An abyssal plain is an underwater plain on the deep ocean floor, usually found at depths between 3000 and 6000 m. Lying generally between the foot of a continental rise and a mid-ocean ridge, abyssal plains cover more than 50% of the Earth’s surface. They are among the flattest, smoothest and least explored regions on Earth. Abyssal plains are key geologic elements of oceanic basins (the other elements being an elevated mid-ocean ridge and flanking abyssal hills). In addition to these elements, active oceanic basins (those that are associated with a moving plate tectonic boundary) also typically include an oceanic trench and a subduction zone.
Abyssal plains were not recognized as distinct physiographic features of the sea floor until the late 1940s and, until very recently, none had been studied on a systematic basis. They are poorly preserved in the sedimentary record, because they tend to be consumed by the subduction process. The creation of the abyssal plain is the end result of spreading of the seafloor (plate tectonics) and melting of the lower oceanic crust. Magma rises from above the asthenosphere (a layer of the upper mantle) and as this basaltic material reaches the surface at mid-ocean ridges it forms new oceanic crust. This is constantly pulled sideways by spreading of the seafloor. Abyssal plains result from the blanketing of an originally uneven surface of oceanic crust by fine-grained sediments, mainly clay and silt. Much of this sediment is deposited by turbidity currents that have been channelled from the continental margins along submarine canyons down into deeper water. The remainder of the sediment is composed chiefly of pelagic sediments. Metallic nodules are common in some areas of the plains, with varying concentrations of metals, including manganese, iron, nickel, cobalt, and copper. These nodules may provide a significant resource for future mining ventures.
Owing in part to their vast size, abyssal plains are currently believed to be a major reservoir of biodiversity. The abyss also exerts significant influence upon ocean carbon cycling, dissolution of calcium carbonate, and atmospheric CO2 concentrations over timescales of 100–1000 years. The structure and function of abyssal ecosystems are strongly influenced by the rate of flux of food to the seafloor and the composition of the material that settles. Factors such as climate change, fishing practices, and ocean fertilization are expected to have a substantial effect on patterns of primary production in the euphotic zone. This will undoubtedly impact the flux of organic material to the abyss in a similar manner and thus have a profound effect on the structure, function and diversity of abyssal ecosystems.
The ocean can be conceptualized as being divided into various zones, depending on depth, and presence or absence of sunlight. Nearly all life forms in the ocean depend on the photosynthetic activities of phytoplankton and other marine plants to convert carbon dioxide into organic carbon, which is the basic building block of organic matter. Photosynthesis in turn requires energy from sunlight to drive the chemical reactions that produce organic carbon.
The stratum of the water column nearest the surface of the ocean (sea level) is referred to as the photic zone. The photic zone can be subdivided into two different vertical regions. The uppermost portion of the photic zone, where there is adequate light to support photosynthesis by phytoplankton and plants, is referred to as the euphotic zone (also referred to as the epipelagic zone, or surface zone). The lower portion of the photic zone, where the light intensity is insufficient for photosynthesis, is called the dysphotic zone (dysphotic means "poorly lit" in Greek). The dysphotic zone is also referred to as the mesopelagic zone, or the twilight zone. Its lowermost boundary is at a thermocline of 12 °C (54 °F), which, in the tropics generally lies between 200 and 1000 metres.
The euphotic zone is somewhat arbitrarily defined as extending from the surface to the depth where the light intensity is approximately 0.1–1% of surface sunlight irradiance, depending on season, latitude and degree of water turbidity. In the clearest ocean water, the euphotic zone may extend to a depth of about 150 metres, or rarely, up to 200 metres. Dissolved substances and solid particles absorb and scatter light, and in coastal regions the high concentration of these substances causes light to be attenuated rapidly with depth. In such areas the euphotic zone may be only a few tens of metres deep or less. The dysphotic zone, where light intensity is considerably less than 1% of surface irradiance, extends from the base of the euphotic zone to about 1000 metres. Extending from the bottom of the photic zone down to the seabed is the aphotic zone, a region of perpetual darkness.
Since the average depth of the ocean is about 4300 metres, the photic zone represents only a tiny fraction of the ocean’s total volume. However, due to its capacity for photosynthesis, the photic zone has the greatest biodiversity and biomass of all oceanic zones. Nearly all primary production in the ocean occurs here. Life forms which inhabit the aphotic zone are often capable of movement upwards through the water column into the photic zone for feeding. Otherwise, they must rely on material sinking from above, or find another source of energy and nutrition, such as occurs in chemosynthetic archaea found near hydrothermal vents and cold seeps.
The aphotic zone can be subdivided into three different vertical regions, based on depth and temperature. First is the bathyal zone, extending from a depth of 1000 metres down to 3000 metres, with water temperature decreasing from 12 °C (54 °F) to 4 °C (39 °F) as depth increases. Next is the abyssal zone, extending from a depth of 3000 metres down to 6000 metres. The final zone includes the deep oceanic trenches, and is known as the hadal zone. This, the deepest oceanic zone, extends from a depth of 6000 metres down to approximately 11000 metres. Abyssal plains are typically located in the abyssal zone, at depths ranging from 3000 to 6000 metres.
The table below illustrates the classification of oceanic zones:
|Zone||Subzone (common name)||Depth of zone||Water temperature||Comments|
|photic||euphotic (epipelagic zone)||0–200 metres||highly variable|
|disphotic (mesopelagic zone, or twilight zone)||200–1000 metres||4 °C or 39 °F – highly variable|
|aphotic||bathyal||1000–3000 metres||4–12 °C or 39–54 °F|
|abyssal||3000–6000 metres||0–4 °C or 32–39 °F||water temperature may reach as high as 464 °C (867 °F) near hydrothermal vents|
|hadal||below 6000 metres||1–2.5 °C or 34–36 °F||ambient water temperature increases below 4000 metres due to adiabatic heating|
Oceanic crust, which forms the bedrock of abyssal plains, is continuously being created at mid-ocean ridges (a type of divergent boundary) by a process known as decompression melting. Plume-related decompression melting of solid mantle is responsible for creating ocean islands like the Hawaiian islands, as well as the ocean crust at mid-ocean ridges. This phenomenon is also the most common explanation for flood basalts and oceanic plateaus (two types of large igneous provinces). Decompression melting occurs when the upper mantle is partially melted into magma as it moves upwards under mid-ocean ridges. This upwelling magma then cools and solidifies by conduction and convection of heat to form new oceanic crust. Accretion occurs as mantle is added to the growing edges of a tectonic plate, usually associated with seafloor spreading. The age of oceanic crust is therefore a function of distance from the mid-ocean ridge. The youngest oceanic crust is at the mid-ocean ridges, and it becomes progressively older, cooler and denser as it migrates outwards from the mid-ocean ridges as part of the process called mantle convection.
