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Thermochronology quantifying exhumation history of the Wudang Complex in the South Qinling Orogenic Belt, central China

Published online by Cambridge University Press:  13 December 2016

CHUANBO SHEN ,
DI HU ,
CHUN SHAO  and
LIANFU MEI
CHUANBO SHEN*
Affiliation:
Key Laboratory of Tectonics and Petroleum Resources, China University of Geosciences, Ministry of Education, Wuhan 430074, China Faculty of Earth Resources, China University of Geosciences, Wuhan 430074, China
DI HU
Affiliation:
Key Laboratory of Tectonics and Petroleum Resources, China University of Geosciences, Ministry of Education, Wuhan 430074, China State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
CHUN SHAO
Affiliation:
Key Laboratory of Tectonics and Petroleum Resources, China University of Geosciences, Ministry of Education, Wuhan 430074, China
LIANFU MEI
Affiliation:
Key Laboratory of Tectonics and Petroleum Resources, China University of Geosciences, Ministry of Education, Wuhan 430074, China
*
†Author for correspondence: cugshen@126.com
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Abstract

The Wudang Complex located in the central part of South Qinling, has been inferred to be a segment of the Yangtze Craton involved in the orogen. In this study, the cooling/exhumation history of the Wudang Complex is revealed through combined published geochronology data and new apatite fission-track results. Three rapid exhumation episodes related to relevant geodynamic events have been identified. Previous 40Ar–39Ar and (U–Th)/He data indicate that the most significant exhumation, induced by the collision between the North and South China Blocks, occurred from c. 237 to 220 Ma after long-term subsidence and sedimentation of the passive continental margin. The second exhumation event, related to the long-distance effect of the Pacific subduction, occurred during the period from c. 126 to 90 Ma. Following the late Cretaceous – Eocene peneplanation stage, the final late Cenozoic exhumation since c. 15 Ma may be attributed to the combined effect of the eastward growth of the Tibetan Plateau uplift and the Asian monsoon.

Keywords

thermochronologyfission trackcooling/exhumationtectonic evolutionQinling Orogen

Information

Type
Original Articles
Information
Geological Magazine , Volume 155 , Issue 4 , May 2018 , pp. 893 - 906
Copyright
Copyright © Cambridge University Press 2016 

1. Introduction

The Central China Orogenic Belt (CCOB), comprising from west to east the Kunlun, Qilian and Qinling–Dabie Mountains, is a critical zone that separates the northern and southern China continent (Ames, Gaozhi & Baocheng, Reference Ames, Gaozhi and Baocheng1996; Rowley et al. Reference Rowley, Xue, Tucker, Peng, Baker and Davis1997; Hacker et al. Reference Hacker, Ratschbacher, Webb, Ireland, Walker and Dong1998; Xiong et al. Reference Xiong, Ma, Jiang and Zhang2016). As part of the CCOB, the Qinling–Dabie Orogenic Belt (QDOB), which is a collision product of the North China Craton (NCC) and South China Block (SCB), provides important information about the tectonic evolution of the Eastern Asian Continent (Mattauer et al. Reference Mattauer, Matte, Malavieille, Tapponnier, Maluski, Qin, Lun and Qin1985; Şengör, Reference Şengör1985; Ames, Gaozhi & Baocheng, Reference Ames, Gaozhi and Baocheng1996; Rowley et al. Reference Rowley, Xue, Tucker, Peng, Baker and Davis1997; Hacker et al. Reference Hacker, Ratschbacher, Webb, Ireland, Walker and Dong1998; Ratschbacher et al. Reference Ratschbacher, Hacker, Webb, McWilliams, Ireland, Dong, Calvert, Chateigner and Wenk2000; Hu et al. Reference Hu, Kohn, Raza, Wang and Gleadow2006a ; Dong et al. Reference Dong, Genser, Neubauer, Zhang, Liu, Yang and Heberer2011a ; Zhao et al. Reference Zhao, Jiang, Dai, Ma and Li2015; Dong & Santosh, Reference Dong and Santosh2016; Wu, Xiao & Ma, Reference Wu, Xiao and Ma2016). Most previous studies focus on two aspects: (1) the continental deep subduction and exhumation process through the ultrahigh-pressure (UHP) metamorphic belt (Ames, Gaozhi & Baocheng, Reference Ames, Gaozhi and Baocheng1996; Hacker et al. Reference Hacker, Ratschbacher, Webb, McWilliams, Ireland, Calvert, Dong, Wenk and Chateigner2000; Faure et al. Reference Faure, Lin, Monié, Breton, Poussineau, Panis and Deloule2003; Hu et al. Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b; Bader et al. Reference Bader, Franz, Ratschbacher, Capitani, Webb, Yang, Pfänder, Hofmann and Linnemann2013a , Reference Bader, Ratschbacher, Franz, Yang, Hofmann, Linnemann and Yuan2013 b); and (2) the dynamic mechanism of the Triassic collision between the NCC and SCB (Kröner, Zhang & Sun, Reference Kröner, Zhang and Sun1993; Li et al. Reference Li, Xiao, Liou, Chen, Ge, Zhang, Sun, Cong, Zhang and Hart1993; Okay, Şengör & Satir, Reference Okay, Şengör and Satir1993; Ratschbacher et al. Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006; Dong et al. Reference Dong, Liu, Zhang, Chen, Zhang, Li and Yang2012). Earlier studies have generally revealed the geological evolution history of the South Qinling and its affiliation with the break-up of the supercontinent Rodinia (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008, Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010; Bader et al. Reference Bader, Franz, Ratschbacher, Capitani, Webb, Yang, Pfänder, Hofmann and Linnemann2013a ; Yang et al. Reference Yang, Ratschbacher, Jonckheere, Enkelmann, Dong, Shen, Wiesinger and Zhang2013). However, issues including the post-collision evolution process and the timing and amount of exhumation processes are still not clear. Moreover, there is still controversy about the geodynamics of tectonic reactivation and topographic adjustment after the Cretaceous. These scenarios comprise (1) back-arc extension triggered by the subduction of the Pacific plate (Zhou & Li, Reference Zhou and Li2000; Wu et al. Reference Wu, Lin, Wilde, Zhang and Yang2005; Li & Li, Reference Li and Li2007; Li et al. Reference Li, Li, Wang, Li, Liu, Tang, Gao and Wu2010); (2) a far-field effect of the India–Eurasia collision (Tapponnier et al. Reference Tapponnier, Zhiqin, Roger, Meyer, Arnaud, Wittlinger and Jingsui2001; Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Ratschbacher et al. Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006; Grave, Buslov & Haute, Reference Grave, Buslov and Haute2007; Grave et al. Reference Grave, Glorie, Buslov, Stockli, Mcwilliams, Batalev and Haute2013); and (3) the changing erosion rate, affected by climate since the Miocene (An et al. Reference An, Kutzbach, Prell and Porter2001; Guo et al. Reference Guo, Ruddiman, Hao, Wu, Qiao, Zhu, Peng, Wei, Yuan and Liu2002; Clift et al. Reference Clift, Hodges, Heslop, Hannigan, Long and Calves2008; Allen & Armstrong, Reference Allen and Armstrong2012).

In this study, we integrate previous geochronology data and our new apatite fission-track (AFT) ages of the Wudang Complex to reconstruct regional thermal history (from break-up, sedimentation, collision, reactivation and cooling to exhumation). These results will help us (1) understand the tectonic–thermal events and related cooling/exhumation processes, and (2) address questions pertinent to the role of Pacific subduction and India–Asia collision in the tectonics of the Yangtze Craton.

2. Geological setting

The Qinling–Dabie Orogenic Belt (QDOB) is a ~2000 km long E–W elongated intra-continental orogeny, connected respectively with Kunlun and Qilian orogeny to the west and eastern China to the east through the Tanlu fault belt (Fig. 1a). The QDOB developed by the collision between the NCC and SCB in the Triassic. Controlled by the palaeo-Pacific subduction since the Cretaceous and the far-field effects of the India–Asia collision at ~50 Ma (Tapponnier et al. Reference Tapponnier, Zhiqin, Roger, Meyer, Arnaud, Wittlinger and Jingsui2001; Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Sharp & Clague, Reference Sharp and Clague2006), the QDOB showed intra-continental reactivation throughout the Jurassic to Cenozoic (e.g. Zhang, Vergely & Mercier, Reference Zhang, Vergely and Mercier1995; Ratschbacher et al. Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003; Dong et al. Reference Dong, Genser, Neubauer, Zhang, Liu, Yang and Heberer2011a ; Dong & Santosh, Reference Dong and Santosh2016).

Figure 1.

(a) Location of the Qinling–Dabie Orogenic Belt (QDOB), between the North China Craton and Yangtze Craton. (b) Relationships between the Wudang Terrain and adjacent tectonic units (modified from Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010). (c) Simplified geological map of the Wudang area modified from Yue, Deng & Bagas (Reference Yue, Deng and Bagas2014) and sample locations. F1: Shiyan fault. (d) Sketch map of tectonic profiles A–B.

