Zining Wang
Xiaosong Xiong
Guowei Wu- Chinese Academy of Geological Sciences, Beijing, China
The collision between the Indian and Eurasian plates continues to drive significant deformation and uplift within the interior of the Tibetan Plateau, together with its outward expansion along the margins. In particular, the North Qilian Shan fold-thrust belt (NQLS) and the Hexi Corridor basins (HXBS) represent the northernmost region of the northeastern Tibetan Plateau. This area serves as a natural laboratory for deciphering mechanisms of crustal deformation and thickening along the plateau’s margins. Specifically, the northeastern Tibetan Plateau has been attributed to 1) southward underthrusting of the Asian lithosphere, 2) distributed shortening and crustal thickening, 3) vertical inflation of the Tibetan crust due to mid-lower crustal channel flow, and 4) intracontinental subduction facilitated by large-scale strike–slip faults. The exact mechanism underlying the most concentrated convergent stress in the western segment of NQLS–HXBS remains a subject of debate. To address this uncertainty, we gathered seismic data along a 130-km-long linear array that extends northward from NQLS, traversing the Jiuquan Basin and reaching the Huahai Basin. Our analysis, conducted through the receiver function method, reveals intriguing findings. The Moho depth deepens from 45–50 km beneath the Huahai Basin to 55–60 km beneath NQLS. Notably, a double Moho structure emerged, marked by a distinctive near-flat positive amplitude at a depth of 45–50 km beneath NQLS within a distance of 0–50 km. Our study presents a comprehensive analysis of the crust-scale deformation mechanism, shedding light on the following key aspects: 1) the development of a decollement at 12–20 km depth decoupling the upper and lower crust; 2) deformation of the upper crust occurring through south-dipping brittle thrust faults, while the lower crust features imbricate structures and duplexes; 3) evidence pointing to the underthrusting of the Beishan Block beneath NQLS, indicated by the double Moho beneath NQLS; and 4) the formation of a Moho ramp beneath the Jiuquan Basin, facilitating the transfer of shortening stress from beneath NQLS and HXBS to the north. In the context of the western segment of NQLS and HXBS, our speculation is that coupled distributed shortening and Beishan Block subduction beneath NQLS work in tandem to accommodate crustal deformation.
1 Introduction
The collision and continued convergence of the Indian and Eurasian plates since ca. 55 Ma have resulted in substantial deformation and uplift within the interior of the Tibetan Plateau, together with the outward expansion of the plateau along its margins (e.g., Molnar and Tapponnier, 1975; Tapponnier et al., 2001; Yin, 2000; Yin, 2010; ; Zhao et al., 2010; Zuza et al., 2018; Xiong et al., 2022). This collision has significantly impacted both the topography and climate of the surrounding regions (Zhang et al., 2004). However, the precise manner in which the Tibetan crust accommodates the convergence of the Indian and Eurasian plates, leading to the development of the Tibetan Plateau, remains a subject of intense debate (e.g., Cheng et al., 2019; Clark and Royden, 2000; Yin and Harrison, 2000; Tapponnier et al., 2001; van Hinsbergen et al., 2011; van Hinsbergen et al., 2012; Yakovlev and Clark, 2014; Ingalls and Stedman, 2016; Zuza et al., 2016; Zheng et al., 2017). Moreover, different segments of the Tibetan Plateau margins may exhibit varying deformation mechanisms, particularly across the northeastern Tibetan Plateau margin that stretches across strike for >1,000 km. (Lin et al., 2011; Duvall et al., 2013).
NQLS and the HXBS comprise the northernmost margin of the Tibetan Plateau. This contractional thrust-fold belt and foreland basin system represent an area of concentrated stress resulting from the convergence of the Indian and Eurasian plates (Xiong et al., 2019). Understanding the geometric and kinematic characteristics of the crustal structure in this region is essential for deciphering the deep interrelation between the Tibetan Plateau and the Eurasian plate. This knowledge holds the potential to significantly enhance our comprehension of continental tectonics (Yin et al., 2002; Molnar, 1988; Zhang et al., 2004; Zhou et al., 2006; Yin, 2010; Lease et al., 2012; Craddock et al., 2011; Craddock et al., 2014; Zuza et al., 2019).
