Takuyo-Daisan is a guyot in the Western Pacific Ocean off Japan. It is 1,409 metres (4,623 ft) deep and has a square-shaped flat top surrounded by a perimeter ridge. Several other seamounts lie nearby.

The seamount formed as a volcanic island during the Cretaceous in the area currently occupied by French Polynesia. Subsequently reefs developed around the volcanic island and generated a carbonate platform which drowned during the Albian along with several other such platforms in the world.

Takuyo-Daisan is located in Oceania
Takuyo-Daisan (Oceania)
Location offshore Japan
Summit depth1,409 m (4,623 ft)
LocationWestern Pacific Ocean
GroupJapanese Seamounts
Coordinates34°12′N 144°18′E / 34.2°N 144.3°ECoordinates: 34°12′N 144°18′E / 34.2°N 144.3°E
Age of rockCretaceous
Last activityAptian

Name and research history

Takuyo-Daisan was formerly known as "Seiko guyot";[1] "Seiko guyot" was used even earlier for Takuyo-Daini while Takuyo-Daisan was named "Eiko".[2] This seamount was drilled by the Ocean Drilling Program, with Site 879 located on the seamount.[3]

Geography and geology

Takuyo-Daisan lies southeast of the city of Yokohama, Japan.[4] It is the easternmost seamount in the "Seiko" cluster[5] of the Japanese Seamounts.[3] The Boso Triple Junction lies only 200 kilometres (120 mi) away from the seamount.[2]


Takuyo-Daisan is a guyot[6] that rises to a minimum depth of 1,409 metres (4,623 ft)[7] and is capped by an approximately square-shaped surface platform at about 1,600 metres (5,200 ft) depth[8] which has a surface area of about 86 square kilometres (33 sq mi).[7] Depressions up to 75 metres (246 ft) deep cover the flat top. The top is surrounded by a 0.6–1 kilometre (0.37–0.62 mi) wide and up to 110 metres (360 ft) high ridge, especially on the northeastern and southern sides.[9] It may be either a bioherm or a karst landform. A 100 metres (330 ft)[10]-110 metres (360 ft) high structure may be part of the old volcanic edifice;[6] the interface between the carbonate platform and the volcanic basement has a sloping aspect.[11]

Away from the platform, the seamount has steep slopes probably formed by short lava flows[6] that rise 4.3 kilometres (2.7 mi) above the seafloor.[12] Channels, debris flow fronts and levees decorate its slopes.[13] Noticeable ridges emanate from the east-southeastern, southwestern, west-northwestern and north-northeastern corners of the seamount;[8] they appear to be rift zones,[14] and flank cones are found on the eastern slopes. The southern slopes feature slump deposits, and the entire seamount is surrounded by a sediment fan.[13] The volume of the entire seamount is about 1,300 cubic kilometres (310 cu mi).[15] Two large seamounts lie west and southwest of Takuyo-Daisan with a smaller seamount between the two;[14] Takuyo-Daini is the western one and Jensen seamount the south-western one.[13] The seafloor underneath Takuyo-Daisan has an age of 143 million years.[16]


The Western Pacific Ocean features many seamounts with flat tops at depths of 1–2 kilometres (0.62–1.24 mi) below sea level which are known as guyots. They were considered to be remnants of eroded islands before Cretaceous carbonate platforms were discovered on them[5] which resemble present-day atolls although they do not have exactly the same properties.[12] Later similar submarine mountains were identified elsewhere in the Pacific Ocean as well. Menard 1958 suggested that the Western Pacific guyots once were part of an elevated region known as the Darwin Rise, later compared to present day French Polynesia.[4]

Many of these seamounts originally formed in the South Pacific, such as in French Polynesia,[17][18] where a number of recent volcanoes and volcanic chains can be found.[17] The original location of Takuyo-Daisan closely matches the present-day location of the Society hotspot,[19] and together with Takuyo-Daini, Winterer Guyot and Isakov Guyot appears to form a linear volcanic chain,[20] the Geisha guyots.[21]


