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Fig. 2 Global distributions of: (a) thickness of sediments; (b) depth to bottom of upper crust; (c) depth to bottom of lower crust; and (d) lithosphere-asthenosphere boundary (LAB) depth.
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The seismic reflection method has been used to map the thickness of sediments in many parts of the oceans.
Moreover, areas of gravity lows have greater thickness of sediments than areas of gravity highs.
In the CRZ, the thickness of sediments is more than 1 m, making cultivation difficult.
These include the convergence rate, the thickness of sediments, seismicity, seismic coupling, and SSEs.
Variable thickness of sediments is also apparent on the seaward horst compared to the graben at the trench axis.
The remaining area where the thickness of sediments is greater than 2 m have remained uncultivated even after 8 years of the event.
The contour (Fig. 3) shows that the thickness of sediments are concentrated towards the central and right bank of the new channel on most of the CRZ and RZ area.
The thickness of sediments between two seismites in the studied sections is almost constant (Fig. 5), implying the nearly-constant time intervals between two large earthquakes.
The total thickness of sediments significantly affects the seismic response at longer periods around the fundamental period of the studied valley sections between 1.8 and 3.6 s.
Generally speaking, the thickness of sediments around the Suibin city in the west part of the study area is about 300 m and the size of deposits is coarser than other parts.
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