early Proterozoic Loch Maree Group of Gairloch, NW Scotland. Precambrian Research 45, 203–214.CrossRefGoogle Scholar
Gao, J, He, GQ and Li, MS (1995) The mineralogy, petrology, metamorphic PTDt trajectory and exhumation mechanism of blueschists, south Tianshan, northwestern China. Tectonophysics 250, 151–168.CrossRefGoogle Scholar
Gao, J, Long, LL, Klemd, R, Qian, Q, Liu, DY, Xiong, XM, Su, W, Liu, W, Wang, YT and Yang, FQ (2009) Tectonic evolution of the South Tianshan Orogen and adjacent regions, NW China: geochemical and age constraints of granitoid rocks. International Journal of Earth Sciences 98, 1221–1238.CrossRefGoogle Scholar
Gao, J, Wang, XS, Klemd, R, Jiang, T, Qian, Q, Mu, LX and Ma, YZ (2015) Record of assembly and breakup of Rodinia in the Southwestern Altaids: evidence from Neoproterozoic magmatism in the Chinese Western Tianshan Orogen. Journal of Asian Earth Sciences 113, 173–193.CrossRefGoogle Scholar
Gu, XX, Liu, JM, Zheng, MH, Tang, JX and Qi, L (2002). Provenance and tectonic setting of the Proterozoic turbidites in Hunan, south China: geochemical evidence. Journal of Sedimentary Research 72, 393–407 CrossRefGoogle Scholar
Han, BF, Guo, ZJ, Zhang, ZC, Zheng, L, Chen, J and Song, B (2010) Age, geochemistry, and tectonic implications of a late Paleozoic stitching pluton in the North Tian Shan suture zone, western China. Geological Society of America Bulletin 122, 627–640.CrossRefGoogle Scholar
He, DF, Li, D, Fan, C and Yang, XF (2013) Geochronology, geochemistry and tectonostratigraphy of Carboniferous strata of the deepest well Moshen-1 in the Junggar Basin, Northwest China: insights into the continental growth of Central Asia. Gondwana Research 24, 560–577.CrossRefGoogle Scholar
Hegner, E, Klemd, R, Kröner, A, Corsini, M, Alexeiev, DV, Iaccheri, LM, Zack, T, Dulski, P, Xia, X and Windley, BF (2010) Mineral ages and P-T conditions of Late Paleozoic high-pressure eclogite and provenance of mélange sediments from Atbashi in the south Tianshan orogen of Kyrgyzstan. American Journal of Science 310, 916–950.CrossRefGoogle Scholar
Herron, MM (1988) Geochemical classification of terrigenous sands and shales from core or log data. Journal of Sedimentary Research 58, 820–829.Google Scholar
Hu, AQ, Wei, GJ, Jahn, BM, Zhang, JB, Deng, WF and Chen, LL (2010) Formation of the 0.9 Ga Neoproterozoic granitoids in the Tianshan Orogen, NW China: constraints from the SHRIMP zircon age determination and its tectonic significance. Geochimica 39, 197–212.Google Scholar
Huang, H, Cawood, PA, Ni, SJ, Hou, MC, Shi, ZQ and Hu, XL (2017) Provenance of late Paleozoic strata in the Yili Basin: implications for tectonic evolution of the south Tianshan orogenic belt. Geological Society of America Bulletin 130, 952–974.CrossRefGoogle Scholar
Huang, H, Wang, T, Tong, Y, Qin, Q, Ma, XX and Yin, JY (2020) Rejuvenation of ancient micro-continents during accretionary orogenesis: insights from the Yili Block and adjacent regions of the SW Central Asian Orogenic Belt. Earth Science Review 208, 103255.CrossRefGoogle Scholar
Huang, ZY, Long, XP, Kröner, A, Yuan, C, Wang, Q, Sun, M, Zhao, GC and Wang, YJ (2013) Geochemistry, zircon U-Pb ages and Lu-Hf isotopes of early Paleozoic plutons in the northwestern Chinese Tianshan: petrogenesis and geological implications. Lithos 182, 48–66.CrossRefGoogle Scholar
Jahn, BM., Windley, B, Natal’in, B and Dobretsov, N (2004) Phanerozoic continental growth in Central Asia. Journal of Asian Earth Sciences 23, 599–603.CrossRefGoogle Scholar