Takuyo-Daisan has erupted basalt[22] containing olivine and plagioclase[23] and which define an intermediary to tholeiitic magma suite.[24] Weathering of volcanic rocks has given rise to calcite,[23] clay[10] which also contains coal,[25] iddingsite and zeolite.[23] Carbonates occur in the form of floatstone, grainstone, limestone, packstone, oncoids, peloids, rudstone and wackestone;[26] the limestone is of reefal origin.Hypersthene andesite samples taken from Takuyo-Daisan were probably brought there by ice rafting[27] as no such rocks have ever been found on this kind of volcanic island.[28]

Geologic history


Obtaining reliable radiometric ages from Takuyo-Daisan has been difficult; the most reliable age has been obtained from nearby Takuyo-Daini, 118.4 ± 1.8 million years ago.[18] From this date an age of 119.0 ± 1.8 million years ago has been inferred for Takuyo-Daisan.[29] A more recent date from Takuyo-Daisan is 117.5 ± 1.1 million years ago.[20] The seamount formed at 9[30]-7 degrees south from the equator.[31]

Volcanic activity formed breccia, lava flows with thicknesses of about 1 metre (3 ft 3 in)[25] and volcanic sediments. The volcanic rocks were subject to weathering, forming over 20 metres (66 ft) thick soils.[10] Phreatomagmatic deposits[11] and rocks interpreted as peperite have also been found,[22] implying that some lava flows may have interacted with wet soils as they were emplaced. Takuyo-Daisan at this time might have been an[25] at least 138 metres (453 ft)[32] and possibly as much as 900 metres (3,000 ft) high[7] tropical volcanic island with marshes that were inhabited by bioturbatory organisms.[25]

Carbonate sedimentation

Carbonate sedimentation at Takyuo-Daisan lasted from the Aptian to the Albian (based on foraminiferal fossils[33]) and led to the deposition of about 150 metres (490 ft)[34]-200 metres (660 ft) of carbonate sediment.[3] Carbonate sedimentation took place while the initial volcanic edifice was still emergent, similar to present-day Truk, Micronesia;[35] this resulted in terrigenous sedimentation in the carbonates.[25] The total duration of carbonate sedimentation is about 15 million years,[36] 3 metres (9.8 ft) thick distinct sequences in the carbonate sediments may be correlated to Milankovich cycles.[37]

The carbonate platform at Takuyo-Daisan featured both barrier shoals and lagoonal environments.[25] Biogenic mounds grew at the margin of the platform.[38] Redeposition of carbonate sediments led to the formation of sandy shoals[39] which formed the later perimeter ridge.[40] Overall the environment of the platform was a warm Tethyan environment.[41]

Algae[a][42] including algal mats,[43] bivalves, corals,[42] cyanobacteria,[43] echinoids, foraminifera[b],[42] molluscs,[26] nannofossil-forming species[45] and rudists inhabited the carbonate platform, and arthropods and woods have been found in the oldest carbonate deposits. The fauna of Takuyo-Daisan was not particularly diverse, probably because the seamount was located close to the paleoequator and away from the Tethyan margin that many species found at Takuyo-Daisan originate from.[42]

Drowning and post-drowning evolution

The drowning of the carbonate platform at Takuyo-Daisan has been attributed to different causes. A large transgression took place in the late Albian and may have caused the drowning. In other guyots nutrient excess has been implicated but there is no evidence of such at Takuyo-Daisan.[46] Other factors may include hostile conditions close to the equator and unfavourable changes of the geomorphology of the platform at the time of its drowning.[47] The drowning of the Takuyo-Daisan platform was simultaneous to the drowning of carbonate platforms elsewhere around the world and may have been caused by tectonically-induced sea level fluctuations.[48]

After cessation of the platform activity, manganese crusts[26] and chalks later modified by phosphate developed on exposed rocks. During the Neogene, oozes,[10] terrigenous sediments,[49] wind-borne material such as pollen[50] and volcanic ash from the approaching Japanese volcanic arc accumulated on Takuyo-Daisan.[10]

