The 2011 off the Pacific coast of Tohoku Earthquake related to a strong velocity gradient with the Pacific plate
© 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: 10 April 2011
Accepted: 18 May 2011
Published: 27 September 2011
We conduct seismic tomography using arrival time data picked by NIED Hi-net, including earthquakes off the coast, outside the seismic network. For these offshore events, we use the NIED F-net focal depth. We detect two low-V. zones in the uppermost subducting oceanic crust. The landward low-V zone with a large anomaly corresponds to the western edge of the coseismic slip zone of the 2011 off the Pacific coast of Tohoku Earthquake. The asperities of the previously known Off-Miyagi and Off-Fukushima earthquakes with magnitudes around 7.0 are also located at the boundary of the low-V and the eastern high-V zones. The initial break point (hypocenter) is associated with the edge of a slightly low-V and low-V p /V s zone. The trenchward low-V and low-V p /V s zone extending southwestward from the hypocenter may indicate the existence of a subducted seamount. The high-V zone and low-V p /V s zone might have accumulated the strain and resulted in the huge coseismic slip zone of the 2011 Tohoku Earthquake. The low-V and low-V p /V s zone is a slight fluctuation within the high-V zone and might have acted as the initial break point of the 2011 Tohoku Earthquake.
Key wordsSeismic tomography the 2011 off the Pacific coast of Tohoku Earthquake high-V coseismic slip zone seamont NIED Hi net lowVoceanic crust asperity
The 2011 off the Pacific coast of Tohoku Earthquake occurred on March 11, 2011. There are few studies (e.g. Zhao et al., 2007) of the velocity structure near the Japan trench using data from inland seismic stations. It is difficult to investigate the velocity structure beneath the ocean with only the inland seismic stations because of the large uncertainty in earthquake focal depth outside of the seismic network. Zhao et al. (2007) estimated the velocity structure near the Japan trench using the focal depths constrained by sP converted waves. The broadband seismograph network (F-net) operated by National Research Institute for Earth Science and Disaster Prevention (NIED) determines the focal depths of events with magnitudes larger than 3.5 using a Green’s function approach (Okada et al., 2004). For the events distant from the seismic network, the depth determined by NIED F-net is more reliable than that determined by the high sensitivity seismograph network (Hi-net) operated by NIED, since there are no stations above the hypocenter. However, NIED determines reliable arrival times from those events at onshore stations. To use those data effectively, we combined the arrival time data picked by NIED Hi-net and the focal depth determined by NIED F-net. By using the distant events off the coast, we can obtain the velocity structure of the lower crust, the upper mantle, and the plate boundary from the trench to the island arc.
2. Data, Method, Resolution, and Comparison with the Results of OBS
We follow the technique of Matsubara et al. (2004, 2005), who introduced spatial velocity correlation and station corrections to the original code of Zhao et al. (1992). Grid nodes were placed with a separation smaller than the spatial resolution, with smoothing performed in order to stabilize the solution. The inverse problem is then solved with the LSQR algorithm (Nolet, 1987) since we can assume arbitrary damping matrix with a combination of diagonal and smoothing matrices.
Grid interval and resolution size.
We solve for the location and origin time of all the earthquakes as well as the P and S-wave slowness at each grid point with more than 10 associated rays. In the final iteration, we estimate the P-wave slowness at 458,234 nodes and the S-wave slowness at 347,037 nodes. The inversion reduces the root mean square of the P-wave traveltime residual from 0.455 s to 0.187 s and that of the S-wave data from 0.692 s to 0.228 s after eight iterations.
We determine the upper boundary of the Pacific plate based on the velocity structure and earthquake hypocen-tral distribution. The upper boundary of the low-V oceanic crust corresponds to the plate boundary where thrust earthquakes are expected to occur. Where we don’t observe low-V oceanic crust, we determine the upper boundary of the upper layer of the double seismic zone within the high-V Pacific plate. We assume the depth at the Japan trench as 7 km.
Figure 3 shows the map view of V p perturbation within the Pacific plate 10 km beneath the boundary. In the inland area, large earthquakes occurred around the region whose lower crust has low-V, suggesting a role of magma and fluid (Zhao et al., 2010). Then we investigate the velocity structure within the Pacific plate such as 10 km beneath the plate boundary.
We detected two low-V zones in the oceanic crust at the uppermost part of the Pacific plate on the west side of the hypocenter (Fig. 3). We define one of them at longitudes of approximately 142.5E adjacent to the hypocenter as the trenchward low-V zone and another at longitudes of 141.5–142.0E as the landward low-V zone. We also call the high-V zone between them the ‘central high-V zone.’ The landward low-V zone extends broadly and has large anomaly; however, the trenchward low-V zone has slight anomaly and is a small fluctuation within the high-V zone. The hypocenter of the 2011 Tohoku Earthquake is located at the northern edge of the resolved zone; however, the structure on the southern side of the hypocenter shows that the hypocenter is located at the boundary of the trenchward slightly low-V and eastern high-V zone.
The vertical cross sections along the direction of the subducting Pacific plate are shown in Fig. 4. The low-V oceanic crust at the uppermost part of the Pacific plate is imaged extending downdip from the hypocentral region and diminishes beneath the land area (Fig. 4(a)–4(e)). The trenchward low-V zone near the Japan trench is imaged off Iwate, Miyagi, and Fukushima and corresponds to the oceanic crust of the Pacific plate (Fig. 4(a)–4(e)); however, there is no clear low-V oceanic crust off the boundary of Fukushima and Ibaraki near the Japan trench (Fig. 4(f)). We only observe low-V oceanic crust at the uppermost part of the Pacific plate at depths of 40–60 km within the landward low-V zone.