The lithosphere, which rides atop the asthenosphere, is divided into a number of tectonic plates that are continuously being created and consumed at their opposite plate boundaries. Oceanic crust and tectonic plates are formed and move apart at mid-ocean ridges. Abyssal hills are formed by stretching of the oceanic lithosphere. Consumption or destruction of the oceanic lithosphere occurs at oceanic trenches (a type of convergent boundary, also known as a destructive plate boundary) by a process known as subduction. Oceanic trenches are found at places where the oceanic lithospheric slabs of two different plates meet, and the denser (older) slab begins to descend back into the mantle. At the consumption edge of the plate (the oceanic trench), the oceanic lithosphere has thermally contracted to become quite dense, and it sinks under its own weight in the process of subduction. The subduction process consumes older oceanic lithosphere, so oceanic crust is seldom more than 200 million years old. The overall process of repeated cycles of creation and destruction of oceanic crust is known as the Supercontinent cycle, first proposed by Canadian geophysicist and geologist John Tuzo Wilson.
New oceanic crust, closest to the mid-oceanic ridges, is mostly basalt at shallow levels and has a rugged topography. The roughness of this topography is a function of the rate at which the mid-ocean ridge is spreading (the spreading rate). Magnitudes of spreading rates vary quite significantly. Typical values for fast-spreading ridges are greater than 100 mm/yr, while slow-spreading ridges are typically less than 20 mm/yr. Studies have shown that the slower the spreading rate, the rougher the new oceanic crust will be, and vice versa. It is thought this phenomenon is due to faulting at the mid-ocean ridge when the new oceanic crust was formed. These faults pervading the oceanic crust, along with their bounding abyssal hills, are the most common tectonic and topographic features on the surface of the Earth. The process of seafloor spreading helps to explain the concept of continental drift in the theory of plate tectonics.
The flat appearance of mature abyssal plains results from the blanketing of this originally uneven surface of oceanic crust by fine-grained sediments, mainly clay and silt. Much of this sediment is deposited from turbidity currents that have been channeled from the continental margins along submarine canyons down into deeper water. The remainder of the sediment comprises chiefly dust (clay particles) blown out to sea from land, and the remains of small marine plants and animals which sink from the upper layer of the ocean, known as pelagic sediments. The total sediment deposition rate in remote areas is estimated at two to three centimeters per thousand years. Sediment-covered abyssal plains are less common in the Pacific Ocean than in other major ocean basins because sediments from turbidity currents are trapped in oceanic trenches that border the Pacific Ocean.
Abyssal plains are typcally covered by very deep sea, but during parts of the Messinian salinity crisis much of the Mediterranean Sea's abyssal plain was exposed to air as an empty hot dry salt-floored sink.
The landmark scientific expedition (December 1872 – May 1876) of the British Royal Navy survey ship HMS Challenger yielded a tremendous amount of bathymetric data, much of which has been confirmed by subsequent researchers. Bathymetric data obtained during the course of the Challenger expedition enabled scientists to draw maps, which provided a rough outline of certain major submarine terrain features, such as the edge of the continental shelves and the Mid-Atlantic Ridge. This discontinuous set of data points was obtained by the simple technique of taking soundings by lowering long lines from the ship to the seabed.
The Challenger expedition was followed by the 1879–1881 expedition of the Jeannette, led by United States Navy Lieutenant George Washington DeLong. The team sailed across the Chukchi Sea and recorded meteorological and astronomical data in addition to taking soundings of the seabed. The ship became trapped in the ice pack near Wrangel Island in September 1879, and was ultimately crushed and sunk in June 1881.
The Jeannette expedition was followed by the 1893–1896 Arctic expedition of Norwegian explorer Fridtjof Nansen aboard the Fram, which proved that the Arctic Ocean was a deep oceanic basin, uninterrupted by any significant land masses north of the Eurasian continent. 
Beginning in 1916, Canadian physicist Robert William Boyle and other scientists of the Anti-Submarine Detection Investigation Committee (ASDIC) undertook research which ultimately led to the development of sonar technology. Acoustic sounding equipment was developed which could be operated much more rapidly than the sounding lines, thus enabling the German Meteor expedition aboard the German research vessel Meteor (1925–27) to take frequent soundings on east-west Atlantic transects. Maps produced from these techniques show the major Atlantic basins, but the depth precision of these early instruments was not sufficient to reveal the flat featureless abyssal plains.
As technology improved, measurement of depth, latitude and longitude became more precise and it became possible to collect more or less continuous sets of data points. This allowed researchers to draw accurate and detailed maps of large areas of the ocean floor. Use of a continuously recording fathometer enabled Tolstoy & Ewing in the summer of 1947 to identify and describe the first abyssal plain. This plain, located to the south of Newfoundland, is now known as the Sohm Abyssal Plain. Following this discovery many other examples were found in all the oceans.
The Challenger Deep is the deepest surveyed point of all of Earth's oceans; it is located at the southern end of the Mariana Trench near the Mariana Islands group. The depression is named after HMS Challenger, whose researchers made the first recordings of its depth on 23 March 1875 at station 225. The reported depth was 4,475 fathoms (8184 meters) based on two separate soundings. On 1 June 2009, sonar mapping of the Challenger Deep by the Simrad EM120 multibeam sonar bathymetry system aboard the R/V Kilo Moana indicated a maximum depth of 10971 meters (6.82 miles). The sonar system uses phase and amplitude bottom detection, with an accuracy of better than 0.2% of water depth (this is an error of about 22 meters at this depth).
A rare but important terrain feature found in the abyssal and hadal zones is the hydrothermal vent. In contrast to the approximately 2 °C ambient water temperature at these depths, water emerges from these vents at temperatures ranging from 60 °C up to as high as 464 °C. Due to the high barometric pressure at these depths, water may exist in either its liquid form or as a supercritical fluid at such temperatures.
At a barometric pressure of 218 atmospheres, the critical point of water is 375 °C. At a depth of 3,000 meters, the barometric pressure of sea water is more than 300 atmospheres (as salt water is denser than fresh water). At this depth and pressure, seawater becomes supercritical at a temperature of 407 °C (see image). However the increase in salinity at this depth pushes the water closer to its critical point. Thus, water emerging from the hottest parts of some hydrothermal vents, black smokers and submarine volcanoes can be a supercritical fluid, possessing physical properties between those of a gas and those of a liquid.
