Variability of megathrust earthquakes in the world revealed by the 2011 Tohoku-oki 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 2012
Received: 10 January 2012
Accepted: 27 April 2012
Published: 28 January 2013
The seismicity of the Pacific coast of Tohoku, Japan, has been investigated in detail and characterized into regional seismic segments. The 2011 megathrust earthquake of Mw 9.0 on 11 March ruptured almost all of the segments in that area, causing devastating tsunamis. The prime factor that had not been recognized before is the double segmentation along the Japan trench: The apparent absence of earthquakes in the trench-ward segments as opposed to the Japan Island-ward segments that have repeated smaller earthquakes. We term this pattern of seismic activity ‘along-dip double segmentation (ADDS)’. The 2011 Tohoku megathrust earthquake is typical of a class of great earthquakes different from that of the 1960 Chile earthquake, in which a young and buoyant plate is subducting rapidly under the continental plate. In the 1960 Chile case, the seismic activity is characterized by ‘along-strike single segmentation (ASSS)’, where there is weak seismic activity before the main event all over the plate interface of the subduction zone. We study the greatest earthquakes around the world and find that there is a variety of megathrust earthquakes characterized by ASSS to ADDS, where the 2004 Sumatra-Andaman, the 1960 Chile, the 1964 Alaska and the 2011 Tohoku-oki earthquakes are typical end-members.
A megathrust earthquake of magnitude (Mw) 9.0 occurred off the Pacific coast of Tohoku, Japan, on 11 March, 2011. This resulted in devastating tsunamis larger than any recorded in this area during the past 1,000 years. Based on past and present seismic activity, earthquakes off the Pacific coast of the Tohoku district had been extensively investigated and characterized as occurring on regional seismic segments. These seismic segments have been generally identified as the aftershock region of largest historical earthquakes there. The segmentation is also identified in Japan and its vicinity on the basis of transverse geologic and bathymetric structures on the underthrust and overriding plates (Ando, 1975), where repeated occurrences of large historical earthquakes are known within a particular single segment, or multiple segments. The geometric boundaries segmenting each seismic activity may be subducted sea mounts or ridges, and the deformation and curvature of trenches.
Official earthquake forecasting of Japan estimated a probability of 99% within 30 years of an earthquake of magnitude about 7.5 in the off Miyagi seismic segment, Tohoku, where the hypocenter of the 2011 megathrust earthquake was located. The 2011 megathrust earthquake ruptured almost all of the seismic segments between the Pacific coast of the Tohoku district and the Japan trench. Contiguous segments of the fault spanning more than 500 km broke at once in the earthquake, rather than one or at most two, as had been anticipated. How did this event grow to such a scale?
As has been pointed out previously (Yomogida et al., 2011), a prime factor that had not been recognized before is the along-dip double segmentation along the Japan trench, due to the distinction between shallow and deep seismic segments perpendicular to the trench axis, and their successive ruptures induced by the strong initial break of the trench-ward segments. The double segmentation in the To-hoku district is due to the apparent absence of earthquakes, historically, in the trench-ward segments, in contrast to the smaller (up to Mw 7.5) earthquakes that repeatedly break the deeper, Japan Island-ward segments.
Since we are not able to study the mechanical and dynamical characteristics of a particular plate-interface in detail, we have undertaken a comparative study of megathrust earthquakes in subduction zones of different ages and different tectonic settings. We investigate the focal process of the 2011 megathrust earthquake by comparing it with the greatest earthquakes which are known to have occurred in the world, considering characteristics such as earthquake activity, focal mechanisms, rupture patterns, geometry of subduction zones, types of overriding plates, and back-arc activity.
