Crustal and upper mantle structure beneath the northeastern Tibetan Plateau from joint analysis of receiver functions and Rayleigh wave dispersions

Zheng, Deyin; Li, Hongyi; Shen, Yang; Tan, Jieqing; Ouyang, Longbin; Li, Xinfu

doi:10.1093/gji/ggv469

Cited by 34 publications

(31 citation statements)

References 38 publications

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“…However, our current V SH model could provide more details on the QOB region with high station coverage compared to the previous V SH model (Li et al, ). Low velocities characterize the crust and uppermost mantle beneath the QOB and the SGT (Figures and ), which is consistent with the slow P wave velocity (Li et al, ; Lei & Zhao, ), slow SV wave velocity from earthquake surface wave tomography (Li et al, ) and from joint inversion of receiver functions and Rayleigh wave dispersions (Zheng et al, ). Li et al () also observed middle‐ to lower‐crustal low SV wave velocity in this area from ambient noise tomography.…”

Section: Resultssupporting

confidence: 76%

Lithospheric SH Wave Velocity Structure Beneath the Northeastern Tibetan Plateau From Love Wave Tomography

Xiao

2019

JGR Solid Earth

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The northeastern (NE) Tibetan plateau has been a prime site to understand the dynamic processes responsible for the rise and lateral growth of the Tibetan plateau. Here we construct a high‐resolution lithospheric scale isotropic SH wave velocity model (down to the depth of 130 km) for the NE Tibetan plateau and its adjacent regions based on the measurements of fundamental‐mode Love wave dispersions (20–100 s) with seismic data recorded by ChinArray II and China Digital Seismic Array using two‐plane wave method. Prominent slow SH wave velocity (VSH) is observed in the midlower crust of the NE Tibetan plateau, specifically in the Qilian Orogenic Belt and the Songpan‐Ganzi Terrane regions, coincident with previously indicated significantly slow SV wave velocity (VSV), probably implying the existence of partial melts in the midlower crust. This low SH wave velocity anomaly could be traced down to the uppermost mantle, indicating a weak and warm lithosphere, which we interpret as a consequence of asthenosphere upwelling after lithospheric mantle removal in the NE Tibetan plateau. The asthenosphere upwelling and associated deep‐seated thermal buoyancy could explain the occurrence of partial melting in the mid‐lower crust and account for parts of high elevations in the NE Tibetan plateau. The western Qinling orogenic belt is characterized with a high velocity anomaly in most of lithosphere, which is inconsistent with the existence of channel flow within the lithosphere along the Qinling orogenic belt from the Tibetan plateau.

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Section: Resultssupporting

confidence: 76%

Lithospheric SH Wave Velocity Structure Beneath the Northeastern Tibetan Plateau From Love Wave Tomography

Xiao

2019

JGR Solid Earth

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“…The estimated crustal thicknesses were further interpolated into meshed 0.2° × 0.2° grids of the study area (Figure a). The crustal thickness varies from ∼65 km in the NETP to ∼40 km in the western NCC (Figure ), which is consistent with previous estimates from the H ‐ κ stacking method [e.g., Li et al ., , , ; Pan and Niu , ; Tian and Zhang , ; H. Wang et al ., ; Wang et al ., ; X. Wang et al ., ; W. Wang et al ., ; Xu et al ., ; Zheng et al ., ] and active‐source seismic profiles [e.g., Jia et al ., ; Liu et al ., ; Teng et al ., ; C. Y. Wang et al ., ; S. J. Wang et al ., ]. A difference in the Moho depth is observed from the QLT to Alxa block by as much as 10 km across the HF and NQF (Figure ).…”

Section: Resultsmentioning

confidence: 99%

“…These general features agree well with previous studies [e.g., Bao et al ., ; Cheng et al ., ; Jiang et al ., ; Li et al ., , , ; Yang et al ., ; Zhang et al ., ; Zheng et al ., ]. For example, the LVZs in the northern SGT, southwestern WQT, and western QLT were also revealed by the surface wave tomography studies [ Bao et al ., ; Jiang et al ., ; Li et al ., , ], but at lower resolution.…”

Section: Resultsmentioning

confidence: 99%

“…We also used a simple initial model with a constant shear wave velocity of 4.6 km/s, a V p / V s ratio of 1.75, and a density of 3.3 kg/m 3 from the surface down to 100 km depth to evaluate the error of our velocity model [e.g., Zheng et al ., ]. The joint inversion results for representative stations 63018 and 63041 are displayed in Figure .…”