Sister Peak (Comfortless Cove Hydrothermal Field, Ascension Island. They are presumed to have been active since an earthquake shook the region in 2002. These vents have been observed to vent phase-separated, vapor-type fluids. In 2008, sustained exit temperatures of up to 407 °C were recorded at one of these vents, with a peak recorded temperature of up to 464 °C. These thermodynamic conditions exceed the critical point of seawater, and are the highest temperatures recorded to date from the seafloor. This is the first reported evidence for direct magmatic-hydrothermal interaction on a slow-spreading mid-ocean ridge., elevation −2996 m), Shrimp Farm and Mephisto (Red Lion Hydrothermal Field, , elevation −3047 m), are three hydrothermal vents of the black smoker category, located on the Mid-Atlantic Ridge near
Another unusual feature found in the abyssal and hadal zones is the cold seep, sometimes called a cold vent. This is an area of the seabed where seepage of hydrogen sulfide, methane and other hydrocarbon-rich fluid occurs, often in the form of a deep-sea brine pool. The first cold seeps were discovered in 1983, at a depth of 3200 meters in the Gulf of Mexico. Since then, cold seeps have been discovered in many other areas of the World Ocean, including the Monterey Submarine Canyon just off Monterey Bay, California, the Sea of Japan, off the Pacific coast of Costa Rica, off the Atlantic coast of Africa, off the coast of Alaska, and under an ice shelf in Antarctica.
Though the plains were once assumed to be vast, desert-like habitats, research over the past decade or so shows that they teem with a wide variety of microbial life. However, ecosystem structure and function at the deep seafloor have historically been very poorly studied because of the size and remoteness of the abyss. Recent oceanographic expeditions conducted by an international group of scientists from the Census of Diversity of Abyssal Marine Life (CeDAMar) have found an extremely high level of biodiversity on abyssal plains, with up to 2000 species of bacteria, 250 species of protozoans, and 500 species of invertebrates (worms, crustaceans and molluscs), typically found at single abyssal sites. New species make up more than 80% of the thousands of seafloor invertebrate species collected at any abyssal station, highlighting our heretofore poor understanding of abyssal diversity and evolution. Richer biodiversity is associated with areas of known phytodetritus input and higher organic carbon flux.
Abyssobrotula galatheae, a species of cusk eel in the family Ophidiidae, is among the deepest-living species of fish. In 1970, one specimen was trawled from a depth of 8370 meters in the Puerto Rico Trench. The animal was dead, however, upon arrival at the surface. In 2008, the hadal snailfish (Pseudoliparis amblystomopsis) was observed and recorded at a depth of 7700 meters in the Japan Trench. These are, to date, the deepest living fish ever recorded. Other fish of the abyssal zone include the fishes of the Ipnopidae family, which includes the abyssal spiderfish (Bathypterois longipes), tripodfish (Bathypterois grallator), feeler fish (Bathypterois longifilis), and the black lizardfish (Bathysauropsis gracilis). Some members of this family have been recorded from depths of more than 6000 meters.
CeDAMar scientists have demonstrated that some abyssal and hadal species have a cosmopolitan distribution. One example of this would be protozoan foraminiferans, certain species of which are distributed from the Arctic to the Antarctic. Other faunal groups, such as the polychaete worms and isopod crustaceans, appear to be endemic to certain specific plains and basins. Many apparently unique taxa of nematode worms have also been recently discovered on abyssal plains. This suggests that the very deep ocean has fostered adaptive radiations. The taxonomic composition of the nematode fauna in the abyssal Pacific is similar, but not identical to, that of the North Atlantic. A list of some of the species that have been discovered or redescribed by CeDAMar can be found here.
Eleven of the 31 described species of Monoplacophora (a class of mollusks) live below 2000 meters. Of these 11 species, two live exclusively in the hadal zone. The greatest number of monoplacophorans are from the eastern Pacific Ocean along the oceanic trenches. However, no abyssal monoplacophorans have yet been found in the Western Pacific and only one abyssal species has been identified in the Indian Ocean. Of the 922 known species of chitons (from the Polyplacophora class of mollusks), 22 species (2.4%) are reported to live below 2000 meters and two of them are restricted to the abyssal plain. Although genetic studies are lacking, at least six of these species are thought to be eurybathic (capable of living in a wide range of depths), having been reported as occurring from the sublittoral to abyssal depths. A large number of the polyplacophorans from great depths are herbivorous or xylophagous, which could explain the difference between the distribution of monoplacophorans and polyplacophorans in the world's oceans.
Peracarid crustaceans, including isopods, are known to form a significant part of the macrobenthic community that is responsible for scavenging on large food falls onto the sea floor. In 2000, scientists of the Diversity of the deep Atlantic benthos (DIVA 1) expedition (cruise M48/1 of the German research vessel RV Meteor III) discovered and collected three new species of the Asellota suborder of benthic isopods from the abyssal plains of the Angola Basin in the South Atlantic Ocean. In 2003, De Broyer et al. collected some 68,000 peracarid crustaceans from 62 species from baited traps deployed in the Weddell Sea, Scotia Sea, and off the South Shetland Islands. They found that about 98% of the specimens belonged to the amphipod superfamily Lysianassoidea, and 2% to the isopod family Cirolanidae. Half of these species were collected from depths of greater than 1000 meters.
In 2005, the Japan Agency for Marine-Earth Science and Technology (JAMSTEC) remotely operated vehicle, KAIKO, collected sediment core from the Challenger Deep. 432 living specimens of soft-walled foraminifera were identified in the sediment samples. Foraminifera are single-celled protists that construct shells. There are an estimated 4,000 species of living foraminifera. Out of the 432 organisms collected, the overwhelming majority of the sample consisted of simple, soft-shelled foraminifera, with others representing species of the complex, multi-chambered genera Leptohalysis and Reophax. Overall, 85% of the specimens consisted of soft-shelled allogromids. This is unusual compared to samples of sediment-dwelling organisms from other deep-sea environments, where the percentage of organic-walled foraminifera ranges from 5% to 20% of the total. Small organisms with hard calculated shells have trouble growing at extreme depths because the water at that depth is severely lacking in calcium carbonate.
While similar lifeforms have been known to exist in shallower oceanic trenches (>7,000 m) and on the abyssal plain, the lifeforms discovered in the Challenger Deep may represent independent taxa from those shallower ecosystems. This preponderance of soft-shelled organisms at the Challenger Deep may be a result of selection pressure. Millions of years ago, the Challenger Deep was shallower than it is now. Over the past six to nine million years, as the Challenger Deep grew to its present depth, many of the species present in the sediment of that ancient biosphere were unable to adapt to the increasing water pressure and changing environment. Those species that were able to adapt may have been the ancestors of the organisms currently endemic to the Challenger Deep.
Polychaetes occur throughout the Earth's oceans at all depths, from forms that live as plankton near the surface, to the deepest oceanic trenches. The robot ocean probe Nereus observed a 2–3 cm specimen (still unclassified) of polychaete at the bottom of the Challenger Deep on 31 May 2009. There are more than 10,000 described species of polychaetes; they can be found in nearly every marine environment. Some species live in the coldest ocean temperatures of the hadal zone, while others can be found in the extremely hot waters adjacent to hydrothermal vents.
