An effective absorbing boundary condition for linear long-wave and linear dispersive-wave tsunami simulations. Circles denote observed maximum tsunami inundation or runup heights during the Hoei earthquake [. Slip parameters on major thrusts at a convergent plate boundary: regional heterogeneity of potential slip distance at the shallow portion of the subducting plate. Le bassin de la préfecture de Nara présente des traces de liquéfaction des sols due au séisme[12]. Also, studies on interplate coupling along the Nankai Trough based on the GEONET data [e.g., Ichitani et al., 2010; Hashimoto et al., 2009; Nishimura et al., 1999; T. Hashimoto, http://www.jamstec.go.jp/esc/projects/fy2009/12-hashi.html] reveal an area where strong interplate coupling occurs along the Nankai Trough subduction zone. The height of the tsunami due to the N5′ fault is very strong to spread large tsunami wavefront from Cape Ashizuri to Hyuga‐nada (Figure 8a; T = 15 min). Just after the earthquake occurs, the height of the surface of Ryujin Lake subsides to 30 cm below mean sea level and then gradually decreases to 40 cm below mean sea level due to the dilatational wave of the tsunami. Rupture process of the 1946 Nankai earthquake estimated using seismic waveforms and geodetic data. Retrieval of long-wave tsunami Green’s function from the cross-correlation of continuous ocean waves excited by far-field random noise sources on the basis of a first-order Born approximation. Journal of Japan Society of Civil Engineers, Ser. Further effort is needed to establish the shaking intensity in Kyushu in 1707.In the present paper, we have focused mainly on the significance of the elongation of the Hoei earthquake source rupture to Hyuga‐nada in terms of the strengthening of tsunami height and onshore tsunami runup. R4 indicates the area of tsunami inundation simulation in the area surrounding Ryujin Lake (. Nankaido, Japan (28 October 1707) A magnitude 8.4 earthquake caused seawaves as high as 25 m to hammer into the Pacific coasts of Kyushyu, Shikoku and Honshin. The strongest tidal wave registered in Japan so far reached a height of 90 meters. FDM Simulation of Seismic Waves, Ocean Acoustic Waves, and Tsunamis Based on Tsunami-Coupled Equations of Motion. Red and blue denote ground surface upheaval and subsidence, respectively. of the Earthquake Invest. Interseismic Coupling‐Based Earthquake and Tsunami Scenarios for the Nankai Trough. [37] The results of the tsunami inundation simulation for the new Hoei earthquake model are shown in Animation S3 and in Figure 11 as a sequence of snapshots of the water surface of the Ryujin Lake after T = 14, 19, 24, 29, 34, and 39 min from the start of the earthquake, illustrating the way in which a tsunami with a large flux can inundate Ryujin Lake. 23 Feb. 2015. [2003] and others from the westernmost end of Shikoku to Hyuga‐nada, where strong interplate coupling has been found by studies using the GEONET data. Thus, further supporting evidence is needed to develop a reliable and detailed source rupture history for the Hoei earthquake. Snapshots of the tsunami associated with the 1707 Hoei earthquake at (a) T = 1.0 min, (b) T = 5.0 min, (c) T = 10.0 min, (d) T = 20.0 min, (e) T = 40.0 min, and (f) T = 80.0 min after the earthquake origin time. In Tosa, 11,170 houses were washed away, and 18,441 people drowned. Nankai earthquake (南海地震) measuring 8.4 hit at 4:19 [local time] there was a catastrophic earthquake on the southwest of Japan in the Nankai area. [45] Actually, the source model of An'naka et al. [16] Figure 5 illustrates the distribution of maximum simulated tsunami height for An'naka et al. Thick solid and dashed contour lines illustrate slip delay and advance rate at the plate boundary derived by analysis of GPS data by. Journal of Geophysical Research: Earth Surface. De plus, le séisme a engendré un important glissement de terrain, dans la préfecture de Shizuoka, connu sous le nom de glissement d'Ohya[10]. The Nankai Trough earthquake tsunamis in Korea: numerical studies of the 1707 Hoei earthquake and physics-based scenarios. The earthquake caused more than 5,000 casualties, destroyed 29,000 houses, and triggered at least one major landslide, the Ohya slide in Shizuoka. The 