2. The 2011 Tohoku-oki Megathrust Earthquake
The map in Fig. 1(b) shows a series of segments with many earthquakes along the island arc of Japan. Seismicity in Segments A and C is particularly high, including several earthquakes as large as Mw 8 in Segment A within the last 150-year record. In contrast, seismic activity in Segments D and E was low, with no earthquakes larger than mw 7.8. Therefore, the 30-year probability of an Mw 7.4 event in Segment D was judged to be less than 7%. In Segment E, an earthquake smaller than Mw 7.0 is expected with a probability of about 90%. Although the plot of Fig. 1(b) uses a limited data set from 1950 to 2010, the general pattern of the seismicity is identical to the classical plots by Utsu (2001) who used the data sets of the International Seismo-logical Center and the Japan Meteorological Agency. This drastic difference in seismic activity between two adjacent segments (e.g., Segments C and D) is explained by inter-plate coupling in the north and decoupling in the south (Kanamori, 1977).
In addition, a long and narrow segment along the Japan trench has been recognized at a shallow depth on the Pacific plate in Fig. 1(b). We name these segments A′, B′, and C′, respectively, corresponding to Segments A, B and C. An area of slow slip after the 1994 earthquake (Mw 7.7) in Segment A extended to Segment A′ (Heki et al., 1997). A large slow earthquake occurred in 1896 on Segment B′, giving rise to a large tsunami that struck the eastern coast of northern Tohoku, causing more than 26,000 casualties (Kanamori, 1972; Usami, 1996). Since this slow earthquake generated weak seismic waves but gave rise to a devastating tsunami, this event was one of the largest tsunami earthquakes in over 1000 years in Japan. Recent earthquakes in 1989 (Mw7.4) and 1992 (Mw6.9) occurred in Segment B and extended into Segment B′ as postseismic slow slips (Kawasaki et al., 2001). Slow slips and slow earthquakes in Segments A′ and B′ released about 30% of the interseismic stress accumulation (Heki et al., 1997; Kawasaki et al., 2001). The rest of the 70% deficit is considered to be relaxed by aseismic slips along the subduction zone, or accounted for by some unknown stress accumulation which has been in effect for more than 1000 years (Kanamori et al., 2006). Seismic activity of large earthquakes within Segments B and B′, as well as all the segments at a shallow depth along the Japan trench, has been, however, extremely low. Thus, there has been no probability estimate for a future large earthquake there. Although a future earthquake on the multiple Segments B′ and C′ has been estimated possibly to grow as large as Mw 8 (Tanioka and Satake, 1996), there has been no evidence to infer such an occurrence. The point is that it has been believed that there is a double seismic segmentation along the Japan Trench, as in Fig. 1, and that the segments along the island-arc side of Japan frequently generate earthquakes as large as Mw 8 but the segments along the Japan Trench rupture aseismically. Hereafter, we call this type of peculiar seismic segmentation as along-dip double segmentation (ADDS). Unfortunately, the 2011 megathrust earthquake extended across all these segments, covering an area of about 200 × 500 km2, as in Fig. 1.
Thus, the question is why and how the rupture extended southward into both seismically-inactive Segments D and E, and also the shallow trench-ward segments of the sub-duction zone, resulting in the unexpected devastating occurrence of the 2011 megathrust earthquake. One possible scenario is that the initial rupture in Segment C was accompanied by a rupture in the adjacent trench-ward Segment C′, where these two segments had been believed to be activated independently if they were ruptured. This combined initial rupture could have been strong enough to produce a stress concentration to overcome any existing strong areas (called barriers) to adjacent segments. We believe that the 2011 megathrust earthquake was not a conventional great earthquake, which had been thought to be confined only to multiple Segments B, C, D and E in the island-arc direction. Instead, there occurred the 2011 megathrust event of these segments that also involved trench-ward shallow segments. Reports on tsunami excitation (Maeda et al, 2011) and seismic waveform inversions of teleseismic and strong motion data (Koketsu et al., 2011; Yoshida et al., 2011) revealed a large fault slip in Segments B′ and C′, supporting the scenario of our strong initial rupture. The lack of strong seismic directivity in the excitation of long-period surface waves (Ide et al, 2011; Yomogida et al, 2011) also supports the contention that the majority of the seismic moment release was concentrated in the initial break of the hypocentral area.