Jahn, BM, Wu, FY and Chen, B (2000) Granitoids of the Central Asian Orogenic Belt and continental growth in the Phanerozoic. Earth and Environmental Science Transactions of the Royal Society of Edinburgh 91, 181–193.CrossRefGoogle Scholar
Jiang, T, Gao, J, Klemd, R, Qian, Q, Zhang, X, Xiong, XM, Wang, XS, Tan, Z and Chen, BX (2014) Paleozoic ophiolitic mélanges from the South Tianshan Orogen, NW China: geological, geochemical and geochronological implications for the geodynamic setting. Tectonophysics 612–613, 106–127.CrossRefGoogle Scholar
Jin, HJ, Li, YC and Li, JY (1989) The flysch facies of Middle Carboniferous in the Northern Tianshan, Xinjiang. Acta Sedimentologica Sinica 7, 49–59.Google Scholar
Kröner, A, Kovach, V, Alexeiev, D, Wang, KL, Wong, J, Degtyarev, K and Kozakov, I (2017) No excessive crustal growth in the Central Asian Orogenic Belt: further evidence from field relationships and isotopic data. Gondwana Research 50, 135–166.CrossRefGoogle Scholar
Kröner, A, Kovach, V, Belousova, E, Hegner, E, Armstrong, R, Dolgopolova, A, Seltmann, R, Alexeiev, DV, Hofmann, JE, Wong, J, Sun, M, Cai, KD, Wang, T, Tong, Y, Wilde, SA, Degtyarev, KE and Rytsk, E (2014) Reassessment of continental growth during the accretionary history of the Central Asian Orogenic Belt. Gondwana Research 25, 103–125 CrossRefGoogle Scholar
Kumon, F and Kiminami, K (1994) Modal and chemical compositions of the representative sandstones from the Japanese Islands and their tectonic implications. In Proceedings of the 29th International Geological Congress: Part A, p. 135–151Google Scholar
Li, C, Xiao, WJ, Han, CM, Zhou, KF, Zhang, JE and Zhang, ZX (2015) Late Devonian–early Permian accretionary orogenesis along the North Tianshan in the southern Central Asian Orogenic Belt. International Geology Review 57, 1023–1050.CrossRefGoogle Scholar
Li, CF, Li, XH, Li, QL, Guo, JH and Yang, YH (2012). Rapid and precise determination of sr and nd isotopic ratios in geological samples from the same filament loading by thermal ionization mass spectrometry employing a single-step separation scheme. Analytica Chimica Acta, 727, 54–60.CrossRefGoogle ScholarPubMed
Li, J, Tang, SH, Zhu, XK and Pan, CX (2017). Production and Certification of the Reference Material GSB 04-3258-2015 as a 143Nd/144Nd Isotope Ratio Reference. Geostandards and Geoanalytical Research 41, 255–262.CrossRefGoogle Scholar
Liu, DD, Cheng, F, Guo, ZJ, Jolivet, M and Song, Y (2015) Lahar facies of the Latest Paleozoic Arbasay Formation: geomorphological characters and paleoenvironment reconstruction of Northern Tian Shan, NW China. Journal of Asian Earth Sciences 113, 282–292.CrossRefGoogle Scholar
Liu, DD, Guo, ZJ, Zhang, ZC and Wu, CD (2012) The Late Paleozoic tectonic relationship between the Tian Shan orogenic belt and Junggar basin: Constraints from zircon SHRIMP U-Pb dating and geochemistry characteristics of volcanic rocks in Arbasay Formation. Acta Petrologica Sinica 28, 2355–2368.Google Scholar
Long, XP and Huang, ZY (2017) Tectonic affinities of microcontinents in the Central Asian Orogenic Belt: a case study of the Chinese Tianshan Orogenic Belt. Bulletin of Mineralogy, Petrology and Geochemistry 36, 771–785.Google Scholar
McLennan, SM, Hemming, S, Mcdaniel, DK and Hanson, GN (1993) Geochemical approaches to sedimentation, provenance, and tectonics. Geological Society of America Bulletin 284, 21–40.Google Scholar