Within the abyssal and hadal zones, the areas around submarine hydrothermal vents and cold seeps have by far the greatest biomass and biodiversity per unit area. Fueled by the chemicals dissolved in the vent fluids, these areas are often home to large and diverse communities of thermophilic, halophilic and other extremophilic prokaryotic microorganisms (such as those of the sulfide-oxidizing Beggiatoa genus), often arranged in large bacterial mats near cold seeps. In these locations, chemosynthetic archaea and bacteria typically form the base of the food chain. Although the process of chemosynthesis is entirely microbial, these chemosynthetic microorganisms often support vast ecosystems consisting of complex multicellular organisms through symbiosis. These communities are characterized by species such as vesicomyid clams, mytilid mussels, limpets, isopods, giant tube worms, soft corals, eelpouts, galatheid crabs, and alvinocarid shrimp. The deepest seep community discovered thus far is located in the Japan Trench, at a depth of 7700 meters.
Probably the most important ecological characteristic of abyssal ecosystems is energy limitation. Abyssal seafloor communities are considered to be food limited because benthic production depends on the input of detrital organic material produced in the euphotic zone, thousands of meters above. Most of the organic flux arrives as an attenuated rain of small particles (typically, only 0.5–2% of net primary production in the euphotic zone), which decreases inversely with water depth. The small particle flux can be augmented by the fall of larger carcasses and downslope transport of organic material near continental margins.
Exploitation of resources
In addition to their high biodiversity, abyssal plains are of great current and future commercial and strategic interest. For example, they may be used for the legal and illegal disposal of large structures such as ships and oil rigs, radioactive waste and other hazardous waste, such as munitions. They may also be attractive sites for deep-sea fishing, and extraction of oil and gas and other minerals. Future deep-sea waste disposal activities that could be significant by 2025 include emplacement of sewage and sludge, carbon-dioxide sequestration, and disposal of dredge spoils.
As fish stocks dwindle in the upper ocean, deep-sea fisheries are increasingly being targeted for exploitation. Because deep sea fish are long-lived and slow growing, these deep-sea fisheries are not thought to be sustainable in the long term given current management practices. Changes in primary production in the photic zone are expected to alter the standing stocks in the food-limited aphotic zone.
Hydrocarbon exploration in deep water occasionally results in significant environmental degradation resulting mainly from accumulation of contaminated drill cuttings, but also from oil spills. While the oil gusher involved in the Deepwater Horizon oil spill in the Gulf of Mexico originates from a wellhead only 1500 meters below the ocean surface, it nevertheless illustrates the kind of environmental disaster that can result from mishaps related to offshore drilling for oil and gas.
Sediments of certain abyssal plains contain abundant mineral resources, notably polymetallic nodules. These potato-sized concretions of manganese, iron, nickel, cobalt, and copper, distributed on the seafloor at depths of greater than 4000 meters, are of significant commercial interest. The area of maximum commercial interest for polymetallic nodule mining (called the Pacific nodule province) lies in international waters of the Pacific Ocean, stretching from 118°–157°, and from 9°–16°N, an area of more than 3 million km². The abyssal Clarion-Clipperton Fracture Zone (CCFZ) is an area within the Pacific nodule province that is currently under exploration for its mineral potential.
Eight commercial contractors are currently licensed by the International Seabed Authority (an intergovernmental organization established to organize and control all mineral-related activities in the international seabed area beyond the limits of national jurisdiction) to explore nodule resources and to test mining techniques in eight claim areas, each covering 150,000 km². When mining ultimately begins, each mining operation is projected to directly disrupt 300–800 km² of seafloor per year and disturb the benthic fauna over an area 5–10 times that size due to redeposition of suspended sediments. Thus, over the 15-year projected duration of a single mining operation, nodule mining might severely damage abyssal seafloor communities over areas of 20,000 to 45,000 km² (a zone at least the size of Massachusetts).
Limited knowledge of the taxonomy, biogeography and natural history of deep sea communities prevents accurate assessment of the risk of species extinctions from large-scale mining. Data acquired from the abyssal North Pacific and North Atlantic suggest that deep-sea ecosystems may be adversely affected by mining operations on decadal time scales. In 1978, a dredge aboard the Hughes Glomar Explorer, operated by the American mining consortium Ocean Minerals Company (OMCO), made a mining track at a depth of 5000 meters in the nodule fields of the CCFZ. In 2004, the French Research Institute for Exploitation of the Sea (IFREMER) conducted the Nodinaut expedition to this mining track (which is still visible on the seabed) to study the long-term effects of this physical disturbance on the sediment and its benthic fauna. Samples taken of the superficial sediment revealed that its physical and chemical properties had not shown any recovery since the disturbance made 26 years earlier. On the other hand, the biological activity measured in the track by instruments aboard the manned submersible bathyscaphe Nautile did not differ from a nearby unperturbed site. This data suggests that the benthic fauna and nutrient fluxes at the water–sediment interface has fully recovered.
List of abyssal plains
- List of oceanic landforms
- List of submarine topographical features
- Oceanic basin
- Oceanic plateau
- Oceanic ridge
- Oceanic trench
- Physical oceanography
- Craig R. Smith, Fabio C. De Leo, Angelo F. Bernardino, Andrew K. Sweetman, and Pedro Martinez Arbizu (2008). "Abyssal food limitation, ecosystem structure and climate change" (PDF). Trends in Ecology and Evolution 23 (9): 518–528. doi:10.1016/j.tree.2008.05.002. PMID 18584909. Retrieved 18 June 2010.
- N.G. Vinogradova (1997). "Zoogeography of the Abyssal and Hadal Zones". Advances in Marine Biology. Advances in Marine Biology 32: 325–387. doi:10.1016/S0065-2881(08)60019-X. ISBN 9780120261321.
- P.P.E. Weaver; J. Thomson; P. M. Hunter (1987). Geology and Geochemistry of Abyssal Plains (PDF). Oxford: Blackwell Scientific Publications. p. x. ISBN 0-632-01744-9. Retrieved 18 June 2010.
- Smith 2008, p. 5
- K.L. Smith, Jr, H.A. Ruhl, B.J. Bett, D.S.M. Billett, R.S. Lampitt & R.S. Kaufmann (17 November 2009). "Climate, carbon cycling, and deep-ocean ecosystems". PNAS 106 (46): 19211–19218. Bibcode:2009PNAS..10619211S. doi:10.1073/pnas.0908322106. PMC 2780780. PMID 19901326.
- Csirke 1997, p. 4.
- Encyclopædia Britannica (2010). "Photic zone". Encyclopædia Britannica Online. Retrieved 18 June 2010.
- Jeananda Col (2004). "Twilight Ocean (Disphotic) Zone". EnchantedLearning.com. Retrieved 18 June 2010.
- Ken O. Buesseler, Carl H. Lamborg, Philip W. Boyd, Phoebe J. Lam et al. (27 April 2007). "Revisiting Carbon Flux Through the Ocean's Twilight Zone". Science 316 (5824): 567–570. Bibcode:2007Sci...316..567B. doi:10.1126/science.1137959. PMID 17463282.
