Mid-ocean ridge

A mid-ocean ridge (MOR) is a seafloor mountain system formed by plate tectonics. It typically has a depth of ~ 2,600 meters (8,500 ft) and rises about two kilometers above the deepest portion of an ocean basin. This feature is where seafloor spreading takes place along a divergent plate boundary. The rate of seafloor spreading determines the morphology of the crest of the mid-ocean ridge and its width in an ocean basin. The production of new seafloor and oceanic lithosphere results from mantle upwelling in response to plate separation. The melt rises as magma at the linear weakness in the oceanic crust, and emerges as lava, creating new crust and lithosphere upon cooling. The Mid-Atlantic Ridge is a spreading center that bisects the North and South Atlantic basins; hence the origin of the name 'mid-ocean ridge'. Most oceanic spreading centers are not in the middle of their hosting ocean basis but regardless, are called mid-ocean ridges. Mid-ocean ridges around the globe are linked by plate tectonic boundaries and the outline of the ridges across the ocean floor appears similar to the seam of a baseball. The mid-ocean ridge system thus is the longest mountain range on Earth, reaching about 65,000 km (40,000 mi).

Mid-ocean ridge cut away view
Mid-ocean ridge cross section (cut away view)

Global system

World Distribution of Mid-Oceanic Ridges
World distribution of mid-oceanic ridges

The mid-ocean ridges of the world are connected and form the Ocean Ridge, a single global mid-oceanic ridge system that is part of every ocean, making it the longest mountain range in the world. The continuous mountain range is 65,000 km (40,400 mi) long (several times longer than the Andes, the longest continental mountain range), and the total length of the oceanic ridge system is 80,000 km (49,700 mi) long.[1]


Mid-ocean ridge topography
A mid-ocean ridge, with magma rising from a chamber below, forming new ocean plate that spreads away from the ridge
Þingvellir National Park, Bláskógabyggð (6969755432)
Mid-ocean ridge in Þingvellir National Park, Iceland


At the spreading center on a mid-ocean ridge the depth of the seafloor is approximately 2,600 meters (8,500 ft).[2][3] On the ridge flanks the depth of the seafloor (or the height of a location on a mid-ocean ridge above a base-level) is closely correlated with its age (age of the lithosphere where depth is measured). The age-depth relation can be modeled by the cooling of a lithosphere plate[4][5] or mantle half-space.[6] A good approximation is that the depth of the seafloor at a location on a spreading mid-ocean ridge proportional to the square root of the age of the seafloor.[6] The overall shape of ridges results from Pratt isostacy: close to the ridge axis there is hot, low-density mantle supporting the oceanic crust. As the oceanic plate cools, away from the ridge axis, the oceanic mantle lithosphere (the colder, denser part of the mantle that, together with the crust, comprises the oceanic plates) thickens and the density increases. Thus older seafloor is underlain by denser material and is deeper.[4][5]

Spreading rate is the rate at which an ocean basin widens due to seafloor spreading. (The rate at which new oceanic lithosphere is added to each tectonic plate on either side of a mid-ocean ridge is the spreading half-rate and is equal to half of the spreading rate). Spreading rates range from approximately 10–200 mm/yr.[2][3] Slow-spreading ridges such as the Mid-Atlantic Ridge have spread much less far (showing a narrower profile) than faster ridges such as the East Pacific Rise (wider profile) for the same amount of time and cooling and consequent bathymetric deepening.[2] Slow-spreading ridges (less than 40 mm/yr) generally have large rift valleys, sometimes as wide as 10–20 km (6.2–12.4 mi), and very rugged terrain at the ridge crest that can have relief of up to a 1,000 m (3,300 ft).[2][3][7][8] By contrast, fast-spreading ridges (greater than 90 mm/yr) such as the East Pacific Rise lack rift valleys. These have narrow, sharp ridge crests surrounded by generally flat topography that slopes away from the crest over many hundreds of miles.[2] The spreading rate of the North Atlantic Ocean is ~ 25 mm/yr, while in the Pacific region, it is 80–145 mm/yr.[9] Ridges that spread at rates <20 mm/yr are referred to as ultraslow spreading ridges[3][10] (e.g., the Gakkel Ridge in the Arctic Ocean and the Southwest Indian Ridge).

