Bulletin of the Seismological Society of America
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Bulletin of the Seismological Society of America; February 2006; v. 96; no. 1; p. 328-333; DOI: 10.1785/0120050074
© 2006 Seismological Society of America
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Probing the Southern Indian Shield with P-Wave Receiver-Function Profiles

Tai-Lin Tseng1 and Wang-Ping Chen1

1 Department of Geology, University of Illinois
1301 W. Green St., 245 NHB
Urbana, Illinois 61801-2939
tseng1{at}uiuc.edu


Figure 001
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  		Figure 1. A schematic diagram showing ray paths of major seismic phases commonly used in crustal receiver functions. P-wave receiver functions emphasize the PpPmp phase on the vertical component, whereas conventional receiver functions accentuate P-to-S conversions such Ps and PsPms on horizontal components.

 

Figure 002
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  		Figure 2. A simplified map of India showing major geologic provinces (Naqvi and Rogers, 1987) and locations of the Gauribidanur array (GBA), a lone- broadband seismograph at Hyderabad (HYB), and proprietary profiles from deep seismic sounding (DSS). The circles show approximately the areas of crust sampled by various types of receiver functions near GBA and HYB.

 

Figure 003
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  		Figure 3. Seismic profiles from event 1 (Table 1). (a) Unprocessed seismic profile and the principal component (marked as AVE, akin to the linear average) among all seismograms. (b) Profile of P-wave receiver functions after observed waveforms are deconvolved by the source wavelet. To show all the data clearly, seismic traces are equally spaced, with their principal component (AVE) also plotted.

 

Figure 004
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  		Figure 4. (a) and (b) Comparisons between the principal component of deconvolved seismograms and synthetic seismograms. For time-domain deconvolution (T.D.), we applied a Gaussian filter: G(f) = exp(–{pi}2f2/a2), where f is frequency and a is the Gaussian width (set to 5 sec–1). For frequency- domain deconvolution (F.D.), we used a six-pole, zero-phase Butterworth filter between 0.1 and 1.2 Hz. (c) Crustal model used to generate synthetic seismograms by the reflectivity algorithm of Randall (1989). For crustal thickness and VS, we smooth the model of Rai et al. (2003) with a single, linear gradient in the crust. The gradient of VP is assumed to be 0.025 km/ sec/km, close to the global average of 0.031 km/sec/ km (Christensen and Mooney, 1995).

 




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