- National Oceanic and Atmospheric Administration (2 December 2008). "How deep is the ocean?". Washington, DC: National Oceanic and Atmospheric Administration. Archived from the original on 23 June 2010. Retrieved 19 June 2010.
- Rebecca Morelle (7 October 2008). "'Deepest ever' living fish filmed". BBC News. Archived from the original on 30 July 2010. Retrieved 18 June 2010.
- Haase, K. M. et al. (13 November 2007). "Young volcanism and related hydrothermal activity at 5°S on the slow-spreading southern Mid-Atlantic Ridge". Geochem. Geophys. Geosyst. 8 (Q11002): 17. Bibcode:2007GGG.....811002H. doi:10.1029/2006GC001509. Retrieved 18 June 2010.
- Andrea Koschinsky, Dieter Garbe-Schönberg, Sylvia Sander, Katja Schmidt, Hans-Hermann Gennerich and Harald Strauss (August 2008). "Hydrothermal venting at pressure-temperature conditions above the critical point of seawater, 5°S on the Mid-Atlantic Ridge". Geology 36 (8): 615–618. doi:10.1130/G24726A.1.
- Catherine Brahic (4 August 2008). "Found: The hottest water on Earth". New Scientist. Retrieved 18 June 2010.
- Josh Hill (5 August 2008). "'Extreme Water' Found at Atlantic Ocean Abyss". The Daily Galaxy. Retrieved 18 June 2010.
- Karsten M. Haase, Sven Petersen, Andrea Koschinsky, Richard Seifert, Colin W. Devey et al. (2009). "Fluid compositions and mineralogy of precipitates from Mid Atlantic Ridge hydrothermal vents at 4°48'S". Germany: Publishing Network for Geoscientific & Environmental Data (PANGAEA). doi:10.1594/PANGAEA.727454.
- Alan J. Jamieson, Toyonobu Fujii, Daniel J. Mayor, Martin Solan and Imants G. Priede (March 2010). "Hadal trenches: the ecology of the deepest places on Earth" (PDF). Trends in Ecology and Evolution 25 (3): 190–197. doi:10.1016/j.tree.2009.09.009. PMID 19846236. Retrieved 18 June 2010.
- Center for Marine Biodiversity and Conservation. "The Hadal Zone: Deep-sea Trenches" (PDF). University of California, San Diego: Scripps Institution of Oceanography. Retrieved 18 June 2010.
- Marjorie Wilson (1993). Igneous petrogenesis. London: Chapman & Hall. ISBN 978-0-412-53310-5.
- R.S. WHITE, T.A. MINSHULL, M.J. BICKLE and C.J. ROBINSON (2001). "Melt Generation at Very Slow-Spreading Oceanic Ridges: Constraints from Geochemical and Geophysical Data". Journal of Petrology 42 (6): 1171–1196. doi:10.1093/petrology/42.6.1171.
- Geoff C. Brown, C. J. Hawkesworth, R. C. L. Wilson (1992). Understanding the Earth (2nd ed.). Cambridge University Press. p. 93. ISBN 0-521-42740-1.
- Condie 1997, p. 50.
- Kobes, Randy and Kunstatter, Gabor.Mantle Convection. Physics Department, University of Winnipeg. Retrieved 23 June 2010.
- W. Roger Buck & Alexei N. B. Poliakov (19 March 1998). "Abyssal hills formed by stretching oceanic lithosphere". Nature 392 (6673): 272–275. Bibcode:1998Natur.392..272B. doi:10.1038/32636.
- Condie 1997, p. 83.
- Gerald Schubert, Donald Lawson Turcotte, Peter Olson (2001). "Chapter 2: Plate tectonics". Mantle convection in the earth and planets. Cambridge University Press. p. 16 ff. ISBN 0-521-79836-1.
- Deep Sea Drilling Project (2010). "About the Deep Sea Drilling Project". Texas A&M University, College Station, Texas: Deep Sea Drilling Project. Retrieved 24 June 2010.
- Christopher Small and David T. Sandwell (10 March 1992). "An analysis of ridge axis gravity roughness and spreading rate" (PDF). Journal of Geophysical Research 97 (B3): 3235–3245. Bibcode:1992JGR....97.3235S. doi:10.1029/91JB02465. Retrieved 23 June 2010.
- W. Roger Buck, Luc L. Lavier & Alexei N.B. Poliakov (7 April 2005). "Modes of faulting at mid-ocean ridges". Nature 434 (7034): 719–723. Bibcode:2005Natur.434..719B. doi:10.1038/nature03358. PMID 15815620.
- Philip Henry Kuenen (August 1946). "Rate and mass of deep-sea sedimentation". American Journal of Science 244 (8): 563–572. doi:10.2475/ajs.244.8.563.
- T.A. Davies and A.S. Laughton (1972). "Chapter 11. Sedimentary Processes in the North Atlantic". In Laughton, A. S., Berggren, W. A. et al. Initial Reports of the Deep Sea Drilling Project, Volume XII (covering Leg 12 of the cruises of the Drilling Vessel Glomar Challenger) (PDF). Washington, D.C.: U.S. Government Printing Office. p. 915. doi:10.2973/dsdp.proc.12.111.1972. ISSN 1936-7392. Retrieved 24 June 2010.
- Michael B. Underwood and Charles R. Norville (May 1986). "Deposition of sand in a trench-slope basin by unconfined turbidity currents". Marine Geology 71 (3–4): 383–392. doi:10.1016/0025-3227(86)90080-0.
- Krijgsman W; Garcés M; Langereis CG; Daams R; Van Dam J et al. (1996). "A new chronology for the middle to late Miocene continental record in Spain". Earth and Planetary Science Letters 142 (3–4): 367–380. Bibcode:1996E&PSL.142..367K. doi:10.1016/0012-821X(96)00109-4.
- Clauzon G, Suc JP, Gautier F, Berger A, Loutre MF (1996). "Alternate interpretation of the Messinian salinity crisis: Controversy resolved?". Geology 24 (4): 363–6. Bibcode:1996Geo....24..363C. doi:10.1130/0091-7613(1996)024<0363:AIOTMS>2.3.CO;2.
- van Dijk JP, Barberis A, Cantarella G, and Massa E (1998). "Central Mediterranean Messinian basin evolution. Tectono-eustasy or eustato-tectonics?". Annales Tectonicae 12 (1–2): 7–27.
- Bachea F, Olivet JL, Gorini C, Rabineaua M, Baztan J et al. (2009). "Messinian erosional and salinity crises: View from the Provence Basin (Gulf of Lions, Western Mediterranean)" (PDF). Earth and Planetary Science Letters 286 (1–2): 139–57. Bibcode:2009E&PSL.286..139B. doi:10.1016/j.epsl.2009.06.021. Retrieved 1 October 2010.