The best-known typical megathrust earthquake in Japan is the 1707 Houei great earthquake along the Nankai trough (multiple-segment rupture of Segments F, G and H of Fig. 1(a)). This classical example exhibits a clear lateral (i.e., along the trench-axis direction) interaction between adjacent segments. However, even given our hypothesis for the 2011 megathrust event, we acknowledge that the 2011 event is not the same as the classical 1707 great earthquake, where little seismicity was observed, neither in the land-ward nor the trench-ward areas (Fig. 1(b)). The inactive seismicity in this region not only applies to the period analyzed in Fig. 1(b), but also to the period from 1924 to the present, according to the Japan Meteorological Agency data 2 2 except for the activity following the 1944 To-nankai earthquake in Segment G of Fig. 1(a) and the 1946 Nankaido earthquake in Segment H. Therefore, Segments G and H are also identified as a seismic gap as well as Segment F, which can be found in Fig. 1(b). This type of multiple-segment great earthquake is referred as an earthquake of along-strike single segmentation (ASSS) in contrast to ADDS of the 2011 Tohoku-oki megathrust event. The difference between these two types of segmentations is that strongly-coupled areas of trench-ward segments give rise to ADDS, whereas almost 100% coupled areas of shallow parts of the subduction zone give rise to ASSS. In other words, any seismic gap can be identified for ASSS earthquakes, while there occurs a doughnut pattern of seismic-ity prior to large ADDS earthquakes (Kelleher and Savino, 1975). To support this argument, we consider recent and well-studied great earthquakes around the world, comparing them with the 2011 megathrust earthquake and the 1707 Houei great earthquake.
3. The 1960 Chile Earthquake and the 1964 Alaska Earthquake
Another similarity between the 1960 Chile earthquake and the Nankai trough (the 1707 Houei ruptured area) is the occurrence of slow-slip events in the deeper part of the seismically-coupled area. Slow slip was observed prior to the 1960 Chile by Kanamori and Ciper (1974), and numerous slow-slip events occur at the Nankai trough (Obara, 2002). In the Cascade subduction zone in Canada, the Geological Survey of Canada has found episodic tremor and slip (ETS) 3 3 in the deeper part of the locked patch that is quite similar to slow-slip events in the Nankai trough. Slow slips in the deeper part of coupled areas along subduction zones would be a common feature for the subduction of young, and warmer, oceanic crust, which has been classified by Uyeda and Kanamori (1979) as Chilean-type sub-duction. The strong coupling of the subduction zone would produce a dominant compression over the overriding plate, high uplift rates of the continental arc, which is known as Cordilleran orogeny, and a well-developed accretion complex in the shallow trench (Uyeda, 1982).
The fault geometries of the 1964 Alaska and 2011 Tohoku-oki megathrust earthquakes are very wide with a ratio of fault width to length of 1 : 2~3, whereas that for the 1960 Chile earthquake is about 1 : 5. Seismic absence along the Chile trench and the Nankai trough implies the smooth and strongly-coupled zone along the subduc-tion. Recent GPS observations by Freymueller et al. (2008) and seismic moment release along the rupture zone of the 1964 Alaska earthquake (Doser et al., 2006) reveal a strong variability along the strike of the Alaska and the Aleutian arc. These are the similarities between the 1964 Alaska and 2011 Tohoku-oki megathrusts, the latter of which was discussed in Section 2. We note, however, that the overriding plate in Alaska is continental, forming the Alaskan range, while in Tohoku it is the Japan Islands continental margin with the back-arc basin. There seems to be a strong difference in overriding plates between Alaska and Tohoku, the stress fields in both regions are compressional (Uyeda, 1982; Freymueller et al., 2008), which leads to thrust fault-ings along subduction zones and consequently gives rise to the Pacific-type orogeny (Maruyama, 1997) to the latter.
