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Shallow inland earthquakes in NE Japan possibly triggered by 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: 26 April 2011
Accepted: 17 June 2011
Published: 27 September 2011
Shallow seismic activity in the crust of the overriding plate west of the source area increased significantly after the 2011 Mw 9.0 Tohoku earthquake which ruptured the plate boundary to the east off northern Japan beneath the Pacific Ocean. In order to understand the cause of this distinctive change in seismicity, we have precisely relocated earthquake hypocenters for several earthquake sequences that occurred during the period March 11–April 6, 2011, following the Tohoku earthquake by the double-difference method. Hypocenter distributions were used to discriminate the fault plane from the auxiliary plane of the focal mechanisms for those earthquake sequences. We then calculated the Coulomb stress change on those fault planes caused by the 2011 Mw 9 earthquake. In all cases, the estimated Coulomb stress changes at the plausible fault planes for those post-mainshock sequences are positive. The positive Coulomb stress change is mainly due to the reduction of normal stress on the fault plane of the earthquake sequences by the large, low-angle thrust fault responsible for the 2011 Mw 9 earthquake. The present observations suggest that static stress transfer possibly triggered those post-mainshock earthquake sequences.
One typical example of a large inland earthquake that occurred after a large interplate earthquake in NE Japan is the 1896 M 7.2 Riku-u earthquake. The earthquake occurred 2.5 months after the 1896 M 8 Sanriku tsunami earthquake (e.g. Kanamori, 1972). Ohtake (1997) suggested the possibility that the reduction of normal stress by the Sanriku earthquake triggered the Riku-u earthquake if the fault plane of the Riku-u earthquake was steeply dipping, although the fault has been estimated to be possibly not steeply dipping in later studies (~30°; from Sato et al., 2002).
To understand the cause of such activation of seismicity in the overriding plate by a large interplate earthquake, we need to know the geometry of the fault plane and the slip on it. In this study, we have investigated, in detail, hypocenter distributions of several events that occurred after the Mw 9.0 earthquake in order to discriminate the fault plane from the auxiliary plane of the focal mechanism. We then calculated the Coulomb stress change (Lin and Stein, 2004; Toda et al., 2005) on each fault attributable to the 2011 Mw 9.0 Tohoku Earthquake to explore whether or not they were likely triggered by the Mw 9.0 event.
2. Determination of the Fault Plane by Focal Mechanism and Relocated Hypocenters
We selected several remarkable sequences of inland earthquakes in the NE Honshu area during the period from March 11 to April 6, whose focal mechanisms have been determined. The focal mechanisms are from GCMT (Nettles et al., 2011), AQUA-CMT by the National Institute for Earth Sciences and Disaster Prevention (NIED) (http://www.hinet.bosai.go.jp), and the Japan Meteorological Agency (JMA) CMT (http://www.jma.go.jp). For smaller events, whose focal mechanisms were not reported, we determined focal mechanisms using the polarities of P-waves by the HASH program (Hardebeck and Shearer, 2002).
To discriminate which of the two nodal planes is the plausible fault plane, we compare the hypocenter distribution with the focal mechanism. We employ a double-difference (DD) hypocenter location method (Waldhauser and Ellsworth, 2000; Waldhauser, 2001) to precisely relocate the individual hypocenters for those inland earthquake sequences. In the case of smaller events (Subsections 2.1, 2, 3, and 4), we used the travel-time difference data for nearby events calculated by the cross-correlation analysis of seismic waveforms.
Data are from the seismic networks of Tohoku University and other Japanese Universities, JMA, and NIED Hi-net. We also used data from six telemetry stations deployed just after the 2011 earthquake by the Group for the aftershock observations of the 2011 off the Pacific coast of To-hoku Earthquake, and those from temporary seismic stations and volcano observation stations operated by Tohoku University.
The focal mechanisms and the plausible fault planes for the relocated hypocenters are also shown in Fig. 1. We show fault geometries of the earthquakes in Subsections 2.1 to 2.9. We show two examples in detail: a larger event—the Mjma 5.1 event in northern Akita (2.1) and a smaller event—the Mjma 3.4 event in central Akita (2.2).
2.1 Northern Akita (Mjma 5.1, 19:49 JST (10:49 UT) April 1)
2.2 Central Akita swarm
We also determined the focal mechanisms of the Mjma 3.2 event at 7:38 JST March 14 (22:38 UT, March 13) and Mjma 4.2 event at 14:38 JST March 28 (5:38 UT, March 28) of this swarm. Those mechanisms are of the strike-slip type. For each event, the aftershock seems to align with an N-S strike, which corresponds with one nodal plane of the focal mechanism.
