# MIT Guyot

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

The volcano was eventually covered by a [carbonate platform](/source/Carbonate_platform) resembling that of a present-day [atoll](/source/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](/source/Albian).

## Name and research history

MIT means [Massachusetts Institute of Technology](/source/Massachusetts_Institute_of_Technology).[1] Drilling in MIT Guyot recovered about 185 metres (607 ft) of [basaltic](/source/Basalt) rocks[2] as part of the [Ocean Drilling Program](/source/Ocean_Drilling_Program) which targeted MIT along with four other guyots of the Pacific Ocean.[3]

## Geography and geology

### Local setting

The seamount lies in the [Western Pacific Ocean](/source/Western_Pacific_Ocean)[2] northwest of [Marcus Island](/source/Marcus_Island)[4] and about halfway between [Japan](/source/Japan) and the [Marshall Islands](/source/Marshall_Islands).[5] The [Marcus-Wake Seamounts](/source/Marcus-Wake_Seamounts) lie nearby,[2] but MIT Guyot is a more isolated volcanic edifice[1] that is sometimes considered to be a member of the [Japanese Seamounts](/source/Japanese_Seamounts).[6] The [crust](/source/Crust_(geology)) beneath the seamount is 160 million years old[7] and the [Kashima fracture zone](/source/Kashima_fracture_zone) passes southwest from MIT Guyot.[8]

MIT Guyot rises from a depth of 6,100 metres (20,000 ft) to 1,390 metres (4,560 ft) below sea level,[7] although drill cores have been taken from depths of 1,323 metres (4,341 ft).[9] The seamount is over 20 kilometres (12 mi) long and 2–6 kilometres (1.2–3.7 mi) wide, widening southwestwards.[10] It has a flat top[6] at a depth of 1,400 metres (4,600 ft)[11] and has been described as a sunken [atoll](/source/Atoll),[6] with a [relief](/source/Relief) of about 100 metres (330 ft).[7] [Karst](/source/Karst) features occur on the seamount and are up to 200 metres (660 ft) deep,[6] including [dolines](/source/Doline) and [sinkholes](/source/Sinkhole).[12] The outer slopes of MIT Guyot are steep, a typical trait for guyot slopes.[13]

### Regional setting

A number of [seamounts](/source/Seamount) occur in the Western Pacific Ocean which often form lines and groups and have the appearance of drowned [atolls](/source/Atoll),[14] with flat tops at depths of 1–2 kilometres (0.62–1.24 mi) below sea level.[5] They often appear to be shallower than would be expected from [plate tectonics](/source/Plate_tectonics) and the normal [thermal subsidence](/source/Thermal_subsidence) of the [oceanic crust](/source/Oceanic_crust). Their formation has been explained by [hotspot](/source/Hotspot_(geology)) volcanism in the region of present-day [French Polynesia](/source/French_Polynesia) although many of them do not appear to have originated from simple [hotspot](/source/Hotspot_(geology)) mechanisms. These seamounts are considered to be part of the [Darwin Rise](/source/Darwin_Rise),[12] which includes MIT.[1]

About five different [hotspots](/source/Hotspot_(geology)) were active in French Polynesia within the last twenty million years.[15] Formation of the MIT Guyot has been linked to the [Tahiti hotspot](/source/Tahiti_hotspot).[16] However, linking specific seamounts to specific hotspots runs into difficulties when the linkage between one hotspot-seamount pair involves a mismatch between another hotspot-seamount pair.[2]

### Composition

MIT Guyot has erupted [basaltic](/source/Basalt) rocks,[1] with rock composition changing over time from [alkali basalts](/source/Alkali_basalt) over [basanite](/source/Basanite) to [hawaiite](/source/Hawaiite).[17] [Phenocryst](/source/Phenocryst) phases include [clinopyroxene](/source/Clinopyroxene), [olivine](/source/Olivine) and [plagioclase](/source/Plagioclase), and [apatite](/source/Apatite), [augite](/source/Augite) and [pyroxene](/source/Pyroxene) are additional components.[16] [Isotope ratios](/source/Isotope_ratio) resemble these of the northern Wake seamounts and of the [Marquesas hotspot](/source/Marquesas_hotspot).[18]