4. The 2004 Sumatra Earthquake and the 1965 Rat Island Earthquake: Oblique Subductions
Megathrust earthquakes had been believed to occur only in so-called Chilean-type subduction zones (e.g., Kanamori, 1977; Lay et al., 1982; Uyeda, 1982): The fault areas of Chilean-type megathrust earthquakes are very narrow, and the seismicity preceding these earthquakes is very weak. In addition, the oceanic plate subducts rapidly and almost orthogonally to the overriding continental plate. In contrast to the 1960 Chile earthquake, the 2004 Sumatra-Andaman earthquake (Mw 9.3) (Stein and Okal, 2007) shows several peculiar characteristics. The first is that the earthquake occurred at the Sunda-Andaman trench, where the Indo-Australian plate subducts obliquely under the Burma-Sunda subplates: a continental margin. The second is that the event ruptured about 1300 km of a curved plate boundary along which the direction of the subduction changes (Lay et al., 2005). The third is that the source area is where the Burma subplate has been sheared off parallel to the subduction zone as a result of the highly-oblique motion of the Indo-Australia plate due to the back-arc activity. The back-arc tectonics of this area is controlled by the active Andaman Sea spreading center and the Sumatra/Sagaing transform system, which is the typical example of slip-partitioning tectonics (McCaffrey, 1992; Stein and Sella, 2002). The fourth is that this active back-arc activity compensates for the oblique motion of the Indo-Australian plate, leaving the predominantly low-angle thrust motion component observed in the 2004 Sumatra- Andaman earthquake (Lay et al., 2005; Stein and Okal, 2007).
5. Summary and Discussion
Variability of megathrust earthquakes in the world.
1960 Rat Island
Recent GPS observations enable us to estimate slip deficits or plate couplings before the earthquakes occur. Moreno et al. (2010) showed a similarity between an inter-seismic locked patch and coseismic slip on the fault zone of the 2010 Maule earthquake, indicating that an almost 100% coupled-fault area arises in the case of an ASSS. The 2010 Maule earthquake is also identifed as a seismic-gap filling event (Moreno et al., 2010), which is characteristic of an ASSS. Ozawa et al. (2011) showed the distributions of the coseismic, and post-seismic, slip of the 2011 Tohoku-oki earthquake from the ground displacement detected by the GPS network in Japan, which matched the area of the pre-seismic locked zone of the event (Suwa et al., 2006). The area of the strongly-coupled zone in the Tohoku-oki region is restricted, suggesting the characteristics of ADDS, although the position of the preseismic locked zone by Suwa et al. (2006) is a little close to the Japan Islands and away from the central part of the coseismic slip in the event.
It seems strange that the focal mechanism of the 2004 Sumatra-Andaman earthquake is of the low-angle thrust type, where the Indo-Australia plate is subducting highly obliquely. Stein and Okal (2007) fully explained the reason, which is presented in Section 4. The body-wave fault plane solutions of the Rat Island earthquake and its aftershocks have been studied in detail by Stauder (1968), suggesting low-angle thrusting. Wu and Kanamori (1973) found that the radiation pattern of long-period surface waves of the Rat Island earthquake is consistent with Stauder’s solutions, but with a considerable strike-slip component. Since then, many large earthquakes have occurred in the Rat-, and the Andreanof-, Island regions whose focal-mechanism solutions are either low-angle thrusting with a small amount of strike-slip component or the right-lateral strike-slip type as in Fig. 5. We could, therefore, conclude that the focal mechanism of great earthquakes along a curved plate boundary, where the subduction of the oceanic plate is highly oblique, would be low-angle thrust faulting. This idea would help us to understand future earthquakes along curved plate boundaries with oblique subduction.