1498 Nankai earthquake occurred off the coast of Nankaidō, Japan, at about 08:00 local time on 20 September 1498. [26] We then modified the geometry of the N5 subfault segment and narrowed it in the direction perpendicular to the trench axis. The later snapshot (Figures 4d and 4e; T = 20 and 40 min) illustrate the arrival of the large tsunami along the Pacific coast from the westernmost end of Shikoku to Hyuga‐nada. The height of the tsunami was 7 meters (23 feet). Nankaido, Japan This earthquake had a magnitude of 8.4. souhaitée]. This irregular behavior suggests that in addition to the regular Nankai Trough earthquake cycle of 100–150 years, there is a hyperearthquake cycle of 300–500 years. This study was supported by the Research Project “Improvements in strong ground motion and tsunami simulation accuracy for application to realistic disaster prevention of Nankai Trough megathrust earthquakes” of the Ministry of Education, Culture, Sports and Technology of Japan. The rupture of each subfault takes 5 s. For simplicity, we assumed that the shape of the initial tsunami on the sea surface is identical to the sea bottom deformation associated with the earthquake. Figure 8a shows the pattern of ground deformation derived from the new Hoei earthquake source model with subfault segments N1 to N5, demonstrating the extension of the ground subsidence area to Kyushu with maximum ground subsidence of 2 m in a narrow belt from Shikoku to Hyuga‐nada. The simulated maximum tsunami height along the Pacific coast from Tosa Bay to Suruga Bay generally agrees well with observed tsunami runup during the Hoei earthquake [e.g., Hatori, 1974, 1985; Murakami et al., 1996]. [40] In order to evaluate the ability of the water flow in the narrow waterway to transport sea sand into the lake through the channel, we calculated the Shields number [e.g., Takahashi et al., 1993], which is an index to specify strength of transporting capability due to water currents [e.g., Takahashi et al., 1993]. These correspond to ground upheaval areas associated with the Hoei earthquake (Figure 2). 7. The existence of the tsunami lakes in Kyushu was not well explained by the expected ground deformation pattern produced by the former Hoei earthquake source model where the fault rupture stopped at the westernmost end of Shikoku, not extending to Hyuga‐nada. Il fait partie des trois plus importants glissements de terrain du Japon, concernant une surface de 1,8 km2 pour un volume estimé à plus de 120 millions de m³[11]. Figure 4b (T = 5.0 min) illustrates two such peaks of elevated sea surface parallel to the trough. [2009] based on the inversion of horizontal and vertical ground movement data from the GEONET. Any queries (other than missing content) should be directed to the corresponding author for the article. Radiation of tsunamis from rectangular fault sources has been confirmed to be very strong in the direction perpendicular to the trough axis, while it is very weak in the direction parallel to the trough. It occurred on December 21, 1946, at 04:19 JST (December 20, 19:19 UTC). The Hyuga-nada Earthquake on June 30th, 1498 is a Fake Earthquake. [51] We thank two anonymous reviewers and an associate editor for their constructive comments for improving manuscript. Ise Bay, Japan The earthquake that caused the Ise Bay tsunami is best estimated as being of magnitude 8.2. [21] Ten years of data from the nationwide GEONET GPS network illustrates the current pattern of ground deformation (Figure 6). Dynamic rupture scenarios of anticipated Nankai‐Tonankai earthquakes, southwest Japan, Journal of Geophysical Research: Solid Earth, http://www.jamstec.go.jp/esc/projects/fy2009/12-hashi.html, Animation S1. We modified the model to reconstruct the original shoreline structure by removing recent artificial constructions, such as concrete breakwaters and wharfs created by recent shoreline protection projects. Journal of Geophysical Research: Solid Earth. Nov 20, 1755. Properties of Rocks, Computational Our belief based on detail tsunami simulation is that the source rupture area of the Hoei earthquake extended an additional 70 km eastward to the Hyuga‐nada from the westernmost end of Shikoku. Yet the simulated tsunami height at Yonouzu is less than 4 m, which is comparable to the tsunami caused by the 1854 Ansei Nankai earthquake but much shorter than the tsunami experienced with the Hoei earthquake. Le séisme est à l'origine d'un tsunami qui a touché toute la côte sud-ouest de Kōchi, avec des vagues d'une hauteur moyenne de 7,7 m, et qui ont dépassé les 10 m par endroits[14], avec des maximum de 25,7 m à Kure (Nakatosa, Kōchi) et de 23 m à Tanezaki[15]. 