2.3 Yamagata-Gassan swarm
In the case of a seismic swarm in the central part of Yamagata Prefecture, we determined the focal mechanisms of an Mjma 2.2 event at 19:43 JST (10:43 UT), April 4. This mechanism is a strike-slip type with a slight component of reverse slip. We determined the hypocenter distribution of this cluster. We relocated 36 events. The RMS residual decreased from 0.11 s to 0.07 s by the relocation. A cluster, including the Mjma 2.2 event, seems to align with a strike of N-S and eastward dipping, which corresponds with one nodal plane of the focal mechanism. We assume this N-S striking plane to be the dominant fault plane in the earthquake sequence.
2.4 Aizu swarm
In the case of a seismic swarm in the northern part (Aizu district) of Fukushima Prefecture, we determined focal mechanism of an Mjma 2.5 event that occurred at 22:02 JST (13:02 UT), March 20. This mechanism is intermediate between strike-slip and a reverse-fault type. We determined the hypocenter distribution of this cluster, and relocated 528 events. The RMS residual decreased from 0.16 s to 0.08 s by the relocation. Events of the cluster near the M 2.5 event seem to align with a NNW-SSE strike, which corresponds with one nodal plane of the focal mechanism. We assume this plane with a NNW-SSE strike would be one of the fault planes of the earthquake swarm.
2.5 Akita-Oki (Mjma 6.4, 04:46 JST March 12 (19:46 UT March 11))
This event is located at the eastern edge of the aftershock area of the 1983 M 7.7 Nihonkai-Chubu earthquake. The Mjma 6.3 event has a strike-slip focal mechanism with striking NNE-SSW according to the GCMT, although the 1983 M 7.7 earthquake was a thrust fault. We relocated 34 events of the sequence. The RMS residual decreased from 0.24 s to 0.15 s by the relocation. The hypocenters of these events align along a vertical plane striking NNE-SSW, which is taken to be the fault plane for the sequence.
2.6 Iwaki (Mjma 6.0, 07:12 JST March 23 (22:12 UT March 22))
The GCMT shows a normal-type focal mechanism with a strike of NNE-SSW. NIED AQUA-CMT and JMA CMT indicate similar conclusions. Hypocenters located by JMA seem to align along a westward-dipping plane. We also relocated 457 events until March 25. The RMS residual decreased from 0.15 s to 0.10 s by the relocation. The hypocenters of these events align along a westward-dipping plane. This plane is assumed to be the fault plane of this event.
2.7 Kita-Ibaraki (Mjma 6.1 18:56 JST (9:56 UT) March 19)
The GCMT shows a normal-type focal mechanism with a strike of NW-SE. NIED AQUA-CMT and JMA CMT are in agreement. The hypocenters of aftershocks from the Mjma 6.1 events align along a SW-dipping plane by NIED (http://www.hinet.bosai.go.jp/topics/nibaraki110319/). This plane is assumed to be the fault plane of the Mjma 6.1 event.
2.8 Northern Nagano (Mjma 6.3 3:59 JST, March 12 (21:59 JST, March 11))
We choose the reverse-type fault plane with a NE-SW strike dipping southeast by the GCMT and relocated hypocenters by NIED (http://www.hinet.bosai.go.jp/topics/n-nagano110312/). Note that JMA-CMT provide a similar solution.
2.9 Eastern Shizuoka (Mjma 6.1, 21:31 JST (13:31 UT), March 15)
We choose the strike-slip-type fault plane with a strike of NNE-SSW by the GCMT and relocated hypocenters by NIED (http://www.hinet.bosai.go.jp/topics/eshizuoka110315/). NIED AQUA-CMT and JMA CMT give similar solutions.
3. Calculation of Coulomb Stress Change
For the fault planes discriminated from auxiliary planes in the previous section, we calculate the Coulomb stress change caused by the 2011 Tohoku earthquake. We also assume the rake from each focal mechanism. We adopted the Coulomb 3.2 (Lin and Stein, 2004; Toda et al., 2005), assuming a frictional coefficient of 0.65. We calculate the static stress on each fault in a uniform and isotropic elastic half-space following Okada (1992). The shear modulus and Poisson’s ratio are 3.2 × 104 MPa and 0.25, respectively. The Coulomb stress change is defined as: Δσf = Δτs + μΔσn. Here, Δσf is the change in failure stress on each fault of the post-megathrust event by the source fault (the 2011 Mw 9 Tohoku earthquake), Δτs is the change in shear stress, Δσn is the change in normal stress, and μ is the frictional coefficient. We used the slip model for the 2011 Mw 9 earthquake provided by Hayes, USGS (Hayes, 2011).
Calculated Coulomb stress change and normal stress change for each earthquake sequence. Normal stress is defined as positive for unclamping.
