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Allison Guyot (formerly known as Navoceano Guyot) is a tablemount (guyot) in the underwater Mid-Pacific Mountains of the Pacific Ocean. It is a trapezoidal flat mountain rising 1,500 metres above the seafloor to a depth of less than 1,500 m, with a summit platform 35 by 70 kilometres wide. The Mid-Pacific Mountains lie west of Hawaii and northeast of the Marshall Islands, but at the time of their formation were located in the Southern Hemisphere.

Allison Guyot
Allison is located in Pacific Ocean
Allison
Allison
Height1.5 kilometres
Summit area35 x 70 kilometres
Location
GroupMid-Pacific Mountains
Coordinates18°16′N 179°20′E / 18.26°N 179.33°E / 18.26; 179.33Coordinates: 18°16′N 179°20′E / 18.26°N 179.33°E / 18.26; 179.33[1]
Geology
TypeGuyot

The tablemount was probably formed by a hotspot in the present-day Southern Pacific before plate tectonics moved it to its current location. Several hotspots, including the Easter, Marquesas and Society hotspots, may have been involved in the formation of the Mid-Pacific Mountains. Volcanic activity is dated to have occurred circa 111–85 million years ago and formed a volcanic island. Subsequently, carbonate deposition commenced as Allison Guyot subsided and eventually buried the island, forming an atoll-like structure and a carbonate platform. Among other animals, crocodilians lived on Allison Guyot.

The platform emerged above sea level during the Albian and Turonian ages. It drowned about 99 ± 2 million years ago for unknown reasons; possibly a phase of renewed emergence damaged the reefs, or it was located in unfavourable waters. Later, pelagic sedimentation commenced on the seamount and led to the deposition of sediments including limestone, ooze and sand, which bear traces of climatic events and ocean currents.

Contents

Name and research historyEdit

Allison Guyot is named after E.C. Allison, an oceanographer and paleontologist at the San Diego State College;[2] formerly it was named "Navoceano Guyot".[3] The name "Hamilton Guyot" has also been applied to Allison Guyot but is not correct;[4] Hamilton Guyot is a separate formation in the Mid-Pacific Mountains.[5] The seamount is the source of the Ocean Drilling Program[a] drill core 865A,[8] which was bored into the summit platform of Allison Guyot[9] in 1992[10] but did not reach the volcanic structure of the underwater mountain.[11] Two other cores 865C and 865B were obtained during the same operation; Allison Guyot is Site 865 Ocean Drilling Program.[8] These drill cores were part of a larger project to investigate and clarify the history of the flat-topped submarine mountains in the Pacific Ocean.[12]

Geography and geologyEdit

Local settingEdit

Allison Guyot is located in the equatorial Pacific Ocean,[1] part of the western Mid-Pacific Mountains.[13] The Mid-Pacific Mountains contain seamounts which were covered by limestones during the Barremian and Albian (circa 129.4 – circa 125 million years ago and circa 113–100.5 million years ago, respectively[14]).[15] Hawaii lies due east and the Marshall Islands southwest;[16] Resolution Guyot is 716 kilometres northwest.[17]

The guyot[4] (also known as tablemount[18]) has an outline resembling a trapezoid[13] and consists of two connected volcanic ridges facing north-northwest to east-northeast.[19] Its western parts may be a distinct volcano.[20] The surface platform has dimensions of 35 by 70 kilometres,[21] with an upwards-doming form 0.3–0.5 kilometres high,[22] and is covered by large sediment mounds;[23] the rim surrounding the platform lies at a depth of about 1,650 metres and there is evidence of former reefs.[21] The structure appears to consist of lagoonal sediments surrounded by a reef,[24] and the shallowest point of Allison Guyot lies at less than 1,500 metres (4,900 ft) depth below sea level.[25] Volcanic cones dot the eastern side of the summit plateau.[26] The seamount bears traces of slumping,[27] which on the southeastern side of Allison Guyot has removed part of the platform perimeter.[28]