The spreading center or axis, commonly connects to a transform fault oriented at right angles to the axis. The flanks of mid-ocean ridges are in many places marked by the inactive scars of transform faults called fracture zones. At faster spreading rates the axes often display overlapping spreading centers that lack connecting transform faults.[2][11] The depth of the axis varies in a systematic way with shallower depths mid-way between offsets such as transform faults and overlapping spreading centers dividing the axis into segments; this is believed due to variations in magma supply to the spreading center.[2] Ultra-slow spreading ridges form both magmatic and amagmatic (currently lack volcanic activity) ridge segments without transform faults.[10]


Mid-ocean ridges exhibit active volcanism and seismicity.[3] The oceanic crust is in a constant state of 'renewal' at the mid-ocean ridges by the processes of seafloor spreading and plate tectonics. New magma steadily emerges onto the ocean floor and intrudes into the existing ocean crust at and near rifts along the ridge axes. The rocks making up the crust below the seafloor are youngest along the axis of the ridge and age with increasing distance from that axis. New magma of basalt composition emerges at and near the axis because of decompression melting in the underlying Earth's mantle.[12] The isentropic upwelling solid mantle material exceeds the solidus temperature and melts. The crystallized magma forms new crust of basalt known as MORB for mid-ocean ridge basalt, and gabbro below it in the lower oceanic crust.[13] Mid-ocean ridge basalt is a tholeiitic basalt and is low in incompatible elements.[14][15] Hydrothermal vents are a common feature at oceanic spreading centers.[16][17]

The oceanic crust and lithosphere is made up of rocks much younger than the Earth itself. Most oceanic crust in the ocean basins is less than 200 million years old.[18][19] As the oceanic crust and lithosphere moves away from the ridge axis, the peridotite in the underlying mantle lithosphere cools and becomes more rigid. The crust and the relatively rigid peridotite below it make up the oceanic lithosphere, which sits above the less rigid and viscous asthenosphere.[3]

Earth seafloor crust age 1996 - 2
Age of oceanic crust. The red is most recent, and blue is the oldest.

Formation processes

Oceanic spreading
Oceanic crust is formed at an oceanic ridge, while the lithosphere is subducted back into the asthenosphere at trenches.

Oceanic lithosphere is formed at an oceanic ridge, while the lithosphere is subducted back into the asthenosphere at ocean trenches. Two processes, ridge-push and slab pull, are thought to be responsible for spreading at mid-ocean ridges.[20] Ridge push refers to the gravitation sliding of the ocean plate that is raised above the hotter asthenosphere, thus creating a body force causing sliding of the plate downslope.[21] In slab pull the weight of a tectonic plate being subducted (pulled) below an overlying plate at a subduction zone drags the rest of the plate along behind it. The slab pull mechanism is considered to be contributing more than the ridge push.[20][22]

A process previously proposed to contribute to plate motion and the formation of new oceanic crust at mid-ocean ridges is the "mantle conveyor" due to deep convection (see image).[23][24] However, some studies have shown that the upper mantle (asthenosphere) is too plastic (flexible) to generate enough friction to pull the tectonic plate along.[25][26] Moreover, mantle upwelling that causes magma to form beneath the ocean ridges appears to involve only its upper 400 km (250 mi), as deduced from seismic tomography and from observations of the seismic discontinuity in the upper mantle at about 400 km (250 mi). The relatively shallow depths from which the upwelling mantle rises below ridges are more consistent with the slab pull process. On the other hand, some of the world's largest tectonic plates such as the North American Plate are in motion, yet are nowhere being subducted, pointing to action by the ridge push body force on this plate.

As crystallized basalt extruded at a ridge axis cools below Curie points of appropriate iron-titanium oxides, magnetic field directions parallel to the Earth's magnetic field are recorded in those oxides. The orientations of the field in the oceanic crust preserve a record of directions of the Earth's magnetic field with time. Because the field has reversed directions at known intervals throughout its history, the pattern of geomagnetic reversals in the ocean crust can be used as an indicator of age; given the crustal age and distance from the ridge axis, spreading rates can be calculated.[2][3][27]

Impact on global sea level

Increased rates of seafloor spreading (i.e. the rate of expansion of the mid-ocean ridge) has caused global (eustatic) sealevel to rise over very long timescales (millions of years).[28][29] Increased seafloor spreading means that the mid-ocean ridge will then expand and form a broader ridge with decreased average depth, taking up more space in the ocean basin. This displaces the overlying ocean and causes sea levels to rise.[30]

Sealevel change can be attributed to other factors (thermal expansion, ice melting, and mantle convection creating dynamic topography[31]). Over very long timescales, however, it is the result of changes in the volume of the ocean basins which are, in turn, affected by rates of seafloor spreading along the mid-ocean ridges.[32]

The high sealevel that occurred during the Cretaceous Period (144–65 Ma) can only be attributed to plate tectonics since thermal expansion and the absence of ice sheets by themselves cannot account for the fact that sea levels were 100–170 meters higher than today.[30]