Slow-slip events would be a general feature in the deeper part of ASSS. We note two slow earthquakes (Kawasaki et al., 2001) and the tsunami earthquake (Tanioka and Satake, 1996) at the northern terminus of the 2011 Tohoku-oki megathrust. The southern terminus of the rupture zone of the 2011 Tohoku-oki megathrust is thought to be a region of little seismic potential for large earthquakes. For the 1964 Alaska, it seems that the creeping zone (Fig. 6), next to the PWS asperity (Fig. 3), prevented the rupture propagation from a strong initial break (Wyss and Brune, 1967; Ruff and Kanamori, 1983), which may result in a seismic directivity of long-period surface waves unoriented to that of its aftershock region (Kanamori, 1970). Therefore, we propose that slow-slip events occur very close to the strongly-coupled zones due to the along-strike variability of subduc-tion zones. However, this hypothesis needs further justification.
What we have found in this study is the variety of megathrust earthquakes associated with the rupture of multiple seismic segments, which are no longer confined to a single or double seismic segments. We need to consider both along-dip, and along-strike, rupture propagations for the possible occurrence of a megathrust earthquake. The along-dip variability of subduction zones can be understood by the evolution of sedimentary layers in its plate interface (Bilek and Lay, 1999). Although along-strike variability of subduction zones has been pointed out by GPS observations (e.g., Freymueller et al., 2008), characterized by various types of slow-seismic events (e.g., Obara, 2009) and classified by the lateral variation of sedimentary layers (e.g., Tsuru et al., 2002), there still remains the questions how the strong initial rupture occurs and how the rupture extends laterally along the strike direction overcoming any existing fault-resistant areas (called barriers) resulting in a multiple-segment rupture.
We should not construct a future large-earthquake scenario in a given region based solely on seismic activity recorded over a short period of time, such as less than 1,000 years. We should also consider short-term (geodetic/seismic), and long-term (geologic or relative plate velocity), observations on strain accumulations along the subduction zones. Although a seismic gap would indicate a possible future earthquake in regions of ASSS, such a gap would not be identified in regions of ADDS due to seismic activity on the land-ward side.
The traditional one-dimensional segmentation scheme, of one subduction zone divided into a series of segments along the trench axis, does not apply in many cases. It would work for ASSS regions, such as is illustrated in Fig. 1. The 1960 Chile great earthquake that ruptured along-strike segments, one by one, where all the segments appear to be fully coupled beforehand. In contrast, for ADDS regions, the successive initial rupture of double segments in the deep and shallow parts of the subduction zone must be considered, which should induce secondary ruptures of surrounding segments.
The successive initial rupture of the double segmentation, which turned out to be dominant in the 2011 megathrust earthquake, has been overlooked completely because of the successive lateral ruptures in the 1960 Chile and 2004 Sumatra earthquakes, as examples in the past. This wide range of variation in rupture behavior is likely to be caused by variations in the nature of subduction due to plate age, convergence rate, amount of accretion sediments, geometrical irregularities including seamounts, overriding plates and back-arc activity. Further new ideas are required with respect to their classifications, based not on the traditional one-dimensional scheme, but on a two-dimensional scheme incorporating the segmentations of seismic zones.
The shallow segment of the subduction zone (Segment C′ in Fig. 1(a)) of the 2011 earthquake had been believed to be safe because of its sparse seismicity and the absence of historical records of large earthquakes. Slow earthquakes and slow slips were believed to be due to weak and soft materials at shallow depths near its trench axis. We must now recognize that such a shallow zone may cause large seismic slips, which can eventually lead to a megathrust earthquake.
Looking only at seismicity near Japan, we find two types of segmentations, ASSS in the Nankai Trough and ADDS in Hokkaido (Fig. 1(b)). Therefore, we need to focus on these areas to learn more about the two different types of megathrust earthquakes that may occur in the near future.
We appreciate the help of Yosio Nakamura of the University of Texas for kindly reading the draft paper in the early stage of this study and helping us to improve the understanding of seismic segmentations. We are also grateful to S. Stein of Northwestern University for his critical reviews to improve and deepen the discussions of our manuscript.