The South Qinling is located between the North Qinling and the northern margin of the SCB (Fig. 1b; Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010; Dong & Santosh, Reference Dong and Santosh2016). The Wudang terrain is located in the eastern margin of the South Qinling and the western margin of the Nanyang basin that divided the Qinling and Dabie orogenic belt. The Wudang Complex mainly consists of the Neoproterozoic Wudang Group that is unconformity surrounded by the early Neoproterozoic Yaolinghe Group and the Sinian to Phanerozoic sedimentary units (Fig. 2; Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008; Yue, Deng & Bagas, Reference Yue, Deng and Bagas2014).

Figure 2.

Stratigraphic columns of the Wudang Complex and its adjacent areas (modified from Dong & Santosh, Reference Dong and Santosh2016). No vertical scale.

The Wudang Group is the largest Precambrian suite (~8000 km2) in the South Qinling and comprises metamorphic volcanic–sedimentary assemblages in greenschist facies, which is subdivided into the Yaoping, Yangping and Shuangtai Formations. This volcanic event may be attributed to the rift-setting according to their bimodal composition (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008, Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010; Xia et al. Reference Xia, Xia, Xiang-Min, Zhong-Ping and Xue-Yi2008; Li et al. Reference Li, Li, Wang, Li, Liu, Tang, Gao and Wu2010). Their geochemical features also suggest this volcanic suite is subduction-related magmatism. Zircon U–Pb dating on the basic volcanic rocks for metarhyolite tuff indicates it formed at ~755 Ma (Table 1; Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008), and the laser ablation inductively coupled mass spectrometry (LA-ICP-MS) U–Pb zircon age of meta-acidic volcanic rocks was 668–680 Ma (Y. Zhang et al. Reference Zhang, Miao, Zhang, Lu, Zhang, Chen, Li, Miao, Feng and Ou2013). The youngest detrital zircon U–Pb age (763 ± 33 Ma) of Shuangtai Formations indicates the timing of the Wudangshan volcanism (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008, Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010). The 40Ar–39Ar ages for hornblende and muscovite are 236.6 ± 0.6 and 231.1 ± 0.9 Ma respectively (Ratschbacher et al. Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003), which likely corresponds to the peak metamorphism timing. The Yaolinghe Group contains greenschist facies metamorphosed quartz–keratophyre tuff and pebbly tuff (Zhang et al. Reference Zhang, Zhang, Tang and Wang2002) and its basaltic volcanisms were dated at c. 685 Ma with minor acidic volcanic rocks at c. 632 Ma (Cai et al. Reference Cai, Xiong, Hong, Dekuang, Sun and Rao2007; Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008). The widespread doleritic–gabbroic mafic sills emplaced into the Wudang and Yaolinghe Group dated at 679.0 ± 3.1 Ma (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008).

Table 1.

Compilation of isotopic ages in the Wudang area

Note: TIMS: thermal ionization mass spectrometry.

3. Samples and methodology

Seven epimetamorphic sandstone samples were collected from the Wudang Group metamorphic rocks. Sample locations are shown in Figure 1c and elevations are determined by GPS (Table 2). The apatite fractions were separated from the rocks using conventional density and magnetic separation techniques after crushing and sieving. The apatites are divided into two separates, one used for age dating (age group) and the other for confined track-length measurements (length group) (Jonckheere, Ratschbacher & Wagner, Reference Jonckheere, Ratschbacher and Wagner2003; Jonckheere et al. Reference Jonckheere, Enkelmann, Min, Trautmann and Ratschbacher2007). All samples were selected for age dating (age group), and five of them (W1, W3, W5, W6 and WD2A) were used for confined track-length measurements. Apatite grains were mounted in epoxy resin, ground, and polished to expose smooth flat internal surfaces. The fission-track analysis was performed at Bergakademie Freiberg following the methods detailed in Shen et al. (Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012) and Yang et al. (Reference Yang, Ratschbacher, Jonckheere, Enkelmann, Dong, Shen, Wiesinger and Zhang2013).

Table 2.

Results of fission-track analysis of apatite from the Wudang Complex

Note: Grains: number of measured grains; Ns: number of spontaneous tracks; Ni: number of induced tracks; ζ: ζ calibration factor; ρd: track density in standard uranium glass; P(χ2): chi-square probability; t-age: fission track age, using pooled ages; 1σ: standard error; M-L: mean track length; S.D.: standard deviation; M-Lc: mean track length after c-axis correction; nL: number of measured confined tracks; Dpar: mean etch pit diameter; Ptw: Proterozoic Wudang Group; –: no data

The age-group apatites were etched in 4.0M HNO3 for 15 s at 25 °C and the muscovite external detectors in 40 % HF for 30 min at room temperature. We used prismatic sections of Durango standard apatite to ensure that tracks are counted in the same facies in the standards and unknowns (Jonckheere et al. Reference Jonckheere, Enkelmann, Min, Trautmann and Ratschbacher2007). Ages were determined using the ζ-calibration approach (Hurford & Green, Reference Hurford and Green1983; Table 2) from a uranium-glass IRMM540R monitor. The zeta values stem from independent calibrations by counting several Durango and Fish Canyon Tuff apatite age standards (Table 2). Track counting was performed on a prismatic apatite surface with a Zeiss Axioplan microscope at magnification of 625 in transmitted light. The muscovite external detector was repositioned, trackside down, on the apatite mounts in the same position as during irradiation. Fossil tracks were counted by focusing on the underside of the external detector without moving the microscope stage (Jonckheere, Ratschbacher & Wagner, Reference Jonckheere, Ratschbacher and Wagner2003). Where possible, at least 20 crystals of each sample were counted for age determination. The length group apatite was etched for 20 s at 21 °C in 5.5M HNO3 (Donelick, Ketcham & Carlson, Reference Donelick, Ketcham and Carlson1999). Track-length measurements were performed at a magnification of 1250 using the Zeiss Axioplan microscope equipped with the Autoscan system; all suitable confined tracks parallel to the prismatic surfaces were measured. Separate mounts for track-length measurements were irradiated with heavy ions at the GSI Helmholtz Centre for Heavy Ion Research, Darmstadt (Germany), to increase the number of etchable confined fission tracks (Jonckheere et al. Reference Jonckheere, Enkelmann, Min, Trautmann and Ratschbacher2007).

4. Results and discussion

4.a. Results and thermal history modelling

The AFT results of seven samples are shown in Table 2; the pooled ages (with 1σ) vary from 76.0 ± 9.0 to 103.7 ± 10.7 Ma with P(χ2 ) > 0.05; mean track lengths range from 10.6 ± 0.1 to 11.6 ± 0.1 μm, and mean track length (μm) after c-axis correction spans 12.9 ± 0.1 to 13.6 ± 0.1 μm (Fig. 3). The Dpar (c-axis parallel etch pit diameter) values (Donelick, Reference Donelick1993; Donelick, Ketcham & Carlson, Reference Donelick, Ketcham and Carlson1999) vary between 2.0 ± 0.3 and 2.5 ± 0.4 μm, which is larger than Durango apatite (1.5–1.9 μm) (McDowell, Mcintosh & Farley, Reference McDowell, McIntosh and Farley2005), indicating our samples have higher resistance to thermal annealing (Donelick, O'Sullivan & Ketcham, Reference Donelick, O'Sullivan and Ketcham2005; Glorie et al. Reference Glorie, Grave, Buslov, Elburg, Stockli, Gerdes and Haute2010).

Figure 3.

Mean track length (left) and that after c-axis correction (right) (μm) vs apatite fission-track age of the Wudang Complex.

The AFT age–elevation relationship suggests a relatively slow exhumation rate of c. 0.027 mm a−1 from c. 110 to 80 Ma for elevations below 800 m (Fig. 4). However, sample WD2A which has the youngest ages and the highest elevation, may be affected by the Shiyan fault zone (Fig. 1c). As this fault cut through the Wudang Complex and activated mainly in the Tertiary (Huang, Reference Huang1993), the apparent age of sample WD2A, located in the hanging wall of the Shiyan fault zone, may be younger. The mean track lengths before c-axis correction decrease from 11.6 to 10.6 μm over a narrow age span (89.0–76.9 Ma), implying that the cooling rate decreased after c. 90 Ma (Fig. 3).

Figure 4.

AFT age–elevation relationship in the Wudang area.

The analytic results by Track Age Spectrum Calculation (TASC; Belton & Raab, Reference Belton and Raab2010) could reveal the onset age of cooling. According to annealing characteristics and thermal information recorded on the apatite, the track age spectra of samples W1, W3, W5 and W6 (Fig. 5) indicate that the maximum cooling onset ages are 126 ± 10 Ma, 124 ± 7 Ma, 117 ± 9 Ma and 120 ± 8 Ma respectively. These similar ages indicate the initial time when apatite entering the partial annealing zone (PAZ) occurred at ~126 Ma.