ΔCFF (μ = 0.65) (MPa)
Normal Stress (MPa)
Apr. 1, 2011
Mar. 14, 2011
Mar. 28, 2011
Apr. 3, 2011
Apr. 4, 2011
Mar. 20, 2011
Mar. 12, 2011
Mar. 23, 2011
Mar. 19, 2011
Mar. 12, 2011
Mar. 15, 2011
As shown in the previous section, the estimation of fault planes of earthquake sequences occurring just after the Mw 9.0 earthquake and the calculation of associated Coulomb stress changes suggest that these post-megathrust events are triggered by the static stress change caused by the large slip along the plate boundary thrust that accompanied the 2011 Mw 9 earthquake.
These triggered earthquake sequences tend to be located in areas of high seismicity prior to the 2011 earthquake as shown in Fig. 1. However, if we consider this in more detail, we note that most of these earthquakes are located at the margin of the high-seismicity areas.
In NE Japan, these high-seismicity areas consist of many reverse-slip earthquake ruptures with E-W or NW-SE oriented P-axes (e.g. Hasegawa et al., 2005). Toda (2011, http://www.rcep.dpri.kyoto-u.ac.jp/events/110311tohoku/toda/index.html) suggested that Coulomb stress changes for such “typical” reverse faults are negative except in the northernmost and southernmost part of NE Japan (i.e. the events 2.1 and 2.8 in this study). In this study, however, some of the post-megathrust events (2.2, 2.3, 2.4, and 2.5) in the central part of NE Japan yield strike-slip solutions with steeply-dipping fault planes (<60°) and NE-SW oriented P-axes. Their dip angle is greater than the lock-up angle for pure reverse faults under the usual stress field with the WNW-ESE directed and horizontal maximum compressional stress axis (σ1) in NE Japan (Sibson, 1990, 2009). A reduction of normal stress may have triggered the occurrence of these post events which could not occur before the 2011 M 9 event.
There occurs a possible change in local stress regimes in some areas (e.g. region 2.2). Hasegawa et al. (2011) have suggested that the change in the local stress regime is due to an almost complete stress drop in the 2011 Mw 9.0 Tohoku Earthquake. They also reported that near the focal areas of Kita-Ibaraki, and Iwaki, an earthquake of normal faulting occurred prior to the 2011 Mw 9 Tohoku earthquake from the NIED F-net catalog. In this study we have analyzed twelve earthquakes and it would be difficult to discuss the change in the stress regime in details. A detailed analysis of the focal mechanisms of the earthquakes following, and prior to, the 2011 Mw 9 Tohoku earthquake is necessary as a further study.
We have estimated the fault planes of several remarkable inland earthquake sequences, that occurred actively after the 2011 Mw 9.0 Tohoku Earthquake, based on double-difference location of earthquake hypocenters. We have also calculated the Coulomb stress change due to the 2011 Mw 9 earthquake on these fault planes. The Coulomb stress change estimated for all the inferred fault planes are positive. This suggests that these inland earthquake sequences in the overriding plate of NE Japan just after the 2011 Mw 9 earthquake were triggered by a static stress transfer.
We have used data from JMA, Hi-net/NIED. This study is a part of a “Multidisciplinary research project for high strain rate zone” promoted by the Ministry of Education, Culture, Sports, Science and Technology (MEXT), Japan. Some of the temporary stations are operated cooperatively with the Japan Nuclear Energy Safety Organization (JNES). We thank S. Miura, R. Hino, Y. Yabe, M. Ichiki, Y. Ito, Y. Ohta, T. Iinuma, M. Ohzono for valuable discussions. We acknowledge the seismic observations of T. Sato, S. Hori, K. Tachibana, T. Kono, T. Nakayama, S. Hirahara, S. Suzuki, T. Demachi and T. Kaida. We would like to thank the editor (Professor K. Yomogida), and the reviewers (Professor R. Sibson and an anonymous reviewer) for helpful comments. This work was conducted under the support of a Grant-in-Aid for Special Purposes, MEXT, Japan.
Group for the aftershock observations of the 2011 off the Pacific coast of Tohoku Earthquake consists of the members from Hokkaido University, Hirosaki University, Chiba University, University of Tokyo, Nagoya University, Kyoto University, Kochi University, Kyushu University, Kagoshima University, National Institute for Earth Sciences and Disaster Prevention, and Tohoku University.