McLennan, SM and Taylor, SR (1991) Sedimentary-Rocks and Crustal Evolution: tectonic Setting and Secular Trends. Journal of Geology 99, 1–21.CrossRefGoogle Scholar
Memtimin, M, Pe-Piper, G, Piper, DJW, Guo, ZJ and Zhang, YY (2020) Carboniferous arc-related volcanism in SW Bogda Mountain, Northwest China, and its implications for regional tectonics. Lithos 360–361, 105413.CrossRefGoogle Scholar
Nesbitt, HW and Young, GM (1984) Prediction of some weathering trends of plutonic andvolcanic rocks based on thermodynamics and kinetic considerations. Geochimica et Cosmochimica Acta 48, 1523–1534.CrossRefGoogle Scholar
Roser, BP, Cooper, RA, Nathan, S and Tulloch, AJ (1996) Reconnaissance sandstone geochemistry, provenance, and tectonic setting of the lower Paleozoic terranes of the West Coast and Nelson, New Zealand. New Zealand Journal of Geology and Geophysics 39, 1–16.CrossRefGoogle Scholar
Roser, BP and Korsch, RJ (1986) Determination of Tectonic Setting of Sandstone-Mudstone Suites Using SiO2 Content and K2O/Na2O Ratio. Journal of Geology 94, 635–650.CrossRefGoogle Scholar
Roser, BP and Korsch, RJ (1988) Provenance signatures of sandstone-mudstone suite determined using discrimination function analysis of major-element data. Chemical Geology 67, 119–139.CrossRefGoogle Scholar
Safonova, I (2017) Juvenile versus recycled crust in the Central Asian Orogenic Belt: implications from ocean plate stratigraphy, blueschist belts and intra-oceanic arcs. Gondwana Research 47, 6–27.CrossRefGoogle Scholar
Safonova, I, Perfilova, A, Obut, O, Kotler, P, Aoki, S, Komiya, T, Wang, B and Sun, M (2022b) Traces of intra-oceanic arcs recorded in sandstones of eastern Kazakhstan: implications from U–Pb detrital zircon ages, geochemistry, and Nd–Hf isotopes. International Journal of Earth Sciences 111, 2449–2468.CrossRefGoogle Scholar
Safonova, I, Perfilova, A, Savinskiy, I, Kotler, P, Sun, M and Wang, B (2022a) Sandstones of the Itmurundy accretionary complex, central Kazakhstan, as archives of arc magmatism and subduction erosion: evidence from U-Pb zircon ages, geochemistry and Hf-Nd isotopes. Gondwana Research 111, 35–52.CrossRefGoogle Scholar
Şengör, AMC, Natal’in, BA and Burtman, US (1993) Evolution of the Altaid tectonic collage and Paleozoic crustal growth in Eurasia. Nature 364, 209–304.CrossRefGoogle Scholar
Sun, SS and McDonough, WF (1989) Chemical and isotopic systematics of oceanic Basalts: implications for mantle composition and processes. Geological Society, London Special Publications 42, 313–45CrossRefGoogle Scholar
Taylor, SR and McLennan, SM (1985) The Continental Crust: Its Composition and Evolution. Oxford, UK: Blackwell Scientific Publications, pp. 312 Google Scholar
Taylor, SR, McLennan, SM, Armstrong, RL and Tarney, J (1981) The composition and evolution of the continental crust: rare earth element evidence from sedimentary rocks. Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences 301, 381–399.Google Scholar
Van de, KPC and Leake, BE (1985) Petrography and geochemistry of feldspathic and mafic sediments of the northeastern Pacific margin. Earth and Environmental Science Transactions of The Royal Society of Edinburgh 76, 411–449.CrossRefGoogle Scholar
Wang, B, Faure, M, Cluzel, D, Shu, LS, Charvet, J, Meffre, S and Ma, Q (2006) Late Paleozoic tectonic evolution of the northern West Tianshan, NW China. Geodinamica Acta 19, 237–247.CrossRefGoogle Scholar