Figure 5.

Onset ages of apatite cooling analysed by Track Age Spectrum Calculation (TASC; Belton & Raab, Reference Belton and Raab2010).

The thermal histories (T[t]-paths) of five samples (Fig. 6) were derived through inverse Monte Carlo modelling using the HeFTy software (version 1.8.2; Ketcham, Reference Ketcham2005; Ketcham et al. Reference Ketcham, Balestrieri, Zattin and Donelick2009) and employing Ketcham, Donelick & Carlson's (Reference Ketcham, Donelick and Carlson1999) annealing model and the c-axis projection of Donelick, Ketcham & Carlson (Reference Donelick, Ketcham and Carlson1999). The initial mean track length of L 0 = 16.0 ± 0.8 μm (Shen et al. Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012) was determined from measurements of induced confined tracks in Durango apatite standards. Measured Dpar values were applied to account for the variation of track length. The Kolmogorov–Smirnov test (GOF) was used to assess the goodness of fit between the modelled and measured results, with thresholds of 0.50 and 0.05 for good and acceptable fits (Ketcham, Reference Ketcham2005). In this work, the monotonic path setting was used to allow for both cooling and heating histories. Allowing the samples to cool above the closure temperature of AFT to simulate uncertainty in the initial thermal history, we take 140 °C as the initial constraint. The second constraint is the surface temperature, which we take as 20 °C at 0 Ma. Meantime, at least 500 good paths were modelled for each sample. The inversion modelling results indicate that the samples entered the apatite PAZ rapidly between 126 and 90 Ma, and there then followed a prolonged period with cooling rates <0.5 °C Ma−1 residing in the apatite PAZ (Donelick, O'Sullivan & Ketcham, Reference Donelick, O'Sullivan and Ketcham2005); accelerated cooling has occurred at an average cooling rate of ~3 °C Ma−1 since c. 15 Ma.

Figure 6.

Low-temperature thermal history and confined track-length distribution modelling by the HeFTy 1.8.2 software (Ketcham, Reference Ketcham2005; Ketcham et al. Reference Ketcham, Balestrieri, Zattin and Donelick2009) based on AFT data. D, determined apatite fission-track age (in Ma with 1σ error) and mean confined track length (in μm with standard deviation). M, modeled apatite fission-track age and mean confined track length. N, number of measured confined track lengths. GOF is the Kolmogorov–Smirnov test, assessing the fit between the modelled and measured results, with thresholds of 0.05 and 0.50 for good and acceptable fits (Ketcham, Reference Ketcham2005).

4.b. The cooling/exhumation history reconstruction

According to distinct closure temperatures of different minerals, the multiple geochronometers allow us to reconstruct the thermal history of a rock unit (e.g. Glorie et al. Reference Glorie, Grave, Buslov, Elburg, Stockli, Gerdes and Haute2010; Dong et al. Reference Dong, Zhang, Neubauer, Liu, Genser and Hauzenberger2011b ; Shen et al. Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012). Figure 7 shows age vs closure temperature plots, illustrating the multi-stage cooling/exhumation process of the Wudangshan Complex. The zircon U–Pb, hornblende 40Ar–39Ar, muscovite 40Ar–39Ar and ZHe (zircon (U–Th/He) data were used to constrain the cooling process under medium-high temperature (>200 °C). The T[t]-paths based on the AFT data (Fig. 6) were used to reveal the cooling procedure at low temperature (<120 °C). Integrating all these data (Table 1), the thermal history of the Wudangshan Complex can be divided into seven stages: (1) Stage I – the temperature decreased from the closure temperature (700–800 °C; Cherniak & Watson, Reference Cherniak and Watson2003) of the U–Pb zircon system to the surface condition (~20 °C) from c. 755 to c. 632 Ma at a fast cooling rate of c. 5.7 °C Ma−1. (2) Stage II – the temperature rose rapidly to the hornblende 40Ar–39Ar system (450–550 °C; McDougall & Harrison Reference McDougall and Harrison1999) from c. 632 Ma to c. 237 Ma. (3) Stage III – the volcanic rocks are recorded as cooling through temperatures of the ZHe system (180–220 °C; Reiners et al. Reference Reiners, Spell, Nicolescu and Zanetti2004) between c. 237 and c. 220 Ma at a rate of c. 17.6 °C Ma−1 which means that exhumation rate may reach 0.4 km Ma−1. (4) Stage IV – from the ZHe system (180–220 °C) to the closure temperature (~120 °C) of AFT (Ketcham, Donelick & Carlson, Reference Ketcham, Donelick and Carlson1999) between c. 220 and c. 126 Ma at a decreasing cooling rate of c. 0.8 °C Ma−1. (5) Stage V – the sample cooled through the apatite PAZ from 126 to 90 Ma at a rate of c. 1.5 °C Ma−1. (6) Stage VI – the slowest cooling stage according to the thermal modelling results (Fig. 6) occurred from c. 90 to c. 15 Ma at an insignificant speed. (7) Stage VII – a final accelerated cooling to the surface temperature (20 °C) occurred from c. 15 Ma to the present at a rate of c. 3 °C Ma−1, corresponding to an exhumation rate of c. 0.1–0.15 km Ma−1.

Figure 7.

Cooling paths for the Wudangshan Complex using multiple thermochronological methods including zircon U–Pb, 40Ar–39Ar, ZHe and AFT. The data are shown in Table 1 and Figure 1c.

4.c. Geodynamic interpretations

The thermal history of the Wudang Complex recorded by the thermochronological data is related to the geodynamic setting and tectonic evolution of the South Qinling orogenic belt. The volcanic suite of the Wudang Group was formed at c. 755 Ma dating by the zircon U–Pb method (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008, Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010), and this rift-related igneous event indicated a complete separation of the South China Block and a break-up of the supercontinent Rodinia (Ling et al. Reference Ling, Duan, Liu, Cheng, Mao, Peng and Liu2008, Reference Ling, Duan, Liu, Cheng, Mao, Peng, Liu, Yang and Ren2010; Xia et al. Reference Xia, Xia, Xiang-Min, Zhong-Ping and Xue-Yi2008; Bader et al. Reference Bader, Franz, Ratschbacher, Capitani, Webb, Yang, Pfänder, Hofmann and Linnemann2013a ). The weathered unconformity between the Wudang Group and the Yaolinghe Group indicates that the Wudang rocks were exposed at the surface in Neoproterozoic times (Huang, Reference Huang1993). Similarly, the disconformities contact between the Yaolinghe Group and the Sinian carbonate formation indicates that the Yaolinghe volcanic suite had experienced the same cooling event. Therefore, a rapid cooling process (stage I) through heat exchange with the surrounding rock can be assumed from c. 755 Ma to c. 632 Ma. This event was followed by a long-term extension and subsidence process under the passive continental margin setting (stage II), which resulted in >10 km sediments from the end of the Neoproterozoic to the mid-Triassic (Fig. 2; Hu, Reference Hu2004). The rocks of the Wudang Group located at the bottom may experience regional metamorphism due to the deep burial depth.

A rapid decrease occurred in the thermal history (stage III) after a long-time sedimentation (Fig. 7), indicating the collision event between the NCC and SCB with intensive deformation and rapid exhumation. The Triassic orogenic event induced by the subduction of the Yangtze plate under the NCC has significant impacts on the entire Qinling–Dabie Belt, North China Craton and South China Block (Ratschbacher et al. Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003, Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006; Hu et al. Reference Hu, Kohn, Raza, Wang and Gleadow2006a , Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006 b). Many pre-existing shear/fault zones (Lonan, Shangxiang, Shangdan) have been reactivated in the North Qinling between 200 and 240 Ma (Ratschbacher et al. Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003). The UHP rocks were formed at ~240 Ma and quickly returned in the Tongbai–Dabie area due to the delamination of the lithospheric mantle (Hu et al. Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b; Zhang, Ma & Holtz, Reference Zhang, Ma and Holtz2010). The Wudang Complex was part of the Yangtze Craton, and the rapid extensional exhumation allowed these greenschist rocks to be exposed on the surface.