Since the 1970s (Burke and Dewey, 1973; Molnar and Tapponnier, 1975), numerous end-member models have been proposed to explain the formation of the Tibetan Plateau, as a result of intensive study (Figure 1). In the northeastern Tibetan Plateau, these models include (1) Cenozoic underthrusting of the Asian lithosphere beneath the Tibetan Plateau (Willett and Beaumont, 1994; Kind et al., 2002; Zhao et al., 2011; Feng et al., 2014; Ye et al., 2015); (2) coupled distributed crustal shortening and underthrusting of the Alxa Block beneath Tibet, accounting for the observed crustal shortening and thickness distribution (England and Houseman, 1986; Dewey et al., 1997; Huang et al., 2018; Xiong et al., 2019; Zuza et al., 2019); (3) vertical inflation of the Tibetan crust due to lateral mid-lower crustal channel flow (Zhao and Morgan, 1987; Bird, 1991; Royden et al., 1997; Clark and Royden, 2000); and (4) intracontinental subduction facilitated by large-scale strike–slip faults (Zuza et al., 2016; Wu et al., 2023b).
FIGURE 1. Crustal growth model map of the northeastern Tibetan Plateau (modified from Zuza et al., 2019; Wu GW. et al., 2023).
These tectonic models offer specific predictions regarding the location, timing of deformation, and kinematics of crustal structures in the northeastern Tibetan Plateau (Lease et al., 2012; He, 2020; Zuza et al., 2016; 2019). Therefore, crustal-scale seismic imaging can provide insights into the dominant deformation mechanism along the northern margin of the Tibetan Plateau. Despite prolific geophysical research conducted over recent decades on the northeastern Tibetan Plateau, the mechanisms driving crustal deformation remain contentious. Given that the west-to-east-trending NQLS and HXBS stretch over a span of 1,000 km, the crustal deformation mechanism may indeed vary across different segments.
In the western segment, the Moho depth is notably deeper than that in the middle-eastern Qilian Shan fold-thrust belt, with a maximum depth of 73 km beneath Hala Lake, as substantiated by studies (Cui et al., 1995; Gao et al., 1999; Jolivet et al., 2001; Huang et al., 2021). This observation supports the hypothesis that the most concentrated convergent stress is accommodated through crustal deformation in the western segment. To address this question, we gathered seismic data from a linear array spanning 130 km, extending northward from NQLS, traversing the entire Jiuquan Basin, and reaching the Huahai Basin. The data were continuously recorded over approximately 30 days using the Smart Solo IGU-16 HR 3C geophones, which are three-component geophones with a dominant frequency of 5 Hz (Figure 2B). The dense seismic array comprises 261 short-period geophones spaced at 500-m intervals. Through receiver function processing of the seismic observations, we have unveiled the crustal structure beneath the North Qilian–Huahai Basin and gained insights into the crustal deformation mechanism within the western segment of NQLS–HXBS.
FIGURE 2. (A) Tectonic fault map of the northeastern Tibetan Plateau, including the Qilian Shan and surrounding regions (modified from Gao et al., 2013; Zuza et al., 2016). The red rectangle shows the location of Figure 2B. (B) Geologic map of the North Qilian Shan fold-thrust belt and the Huahai Basin (modified from Ye et al., 2021). The blue line segment represents the dense-seismic array. The red dashed line represents the CMP line. The green dashed line represents the MT line. The black dashed line represents the DSS line. (C) Cross section along line (A, B) in Figure 2B. CMF, Changma Fault; NQLF, North Qilian Fault; HXF, Hanxia Fault; NBT, North Border Thrust.
2 Geological setting
The northeastern Tibetan Plateau has an average elevation of ∼4.5 km, with the high topography decreasing rapidly to <1.5 km in HXBS to the north (Figure 2). Previous geophysical observations indicate that the Moho depth ranges from 55 to 73 km (Zhao et al., 2001; Yue et al., 2012; Gao et al., 2013; Yuan et al., 2013; Xu et al., 2018; Wu et al., 2023b). Additionally, the relatively stable crust beneath HXBS has a thickness of approximately 42–51 km (Cui et al., 1995; Xiong et al., 2019).
The NQLS formed as an accretionary complex due to the closure of the Qilian Ocean in the Early Paleozoic and was later reactivated following the Indian–Eurasian plate collision in the Cenozoic. The present-day tectonic belt, located between the northern Alxa Block–Beishan Block and the southern Middle Qilian Block, follows a narrow NW–SE-trending structure. This belt is truncated by the Altyn Tagh faults to the northwest (Figure 2). The Qilian Shan fold-thrust belt exhibits volcanic and magmatic rock distributions from the Paleoproterozoic to the early Paleozoic (Wu et al., 2023a). Since the Cenozoic era, NQLS has been involved in crustal thickening and deformation, marking its northernmost extension onto the Tibetan Plateau.