The seamount rises 1.5 kilometres[29] above the seafloor. Underneath Allison Guyot, the seafloor is about 130–119 million years old,[15] and a 128-million year-old magnetic lineation is located nearby.[30] The Molokai Fracture Zone forms a ridge which passes close to Allison Guyot and intersects with another ridge at the seamount.[31] Tectonically the seamount is part of the Pacific Plate.[4]

Regional settingEdit

 
Diagram showing a cross section through the Earth's lithosphere (in yellow) with magma rising from the mantle (in red)

The west central and south central Pacific Ocean seafloor contains many guyots of the Mesozoic age that developed in seas shallower than typical of the present-day ocean.[32] These are submarine mountains which are characterised by a flat top and usually the presence of carbonate platforms that rose above the sea surface during the middle Cretaceous period.[33] Many of these seamounts were formerly atolls,[34] though there are some differences to present-day reef systems.[35][36] All these structures originally formed as volcanoes in the Mesozoic ocean.[34] The crust underneath these volcanoes tends to subside as it cools, and thus the islands and seamounts sink.[37] Fringing reefs may have developed on the volcanoes, which then became barrier reefs as the volcanoes subside and turn into atolls;[34] these rims surround lagoons or tidal flats.[38] Continued subsidence offset by growth of the reefs led to the formation of thick carbonate platforms.[39] Sometimes volcanic activity continued after the formation of the atoll or atoll-like structure, and during episodes where the platforms rose above sea level erosional features such as channels and blue holes[b] developed.[41] Eventually, these platforms drowned for reasons that are often unclear.[33]

The formation of many such seamounts has been explained with the hotspot theory, which describes the formation of chains of volcanoes that get progressively older along the length of the chain,[42] with an active volcano only at one end of the system. This volcano lies on a spot of the lithosphere heated from below; as the plate moves the volcano is moved away from the heat source and volcanic activity ceases, producing a chain of volcanoes that become older away from the currently active one.[43]

The "South Pacific Superswell" is a region in the Southern Pacific at the present-day Austral Islands, Cook Islands and Society Islands, where intense volcanic activity was underway during the Cretaceous, and is where the Cretaceous seamounts of the Mid-Pacific Mountains originated. The Easter hotspot, Marquesas hotspot and the Society hotspot may have been involved in the formation of the Mid-Pacific Mountains. After the Mountains had formed, plate tectonics shifted them northwards to their present-day position.[15] Allison Guyot appears to have formed in the same region.[11]

CompositionEdit

One drill core on Allison Guyot has found a 136-metre-thick layer of pelagic sediments, under which are 735-metre-thick limestones that formed in lagoons[9] and might continue down for almost 600 metres.[17] The limestone consists mostly of calcite with little dolomite[44] and occurs in the form of bafflestone,[45] grainstone, packstone, peloid, rudstone and wackestone;[46][47] ooliths have also been found.[48] The carbonates are of biogenic origin,[49] and fossils of dasyclads,[50] echinoderms,[19] gastropods, green algae,[50] molluscs,[22] ostracods,[46] oysters,[51] red algae,[19] rudists and sponges occur within the limestones;[50] some of the fossils have partially dissolved and are thus poorly preserved.[52] Remnants of crocodilians have been found within Aptian[c]–Albian mudstones, together with fossils of fish and unidentified vertebrates.[53] The limestone is partly altered by karstification and phosphatisation, and manganese has accumulated in the upper layers.[50]

Basalts occur in the form of cobbles[47] and sills within the limestones.[54] These basalts define an alkali basalt suite[55] and contain clinopyroxene, feldspar, ilmenite, plagioclase, pyroxene, spinel and titanomagnetite. They probably also contained olivine but the basaltic rocks sampled are so heavily altered that no olivine is left.[56][57] The basalts are typical of intraplate volcanism[58] and their geochemistry shows evidence that fractional crystallisation and mixing between different magmas were involved in their genesis.[59] The component minerals have often been completely altered to calcite, clays, gypsum, hematite, quartz and other, unidentified minerals,[60] either when exposed above sea level or through hydrothermal fluids when the sills formed.[61] The formation of the sills led to the hardening and hydrothermal alteration of the surrounding sediments.[54]