The decreasing cooling, at c. 0.8 °C Ma−1, from c. 220 to 126 Ma (stage IV; Fig. 7) clearly reflects a gravitational adjustment after the rapid exhumation during orogeny, which is also in accordance with the slight deformation and sedimentation investigated in the Qinling area from the Jurassic to the Early Cretaceous (Ratschbacher et al. Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006). After that, the inversion modelling results according to the AFT data indicate that the samples passed rapidly through the apatite PAZ between 126 Ma and 90 Ma (stage V). Previous studies have already indicated that the late Jurassic – early Cretaceous tectonic-reactivated and magmatism throughout eastern China (e.g. Tongbai–Dabie, Yangtze craton and eastern NCC (Hacker et al. Reference Hacker, Ratschbacher, Webb, Ireland, Walker and Dong1998; Wu et al. Reference Wu, Lin, Wilde, Zhang and Yang2005; Li & Li, Reference Li and Li2007; Chen et al. Reference Chen, Ma, She, Mason, Zhang and Zhang2009; Li et al. Reference Li, Li, Wang, Li, Liu, Tang, Gao and Wu2010; Zhang, Ma & Holtz, Reference Zhang, Ma and Holtz2010; Xie, Mao & Zhao, Reference Xie, Mao and Zhao2011)) were induced by the subduction of the palaeo-Pacific plate (Wu et al. Reference Wu, Lin, Wilde, Zhang and Yang2005; Zhou et al. Reference Zhou, Sun, Shen, Shu and Niu2006; Huang et al. Reference Huang, Li, Dong, Li, Chen, Wang and Yang2007; Chen et al. Reference Chen, Ma, She, Mason, Zhang and Zhang2009; Zhang et al. Reference Zhang, Ma, Liao, Zhang and She2011). Hu et al. (Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b) also related the large-scale transtensional deformation between ~140 and 110 Ma observed in the Tongbai–Dabie region to the subduction of the Pacific Plate. Hence, the Pacific back-arc extension could contribute to entering the apatite PAZ from c. 126 to 90 Ma despite the large distance to the coast.

Stage VI is characterized by very slow cooling or even reheating during the late Cretaceous – Eocene, but local burial in the sedimentary basin and rapid erosion in the edge shoulder occurred (Shen et al. Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012). For example, the Late Cretaceous – Eocene red bed deposition in pull-apart basins occurred in eastern China (e.g. Arne et al. Reference Arne, Worley, Wilson, She, Foster, Zhi, Shu and Dirks1997; Ratschbacher et al. Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006) coeval with widespread Cretaceous strike-slip and extensional deformation in eastern Asia (Hacker et al. Reference Hacker, Ratschbacher, Webb, McWilliams, Ireland, Calvert, Dong, Wenk and Chateigner2000; Ratschbacher et al. Reference Ratschbacher, Hacker, Webb, McWilliams, Ireland, Dong, Calvert, Chateigner and Wenk2000, Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003; Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006). This peneplanation stage is widespread from the eastern Tibetan Plateau to eastern China including the Sichuan basin (Richardson et al. Reference Richardson, Densmore, Seward, Fowler, Wipf, Ellis, Yong and Zhang2008; Deng et al. Reference Deng, Liu, Li, Jansa, Liu, Wang and Sun2013; Tian et al. Reference Tian, Kohn, Gleadow and Hu2013, Reference Tian, Kohn, Hu and Gleadow2015), the Yangtze Craton (Hu et al. Reference Hu, Kohn, Raza, Wang and Gleadow2006a ; Shen et al. Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012) and the Qinling–Dabie orogen (Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Hu et al. Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b; Ratschbacher et al. Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006; Heberer et al. Reference Heberer, Anzenbacher, Neubauer, Genser, Dong and Dunkl2014). The peneplanation period in the South Qinling region initiated at c. 90 Ma, which is similar to the Hannan–Micang massif (Tian et al. Reference Tian, Kohn, Zhu, Xu, Hu and Gleadow2012; Yang et al. Reference Yang, Ratschbacher, Jonckheere, Enkelmann, Dong, Shen, Wiesinger and Zhang2013) but different from the Sichuan basin (Shen, Mei & Xu, Reference Shen, Mei and Xu2009; Deng et al. Reference Deng, Liu, Li, Jansa, Liu, Wang and Sun2013), the middle-Yangtze craton (Shen et al. Reference Shen, Mei, Peng, Chen, Yang and Hong2011, Reference Shen, Mei, Min, Jonckheere, Ratschbacher, Yang, Peng and Liu2012) and the Dabie orogenic belt (Hu et al. Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b). A regional low-relief landscape across the eastern Tibetan Plateau and much of central China may also have resulted in this thermal stagnation period (Arne et al. Reference Arne, Worley, Wilson, She, Foster, Zhi, Shu and Dirks1997; Kirby et al. Reference Kirby, Reiners, Krol, Whipple, Hodges, Farley, Tang and Chen2002; Ratschbacher et al. Reference Ratschbacher, Hacker, Calvert, Webb, Grimmer, McWilliams, Ireland, Dong, Hu and Calvert2003, Reference Ratschbacher, Franz, Enkelmann, Jonckheere, Pörschke, Hacker, Dong and Zhang2006; Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Deng et al. Reference Deng, Liu, Li, Jansa, Liu, Wang and Sun2013).

The final accelerated cooling since c. 15 Ma (stage VII; Fig. 7) has also been documented (Fig. 8a), in the eastern Tibetan Plateau (Clark et al. Reference Clark, House, Royden, Whipple, Burchfiel, Zhang and Tang2005; Ouimet et al. Reference Ouimet, Whipple, Royden, Reiners, Hodges and Pringle2010), the Longmen Shan (Arne et al. Reference Arne, Worley, Wilson, She, Foster, Zhi, Shu and Dirks1997; Tian et al. Reference Tian, Kohn, Gleadow and Hu2013), the Sichuan Basin (Shen, Mei & Xu, Reference Shen, Mei and Xu2009; Deng et al. Reference Deng, Liu, Li, Jansa, Liu, Wang and Sun2013), the Hannan–Micang massif (Tian et al. Reference Tian, Kohn, Zhu, Xu, Hu and Gleadow2012; Yang et al. Reference Yang, Ratschbacher, Jonckheere, Enkelmann, Dong, Shen, Wiesinger and Zhang2013), the Daba Shan (Z. Zhang et al. Reference Zhang, Miao, Zhang, Lu, Zhang, Chen, Li, Miao, Feng and Ou2013; Yang, Reference Yang2014), the Qinling (Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Hu et al. Reference Hu, Raza, Min, Kohn, Reiners, Ketcham, Wang and Gleadow2006b) and even northern Kyrgyz Tien Shan (Glorie et al. Reference Glorie, Grave, Buslov, Elburg, Stockli, Gerdes and Haute2010; Macaulay et al. Reference Macaulay, Sobel, Mikolaichuk, Kohn and Stuart2014). Most previous studies suggest that this rapid cooling since c. 15 Ma is due to the eastward growth of the Tibetan Plateau after the collision of India and Asia (Tapponnier et al. Reference Tapponnier, Zhiqin, Roger, Meyer, Arnaud, Wittlinger and Jingsui2001; Liu, Cui & Liu, Reference Liu, Cui and Liu2004; Clark et al. Reference Clark, House, Royden, Whipple, Burchfiel, Zhang and Tang2005; Enkelmann et al. Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006; Tian et al. Reference Tian, Kohn, Zhu, Xu, Hu and Gleadow2012; Macaulay et al. Reference Macaulay, Sobel, Mikolaichuk, Kohn and Stuart2014). The unconformity between Eocene and Neogene in the adjacent basin (Fig. 8c) supports this event. Tada, Zheng & Clift (Reference Tada, Zheng and Clift2016) attributed the uplift of the northern and eastern Tibetan Plateau at c. 15–10 Ma to lower crustal flow, which is due to crustal thickening and northeastward expansion of the partial melting materials (Clark & Royden Reference Clark and Royden2000; Yuan et al. Reference Yuan, Ge, Chen, Li, Wang, Zhang, Zhang, Zheng, Zheng and Craddock2013). However, we also cannot ignore the influence of climate change on the rapid exhumation and landscape adjustment because this exhumation process coincides with the regional climate change in East Asia (Fig. 8b; Allen & Armstrong, Reference Allen and Armstrong2012). Late Cenozoic global cooling and the onset of the Asian monsoon in the early Miocene have been widely cited for Himalayan–Tibet uplift (Guo et al. Reference Guo, Ruddiman, Hao, Wu, Qiao, Zhu, Peng, Wei, Yuan and Liu2002; Clift et al. Reference Clift, Hodges, Heslop, Hannigan, Long and Calves2008; Armstrong & Allen, Reference Armstrong and Allen2011; Allen & Armstrong, Reference Allen and Armstrong2012). The East Asian monsoon climate has been mainly dominated by the widespread East Asian summer monsoon (EASM) since the Miocene, characterized by high moisture levels and heavy summer rainfall (Guo et al. Reference Guo, Sun, Zhang, Peng, Xiao, Ge, Hao, Qiao, Liang and Liu2008; Molnar, Boos & Battisti, Reference Molnar, Boos and Battisti2010). The South Qinling area located in the south of the Chinese loess plateau developed rich river and rainfall that induced rapid erosion. The famous Three Gorges is the consequence of incision by the Yangtze River, and similar river incision also occurred in the central Sichuan Basin and Yangtze River Delta (Kirby et al. Reference Kirby, Reiners, Krol, Whipple, Hodges, Farley, Tang and Chen2002; Richardson et al. Reference Richardson, Densmore, Seward, Fowler, Wipf, Ellis, Yong and Zhang2008; P. Zhang et al. Reference Zhang, Miao, Zhang, Lu, Zhang, Chen, Li, Miao, Feng and Ou2013). Hence, we may not exclude the effect of the Asian monsoon from the Late Miocene to the present on enhanced exhumation/cooling, although as a secondary cause with respect to tectonic activity.