Alteration of basalts has given rise to [clay](/source/Clay),[19] [chlorite](/source/Chlorite), [goethite](/source/Goethite), [hematite](/source/Hematite), [hydromica](/source/Hydromica), [kaolinite](/source/Kaolinite) and especially [smectite](/source/Smectite)[1] but also [zeolite](/source/Zeolite). [Palagonite](/source/Palagonite) and [sideromelane](/source/Sideromelane) have been found in some samples.[19] [Clays](/source/Clay) contain [pyrite](/source/Pyrite).[1] Carbonates include both [bindstone](/source/Bindstone),[20] [grainstone](/source/Grainstone), [packstone](/source/Packstone) and [wackestone](/source/Wackestone) with subordinate [rudstone](/source/Rudstone).[1] Some carbonate sediments take the form of [ooids](/source/Ooid), [peloids](/source/Peloid) and [pisoids](/source/Pisoid)[21] or contain [vuggy](/source/Vug) porosities.[19]

## Geologic history

MIT Guyot formed during the [Cretaceous](/source/Cretaceous)[22] about 123 million years ago.[1] Based on [paleomagnetic](/source/Paleomagnetic) data, the seamount formed at a [latitude](/source/Latitude) of 11.5 ± 2.3 degrees south[2] and is at least 118 million years old.[7] A paleolatitude of 32.8 degrees south may also be possible and would be consistent with that of the [Macdonald hotspot](/source/Macdonald_hotspot).[23]

### First volcanism

[Argon–argon dating](/source/Argon%E2%80%93argon_dating) has yielded ages of 119.6[11]–124 million years for volcanic rocks taken from MIT Guyot.[2] There appear to have been three separate volcanic episodes[1] which generated three sets of volcanic rocks with different composition.[16] [Basaltic](/source/Basalt) [lava flows](/source/Lava_flow) form stacks that were emplaced one on top of another and on top of other types of volcanic deposits. The flows are often separated by [weathered](/source/Weathering) layers.[1] A 9.6 metres (31 ft) thick [soil](/source/Soil) developed on these lava flows;[24] the soil was probably removed by erosion such as wave action in some places.[25]

### Carbonate platform and late volcanism

During the [Aptian](/source/Aptian), a carbonate platform started developing on the exposed volcanic rocks of MIT. It developed in marine settings and formed two 118 metres (387 ft) and 396 metres (1,299 ft) thick carbonate layers continuing into the [Albian](/source/Albian), the two layers being separated by a 204 metres (669 ft) thick volcanic succession.[1] The carbonate platform probably started out as a [fringing reef](/source/Fringing_reef) or [barrier reef](/source/Barrier_reef)[26] with the sole drill core from MIT indicating a delay of about 1-2 million years between the end of volcanism and the beginning of platform growth,[27] and at least seven different stages of sea level rise have been recognized.[28] The total lifespan of the active carbonate platform is about 19 million years.[29]

The MIT Guyot platform was characterized by the presence of both a carbonate platform and an [atoll](/source/Atoll)-like structure[30] with [lagoonal](/source/Lagoon) structures that were progressively filled with sands, some of which were of biogenic origin. The lagoonal structure was affected by a secondary volcanic event but continued shallowing afterwards.[31] Elsewhere [bioherms](/source/Bioherm) as well as [patch reef](/source/Patch_reef) like structures evolved[32] and sandy shoals rimmed the lagoon.[28] Shallow muddy environments developed in some places of the platform, including [freshwater](/source/Freshwater) areas where [charophytes](/source/Charophyte) developed.[31] However, there is no evidence that the carbonate platform of MIT featured [vegetation](/source/Vegetation) at that time.[33]

Some [algae](/source/Alga)[a][31] and [foraminifera](/source/Foraminifera)[b] lived on the MIT Guyot platform,[1] the former were the source of [rhodoliths](/source/Rhodolith).[30] The algae are warm water shallow sea genera, reflecting warm waters at MIT when it was a carbonate platform.[34] [Storm](/source/Storm) activity led to the redeposition of carbonate sediments, forming [shoals](/source/Shoal).[35]

Various animals have been identified in the carbonate deposit as well, they inhabited the platform when it was still active.[1] These include [bivalves](/source/Bivalve), [bryozoans](/source/Bryozoan), [corals](/source/Coral), [echinoids](/source/Echinoid), [gastropods](/source/Gastropod), [ostracods](/source/Ostracod),[31] [oysters](/source/Oyster),[1] [rudists](/source/Rudist), [sponges](/source/Sponge)[31] and [stromatoporoids](/source/Stromatoporoid).[20] Additionally, [crustacean](/source/Crustacean) [coproliths](/source/Coprolite) have been dredged from the seamount.[6]

