Yonaguni Knoll IV

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Coordinates: 24°54′N 122°48′E / 24.900°N 122.800°E / 24.900; 122.800[1]
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Yonaguni Knoll IV
Yonaguni Knoll IV is located in Ryukyu Islands
Yonaguni Knoll IV
Location in Okinawa Trough
Summit depth745 metres (2,444 ft)
Location
LocationOkinawa Trough, east of Taiwan
Coordinates24°54′N 122°48′E / 24.900°N 122.800°E / 24.900; 122.800[1]

Yonaguni Knoll IV is a seamount in the Okinawa Trough, east of Taiwan. It lies at about 745 metres (2,444 ft) depth and formed through Quaternary volcanism that yielded dacitic and rhyolitic magmas. The seamount is hydrothermally active, with numerous sites that are colonized by mussels and other marine animals. A submarine underground "lake" of liquid carbon dioxide has been identified at Yonaguni Knoll IV.

Geology and geomorphology

Yonaguni Knoll IV (also known as Daiyon-Yonaguni

hydrothermal systems are known from the trough, where conditions are favourable for hydrothermal activity[7] and which began to open in the Miocene.[8]

The seamount reaches a minimum depth of about 745 metres (2,444 ft).

barite, montmorillonite, quartz and sulfur.[8] A flat,[8] north-northwest-south-southeast trending,[10] 1 kilometre (0.62 mi) long and 500 metres (1,600 ft) wide valley lies southwest of Yonaguni Knoll IV and is covered by mud,[13] except near the vents and the breccia-covered northern slope. [14] It tilts to the southeast, [15] and may represent a geological fault[10] at about 1,400 metres (4,600 ft) depth.[9]

Yonaguni Knoll IV lies at the southwestern end[12] of a northeast–southwest trending chain of volcanic seamounts in the southern Okinawa Trough,[13] and may be a product of the subduction of the Gagua submarine ridge, which commenced in the early Pleistocene[16] and generated a slab window under the Okinawa Trough. There are more than 70 volcanoes in this chain.[10] These volcanoes were active during the Quaternary and erupted dacites and rhyolites. The magma formed through the fractional crystallization mixing of basalt from the mantle and felsic magmas from the crust.[6]

Hydrothermal venting

The area of Yonaguni Knoll IV first drew attention in 1996 during a joint French-Taiwanese expedition on the R/V L'Atalante.[17] Hydrothermal venting at the knoll was discovered in 2000 by the DSV Shinkai 6500 submersible, and the venting of liquid CO
2 by the same submersible three years later. Liquid CO
2 was observed venting from the JADE hydrothermal site also in the Okinawa Trough in 1989.[18]

Multiple separate hydrothermal vent sites occur in the valley southwest of Yonaguni Knoll IV;

white smokers.[21] Radiometric dating of some vents has indicated ages of a couple of centuries, with one approaching 1000 years.[22]

Liquid carbon dioxide

The liquid CO
2 is vented from areas between the Tiger and Swallow vents and at the Crystal site.[23] Liquid CO
2 appears to pool beneath the seafloor[21] and a "lake" of liquid CO
2 has been found, buried beneath 20–40 centimetres (8–16 in) thick sediment, 50 metres (160 ft) south of the hydrothermal vents. Given that at such depths CO
2 is less dense than water, it may be trapped under a layer of CO
2 hydrate beneath the sediment layers.[24]

Origin of the hydrothermal fluids

An intense hydrothermal system must exist there to power the various seafloor surface manifestations.

megawatt.[26]

The liquid CO
2 ultimately derives from the hydrothermal fluids but accumulates there before giving rise to the CO
2 hydrate that eventually produces the liquid droplets, and the hydrothermal fluids vented are not the same as these that give rise to the CO
2. The hydrothermal fluids are partitioned underground into separate brine-rich, vapour-rich and residual fluids[27] which rise to the surface and give rise to numerous separate vents.[11] Hydrothermal plumes rise from above the vent sites[26] and the seawater above Yonaguni has unusually high methane concentrations.[28]

Hydrothermal deposits

Red and yellow

black smokers.[30] Numerous minerals of elements such as arsenic, barium, copper, iron,[31] lead, manganese and zinc[32][a] form five different assemblages of mineralization.[7] The assemblages appear to correlate with modes of sulfide/sulfate mineralization.[33] Inversely, silicate and carbonate weathering occurs on pre-existent rocks.[9] The age of the vent deposits reaches 11,000 years.[34]

Life

Hydrothermal communities occur at Yonaguni Knoll IV, with dense assemblages of vent animals at the "Crystal" site

holothurians and starfish, with crabs and mussels found around the vents. Fish, octopuses, polychaetes in tubes, sea anemones and shrimps are also found. Fish, sea spiders, sponges and starfish settle on extinct vents.[36][c]