The Jiuquan Basin is situated at the western terminus of HXBS, and the Jiuquan Basin is bounded by the Jiayuguan fault, Altyn Tagh fault, Qilian Shan North Margin fault, and Heishan fault. Sedimentation in the Jiuquan Basin initiated in the Mesozoic, and this northwest-trending basin was subsequently influenced by the uplift of NQLS. Deep seismic reflection profiles reveal that the thickness of the Cenozoic sedimentary cover ranges between 1.5 and 2 km (Song et al., 2001; Huang et al., 2018).
The Huahai Basin lies to the north of the Jiuquan Basin bounded by the Kuantan Shan fault, Heishan fault, and Jintana Shan fault. Initially part of the Dunhuang Block, a relatively stable Precambrian block, the Huahai Basin is covered by Mesozoic–Cenozoic sediments with a sedimentary thickness of 5 km (Chen and Yang, 2010). Paleozoic granitoids have locally intruded into the sedimentary cover (refer to Figure 2).
3 Methods and principles
In this study, we deployed a dense array of 261 Smart Solo 16 HR 3C nodal short-period seismometers for observations. These were positioned with an average spacing of 500 m in the field and operated for approximately 30 days. A receiver function is a time sequence derived from deconvolving the radial component of teleseismic P-waves. This process yields the vertical component that represents P-to-S wave conversion. Receiver function analysis is an effective approach for imaging crustal structures. By stacking multiple receiver functions with similar ray paths, the dense nodal array enhances the vertical resolution of receiver function images and boosts high-frequency signals (Langston, 1979; Xu et al., 2018; Ammon et al., 1990; Xu et al., 2020; Tian et al., 2021).
After obtaining the raw seismic data, several steps are typically followed to extract receiver functions. This process involves filtering, receiver function separation, and deconvolution. In practical research, receiver function studies usually focus on earthquakes with a magnitude of 5 or higher. For data preprocessing, earthquakes within 30°–90° epicentral distances (refer to Figure 3) were selected. We acquired a total of 47 seismic events with a magnitude (Ms) of ≥5 and epicentral distances between 30° and 90° from the IRIS website during the data acquisition period. Data for each station were extracted from 900 s after the origin time. Raw seismic data at stations contain not only information about the subsurface medium structure but also various types of noise from surface human activities, unrelated to underground structures and tectonics. Hence, noise filtering is essential, often using low-pass and band-pass filters. After removing the instrument response, the data were down-sampled from 500 Hz to 50 Hz (0.002 s–0.02 s), and band-pass filtering was conducted within the frequency range of 0.5 Hz–10 Hz. The raw three-component data coordinate system was rotated from NEZ to RTZ. Ray parameters and theoretical arrival times were computed. After rotation, P-wave energy concentrated mainly in the radial R component, while azimuthal energy in the tangential T component. Finally, time-domain deconvolution algorithm calculations were performed (Ligorria and Ammon, 1999), using a Gaussian filter factor 2. This iterative deconvolution subtracts the radial component of observed seismic records from calculated theoretical receiver functions, iteratively updating differences until either iterations exceed a threshold or differences fall within a given tolerance range (refer to Figure 4). Computed receiver functions were then selected, focusing on data with clear P-wave phases, distinct seismic phases, and good Ps–PpPs consistency.
FIGURE 3. Seismic distribution map (the black triangle represents the location of the station, red circles represent the earthquake of magnitude 5–5.5, and blue circles represent the earthquake of magnitude 5.5 or above).
FIGURE 4. Receiver function image (receiver function of all stations in a single seismic event).
The common midpoint (CMP) stacking concept, initially introduced by Dueker and Sheehan (1997) for reflection waves, was adapted for imaging converted waves in receiver functions. This method corrects and stacks slanting receiver functions dynamically to create a wavefield image of the interface below the array. Building on this, Zhu and Kanamori (2000) proposed the CCP stacking method for receiver functions. Based on a given velocity model, each receiver function is projected back into the spatial domain using ray paths, followed by stacking imaging in the spatial domain (Chen et al., 2022; Cheng et al., 2023). In our study, we applied the CCP stacking method to stack the processed receiver functions. The method assumes a horizontally layered medium beneath the station, mapping amplitude information of processed and deconvolved receiver functions along the ray path to the conversion point. The amplitudes of receiver functions at the conversion point are stacked to obtain the medium structure below the station (refer to Figure 4).
