Remotely triggered seismicity in north China following the 2008 M w 7.9 Wenchuan earthquake

Peng, Zhigang; Chen, Qi‐Fu; Tao, Jiang

doi:10.5047/eps.2009.03.006

Cited by 32 publications

(29 citation statements)

References 30 publications

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“…Dynamic triggering has subsequently been shown to occur after the passing of the waves from large earthquakes, for example, the 2002 Denali event ( M w = 7.9) [ Eberhart‐Phillips et al , 2003; Gomberg et al , 2004; Pankow et al , 2004; Prejean et al , 2004; Hough , 2007; Jiang et al , 2010], and the 2004 Sumatra event ( M w = 9.1) [ West et al , 2005; Velasco et al , 2008] earthquakes. While remotely triggered seismicity is mostly found in active plate boundary regions [e.g., Gomberg et al , 2004; Brodsky and Prejean , 2005; Hill and Prejean , 2007]; recently, several studies have shown that remote triggering could also occur in intraplate regions with relatively low background seismicity [ Hough et al , 2003; Hough , 2007; Peng et al , 2009]. Indeed, Velasco et al [2008] studied 15 large events and showed that 12 of them had some evidence of dynamic triggering and their occurrence was virtually independent of tectonic province.…”

Section: Introductionmentioning

confidence: 99%

Dynamic triggering: Stress modeling and a case study

Gonzalez-Huizar

Velasco

2011

J. Geophys. Res.

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Changes in the static stress can trigger nearby earthquakes that occur within a few fault lengths from the causative event. Transient stresses caused by passage of surface waves commonly trigger events at remote distances, yet little is documented or understood about the processes and stresses necessary for remote triggering. To understand the causative stresses and environments behind remote, or dynamic, triggering, we must decipher the stresses caused by the passage of the surface waves in relation to the local stress field and fault conditions where the triggered events occur. In this study, we model the change in the stress field that the passing of Rayleigh and Love waves causes on a fault plane of arbitrary orientation relative to the direction of propagation of the waves, and we apply a Coulomb failure criterion to calculate the potential of these stress changes to trigger reverse, normal, or strike‐slip failure. We compare these model results with data from dynamically triggered earthquakes in the Australian Bowen Basin, an area with low seismicity and mapped regional stress and that is at the margin of a stable continental craton. Our data analysis shows that for this region, surface waves arriving at 45° from the average strike direction are the most likely to trigger local seismicity. This agrees with our observations.

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Section: Introductionmentioning

confidence: 99%

Dynamic triggering: Stress modeling and a case study

Gonzalez-Huizar

Velasco

2011

J. Geophys. Res.

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“…The magnitudes of earthquakes triggered remotely by the passage of seismic waves are generally small (M < ~4) (e.g., Miyazawa et al 2005;Miyazawa 2011;Peng et al 2010;Yukutake et al 2013). Thus, studying the Oita earthquake could advance our fundamental understanding of the triggering processes of large earthquakes.…”

Section: Introductionmentioning

confidence: 99%

An investigation into the remote triggering of the Oita earthquake by the 2016 Mw 7.0 Kumamoto earthquake using full wavefield simulation

Miyazawa

2016

Earth Planets Space

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High-amplitude seismic waves from the Mw 7.0 Kumamoto earthquake of April 16, 2016, triggered another large earthquake 80 km to the NE roughly 30 s later. The source was located at shallow depths beneath the Yufuin geothermal field, Oita Prefecture, Japan, and the event magnitude was approximately 5.9. To date, this is one of the clearest known examples of a remotely triggered large earthquake. The triggered Oita event was followed by significant seismicity, which was distinct from the aftershocks of the Kumamoto earthquake. The Coulomb failure stress change around the hypocenter, calculated for the passing waves of the Kumamoto earthquake by full wavefield simulation, was about 0.7 MPa when the Oita earthquake was triggered, with the static stress change being an order of magnitude smaller. The dynamic stress changes likely played an important role in triggering. A return to low seismicity levels 1 month after the triggered earthquake may have important implications for seismic hazard due to dynamic triggering.

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“…These values correspond to peak dynamic stresses of ≥0.09 MPa. The stress threshold therefore is in the range 0.03–0.09 MPa, which lies at the lower end of the range of peak dynamic stresses observed worldwide spanning 0.01–0.5 MPa [ Brodsky et al ., ; Prejean et al ., ; Husen et al ., ; Pankow et al ., ; Peng et al ., ]. This suggests that triggering thresholds in the compressional regime of the Southern Alps are of the same order as those in transtensional and extensional settings, where triggering has been observed previously.…”

Section: Discussionmentioning

confidence: 99%

Background and delayed-triggered swarms in the central Southern Alps, South Island, New Zealand

Boese

Jacobs

Smith

et al. 2014

Geochem. Geophys. Geosyst.

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Low-magnitude earthquake swarms (M L 2.8), consisting of up to 47 events of similar waveforms, have been observed repeatedly in the central Southern Alps, a rapidly uplifting orogen bounded by the transpressive Alpine Fault in the South Island of New Zealand. We compare nine background swarms recorded between November 2008 and April 2010 with five delayed-triggered swarms that occurred after the M W 7.8 Dusky Sound and the M W 7.1 Darfield (Canterbury) earthquakes. The two types of swarms are similar in terms of the magnitudes, depths, focal mechanisms, and interevent times of the constituent microearthquakes, and appear to both involve the rupture of steeply dipping faults in highly fractured crust in a 10 km 3 12 km area in the center of the SAMBA network. The delayed-triggered swarms occurred at similar epicentral distances (c. 4.53 the rupture length of the mainshocks) to the Dusky Sound and Darfield earthquakes, commenced shortly after the passage of the surface waves, continued for 5 and 2 days, respectively, and were followed in each case by a 2 day long quiescent period, which may suggest clockadvanced of faults in their failure-cycle. Triggering thresholds of 0.01 MPa proposed elsewhere are similar to the dynamic stress changes computed for the Southern Alps (0.09 MPa). However, as 98% of the locatable triggered events occurred several hours after the surface waves had passed, the dynamic stress changes associated with the surface waves themselves are unlikely to have triggered the earthquakes directly. Instead, we suggest that the locations and delays of the triggered swarms are more consistent with triggering by pore pressure diffusion.

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Remotely triggered seismicity in north China following the 2008 M w 7.9 Wenchuan earthquake

Cited by 32 publications

References 30 publications

Dynamic triggering: Stress modeling and a case study

Dynamic triggering: Stress modeling and a case study

An investigation into the remote triggering of the Oita earthquake by the 2016 Mw 7.0 Kumamoto earthquake using full wavefield simulation

Background and delayed-triggered swarms in the central Southern Alps, South Island, New Zealand

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