- Hardebeck, J. L. and P. M. Shearer, A New Method for Determining FirstMotion Focal Mechanisms, Bull. Seismol. Soc. Am., 92, 2264–2276, 2002.View ArticleGoogle Scholar
- Hasegawa, A., J. Nakajima, N. Umino, and S. Miura, Deep structure of the northeastern Japan arc and its implications for crustal deformation and shallow seismic activity, Tectonophysics, 403, 59–75, 2005.View ArticleGoogle Scholar
- Hasegawa, A., J. Nakajima, N. Uchida, T. Okada, D. Zhao, T. Matuzawa, and N. Umino, Plate subduction, and generation of earthquakes and magmas in Japan as inferred from seismic observations: An overview, Gondowana Res., 16, 370–400, 2009.View ArticleGoogle Scholar
- Hasegawa, A., K. Yoshida, and T. Okada, Nearly complete stress drop in the 2011 Mw 9.0 off the Pacific coast of Tohoku Earthquake, Earth Planets Space, 63, this issue, 703–707, 2011.View ArticleGoogle Scholar
- Hayes, G., Updated Result of the Mar 11, 2011 Mw 9.0 Earthquake Offshore Honshu, Japan, http://earthquake.usgs.gov/earthquakes/eqinthenews/2011/usc0001xgp/finitefault.php, 2011.
- Iinuma, T., M. Ohzono, Y. Ohta, and S. Miura, Coseismic slip distribution of the 2011 off the Pacific coast of Tohoku Earthquake (M 9.0) estimated based on GPS data—Was the asperity in Miyagi-oki ruptured?, Earth Planets Space, 63, this issue, 643–648, 2011.View ArticleGoogle Scholar
- Kanamori, H., Mechanism of tsunami earthquakes, Phys. Earth Planet. Inter., 6, 346–359, 1972.View ArticleGoogle Scholar
- Lin, J. and R. S. Stein, Stress triggering in thrust and subduction earthquakes, and stress interaction between the southern San Andreas and nearby thrust and strike-slip faults, J Geophys Res, 109, 10.1029/2003JB002607, 2004.Google Scholar
- Miller, S. A., C. Colletini, L. Chairaluce, M. Cocco, M. Marchi, and B. J. Kaus, Aftershocks driven by a high-pressure CO2 source at depth, Nature, 427, 724–727, 2004.View ArticleGoogle Scholar
- Nettles, M., G. Ekström, and H. C. Koss, Centroid-moment-tensor analysis of the 2011 off the Pacific coast of Tohoku Earthquake and its larger foreshocks and aftershocks, Earth Planets Space, 63, this issue, 519–523, 2011.View ArticleGoogle Scholar
- Ohtake, M., A possibility that the 1896 Off Sanriku Great Earthquake Triggered the Riku U earthquake, Abstract for the 1997 JPGU Meeting, 1997.Google Scholar
- Okada, T., N. Umino, and A. Hasegawa, Deep structure of the Ou mountain range strain concentration zone and the focal area of the 2008 Iwate-Miyagi Nairiku earthquake, NE Japan - Seismogenesis related with magma and crustal fluid, Earth Planets Space, 62, 347–352, 2010.View ArticleGoogle Scholar
- Okada, Y, Internal deformation due to shear and tensile faults in a half space, Bull. Seismol. Soc. Am., 82, 1018–1040, 1992.Google Scholar
- Sato, H., N. Hirata, T. Iwasaki, M. Matsubara, and T. Ikawa, Deep seismic reflection profiling across the Ou Backbone range, northern Honshu Island, Japan, Tectonophysics, 355, 41–52, 2002.View ArticleGoogle Scholar
- Sibson, R. H., Rupture nucleation on unfavorably oriented faults, Bull. Seismol. Soc. Am., 80, 1580–1604, 1990.Google Scholar
- Sibson, R., Rupturing in overpressured crust during compressional inversion—the case from NE Japan, Tectonophysics, 473, 404–416, 2009.View ArticleGoogle Scholar
- Toda, S., http://www.rcep.dpri.kyotou.ac.jp/events/110311tohoku/toda/index.html, 2011.
- Toda, S., R. S. Stein, K. Richards-Dinger, and S. Bozkurt, Forecasting the evolution of seismicity in southern California: Animations built on earthquake stress transfer, J Geophys Res, B05S16, 10.1029/2004JB003415, 2005.Google Scholar
- Waldhauser, F., HypoDD: A computer program to compute double-difference hypocenter locations, US Geol. Surv. Open File Rep., 01-113, 25 pp. 2001.Google Scholar
- Waldhauser, F. and W. L. Ellsworth, A double-difference earthquake location algorithm: method and application to the Northern Hayward fault, Bull. Seismol. Soc. Am., 90, 1353–1368, 2000.View ArticleGoogle Scholar
- Zhang, H. and C. Thurber, Double-Difference Tomography: the method and its application to the Hayward Fault, California, Bull. Seismol. Soc. Am., 93, 1875–1889, 2003.View ArticleGoogle Scholar