- Ammon, C. J., C. Ji, H.-K. Thio, D. Robson, S. Ni, V. Hjorleifsdottir, H. Kanamori, T. Lay, S. Das, D. Helmberger, G. Ichinose, J. Polet, and D. Wald, Rupture process of the 2004 Sumatra-Andaman earthquake, Science, 308, 1133–1139, 2005.View ArticleGoogle Scholar
- Ando, M., Source mechanisms and tectonic significance of historical earthquakes along the Nankai trough, Japan, Tectonophysics, 27, 119–140, 1975.View ArticleGoogle Scholar
- Bilek, S. L. and T. Lay, Rigidity variations with depth along interpolate megathrust faults in subduction zones, Nature, 400, 443–446, 1999.View ArticleGoogle Scholar
- Cisternas, M., B. F. Atwater, F. Torrejon, Y. Sawai, G. Machuca, M. Lagos, A. Eipert, C. Youlton, I. Salgado, T. Kamataki, M. Shishikura, C. P. Rajendran, J. K. Malik, Y. Rizal, and M. Husni, Predecessors of the giant 1960 Chile earthquake, Nature, 437, doi:10.1038/nature03943, 2005.Google Scholar
- Comte, D. and S. Beck, The 2010 Chile earthquake-Variations in the rupture mode, in Giant Earthquakes and Their Tsunamis, AGU Chapman Conference, 56pp, USGS, Valparaiso, 2010.Google Scholar
- Doser, D. I., A. M. Veileux, C. Flores, and W. A. Brown, Changes in seismic-moment rates along the rupture zones of the 1964 great Alaska earthquake, Bull. Seismol. Soc. Am., 96, 1545–1550, 2006.View ArticleGoogle Scholar
- Engdahl, E. R., R. van der Hilst, and R. Buland, Global teleseismic earthquake relocation with improved travel times and procedures for depth determination, Bull. Seismol. Soc. Am., 88, 722–743, 1998.Google Scholar
- Freymueller, J. T., H. Woodard, S. C. Cohen, R. Cross, J. Elliot, C. F. Larson, S. Hreinsdottir, and C. Zweck, Active deformation process in Alaska, based on 15 years of GPS measurements, in Active Tectonics and Seismic Potential in Alaska, edited by J. T. Freymueller, P. T. Haeussler, R. L. Wesson, and G. Ekstrom, 431 pp., Geophysical Monograph Series, AGU, 179, Washington D.C., 2008.View ArticleGoogle Scholar
- Heki, K., S. Miyazaki, and Y. Tamura, Silent fault slip following an interpolate thrust earthquake at the Japan trench, Nature, 386, 595–597, 1997.View ArticleGoogle Scholar
- Ide, S., A. Baltay, and G. C. Beroza, Shallow dynamic overshoot and energetic deep rupture in the 2011 Mw9.0 Tohoku-oki earthquake, Science Mag., 332, 1426–1429, 2011.Google Scholar
- Johnson, J. M., K. Satake, S. R. Holdahl, and J. Sauber, The 1964 Prince William Sound earthquake: Joint Inversion of tsunami and geodetic data, J. Geophys. Res., 101, 523–532, 1996.View ArticleGoogle Scholar
- Kanamori, H., The Alaska earthquake of 1964: Radiation of long-period surface waves and source mechanism, J. Geophys. Res., 75, 5029–5040, 1970.View ArticleGoogle Scholar
- Kanamori, H., Mechanism of tsunami earthquakes, Phys. Earth Planet. Inter., 6, 346–359, 1972.View ArticleGoogle Scholar
- Kanamori, H., Seismic and aseismic slip along subduction zones and their tectonic implications, in Island Arcs, Deep Sea Trenches and Back-arc Basins, edited by M. Talwani and W. C. Pitman III, 470 pp., AGU, Washington D.C., 1977.Google Scholar
