Evidence from earthquake data for a partially molten crustal layer in southern Tibet

Science

Volumn 274, Issue 5293, 1996, Pages 1692-1694

  Kind, Rainer ^a   Ni, James ^b   Zhao, Wenjin ^c   Wu, Jianxin ^b   Yuan, Xiaohui ^a   Zhao, Lianshe ^d   Sandvol, Eric ^e   Reese, Chris ^b   Nabelek, John ^f   Hearn, Thomas ^b  

^a GFZ GERMAN RESEARCH CENTRE FOR GEOSCIENCES   (Germany)

^b NEW MEXICO STATE UNIVERSITY   (United States)

^c INSTITUTE OF MINERAL RESOURCES   (China)

^d UNIVERSITY OF TEXAS AT AUSTIN   (United States)

^e Department of Population Medicine and Diagnostic Sciences   (United States)

^f OREGON STATE UNIVERSITY   (United States)

Author keywords

[No Author keywords available]

Indexed keywords

ANALYTIC METHOD; ARTICLE; CHINA; EARTHQUAKE; GEOGRAPHIC DISTRIBUTION; GEOLOGY; PRIORITY JOURNAL; VELOCITY; WAVEFORM;

CRUSTAL STRUCTURE; EARTHQUAKE DATA; INDEPTH PROJECT; PARTIALLY MOLTEN LAYER; VELOCITY STRUCTURE;

CHINA, TIBET;

EID: 0029659561     PISSN: 00368075     EISSN: None     Source Type: Journal    
DOI: 10.1126/science.274.5293.1692     Document Type: Article

References (11)

1. K. D. Nelson 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. R. Kind, G. L. Kosarev, N. V. Peterson, Geophys. J. Int. 121, 191 (1995).
4. N. A. Haskell, 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.
6. L. D. Brown et al., Science 274, 1688 (1996).
7. The two-station phase velocity dispersion of the fundamental mode Rayleigh wave was computed using programs developed by R. Herrmann. In the data analysis we first extracted the group velocity dispersion curve of the fundamental mode by applying a Gabor Transform to the recorded Rayleigh wave train. The fundamental mode Rayleigh waveforms were isolated from the recorded Rayleigh waves by applying a phase match filter.
8. J. Wu et al., Eos 76, F392 (1995).
9. L.-S. Zhao and C. Frohlich, Geophy. J. Int. 124, 525 (1996); L.-S. Zhao, M. K. Sen, P. Stoffa, C. Frohlich, ibid, 125, 355 (1996).
10. L.-S. Zhao and C. Frohlich, Geophy. J. Int. 124, 525 (1996); L.-S. Zhao, M. K. Sen, P. Stoffa, C. Frohlich, ibid, 125, 355 (1996).
11. We thank I. Billings, M, Brunner, A. Fabritius, S. Klemperer, Y. Makovksy, K. Wu, and Chinese scientists in helping to collect the seismic data used in this study. This research was funded by the National Science Foundation Grant NSF EAR-9316814.