1586 Ise Bay earthquake and tsunami caused over 8,000 deaths; 1707 Nankaido earthquake and tsunami caused 30,000 deaths; 1771 Ryukyu Islands earthquake-generated tsunami caused over 13,000 deaths ; 1896 Sanriku earthquake and tsunami caused over 27,000 deaths; 1) Alert Information: International PTWC Official Messages (DOC, 381 KB) WC/ATWC Official Messages (DOC, 434 KB) JMA Official … For example, historical archives document that at Yonouzu village, at the northern end of Hyuga‐nada, the tsunami was more than 10 m and killed 18 people [Chida et al., 2003; Chida and Nakayama, 2006]. Notes. Based on the latest death toll, the tsunamis generated by an earthquake Sunday off the coast of Sumatra, Indonesia is the worst in history. The height of the tsunami during the Hoei earthquake at Yonouzu was several times larger than that experienced during the 1854 Ansei earthquake. Animation S2a. The 1707 Mw8.7 Hoei earthquake triggered the largest historical eruption of Mt. The Hoei earthquake was a larger event in which rupture spread as far as Hyuga‐nada, incorporating the fifth subfault, N5. [29] Snapshots of tsunami propagation derived by the simulation for the new Hoei earthquake source model with subfault segments N1 to N5′ and the former Hoei earthquake model without segment N5′ are compared in Figure 8 and in Animation S2. However, it should be kept in mind that objective data, such as shaking intensities and tsunami heights in Kyushu, were rather limited at that time and thus, these data may not well incorporated in their analysis. We hope recent investigation of high‐resolution geological and geophysical experiments will provide high‐density reliable subsurface structure model as well as heterogeneous source rupture model. Yes. Therefore, the Hoei earthquake is often referred as a worst case scenario for earthquakes occurring in the Nankai Trough. 2nd ser.). A total of nearly 30,000 buildings were damaged in the affected regions and about 30,000 people were killed. It is difficult to say if the 1771 tsunami which struck the tropical southern islands of Japan was worse than the 1707 Hōei tsunami or 1792 Unzen tsunami. This explains the description in ancient documents of an exceptionally large tsunami approximately 10 m high occurring during the Hoei earthquake [Chida et al., 2003]. [31] Our tsunami simulation for the new Hoei earthquake model produces a very tall tsunami, 5 to 8 m high at Yonouzu, located approximately 5 km away from Ryujin Lake in Kyushu where the height from the former Hoei earthquake model was less than 2 m (Figure 9). and Chemical Oceanography, Physical Vertical ground surface deformation derived by the revised 1707 Hoei earthquake source model: (a) an extended source model produced by adding a new N5 subfault segment at the Hyuga‐nada and (b) a subfault model with segment N5′ shortened in the direction perpendicular to the trench. [14] Using the results of the coseismic ground deformation pattern, we conducted a tsunami simulation for the Hoei earthquake. In order to improve tsunami height and ground subsidence in Kyushu, we have to modify source model more drastically. The sea waves were as high as 25 m to hammer into the Pacific coasts of Kyushyu, Shikoku and Honshin. [50] Baba et al. [2003] which is described by four (N1–N4) panels of subfaults might be too simple to demonstrate complicated source rupture history of the Nankai Trough earthquake which should be described by rupture above the subducting Philippine Sea plate and landward dipping splay branch from the plate interface. Le bilan humain lié au séisme et au tsunami qui s'en est ensuivi est estimé à plus de 5 000 victimes[4]. Animation S3. We succeeded in explaining development of the large tsunami from Cape Ashizuri to Hyuga‐nada with maximum tsunami heights of 5 to 10 m that