- Kanamori, H. and J.J. Cipar, Focal process of the great Chilean earthquake May 22, 1960, Phys. Earth Planet. Inter., 9, 128–136, 1974.View ArticleGoogle Scholar
- Kanamori, H., M. Miyazawa, and J. Mori, Investigation of the earthquake off Miyagi prefecture with historical seismograms, Earth Planets Space, 58, 1533–1541, 2006.View ArticleGoogle Scholar
- Kawasaki, I., Y. Asai, and Y. Tamura, Space-time distribution of interpolate moment release inducing slow earthquakes and the seismo-geodetic coupling in the Sanriku-oki region along the Japan trench, Tectono-physics, 330, 267–283, 2001.View ArticleGoogle Scholar
- Kelleher, J. and J. Savino, Distribution of seismicity before large strike-slip and thrust-type earthquakes, J. Geophys. Res., 80, 260–271, 1975.View ArticleGoogle Scholar
- Koketsu, K., Y. Yokota, N. Nishimura, Y. Yagi, S. Miyazaki, K. Satake, Y. Fujii, H. Miyake, S. Sakai, Y. Yamanaka, and T. Okada, A unified source model for the 2011 Tohoku earthquake, Earth Planet. Sci. Lett., 310, 480–487, 2011.View ArticleGoogle Scholar
- Lay, T., H. Kanamori, and L. Ruff, The asperity model and the nature of large subduction zone earthquakes, Earthq. Predict. Res., 1, 3–71, 1982.Google Scholar
- Lay, T., H. Kanamori, C. J. Ammon, M. Nettles, S. N. Ward, R. C. Aster, S. L. Beck, S. L. Bilek, M. R. Brudzinski, R. Butler, H. R. DeShon, G. Ekstrom, K. Satake, and S. Sipkin, The great Sumatra-Andaman earthquake of 26 December 2004, Science, 308, 1127–1133, 2005.View ArticleGoogle Scholar
- Maeda, T., T. Furumura, S. Sakai, and M. Shinohara, Significant tsunami observed at ocean-bottom pressure gauges during the 2011 off the Pacific coast of Tohoku Earthquake, Earth Planets Space, 63, 803–808, 2011.View ArticleGoogle Scholar
- Marlow, M. S., A. K. Cooper, S. V. Dadisman, E. L. Geist, and P. R. Carlson, Bowers swell: evidence for a zone of compressive deformation concentric with Bowers ridge, Bering Sea, Mar. Petrol. Geol., 7, 398–408, 1990.View ArticleGoogle Scholar
- Maruyama, S., Pacific-type orogeny revisited: Miyamushiro-type orogeny produced, Island Arc, 6, 91–120, 1997.View ArticleGoogle Scholar
- McCaffrey, R., Oblique plate convergence, slip vectors and forearc deformation, J. Geophys. Res., 97, 8905–8915, 1992.View ArticleGoogle Scholar
- Moreno, M., M. Rosenau, and O. Oncken, 2010 Maule earthquake slip correlates with pre-seismic locking of Andean subduction zone, Nature, 467, 198–202, 2010.View ArticleGoogle Scholar
- Neprochnov, Y. P., V. V. Sedov, L. R. Merklin, V. P. Zinkevich, O. V. Levchenko, B. V. Baranov, and G. B. Rudnik, Tectonics of the Shirshov ridge, Bering sea, Geotectonics, 19, 194–206, 1985.Google Scholar
- Obara, K., Nonvolcanic deep tremor associated with subduction in southwest Japan, Science, 296, 1679–1681, 2002.View ArticleGoogle Scholar
- Obara, K., Inhomogeneous distribution of deep slow earthquake activity along the strike of the subducting Philippine Sea Plate, Gondwana Res., 16, 512–526, doi:10.1016/j.gr.2009.04.011, 2009.View ArticleGoogle Scholar