Clays are found both within the limestones[54] and in layers between the carbonates.[49] They consist of berthierine, chlorite, feldspar, hydromica, illite, kaolinite, mica, quartz, serpentine, smectite and possible zeolite.[62][63][64] The clays were in part derived from lateritic soils that developed on the volcanic island before they were completely buried in carbonates,[65] and in part formed in settings with limited water exchange during lagoonal stages.[66] Dolomite, gypsum and pyrite co-occur with some clays,[67] and claystones[d] have been found in some places.[46] Mudstones with evidence of animal burrows[69] and containing amber, glauconite, organic material including plant debris and pyrite have also been encountered;[53] pyrite indicates that anoxic environments existed on Allison Guyot.[9]

Black shale and coal form layers in one drill core.[47] The lower limestones contain substantial amounts of organic material that originated from terrestrial settings,[70] and remnants of animal burrows[71] and plant roots have been found[51] in many layers of the platform.[19] The clays and mudstones are rich in organic material.[49] Most of this organic material appears to come from plants[72] but some material has been attributed to algae.[73] Cells and tracheids can be found in the plant remnants.[74]

Geological historyEdit

 
Eniwetok Atoll today. Allison Guyot may have resembled Eniwetok in the past.

Radiometric dating has been performed on some of the volcanic rocks. Potassium–argon dating on the sills has yielded ages of 102 ± 6 million years ago and 87 ± 3 million years ago, while argon–argon dating also on the sills produced ages of 111.1 ± 2.6 million years,[54] 111.2 ± 1.2 million years ago and 104.8 ± 0.8 million years ago.[9] Other ages from the sills are about 110.7 ± 1.2 million years ago and 104.9 ± 2.0 million years ago.[75] Rocks dredged from the slopes of Allison Guyot have yielded ages of 101.2 ± 0.8 million years,[9] 102.7 ± 2.7 million years and 85.6 ± 1.3 million years ago.[75] Overall, the volcano is considered to be at least 111 million years old[75] and volcanic activity probably spanned 30[26]–25 million years and several stages.[29]

Both the sills and the dredged rocks were probably erupted after the main shield stage[29] and they may constitute a late stage of secondary volcanism;[11] two or three separate stages might have taken place, including one which formed a secondary cone on the eastern side of Allison Guyot. This may indicate that the seamount passed over more than one hotspot.[75] The volcano of Allison Guyot was apparently already partially eroded when the secondary volcanism took place.[55] Paleomagnetic data taken from limestones show that Allison Guyot developed in the Southern Hemisphere, at a latitude of about 11.2° ± 2.0° south.[76]

Emergent phaseEdit

 
Aerial image of the rim of Bikini Atoll. Allison Guyot during its carbonate platform stage may have resembled Bikini.

Allison Guyot began as a volcanic island[9] with a relief of perhaps 1.3 kilometres.[19] Located in equatorial waters suited to the deposition of carbonate platforms,[77] limestone[9] platform grew on the guyot[77] as it rapidly subsided during the Albian.[78] Eventually, the seamount became an atoll. Volcanic rocks cropped out for some time before they were buried into the carbonates,[9] and weathering products of the volcanic rocks accumulated in the limestones.[79] The islands were covered by vegetation, and vegetation cover decreased over time as the volcanic edifice sank.[72] The climate was probably humid and runoff was intense.[80]

The platform contains lagoon and swamp environments,[9] with water depths not exceeding 10 metres,[77] and at some stage contained sand shoals and islands formed by storms as well. The interior was not protected from the sea[77] and the sector of the platform that was investigated by drill cores apparently became increasingly accessible to it over time.[19] The inner platform had a quiet muddy water setting;[81] generally Allison Guyot at that time resembled the present-day Bikini and Eniwetok atolls in terms of morphology when Allison Guyot was emergent.[82]