Section: Methodsmentioning

confidence: 99%

“…Among them, three models have received the most attention: rigid block extrusion [ Tapponnier and Molnar , ; Tapponnier et al ., ], continuous deformation of the entire lithosphere [ England and McKenzie , ; England and Houseman , ], and channel flow in the lower crust [ Clark and Royden , ; Royden et al ., ]. Tomography studies [e.g., Bao et al ., ; Cheng et al ., ; Jiang et al ., ; Li et al ., , , ; Yang et al ., ; Zhang et al ., ; Zheng et al ., ] and active‐source seismic profiling [e.g., Liu et al ., ; Zhang et al ., ] revealed low‐velocity zones (LVZs) in the crust beneath NETP, which seemed to support the channel flow model. However, the extent and magnitude of the LVZs beneath NETP are still poorly constrained, because the previous tomographic results have a limited spatial resolution.…”

Section: Introductionmentioning

confidence: 99%

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Three‐dimensional lithospheric S wave velocity model of the NE Tibetan Plateau and western North China Craton

Xingchen

Ding

et al. 2017

JGR Solid Earth

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We present a new 3‐D lithospheric Vs model for the NE Tibetan Plateau (NETP) and the western North China Craton (NCC). First, high‐frequency receiver functions (RFs) were inverted using the neighborhood algorithm to estimate the sedimentary structure beneath each station. Then a 3D Vs model with unprecedented resolution was constructed by jointly inverting RFs and Rayleigh wave dispersions. A low‐velocity sedimentary layer with thicknesses varying from 2 to 10 km is present in the Yinchuan‐Hetao graben, Ordos block, and western Alxa block. Velocities from the middle‐lower crust to the uppermost mantle are generally high in the Ordos block and low in the Alxa block, indicating that the Alxa block is not part of the NCC. The thickened crust in southwestern Ordos block and western Alxa block suggests that they have been modified. Two crustal low‐velocity zones (LVZs) were detected beneath the Kunlun Fault (KF) zone and western Qilian Terrane (QLT). The origin of the LVZ beneath the KF zone may be the combined effect of shear heating, localized asthenosphere upwelling, and crustal radioactivity. The LVZ in the western QLT, representing an early stage of the LVZ that has developed in the KF zone, acts as a decollement to decouple the deformation between the upper and lower crust and plays a key role in seismogenesis. We propose that the crustal deformation beneath the NETP is accommodated by a combination of shear motion, thickening of the upper‐middle crust, and removal of lower crust.

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Radial anisotropy beneath northeast T ibet, implications for lithosphere deformation at a restraining bend in the K unlun fault and its vicinity

Murphy

et al. 2016

Geochem. Geophys. Geosyst.

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Three‐dimensional shear wave velocity and radial anisotropy models of the crust and upper mantle beneath the NE Tibetan plateau are constructed from new measurements of Love wave dispersions (20–77s) and previously obtained Rayleigh wave dispersions (20–87s) using a two‐plane‐wave method. The mid‐lower crust is characterized with positive anisotropy (VSH > VSV) with large strength beneath the Qinling and Qilian Mountains and small values beneath the Anyemaqen Mountain. The large positive anisotropy can be explained by horizontal alignment of anisotropic minerals in the mid‐lower crust due to crustal flow. The mantle lithosphere above 90 km is largely isotropic while weak positive anisotropy appears beneath 90 km, which probably marks the lithosphere‐asthenosphere boundary (LAB). A low shear wave velocity anomaly and relatively negative radial anisotropy are imaged in the entire lithosphere beneath the restraining bend in the eastern Kunlun fault, consistent with a weak lithosphere experiencing vertical thickening under horizontal compression. The asthenosphere at the restraining bend is characterized by significant low velocity and positive radial anisotropy, reflecting that the asthenosphere here is probably hotter, has more melts, and deforms more easily than the surrounding region. We propose that the lithosphere at the restraining bend was vertically thickened and subsequently delaminated locally, and induced asthenosphere upwelling. This model explains the observations of velocity and anisotropy anomalies in the lithosphere and asthenosphere as well as geological observations of rapid rock uplift at the restraining bend of the Kunlun fault.

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Crustal and upper mantle structure beneath the northeastern Tibetan Plateau from joint analysis of receiver functions and Rayleigh wave dispersions

Cited by 34 publications

References 38 publications

Lithospheric SH Wave Velocity Structure Beneath the Northeastern Tibetan Plateau From Love Wave Tomography

Lithospheric SH Wave Velocity Structure Beneath the Northeastern Tibetan Plateau From Love Wave Tomography

Three‐dimensional lithospheric S wave velocity model of the NE Tibetan Plateau and western North China Craton

Radial anisotropy beneath northeast T ibet, implications for lithosphere deformation at a restraining bend in the K unlun fault and its vicinity

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