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Abstract
The North China Craton (NCC) has experienced strong tectonic deformation and lithospheric thinning since the Cenozoic. To better constrain the geodynamic processes and mechanisms of the lithospheric deformation, we used a linear damped least squares method to invert simultaneously Rayleigh wave phase velocity and azimuthal anisotropy at periods of 10–80 s with teleseismic data recorded by 388 permanent stations in the NCC and its adjacent areas. The results reveal that the anomalies of Rayleigh wave phase velocity and azimuthal anisotropy are in good agreement with the tectonic domains in the study area. Low-phase velocities appear in the rift grabens and sedimentary basins at short periods. A rotation pattern of the fast axis direction of the Rayleigh wave together with a distinct low-velocity anomaly occurs around the Datong volcano. A NW–SE trending azimuthal anisotropy and a low-velocity anomaly at periods of 60–80 s are observed subparallel to the Zhangbo fault zone. The whole lithosphere domain of the Ordos block shows a high-phase velocity and counterclockwise rotated fast axis. The northeastern margin of the Tibetan plateau is dominated by a low-velocity and coherent NW–SE fast axis direction. We infer that the subduction of the Paleo-Pacific plate and eastward material escape of the Tibetan plateau mainly contribute to the deformation of the crust and upper mantle in the NCC.
Highlights
The North China Craton (NCC) is the oldest Archean craton in China where the earliest crustal rock can be dated back to 3.8 Ga [1]
Rayleigh wave phase velocity and azimuthal anisotropy at periods of 10–80 s was estimated from the teleseismic data recorded by 388 permanent stations in the NCC and its adjacent areas
Our results reveal the detailed crustal and upper mantle structures of the NCC and its adjacent areas, which provides a new reference for understanding the lithospheric deformation
Summary
The North China Craton (NCC) is the oldest Archean craton in China where the earliest crustal rock can be dated back to 3.8 Ga [1]. North China Craton was amalgamated by the collision between the eastern NCC (ENCC). Western NCC (WNCC) along the Trans-North China orogen (TNCO) until its final cratonization [2] (Figure 1a). The NCC is currently surrounded by orogenic belts formed in different geological episodes. The central Asian orogenic belt (CAOB) is a product of the closure of the Paleo-Asian ocean in the Paleozoic–Mesozoic [3]. The Qinling–Dabie orogenic belt (QDO) has been formed by the collision between the Yangtze plate and the NCC in the Triassic [2]
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