Daiichi-Kashima Seamount

Daiichi-Kashima Seamount is a guyot in the Pacific Ocean off Japan. It is about 3.5 kilometres (2.2 mi) high and reaches a depth of 3,540 metres (11,610 ft). Daiichi-Kashima formed during the Barremian as a result of volcanic activity; during the Albian reefs formed on the seamount and generated a limestone cap. The seamount later.

Daiichi-Kashima
Daiichi-Kashima
Daiichi-Kashima (Oceania)
Location offshore Japan
Location
LocationWestern Pacific Ocean
Coordinates34.2°N 144.3°E / 34.2; 144.3
CountryJapan

The seamount has been approaching the Japan Trench and a noticeable vertical offset of about 1.5 kilometres (0.93 mi) between the eastern and western halves of Daiichi-Kashima appears to be the result of normal faulting as the seamount enters the trench, with the western half dropping down; it may also reflect a past sector collapse when the volcano was still active.

Geography and geology

Regional

The Daiichi-Kashima seamount lies 150 kilometres (93 mi) east of Cape Inubō[1] and Chōshi[2] off the eastern coast of Honshu, Japan.[3] Other seamounts in the area are Katori Seamount northeast of Daiichi-Kashima and Daini-Kashima Seamount east of Katori Seamount[4] and the Kashima Fracture Zone ends southeast of the seamount.[5]

Local

Daiichi-Kashima is a 3.5 kilometres (2.2 mi) high and 50 kilometres (31 mi) wide[6] guyot[7] and rises to a depth of 3,540 metres (11,610 ft).[8] On the eastern part of the volcano lies an at least 0.6 kilometres (0.37 mi) thick platform of clay and reef limestone[6] with traces of past barrier reefs at its margins.[9] The summit platform of Daiichi-Kashima covers an area of 83 square kilometres (32 sq mi).[10]

It is cut by several normal faults that run approximately parallel to the trench and have an offset of about 1.5 kilometres (0.93 mi) in the central sector of the volcano; the carbonate platform is also offset in such a manner[6] by a normal fault represented by a[11] scarp into a lower western and a higher eastern part.[1] This fault, which appears to be split in two or three subsidiary faults separated by grabens,[12] extends past the Daiichi-Kashima seamount[11] and covers a length of 100 kilometres (62 mi); evidently Daiichi-Kashima has been split in half by the fault, which is much younger than the ocean floor[13] and moved at a rate of 1.2 centimetres per year (0.47 in/year)[14] but does not appear to be presently active in light of the sediment cover on the scarp.[15] Aside from a normal motion, the western half of the seamount has also been moved away from the eastern half and is tilted west.[9]

The seamount appears to be part of a seamount chain called Joban Seamount Chain[16] or Kashima-Ryofu No.1 that formed during the Cretaceous in the Equatorial Pacific[17] and about 30° south of their present-day position.[18] Based on isotope ratios it was once inferred that Daiichi-Kashima consists of two separate volcanoes[19][20] but a later theory indicates that these are two separate stages of the same volcano.[21]

Relation to the Japan Trench

Daiichi-Kashima lies south of the Japan Trench on a seafloor of Valanginian age,[6] very close to the trench.[4] The Pacific Plate is subducting beneath Japan at a rate of 9 centimetres per year (3.5 in/year)[6] and close to the Daiichi-Kashima Seamount lies the Boso Triple Junction between the Japan Trench, the Sagami Trench and the Izu-Bonin Trench.[22] The subduction process may cause the downgoing oceanic plate to buckle and form normal faults that run parallel to the trench.[4]

Since about 100,000 years, the western half of Daiichi-Kashima is being subducted in the Japan Trench[13] and about one third[23] to one quarter of the seamount has been subducted already.[6] Part of the landward margin of the trench close to Daiichi-Kashima is uplifted, perhaps as a consequence of the subduction of the seamount,[4] and there is periodic earthquake activity in front of Daiichi-Kashima seamount with magnitude 7 earthquakes about every 20 years.[24] The seamount might also influence the segmentation of the trench and its earthquakes, considering that the rupture of the 2011 Tohoku earthquake spanned the trench length between Erimo Seamount and Daiichi-Kashima.[25] The other seamounts in the area will likely be subducted after Daiichi-Kashima has been.[26]

Composition

Volcanic rocks from Daiichi-Kashima include basanite, benmoreite and mugearite. There is a distinction between the eastern and western sectors of the volcano, with the western one consisting mainly of mugearite.[20] Phenocrysts identified in sampled rocks include aegirine-augite, alkali feldspar, amphibole, chromium spinel, clinopyroxene, magnetite, olivine and plagioclase.[27]

Dredging has found limestones on Daiichi-Kashima[28] which have been subdivided into an upper and a lower formation.[29] Especially on its western part ferromanganese crusts and phosphorites have been encountered as well.[28] Other rocks are rudistid-coral floatstones, oolithic grainstones[15] and peloidal wackestones containing algal pisolites[30] and other algal remnants. Other fossils include bivalves, corals, echinoids, foraminifers and stromatoporoidea.[31][29] The rudist Praecaprotina kashimae is named after the seamount.[32]