Figure 8.

(a) Simplified geological map showing the regional denudation event after c. ~15 Ma. Reference codes are [1] = Clark et al. (Reference Clark, House, Royden, Whipple, Burchfiel, Zhang and Tang2005); [2] = Ouimet et al. (Reference Ouimet, Whipple, Royden, Reiners, Hodges and Pringle2010); [3] = Tian et al. (Reference Tian, Kohn, Gleadow and Hu2013); [4] = Arne et al. (Reference Arne, Worley, Wilson, She, Foster, Zhi, Shu and Dirks1997); [5] = Deng et al. (Reference Deng, Liu, Li, Jansa, Liu, Wang and Sun2013); [6] = Shen, Mei & Xu (Reference Shen, Mei and Xu2009); [7] = Zhang et al. (2006); [8] = Tian et al. (Reference Tian, Kohn, Zhu, Xu, Hu and Gleadow2012); and Yang et al. (Reference Yang, Ratschbacher, Jonckheere, Enkelmann, Dong, Shen, Wiesinger and Zhang2013); [9] =Wang et al. (Reference Wang, Zattin, Li, Song, Peng, Liu and Liu2011); [10] = Enkelmann et al. (Reference Enkelmann, Ratschbacher, Jonckheere, Nestler, Fleischer, Gloaguen, Hacker, Zhang and Ma2006); [11] = Lin et al. (Reference Lin, Chen, Wyrwoll and Cheng2010); and [12] = Liu et al. (2013). (b) Possible geodynamic mechanism of the late-Cenozoic tectonic and climate events. (c) Discontinuity of Lushi basin located in the northeast of the Wudang Terrain between Eocene and Neogene. Location of Lushi basin is shown in Figure 1b.

5. Conclusions

Tectonic evolution of the South Qinling orogenic belt was clarified through joint analysis of previous multiple geochronologic data and our new AFT data from the Wudang Complex. A gravitational adjustment period from c. 220 to 126 Ma occurred after the fierce exhumation in the Triassic due to collision between the NCC and SCB, which was a response to minor tectonism and sedimentation in the Qinling area during Jurassic to Early Cretaceous time. Meantime, the South Qinling area could also be affected by Pacific subduction to induce the apatite cooling through the PAZ from c. 126 to c. 90 Ma. The AFT thermal history modelling indicates the late Cretaceous – Eocene peneplanation stage is characterized by insignificant exhumation, coinciding with the formation of regional low-relief landscape. The widespread late Cenozoic accelerated cooling has taken place since 15 Ma in the South Qinling area. It could be influenced by the eastward growth of the Tibetan Plateau uplift and the Asian monsoon as a combined effect of endogenic and exogenic geological process.

Acknowledgements

This work was supported by the National Natural Science Foundation of China (No. 41372140, 40902038), the Fundamental Research Fund for the Central Universities, China University of Geosciences (Wuhan, No. 201536), the Outstanding Youth Funding of Natural Science Foundation of Hubei Province (No. 2016CFA055) and the Wuhan Science and Technology Project (No. 2016070204010145). We are very grateful to Professor Lothar Ratschbacher, Dr Raymond Jonckheere, Dr Zhao Yang and Dr Bastian Wauschkuhn for their kind help with and discussion of fission-track analysis; Professor Richard Ketcham for providing the HeFTy software; Dr Adam Szulc, Dr Tom Wittenschlaeger and Dr Xiang Ge for polishing the English; and Editor-in-Chief, Professor Allen Mark and three anonymous reviewers for their comments and suggestions. Shen's stay at Freiberg was funded by the China Scholarship Council.