Wang, B, Jahn, BM, Shu, LS, Li, KS, Chung, SL and Liu, DY (2012) Middle-Late Ordovician arc-type plutonism in the NW Chinese Tianshan: implication for the accretion of the Kazakhstan continent in Central Asia. Journal of Asian Earth Sciences 49, 40–53.CrossRefGoogle Scholar
Wang, B, Liu, HS, Shu, LS, Jahn, BM, Chung, SL, Zhai, YZ and Liu, DY (2014) Early Neoproterozoic crustal evolution in northern Yili block: insights from migmatite, orthogneiss and leucogranite of the Wenquan metamorphic complex in the NW Chinese Tianshan. Precambrian Research 242, 58–81.CrossRefGoogle Scholar
Wang, B, Shu, LS, Faure, M, Jahn, BM, Cluzel, D, Charvet, J, Chung, SL and Meffre, S (2011) Paleozoic tectonics of the southern Chinese Tianshan: insights from structural, chronological and geochemical studies of the Heiyingshan ophiolitic mélange (NW China). Tectonophysics 497, 85–104 CrossRefGoogle Scholar
Wang, B, Zhai, YZ, Kapp, P, de Jong, K, Zhong, LL, Liu, HS, Ma, YZ, Gong, HJ and Geng, H (2018b) Accretionary tectonics of back-arc oceanic basins in the South Tianshan: insights from structural, geochronological, and geochemical studies of the Wuwamen ophiolite mélange. Geological Society of America Bulletin 130, 284–306.CrossRefGoogle Scholar
Wang, JL, Wu, CD, Li, Z, Zhu, W, Chen, YW, Li, QY, Wu, J, Deng, LJ and Chen, L (2017) Geochronology and geochemistry of volcanic rocks in the Arbasay Formation, Xinjiang Province (Northwest China): implications for the tectonic evolution of the North Tianshan. International Geology Review 59, 1324–1343.CrossRefGoogle Scholar
Wang, M, Zhang, B, Ren, R, Pei, XZ, Zhang, JJ, Chen, YX, Li, ZC and Ge, MH (2022) Tracing tectonic processes from oceanic subduction to continental collision through detrital zircon U-Pb and Lu-Hf isotope data: an example from the Chinese West Tianshan Orogen. Gondwana Research 105,185–200.CrossRefGoogle Scholar
Wang, M, Zhang, JJ, Pei, XZ, Liu, K, Zhang, B and Chen, YX (2018a) Significant Carboniferous magmatism and continental growth in the northern West Tianshan orogen, NW China: revealed by detrital zircon U-Pb and Lu-Hf analyses for turbidites from the North Tianshan Accretionary Complex. Journal of Geodynamics 118, 11–31.CrossRefGoogle Scholar
Wang, M, Zhang, JJ, Pei, XZ, Zhang, B, Chen, YX, Xiao, ZB and Zheng, YR (2018c) Detrital zircon U-Pb-Hf isotopes study of the Lower Carboniferous Anjihai Formation from the northern margin of the Yili Block, NW China. Geological Journal 53, 223–236.CrossRefGoogle Scholar
Wang, M, Zhang, JJ, Qi, GW and Liu, J (2014) Geochemistry and geochronology of Early Permian acid volcanic rocks along Kuqa River and its tectonic implication in the southern margin of South Tianshan Orogen, Xinjiang. Chinese Journal of Geology 49, 242–258.Google Scholar
Wang, M, Zhang, JJ, Zhang, B, Liu, K and Ge, MH (2016a) Bi-directional subduction of the South Tianshan Ocean during the Late Silurian: magmatic records from both the southern Central Tianshan Block and northern Tarim Craton. Journal of Asian Earth Sciences 128, 64–78.CrossRefGoogle Scholar
Windley, BF, AlexeIev, D, Xiao, WJ, Kröner, A and Badarch, G (2007) Tectonic models for accretion of the Central Asian Orogenic Belt. Journal of the Geological Society, London 164, 31–47.CrossRefGoogle Scholar
XBGMR (1993) Regional Geology of Xinjiang Uygur Autonomy Region. Beijing: Geological Publishing House.Google Scholar
Xia, LQ, Xu, XY, Xia, ZC, Li, XM, Ma, ZP and Wang, LS (2004) Petrogenesis of Carboniferous rift-related volcanic rocks in the Tianshan, northwestern China. Geological Society of America Bulletin 116, 419–433.CrossRefGoogle Scholar