Presently, Takuyo-Daisan lies in a region of high plankton productivity which has led to a high diatom[c] deposition rate[52] as well as high sedimentation rates in general. Corals and sponges have been found on the seamount; crinoids may also occur there.[53]


  1. ^ Such as Marinella, Neomeris, Pycnoporidium, Terquemella and Zittelina.[41]
  2. ^ Genera include Arenobulimina, Axiopolina, Bdelloidina, Cuneolina, Daxia, Debarina, Fischerina, Istriloculina, Lituola, Nezzazata, Novalesia, Orbitolina, Paracoskinolina, Trocholina, and Vercorsella.[44]
  3. ^ Diatom genera include Asterolampra, Asteromphalus, Chaetoceros, Cyclotella, Neodenticula, Nitzschia, Odontella, Paralia, Rhizosolenia, Stephanopyxis, Thalassionema, Thalassiosira, Thalassiothrix and Xanthiopyxis.[51]


  1. ^ Camoin, G. F.; Davies, P. J. (2009). Reefs and Carbonate Platforms in the Pacific and Indian Oceans. John Wiley & Sons. p. 105. ISBN 9781444304886.
  2. ^ a b Vogt & Smoot 1984, p. 11087.
  3. ^ a b c Arnaud Vanneau & Premoli Silva 1995, p. 199.
  4. ^ a b Haggerty & van Waasbergen 1995, p. 842.
  5. ^ a b Haggerty & van Waasbergen 1995, p. 841.
  6. ^ a b c Rack, Lawyer & Gee 1995, p. 973.
  7. ^ a b c Vogt & Smoot 1984, p. 11088.
  8. ^ a b Haggerty & van Waasbergen 1995, p. 845.
  9. ^ Haggerty & van Waasbergen 1995, p. 843.
  10. ^ a b c d e Ogg, Camoin & Jansa 1995, p. 361.
  11. ^ a b Haggerty & Premoli Silva 1995, p. 943.
  12. ^ a b Larson et al. 1995, p. 915.
  13. ^ a b c Vogt & Smoot 1984, p. 11093.
  14. ^ a b Sigurdsson, Haraldur; Houghton, Bruce; Rymer, Hazel; Stix, John; McNutt, Steve (1999). Encyclopedia of Volcanoes. Academic Press. p. 396. ISBN 9780080547985.
  15. ^ Vogt & Smoot 1984, p. 11090.
  16. ^ Larson et al. 1995, p. 919.
  17. ^ a b Christie, Dieu & Gee 1995, p. 495.
  18. ^ a b Pringle & Duncan 1995, p. 553.
  19. ^ Pringle & Duncan 1995, p. 548.
  20. ^ a b Koppers, Anthony A. P.; Staudigel, Hubert; Pringle, Malcolm S.; Wijbrans, Jan R. (October 2003). "Short-lived and discontinuous intraplate volcanism in the South Pacific: Hot spots or extensional volcanism?". Geochemistry, Geophysics, Geosystems. 4 (10): 23. doi:10.1029/2003GC000533.
  21. ^ Vogt & Smoot 1984, p. 11086.
  22. ^ a b Pringle & Duncan 1995, p. 549.
  23. ^ a b c Christie, Dieu & Gee 1995, p. 502.
  24. ^ Christie, Dieu & Gee 1995, p. 505.