References

Allen, M. B. & Armstrong, H. A. 2012. Reconciling the intertropical convergence zone, Himalayan/Tibetan tectonics, and the onset of the Asian monsoon system. Journal of Asian Earth Sciences 44 (1), 36–47.CrossRefGoogle Scholar
Ames, L., Gaozhi, Z. & Baocheng, X. 1996. Geochronology and isotopic character of ultrahigh-pressure metamorphism with implications for collision of the Sino-Korean and Yangtze cratons, central China. Tectonics 15 (2), 472–89.CrossRefGoogle Scholar
An, Z., Kutzbach, J. E., Prell, W. L. & Porter, S. C. 2001. Evolution of Asian monsoons and phased uplift of the Himalaya-Tibetan plateau since Late Miocene times. Nature 411 (6833), 62–6.Google Scholar
Armstrong, H. A. & Allen, M. B. 2011. Shifts in the intertropical convergence zone, Himalayan exhumation, and late Cenozoic climate. Geology 39 (1), 11–14.CrossRefGoogle Scholar
Arne, D., Worley, B., Wilson, C., She, F. C., Foster, D., Zhi, L. L., Shu, G. L. & Dirks, P. 1997. Differential exhumation in response to episodic thrusting along the eastern margin of the Tibetan Plateau. Tectonophysics 280 (3–4), 239–56.Google Scholar
Bader, T., Franz, L., Ratschbacher, L., Capitani, C. D., Webb, A. A. G., Yang, Z., Pfänder, J. A., Hofmann, M. & Linnemann, U. 2013a. The Heart of China revisited: II Early Paleozoic (ultra)high-pressure and (ultra)high-temperature metamorphic Qinling orogenic collage. Tectonics 32 (4), 922–47.Google Scholar
Bader, T., Ratschbacher, L., Franz, L., Yang, Z., Hofmann, M., Linnemann, U. & Yuan, H. 2013b. The Heart of China revisited, I. Proterozoic tectonics of the Qin Mountains in the core of supercontinent Rodinia. Tectonics 32 (3), 1497–505.CrossRefGoogle Scholar
Belton, D. X. & Raab, M. J. 2010. Cretaceous reactivation and intensified erosion in the Archean–Proterozoic Limpopo Belt, demonstrated by apatite fission track thermochronology. Tectonophysics 480 (s 1–4), 99–108.CrossRefGoogle Scholar
Cai, Z., Xiong, X., Hong, L., Dekuang, W. U., Sun, S. & Rao, B. 2007. Forming age of the volcanic rocks of the Yaolinghe Group from Wudang Block, Southern Qinling Mountain: constraint from grain-zircon U-Pb dating. Acta Geologica Sinica 81 (5), 620–5.Google Scholar
Chen, L., Ma, C. Q., She, Z. B., Mason, R., Zhang, J. Y. & Zhang, C. 2009. Petrogenesis and tectonic implications of A-type granites in the Dabie orogenic belt, China: geochronological and geochemical constraints. Geological Magazine 146 (5), 638–51.CrossRefGoogle Scholar
Cherniak, D. J. & Watson, E. B. 2003. Diffusion in zircon. Physics & Chemistry of Minerals 53, 113–39.Google Scholar
Clark, M. K., House, M. A., Royden, L. H., Whipple, K. X., Burchfiel, B. C., Zhang, X. & Tang, W. 2005. Late Cenozoic uplift of southeastern Tibet. Geology 33 (6), 525–38.Google Scholar
Clark, M. K. & Royden, L. H. 2000. Topographic ooze: building the eastern margin of Tibet by lower crustal flow. Geology 28 (8), 703–6.2.0.CO;2>CrossRefGoogle Scholar
Clift, P. D., Hodges, K. V., Heslop, D., Hannigan, R., Long, H. V. & Calves, G. 2008. Correlation of Himalayan exhumation rates and Asian monsoon intensity. Nature Geoscience 1 (12), 875–80.Google Scholar
Deng, B., Liu, S. G., Li, Z. W., Jansa, L. F., Liu, S., Wang, G. Z. & Sun, W. 2013. Differential exhumation at eastern margin of the Tibetan Plateau, from apatite fission-track thermochronology. Tectonophysics 591, 98–115.CrossRefGoogle Scholar
Donelick, R. A. 1993. Method of fission track analysis utilizing bulk chemical etching of apatite. US Patent No. 5267274.Google Scholar
Donelick, R. A., Ketcham, R. A. & Carlson, W. D. 1999. Variability of apatite fission-track annealing kinetics: II. Crystallographic orientation effects. American Mineralogist 84, 1224–34.CrossRefGoogle Scholar
Donelick, R. A., O'Sullivan, P. B. & Ketcham, R. A. 2005. Apatite fission-track analysis. Reviews in Mineralogy & Geochemistry 58, 49–94.CrossRefGoogle Scholar
Dong, Y., Genser, J., Neubauer, F., Zhang, G., Liu, X., Yang, Z. & Heberer, B. 2011a. U-Pb and 40Ar/39Ar geochronological constraints on the exhumation history of the North Qinling terrane, China. Gondwana Research 19 (4), 881–93.Google Scholar
Dong, Y., Liu, X., Zhang, G., Chen, Q., Zhang, X., Li, W. & Yang, C. 2012. Triassic diorites and granitoids in the Foping area: constraints on the conversion from subduction to collision in the Qinling orogen, China. Journal of Asian Earth Sciences 47 (1), 123–42.Google Scholar
Dong, Y. P. & Santosh, M. 2016. Tectonic architecture and multiple orogeny of the Qinling Orogenic Belt, Central China. Gondwana Research 29 (1), 1–40.CrossRefGoogle Scholar
Dong, Y., Zhang, G., Neubauer, F., Liu, X., Genser, J. & Hauzenberger, C. 2011b. Tectonic evolution of the Qinling orogen, China: review and synthesis. Journal of Asian Earth Sciences 41 (3), 213–37.CrossRefGoogle Scholar
Enkelmann, E., Ratschbacher, L., Jonckheere, R., Nestler, R., Fleischer, M., Gloaguen, R., Hacker, B. R., Zhang, Y. Q. & Ma, Y. S. 2006. Cenozoic exhumation and deformation of northeastern Tibet and the Qinling: is Tibetan lower crustal flow diverging around the Sichuan Basin? Geological Society of America Bulletin 118 (5–6), 651–71.Google Scholar
Faure, M., Lin, W., Monié, P., Breton, N. L., Poussineau, S., Panis, D. & Deloule, E. 2003. Exhumation tectonics of the ultrahigh-pressure metamorphic rocks in the Qinling orogen in east China: new petrological-structural-radiometric insights from the Shandong Peninsula. Tectonics 22 (3), 127–43.Google Scholar
Glorie, S., Grave, J. D., Buslov, M. M., Elburg, M. A., Stockli, D. F., Gerdes, A. & Haute, P. V. D. 2010. Multi-method chronometric constraints on the evolution of the Northern Kyrgyz Tien Shan granitoids (Central Asian Orogenic Belt): from emplacement to exhumation. Journal of Asian Earth Sciences 38 (3–4), 131–46.Google Scholar
Grave, J. D., Buslov, M. M. & Haute, P. V. D. 2007. Distant effects of India–Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: constraints from apatite fission-track thermochronology. Journal of Asian Earth Sciences 29 (2–3), 188–204.CrossRefGoogle Scholar
Grave, J. D., Glorie, S., Buslov, M. M., Stockli, D. F., Mcwilliams, M. O., Batalev, V. Y. & Haute, P. V. D. 2013. Thermo-tectonic history of the Issyk-Kul basement (Kyrgyz Northern Tien Shan, Central Asia). Gondwana Research 23 (3), 998–1020.CrossRefGoogle Scholar
Guo, Z. T., Ruddiman, W. F., Hao, Q. Z., Wu, H. B., Qiao, Y. S., Zhu, R. X., Peng, S. Z., Wei, J. J., Yuan, B. Y. & Liu, T. S. 2002. Onset of Asian desertification by 22 Myr ago inferred from loess deposits in China. Nature 416 (6877), 159–63.CrossRefGoogle ScholarPubMed
Guo, Z. T., Sun, B., Zhang, Z. S., Peng, S. Z., Xiao, G. Q., Ge, J. Y., Hao, Q. Z., Qiao, Y. S., Liang, M. Y. & Liu, J. F. 2008. A major reorganization of Asian climate by the early Miocene. Climate of the Past 4 (3), 153–74.Google Scholar
Hacker, B. R., Ratschbacher, L., Webb, L., Ireland, T., Walker, D. & Dong, S. 1998. U/Pb zircon ages constrain the architecture of the ultrahigh-pressure Qinling–Dabie Orogen, China. Earth & Planetary Science Letters 161 (1), 215–30.Google Scholar
Hacker, B. R., Ratschbacher, L., Webb, L., McWilliams, M. O., Ireland, T., Calvert, A., Dong, S., Wenk, H. R. & Chateigner, D. 2000. Exhumation of ultrahigh-pressure continental crust in east central China: Late Triassic-Early Jurassic tectonic unroofing. Journal of Geophysical Research Solid Earth 105, 13,339–64.Google Scholar
Heberer, B., Anzenbacher, T., Neubauer, F., Genser, J., Dong, Y. & Dunkl, I. 2014. Polyphase exhumation in the western Qinling Mountains, China: rapid Early Cretaceous cooling along a lithospheric-scale tear fault and pulsed Cenozoic uplift. Tectonophysics 617 (4), 31–43.CrossRefGoogle ScholarPubMed
Hu, J. 2004. Mid-Late Palaeozoic extension of the Wudang block in the South Qinling tectonic belt, China. Chinese Journal of Geology 39 (3), 305–19.Google Scholar
Hu, S., Kohn, B. P., Raza, A., Wang, J. & Gleadow, A. J. W. 2006a. Cretaceous and Cenozoic cooling history across the ultrahigh pressure Tongbai–Dabie belt, central China, from apatite fission-track thermochronology. Tectonophysics 420 (3–4), 409–29.Google Scholar
Hu, S., Raza, A., Min, K., Kohn, B. P., Reiners, P. W., Ketcham, R. A., Wang, J. & Gleadow, A. J. W. 2006b. Late Mesozoic and Cenozoic thermotectonic evolution along a transect from the north China craton through the Qinling orogen into the Yangtze craton, central China. Tectonics 25 (6), 97–112.Google Scholar
Huang, W. 1993. Multiphase deformation and displacement within a basement complex on a continental margin: the Wudang Complex in the Qinling Orogen, China. Tectonophysics 224 (224), 305–26.Google Scholar
Huang, F., Li, S., Dong, F., Li, Q., Chen, F., Wang, Y. & Yang, W. 2007. Recycling of deeply subducted continental crust in the Dabie Mountains, central China. Lithos 96 (1–2), 151–69.Google Scholar
Hurford, A. J. & Green, P. F. 1983. The zeta age calibration of fission-track dating. Chemical Geology 41 (83), 285–317.CrossRefGoogle Scholar
Jonckheere, R., Enkelmann, E., Min, M., Trautmann, C. & Ratschbacher, L. 2007. Confined fission tracks in ion-irradiated and step-etched prismatic sections of Durango apatite. Chemical Geology 242 (1), 202–17.CrossRefGoogle Scholar
Jonckheere, R., Ratschbacher, L. & Wagner, G. A. 2003. A repositioning technique for counting induced fission tracks in muscovite external detectors in single-grain dating of minerals with low and inhomogeneous uranium concentrations. Radiation Measurements 37 (3), 217–9.Google Scholar
Ketcham, R. A. 2005. Forward and inverse modeling of low-temperature thermochronometry data. Reviews in Mineralogy & Geochemistry 58 (1), 275–314.Google Scholar
Ketcham, R. A., Balestrieri, M. L., Zattin, M. & Donelick, R. A. 2009. Reproducibility of apatite fission-track length data and thermal history reconstruction. Earth & Planetary Science Letters 284 (3), 504–15.Google Scholar
Ketcham, R. A., Donelick, R. A. & Carlson, W. D. 1999. Variability of apatite fission-tack annealing kinetics III: extrapolation to geological time scales. American Mineralogist 84, 1235–55.Google Scholar
Kirby, E., Reiners, P. W., Krol, M. A., Whipple, K. X., Hodges, K. V., Farley, K. A., Tang, W. & Chen, Z. 2002. Late Cenozoic evolution of the eastern margin of the Tibetan Plateau: inferences from 40Ar/39Ar and (U-Th)/He thermochronology. Tectonics 21 (1), 1–20.Google Scholar
Kröner, A., Zhang, G. W. & Sun, Y. 1993. Granulites in the Tongbai Area, Qinling Belt, China: geochemistry, petrology, single zircon geochronology, and implications for the tectonic evolution of eastern Asia. Tectonics 12 (1), 245–55.Google Scholar
Li, S., Xiao, Y., Liou, D., Chen, Y., Ge, N., Zhang, Z., Sun, S. S., Cong, B., Zhang, R. & Hart, S. R. 1993. Collision of the North China and Yangtse Blocks and formation of coesite-bearing eclogites: timing and processes. Chemical Geology 109 (1–4), 89–111.Google Scholar
Li, X. H., Li, W. X., Wang, X. C., Li, Q. L., Liu, Y., Tang, G. Q., Gao, Y. Y. & Wu, F. Y. 2010. SIMS U–Pb zircon geochronology of porphyry Cu–Au–(Mo) deposits in the Yangtze River Metallogenic Belt, eastern China: magmatic response to early Cretaceous lithospheric extension. Lithos 119 (3–4), 427–38.CrossRefGoogle Scholar
Li, Z. X. & Li, X. H. 2007. Formation of the 1300-km-wide intracontinental orogen and postorogenic magmatic province in Mesozoic South China: a flat-slab subduction model. Geology 35 (2), 179–82.Google Scholar
Lin, X., Chen, H., Wyrwoll, K. H. & Cheng, X. 2010. Commencing uplift of the Liupan Shan since 9.5 Ma: evidences from the Sikouzi section at its east side. Journal of Asian Earth Sciences 37 (4), 350–60.Google Scholar
