Rupture Dynamics of Large Earthquakes inferred from Hydroacoustic Data
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1 Rupture Dynamics of Large Earthquakes inferred from Hydroacoustic Data Catherine de Groot-Hedlin Scripps Institution of Oceanography University of California, San Diego
2 Great Sumatra Earthquake (Boxing Day 2004 Tsunami) Marked the first use of hydroacoustic data to constrain rupture dynamics of large earthquakes de Groot-Hedlin, 2005, Estimation of the rupture length and velocity of the Great Sumatra earthquakes of Dec 26, 2004 using hydroacoustic signals Guilbert et.al, 2005, Use of hydroacoustic and seismic arrays to observe rupture propagation and source extent of the Mw=9.0 Sumatra earthquake Tolstoy & Bohnenstiehl, 2005, Hydroacoustic constraints on the rupture duration, length and speed of the great Sumatra-Andaman earthquake Since this event, hydroacoustic data have not been used to constrain the rupture dynamics of large earthquakes
3 Outline Overview of hydroacoustic propagation Boxing Day 2004 event Complications in inferring rupture dynamics Blockage Seismic to T-phase coupling Source-receiver geometry March 28, 2005 event
4 Hydroacoustic propagation Sound speed increases with increasing T and P, creating a sound channel
5 Ducting within sound channel Cylindrical spreading within the sound channel Acoustic velocity ~1.48 km/s
6 Hydroacoustic blockage Unblocked path Acoustic path blocked by ridge
7 Boxing Day event
8 Configuration of each triad Hydrophones at the sound speed minimum depth 3 hydrophones in each array arranged in a triangle, allowing for computation of azimuths at low frequencies
9 H08: Diego Garcia signal and spectra P-wave propagation velocity: 6-8 km/s T-waves: 1.5km/s Tsunami velocity: 200 m/s
10 Estimation of azimuth Find time lags between hydrophones using cross-correlations (computed for 4-6 Hz band-passed data) T ab +T bc +T ca =0 holds for a plane wave Potential problems with spatial aliasing resolved by ensuring that x-correlation values are high, ie waveforms are coherent
11 Source direction
12 Azimuth vs. time Azimuths computed for 10 s windows with 5 s overlap
13 Source direction inferred from DGS triplet Apparent source swings to Northerly direction
14 Signals observed throughout Indian Ocean
15 Azimuths computed at each IMS station
16 Source direction inferred from each IMS station
17 Derived acoustic source locations for Dec 26, 2004 event
18 The data suggest 2 phases of rupture 1st propagated northward at 2.4+/- 0.3 km/s for nearly 600km Rupture slowed to 1.5+/- 0.4 km/s further to the north
19 Tolstoy & Bohnenstiehl, Surv. Geophys.
20 T-phases generated by seismic to acoustic coupling over an extended region Tolstoy & Bohnenstiehl, Surv. Geophys.
21 Azimuth vs. time for a small earthquake Can we discern between T wave coupling effects and rupture dynamics?
22 Estimation of T-phase back azimuths for a small event (rough forward model) Seismic phases travel at 6 km/s convert to T-phases Near the epicenter At SOFAR channel depths At steep slopes T-phases travel at 1.48 km/s
23
24 Extended source region for a point source at Dec 26 epicenter
25 Comparison with observed back azimuths
26 Agreement between extended rupture model and observed back azimuths Black circles show measured azimuth vs. time Green x es show fit to data for derived acoustic source locations and times Red x es show predicted azimuth vs. time for instantaneous rupture
27 March 28 event: Mb=8.6
28 Sonograms For March 28, 2005 event
29 Back Azimuths estimated from data Is the lengthy rupture duration due to T wave coupling or to extended rupture?
30 Prediction based on Forward Modeling
31 Back Azimuths
32 March 28, 2005 rupture solution Rupture to the SSE at 2.5 km/s
33 Comparison with Seismic solution Walker, Ishii & Shearer infer 2 rupture stages Smaller one to the North Larger one to the SE Velocities between km/s
34 Conclusions Rupture dynamics based on hydroacoustic data Dec 26, 2004 event had an initial velocity of 2.4 +/- 0.3 km/s to the NNW, slowing to 1.5+/-0.4 km/s at a distance of 600 km from the epicenter Average velocity for March 28, 2005 was 2.5 km/s to SSE. Complicating factors Shadow zones Extended seismic to acoustic coupling region Source-receiver geometry
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