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Remotely-triggered seismicity in the Hakone volcano following the 2011 off the Pacific coast of Tohoku Earthquake
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2011
Received: 8 April 2011
Accepted: 1 May 2011
Published: 27 September 2011
Seismic activity in the Hakone volcano at an epicentral distance of 450 km was remarkably activated just after the 2011 off the Pacific coast of Tohoku Earthquake. More than 1600 events were observed in the caldera of the volcano, from 15:00 on March 11 to 12:00 on April 2. To clarify the relationship between the occurrence of the main shock and the induced activity in the Hakone volcano, we investigated the spatial distribution of hypocenters and temporal changes of the seismicity, and we examined seismographs of the main shock to identify small local events during the passage of the surface waves. Hypocenters determined with the double-difference method are mostly distributed in the N-S direction, showing several clusters of seismicity. Focal mechanisms of major earthquakes are predominantly strike-slip having the P axis in the NNW-SSE direction. These features of the hypocenter distribution and the focal mechanisms are consistent with those of earthquakes that occur ordinarily in the Hakone volcano. The onset of the local event was initiated during the Love and Rayleigh waves from the main shock, suggesting that large dynamic stress changes of 0.6 MPa dominantly contributed to initiate the sequence of seismic activity.
Several studies have shown that seismicity in volcanic or geothermal regions has been activated by passing surface or coda waves from a far-distant large earthquake (e.g. Hill et al., 1993; Husen et al., 2004; Prejean et al., 2004). The purpose of this paper is to clarify the relationship between the occurrence of the MJMA 9.0 main shock and the induced activity in the Hakone volcano. We show the spatial distribution of hypocenters and temporal changes of seismicity in the Hakone volcano after the main shock. Next, we examine the temporal correspondence of the passing of the seismic wave from the main shock and the occurrence of small local events, based on recordings of the main shock wave train.
2. Tectonic Settingand Swarm Earthquakesinthe Hakone Volcano
The Hakone volcano is located at the northern boundary zone of the Izu-Mariana volcanic arc in central Japan (Fig. 1). There are many hot springs in the caldera. The hot springs in the Gora area are high-temperature and rich in sodium chloride, which is considered to be derived from the volatile phase from a deep-seated magma source beneath the Hakone volcano (Oki and Hirano, 1970; Matsuo et al., 1985). Intense swarm activity has occasionally occurred in the caldera (Hiraga, 1987; Mannen, 2003). Strong ground motion and fumarolic activity has sometimes accompanied intense swarm activity (Mannen, 2003). The Hot Springs Research Institute of Kanagawa Prefecture (HSRI) has monitored activity of swarm earthquakes with a seismic network of 15 online stations that were installed in and around the Hakone caldera in 1989 (Fig. 1). The swarm activity in 2001, 2006, 2008 and 2009 were especially notable. From the precisely determined hypocen-ter distribution, Yukutake et al. (2010) indicated that most of the swarm earthquakes in the Hakone volcano are distributed on thin, vertically-oriented plane-like zones, which probably reflect a network of small faults developed by the interaction of Tanna and Hirayama Faults. Yukutake et al. (2011) demonstrated a diffusion-like migration of hypocen-ters during the activity of August 2009, which suggests that pressurized fluid in the fault zone plays a substantial role in the occurrence of the swarm earthquakes.
3. Seismicity after the Great Earthquake on 11 March, 2011
From the time-magnitude diagram (Fig. 2(c)), we can see that the seismicity in the Hakone volcano abruptly increased just after the main shock. 1688 events occurred in the period between 15:00 on March 11 and 12:00 on April 2. During the year before the main shock, an average of 20 events per month were recorded in the Hakone volcano (Honda, 2011). The first event of the swarm-like activity in the volcano occurred 17 minutes after the main shock (15:03, March 11). At 15:08 on March 11, the largest event with a local magnitude of 4.8 occurred in the southern part of the caldera (Fig. 2(a, b)). Although the seismicity increased abruptly on March 20, 22 and 31, the occurrence rate of earthquakes decayed with time (Fig. 2(c))
The epicenters distribute mostly in the N-S direction, in several clusters (Fig. 2(a, b)). The focal mechanisms of the major earthquakes are strike-slip having the P axis in the NNW-SSE direction. These features of the hypocenter distribution and the focal mechanisms are consistent with those of the earthquakes that ordinarily occur in the Hakone volcano (e.g. Yukutake et al., 2010). The seismicity following the main shock occurred primarily at sites that were previously seismically active. However, several earthquakes were observed around the northern end of the Tanna Fault outside the caldera (Fig. 2(a)), where the seismicity was rather low before the main shock.
