Mainshock and aftershock analysis of the June 17, 1996, deep Flores Sea earthquake sequence: Implications for the mechanism of deep earthquakes and the tectonics of the Banda Sea

Tinker, Mark Andrew; Beck, S. L.; Jiao, Wenjie; Wallace, Terry C.

doi:10.1029/97jb03533

Cited by 15 publications

(8 citation statements)

References 26 publications

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“…The location of the rupture termination determined in this study agrees with the analysis of Goes et al (1997) and Tinker et al (1998), who located this point at a distance of 75 km at an azimuth of 100 0^1 20 0 with respect to the nucleation point. Our rupture model is in agreement with the result of Wiens (1998b), who located aftershocks extending 15 km westwards and about 75 km eastwards of the initiation point of the main shock.…”

Section: Modelsupporting

confidence: 88%

“…Wiens (1998b) studied main and aftershocks using a relative location technique and inferred a substantial change in the focal mechanisms during the main shock rupture. Tinker et al (1998) reported unilateral rupture propagation based on the modelling of broad-band waveforms and directivity analysis. The results of our study con¢rm the ¢ndings of these studies, but there are also di¡erences in the source time histories, focal mechanisms and spatial distribution of the moment release inferred from our study and those of Goes et al (1997) and Tinker et al (1998).…”

Section: The 19 96 Flores Sea Eventmentioning

confidence: 99%

“…The phase PcP is not modelled in the Na¨be lek inversion method. It may interfere with the P wave group at distances greater than about 65 0 (Tinker et al 1998), whilst at smaller epicentral distances it arrives well outside the time window of P. Synthetic seismograms calculated with the re£ectivity method for the source mechanisms of the centroid model and subevent S1 of model M6 (Table 2) revealed that PcP/P decreases from about 1 at 65 0 to about 0.15 at 75 0 . For the key station ABKT, we calculated re£ectivity synthetics for our preferred source model M6 (Table 2) under some simplifying assumptions of the source time function.…”

Section: Modelmentioning

confidence: 99%

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The 1996 June 17 Flores Sea and 1994 March 9 Fiji-Tonga earthquakes: source processes and deep earthquake mechanisms

Tibi¹,

Estabrook²,

Bock³

1999

Geophys. J. Int.

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Summary Source parameters of the 1996 Flores Sea and 1994 Fiji–Tonga deep earthquakes are derived from teleseismic body waves recorded by the global seismic network of broad‐band seismograph stations. Both events consisted of several subevents. Models to approximate the spatial and temporal extent of the source process include point sources, propagating point sources and a combination of these. For the Flores Sea event, rupture lasted about 23 s and terminated some 70 km east of the nucleation point as inferred from the duration of P‐wave pulses, in agreement with the findings reported by other investigators. Our preferred model suggests bilateral rupture propagation. It consists of four point sources that have variable double‐couple radiation patterns and source time histories, and explains well the large compensated linear vector dipole (CLVD) component inferred from the Harvard centroid moment tensor (CMT) solution. The main moment release in the Fiji–Tonga event lasted only about 15 s. Our best model consists of two point sources with a total moment release of 2.8 × 1020 N m. Rupture propagated subhorizontally from the nucleation point to the north. The termination of rupture was located about 40 km to the north of rupture initiation. The inferred velocity of moment release in the Flores Sea and Fiji–Tonga events was 3–5 km s‐1, a value which is higher than that inferred for the great Bolivian earthquake of June 1994. Other derived source parameters (static stress drop, radiated seismic energy and maximum seismic efficiency) are also significantly different from those inferred for the 1994 Bolivian event, suggesting that deep earthquake processes do not follow an easily detectable common mechanism.

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Section: Modelsupporting

confidence: 88%

Section: The 19 96 Flores Sea Eventmentioning

confidence: 99%

Section: Modelmentioning

confidence: 99%

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The 1996 June 17 Flores Sea and 1994 March 9 Fiji-Tonga earthquakes: source processes and deep earthquake mechanisms

Tibi¹,

Estabrook²,

Bock³

1999

Geophys. J. Int.

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“…Most of the moment release can be contained within a distance of 25 km along the slab dip. In addition, the larger afterhsocks of the event have been relocated by the joint hypocentral determination method [Tinker et al, 1998] and are shown in Figure 25 projected onto the fault plane. The majority of the relocated afterhshocks occurred around the edges of the rupture, particularly the large area of moment release to the west of the hypocenter.…”

Section: June 17 1996 Flores Sea Earthquakementioning

confidence: 99%

Rupture processes of large deep‐focus earthquakes from inversion of moment rate functions

Antolik¹,

Dreger²,

Romanowicz³

1999

J. Geophys. Res.

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Abstract. We determine the source time histories of five recent (1994)(1995)(1996) large, deep-focus earthquakes using a method that inverts for fault slip from farfield moment rate functions. The moment rate functions are obtained through the deconvolution of multiple body wave phases using broadband records from Global Seismic Network (GSN) and GEOSCOPE stations. Tests of this method on synthetic data indicate that it is successful in determining the low-frequcncy rupture charactersitics of deep earthquakes under a variety of complicating conditions. We find that source parameters such as average rupture velocity and stress drop are highly variable among the events studied and that some unusual characteristics exhibited by the June 9, 1994, great Bolivian earthquake are also found for other events. Comparison of the slip distributions with background seismicity and aftershock locations indicates that most of the moment release for large deep-focus earthquakes is probably occurring within the active slab interior. This provides further evidence that temperature-controlled mechanisms (such as transformational faulting) play a large role in deep earthquake faulting. Most of the events studied also show a tendency for horizontal rupture propagation, suggesting that isobaric processes may be an important factor in controlling progression of the rupture. Large gaps in the slip distributions point to possible occurrence on multiple fault planes.

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“…The large 1996 Flores Sea earthquake was an exception and had several aftershocks. The rupture plane was identified using waveform studies [Tinker et al, 1998], as that nodal plane (strike 100 ø , dip 55 ø , the southeast striking plane in map view) for which the rotated cmt in the vertical profile (Figure 2) has a left-lateral sense. It was also shown that the plane of faulting coincided with the aftershock-delineated plane.…”

Section: Accurate Earthquake Hypocenters and Cmt Mechanismsmentioning

confidence: 99%

Mechanism of slab thickening near 670 km under Indonesia

Das¹,

Schöffel²,

Gilbert³

2000

Geophysical Research Letters

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Mainshock and aftershock analysis of the June 17, 1996, deep Flores Sea earthquake sequence: Implications for the mechanism of deep earthquakes and the tectonics of the Banda Sea

Cited by 15 publications

References 26 publications

The 1996 June 17 Flores Sea and 1994 March 9 Fiji-Tonga earthquakes: source processes and deep earthquake mechanisms

The 1996 June 17 Flores Sea and 1994 March 9 Fiji-Tonga earthquakes: source processes and deep earthquake mechanisms

Rupture processes of large deep‐focus earthquakes from inversion of moment rate functions

Mechanism of slab thickening near 670 km under Indonesia

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