For time–depth conversion, we utilized the reference velocity model IASP91, with a rectangular shape and a maximum depth of 100 km (Chen et al., 2022). Bins were spaced at intervals of 5 km. The time-to-depth conversion used a depth interval of 1 km, with intervals of 2 km from 0 km to 100 km. After stacking receiver functions with these settings, the CCP profile image was generated (refer to Figure 5).
FIGURE 5. CCP superposition profile. The red colors indicate positive amplitudes (increased velocity downward); the blue colors indicate negative amplitudes (decreased velocity downward). Decollement is marked by red crosses and labeled as D1. Moho is marked by black and green crosses and labeled as L1, M1, and M2. The ductile shear zone is marked by blue crosses and labeled as L2.
4 Results
In the CCP image, red colors indicate positive amplitudes (increased velocity downward), while blue colors indicate negative amplitudes (decreased velocity downward). Our new seismic imaging reveals the following features.
A continuous positive amplitude stretches throughout the section at depths of 0–5 km; it deepens to 8 km in the contact zone of North Qilian and Jiuquan Basin and the center of the Huahai Basin; two distinct large negative amplitude bodies are visible at depths of 8–20 km below the NQLS and Jiuquan Basin; a relatively continuous positive amplitude extends at a depth of 12–20 km; the Moho, the most prominent positive velocity discontinuity, deepens from 45–50 km beneath the Huahai Basin to 55–60 km beneath NQLS; above the bottom Moho, a distinct positive amplitude at a depth of 45–50 km beneath NQLS, within 0–50 km distance, may represent the original Moho of the marginal NQLS (Figure 5).
5 Discussion
5.1 Crustal structures
The dense stations along our profile provide high-resolution images, revealing clear and strong crustal deformations from NQLS across the Jiuquan Basin to the Huahai Basin. At a depth of 20 km along the entire section, D1 is captured, exhibiting a subtle increase beneath NQLS (Figure 5). The Golmud–Ejinaqi DSS profile showed a relatively lower velocity zone at a depth of 20 km with a P-wave velocity of 5.9 km/s compared to the surrounding 6.1 km/s P-wave velocity (Cui et al., 1995). The Diaodaban–Huahai basin deep seismic reflection profile revealed a strong reflector at the depth of 3.5–4 s TWT (approximately 12 km), which could indicate the intracrustal decollement (Wu et al., 1995; Cui et al., 1995). These data consistently suggest that D1 is the main decollement in the crust, separating it into upper and lower parts. By projecting earthquakes from 1900 to 2023 located within 100 km of our profile (Figure 8) onto the seismic section, we found that seismic activities mostly occurred above 20 km depth. A cluster of earthquakes was distributed along the decollement, in alignment with geophysical observations. A continuous L1 is present at a depth of 50 km beneath the North Qilian and southern Jiuquan Basin, forming a lateral-stretching wedge with M1 below (Figure 5). Below the northern Jiuquan and Huahai basins, a near-flat M2 is distinct at depths of 45–50 km, abruptly deepening to 60 km (M1) beneath the middle Jiuquan Basin. We interpret M1 and L1 to signify a double Moho beneath NQLS, formed by the underthrusting of the North Block beneath NQLS. This double Moho was also observed in the Eastern Qilian Shan fold-thrust belt (Ye et al., 2015), representing the underthrusting of the Alxa Block beneath the Eastern Qilian Shan fold-thrust belt. In other global orogenic belts, a double Moho was detected through passive- or active-source seismic methods in West Kunlun, China, and the northern and western margins of the Yilgarn Craton, Australia (Kao et al., 2001; Kennett and Saygin, 2015). L2, preserved above M2 in the northern Jiuquan and Huahai basins, may indicate a ductile shear zone accommodating deformation in the lower crust (Figure 5).
The electrical structure of the crust shown in the MT profile (Figure 7; Xiao et al., 2012) reveals higher resistivity in NQLS compared to HXBS and beneath the Huahai Basin. The MT data display higher resistivity beneath the Huahai Basin, similar to the characteristics beneath NQLS. Three areas with lower resistivity beneath the basin, labeled C1, C2, and C3, align with the CCP image. However, the CCP image’s alignment with seismic activities is more pronounced.