The high-V region on the east side of the hypocenter and the central high-V region between the two low-V zones are covered with the coseismic slip regions estimated using GPS data (Geospatial Information Authority, 2011) or waveform data (e.g. Yagi, 2011; Shao et al., 2011). Honda et al. (2011) estimate a rupture of the earthquake with the seismic network in the metropolitan area (MeSO-net). The area of strong energy radiation is located at the west side of the hypocenter offshore of Miyagi and extends eastward and southward. The area of the strongest energy radiation is consistent with the central high-V zone between the trenchward and landward low-V zones (Fig. 3). The landward low-V zone is located at the western boundary of the zone of strong energy radiation. The asperities of the preknown Off-Miyagi and Off-Fukushima earthquakes with magnitude around 7.0 (Sato et al., 1989) are also located at the boundary of the landward low-V zone and the central high-V zone.
The initial break point (hypocenter) of the 2011 Tohoku Earthquake is located at the boundary of the trench-ward slightly low-V and high-V zone (Fig. 3). There are some seamount chains offshore Fukushima and Ibaraki (Yamasaki and Okamura, 1989). A convex seafloor configuration may indicate the existence of subducted seamounts beneath the cross sections D–D′ and E−E′ (Hudnut, 2011) corresponding to the trenchward low-V zone. In terms of E−E′, there is a convex undulation at the plate boundary imaged by refraction seismology (Miura et al., 2003). The trenchward low-V region on the west side of the hypocenter has low-V p /V s (Fig. 4(h), 4(j)). We propose that fluid with high aspect ratio pores exists there, as proposed by Matsubara et al. (2004, 2009) based on the result of Takei (2002). Nakamichi et al. (2007) and Kato et al. (2010) also considered the high aspect ratio crack with low-V p /V s zone. If a large seamount has already subducted beneath the plate, a low-V zone would be imaged (Cummins et al., 2002). The low-V and low-V p /V s zone beneath D–D′ may indicate the subducted seamount. This trenchward low-V p /V s zone extends to the initial break point of the main-shock (B–B′).
The area of strong energy radiation also extends to the high-V zone on the east side of the hypocenter (Fig. 3). The high-V zone on the east side of the landward low-V zone and low-V p / V s zone might have accumulated the strain and resulted in the huge coseismic slip zone of the 2011 Tohoku Earthquake. The trenchward low-V and low-V p /V s zone is a slight fluctuation within the high-V zone and might have acted as the initial break point of the 2011 Tohoku Earthquake.
Beneath the southern Ibaraki prefecture, the low-V oceanic crust of the Pacific plate is clearly imaged at depths of 40-130 km (Fig. 4(g)), which is consistent with previous studies (e.g. Matsubara et al., 2005; Shelly et al., 2006). Matsubara et al. (2005) proposed that the subducting Philippine Sea plate distorts the corner flow induced by the Pacific plate and suppresses thermal recovery in the mantle wedge. There is a large aftershock with magnitude 7.7 off southern Ibaraki half an hour after the 2011 Tohoku Earthquake. The hypocenter is also located at the boundary of the eastern low- and western high-V zones.
We combine the NIED F-net hypocentral and Hi-net arrival time data and apply seismic tomography to estimate the seismic velocity structure outside of the network. We obtain the horizontal 20-km and vertical 10-km scale structure near the Japan trench. There are two low-V zones within the subducting oceanic crust. The landward low-V zone with a large anomaly is consistent with the western edge of the coseismic slip zone of the 2011 off the Pacific coast of Tohoku Earthquake. The asperities of the previously known Off-Miyagi and Off-Fukushima earthquakes with magnitudes around 7.0 are also located at the boundary of the landward low-V zone and the central high-V zone. The zone beneath the initial break point of the 2011 To-hoku Earthquake is associated with the edge of the slightly low-V and low-V p /V s zone corresponding to the boundary of the low- and high-V zone. The trenchward low-V and low-V p /V s materials extending to the southwest from the hypocenter may indicate a subducted seamount. The high-V zone on the east side of the landward low-V zone and low-V p /V s zone might have accumulated the strain and resulted in the huge coseismic slip zone of the 2011 Tohoku Earthquake. The low-V and low-V p /V s zone is a slight fluctuation within the high-V zone and might have acted as the initial break point of the 2011 Tohoku Earthquake.
We used the seismic data provided by the National Research Institute for Earth Science and Disaster Prevention , the Japan Meteorological Agency, Hokkaido University, Hirosaki University, Tohoku University, the University of Tokyo, Nagoya University, Kyoto University, Kochi University, Kyushu University, Kagoshima University, the National Institute of Advanced Industrial Science and Technology, the Geographical Survey Institute, Tokyo Metropolis, Shizuoka Prefecture, the Hot Springs Research Institute of Kanagawa Prefecture, Yokohama City, and the Japan Agency for Marine-Earth Science and Technology . We are very grateful to David Shelly for kindly discussing and improving our paper. We also thank William Ellsworth for the kind discussion and suggestions. We appreciate the many suggestions from the two anonymous reviewers. This study was supported by the project on the Operation of Seismograph Networks for the NIED. Some of the figures were drawn using Generic Mapping Tools software (Wessel and Smith, 1995) and the software for viewing 3D velocity structures beneath whole Japanese Islands (Matsubara, 2010).
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