- John Murray & Rev. A.F. Renard (1891). Report of the scientific results of the voyage of H.M.S. Challenger during the years 1873 to 1876. London: Her Majesty's Stationery Office. Retrieved 26 June 2010.[page needed]
- Naval Historical Center (1977) [First published in 1968]. "Jeannette". In James L. Mooney. Dictionary of American Naval Fighting Ships, Volume 3, G-K. Washington DC: Defense Department, Department of the Navy, Naval History Division. ISBN 0-16-002019-0. OCLC 2794587. Archived from the original on 8 July 2010. Retrieved 26 June 2010.
- James S. Aber (2006). "History of Geology: Fridtjof Nansen". Emporia, Kansas: Emporia State University. Retrieved 26 June 2010.
- Krishfield, Rick. "Nansen and the Drift of the Fram (1893–1896)". Beaufort Gyre Exploration Project. Woods Hole Oceanographic Institution. Retrieved 26 June 2010.
- Hans Maurer & Theodor Stocks (May–June 1933). "Die Echolotengen des 'Meteor' Deutschen Atlantischen Exped. Meteor, 1925–1927". Wissenschaftliche Ergebnisse (Blackwell Publishing) 2 (5): 1–309. JSTOR 1786634.
- Theodor Stocks & Georg Wust (1935). "Die Tiefenverhaltnisse des offenen Atlantischen Ozeans: Deutsche Atlantischen Exped. Meteor, 1925–1927". Wissenschaftliche Ergebnisse 3: 1–31. Retrieved 26 June 2010.
- Ivan Tolstoy & Maurice Ewing (October 1949). "North Atlantic hydrography and the mid-Atlantic Ridge". Geological Society of America Bulletin 60 (10): 1527–40. Bibcode:1949GSAB...60.1527T. doi:10.1130/0016-7606(1949)60[1527:NAHATM]2.0.CO;2. ISSN 0016-7606.
- Bruce C. Heezen, Maurice Ewing and D.B. Ericson (December 1951). "Submarine topography in the North Atlantic". Geological Society of America Bulletin 62 (12): 1407–1417. Bibcode:1951GSAB...62.1407H. doi:10.1130/0016-7606(1951)62[1407:STITNA]2.0.CO;2. ISSN 0016-7606.
- Bruce C. Heezen, D.B. Ericson and Maurice Ewing (July 1954). "Further evidence for a turbidity current following the 1929 Grand banks earthquake". Deep Sea Research 1 (4): 193–202. Bibcode:1954DSR.....1..193H. doi:10.1016/0146-6313(54)90001-5.
- F.F. Koczy (1954). "A survey on deep-sea features taken during the Swedish deep-sea expedition". Deep Sea Research 1 (3): 176–184. Bibcode:1954DSR.....1..176K. doi:10.1016/0146-6313(54)90047-7.
- Bruce C. Heezen, Marie Tharp, and Maurice Ewing (1962). "The Floors of the Oceans. I. The North Atlantic. Text to Accompany the Physiographic Diagram of the North Atlantic". In H. Caspers. Internationale Revue der gesamten Hydrobiologie und Hydrographie 47 (3). Weinheim: WILEY-VCH Verlag GmbH & Company. p. 487. doi:10.1002/iroh.19620470311.
- Bruce C. Heezen & A.S. Laughton (1963). "Abyssal plains". In M.N. Hill. The Sea 3. New York: Wiley-Interscience. pp. 312–64.
- University of Hawaii Marine Center (4 June 2009). "Daily Reports for R/V KILO MOANA June & July 2009". Honolulu, Hawaii: University of Hawaii. Retrieved 26 June 2010.
- University of Hawaii Marine Center (4 June 2009). "Inventory of Scientific Equipment aboard the R/V KILO MOANA". Honolulu, Hawaii: University of Hawaii. Retrieved 26 June 2010.
- Paull, C. K.; Hecker, B.; Commeau, R.; Freeman-Lynde, R. P.; Neumann, C.; Corso, W. P.; Golubic, S.; Hook, J. E.; Sikes, E.; Curray, J. (23 November 1984). "Biological communities at the Florida Escarpment resemble hydrothermal vent taxa". Science 226 (4677): 965–967. Bibcode:1984Sci...226..965P. doi:10.1126/science.226.4677.965. PMID 17737352.
- Caitlyn H. Kennedy (26 July 2007). "Demise of Antarctic Ice Shelf Reveals New Life". National Science Foundation. Retrieved 19 June 2010.
- Frank Scheckenbach, Klaus Hausmann, Claudia Wylezich, Markus Weitere and Hartmut Arndt (5 January 2010). "Large-scale patterns in biodiversity of microbial eukaryotes from the abyssal sea floor". Proceedings of the National Academy of Sciences 107 (1): 115–120. Bibcode:2010PNAS..107..115S. doi:10.1073/pnas.0908816106. PMC 2806785. PMID 20007768.
- Jørgensen BB, Boetius A. (October 2007). "Feast and famine—microbial life in the deep-sea bed". Nature Reviews Microbiology 5 (10): 770–81. doi:10.1038/nrmicro1745. PMID 17828281.
- Census of Diversity of Abyssal Marine Life (CeDAMar). "Abstract and Bio: Census of the Diversity of Abyssal Marine Life (Dr. Craig Smith)". Office of Ocean Exploration & Research, National Oceanic and Atmospheric Administration. Retrieved 26 June 2010.
- Glover, A.G., Smith, C.R., Paterson, G.L.J., Wilson, G.D.F., Hawkins, L. and Sheader, M. (2002). "Polychaete species diversity in the central Pacific abyss: local and regional patterns and relationships with productivity". Marine Ecology – Progress Series 240: 157–170. doi:10.3354/meps240157.
- Pedro Martínez Arbizu and Horst Kurt Schminke (18 February 2005). "DIVA-1 expedition to the deep sea of the Angola Basin in 2000 and DIVA-1 workshop 2003". Organisms Diversity & Evolution 5 (Supplement 1): 1–2. doi:10.1016/j.ode.2004.11.009.
- Paul V.R. Snelgrove & Craig R. Smith (2002). "A riot of species in an environmental calm: the paradox of the species-rich deep-sea floor". Oceanography and Marine Biology Annual Review 40: 311–342. INIST:14868518.
- P John D Lambshead, Caroline J Brown, Timothy J Ferrero, Lawrence E Hawkins, Craig R Smith and Nicola J Mitchell (9 January 2003). "Biodiversity of nematode assemblages from the region of the Clarion-Clipperton Fracture Zone, an area of commercial mining interest". BMC Ecol 3: 1. doi:10.1186/1472-6785-3-1. PMC 140317. PMID 12519466. Retrieved 19 June 2010.
- Ellis, R. (1996). Deep Atlantic: Life, Death, and Exploration in the Abyss. New York: Alfred A. Knopf, Inc. ISBN 1-55821-663-4.
