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389 results on '"Iio, Yoshihisa"'

21. The 2018 Hokkaido Eastern Iburi earthquake (MJMA = 6.7) was triggered by a strike-slip faulting in a stepover segment: insights from the aftershock distribution and the focal mechanism solution of the main shock

Author

Katsumata, Kei, Ichiyanagi, Masayoshi, Ohzono, Mako, Aoyama, Hiroshi, Tanaka, Ryo, Takada, Masamitsu, Yamaguchi, Teruhiro, Okada, Kazumi, Takahashi, Hiroaki, Sakai, Shin’ichi, Matsumoto, Satoshi, Okada, Tomomi, Matsuzawa, Toru, Hirano, Shuichiro, Terakawa, Toshiko, Horikawa, Shinichiro, Kosuga, Masahiro, Katao, Hiroshi, Iio, Yoshihisa, Nagaoka, Airi, Tsumura, Noriko, Ueno, Tomotake, and the Group for the Aftershock Observations of the 2018 Hokkaido Eastern Iburi Earthquake

Published
2019
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Author

IIO, Yoshihisa and IIO, Yoshihisa

Abstract

On the occasion of my retirement, I summarized the main seismic observations I have been involved in. I started with the observation of micro-fractures in mines and progressed to the observation of very small earthquakes. Advances in electronic technology, especially the practical use of GPS satellites, made it possible to carry out long-term observations in mountainous areas without a power source, which had previously been impossible. In the Western Nagano Prefecture region, high-frequency seismic observations with 10 kHz sampling and trigger method were started in 1995 and continued until my retirement. From around 2008, a device named the “Manten System” was developed in collaboration with a group of small and medium-sized enterprises in the Kansai region. The Manten system can continuously record 250 Hz sampling for more than half a year using about 32 single dry cell batteries. They were deployed in western Nagano Prefecture, the central and northern Kinki region, the San-in earthquake zone and the northern part of the South Island of New Zealand, in collaboration with related research institutions. Some unexpected and remarkable earthquakes, such as the 2017 Kaikoura, New Zealand earthquake (Mw7.8), occurred in all of the above observation networks, and these observations provided important data on the process by which intraplate earthquakes are generated.

Published
2023

29. Spatial change in differential stress magnitudes around the source fault before intraplate earthquakes

Author

Iio, Yoshihisa, primary, Matsumoto, Satoshi, additional, Yamashita, Yusuke, additional, Sakai, Shin'ichi, additional, Tomisaka, Kazuhide, additional, Sawada, Masayo, additional, Iidaka, Takashi, additional, Iwasaki, Takaya, additional, Kamizono, Megumi, additional, Katao, Hiroshi, additional, Kato, Aitaro, additional, Kurashimo, Eiji, additional, Teguri, Yoshiko, additional, Tsuda, Hiroo, additional, and Ueno, Takashi, additional

Published
2022
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34. Fracturing and pore-fluid distribution in the Marlborough region, New Zealand from body-wave tomography: Implications for regional understanding of the Kaikōura area

Author

Heath, Benjamin A., primary, Eberhart-Phillips, Donna, additional, Lanza, Federica, additional, Thurber, Clifford, additional, Savage, Martha K., additional, Okada, Tomomi, additional, Matsumoto, Satoshi, additional, Iio, Yoshihisa, additional, and Bannister, Stephen, additional

Published
2022
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36. Spatial change in differential stress magnitudes around the source fault before intraplate earthquakes.

Author

Iio, Yoshihisa, Matsumoto, Satoshi, Yamashita, Yusuke, Sakai, Shin'ichi, Tomisaka, Kazuhide, Sawada, Masayo, Iidaka, Takashi, Iwasaki, Takaya, Kamizono, Megumi, Katao, Hiroshi, Kato, Aitaro, Kurashimo, Eiji, Teguri, Yoshiko, Tsuda, Hiroo, and Ueno, Takashi

Subjects
*EARTHQUAKE aftershocks, *DEVIATORIC stress (Engineering), *EARTHQUAKES, *SEISMIC networks, *FAULT zones
Abstract

