Outline of the 2011 off the Pacific coast of Tohoku Earthquake (Mw 9.0) —Seismicity: foreshocks, mainshock, aftershocks, and induced activity—
© 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: 19 May 2011
Published: 27 September 2011
A massive earthquake of a magnitude (M) of 9.0 occurred on March 11, 2011, off the Pacific coast of the northeastern part of Honshu, Japan. Centroid Moment Tensor analysis of the mainshock indicates that it was the reverse fault type, with a WNW-ESE compressional axis. The earthquake occurred on the plate boundary between the island arc and the Pacific plates. Three aftershocks exceeding M 7 occurred within 40-min after the mainshock, and the aftershock area covered a wide range of 500-km × 200-km. Seismicity became active one month before the mainshock, and it continued for two weeks in an adjacent area northeast of the mainshock. Furthermore, foreshock activity with maximum M 7.3 started in the same area two days before the mainshock. Seismic activities increased in almost the entire area of the Japanese Islands after the mainshock. We infer that these earthquakes were induced by the mainshock. JMA displacement-amplitude magnitude of the mainshock was determined to be 8.4, which was smaller than the moment magnitude of 9.0.
Key wordsForeshock and aftershock massive earthquake on the plate boundary induced seismicity northeastern Japan
We belong to the Japan Meteorological Agency (JMA) which determines routinely the hypocenter, the magnitude, and the Centroid Moment Tensor (CMT) solution of each earthquake in and around Japan. JMA also has the naming rights for the great natural disaster. A massive earthquake of MW 9.0 occurred on March 11,2011, off the Pacific coast of the northeastern part of Honshu, Japan. The earthquake caused a huge tsunami which killed more than 10,000 people. JMA named the earthquake “The 2011 off the Pacific coast of Tohoku Earthquake”. In this paper, for the 2011 Tohoku Earthquake, we will report the fundamental information and features of seismicity which we estimated for foreshocks, the mainshock, aftershocks, and induced activity.
2. Method for Estimating Parameters
We determine hypocenters using the arrival times of P-wave and S-wave at seismic stations in Japan. Iterative method (Hamada et al., 1983) is used to calculate hypocenters by taking into consideration the data weight related to the hypocentral distance (Ueno et al., 2002).
Magnitudes are calculated from the maximum seismic wave amplitudes. The displacement magnitude (MD) is adopted to be an official magnitude of JMA, MJ, for relatively large earthquakes (Katsumata, 2004), and the velocity magnitude (MV) is for relatively small earthquakes (Funasaki and Earthquake Prediction Information division, 2004). The MD is determined from the maximum amplitudes of horizontal displacement record obtained with a filter of the period 6 s and the damping the factor 0.55. The MV is determined from the maximum amplitudes of vertical component. MD is adopted as MJ only when MD is able to be estimated. It is well known that MJ is almost the same as MW up to around 8 on the average (Utsu, 1982; Katsumata, 2004). However, when a magnitude is more than 8, MJ is not appropriate due to the saturation of amplitude-magnitude. MW was adopted exceptionally for the official magnitude of the mainshock and the largest aftershock, although it was different from the official procedure, which will be explained in Sections 3.1 and 3.3. In this paper, both M and MJ mean the official magnitude of JMA.
In JMA, the Centroid Moment Tensor (CMT) inversion analysis of earthquakes in and around Japan has been managed since 1994 using the broadband seismographs. The processing technique is based on the methods developed by Kawakatsu (1989). For further details, see Nakamura et al. (2003).
We applied the maximum likelihood estimation method (Aki, 1965) to estimate the b-value, which is a parameter in the Gutenberg-Richter’s formula (Gutenberg and Richter, 1944), of aftershocks. We also estimated the p-value, which is a parameter related with the attenuation of aftershocks, by applying the modified Omori formula (Utsu, 1957) to earthquake data from the occurrence of the mainshock to March 31, 2011.
3. Features of Seismicity
MD of this event was estimated at 8.4 while MW was 9.0. This large difference between MD and MW results from the saturation of amplitude-magnitude. At first, MW was estimated at 8.8 by CMT analysis using a filter of 100–300 s for 30-min teleseismic data. And then, MW was revised to be 9.0 by CMT analysis using a filter of 200–1000 s for 50-min teleseismic data because the filter of 100–300 s and waveforms of 30-min are too short for the analysis of the event. Thus we adopted the value of moment magnitude of 9.0 exceptionally for the official magnitude of JMA with consideration also of the relation between the magnitude of the mainshock and the aftershock area (Utsu, 1961).