The carbonate deposits indicate sea level changes following orbital cycles[83] consistent with Milankovitch forcing;[77] parts of the platform occasionally rose above sea level.[84] At some point, karst environments existed on Allison Guyot and are probably the reason for the irregular surface of the summit platform[85] and the presence of sinkholes; there are clear indications of about 200 metres of emergence.[86]

Bivalves[87] including rudists,[81] corals, echinoderms, foraminifera, green algae, hydrozoans, red algae and sponges have been found in the platform's deposits.[88] Rudists were at that time important reef builders[89] and together with sponges colonised the margin of the platform.[77] Among the rudist species discovered on Allison Guyot is Requienia cf. migliorinii.[81] Teeth of crocodilians have been found on the seamount.[53] Its 110 million years old[90] remnants are the oldest known crocodilians in the region of the Pacific Ocean. They indicate that such species lived within the lagoon of Allison Guyot and may give clues about the history of Pacific animals and their dispersal.[53]

Drowning and post-drowning evolutionEdit

A carbonate platform is said to 'drown' when sedimentation can no longer keep up with relative rises in sea level.[91] Carbonate sedimentation on Allison Guyot ended during late Albian times,[85] about 99 ± 2 million years ago, at the same time as at Resolution Guyot.[92] By Turonian times (93.9 – 89.8 ± 0.3 million years ago[14]), pelagic sedimentation was prevailing on Allison Guyot.[93] On both Allison and Resolution Guyots, the drowning was preceded by an episode where the platform rose above the sea;[94] possibly it was this emergence and the following submergence which terminated carbonate deposition and prevented it from beginning again.[95] Such emergence and drowning has been recorded at carbonate platforms of that age around the world and may be the consequence of tectonic events across the Pacific Ocean,[86] culminating in the uplift of a part thereof.[77] At that time, a last phase of volcanic activity on Allison Guyot generated several cones on its eastern part.[96] The evidence for this theory is not conclusive,[97] and another theory holds that the drowning of Allison Guyot occurred when it moved through equatorial waters, where upwelling increased the amount of nutrients available,[98] hampering the growth of platforms.[e][99] The waters might also have been too hot to support the survival of reef builders, as happens in present-day coral bleaching events.[100]

About 160 metres[f] of pelagic sediment[17] in the form of sand, ooze[101] and pelagic limestone accumulated on Allison Guyot; pelagic limestone is of Turonian to Campanian (83.6 ± 0.2 − 72.1 ± 0.2 million years ago[14]) age while the oozes and sands were deposited starting in the early Paleocene (66–56 million years ago[14]).[84] In drill cores, the ooze has a sandy, watery habitus owing to the prevalence of fossil foraminifera in the sediment.[13] The pelagic sediments have been bioturbated[g] in some places[103] and modified by sea currents, which have formed the large mound of pelagic sediment.[23] In drill cores, the ooze overlies Cretaceous shallow-water limestones,[104] which were modified by phosphatisation and manganese accumulation.[50] As plate tectonics moved Allison Guyot northward, its surrounding water masses changed, as did the properties of the pelagic cap.[85] Slumping of the platform occurred during the Cenozoic (the last 66 million years).[14][27]

The pelagic ooze bears evidence of the Paleocene–Eocene thermal maximum,[h] including temporary dissolution of carbonates, changes in the isotope ratios of carbon in sediments on Allison Guyot[106] and changes in foraminifera[107] and ostracod fossils found in the ooze. The latter underwent a major extinction during the Paleocene–Eocene Thermal Maximum on the seamount and took a long time to recover.[108]

Sea currents have altered the pelagic deposits by removing smaller particles. In particular deposits from warmer periods have been altered in this way on Allison Guyot, perhaps because warmer climates increased hurricane activity and thus the energy available in sea currents or deep-sea circulations shifted.[109] Furthermore, pauses in the sedimentation or episodes of slowdown have been identified.[110]

