From these facts, Nakajima and Matsuzawa (2017) concluded that the differences in the depths of elastically weakened parts of crust probably result in a first-order spatial variation in surface deformation, which is in agreement with our discussion through the correlation between the coda Q, the strain rate, and the S-wave velocity.
Basin and Range-associated stretching of large parts of crust below southwestern United States and northwestern Mexico started around 16 million years ago and the region is still spreading.
In this case the ductile lower part of the crust is flowing away from the areas of thickened (unextended) crust towards thinner regions in the way that might be anticipated given the gravitational potential, and similar to the situation highlighted by Clark and Royden (2000).
The region was subsequently shortened, probably in a northeast southwest direction, with most shortening accommodated in the seismically reflective, probably oceanic part of the crust, and little or no shortening in the block-faulted, and extended continental crust.
Finally, synthetic data had to be time corrected (zero-offset) to compensate for errors in the overall velocity model, source depth, etc. Fault plane solutions of earthquakes occurring in the brittle part of the crust are expressions of the present regional stress field, and how these stresses act on existing structures in the crust.
That meant the zircons formed in a cool part of the crust.
The middle part of the crust is characterized by a heterogeneous zone with P velocities of nearly 6 to 6.3 km per second.
One possibility is that part of the crust was knocked off Ceres in a cosmic impact, exposing hard ice beneath, which vaporises in sunlight.
Newly formed sea floor becomes part of that crust.
The shallow part of the crust beneath the Marmara Sea shows significant lateral velocity variations.