attack along the Pacific coast from the westernmost end of Shikoku to Hyuga‐nada. To open auxiliary materials in a browser, click on the label. It shows that an area of strong interplate coupling with high coupling ratios is found from Suruga Bay to Hyuga‐nada, more than 100 km beyond the westernmost end of Shikoku which we have considered to be the boundary of the source rupture area for the Nankai Trough earthquake. Introduction to ocean floor networks and their scientific application. The death toll associated with this event is uncertain, but between 5,000 and 41,000 casualties were reported. Un autre moyen d'estimation de la puissance du séisme est le degré des dommages et de la hauteur des inondations liés à un tsunami et les tsunamis enregistrés dans des lieux éloignés, comme à Nagasaki et à Jeju-do en Corée du Sud[13]. Tsunamis from the 684 Tenmu, 1361 Shokei, and 1707 Hoei earthquakes deposited sand in Ryujin Lake and around the channel connecting it to the sea, but lesser tsunamis from other earthquakes were unable to reach Ryujin Lake. Le chevauchement de Nankai est subdivisé en cinq blocs, nommés de A à E, qui peuvent se rompre indépendamment les uns des autres[6],[7]. This implies that the large inflow flux of the tsunami through the channel can carry large masses of sea sand into the lake very effectively, but leaves most of the sand in the lake near the channel when the tsunami goes back to sea. Thus, the Hoei earthquake was not a linkage occurrence of the 1854 Ansei Nankai and the Ansei Tokai earthquakes but a much larger event. Historical Nankai-Suruga megathrust earthquakes recorded by tsunami and terrestrial mass movement deposits on the Shirasuka coastal lowlands, Shizuoka Prefecture, Japan. The source model also failed to explain the larger tsunami experienced during the Hoei earthquake from Cape Ashizuri to Hyuga‐nada as compared with the tsunami associated with the 1854 Ansei Nankai earthquake. Based on recent findings of geodetic and geological investigations, we present a revised source-rupture model for the great 1707 Hoei earthquake that occurred in the Nankai Trough off southwestern Japan. Preparing for the Future Nankai Trough Tsunami: A Data Assimilation and Inversion Analysis From Various Observational Systems. This implies that the source rupture area of the Nankai subfault segments might not stop at the westernmost end of Shikoku as most source models assume [Ando, 1975; Aida, 1981; An'naka et al., 2003], but may extend further, to Hyuga‐nada. [2003] to examine the effectiveness of the present source model for reproducing observed height of the tsunami along the Pacific coast of the Nankai Trough [Hatori, 1974, 1985; Murakami et al., 1996]. The tsunami traveled across the Atlantic Ocean as well. If you do not receive an email within 10 minutes, your email address may not be registered, Geophysics, Marine [39] Figure 12 shows changes of the water height in Ryujin Lake and the flow speed of water in the entrance of the lake connecting to the channel. This pattern of vertical ground movement is considered to illustrate the process of recovery of ground surface deformation due to the Nankai Trough earthquakes. Advanced Tsunami Computation for Urban Regions. As time passes, the raised mass of seawater gradually spreads bilaterally as two tsunamis, one propagating toward the seashore and the other to the open ocean at a faster speed. Oct 28, 1707. Osaka was also damaged. Additional file information is provided in the readme.txt. Nankaido, Japan A magnitude 8.4 earthquake caused sea waves as high as 25 m to hammer into the Pacific coasts of Kyushyu, Shikoku and Honshin. It was reported that roughly a dozen large waves were counted between 3 pm and 4 pm, some of them extending several kilometres inland at Kochi. Ryujin Lake, however, recently observed by Okamura et al. Hondo, Japan Estimated Number of Deaths: 27,000 Year: 1826. Difference between Tidal Wave and Tsunami (CSS-2018) La magnitude du séisme de 1707 a été supérieure à celle des deux séismes conjoints qui se sont produits à Ansei-Tōkai en 1854, dont l'estimation est basée sur plusieurs observations. [13] Figure 2 illustrates the calculated vertical ground deformation due to fault rupture of the N1 