Eifuku

Coordinates: 21°29′06″N 144°02′35″E / 21.485°N 144.043°E / 21.485; 144.043[1]
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Eifuku
Bathymetic image of NW Eifuku as viewed to the northeast
Eifuku is located in North Pacific
Eifuku
Location
Coordinates21°29′06″N 144°02′35″E / 21.485°N 144.043°E / 21.485; 144.043[1]

Eifuku (Japanese: 永福) and NW Eifuku (北西永福) are two seamounts in the Pacific Ocean. The better known one is NW Eifuku, where an unusual hydrothermal vent called "Champagne" produced droplets of liquid CO
2. Both seamounts are located in the Northern Marianas and are volcanoes, part of the Izu-Bonin-Mariana Arc. NW Eifuku rises to 1,535 metres (5,036 ft) depth below sea level and is a 9 kilometres (5.6 mi) wide volcanic cone.

Both Eifuku seamounts are hydrothermally active, with numerous vent sites found on NW Eifuku including the "Champagne" vent site, where there are a number of

white smokers. Diverse ecosystems dominated by mussels
live in proximity and around the hydrothermal vent sites.

Geography and geology

The Eifuku seamounts are located northwest of

Philippine Plate[5] that began in the Eocene. About 40 submarine and island volcanoes make up the Northern Marianas arc.[6]

NW Eifuku and Eifuku are small volcanoes at the northwestern end of a volcano chain that also includes Daikoku,[1] which is larger than NW Eifuku.[7] Daikoku also features hydrothermal venting[8] and has been considered a twin cone with Eifuku.[9] Eifuku proper is composed of boulders, dykes and lava domes.[10] The occurrence of volcanic breccia, hydrothermal muds, sandstone and sulfides has been reported but without a clear attribution to either Eifuku or NW Eifuku.[11]

NW Eifuku seamount rises to 1,535 metres (5,036 ft) depth below sea level

pillow basalts are found in the summit region.[13] The southwestern slope of NW Eifuku and its summit are cut by the scar of a sector collapse.[1] A northwest-southeast trending fracture may underlie the seamount and could be responsible for the mass wasting observed on the seamount.[14] The venting at "Champagne" appears to indicate that there is degassing magma.[3]

Composition

Rocks erupted by Eifuku range from

Silica and iron oxides form fluffy sediments.[12]

Hydrothermal vents

Chimneys and white smokers on Eifuku

Both Eifuku

white smokers[1] and hydrothermal vents dispersed over several sites on the volcano.[18] There are several sites, including diffuse venting at the summit,[19] a low-temperature area at 1,570 metres (5,150 ft) depth and high-temperature vents at 1,610 metres (5,280 ft) depth which include the so-called "Champagne" site[20] about 80 metres (260 ft) west-northwest of the summit.[7] Two other vent sites northeast and north of "Champagne" are known as "Cliff House" and "Sulfur Dendrite", respectively.[21] Additional vents are "Yellow Cone" and "Yellow Top" which are low-temperature iron-rich vents[22] and the latter of which is located south of the summit.[23] A sixth vent site is known as "Bacto Balls".[24] The seawater above NW Eifuku has anomalous composition, a sign of hydrothermal degassing.[7]

Champagne vent

Milky white bubbles rising from the ground
Carbon dioxide bubbles rising from Eifuku volcano

The "Champagne" vent was discovered either in 2004 by the

white smokers that form chimneys) and diffuse venting. Temperatures of the discharge reach 105 °C (221 °F)[2] in gas-rich fluids that contain H
2S.[18] The chimneys are formed by sulfur.[25]

"Champagne" is known for being one of only two sites on Earth[b] where liquid CO
2 is emitted. The CO
2 rises from the pumice and sulfur deposits on the ground[20] through crevices,[21] and it forms cold droplets with a milky skin[18] that stick to surfaces such as ROV tools and ascend slowly[7] owing to their buoyancy under the conditions at the vent. They appear to originate from a layer underneath the ground surface, as disturbing the vent leads to increasing exhalations.[21] The name "Champagne" is based on the appearance of the exhalations.[28]

Apart from CO
2, they contain

isotope ratios, much of this CO
2 is derived from the subduction of carbonates rather than from the mantle.[18] The emission rate may not be steady over time, as output varied between different expeditions.[14]