Impact on seawater chemistry and carbonate deposition

Magnesium/calcium ratio changes at mid-ocean ridges

Seafloor spreading on mid-ocean ridges is a global scale ion-exchange system.[33] Hydrothermal vents at spreading centers introduce various amounts of iron, sulfur, manganese, silicon and other elements into the ocean, some of which are recycled into the ocean crust. Helium-3, an isotope that accompanies volcanism from the mantle, is emitted by hydrothermal vents and can be detected in plumes within the ocean.[34]

Fast spreading rates will expand the mid-ocean ridge causing basalt reactions with seawater to happen more rapidly. The magnesium/calcium ratio will be lower because more magnesium ions are being removed from seawater and consumed by the rock, and more calcium ions are being removed from the rock and released to seawater. Hydrothermal activity at ridge crest is efficient in removing magnesium.[35] A lower Mg/Ca ratio favors the precipitation of low-Mg calcite polymorphs of calcium carbonate (calcite seas).[36][37]

Slow spreading at mid-ocean ridges has the opposite effect and will result in a higher Mg/Ca ratio favoring the precipitation of aragonite and high-Mg calcite polymorphs of calcium carbonate (aragonite seas).[37]

Experiments show that most modern high-Mg calcite organisms would have been low-Mg calcite in past calcite seas,[38] meaning that the Mg/Ca ratio in an organism's skeleton varies with the Mg/Ca ratio of the seawater in which it was grown.

The mineralogy of reef-building and sediment-producing organisms is thus regulated by chemical reactions occurring along the mid-ocean ridge, the rate of which is controlled by the rate of sea-floor spreading.[35][38]



The first indications that a ridge bisects the Atlantic Ocean basin came from the results of the British Challenger Expedition in the nineteenth century.[39] Soundings from lines dropped to the seafloor were analyzed by oceanographers Matthew Fontaine Maury and Charles Wyville Thomson and revealed a prominent rise in the seafloor that ran down the Atlantic basin from north to south. Sonar echo sounders confirmed this in the early twentieth century.[40]

It was not until after World War II, when the ocean floor was surveyed in more detail, that the full extent of mid-ocean ridges became known. The Vema, a ship of the Lamont-Doherty Earth Observatory of Columbia University, traversed the Atlantic Ocean, recording echo sounder data on the depth of the ocean floor. A team led by Marie Tharp and Bruce Heezen concluded that there was an enormous mountain chain with a rift valley at its crest, running up the middle of the Atlantic Ocean. Scientists named it the 'Mid-Atlantic Ridge'. Other research showed that the ridge crest was seismically active[41] and fresh lavas were found in the rift valley.[42] In addition, crustal heat flow was higher here than elsewhere in the Atlantic ocean basin.[43]

At first, the ridge was thought to be a feature specific to the Atlantic Ocean. However, as surveys of the ocean floor continued around the world, it was discovered that every ocean contains parts of the mid-ocean ridge system. The German Meteor Expedition traced the mid-ocean ridge from the South Atlantic into the Indian Ocean early in the twentieth century. Although the first-discovered section of the ridge system runs down the middle of the Atlantic Ocean, it was found that most mid-ocean ridges are located away from the center of other ocean basins.[2][3]

Impact of discovery: seafloor spreading

Alfred Wegener proposed the theory of continental drift in 1912. He stated: "the Mid-Atlantic Ridge ... zone in which the floor of the Atlantic, as it keeps spreading, is continuously tearing open and making space for fresh, relatively fluid and hot sima [rising] from depth".[44] However, Wegener did not pursue this observation in his later works and his theory was dismissed by geologists because there was no mechanism to explain how continents could plow through ocean crust, and the theory became largely forgotten.

Following the discovery of the worldwide extent of the mid-ocean ridge in the 1950s, geologists faced a new task: explaining how such an enormous geological structure could have formed. In the 1960s, geologists discovered and began to propose mechanisms for seafloor spreading. The discovery of mid-ocean ridges and the process of seafloor spreading allowed for Wegner's theory to be expanded so that it included the movement of oceanic crust as well as the continents.[45] Plate tectonics was a suitable explanation for seafloor spreading, and the acceptance of plate tectonics by the majority of geologists resulted in a major paradigm shift in geological thinking.

It is estimated that 20 volcanic eruptions occur each year along earth's mid-ocean ridges and that every year 2.5 km2 (0.97 sq mi) of new seafloor is formed by this process. With a crustal thickness of 1 to 2 km (0.62 to 1.24 mi), this amounts to about 4 km3 (0.96 cu mi) of new ocean crust formed every year.