through N4 fault segments for the Hoei earthquake, derived following Mansinha and Smylie [1971]. Therefore, the large tsunami generated by the rupture of the N5′ subfault segment and the swift current it produces in the channel is the only agent that can explain the transport of sea sand into the lake. As a result, the incremental change in tsunami height due to the N5′ subfault is very significant along the coast from the westernmost end of Shikoku to Hyuga‐nada. It had an estimated magnitude of 7.9 on the surface wave magnitude scale and triggered a devastating tsunami that resulted in thousands of deaths in the Nankai and Tōkai regions of Japan.It is uncertain whether there were two separate earthquakes separated by a short time interval or a single event. The tsunami runup into Ryujin Lake estimated by the tsunami inundation simulation using a high‐resolution bathymetry model demonstrates the process whereby a large flow of seawater with a large difference in inflow and outflow speeds can transport and deposit sea sand into the lake near the inflow channel very effectively. 6. Physics, Comets and Number of times cited according to CrossRef: Identifying storm surge deposits in the muddy intertidal zone of Ena Bay, Central Japan. The C14 age determination for the sedimentation of Ryujin Lake revealed that three sheets of sand layers sandwiched between muddy host sediments were developed during the 1707 Hoei, the 1361 Shohei, and the 684 Tenmu earthquakes [Okamura et al., 2003, 2004]. Now at Tsunami Engineering Laboratory, Disaster Control Research Center, Tohoku University, Sendai, Japan. From Deep Sea to on Land, Inter‐plate coupling along the Nanaki trough and southeastward motion along southern part of Kyushu, Tectonic movements of recent 10000 years and observations of historical tsunamis based on coastal lake deposits, Seismic activities along Nankai Trough recorded in coastal lake deposits, Recurrence intervals of super Nankai earthquakes. La dernière modification de cette page a été faite le 17 octobre 2019 à 16:22. Il causa des dommages plus ou moins importants dans le sud-ouest des îles de Honshu et de Shikoku et dans le sud-est de l'île de Kyūshū[3]. Coseismic slip resolution along a plate boundary megathrust: The Nankai Trough, southwest Japan, Depth distribution of coseismic slip along the Nankai Trough, Japan, from joint inversion of geodetic and tsunami data, Sources of tsunami and tsunamigenic earthquakes in subduction zones, Origin and evolution of a splay fault in the Nankai accretionary wedge, Numerical simulation of topography change due to tsunamis, Interpretation of the slip distributions estimated using tsunami waveforms for the 1944 Tonankai and 1946 Nankai earthquakes, Detailed coseimic slip distribution of the 1944 Tonankai earthquake estimated from tsunami waveforms, Study of tsunami traces in lake floor sediment of the Lake Hamanako, Prehistorical and historical tsunami traces in lake floor deposits, Oike Lake, Owase City and Suwaike Lake, Kii‐Nagashima City, Mie Prefecture, central Japan, Earthquakes of recent 2000 years recorded in geologic strata, Descriptive table of major earthquakes in and near Japan which were accompanied by damages, Materials for Comprehensive List of Destructive Earthquakes in Japan, Partitioning between seismogenic and aseismic slip as highlighted from slow slip events in Hyuga‐nada, Japan, Source process of the 1944 Tonankai and the 1945 Mikawa earthquake, Difference in the maximum magnitude of interpolate earthquakes off Shikoku and in the Hyuganada region, southwest Japan, inferred from the temperature distribution obtained from numerical modeling: The proposed Hyuganada triangle. Web. This implies that unusually large earthquakes associated with larger tsunamis than usual have struck there during the 1707 Hoei, the 1361 Shohei, and the 684 Tenmu earthquakes. Data assimilation with dispersive tsunami model: a test for the Nankai Trough. [20] We therefore examined other findings supporting our hypothesis of an extended source of the Hoei earthquake. Oct 28, 1707. [38] At 29 min from the time the earthquake started and about 10 min after the beginning of the lake inundation, flow into the lake almost stops (Figure 11d; T = 29 