Ling, W. L., Duan, R. C., Liu, X. M., Cheng, J. P., Mao, X. W., Peng, L. H. & Liu, Z. X. 2008. Timing of the Wudangshan, Yaolinghe volcanic sequences and mafic sills in South Qinling: U-Pb zircon geochronology and tectonic implication. Chinese Science Bulletin 53 (14), 2192–9.Google Scholar
Ling, W. L., Duan, R. C., Liu, X. M., Cheng, J. P., Mao, X. W., Peng, L. H., Liu, Z. X., Yang, H. M. & Ren, B. F. 2010. U-Pb dating of detrital zircons from the Wudangshan Group in the South Qinling and its geological significance. Chinese Science Bulletin 55 (22), 2440–8.Google Scholar
Liu, J., Zhang, P., Lease, R. O., Zheng, D., Wan, J., Wang, W. & Zhang, H. 2012. Eocene onset and late Miocene acceleration of Cenozoic intracontinental extension in the North Qinling range–Weihe graben: insights from apatite fission track thermochronology. Tectonophysics 584 (1), 281–96.Google Scholar
Liu, M., Cui, X. & Liu, F. 2004. Cenozoic rifting and volcanism in eastern China: a mantle dynamic link to the Indo–Asian collision? Tectonophysics 393 (1), 29–42.Google Scholar
Macaulay, E. A., Sobel, E. R., Mikolaichuk, A., Kohn, B. & Stuart, F. M. 2014. Cenozoic deformation and exhumation history of the Central Kyrgyz Tien Shan. Tectonics 33 (2), 135–65.Google Scholar
Mattauer, M., Matte, P., Malavieille, J., Tapponnier, P., Maluski, H., Qin, X. Z., Lun, L. Y. & Qin, T. Y. 1985. Tectonics of the Qinling Belt: build-up and evolution of eastern Asia. Nature 317 (6037), 496–500.Google Scholar
McDougall, I. & Harrison, T. M. 1999. Geochronology and thermochronology by the 40Ar/39Ar method. Oxford: Oxford University Press, 269 pp.Google Scholar
McDowell, F. W., McIntosh, W. C. & Farley, K. A. 2005. A precise 40Ar–39Ar reference age for the Durango apatite (U–Th)/He and fission-track dating standard. Chemical Geology 214 (3), 249–63.Google Scholar
Molnar, P., Boos, W. R. & Battisti, D. S. 2010. Orographic controls on climate and paleoclimate of Asia: thermal and mechanical roles for the Tibetan Plateau. Annual Review of Earth & Planetary Sciences 38 (1), 77–102.Google Scholar
Okay, A. I., Şengör, A. M. C. & Satir, M. 1993. Tectonics of an ultrahigh-pressure metamorphic terrane: the Dabie Shan/Tongbai Shan Orogen, China. Tectonics 12 (6), 1320–34.Google Scholar
Ouimet, W., Whipple, K., Royden, L., Reiners, P., Hodges, K. & Pringle, M. 2010. Regional incision of the eastern margin of the Tibetan Plateau. Lithosphere 2 (1), 50–63.CrossRefGoogle Scholar
Ratschbacher, L., Franz, L., Enkelmann, E., Jonckheere, R., Pörschke, A., Hacker, B. R., Dong, S. & Zhang, Y. 2006. The Sino-Korean–Yangtze suture, the Huwan detachment, and the Paleozoic–Tertiary exhumation of (ultra)high-pressure rocks along the Tongbai-Xinxian-Dabie Mountains. Special Paper of the Geological Society of America 403, 45–75.Google Scholar
Ratschbacher, L., Hacker, B. R., Calvert, A., Webb, L. E., Grimmer, J. C., McWilliams, M. O., Ireland, T., Dong, S., Hu, J. & Calvert, A. 2003. Tectonics of the Qinling (Central China): tectonostratigraphy, geochronology, and deformation history. Tectonophysics 366 (1–2), 1–53.Google Scholar
Ratschbacher, L., Hacker, B. R., Webb, L. E., McWilliams, M., Ireland, T., Dong, S., Calvert, A., Chateigner, D. & Wenk, H. R. 2000. Exhumation of the ultrahigh-pressure continental crust in east central China: Cretaceous and Cenozoic unroofing and the Tan-Lu fault. Journal of Geophysical Research Solid Earth 105 (B6), 13,303–38.Google Scholar
Reiners, P. W., Spell, T. L., Nicolescu, S. & Zanetti, K. A. 2004. Zircon (U-Th)/He thermochronometry: He diffusion and comparisons with 40Ar/39Ar dating. Geochimica et Cosmochimica Acta 68 (8), 1857–87.Google Scholar
Richardson, N. J., Densmore, A. L., Seward, D., Fowler, A., Wipf, M., Ellis, M. A., Yong, L. & Zhang, Y. 2008. Extraordinary denudation in the Sichuan Basin: insights from low-temperature thermochronology adjacent to the eastern margin of the Tibetan Plateau. Journal of Geophysical Research 113, B04409. doi: 10.1029/2006/JB004739.Google Scholar
Rowley, D. B., Xue, F., Tucker, R. D., Peng, Z. X., Baker, J. & Davis, A. 1997. Ages of ultrahigh pressure metamorphism and protolith orthogneisses from the eastern Dabie Shan: U/Pb zircon geochronology. Earth & Planetary Science Letters 151 (3–4), 191–203.Google Scholar
Şengör, A. M. C. 1985. Geology: East Asian tectonic collage. Nature 318 (6041), 16–7.CrossRefGoogle Scholar
Sharp, W. D. & Clague, D. A. 2006. 50-Ma initiation of Hawaiian-Emperor bend records major change in Pacific plate motion. Science 313 (5791), 1281–4.Google Scholar
Shen, C., Mei, L., Min, K., Jonckheere, R., Ratschbacher, L., Yang, Z., Peng, L. & Liu, Z. 2012. Multi-chronometric dating of the Huarong granitoids from the middle Yangtze Craton: implications for the tectonic evolution of eastern China. Journal of Asian Earth Sciences 52 (3), 73–87.Google Scholar
Shen, C., Mei, L., Peng, L., Chen, Y., Yang, Z. & Hong, G. 2011. LA-ICPMS U–Pb zircon age constraints on the provenance of Cretaceous sediments in the Yichang area of the Jianghan Basin, central China. Cretaceous Research 34 (3), 172–83.Google Scholar
Shen, C. B., Mei, L. F. & Xu, S. H. 2009. Fission track dating of Mesozoic sandstones and its tectonic significance in the Eastern Sichuan Basin, China. Radiation Measurements 44 (9), 945–9.CrossRefGoogle Scholar
Tada, R., Zheng, H. & Clift, P. D. 2016. Evolution and variability of the Asian monsoon and its potential linkage with uplift of the Himalaya and Tibetan Plateau. Progress in Earth & Planetary Science 3 (1), 1–26.Google Scholar
Tapponnier, P., Zhiqin, Xu, Roger, F., Meyer, B., Arnaud, N., Wittlinger, G. & Jingsui, Y. 2001. Oblique stepwise rise and growth of the Tibet plateau. Science 294 (5547), 1671–7.Google Scholar
Tian, Y., Kohn, B. P., Gleadow, A. J. W. & Hu, S. 2013. Constructing the Longmen Shan eastern Tibetan Plateau margin: insights from low-temperature thermochronology. Tectonics 32 (3), 576–92.Google Scholar
Tian, Y., Kohn, B. P., Hu, S. & Gleadow, A. J. W. 2015. Synchronous fluvial response to surface uplift in the eastern Tibetan Plateau: implications for crustal dynamics. Geophysical Research Letters 42 (1), 29–35.Google Scholar
Tian, Y., Kohn, B. P., Zhu, C., Xu, M., Hu, S. & Gleadow, A. J. W. 2012. Post-orogenic evolution of the Mesozoic Micang Shan Foreland Basin system, central China. Basin Research 24 (1), 70–90.Google Scholar
Wang, X., Zattin, M., Li, J., Song, C., Peng, T., Liu, S. & Liu, B. 2011. Eocene to Pliocene exhumation history of the Tianshui-Huicheng region determined by apatite fission track thermochronology: implications for evolution of the northeastern Tibetan Plateau margin. Journal of Asian Earth Sciences 42 (1–2), 97–110.Google Scholar
Wu, F. Y., Lin, J. Q., Wilde, S. A., Zhang, X. O. & Yang, J. H. 2005. Nature and significance of the Early Cretaceous giant igneous event in eastern China. Earth & Planetary Science Letters 233 (1), 103–19.Google Scholar
Wu, T., Xiao, L. & Ma, C. 2016. U-Pb Geochronology of detrital and inherited zircons in the Yidun Arc Belt, Eastern Tibet Plateau and its tectonic implications. Journal of Earth Science 27 (3), 461–73.CrossRefGoogle Scholar
Xia, L. Q., Xia, Z. C., Xiang-Min, L. I., Zhong-Ping, M. A. & Xue-Yi, X. U. 2008. Petrogenesis of the Yaolinghe Group, Yunxi Group, Wudangshan Group volcanic rocks and basic dyke swarms from eastern part of the South Qinling Mountains. Northwestern Geology 41 (3), 1–29.Google Scholar
Xie, G., Mao, J. & Zhao, H. 2011. Zircon U–Pb geochronological and Hf isotopic constraints on petrogenesis of Late Mesozoic intrusions in the southeast Hubei Province, Middle–Lower Yangtze River belt (MLYRB), East China. Lithos 125 (1–2), 693–710.CrossRefGoogle Scholar
Xiong, F., Ma, C., Jiang, H. & Zhang, H. 2016. Geochronology and petrogenesis of Triassic high-K Calc-Alkaline granodiorites in the East Kunlun Orogen, West China: juvenile lower crustal melting during post-collisional extension. Journal of Earth Science 27 (3), 474–90.Google Scholar
Yang, Z. 2014. Geochronologic constraints on tectonics of the Qin and Daba Mountains. PhD Thesis. Technische Universität Bergakademie Freiberg, Freiberg, Germany. Published thesis.Google Scholar
Yang, Z., Ratschbacher, L., Jonckheere, R., Enkelmann, E., Dong, Y., Shen, C., Wiesinger, M. & Zhang, Q. 2013. Late-stage foreland growth of China's largest orogens (Qinling, Tibet): evidence from the Hannan-Micang crystalline massifs and the northern Sichuan Basin, central China. Lithosphere 5 (4), 420–37.Google Scholar
Yuan, D. Y., Ge, W. P., Chen, Z. W., Li, C. Y., Wang, Z. C., Zhang, H. P., Zhang, P. Z., Zheng, D. W., Zheng, W. J. & Craddock, W. H. 2013. The growth of northeastern Tibet and its relevance to large-scale continental geodynamics: a review of recent studies. Tectonics 32 (5), 1358–70.CrossRefGoogle Scholar
Yue, S. W., Deng, X. H. & Bagas, L. 2014. Geology, isotope geochemistry, and ore genesis of the Yindonggou Ag–Au(–Pb–Zn) deposit, Hubei Province, China. Geological Journal 49 (4–5), 442–62.Google Scholar
Zhang, C., Ma, C. Q. & Holtz, F. 2010. Origin of high-Mg adakitic magmatic enclaves from the Meichuan pluton, southern Dabie orogen (cental China): implications for delamination of the lower continental crust and melt–mantle interaction. Lithos 119 (3–4), 467–84.Google Scholar
Zhang, C., Ma, C. Q., Liao, Q. A., Zhang, J. Y. & She, Z. B. 2011. Implications of subduction and subduction zone migration of the Paleo-Pacific Plate beneath eastern North China, based on distribution, geochronology, and geochemistry of Late Mesozoic volcanic rocks. International Journal of Earth Sciences 100 (7), 1665–84.Google Scholar
Zhang, P., Miao, Y., Zhang, Z., Lu, S., Zhang, Y., Chen, H., Li, X., Miao, Q., Feng, W. & Ou, J. 2013. Late Cenozoic sporopollen records in the Yangtze River Delta, East China and implications for East Asian summer monsoon evolution. Palaeogeography Palaeoclimatology Palaeoecology 388 (6), 153–65.Google Scholar
Zhang, Y. Q., Vergely, P. & Mercier, J. 1995. Active faulting in and along the Qinling Range (China) inferred from SPOT imagery analysis and extrusion tectonics of south China. Tectonophysics 243 (1), 69–95.CrossRefGoogle Scholar
Zhang, Y., Zhang, J. & Huaikun, L. I. 2013. Zircon U-Pb geochronology of the meta-acidic volcanic rocks from the Wudangshan Group, Southern Qinling Mountains, Central China. Acta Geologica Sinica 61 (9), 4447–55.Google Scholar
Zhang, Z. Q., Zhang, G. W., Tang, S. H. & Wang, J. H. 2002. The age of metamorphic rocks of the Wudang Group. Geology in China 29 (2), 117–25.Google Scholar
Zhang, Z. B., Shen, C. B., Shao, C. & Liu, Z. Q. 2013. Tectonothermal evolution of the eastern Tibetan Plateau Foreland: fission-track thermochronology of the southern Dabashan Fold-Thrust Belt. Journal of Earth Science 24 (4), 479–90.CrossRefGoogle Scholar
Zhao, H. X., Jiang, S. Y., Dai, B. Z., Ma, L. & Li, J. W. 2015. Geochronology and Hf isotope study of pegmatite in the Xiaoqinling Area of NW China: implication for petrogenesis and regional metamorphism. Journal of Earth Science 26 (3), 295–305.CrossRefGoogle Scholar
Zhou, B. X., Sun, T., Shen, W., Shu, L. & Niu, Y. 2006. Petrogenesis of Mesozoic granitoids and volcanic rocks in South China: a response to tectonic evolution. Episodes 29 (1), 26.Google Scholar
Zhou, X. M. & Li, W. X. 2000. Origin of late Mesozoic igneous rocks in Southeastern China: implications for lithosphere subduction and underplating of mafic magmas. Tectonophysics 326 (3–4), 269–328.Google Scholar
Figure 0

