[5] The source rupture histories of the recent 1944 Tonankai and 1946 Nankai earthquakes were examined extensively based on the analysis of modern instrumental data, such as tide gauge records of tsunami waveforms [Aida, 1981; Tanioka, 2001; Tanioka and Satake, 2001; Baba et al., 2002, 2006], seismograms of regional strong ground motions and teleseismic waveforms [Ichinose et al., 2003; Murotani, 2007; Yamanaka, 2004], geodetic data derived from leveling surveys [Fitch and Scholz, 1971; Kanamori, 1972; Ando, 1975; Ishibashi, 1981; Sagiya and Thatcher, 1999], and combinations of these data [Satake, 1993]. 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. The 11 March 2011 Tohoku Tsunami Survey in Rikuzentakata and Comparison with Historical Events. 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. Slip parameters on major thrusts at a convergent plate boundary: regional heterogeneity of potential slip distance at the shallow portion of the subducting plate. The map on the top shows the Pacific coastline from Hyuga‐nada to Suruga Bay with representative locations. This pattern of vertical ground movement is considered to illustrate the process of recovery of ground surface deformation due to the Nankai Trough earthquakes. [28] We then conducted a tsunami simulation for the earthquake using the revised source model of the Hoei earthquake (Figure 7b) to see the contribution of the N5′ subfault segment in increasing simulated tsunami height along the coast from Shikoku to Kyushu and in producing tsunami inundation of Ryujin Lake. Structural control on the nucleation of megathrust earthquakes in the Nankai subduction zone. 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. Comparison of tsunami inundation of Ryujin Lake for the new Hoei earthquake model (solid lines) and former earthquake model (dashed lines). 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. A high‐density digital elevation map was constructed on a basis of recent geographical surveys conducted by the Yonouzu Promotion Office, Oita Prefecture. Web. 23 Feb. 2015. [50] Baba et al. The bottom four plots show the distribution of maximum tsunami height calculated using the simulation of the Hoei earthquake by, Pattern of average vertical movements of uplift (red) and subsidence (blue) derived using the GEONET GPS data from August 1999 to August 2009 are illustrated by blue‐red color scale. This agrees with the heights of tsunamis observed along the Pacific coast from Cape Ashizuri to Hyuga‐nada during the Hoei earthquake [Hatori, 1974, 1985; Murakami et al., 1996] very consistently. [2006] revealed from tsunami data that the area of large tsunami generation on the fault plane extended along the entire source rupture area in of the 1946 Nankai earthquake. The 2011 Tohoku-oki tsunami — Three years on. 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. The Hoei earthquake was a larger event in which rupture spread as far as Hyuga‐nada, incorporating the fifth subfault, N5. Of the series Nankai Trough M8 earthquakes that recur approximately every 100 to 150 years, the Hoei earthquake is considered to be the largest shock. The linkage process between different subfaults in Nankai Trough earthquakes may contribute significantly to the severity of the disaster, especially the tsunamis. Le séisme de 1707 a ainsi pu être à l'origine d'un changement de pression dans la chambre magmatique sous le mont Fuji, qui est entré en éruption le 16 décembre 1707, soit 49 jours après le séisme[16]. [30] In a later snapshot the larger tsunami is radiating into the Bungo Channel and propagating into the Inland Sea of Japan (Figure 8a; T = 30 min), which enhances the height of the tsunami in the Inland Sea. 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]. Journal of Geomagnetism and Aeronomy, Nonlinear The modeled height is much larger than the maximum height of the tsunamis associated with the 1856 Ansei Nankai and 1946 Nankai earthquakes, which were less than 4 m at Yonouzu [Chida et al., 2003; Chida and Nakayama, 2006]. Machine Learning Algorithms for Real-time Tsunami Inundation Forecasting: A Case Study in Nankai Region. [2003] modified the source model of Aida [1981] and improved the agreement between tsunami simulations and observed tsunami height distributions. Any queries (other than missing content) should be directed to the corresponding author for the article. Le bilan total s'élève à plus de 29 000 bâtiments détruits et plus de 5 000 victimes. The earthquake occurrence pattern can be characterized by three fault segments: the Nankai, the Tonankai, and the Tokai, from west to east. Most of these monuments were built just after the earthquakes to pray for the repose of the tsunami victims or to sound a warning to inhabitants. The bathymetric model of each resolution was provided by the Central Disaster Mitigation Council, Cabinet Office, Government of