NotesEdit

  1. ^ The Ocean Drilling Program was a multinational research program that aimed at elucidating the geological history of the sea by obtaining drill cores from the oceans[6] and lasted from 1983 to 2003.[7]
  2. ^ Pit-like depressions within carbonate rocks that are filled with water.[40]
  3. ^ Between circa 125 and 113 million years ago[14]
  4. ^ Clays that became solid rocks.[68]
  5. ^ Increased nutrient levels favour plankton growth and reduce the amount of sunlight available to symbiotic organisms in the platform builders.[99]
  6. ^ Some of which was later probably eroded away.[17]
  7. ^ Animals have stirred, mixed and otherwise modified the sediments.[102]
  8. ^ The Paleocene–Eocene Thermal Maximum was an episode of extreme global warmth about 55.5 million years ago, during which temperatures rose by about 5–8 °C.[105]

ReferencesEdit

  1. ^ a b Arreguín-Rodríguez, Alegret & Thomas 2016, p. 348.
  2. ^ "Allison Guyot". GEOnet Names Server. Retrieved 2019-02-24.
  3. ^ Winterer, Edward L.; Metzler, Christopher V. (10 November 1984). "Origin and subsidence of Guyots in Mid-Pacific Mountains". Journal of Geophysical Research: Solid Earth. 89 (B12): 9973. Bibcode:1984JGR....89.9969W. doi:10.1029/jb089ib12p09969. ISSN 0148-0227.
  4. ^ a b c "Allison Guyot". Seamount Catalog. Retrieved 7 October 2018.
  5. ^ "Search Results". Seamount Catalog. Retrieved 24 February 2019.
  6. ^ "Ocean Drilling Program". Texas A&M University. Retrieved 8 July 2018.
  7. ^ "Ocean Drilling Program Legacy". Consortium for Ocean Leadership. Retrieved 10 January 2019.
  8. ^ a b Bralower & Mutterlose 1995, p. 31.
  9. ^ a b c d e f g h i Sager & Tarduno 1995, p. 399.
  10. ^ Winterer, Sager & Firth 1992, pp. 56–57.
  11. ^ a b c Baker, Castillo & Condliffe 1995, p. 255.
  12. ^ Winterer & Sager 1995, p. 497.
  13. ^ a b c Bralower & Mutterlose 1995, p. 32.
  14. ^ a b c d e f "International Chronostratigraphic Chart" (PDF). International Commission on Stratigraphy. August 2018. Retrieved 22 October 2018.
  15. ^ a b c Baker, Castillo & Condliffe 1995, p. 245.
  16. ^ Bralower et al. 1995, p. 843.
  17. ^ a b c d Winterer & Sager 1995, p. 501.
  18. ^ Bouma, Arnold H. (September 1990). "Naming of undersea features". Geo-Marine Letters. 10 (3): 121. Bibcode:1990GML....10..119B. doi:10.1007/bf02085926. ISSN 0276-0460.
  19. ^ a b c d e f Winterer & Sager 1995, p. 516.
  20. ^ Röhl & Ogg 1996, p. 606.
  21. ^ a b Grötsch & Flügel 1992, p. 156.
  22. ^ a b Iryu & Yamada 1999, p. 476.
  23. ^ a b Winterer & Sager 1995, p. 527.
  24. ^ Winterer, Sager & Firth 1992, p. 10.
  25. ^ Shipboard Scientific Party 1993, p. 15.
  26. ^ a b Pringle, M.S.; Duncan, R.A. (May 1995). "Radiometric Ages of Basaltic Lavas Recovered at Sites 865, 866, and 869" (PDF). Proceedings of the Ocean Drilling Program, 143 Scientific Results. Proceedings of the Ocean Drilling Program. 143. Ocean Drilling Program. p. 282. doi:10.2973/odp.proc.sr.143.218.1995. Retrieved 2018-10-08.