min). However, another source model for this event based on strong ground motion and teleseismic waveform data shows a large fault slip only in the eastern part (N3) of the Nankai earthquake fault segment [Murotani, 2007]. The 2011 Tohoku-oki tsunami — Three years on. of Deaths, as follows: Such ground deformations caused by the rupture of the N1 to N4 segments is consistent with the observed ground deformation pattern of the Hoei earthquake compiled by Kawasumi [1950], which includes large vertical upheavals of 2 to 2.5 m at Cape Muroto, 1 m at Omaezaki, and subsidence of 2 m at Kochi. Other source parameters, including strike, dip, rake and slip were assumed to be the same as for the N4 subfault segment (Table 2). A number of tsunami trains are captured within Tosa Bay (Figure 4f). The geometry and source parameters of each segment are shown in Table 1. Tsunamis therefore occur comparatively often in this country. The 1605 Nankai earthquake occurred at about 20:00 local time on 3 February. Also, sporadic areas of large (>2 mm/yr) ground subsidence appear on land along the shoreline of the Pacific coast such as at Cape Ashizuri, Cape Muroto, Cape Shiono, and Omaezaki. [25] We first set a 70 km by 120 km subfault segment, N5, on the west of the N4 subfault segment and extended the source rupture area of the Hoei earthquake to Hyuga‐nada (Figure 7). Also shown are the distributions of maximum tsunami inundation height derived from the simulation of the new Hoei earthquake source model (red lines) and the former Hoei earthquake model (black lines). Okamura et al. The speed of the seawater at each point is illustrated by red arrows superimposed on the snapshots. Numerical simulation of the tsunami using a new source rupture model for the Hoei earthquake explains the distribution of the very high tsunami observed along the Pacific coast from western Shikoku to Kyushu more consistently. Moreover the simulated uplift of 100 cm at Cape Ashizuri is far larger than the uplift observed by Kawasumi [1950]. [32] The maximum tsunami height along the coast near Ryujin Lake as calculated by the present simulation is 6 m, while it is a maximum of 2 m for the former Hoei earthquake source model without the N5′ subfault segment (Figure 9). [47] In the Hyuga‐nada region a relatively large (M6.5–7.5) interplate earthquakes have occurred frequently at interval approximately 20–30 years. (a) New Hoei earthquake model with fault segments N1 to N5′ and (b) former Hoei model [after, Maximum tsunami height along the Pacific coast of Japan. An observation of repeatable slow slip events associated with deep tremor activity around the Bungo Channel noted by Hirose and Obara [2005] may mean that accumulation of strain energy above the plate boundary is not as strong as would be expected based only on the large plate coupling rate deduced from the GEONET data analysis. It was the largest earthquake in Japanese history. Overall there were 1,250 fatalities, 2,970 injured, and 16,455 houses totally collapsed. A long source area of the 1906 Colombia–Ecuador earthquake estimated from observed tsunami waveforms. As the height of the sea surface increases with passing time, the width of the channel grows very dramatically (Figures 11c and 11d; T = 24 and 29 min). There are many old monuments of the Nankaido tsunamis of Hoei (Oct. 28, 1707) and the 2nd Ansei (Dec. 24, 1854) along the Osaka and Wakayama coasts, Western Japan. The first recorded tsunami in Japan, it hit on November 29, 684 on the shore of the Kii Peninsula, Nankaido, Shikoku, Kii, and Awaji region. The spread of the source area of the 1944 Tonankai earthquake was rather short and stopped before the Tokai earthquake fault segment. Related to Geologic Time, Mineralogy The tsunami lakes distributed along the Nankai Trough shoreline lie along a larger zone that subsides during the Nankai Trough earthquakes have developed and preserved in such way. Comm. These physical constants are assumed from the geology and sedimentation properties of the Ryujin Lake demonstrated by Okamura et al. A set of tsunami trains with large water fluxes might transport sea sand into the lake very effectively and the relatively slow return current from the lake would leave those sea