Xiao, WJ, Windley, BF, Allen, MB and Han, CM (2013) Paleozoic multiple accretionary and collisional tectonics of the Chinese Tianshan orogenic collage. Gondwana Research 23, 1316–1341.CrossRefGoogle Scholar
Xiao, XC, Tang, YQ, Feng, YM, Zhu, BQ, Li, JY and Zhao, M (1992) Tectonic Evolution of the Northern Xinjiang and its Adjacent Regions. Beijing: Geological Publishing House, pp. 1–169.Google Scholar
Xie, W, Luo, ZY, Xu, YG, Chen, YB, Hong, LB, Ma, L and Ma, Q (2016) Petrogenesis and geochemistry of the late Carboniferous reararc (or back-arc) pillow basaltic lava in the Bogda Mountains, Chinese north Tianshan. Lithos 244, 30–42.CrossRefGoogle Scholar
Xu, XW, Li, XH, Jiang, N, Li, Q, Qu, X, Yang, YH, Zhou, G and Dong, LH (2015) Basement nature and origin of the Junggar terrane: new zircon U–Pb–Hf isotope evidence from Paleozoic rocks and their enclaves. Gondwana Research 28, 288–310 CrossRefGoogle Scholar
Xu, XY, Li, XM, Ma, ZP, Xia, LQ, Xia, ZC and Peng, SX (2006b) LA-ICPMS zircon U-Pb dating of gabbro from the Bayingou ophiolite in the Northern Tianshan Mountains. Acta Geologica Sinica 80, 1168–1176.Google Scholar
Xu, XY, Wang, HL, Li, P, Chen, JL, Ma, ZP, Zhu, T, Wang, N and Dong, YP (2013) Geochemistry and geochronology of Paleozoic intrusions in the Nalati (Narati) area in western Tianshan, Xinjiang, China: implications for Paleozoic tectonic evolution. Journal of Asian Earth Sciences 72, 33–62.CrossRefGoogle Scholar
Xu, XY, Xia, LQ, Ma, ZP, Wang, YB, Xia, ZC, Li, XM and Wang, LS (2006a) SHRIMP zircon U-Pb geochronology of the plagiogranite from Bayingou ophiolite in North Tianshan mountains and the petrogenesis of the ophiolite. Acta Petrologica Sinica 22, 83–94.Google Scholar
Yang, GX, Li, YJ, Kerr, AC and Tong, LL (2018) Accreted seamounts in North Tianshan, NW China: implication for the evolution of the Central Asian Orogenic Belt. Journal of Asian Earth Sciences 153, 223–237.CrossRefGoogle Scholar
Zhang, JJ, Wang, T, Tong, Y, Zhang, Z, Song, P, Zhang, L, Huang, H, Guo, L and Hou, Z (2017) Tracking deep ancient crustal components by xenocrystic/inherited zircons of Palaeozoic felsic igneous rocks from the Altai-East Junggar terrane and adjacent regions, western Central Asian Orogenic Belt and its tectonic significance. International Geology Review 59, 2021–2040 CrossRefGoogle Scholar
Zhang, KJ (2004) Secular geochemical variations of the Lower Cretaceous siliciclastic rocks from central Tibet (China) indicate a tectonic transition from continental collision to back-arc rifting. Earth and Planetary Science Letters 229, 73–89.CrossRefGoogle Scholar
Zhang, W, Hu, ZC and Liu, YS (2020) Iso-Compass: new freeware software for isotopic data reduction of LA-MC-ICP-MS. Journal of Analytical Atomic Spectrometry 35, 1087–1096.CrossRefGoogle Scholar
Zheng, H, Zhong, LF, Wang, R, Yang, LH, Kapsiotis, A, Xiao, Y and Wan, ZF (2019) Geochemistry and geochronology of mafic rocks from the Jinghe ophiolitic melange, northwest China: implications for plume-related magmatism and accretionary processes within the North Tianshan Ocean. Lithos 350, 105246.CrossRefGoogle Scholar
Zhong, LL, Wang, B, Alexeiev, DV, Cao, YC, Biske, Y., Liu, HS, Zhai, YZ and Xing, LZ (2017) Paleozoic multi-stage accretionary evolution of the SW Chinese Tianshan: new constraints from plutonic complex in the Nalati Range. Gondwana Research 45, 254–274.CrossRefGoogle Scholar
Figure 0