Hydrothermal sediments at Yonaguni Knoll IV have diverse microbial communities, with over one billion cells per 1 cm3 (0.061 cu in).

chemolithoautotrophs that feed on H
2, as the exhalations there are the most H
2 rich in the Okinawa Trough. Heterotrophic lineages have also been found.[52] Microbial communities have also been sampled from hydrothermal plumes.[53]

The emission of CO
2 is detrimental to ecosystems on Yonaguni Knoll IV, as there are fewer animals where the emissions take place and hydrates form.[54] On the other hand, a diverse microbial ecosystem has been identified from the margins of the liquid CO
2 "lake".[55]

Notes

  1. barite, bornite, calcite, chalcopyrite, covellite, galena, nukudamite, pyrite, rhodochrosite, sphalerite, stibnite, tennanite-tetrahedrite series and wurtzite.[8]
  2. ^ The shrimp Lebbeus shinkaiae was discovered at Yonaguni Knoll IV and on Hatoma Knoll, also in the Okinawa Trough.[39]
  3. Bathyacmaea secunda, Lepetodrilus nux, Margarites ryukyuensis, Peltospiridae sp., Provanna sp., Puncturella parvinobilis and Pyropelta ryukyuensis.[46][50]

References

  1. ^ a b Wu et al. 2019, p. 2.
  2. ^ Ishibashi, Okino & Sunamura 2015, p. 388.
  3. ^ a b Suzuki et al. 2008, p. 268.
  4. ^ a b Konno et al. 2006, p. 2.
  5. S2CID 208083816
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  6. ^ a b Chen et al. 2020, p. 4280.
  7. ^
    ISSN 0169-1368
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  8. ^ a b c d Gena et al. 2013, p. 361.
  9. ^ a b c d Kedzior et al. 2016, p. 6621.
  10. ^ a b c d Chen et al. 2020, p. 4281.
  11. ^ a b Nunoura et al. 2010, p. 1199.
  12. ^ a b c Wu et al. 2019, p. 8.
  13. ^ a b c d e Suzuki et al. 2008, p. 269.
  14. ^ Ishibashi, Okino & Sunamura 2015, p. 341.
  15. ^ Rehder & von Deimling 2008, p. 31.
  16. ^ Wu et al. 2019, p. 1.
  17. ^ Rehder & von Deimling 2008, p. 6.
  18. ^ Konno et al. 2006, p. 1.
  19. ^ Gena et al. 2013, p. 362.
  20. ^ Nunoura & Takai 2009, p. 355.
  21. ^ a b Nunoura & Takai 2009, p. 352.
  22. ^ Ishibashi, Okino & Sunamura 2015, p. 380.
  23. ^ Suzuki et al. 2008, p. 270.
  24. ^ Inagaki et al. 2006, p. 14165.
  25. ^ Chen et al. 2020, p. 4296.
  26. ^
    Bibcode:2011AGUFMOS21B..07B
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  27. ^ Konno et al. 2006, pp. 4–5.
  28. S2CID 202641187
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  29. ^ Suzuki et al. 2008, p. 271.
  30. ^ Suzuki et al. 2008, p. 273.
  31. ^ Suzuki et al. 2008, p. 278.
  32. ^ Suzuki et al. 2008, pp. 276–277.
  33. ^ a b Ishibashi, Okino & Sunamura 2015, p. 342.
  34. ^ Ishibashi, Okino & Sunamura 2015, p. 53.
  35. ^ Ishibashi, Okino & Sunamura 2015, p. 430.
  36. ^ Rehder & von Deimling 2008, p. 60.
  37. PMID 27470798
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  38. ^ Ishibashi, Okino & Sunamura 2015, p. 452.
  39. doi:10.11646/zootaxa.3241.1.2
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  40. ^ Ishibashi, Okino & Sunamura 2015, pp. 452–453.
  41. S2CID 84024667
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  42. PMID 18319477
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  44. PMID 17329770
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  45. PMID 23847597
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  46. ^ a b Ishibashi, Okino & Sunamura 2015, p. 451.
  47. doi:10.5179/benthos.58.84
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  48. ^ Ishibashi, Okino & Sunamura 2015, p. 453.
  49. doi:10.26107/RBZ-2020-0017
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  50. ISSN 0171-8630
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  51. doi:10.2343/geochemj.2.0357
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  52. ^ Nunoura et al. 2010, p. 1208.
  53. ^ Ishibashi, Okino & Sunamura 2015, p. 33.
  54. ISSN 1750-5836
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  55. ^ Inagaki et al. 2006, p. 14168.

Sources

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