Figure 1. (a) Location of the Qinling–Dabie Orogenic Belt (QDOB), between the North China Craton and Yangtze Craton. (b) Relationships between the Wudang Terrain and adjacent tectonic units (modified from Ling et al.2010). (c) Simplified geological map of the Wudang area modified from Yue, Deng & Bagas (2014) and sample locations. F1: Shiyan fault. (d) Sketch map of tectonic profiles A–B.

Figure 1

Figure 2. Stratigraphic columns of the Wudang Complex and its adjacent areas (modified from Dong & Santosh, 2016). No vertical scale.

Figure 2

Table 1. Compilation of isotopic ages in the Wudang area

Figure 3

Table 2. Results of fission-track analysis of apatite from the Wudang Complex

Figure 4

Figure 3. Mean track length (left) and that after c-axis correction (right) (μm) vs apatite fission-track age of the Wudang Complex.

Figure 5

Figure 4. AFT age–elevation relationship in the Wudang area.

Figure 6

Figure 5. Onset ages of apatite cooling analysed by Track Age Spectrum Calculation (TASC; Belton & Raab, 2010).

Figure 7

Figure 6. Low-temperature thermal history and confined track-length distribution modelling by the HeFTy 1.8.2 software (Ketcham, 2005; Ketcham et al.2009) based on AFT data. D, determined apatite fission-track age (in Ma with 1σ error) and mean confined track length (in μm with standard deviation). M, modeled apatite fission-track age and mean confined track length. N, number of measured confined track lengths. GOF is the Kolmogorov–Smirnov test, assessing the fit between the modelled and measured results, with thresholds of 0.05 and 0.50 for good and acceptable fits (Ketcham, 2005).

Figure 8

Figure 7. Cooling paths for the Wudangshan Complex using multiple thermochronological methods including zircon U–Pb, 40Ar–39Ar, ZHe and AFT. The data are shown in Table 1 and Figure 1c.

Figure 9

Figure 8. (a) Simplified geological map showing the regional denudation event after c. ~15 Ma. Reference codes are [1] = Clark et al. (2005); [2] = Ouimet et al. (2010); [3] = Tian et al. (2013); [4] = Arne et al. (1997); [5] = Deng et al. (2013); [6] = Shen, Mei & Xu (2009); [7] = Zhang et al. (2006); [8] = Tian et al. (2012); and Yang et al. (2013); [9] =Wang et al. (2011); [10] = Enkelmann et al. (2006); [11] = Lin et al. (2010); and [12] = Liu et al. (2013). (b) Possible geodynamic mechanism of the late-Cenozoic tectonic and climate events. (c) Discontinuity of Lushi basin located in the northeast of the Wudang Terrain between Eocene and Neogene. Location of Lushi basin is shown in Figure 1b.