To the east of our study area, a deep reflection seismic profile and a 1200-km-long deep seismic sounding were previously acquired (Cui et al., 1995; Gao et al., 1999). Comparing the crustal structures of our seismic imaging with the two active-source seismic profiles along the NNE–SSW-trending survey line (Figure 6), we find that the main crustal interferences and features are relatively consistent, further validating our observations.
FIGURE 6. Crustal structure and Moho from different studies. Deep reflection seismic image (Wu et al., 1995) is overlain by our receiver function image (transparent) showing our interpretations of Moho and intracrustal boundaries. The CMP Moho depth is shown by the yellow line (Liu et al., 2006), and the CCP Moho depths, including the double Moho, are shown by the green dashed lines. Significant velocity boundaries are labeled with Vp (km/s) (Cui et al., 1995).
5.2 Implication to the crustal deformation mechanism
Extensive research on the Qilian Shan fold-thrust belt and HXBS regarding their development, evolution, and outward expansion within the northern Tibetan Plateau has been conducted using active- and passive-source seismic observations and MT soundings (Gao et al., 2001; Xiao et al., 2012; Ye et al., 2015; Shen et al., 2020; Huang et al., 2021; Sun et al., 2021; Ye et al., 2021). Different observations have led to various proposed deformation mechanism models, yet the debate persists. Our recent seismic imaging provides evidence supporting a combination of underthrusting and decoupled crustal shortening mechanisms in the western NQLS and Jiuquan Basin.
The discovery of a double Moho (L1 and M1) in the western Qilian Shan fold-thrust belt, a characteristic geodynamic feature of underthrusting globally (Zhao et al., 1993; Kao et al., 2001; Ye et al., 2015; Xu et al., 2019), suggests the southward underthrusting of the Beishan Block–Alxa Block beneath the Qilian Shan fold-thrust belt. This underthrusting might extend at least as far as NQLS. This phenomenon has been substantiated by the electrical structure and other seismic findings (Figure 7; Gao et al., 2001; Xiao et al., 2012; Huang et al., 2021; Ye et al., 2021). Recent geophysical data increasingly confirm the stable and rigid nature of the Beishan Block, which could potentially underthrust beneath more active units. The slow-dipping nature of the North Qilian fault along the top of a high-resistivity body beneath the NQLS, as indicated by an electrical structure (Xiao et al., 2012), points toward underthrusting as the principal factor, contributing to the complex crustal structure in the northern Tibetan Plateau.
FIGURE 7. The electrical structure and deep reflection stack map (C1, C2, and C3) modified from Xiao et al. (2012) and Wu et al. (1995) are the centers of relatively low resistivity in the crust along the profile. R1, R3, R4, and R5 are the locations along the high-resistivity body at different temperatures. The red solid line represents the fault, and the red dotted line represents the boundary between the Hexi Corridor and its north. The short black line shows the seismic reflection mentioned in Wu et al. (1995) on the resistivity image. The white solid circles show the seismic activities from 1980 to 2008.
The distributed shortening model has also played a role in the crustal deformation of the northern Tibetan Plateau, as indicated by the presence of D1 in our seismic imaging. A recent deep seismic reflection profile also provided evidence for decoupled crustal deformation (Huang et al., 2021), aligning with our observations (Figure 8). Thrust faults are prevalent in NQLS, extending northward into HXBS (Zheng et al., 2013; Zuza et al., 2018; Xiong et al., 2019). Surface active fault surveys unveiled north-directed overthrusting faults that traverse through HXBS and enter the Beishan Block (Zheng et al., 2021; Wang et al., 2022). Combining our seismic imaging with earthquake distribution, we deduced that the primary mechanism accommodating upper crust deformation involves folding and northward overthrusting. Notably, several near-flat, arc-shaped positive amplitudes above the Moho suggest that duplexing plays a crucial role in lower crustal shortening. This is supported by prominent reflections recorded in deep seismic profiles (Huang et al., 2021).
FIGURE 8. The upper image is the geological section, corresponding to Panel (C) in Figure 2. And the lower image is the crustal profile of local seismic superposition (the fine lines with the arrow are the ductile shear zone, and the arrows are the extension direction of the ductile shear zone. The fine dashed lines are the brittle thrust faults in the upper crust; the fine solid lines are the imbricate structures and duplexes in the lower crust. The bold dashed line represents the decollement. The Moho and the double Moho have been marked in the figure).