- Froese, Rainer and Pauly, Daniel, eds. (2006). "Abyssobrotula galatheae" in FishBase. April 2006 version.
- Nielsen, J.G. (1977). "The deepest living fish Abyssobrotula galatheae: a new genus and species of oviparous ophidioids (Pisces, Brotulidae)". Galathea Report 14: 41–48.
- Froese, Rainer and Pauly, Daniel, eds. (2006). "Pseudoliparis amblystomopsis" in FishBase. April 2006 version.
- Elizabeth Keller (2010). "Deepest Fish: Snailfish (Pseudoliparis amblystomopsis)". Archived from the original on 28 June 2010. Retrieved 26 June 2010.
- Mark McGrouther (22 April 2010). "Spiderfishes, Bathypterois spp". Sydney, NSW: Australian Museum. Retrieved 26 June 2010.
- K. Akimoto, M. Hattori, K. Uematsu and C. Kato (May 2001). "The deepest living foraminifera, Challenger Deep, Mariana Trench". Marine Micropaleontology 42 (1–2): 95–97. doi:10.1016/S0377-8398(01)00012-3.
- Enrico Schwab (2008). "A summary of reports of abyssal and hadal Monoplacophora and Polyplacophora (Mollusca)". In Pedro Martinez Arbizu & Saskia Brix. Bringing light into deep-sea biodiversity (Zootaxa 1866) (PDF). Auckland, New Zealand: Magnolia Press. pp. 205–222. ISBN 978-1-86977-260-4. Retrieved 26 June 2010.
- De Broyer, C., Nyssen, F. & P. Dauby (July–August 2004). "The crustacean scavenger guild in Antarctic shelf, bathyal and abyssal communities". Deep Sea Research Part II: Topical Studies in Oceanography 51 (14–16): 1733–1752. Bibcode:2004DSR....51.1733D. doi:10.1016/j.dsr2.2004.06.032.
- Mursch 2008, pp. 493–539.
- Schmid, C., Brenke, N. & J.W. Wägele (2002). "On abyssal isopods (Crustacea: Isopoda: Asellota) from the Angola Basin: Eurycope tumidicarpus n.sp. and redescription of Acanthocope galathea Wolff, 1962". Organisms, Diversity & Evolution 2 (1): 87–88. doi:10.1078/1439-6092-00030.
- J.K. Lowry (2 October 1999). "Crustacea, the Higher Taxa: Description, Identification, and Information Retrieval (Asellota)". Australian Museum. Retrieved 26 June 2010.
- Yuko Todo, Hiroshi Kitazato, Jun Hashimoto, Andrew J. Gooday (4 February 2005). "Simple Foraminifera Flourish at the Ocean's Deepest Point". Science 307 (5710): 689. doi:10.1126/science.1105407. PMID 15692042.
- John Roach (3 February 2005). "Life Is Found Thriving at Ocean's Deepest Point". National Geographic News. Retrieved 26 June 2010.
- Karl K. Turekian, J. Kirk Cochran, D.P. Kharkar, Robert M. Cerrato, J. Rimas Vaisnys, Howard L. Sanders, J. Frederick Grassle, and John A. Allen (July 1975). "Slow growth rate of a deep-sea clam determined by 228Ra chronology". Proceedings of the National Academy of Sciences of the United States of America 72 (7): 2829–2832. Bibcode:1975PNAS...72.2829T. doi:10.1073/pnas.72.7.2829. PMC 432865. PMID 1058499.
- Bernice Santiago (15 June 2009). "Robotic vehicle explores Challenger Deep". Guam Pacific Daily News, Hagatna, Guam. Retrieved 26 June 2010.
- Lonny Lippsett, Amy E. Nevala (4 June 2009). "Nereus Soars to the Ocean's Deepest Trench". Oceanus Magazine. Archived from the original on 1 June 2010. Retrieved 26 June 2010.
- WHOI Media Relations (2 June 2009). "Hybrid Remotely Operated Vehicle "Nereus" Reaches Deepest Part of the Ocean". Woods Hole Oceanographic Institution. Retrieved 26 June 2010.
- Minerals Management Service, Gulf of Mexico OCS Region (November 2006). "Chapters 3: DESCRIPTION OF THE AFFECTED ENVIRONMENT". In Chris C. Oynes. Gulf of Mexico OCS Oil and Gas Lease Sales: 2007–2012. Western Planning Area Sales 204, 207, 210, 215, and 218. Central Planning Area Sales 205, 206, 208, 213, 216, and 222. Draft Environmental Impact Statement. Volume I (PDF). New Orleans: United States Department of the Interior, Minerals Management Service, Gulf of Mexico OCS Region. pp. 3–27–3–31. Retrieved 20 June 2010.
- Smith, C.R. and Demoupolos, A.W.J. (2003) Ecology of the Pacific ocean floor. In: Ecosystems of the World (Tyler, P.A., ed.), pp. 179–218, Elsevier
- Adrian G. Glover and Craig R. Smith (2003). "The deep-sea floor ecosystem: current status and prospects of anthropogenic change by the year 2025". Environmental Conservation 30 (3): 219–241. doi:10.1017/S0376892903000225.
- Macdonald, Ian R.; John Amos, Timothy Crone and Steve Wereley (21 May 2010). "The Measure of an Oil Disaster". The New York Times. Archived from the original on 26 May 2010. Retrieved 18 June 2010.
- Smith 2008, p. 4
- Alexis Khripounoff, Jean-Claude Caprais, Philippe Crassous and Joël Etoubleau (1 September 2006). "Geochemical and Biological Recovery of the Disturbed Seafloor in Polymetallic Nodule Fields of the Clipperton-Clarion Fracture Zone (CCFZ) at 5,000-m Depth" (PDF). Limnology and Oceanography 51 (5): 2033–2041. doi:10.4319/lo.2006.51.5.2033. Retrieved 19 June 2010.
- Böggemann M. & Purschke G. (2005). "Abyssal benthic Syllidae (Annelida: Polychaeta) from the Angola Basin". Organisms, Diversity & Evolution 5 (Supplement 1): 221–226. doi:10.1016/j.ode.2004.11.006.
- Bohn, J.M. (2005). "On two rare abyssal Myriotrochidae (Echinodermata: Holothuroidea: Apodida) new to the South Atlantic: Siniotrochus myriodontus Gage and Billet, 1986 and Lepidotrochus parvidiscus angolensis subsp. nov". Organisms, Diversity & Evolution 5 (Supplement 1): 231–238. doi:10.1016/j.ode.2004.11.008.
- Brandt A., Brenke N., Andres H.-G., Brix S., Guerrero-Kommritz J., Mühlenhardt-Siegel U., & Wägele J.-W. (2005). "Diversity of peracarid crustaceans (Malacostraca) from the abyssal plain of the Angola Basin". Organisms, Diversity and Evolution 5: 105–112. doi:10.1016/j.ode.2004.10.007.