4. Seismicity during the Main Shock Wave Train
We found that the onset of seismicity in the Hakone volcano began during the passing of the Love and Rayleigh waves with a period of < 10 s from the main shock. We calculated dynamic stress changes induced by the surface wave following the method of Hill et al. (1993). The peak dynamic stress changes during the surface waves were roughly 0.6 MPa. We also estimated static stress changes around the Hakone volcano caused by the main shock, based on the fault source model by the Geographical Survey Institute (2011). Static stress changes are calculated using the formula presented by Okada (1992). ΔCFF calculated for the location and orientation of the M 4.8 earthquake that occurred just after the main shock (Fig. 2) is +0.04 MPa. The magnitude of static stress changes caused by the main shock is significantly smaller than that of dynamic stress changes. Moreover, it seems that seismicity during the main shock wave train is high during the arrival of large amplitude Love and Rayleigh waves (Fig. 3). Belardinelli et al. (2003) indicated that large dynamic stress changes can trigger earthquakes without a time delay. The instantaneous response of the seismicity to the arrival of the large amplitude surface waves (Fig. 3) strongly suggests that the dynamic stress changes predominantly contributed to initiate a sequence of seismic activity in the Hakone volcano. Belardinelli et al. (2003) also showed that static stress changes can trigger earthquakes with a wide variety of time delays, while dynamic stress changes can only cause instantaneous failures. Since the previous studies showed that a static stress change of 0.01 MPa promoted seismicity (e.g. Hardebeck et al., 1998), the static stress changes of 0.04 MPa may be large enough to trigger earthquakes. Indeed, in the Hakone volcano, Yukutake et al. (2011) demonstrated that the static stress changes of 0.01–0.045 MPa probably triggered the swarm earthquakes in the later stage of the 2009 activity. The long duration of the seismicity over a month and its slow decay (Fig. 2(c)) might suggest that the static stress changes were responsible for the activity as well as the dynamic stress changes.
Prejean et al. (2004) indicated that dynamic stress changes induced by the 2002 Denali Fault Earthquake (Mw 7.9), Alaska, remotely triggered seismicity in a geothermally active region of the west coast of the United States, such as Long Valley, the Geysers geothermal field and Mount Rainer. Peak dynamic stress changes from the Denali Fault Earthquake at these sites are 0.01–0.09 MPa, that is a small order of magnitude compared with those of the main shock. We examined whether the seismicity in the Hakone volcano showed temporal changes in response to prior large distant earthquakes: the 2003 Tokachi-oki earthquake (MJMA 8.0) and the 2008 Iwate-Miyagi Nairiku earthquake (MJMA 7.2). The peak dynamic stress changes caused by these earthquakes are 0.04 and 0.02 MPa, respectively, around the Hakone volcano. Unfortunately, highdynamic-range instruments had not yet been installed for the HSRI station network at the occurrence times of these earthquakes. Since the waveforms of the stations within the caldera were saturated during large ground motion, we could not look for local shocks hidden in the surface wave arrivals. However, we did not find any significant temporal change in the seismicity in the HSRI catalog following these earthquakes. This suggests that the dynamic stress threshold to initiate triggered activity in the Hakone volcano might be high compared with the geothermal regions in the west coast of the United States or the threshold might be changed according to the tectonic stress level in the study region.
Seismic activity in the Hakone volcano was significantly activated just after the occurrence of the 2011 off the Pacific coast of Tohoku Earthquake. The onset of seismicity was initiated during the Love and Rayleigh waves from the main shock. The seismic activity persisted for approximately one month, with more than 1600 events occurring. The large dynamic stress changes of 0.6 MPa probably contributed to initiate a sequence of seismic activity. The features of the hypocenter distribution and the focal mechanisms are almost consistent with those of the earthquakes that ordinarily occur in the Hakone volcano. We would like to note that seismicity around the northern end of the Tanna Fault was activated after the main shock, where earthquakes were previously hardly observed. We installed 21 offline temporary stations in and around the Hakone caldera prior to the main shock and we are continuing the observation. Temporal and spatial distribution of the induced earthquakes and their focal mechanisms determined from this dense seismic network will help us to quantitatively understand the physical processes of the triggering in the region.
We are grateful to Dr. F. Waldhauser for the hypoDD program code. We are thankful to Dr. David P. Hill and anonymous reviewer, who greatly helped us to improved this manuscript, and Dr. Kiyoshi Yomogida for editing it. We thank the Earthquake Research Institute of the University of Tokyo, and National Research Institute for Earth Science and Disaster Prevention Hi-net and F-net for allowing us to use their waveform data. A majority of the figures were created using Generic Mapping Tools (GMT) (Wessel and Smith, 1995).
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