How are the sizes of the earthquakes determined? To solve this important problem, we analysed the data from a dense temporary seismic observation network installed in the aftershock area of the 2016 Mw 6.2 Central Tottori earthquake, which occurred in an intraplate region in Japan. We compared the stress field estimated from approximately 10   000 accurate focal mechanisms of aftershocks with the calculated post-earthquake stress field and found that the differential stress before the earthquake was very small near both horizontal edges. These results did not depend significantly on the modeled slip distribution and the orientation of the principal stress before the earthquake. Similar results were obtained for the 2000 Mw 6.7 Western Tottori earthquake, which also occurred in the same intraplate region in Japan. These results suggest that the fault size of large intraplate earthquakes can be determined by the region of small differential stress surrounding future earthquake faults. [ABSTRACT FROM AUTHOR]

Published
2023
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40. Additional file 1 of Ambient noise tomography for a high-resolution 3D S-wave velocity model of the Kinki Region, Southwestern Japan, using dense seismic array data

Author

Nthaba, Bokani, Ikeda, Tatsunori, Nimiya, Hiro, Tsuji, Takeshi, and Iio, Yoshihisa

Abstract

Additional file 1: Figure S1. Weakly smoothed S-wave velocity models with topography correction. This figure is relevant to Figure 7, but the smoothing parameter in velocity inversion is weaker. (a–f) S-wave velocity models overlaid with active faults (black lines). Figure S2. Strongly smoothed S-wave velocity models with topography correction. This figure is relevant to Figure 7, but the smoothing parameter in velocity inversion is stronger. (a–f) S-wave velocity models overlaid with active faults (black lines). Figure S3. Weakly smoothed S-wave velocity models without topographic correction. This figure is relevant to Figure S1. (a–f) S-wave velocity models overlaid with active faults (black lines). Figure S4. Moderately smoothed S-wave velocity models without topographic correction. This figure is relevant to Fig. 7. (a–f) S-wave velocity models overlaid with active faults (black lines). Figure S5. Strongly smoothed S-wave velocity models without topographic correction. This figure is relevant to Figure S2. (a–f) S-wave velocity models overlaid with active faults (black lines). Figure S6. S-wave velocity perturbation of the northern part of the Kinki region without topographic correction. (a) S-wave velocity perturbation at a depth of 1 km below sea level. Also shown are the locations of the Yamada Fault (YDF), Yamasaki Fault (YSF), Yagi-Yabu Fault (YGF-YBF), Mitoke Fault (MTF), Hanaore Fault (HOF) and the Biwako-seigan Fault Zone members (Chinai Fault, CF; Aibano Fault, AF; Kamidera Fault, KF; Katsuno, KtF; Hira Fault, HiF; Katata, KaF; Hiei Fault, HF; Zeze Fault, ZF). (b) S-wave velocity perturbation at a depth of 3 km below sea level. Solid black lines represent documented active faults.

Published
2022
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50. Stress relaxation arrested the mainshock rupture of the 2016 Central Tottori earthquake

Author

50159547, 80725052, 80221878, Iio, Yoshihisa, Matsumoto, Satoshi, Yamashita, Yusuke, Sakai, Shin’ichi, Tomisaka, Kazuhide, Sawada, Masayo, Iidaka, Takashi, Iwasaki, Takaya, Kamizono, Megumi, Katao, Hiroshi, Kato, Aitaro, Kurashimo, Eiji, Teguri, Yoshiko, Tsuda, Hiroo, Ueno, Takashi, 50159547, 80725052, 80221878, Iio, Yoshihisa, Matsumoto, Satoshi, Yamashita, Yusuke, Sakai, Shin’ichi, Tomisaka, Kazuhide, Sawada, Masayo, Iidaka, Takashi, Iwasaki, Takaya, Kamizono, Megumi, Katao, Hiroshi, Kato, Aitaro, Kurashimo, Eiji, Teguri, Yoshiko, Tsuda, Hiroo, and Ueno, Takashi

Abstract

After a large earthquake, many small earthquakes, called aftershocks, ensue. Additional large earthquakes typically do not occur, despite the fact that the large static stress near the edges of the fault is expected to trigger further large earthquakes at these locations. Here we analyse ~10, 000 highly accurate focal mechanism solutions of aftershocks of the 2016 Mw 6.2 Central Tottori earthquake in Japan. We determine the location of the horizontal edges of the mainshock fault relative to the aftershock hypocentres, with an accuracy of approximately 200 m. We find that aftershocks rarely occur near the horizontal edges and extensions of the fault. We propose that the mainshock rupture was arrested within areas characterised by substantial stress relaxation prior to the main earthquake. This stress relaxation along fault edges could explain why mainshocks are rarely followed by further large earthquakes.

Published
2021

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