The aftershock area covered a wide range of 500-km × 200-km (Fig. 1), and aftershocks occurred at an edge of the relatively large slip area of the mainshock (Yoshida et al., 2011). Three aftershocks of M ~ 7 occurred successively within 40-min after the mainshock. Among them, the focal mechanisms of the M 7.4 and M 7.7 events indicate a reverse fault type like the mainshock. MW of the aftershock which occurred off Ibaraki was estimated to be 7.7 by CMT analysis using a filter of 45–200 s for 10-min local data while MD was 7.4. The difference between MD and MW is very large. We compared seismic waveforms of this aftershock event with those of the largest foreshock (MJ 7.3, MW 7.3) because MD of the two events is similar. As the result, we found that MW of the aftershock was larger than MD because long-period components of waveforms used by CMT analysis of the aftershock were more prominent than that of the largest foreshock. We also checked MW estimated by the U.S. Geological Survey (USGS) and confirmed that both MW were the almost same. Thus we adopted the value of 7.7 exceptionally for the official magnitude. A M 7.5 aftershock occurred beneath the outer rise, and the focal mechanism of this event indicates a normal fault type.
We used the Preliminary Determination of Epicenters of the USGS for aftershock of the 2004 Sumatra and 2010 Chile earthquakes. Aftershocks of the 2011 Tohoku Earthquake are more active than those of the 2004 Sumatra and 2010 Chile earthquakes of almost the same magnitude. Numerous aftershocks have occurred especially in the southern part of the aftershock area (Fig. 4). A p-value of 1.05 and a b-value of 0.78 were estimated for the aftershock of the 2011 Tohoku Earthquake by using events with M ≥ 5.0 immediately after the mainshock until Mar. 31, 2011. Hosono (2006) had estimated the parameters for many aftershock activities in Japan. The estimated p-value ranged from 0.78 to 1.38, and its median was 0.93. The estimated b-value ranged from 0.46 to 0.92, and its median was 0.64. These were estimated from 8 mainshock-aftershock sequences in northeastern Japan. The parameters for the aftershock of the 2011 Tohoku Earthquake are larger than the medians.
3.4 Induced activity
Some aftershocks of the normal fault type occurred beneath the outer rise (Figs. 1(a), 3(d)). It is thought that normal fault type events occur under the influence of the slab bending (Seno and Gonzalez, 1987). In the present case, in addition, some aftershocks beneath the outer rise were induced by the east-west extension field made by the main-shock which released the compressional stress caused by the subduction of the Pacific plate.
Shallow earthquakes of the normal fault type near the Pacific coast in Fukushima, Ibaraki, and Chiba prefectures (Fig. 3(d)) would be “induced earthquakes” rather than “off-fault aftershocks” although these events occurred in the aftershock area we defined. Here the term “off-fault after-shocks” implies descendants while the term “induced earthquakes” means others. It is thought that the shallow earthquakes shown in Fig. 5 were induced by both the dynamic effect due to the seismic wave of the mainshock and the static effect due to crustal deformation. For example, events in volcanic zones may be activated by the degassing reaction of the magma due to the seismic wave. In addition, the shallow earthquakes that occurred in the inland crust may also have been induced by the east-west extension field when the locked region of the plate boundary was slipped by the mainshock and its after-slip. We cannot predict terminations of activated seismicity at the present (Mar. 31, 2011), but, for example, seismicity in volcanic zones in the Hokkaido district induced by the Tokachi-oki earthquake in 2003 (M 8.0) continued for more than half a year (Japan Meteorological Agency, 2005).