Our investigation unearthed a Moho ramp within the Jiuquan Basin. Seismic phases indicate that M2 gradually deepens to approximately 50 km beneath the Huahai Basin but abruptly descends to 60 km below the Jiuquan Basin (Figure 8). Although most studies suggest gradual Moho deepening in this region, wide-angle reflection/refraction data confirm this trend (Gao et al., 2001; Huang et al., 2021; Ye et al., 2021). The concept of a lithospheric ramp, introduced by Zuza et al. (2018), posits that both underthrusting and crustal shortening have been continuously occurring since the Miocene on the same lithospheric ramp. The disrupted stair-like Moho features beneath the Jiuquan Basin, gradually deepening toward the southwest, closely resemble the lithospheric ramp model (Vergne et al., 2002; Zhou and Murphy, 2005; Hazarika et al., 2017; Lu et al., 2019; Tan et al., 2019). We contend that compressive stress generated by the Moho underthrusting ramp propagates from the Jiuquan Basin to NQLS and HXBS to the south, thereby inducing crustal deformation above this ramp. The Moho ramp model we propose strongly supports the crustal compression model in the Qilian Shan Block–Huahai Basin region (Figure 9).
FIGURE 9. Sketch of the crustal deformation patterns across the North Qilian Shan fold-thrust belt and Huahai Basin. In the cross section, bold black lines are crustal interfaces and Moho constrained by CCP stacking; dashed lines mark decollement; red lines are the brittle thrust faults in the upper crust; red dashed lines are the imbricate structures and duplexes in the lower crust; and Moho ramp is marked in the lower crust.
6 Conclusion
Drawing on our receiver function image and the analysis presented previously, we have outlined a comprehensive tectonic representation on a crustal scale that encapsulates our observations and interpretations beneath the North Qilian–Huahai Basin (Figure 9). By amalgamating our seismic imaging with additional geological and geophysical data, we propose the existence of a potential decoupling plane situated at a depth of 12–20 km. Within this framework, south-dipping brittle thrust faults govern upper crustal deformation, while imbricate structures and duplexes operate in the lower crust. Notably, we conjecture that the underthrusting of the Beishan Block beneath NQLS might be accountable for the occurrence of a double Moho. In addition, we posit that a Moho ramp could be developing beneath the Jiuquan Basin to accommodate the pronounced compression. In the western stretch of NQLS and HXBS, we propose that coupled distributed shortening and the underthrusting of the Beishan Block beneath the Qilian Shan fold-thrust belt might collaboratively contribute to the intricate crustal deformation.
Data availability statement
The original contributions presented in the study are included in the article/Supplementary Material; further inquiries can be directed to the corresponding author.
Author contributions
ZW: data curation, formal analysis, methodology, visualization, and writing–original draft. XX: conceptualization, funding acquisition, investigation, methodology, project administration, supervision, writing–original draft, and writing–review and editing. GW: data curation, investigation, methodology, visualization, and writing–original draft. ZL: investigation, visualization, and writing–original draft. ZY: formal analysis, software, and writing–original draft. ZJ: formal analysis, software, and writing–original draft.
Funding
This study was funded by the National Natural Science Foundation of China (42274134, 41774114, and 42261144669) and the China Geological Survey Project (Grant Nos DD20230229 and DD20179342).
Conflict of interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Publisher’s note
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors, and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.
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Keywords: Qilian Shan fold-thrust belt, northern Tibetan Plateau, Jiuquan Basin, receiver function, crustal deformation, double Moho
Citation: Wang Z, Xiong X, Wu G, Li Z, Ye Z and Jin Z (2023) Crustal structure and deformation mechanism of the western northeast Tibetan Plateau. Front. Earth Sci. 11:1255813. doi: 10.3389/feart.2023.1255813
Received: 09 July 2023; Accepted: 03 October 2023;
Published: 20 October 2023.
Edited by:
Jie Liao, Sun Yat-sen University, ChinaReviewed by:
Lianghui Guo, China University of Geosciences, ChinaZhongtai He, China Earthquake Administration, China
Gaofeng Ye, China University of Geosciences, China
Copyright © 2023 Wang, Xiong, Wu, Li, Ye and Jin. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Xiaosong Xiong, benxung@126.com