Geological history

The volcano is of Barremian age, the limestones are of Aptian to Albian age.[6] Magnetic traits in the seamount suggest that it formed 140 - 120 million years ago close to a spreading center, which is older than the age of 100 million years inferred from fossils[33] but comparable to ages inferred from radiometric dating.[34] Radiometric dating has yielded ages of 120.4 ± 2.7 million years ago for the eastern and of 117.8 ± 8.4 million years ago for the western side of the seamount.[10] The seamount is thus considered to be 120 - 100 million years old, while the underlying crust is about 20 million years older.[20] At the time of its formation, Daiichi-Kashima was located between 7.6° northern and 1° southern latitude, with one proposed coordinate being 1°S 165°W.[35]

One proposal envisages that volcanism took place in two separate stages, between which the western flank of the volcano underwent a large-scale collapse. In the first stage, basalts formed a volcanic island that eventually erupted trachytes. In a second stage, the western flank of the volcano collapsed and subsequently chemically different lavas and pyroclastics were emplaced, covering the bulk of the volcano and giving it a paired appearance similar to Reunion.[21]

During the Albian erosion and subsidence levelled the volcano, forming a flat surface. A carbonate platform developed on this surface first with fringing reefs and then with barrier reefs.[21] The carbonate platform continued to be active for 10 million years.[36] A research group of the Tokai University after studying dredged samples proposed that the limestones west and east of the central scarp are of different ages and developed at different sea levels: The western part would be of Barremian age and the eastern one of Albian age. This would explain why they lie at distinct depths.[37]

After its drowning, Daiichi-Kashima continued to subside until it arrived at the Japan Trench[36] between 250,000 and 150,000 years ago.[24] The buckling of the ocean crust as it approached the trench induced faulting across Daiichi-Kashima and eventually another collapse of the western flank took place.[38]

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References
  1. Kobayashi et al. 1987, p. 257.
  2. Oikawa et al. 2009, p. e5.
  3. Tani 1989, p. 32.
  4. Kobayashi et al. 1987, p. 258.
  5. Ferrand, Thomas P.; Kita, Saeko (19 November 2018). "Physical mechanisms of oceanic mantle earthquakes: Comparison of natural and experimental events". Scientific Reports. 8 (1): 2. doi:10.1038/s41598-018-35290-x. ISSN 2045-2322. PMC 6242829. PMID 30451925.
  6. Dominguez et al. 1995, p. 404.
  7. Tani 1989, p. 44.
  8. Dominguez et al. 1995, p. 405.
  9. Tani 1989, p. 45.
  10. Konishi 1989, p. 251.
  11. Kobayashi et al. 1987, p. 260.
  12. Lallemand, Culotta & Von Huene 1989, p. 237.
  13. Kobayashi et al. 1987, p. 265.
  14. Tani 1989, p. 46.
  15. Konishi 1989, p. 255.
  16. Oikawa et al. 2009, p. e6.
  17. Konishi 1989, p. 249.
  18. Masse & Shiba 2010, p. 152.
  19. Dominguez et al. 1995, pp. 404-405.
  20. Lallemand, Culotta & Von Huene 1989, p. 240.
  21. Dominguez et al. 1995, p. 407.
  22. Lallemand et al. 1986, p. 103.
  23. Lallemand et al. 1986, p. 104.
  24. Kanazawa, Toshihiko; Yamanaka, Yoshiko; Shinohara, Masanao; Yamada, Tomoaki; Mochizuki, Kimihiro (29 August 2008). "Weak Interplate Coupling by Seamounts and Repeating M ~ 7 Earthquakes". Science. 321 (5893): 1194–7. Bibcode:2008Sci...321.1194M. doi:10.1126/science.1160250. ISSN 1095-9203. PMID 18755973.
  25. Catherine, J. K.; Gahalaut, V. K.; Kundu, Bhaskar (1 March 2012). "Seamount subduction and rupture characteristics of the March 11, 2011, Tohoku earthquake". Journal of the Geological Society of India. 79 (3): 249. doi:10.1007/s12594-012-0047-6. ISSN 0974-6889.
  26. Yamazaki, Toshitsugu; Okamura, Yukinobu (March 1989). "Subducting seamounts and deformation of overriding forearc wedges around Japan". Tectonophysics. 160 (1–4): 225. Bibcode:1989Tectp.160..207Y. doi:10.1016/0040-1951(89)90392-2. ISSN 0040-1951.
  27. Takigami et al. 1989, p. 72.
  28. Konishi 1989, p. 252.
  29. Masse & Shiba 2010, p. 148.
  30. Konishi 1989, p. 253.
  31. Konishi 1989, p. 254.
  32. Masse & Shiba 2010, p. 149.
  33. Kobayashi et al. 1987, p. 264.
  34. Takigami et al. 1989, p. 79.
  35. Uchiyama, Akinori; Kubota, Ryuji (1 August 2005). "Three-dimensional magnetization vector inversion of a seamount". Earth, Planets and Space. 57 (8): 697. Bibcode:2005EP&S...57..691K. doi:10.1186/BF03351849. ISSN 1880-5981.
  36. Konishi 1989, p. 260.
  37. Kobayashi et al. 1987, p. 259.
  38. Dominguez et al. 1995, p. 408.

Sources
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