  25. ^ a b c d e f Ogg, Camoin & Jansa 1995, p. 366.
  26. ^ a b c Haggerty & van Waasbergen 1995, p. 867.
  27. ^ Heezen et al. 1973, p. 693.
  28. ^ Heezen et al. 1973, p. 684.
  29. ^ Larson et al. 1995, p. 927.
  30. ^ Haggerty & Premoli Silva 1995, p. 942.
  31. ^ Haggerty & Premoli Silva 1995, p. 941.
  32. ^ Larson et al. 1995, p. 929.
  33. ^ Arnaud Vanneau & Premoli Silva 1995, p. 211.
  34. ^ Flood, Peter (March 1999). "Development of northwest Pacific guyots: General results from Ocean Drilling Program legs 143 and 144". The Island Arc. 8 (1): 94. doi:10.1046/j.1440-1738.1999.00222.x. ISSN 1038-4871.
  35. ^ Ogg, Camoin & Jansa 1995, p. 371.
  36. ^ Haggerty & Premoli Silva 1995, p. 946.
  37. ^ Ogg, Camoin & Jansa 1995, p. 373.
  38. ^ Jansa, L.F.; Arnaud Vanneau, A. (December 1995), "Carbonate Buildup and Sea-Level Changes at MIT Guyot, Western Pacific" (PDF), Proceedings of the Ocean Drilling Program, 144 Scientific Results, Proceedings of the Ocean Drilling Program, 144, Ocean Drilling Program, p. 319, doi:10.2973/odp.proc.sr.144.039.1995, retrieved 2018-08-07
  39. ^ Ogg, Camoin & Jansa 1995, p. 370.
  40. ^ Haggerty & Premoli Silva 1995, p. 945.
  41. ^ a b Masse, J.-P.; Arnaud Vanneau, A. (December 1995), "Early Cretaceous Calcareous Algae of the Northwest Pacific Guyots" (PDF), Proceedings of the Ocean Drilling Program, 144 Scientific Results, Proceedings of the Ocean Drilling Program, 144, Ocean Drilling Program, p. 225, doi:10.2973/odp.proc.sr.144.073.1995, retrieved 2018-08-06
  42. ^ a b c d Arnaud Vanneau & Premoli Silva 1995, p. 212.
  43. ^ a b Ogg, Camoin & Jansa 1995, p. 365.
  44. ^ Arnaud Vanneau & Premoli Silva 1995, pp. 202-210.
  45. ^ Erba, Premoli Silva & Watkins 1995, p. 164.
  46. ^ Ogg, Camoin & Jansa 1995, p. 374.
  47. ^ Ogg, Camoin & Jansa 1995, p. 375.
  48. ^ Winterer, E.L.; Sager, W.W. (December 1995), "Synthesis of Drilling Results from the Mid-Pacific Mountains: Regional Context and Implications" (PDF), Proceedings of the Ocean Drilling Program, 143 Scientific Results, Proceedings of the Ocean Drilling Program, 143, Ocean Drilling Program, p. 525, doi:10.2973/odp.proc.sr.143.245.1995, retrieved 2018-08-07
  49. ^ Rack, Lawyer & Gee 1995, p. 981.
  50. ^ Fenner 1995, p. 62.
  51. ^ Fenner 1995, pp. 73-74.
  52. ^ Fenner 1995, p. 73.
  53. ^ Fenner 1995, p. 76.