deposits in the lake. The death toll associated with this event is uncertain, … It should also be noted that such tsunami‐induced onshore deposits have not accrued regularly in Ryujin Lake due to the Nankai earthquakes that occur every 100 to 150 years, but were only deposited in the 1707 Hoei earthquake, the 1361 Shohei earthquake, and the 684 Tenmu earthquake, which are probably associated with larger tsunamis than the other Nankai earthquakes [Matsuoka and Okamura, 2009; Okamura et al., 2004]. We designated these segments as N4′ and N5′ (Table 2 and Figure 7b). Dans chacun de ces cas, c'est le bloc nord-est qui a rompu avant le bloc sud-ouest[9]. The resultant large Shields number, (s > 11), associated with the tsunami's inflow 25 min from the start of the earthquake (Figure 11c), promises that tsunami could efficiently transport sea sand into the lake with very large Shields number of tsunami due to the rupture on the N5′ subfault [see, e.g., Takahashi et al., 1993]. Such a slow inflow speed (<1 m/s) and the resultant small Shields number (s < 1) indicate that such a tsunami could not transport sea sand into the lake as compare with large Shields number (s > 11) of former simulation with the N5′ subfault segment. A magnitude 8.4 earthquake caused sea waves as high as 25 m to hammer into the Pacific coasts of Kyushyu, Shikoku and Honshin. Tokaido-Nankaido, Japan Estimated Number of Deaths: 30,000 Year: 1707. Nankaido japan 28 october 1707 a magnitude 84. These studies endeavor to clarify the tsunami history of the historical and prehistorical Nankai Trough earthquakes [e.g., Tsukuda et al., 1999; Okamura et al., 1997, 2000, 2003, 2004; Tsuji et al., 1998, 2002; Nanayama and Shigeno, 2004; Komatsubara and Fujiwara, 2007; Matsuoka and Okamura, 2009]. Thus, the effect of adding the N5′ subfault is only a very minor amplification of the tsunami along the coast from east of Shikoku to Honshu, confirmed by comparing snapshots of Figures 8a and 8b in later time frames (T = 15 and 30 min). Pages 173 This preview shows page 149 - 152 out of 173 pages. Since more than 60 years have been passed since the former earthquake cycle we expect that next earthquake sequence might occur along the Nankai Trough in the next 30 years. Nankai, Japan: 1707 Hōei earthquake: Earthquake: On 28 October 1707, during the Hōei era, a magnitude 8.4 earthquake and tsunami up to 10 meters (33 feet) in height struck Tosa Province (Kōchi Prefecture). [44] However, the recent discovery of the tsunami lakes in Kyushu (Ryujin Lake) with their thick cover of tsunami‐induced deposits caused by the Hoei earthquake has overturned our understanding. Maximum tsunami height along the Pacific coast of Japan. Small Bodies, Solar Systems Steadily improving high‐performance computing technologies together with high‐resolution earthquake model will enable us for simulating strong ground motion near future. Structural control on the nucleation of megathrust earthquakes in the Nankai subduction zone. YouTube, n.d. A total of nearly 30,000 buildings were damaged in the affected regions and about 30,000 people were killed due to this disaster. A systematic review of geological evidence for Holocene earthquakes and tsunamis along the Nankai-Suruga Trough, Japan. Géolocalisation sur la carte : Japon. [42] The results of tsunami inundation simulation indicate that tsunami‐related deposits observed in Ryujin Lake do not occur regularly during Nankai Trough earthquakes but occur during unusually large earthquakes when the fault rupture extends beyond westernmost Shikoku to Hyuga‐nada. An'naka et al. It was 300 years ago, but it was one of the tragedies caused by the tsunami in Japan. Propagation of tsunami from Kii Peninsula to Kyushu for former source model with N1 to N4 subfault segments. [12] The source model of the Hoei earthquake deduced by An'naka et al. And crustal deformation Nankai region afternoon when an 8.4 magnitude earthquake sent sea waves as high as 25 m hammer... 20:00 local time on 3 February condition for linear long-wave and linear dispersive-wave tsunami simulations observed! Tsunami since 684 a total of 141 tidal waves classified as a dozen occurred over a one period! 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