- Ozawa, S., T. Nishimura, H. Suito, T. Kobayashi, M. Tobita, and T. Imakiire, Coseismic and postseismic slip of the 2011 magnitude-9 Tohoku-oki earthquake, Nature, 475, 373–377, 2011.View ArticleGoogle Scholar
- Ruff, L. and H. Kanamori, The rupture process and asperity distribution of three great earthquakes from long-period diffracted P-waves, Phys. Earth Planet. Inter., 31, 202–230, 1983.View ArticleGoogle Scholar
- Shao, G., X. Li, C. Ji, and T. Maeda, Focal mechanism and slip history of the 2011 Mw 9.1 off the Pacific coast of Tohoku Earthquake, constrained with teleseismic body and surface waves, Earth Planets Space, 63, 559–564, 2011.View ArticleGoogle Scholar
- Stauder, W., Mechanism of the Rat Island earthquake sequence of February 4, 1965, with relation to island arcs and sea floor spreading, J. Geophys. Res., 73, 3847–3858, 1968.View ArticleGoogle Scholar
- Stein, S. and E. A. Okal, Ultralong period seismic study of the December 2004 Indian ocean earthquake and implication for regional tectonics and the subduction process, Bull. Seismol. Soc. Am., 97, S279–S295, 2007.View ArticleGoogle Scholar
- Stein, S. and G. F. Sella, Plate boundary zones: Concept and approaches, in Plate Boundary Zones, edited by S. Stein and J. Freymueller, AGU Geodynamics Series, 30, 425 pp., AGU, Washington D.C., 2002.View ArticleGoogle Scholar
- Suwa, Y., S. Miura, A. Hasegawa, T. Sato, and K. Tachibana, Interplate coupling beneath NE Japan inferred from three-dimensional displacement field, J. Geophys. Res., 111, B04402, doi:10.1029/2004JB003203, 2006.Google Scholar
- Tanioka, Y. and K. Satake, Fault parameters of the 1896 Sanriku tsunami earthquake estimated from tsunami numerical modeling, Geophys. Res. Lett., 23, 1549–1552, 1996.View ArticleGoogle Scholar
- Tsuru, T., J. O. Park, S. Miura, S. Kodaira, Y. Kido, and T. Hayashi, Along-arc structural variation of the plate boundary at the Japan Trench margin: Implication of interpolate coupling, J. Geophys. Res., 107(B12), 2357, doi:10.1029/2001JB001664, 2002.Google Scholar
- Usami, T., Catalogue of Disastrous Earthquakes in Japan from 416 to 1995, 493 pp., Tokyo Univ. Press, Tokyo, 1996 (in Japanese).Google Scholar
- Utsu, T., Seismology, third edition, 376 pp., Kyoritsu Pub., Tokyo, 2001 (in Japanese).Google Scholar
- Uyeda, S., Subduction zones: An introduction to comparative subductol-ogy, Tectonophysics, 81, 133–159, 1982.View ArticleGoogle Scholar
- Uyeda, S. and H. Kanamori, Back-arc opening and the mode of subduc-tion, J. Geophys. Res., 84, 1049–1061, 1979.View ArticleGoogle Scholar
- Wu, F. T. and H. Kanamori, Source mechanism of February 4, 1965, Rat Island earthquake, J. Geophys. Res., 78, 6082–6092, 1973.View ArticleGoogle Scholar
- Wyss, M. and J. N. Brune, The Alaska earthquake of 28 March 1964: A complex multiple rupture, Bull. Seismol. Soc. Am., 57, 1017–1023, 1967.Google Scholar
- Yomogida, K., K. Yoshizawa, J. Koyama, and M. Tsuzuki, Along-dip segmentation of the 2011 off the Pacific coast of Tohoku Earthquake and comparison with other megathrust earthquakes, Earth Planets Space, 63, 697–701, 2011.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, 565–569, 2011.View ArticleGoogle Scholar