  27. ^ a b Winterer, Jerry. "Relative changes in Cretaceous sea level as recorded on guyots of the Mid-Pacific Mountains" (PDF). ODP Legacy. Retrieved 8 October 2018.
  28. ^ Winterer & Sager 1995, p. 509.
  29. ^ a b c Janney & Castillo 1999, p. 10574.
  30. ^ Winterer & Sager 1995, p. 508.
  31. ^ Smoot, N.Christian (December 1999). "Orthogonal intersections of megatrends in the Western Pacific ocean basin: a case study of the Mid-Pacific mountains". Geomorphology. 30 (4): 344. Bibcode:1999Geomo..30..323S. doi:10.1016/S0169-555X(99)00060-4. ISSN 0169-555X.
  32. ^ Janney & Castillo 1999, p. 10571.
  33. ^ a b Grötsch & Flügel 1992, p. 153.
  34. ^ a b c Pringle et al. 1993, p. 359.
  35. ^ Iryu & Yamada 1999, p. 485.
  36. ^ Röhl & Strasser 1995, p. 211.
  37. ^ Röhl & Ogg 1996, pp. 595–596.
  38. ^ Röhl & Ogg 1996, p. 596.
  39. ^ Strasser, A.; Arnaud, H.; Baudin, F.; Rohl, U. (May 1995). "Small-Scale Shallow-Water Carbonate Sequences of Resolution Guyot (Sites 866, 867, and 868)" (PDF). Proceedings of the Ocean Drilling Program, 143 Scientific Results. Proceedings of the Ocean Drilling Program. 143. Ocean Drilling Program. p. 119. doi:10.2973/odp.proc.sr.143.228.1995. Retrieved 2018-10-08.
  40. ^ Mylroie, John E.; Carew, James L.; Moore, Audra I. (September 1995). "Blue holes: Definition and genesis". Carbonates and Evaporites. 10 (2): 225. doi:10.1007/bf03175407. ISSN 0891-2556.
  41. ^ Pringle et al. 1993, p. 360.
  42. ^ Winterer & Sager 1995, p. 498.
  43. ^ Sleep, N H (May 1992). "Hotspot Volcanism and Mantle Plumes". Annual Review of Earth and Planetary Sciences. 20 (1): 19. Bibcode:1992AREPS..20...19S. doi:10.1146/annurev.ea.20.050192.000315.
  44. ^ Paull et al. 1995, p. 232.
  45. ^ Winterer & Sager 1995, p. 518.
  46. ^ a b c Iryu & Yamada 1999, p. 477.
  47. ^ a b c Baker, Castillo & Condliffe 1995, p. 253.
  48. ^ Jenkyns, H.C.; Strasser, A. (May 1995). "Lower Cretaceous Oolites from the Mid-Pacific Mountains (Resolution Guyot, Site 866)" (PDF). Proceedings of the Ocean Drilling Program, 143 Scientific Results. Proceedings of the Ocean Drilling Program. 143. Ocean Drilling Program. p. 111. doi:10.2973/odp.proc.sr.143.211.1995. Retrieved 2018-10-08.
  49. ^ a b c Murdmaa & Kurnosov 1995, p. 459.
  50. ^ a b c d e Bralower & Mutterlose 1995, p. 33.
  51. ^ a b Iryu & Yamada 1999, p. 478.
  52. ^ Grötsch & Flügel 1992, p. 158.
  53. ^ a b c d Firth, J.V; Yancey, T.; Alvarez-Zarikian, C. (December 2006). "An 110 Ma Crocodilian-Bearing Vertebrate Assemblage Preserved Between Basalt Flows on a mid-Pacific Seamount, ODP Site 865, Allison Guyot". AGU Fall Meeting Abstracts. 2006: V13A–0651. Bibcode:2006AGUFM.V13A0651F.
  54. ^ a b c d Baker, Castillo & Condliffe 1995, p. 250.
  55. ^ a b Winterer & Sager 1995, p. 503.
  56. ^ Kurnosov et al. 1995, p. 476.
  57. ^ Baker, Castillo & Condliffe 1995, p. 251.
  58. ^ Kurnosov et al. 1995, p. 486.