Figure 1. (a) Tectonic framework of the Central Asian Orogenic Belt (modified after Şengör et al.1993 and Xiao et al.2013). (b) Geological map of the Chinese West Tianshan Orogen and adjacent regions (modified after Gao et al.2009). Numbers in circle refer to the tectonic boundaries: 1) North Tianshan Suture Zone; 2) Nikolaev line-North Nalati Suture Zone; 3) Southern Central Tianshan Suture Zone; and 4) North Tarim Thrust. Abbreviations for the tectonic unites are: NTAC = North Tianshan Accretionary Complex; YB = Yili Block; CTB = Central Tianshan Block; STB = South Tianshan Belt.

Figure 1

Figure 2. Geological map of the study area (modified from XBGMR, 1993), showing sample locations. The sample locations for detrital zircon U-Pb dating are from Wang et al. (2018a).

Figure 2

Figure 3. Representative outcrop (a, b; from Wang et al.2018a) and microphotographs (c, d) of the turbidites from the NTAC.

Figure 3

Table 1. Whole rock geochemical composition of the Carboniferous turbidites in the NTAC

Figure 4

Table 2. Sr-Nd isotopic composition of the Carboniferous turbidites in the NTAC

Figure 5

Figure 4. Geochemical classification diagram of the turbidites in the NTAC (after Herron, 1988).

Figure 6

Figure 5. Chondrite-normalized REE patterns and upper crust-normalized spider diagrams for the Paleozoic graywackes. Symbols are the same as in Fig. 4. Chondrite and PM normalizing values are from Sun and McDonough (1989) and upper crust-normalizing data are from Taylor and McLennan (1985). Geochemical data for volcanic rocks in the NTAC are from Liu et al. (2012), Wang et al. (2017) and Bai et al. (2020).

Figure 7

Figure 6. εNd(t) versus age diagram for the Paleozoic igneous rocks and sediments in the northern Chinese West Tianshan. Nd isotopic Data for the igneous rocks can be found in Supplementary Table S1.

Figure 8

Figure 7. Discrimination diagrams illustrating weathering and sediment recycling. (a) Th/Sc versus Zr/Sc diagram (after McLennan et al.1993); (b) A-CN-K diagram (after Fedo et al.1995), Data for basalt (Ba) tonalite (To), granodiorite (Gd), granite (Gr), and average post-Archean upper crust are from Condie (1993) and Nesbitt and Young (1984); (c) Th/U versus Th (after McLennan et al.1993); (d) ICV versus CIA diagram (after Nesbitt and Young, 1984).

Figure 9

Figure 8. Source rock discrimination diagrams. (a) discriminant function diagram using major elements after Roser and Korsch (1988); (b) La/Th versus Hf diagram (after Floyd and Leveridge, 1987); (c) K2O versus Rb diagram (after Folyd et al.1989); (d) Co/Th versus La/Sc diagram (after Gu et al.2002).

Figure 10

Figure 9. Tectonic setting discrimination diagrams using major elements for turbidites in the NTAC (after Bhatia, 1983; Kumon and Kiminami, 1994). (a) K2O/Na2O versus (Fe2O3+ MgO) diagram; (b) Al2O3/(Na2O + CaO) versus (Fe2O3+ MgO) diagram; (c) TiO2 versus (Fe2O3+ MgO) diagram; (d) Al2O3/SiO2 versus (Fe2O3+ MgO) diagram; (e) Df1 versus Df2 diagram; (f) Al2O3/SiO2 versus (Fe2O3+ MgO)/(SiO2+ Na2O + K2O) diagram. The discriminant functions are: Df1 = −0.0447 × SiO2 − 0.972 × TiO2 + 0.008 × Al2O3- 0.267 × Fe2O3 + 0.208 × FeO − 3.082 × MnO + 0.14 + MgO + 0.195 × CaO + 0.719 × Na2O − 0.032 × K2O + 7.510 × P2O5 + 0.303; Df2 = −0.421 × SiO2 + 1.988 × TiO2 − 0.526 × Al2O3 − 0.551 × Fe2O3 − 1.61 × FeO + 2.72 × MnO + 0.881 × MgO − 0.907 × CaO − 0.177 × Na2O − 1.84 × K2O + 7.244 × P2O5 + 43.57. Abbreviations for tectonic settings: A, oceanic island arc; B, continental arc; C, active continental margin; D, passive continental margin; IIA, immature island arc; EIA, evolved island arc; MMA, mature magmatic arc.

Figure 11

Figure 10. Tectonic setting discrimination diagrams using trace elements for turbidites in the NTAC (after Bhatia and Crook, 1986). (a) Ti/Zr versus La/Sc diagram; (b) La/Y versus Sc/Cr; (c) Th-Sc-Zr/10 diagram; (d) Th-Co-Zr/10 diagram; (e) La-Th-Sc diagram. Abbreviations for tectonic settings are the same as in Fig. 9.

Figure 12

Figure 11. (a) Relative probability plot for detrital zircons from turbidites in the NTAC (after Wang et al.2018a); (b) Plot of εHf(t) versus U-Pb age for detrital zircons from turbidites in the NTAC (after Wang et al.2018a).

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