Renewed volcanic activity took place after the start of carbonate deposition, perhaps separated from the previous volcanic episodes by about 4 million years, leading to [eruptions](/source/Eruption) through the carbonate platform.[19] After a prelude characterized by the deposition of several ash layers, two major [explosive eruptions](/source/Explosive_eruption) shook the platform[36] The late volcanic activity[1] at MIT took place [underwater](/source/Submarine_eruption), forming [pyroclastic](/source/Pyroclastic_rock) material including [lapilli](/source/Lapilli) and [tephra](/source/Tephra) but also reworked [carbonate](/source/Carbonate) material.[22] Also, [tuffs](/source/Tuff) and [volcanic ash](/source/Volcanic_ash) layers were emplaced.[1] The eruption may have started as a [phreatomagmatic](/source/Phreatomagmatic) eruption when water within a [lagoon](/source/Lagoon) or within pores of the carbonate platform interacted with the rising [magma](/source/Magma).[37] The eruption formed an [eruption column](/source/Eruption_column) and a [crater](/source/Volcanic_crater) within the carbonate platform that was subsequently filled by other eruption products.[13] It is likely that this volcanic activity caused the formation of a volcanic island above the carbonate platform.[38]

### Drowning and later evolution

Growth of the carbonate platform ceased during the late [Albian](/source/Albian).[39] Such a drowning process has been observed at other Pacific guyots such as [Takuyo-Daisan](/source/Takuyo-Daisan), [Limalok](/source/Limalok) and [Wōdejebato](/source/W%C5%8Ddejebato) at different times and appears to occur for a multitude of reasons. One of these is a brief period of emergence of the carbonate platform which reduces the space available for carbonate-producing organisms and thus their carbonate production rate[40] until it can no longer compete with sea level rises. Another factor is an increasingly unfavourable environment as the platforms approach the equator; all these platforms drowned as they approached the equator perhaps owing to excessively hot waters and too many nutrients that favour the growth of algae; such algal growth is found in the last carbonates deposited at MIT.[41] In the case of MIT, the platform underwent a temporary uplift before drowning.[28]

A pelagic cap has formed on MIT but is rather thin, only 3.2 metres (10 ft) of material have accumulated[1] and that mainly in surface depressions.[42] It includes [manganese](/source/Manganese) crusts[c][11] which were emplaced over the 95 million years that lapsed between the drowning of the platform and the [Miocene](/source/Miocene), when [pelagic](/source/Pelagic) sedimentation commenced at MIT.[26] Three different phases of pelagic sedimentation during the Miocene-[Pliocene](/source/Pliocene), Pliocene and [Pleistocene](/source/Pleistocene) have been found.[42]

### Notes

1. Among the algae genera found on MIT are *[Acroporella](/source/Acroporella)*, *[Boueina](/source/Boueina)*, *[Cylindroporella](/source/Cylindroporella)*, *[Montiella](/source/Montiella)*, *[Parachaetetes](/source/Parachaetetes)*, *[Polystrata](/source/Polystrata)*, *[Salpingoporella](/source/Salpingoporella)*, *[Similiclypeina](/source/Similiclypeina)*, *[Solenopora](/source/Solenopora)*, *[Suppiluliumaella](/source/Suppiluliumaella)* and *[Triploporella](/source/Triploporella)*.[34]

1. Among the foraminifera genera found on MIT are *[Ammobaculites](/source/Ammobaculites)*, *[Arenobulimina](/source/Arenobulimina)*, *[Axiopolina](/source/Axiopolina)*, *[Bdelloidina](/source/Bdelloidina)*, *[Coskinolinella](/source/Coskinolinella)*, *[Cuneolina](/source/Cuneolina)*, *[Daxia](/source/Daxia_(genus))*, *[Debarina](/source/Debarina)*, *[Lituola](/source/Lituola)*, *[Neotrocholina](/source/Neotrocholina)*, *[Nezzazata](/source/Nezzazata)*, *[Novalesia](/source/Novalesia)*, *[Orbitolina](/source/Orbitolina)*, *[Pseudonummoloculina](/source/Pseudonummoloculina)*, *[Praechrysalidina](/source/Praechrysalidina)*, *[Sabaudia](/source/Sabaudia_(genus))*, *[Tubiphytes](/source/Tubiphytes)*, *[Valvulineria](/source/Valvulineria)*, *[Vercorsella](/source/Vercorsella)* and *[Voloshinoides](/source/Voloshinoides)*.[43]

1. Containing [asbolane](/source/Asbolane), [buserite](/source/Buserite) and [vernadite](/source/Vernadite) minerals.[44]

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Adapted from the Wikipedia article [MIT Guyot](https://en.wikipedia.org/wiki/MIT_Guyot) by Wikipedia contributors ([contributor history](https://en.wikipedia.org/wiki/MIT_Guyot?action=history)). Available under [Creative Commons Attribution-ShareAlike 4.0 International](https://creativecommons.org/licenses/by-sa/4.0/). Changes may have been made.