  59. ^ Baker, Castillo & Condliffe 1995, p. 254.
  60. ^ Kurnosov et al. 1995, p. 479.
  61. ^ Kurnosov et al. 1995, p. 487.
  62. ^ Kurnosov et al. 1995, pp. 478–479.
  63. ^ Winterer & Sager 1995, p. 519.
  64. ^ Murdmaa & Kurnosov 1995, p. 462.
  65. ^ Murdmaa & Kurnosov 1995, p. 466.
  66. ^ Murdmaa & Kurnosov 1995, p. 467.
  67. ^ Murdmaa & Kurnosov 1995, p. 461.
  68. ^ "Claystone". Dictionary Geotechnical Engineering/Wörterbuch Geo Technik. Springer Berlin Heidelberg. 2014. p. 232. doi:10.1007/978-3-642-41714-6_32252. ISBN 9783642417139.
  69. ^ Shipboard Scientific Party 1993, p. 16.
  70. ^ Littke, Ralf; Sachsenhofer, Reinhard F. (November 1994). "Organic Petrology of Deep Sea Sediments: A Compilation of Results from the Ocean Drilling Program and the Deep Sea Drilling Project". Energy & Fuels. 8 (6): 1505. doi:10.1021/ef00048a041. ISSN 0887-0624.
  71. ^ Baudin & Sachsenhofer 1996, p. 311.
  72. ^ a b Baudin & Sachsenhofer 1996, p. 320.
  73. ^ Baudin et al. 1995, p. 189.
  74. ^ Baudin et al. 1995, p. 176.
  75. ^ a b c d Winterer & Sager 1995, p. 504.
  76. ^ Sager & Tarduno 1995, p. 402.
  77. ^ a b c d e f g Winterer & Sager 1995, p. 532.
  78. ^ Röhl & Ogg 1996, p. 608.
  79. ^ Sager & Tarduno 1995, p. 403.
  80. ^ Baudin et al. 1995, p. 191.
  81. ^ a b c Swinburne & Masse 1995, p. 9.
  82. ^ Paull et al. 1995, p. 231.
  83. ^ Winterer & Sager 1995, p. 521.
  84. ^ a b Shipboard Scientific Party 1993, p. 17.
  85. ^ a b c Sliter 1995, p. 20.
  86. ^ a b Winterer & Sager 1995, p. 525.
  87. ^ Grötsch & Flügel 1992, p. 155.
  88. ^ Grötsch & Flügel 1992, pp. 155–156.
  89. ^ Swinburne & Masse 1995, p. 3.
  90. ^ Paduan, Jennifer B.; Clague, David A.; Davis, Alicé S. (November 2007). "Erratic continental rocks on volcanic seamounts off the US west coast". Marine Geology. 246 (1): 7. Bibcode:2007MGeol.246....1P. doi:10.1016/j.margeo.2007.07.007. ISSN 0025-3227.
  91. ^ Jenkyns & Wilson 1999, p. 342.
  92. ^ Jenkyns & Wilson 1999, p. 372.
  93. ^ Sliter 1995, p. 23.
  94. ^ Winterer & Sager 1995, p. 523.
  95. ^ Winterer & Sager 1995, pp. 532–533.
  96. ^ Winterer & Sager 1995, p. 526.
  97. ^ Jenkyns & Wilson 1999, p. 373.
  98. ^ Jenkyns & Wilson 1999, p. 374.
  99. ^ a b Jenkyns & Wilson 1999, p. 375.
  100. ^ Jenkyns & Wilson 1999, p. 378.
  101. ^ Jenkyns & Wilson 1999, p. 355.
  102. ^ Graf, Gerhard (2014). "Bioturbation". Encyclopedia of Marine Geosciences. Springer Netherlands. pp. 1–2. doi:10.1007/978-94-007-6644-0_132-1. ISBN 9789400766440.
  103. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 350.
  104. ^ Bralower et al. 1995, p. 842.
  105. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 346.
  106. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 349.
  107. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 354.
  108. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 359.
  109. ^ Arreguín-Rodríguez, Alegret & Thomas 2016, p. 355.
  110. ^ Bralower & Mutterlose 1995, p. 52.

SourcesEdit