Evidence from Earthquake Data for a Partially Molten Crustal Layer in Southern Tibet-Reference-Cited by-同舟云学术

Evidence from Earthquake Data for a Partially Molten Crustal Layer in Southern Tibet

Published:1996-12-06 Issue:5293 Volume:274 Page:1692-1694
ISSN:0036-8075
Container-title:Science
language:en
Short-container-title:Science

Author:

Kind Rainer¹,Ni James²,Zhao Wenjin³,Wu Jianxin²,Yuan Xiaohui¹,Zhao Lianshe⁴,Sandvol Eric⁵,Reese Chris²,Nabelek John⁶,Hearn Thomas²

Affiliation:

1. R. Kind and Xiaohui Yuan, GeoForschungsZentrum Potsdam, 14473 Potsdam, Germany.

2. James Ni, Jianxin Wu, C. Reese, T. Hearn, Department of Physics, New Mexico State University, Las Cruces, NM 88003, USA.

3. Wenjin Zhao, Chinese Academy of Geological Sciences, Beijing, China

4. Lianshe Zhao, Institute for Geophysics, University of Texas at Austin, Austin, TX 78759, USA.

5. E. Sandvol, Department of Geological Sciences, Cornell University, Ithaca, NY 14853, USA.

6. J. Nabelek, College of Oceanography, Oregon State University, Corvalis, OR 97331, USA.

Publisher

American Association for the Advancement of Science (AAAS)

Subject

Multidisciplinary

Reference11 articles.

1. Nelson K. D., et al., Science 274, 1684 (1996).

2. Before processing the data the ground displacement was restored at all broadband and short period stations. Each seismogram was rotated from the standard vertical north and east coordinate system into a ray system [Longitudinal ( L ) and T components] using the eigenvalues of the covariance matrix for the computation of the rotation angles at a time window following the P -wave arrival. The L and Q components result from a rotation of Z (vertical) and R (radial) around the angle of incidence of the P wave. The Q component is perpendicular to the incoming P phase in the plane of incidence and contains mostly SV energy and little P -wave energy. Source equalization was accomplished by deconvolution of the Q component with the P wave of the L component.

3. Kind R., Kosarev G. L., Peterson N. V., Geophys. J. Int. 121, 191 (1995).

4. Haskell N. A., J. Geophys. Res. 67, 4751 (1990).

5. Trace A36 results from averaging receiver functions from BB10 BB36 and SP12 and trace A18 is an averaging of receiver functions from stations BB34 BB18 and BB20.

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