Biology

Mussel beds at Eifuku volcano

Several ecological communities have been found at NW Eifuku, at 1,550 metres (5,090 ft) depth[2] and with distinct microbiotas:[30]

The properties of exhaled fluids strongly influence the ecosystems surrounding hydrothermal vents,[36] and the environment of NW Eifuku has been used as an example for an ecosystem under heavy CO
2 concentrations.[37] Compared to other hydrothermal vent sites in the Pacific Ocean, mussels at NW Eifuku grow more slowly and have eroded shells, but they also are less subject to predation by crabs[38] and their body condition is not uniformly inferior.[39]

Orange coloured

sea stars and sponges occur on Eifuku seamount. The fish species Randall's snapper[13][40] and an unidentified species of the fish genus Grammatonotus were observed on Eifuku.[41]

Notes

  1. ^ Authors of a 2016 NOAA report into Eifuku say they are not aware of any previous ROV dive.[13]
  2. Vailulu'u seamount[26] and North Su in the Manus Basin.[27]
  3. ^ Including a species discovered on Eifuku at the "Golden Lips" and "Champagne" sites, Provanna exquisita.[31]
  4. Myojin Knoll, Munidopsis myojinensis.[33]
  5. Myojin Knoll, Alvinocaris marimonte.[34]

References

  1. ^ a b c d e f g h "NW Eifuku". Global Volcanism Program. Smithsonian Institution.
  2. ^ a b c d e f g h i Limen & Juniper 2006, p. 450.
  3. ^
    Bibcode:2004AGUFM.V43F..07S
    .
  4. ^ Metaxas 2011, p. 104.
  5. ^ Metaxas 2011, p. 105.
  6. ^ Kurzawa et al. 2019, p. 240.
  7. ^ a b c d Lupton et al. 2006, p. 3.
  8. ^ Cantwell, Kasey; Newman, Jim (2016). Okeanos Explorer ROV dive summary, EX1605L3, June 26, 2016 (Report).
  9. S2CID 129715492
    .
  10. ^
    University of Texas Dallas
    . Retrieved 4 July 2021.
  11. ^ a b Hein, J. R.; Fleishman, C. L.; Morgenson, L. A.; Bloomer, S. H.; Stern, R. J. (1987). Submarine ferromanganese deposits from the Mariana and Volcano volcanic arcs, West Pacific (Report). pp. 13–14.
  12. ^ a b c Makita et al. 2016, p. 5744.
  13. ^ a b c Cantwell & Newman 2016, p. 3.
  14. ^ a b c Lupton et al. 2006, p. 17.
  15. ISSN 0022-3530
    .
  16. ^ Kurzawa et al. 2019, p. 242.
  17. Bibcode:2004AGUFM.V54A..04D
    .
  18. ^
    Bibcode:2004AGUFM.V43F..08L
    .
  19. Bibcode:2004AGUFM.V43F..06C
    .
  20. ^ a b c d Tunnicliffe et al. 2009, p. 344.
  21. ^ a b c Lupton et al. 2006, p. 4.
  22. ^ Davis & Moyer 2008, p. 2.
  23. ^ Makita et al. 2016, p. 5743.
  24. ^ Davis & Moyer 2008, p. 4.
  25. ^ Tunnicliffe et al. 2009, p. 345.
  26. Bibcode:2005AGUFM.V44A..07B
    .
  27. S2CID 133336199
    .
  28. ^
    Bibcode:2004AGUFM.V41B1388D
    .
  29. ^ Lupton et al. 2006, p. 12.
  30. Bibcode:2005AGUFM.V51C1509D
    .
  31. PMID 36760627
    .
  32. ^ Metaxas 2011, p. 107.
  33. ^
    ISSN 1175-5334
    .
  34. S2CID 213034894
    .
  35. ^ Limen & Juniper 2006, p. 452.
  36. ^ Limen & Juniper 2006, p. 449.
  37. ^ Klapper, Regina; Widdicombe, Steve (2013). ECO2 Briefing Paper No. 2: Potential impacts of CO2 leakage from sub-surface storage on seabed biology (Report). Kiel, Germany.
  38. ^ Tunnicliffe et al. 2009, p. 347.
  39. ^ Rossi & Tunnicliffe 2017, p. 61.
  40. ^ Metaxas 2011, p. 108.
  41. ^ Anderson, Johnson & Nonaka 2018, p. 77.

Sources

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