- Condie, Kent C. (1997). Plate Tectonics and Crustal Evolution. Boston: Butterworth-Heinemann Ltd. ISBN 0-7506-3386-7. Retrieved 23 June 2010.
- Csirke, Jorge (1997). "II. The Limits of Marine Productivity". In Laws, Edward A. El Niño and the Peruvian Anchovy Fishery (series: Global Change Instruction Program) (PDF). Reviews in Fish Biology and Fisheries 9 (Sausalito: University Science Books). p. 118. doi:10.1023/A:1008801515441. ISBN 0-935702-80-6. Retrieved 23 June 2010.
- Gad G. (2005). "Giant Higgins-larvae with paedogenetic reproduction from the deep sea of the Angola Basin- evidence for a new life cycle and for abyssal gigantism in Loricifera?". Organisms, Diversity & Evolution 5 (Supplement 1): 59–76. doi:10.1016/j.ode.2004.10.005.
- Gill Adrian E. (1982). Atmosphere-Ocean Dynamics. San Diego: Academic Press. ISBN 0-12-283520-4.
- Gooday A.J., Nomaki H., & Kitazato H. (2008). "Modern deep-sea benthic foraminifera: a brief review of their morphology-based biodiversity and trophic diversity". Geological Society 303 (Special Publications 303): 97–119. doi:10.1144/SP303.8.
- Gooday A.J., Kamenskaya O.E. & Cedhagen T. (2007). "New and little-known Komokiacea (Foraminifera) from the bathyal and abyssal Weddell Sea and adjacent areas". Zoological Journal of the Linnean Society 151 (2): 219–251. doi:10.1111/j.1096-3642.2007.00326.x.
- Gooday A.J. & Malzone G. (2004). "Hyperammina micaceus sp. nov.: a new foraminiferan species (Protista) from the Porcupine Abyssal Plain, Northeast Atlantic". Journal of Micropalaeontology 23 (2): 171–179. doi:10.1144/jm.23.2.171.
- Janussen D. & Tendal O.S. (2007). "Diversity and distribution of Porifera in the bathyal and abyssal Weddell Sea and adjacent areas". Deep-Sea Research II 54 (16–17): 1864–1875. Bibcode:2007DSR....54.1864J. doi:10.1016/j.dsr2.2007.07.012.
- Markhaseva E.L. & Schulz K. (2006). "Sensiava longiseta (Copepoda, calanoidea): a new genus and species from the abyssal of the Weddell Sea". Zootaxa (1368): 1–18.
- Mühlenhardt-Siegel U. (2008). "Phalloleucon abyssalis, a new cumacean genus and species (Crustacea: Peracarida: Leuconidae) from the Peru Basin". Zootaxa (1829). pp. 61–68.
- Mursch, A.; Brenke, N.; Wägele, J.W. (2008). "Results of the DIVA-1 expedition of RV "Meteor" (Cruise M48:1): Three new species of Munnopsidae Sars, 1864 from abyssal depths of the Angola Basin (Crustacea: Isopoda: Asellota)". In Martinez, Pedro; Brix, Arbizu & Saskia. Bringing light into deep-sea biodiversity (Zootaxa 1866) (PDF). Auckland, New Zealand: Magnolia Press. ISBN 978-1-86977-260-4. Retrieved 23 June 2010.
- Nozawa F., Kitazato H., Tsuchiya M. & Gooday A.J. (2006). "'Live' benthic foraminifera at an abyssal site in the equatorial Pacific nodule province: abundance, diversity and taxonomic composition". Deep-Sea Research I 53 (8): 1406–1422. Bibcode:2006DSRI...53.1406N. doi:10.1016/j.dsr.2006.06.001.
- Sabbatini A., Morigi C., Negri A., & Gooday A.J. (2007). "Distribution and Biodiversity of Stained Monothalamous Foraminifera from Templejord, Svalbard". Journal of Foraminiferal Research 37 (2): 93–106. doi:10.2113/gsjfr.37.2.93.
- Schrödl M., Linse K. & Schwabe E. (2006). "Review on the distribution and biology of Antarctic Monoplacophora, with first abyssal record of Laevipilina antarctica". Polar Biology 29 (9): 721–727. doi:10.1007/s00300-006-0132-7.
- Schwabe E., Bohn J.M., Engl W., Linse K. & Schrödl M. (2007). "Rich and rare – first insights into species diversity and abundance of Antarctic abyssal Gastropoda (Mollusca)". Deep-Sea Research II 54 (16–17): 1831–1847. Bibcode:2007DSR....54.1831S. doi:10.1016/j.dsr2.2007.07.010.
- Sebastian S., Raes M., De Mesel I. & Vanreusel A. (2007). "Comparison of the nematode fauna from the Weddell Sea Abyssal Plain with two North Atlantic abyssal sites". Deep-Sea Research II 54 (16–17): 1727–1736. Bibcode:2007DSR....54.1727S. doi:10.1016/j.dsr2.2007.07.004.
- Seifried S., Plum Ch. & Schulz M. (2007). "A new species of Parabradya Lang, 1944 (Copepoda: Harpacticoida: Ectinosomatidae) from the abyssal plain of the Angola Basin" (PDF). Zootaxa (1432): 1–21. Retrieved December 5, 2013.
- Smith, Craig R.; Paterson, Gordon; Lambshead, John; Adrian G. Glover; Andrew Gooday; Alex Rogers; Myriam Sibuet; Hiroshi Kitazato; Joëlle Galéron; Menot, Lenaïck (2008). "Biodiversity, species ranges, and gene flow in the abyssal Pacific nodule province: predicting and managing the impacts of deep seabed mining". International Seabed Authority Technical Study: No.3 (PDF). Kingston, Jamaica: International Seabed Authority. ISBN 978-976-95217-2-8. OCLC 236437700. Retrieved 23 June 2010.
- Robert H. Stewart (2007). "Introduction to Physical Oceanography" (PDF). College Station: Texas A&M University. OCLC 169907785.
- Willen E. (2005). "A new species of Paranannopus Lang, 1936 (Copepoda, Harpacticoida, Pseudotachidiidae) with atrophic mouthparts from the abyssal of the Angola Basin". Organisms, Diversity & Evolution 5 (Supplement 1): 19–27. doi:10.1016/j.ode.2004.10.002.
- Yasuhara M., Cronin T.M. & Martinez Arbizu P. (2008). "Abyssal ostracods from the South and Equatorial Atlantic Ocean: biological and paleoceanographic implications". Deep-Sea Research I 55 (4): 490–497. Bibcode:2008DSRI...55..490Y. doi:10.1016/j.dsr.2008.01.004.
- Monterey Bay Aquarium Research Institute (3 November 2009). "Deep-sea Ecosystems Affected By Climate Change". ScienceDaily. Retrieved 18 June 2010.