Japan Earthquake today M 5.6 - 27 km SE of Miyazaki, Japan 2022-12-17 18:06:03

 M 5.6 - 27 km SE of Miyazaki, Japan

2022-12-17 18:06:03 (UTC)31.772°N 131.647°E37.9 km profundity

Close by Spots💫

Miyazaki, Miyazaki, Japan

27 km (16.8 mi) NWPopulation: 311203

Nichinan, Miyazaki, Japan

32.7 km (20.3 mi) SWPopulation: 44243

Takanabe, Miyazaki, Japan

42.5 km (26.4 mi) NNWPopulation: 22513

Tsuma, Miyazaki, Japan

43.3 km (26.9 mi) NNWPopulation: 34318

Kushima, Miyazaki, Japan

49.8 km (30.9 mi) SWPopulation: 22102

Distance and bearing from focal point to local spot.

Structural Outline💫

Seismotectonics of the Philippine Ocean and Area

The Philippine Ocean plate is lined by the bigger Pacific and Eurasia plates and the more modest Sunda plate. The Philippine Ocean plate is uncommon in that its boundaries are essentially all zones of plate combination. The Pacific plate is subducted into the mantle, south of Japan, underneath the Izu-Bonin and Mariana island bends, which expand in excess of 3,000 km along the eastern edge of the Philippine Ocean plate. This subduction zone is portrayed by fast plate assembly and undeniable level seismicity stretching out to profundities of north of 600 km. Despite this broad zone of plate combination, the plate interface has been related with not many incredible (M>8.0) 'megathrust' seismic tremors. This low seismic energy discharge is remembered to result from frail coupling along the plate interface (Scholz and Campos, 1995). These merged plate edges are additionally connected with surprising zones of back-curve expansion (alongside coming about seismic movement) that decouple the volcanic island bends from the rest of the Philippine Ocean Plate (Karig et al., 1978; Klaus et al., 1992).

South of the Mariana curve, the Pacific plate is subducted underneath the Gab Islands along the Gab channel. The long zone of Pacific plate subduction at the eastern edge of the Philippine Ocean Plate is answerable for the age of the profound Izu-Bonin, Mariana, and Gab channels as well as equal chains of islands and volcanoes, run of the mill of circum-pacific island bends. Essentially, the northwestern edge of the Philippine Ocean plate is subducting underneath the Eurasia plate along a concurrent zone, stretching out from southern Honshu toward the northeastern bank of Taiwan, appeared by the Ryukyu Islands and the Nansei-Shoto (Ryukyu) channel. The Ryukyu Subduction Zone is related with a comparative zone of back-bend expansion, the Okinawa Box. At Taiwan, the plate limit is described by a zone of curve landmass impact, by which the northern finish of the Luzon island circular segment is slamming into the light outside of the Eurasia mainland edge seaward China.

Along its western edge, the Philippine Ocean plate is related with a zone of sideways union with the Sunda Plate. This exceptionally dynamic united plate limit reaches out along the two sides the Philippine Islands, from Luzon in the north to the Celebes Islands in the south. The structural setting of the Philippines is uncommon in a few regards: it is portrayed by inverse confronting subduction frameworks on its east and west sides; the archipelago is cut by a significant change shortcoming, the Philippine Issue; and the circular segment complex itself is set apart by dynamic volcanism, blaming, and high seismic movement. Subduction of the Philippine Ocean Plate happens at the eastern edge of the archipelago along the Philippine Channel and its northern expansion, the East Luzon Box. The East Luzon Box is believed to be an uncommon illustration of a subduction zone during the time spent development, as the Philippine Channel framework slowly expands toward the north (Cheeseburger et al., 1983). On the west side of Luzon, the Sunda Plate subducts toward the east along a progression of channels, incorporating the Manila Channel in the north, the more modest less advanced Negros Channel in the focal Philippines, and the Sulu and Cotabato channels in the south (Cardwell et al., 1980). At its northern and southern terminations, subduction at the Manila Channel is intruded on by circular segment landmass impact, between the northern Philippine curve and the Eurasian mainland edge at Taiwan and between the Sulu-Borneo Block and Luzon at the island of Mindoro. The Philippine shortcoming, which reaches out more than 1,200 km inside the Philippine circular segment, is seismically dynamic. The issue has been related with major authentic tremors, including the disastrous M7.6 Luzon quake of 1990 (Yoshida and Abe, 1992). Various other dynamic intra-circular segment issue frameworks are related with high seismic movement, including the Cotabato Shortcoming and the Verde Entry Sibuyan Ocean Shortcoming (Galgana et al., 2007).

Relative plate movement vectors close to the Philippines (around 80 mm/yr) is diagonal to the plate limit along the two plate edges of focal Luzon, where it is parceled into symmetrical plate combination along the channels and almost unadulterated translational movement along the Philippine Shortcoming (Hindrance et al., 1991). Profiles B and C uncover proof of restricting slanted seismic zones at halfway profundities (approximately 70-300 km) and complex tectonics at the surface along the Philippine Shortcoming.

A few important structural components, plate limits and dynamic volcanoes, give a setting to the seismicity introduced on the principal map. The plate limits are most exact along the hub of the channels and more diffuse or speculative in the South China Ocean and Lesser Sunda Islands. The dynamic volcanic bends (Siebert and Simkin, 2002) follow the Izu, Spring of gushing lava, Mariana, and Ryukyu island chains and the super Philippine islands lined up with the Manila, Negros, Cotabato, and Philippine channels.

Seismic action along the limits of the Philippine Ocean Plate (Allen et al., 2009) has created 7 extraordinary (M>8.0) quakes and 250 enormous (M>7) occasions. Among the most damaging occasions were the 1923 Kanto, the 1948 Fukui and the 1995 Kobe (Japan) quakes (99,000, 5,100, and 6,400 losses, separately), the 1935 and the 1999 Chi (Taiwan) tremors (3,300 and 2,500 setbacks, individually), and the 1976 M7.6 Moro Inlet and 1990 M7.6 Luzon (Philippines) tremors (7,100 and 2,400 setbacks, separately). There have likewise been various wave creating occasions in the district, including the Moro Bay seismic tremor, whose torrent brought about in excess of 5000 passings.