Japan. The map shows the Pacific coastline of Kyushu and Shikoku with representative locations (squares). [23] We also consulted recent studies on the spatial distribution of interplate coupling rates along the Nankai Trough [e.g., Hashimoto et al., 2009; Ichitani et al., 2010; Nishimura et al., 1999; T. Hashimoto, http://www.jamstec.go.jp/esc/projects/fy2009/12-hashi.html]. [49] The Hoei earthquake, extending as it did from Suruga Bay to Hyuga‐nada, approximately 700 km, broke five fault segments (N1–N5′), each with a different geometry. The Nankai Trough extends from Suruga Bay to the Hyuga‐nada. It was a hot afternoon when an 8.4 magnitude earthquake sent sea waves at a height of 25 meters to hammer parts of Japan. Estimated Number of Deaths: 36,000 Year: 1883. The speed of the seawater at each point is illustrated by red arrows superimposed on the snapshots. (d) An index map illustrating major place names. 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. Please note: The publisher is not responsible for the content or functionality of any supporting information supplied by the authors. Osaka was also damaged. Also we slightly modified the length of the N4 subfault segment in the direction parallel to the trench axis in order to improve the fitness between synthesized and observed ground deformation pattern reported by Kawasumi [1950]. [2009] based on the inversion of horizontal and vertical ground movement data from the GEONET. We used a nested mesh model that connects gradually 30 m, 90 m, and 270 m mesh model to allow efficient simulation of the tsunami in heterogeneous bathymetry (Figure 3). Geophysics, Geomagnetism The fault rupture area of the Hoei earthquake has been thought to spread from Suruga Bay to the westernmost end of Shikoku, i.e., the whole extent of the 1854 Ansei Tokai and the 1854 Ansei Nankai earthquake source segments. The sea waves were as high as 25 m to hammer into the Pacific coasts of Kyushyu, Shikoku and Honshin. We thank the Central Disaster Mitigation Council, Cabinet Office, government of Japan, and Yonouzu Promotion Office, Oita Prefecture, Japan, for providing bathymetry map data. Development and Assessment of Real-Time Fault Model Estimation Routines in the GEONET Real-Time Processing System. The tsunami radiates very strongly in the direction perpendicular to the Nankai Trough trench axis (Figure 8a; T = 5 min). The MW 9.0 Tohoku Earthquake, Japan, March 11, 2011. Before starting the simulation, we subsided the altitude of the simulation model at −60 cm in consideration of the results of the ground deformation simulation shown in Figure 7b. Propagation of tsunami from Kii Peninsula to Kyushu for former source model with N1 to N4 subfault segments. Its total length is approximately 800 km. The death toll associated with this event is uncertain, but between 5,000 and 41,000 casualties were reported. Difference between Tidal Wave and Tsunami (CSS-2018) Geology and Geophysics, Physical These physical constants are assumed from the geology and sedimentation properties of the Ryujin Lake demonstrated by Okamura et al. Learn about our remote access options, Center for Integrated Disaster Information Research, Interfaculty Initiative in Information Studies, University of Tokyo, Tokyo, Japan, Earthquake Research Institute, University of Tokyo, Tokyo, Japan. Surface displacement for the 1707 Hoei earthquake calculated using the source model of, The area of tsunami simulation and mesh configuration connecting gradually from coarser 270 m (R1) to finer 90 m (R2) and 30 m (R3) mesh models. However, the height of the simulated tsunami from western Shikoku to Hyuga‐nada in Kyushu is less than half of the actual height observed. Ryujin Lake is now locating over an area of large (150 cm) ground subsidence. and you may need to create a new Wiley Online Library account. From historical records, tsunami heights of 9 m at Tosa Shimizu and Ashizuri Cape and more than 4 m along the coast from Ashizuri Cape to Hyuga‐nada are known to have occurred (shown as circles in Figure 5 [Murakami et al., 1996]). It is thought that ground surface subsidence due to the earthquakes results in particularly deep tsunami inundation on land, which transports sea sand into onshore lakes very effectively. 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). However, the level of ground subsidence in the area around Ryujin Lake derived by the new model is several times larger than we expected (60 cm). 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. Nankaido, Japan - 28 October 1707. However, further studies evaluating shaking intensity such as, e.g., based on the FDM simulation of ground motion is needed to completely understand earthquake‐related disasters associated with the Nankai Trough earthquakes. 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. 2nd ser.). 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