A massive MW 9.0 earthquake occurred at 14:46 JST (05:46 UTC) on Mar. 11, 2011, off the Pacific coast of the northeastern part of Japan. The earthquake occurred on the plate boundary between the island arc and the Pacific plates. The focal mechanism of the mainshock indicates a reverse fault type with a WNW-ESE compressional axis. Three aftershocks exceeding M 7 class occurred within 40-min after the mainshock, and the aftershock area covered a wide range of 500-km × 200-km. The aftershocks of the 2011 Tohoku Earthquake are more active than those of the 2004 Sumatra and 2010 Chile earthquakes. Seismic activity occurred one month before the mainshock in an adjacent area northeast of the mainshock, and it continued for two weeks. Furthermore, the largest foreshock of M 7.3 occurred in the same area two days before the M 9 mainshock. The fore-shock area spread around the epicenter of the M 9 main-shock. Seismic activities increased in almost all of Japan after the mainshock. We infer that these earthquakes were induced by both the dynamic effect of the seismic wave from the mainshock and the static effect of crustal deformation. We think that shallow earthquakes of the normal fault type that occurred in the inland crust as well as beneath the outer rise were induced by the east-west extension field resulting from the mainshock, which released compressional stress caused by the subduction of the Pacific plate.
We thank the institutions, universities, and JMA for providing the unified hypocenter catalog. This manuscript was greatly improved by the careful reviews of Dr. A. Hasemi and an anonymous reviewer. Figures were prepared using GMT (Wessel and Smith, 1991).
- Aki, K., Maximum likelihood estimate of b in the formula logN=a-bM and its confidence limits, Bull. Earthq. Res. Inst., 43, 237–239, 1965.Google Scholar
- Funasaki, J. and Earthquake Prediction Information division, Revision of the JMA velocity magnitude, Quart. J. Seismol., 67, 11–20, 2004 (in Japanese with English abstract).Google Scholar
- Gutenberg, B. and C. F. Richter, Frequency of earthquakes in California, Bull. Seismol. Soc. Am., 34, 185–188, 1944.Google Scholar
- Hamada, N., A. Yoshida, and H. Hashimoto, Improvement of the hypocenter determination program of the Japan Meteorological Agency (Reanalyses of the hypocenter distribution of the 1980 Earthquake Swarm off the east coast of the Izu Peninsula and the Matsushiro Earthquake Swarm), Quart. J. Seismol., 48, 35–55, 1983 (in Japanese with English abstract).Google Scholar
- Hosono, K., New standard parameters of aftershocks in Japan, Quart. J. Seismol., 69, 171–176, 2006 (in Japanese).Google Scholar
- Japan Meteorological Agency, Report on the Tokachi-oki Earthquake in 2003, Technical Report of the Japan Meteorological Agency, 126, 228 pp., 2005 (in Japanese with English abstract).Google Scholar
- Katsumata, A., Revision of the JMA displacement magnitude, Quart. J. Seismol., 67, 1–11, 2004 (in Japanese with English abstract).Google Scholar
- Kawakatsu, H., Centroid single force inversion of seismic waves generated by landslides, J. Geophys. Res., 94, 12,363–12,374, 1989.View ArticleGoogle Scholar
- Nakamura, K., S. Aoki, and Y. Yoshida, Centroid moment tensor analysis by using the JMA broadband seismic observation network, Quart. J. Seismol., 66, 1–15, 2003 (in Japanese with English abstract).Google Scholar
- Seno, T. and D. G. Gonzalez, Faulting caused by earthquakes beneath the outer slope of the Japan Trench, J. Phys. Earth, 35, 381–407, 1987.View ArticleGoogle Scholar
- Ueno, H., S. Hatakeyama, T. Aketagawa, J. Funasaki, and N. Hamada, Improvement of hypocenter determination procedures in the Japan Meteorological Agency, Quart. J. Seismol., 65, 123–134, 2002 (in Japanese with English abstract).Google Scholar
- Utsu, T., Magnitude of earthquakes and occurrence of their aftershocks, J. Seismol. Soc. Jpn., 2(10), 35–45, 1957 (in Japanese with English abstract).Google Scholar
- Utsu, T., A statistical study on the occurrence of aftershocks, Geophys. Mag., 30, 521–605, 1961.Google Scholar
- Utsu, T., Relationships between earthquake magnitude scales, Bull. Earthq. Res. Inst., 57, 465–497, 1982.Google Scholar
- Wessel, P. and W. H. F. Smith, Free software helps map and display data, Eos Trans. AGU, 72, 441, 1991.View ArticleGoogle Scholar
- Yoshida, Y., H. Ueno, D. Muto, and S. Aoki, Source process of the 2011 off the Pacific coast of Tohoku Earthquake with the combination of teleseismic and strong motion data, Earth Planets Space, 63, this issue, 565–569, 2011.View ArticleGoogle Scholar