Geology of the Pacific Ocean

The Pacific Ocean evolved in the Mesozoic from the Panthalassic Ocean, which had formed when Rodinia rifted apart around 750 Ma. The first ocean floor which is part of the current Pacific Plate began 160 Ma to the west of the central Pacific and subsequently developed into the largest oceanic plate on Earth.The tectonic plates continue to move today. The slowest spreading ridge is the Gakkel Ridge on the Arctic Ocean floor, which spreads at less than 2.5 cm/year (1 in/year), while the fastest, the East Pacific Rise near Easter Island, has a spreading rate of over 15 cm/year (6 in/year).


Limalok (formerly known as Harrie or Harriet) is a Cretaceous-Paleocene guyot/tablemount in the southeastern Marshall Islands, one of a number of seamounts (a type of underwater volcanic mountain) in the Pacific Ocean. It was probably formed by a volcanic hotspot in present-day French Polynesia. Limalok lies southeast of Mili Atoll and Knox Atoll, which rise above sea level, and is joined to each of them through a volcanic ridge. It is located at a depth of 1,255 metres (4,117 ft) and has a summit platform with an area of 636 square kilometres (246 sq mi).

Limalok is formed by basaltic rocks and was probably a shield volcano at first; the Macdonald, Rarotonga, Rurutu and Society hotspots may have been involved in its formation. After volcanic activity ceased, the volcano was eroded and thereby flattened, and a carbonate platform formed on it during the Paleocene and Eocene. These carbonates were chiefly produced by red algae, forming an atoll or atoll-like structure with reefs.

The platform sank below sea level 48 ± 2 million years ago during the Eocene, perhaps because it moved through the equatorial area, which was too hot or nutrient-rich to support the growth of a coral reef. Thermal subsidence lowered the drowned seamount to its present depth. After a hiatus lasting into the Miocene, sedimentation commenced on the seamount leading to the deposition of manganese crusts and pelagic sediments; phosphate accumulated in some sediments over time.

MIT Guyot

MIT Guyot is a guyot in the Pacific Ocean that rises to a depth of 1,323 metres (4,341 ft). It has a 20-kilometre-long (12 mi) summit platform and formed during the Cretaceous in the region of present-day French Polynesia through volcanic eruptions.

The volcano was eventually covered by a carbonate platform resembling that of a present-day atoll which was colonized by a number of animals. A major volcanic episode disrupted this platform, which subsequently redeveloped until it drowned in the late Albian.

Outline of oceanography

The following outline is provided as an overview of and introduction to Oceanography.


Takuyo-Daini is a seamount in the Pacific Ocean.

Takuyo-Daini is part of the so-called "Seiko" cluster or the "Geisha Guyots" in the Japanese Seamounts; it lies just west of Takuyo-Daisan seamount with which it forms a pair. Takuyo-Daini rises from a depth of 5,195 metres (17,044 ft) to a minimum depth of 1,420 metres (4,660 ft) and has a regular round shape with a small volume of 2,237 cubic kilometres (537 cu mi). Both seamounts are guyots and together with two other guyots known as Winterer and Isakov have been interpreted as being part of a hotspot track.The Western Pacific Ocean contains a large number of seamounts which often from clusters or groups. Many of them have flat tops 1–2 kilometres (0.62–1.24 mi) below sea level. A number of these formed during a large-scale volcanic episode in the Albian-Aptian era of the Cretaceous; this includes Takuyo-Daini, where radiometric dating has yielded ages of 118.6 million years ago. At the time of its formation this seamount was located in the central Pacific Ocean. Fossils of rudist bivalves have been found on Takuyo-Daini; the seamount once featured rudist reefs that ceased growing during the Albian. The rudist genera Magallanesia was discovered on Takuyo-Daini and on Cebu in the Philippines.


Wōdejebato (formerly known as Sylvania) is a Cretaceous guyot or tablemount in the northern Marshall Islands, Pacific Ocean. Wōdejebato is probably a shield volcano and is connected through a submarine ridge to the smaller Pikinni Atoll 74 kilometres (46 mi) southeast of the guyot; unlike Wōdejebato, Pikinni rises above sea level. The seamount rises for 4,420 metres (14,500 ft) to 1,335 metres (4,380 ft) depth and is formed by basaltic rocks. The name Wōdejebato refers to a sea god of Pikinni.

It was probably formed by a hotspot in what is present-day French Polynesia before plate tectonics moved it to its present-day location. The Macdonald, Rarotonga, Rurutu and Society hotspots may have been involved in its formation. The first volcanic phase took place in the Cenomanian and was followed by the formation of a carbonate platform that quickly disappeared below the sea. A second volcanic episode between 85 and 78.4 million years ago (in the Campanian) led to the formation of an island. This island was eventually eroded and rudist reefs generated an atoll or atoll-like structure, covering the former island with carbonates and thus a second carbonate platform.

The second carbonate platform drowned about 68 million years ago (in the Maastrichtian), perhaps because at that time it was moving through the equatorial area which may have been too hot or too nutrient-rich to support the growth of a coral reef. Thermal subsidence lowered the drowned seamount to its present depth. After a hiatus, sedimentation commenced on the seamount and led to the deposition of manganese crusts and pelagic sediments, some of which were later modified by phosphate.

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