Deep Sea Vent Chemistry Diagram

Oceanic ridge and deep sea vent chemistry

Plates tect2 en

Plates in the crust of the earth, according to the plate tectonics theory


A demonstration of magnetic striping

List of oceanic ridges

  • Aden Ridge – Part of an active oblique rift system in the Gulf of Aden, between Somalia and the Arabian Peninsula
  • Cocos Ridge
  • Explorer Ridge – A mid-ocean ridge west of British Columbia, Canada
  • Gorda Ridge – A tectonic spreading center off the northern coast of California and southern Oregon
  • Juan de Fuca Ridge – A divergent plate boundary off the coast of the Pacific Northwest region of North America.
  • South American–Antarctic Ridge – Mid-ocean ridge in the South Atlantic between the South American Plate and the Antarctic Plate
  • Chile Rise – An oceanic ridge at the tectonic divergent plate boundary between the Nazca and Antarctic plates
  • East Pacific Rise – A mid-oceanic ridge at a divergent tectonic plate boundary on the floor of the Pacific Ocean
  • East Scotia Ridge
  • Gakkel Ridge – A mid-oceanic ridge under the Arctic Ocean between the North American Plate and the Eurasian Plate(Mid-Arctic Ridge)
  • Nazca Ridge – A submarine ridge on the Nazca Plate off the west coast of South America
  • Pacific-Antarctic Ridge – A divergent tectonic plate boundary located on the seafloor of the South Pacific Ocean, separating the Pacific Plate from the Antarctic Plate
  • Central Indian Ridge – A north-south-trending mid-ocean ridge in the western Indian Ocean
    • Carlsberg Ridge – The northern section of the Central Indian Ridge between the African Plate and the Indo-Australian Plate
  • Southeast Indian Ridge – A mid-ocean ridge in the southern Indian Ocean
  • Southwest Indian Ridge – A mid-ocean ridge on the bed of the south-west Indian Ocean and south-east Atlantic Ocean
  • Mid-Atlantic Ridge – A divergent tectonic plate boundary that in the North Atlantic separates the Eurasian and North American plates, and in the South Atlantic separates the African and South American plates
    • Kolbeinsey Ridge (North of Iceland)
    • Mohns Ridge
    • Knipovich Ridge (between Greenland and Spitsbergen)
    • Reykjanes Ridge (South of Iceland)

List of ancient oceanic ridges

  • Aegir Ridge – An extinct mid-ocean ridge in the far-northern Atlantic Ocean
  • Alpha Ridge – A major volcanic ridge under the Arctic Ocean
  • Kula-Farallon Ridge – An ancient mid-ocean ridge that existed between the Kula and Farallon plates in the Pacific Ocean during the Jurassic period
  • Pacific-Farallon Ridge – A spreading ridge during the late Cretaceous that separated the Pacific Plate to the west and the Farallon Plate to the east
  • Pacific-Kula Ridge – A mid-ocean ridge between the Pacific and Kula plates in the Pacific Ocean during the Paleogene period
  • Phoenix Ridge – An ancient mid-ocean ridge between the Phoenix and Pacific plates

See also


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External links

Amasia (continent)

Amasia is a possible, future supercontinent that could be formed by the merger of Asia and North America. This prediction relies mostly on the fact that the Pacific Plate is already subducting under Eurasia and North America, a process which if continued will eventually cause the Pacific to close. Meanwhile, because of the Atlantic mid-ocean ridge, North America would be pushed westward. Thus, the Atlantic at some point in the future would be larger than the Pacific. In Siberia, the boundary between the Eurasian and North American Plates has been stationary for millions of years. The combination of these factors would cause North America to be combined with Asia, thus forming a supercontinent. A February 2012 study predicts Amasia will form over the North Pole, in about 50 million to 200 million years.

Antarctic Plate

The Antarctic Plate is a tectonic plate containing the continent of Antarctica, the Kerguelen Plateau and extending outward under the surrounding oceans. After breakup from Gondwana (the southern part of the supercontinent Pangea), the Antarctic plate began moving the continent of Antarctica south to its present isolated location causing the continent to develop a much colder climate. The Antarctic Plate is bounded almost entirely by extensional mid-ocean ridge systems. The adjoining plates are the Nazca Plate, the South American Plate, the African Plate, the Somali Plate, the Indo-Australian Plate, the Pacific Plate, and, across a transform boundary, the Scotia Plate.

The Antarctic Plate has an area of about 60,900,000 km2 (23,500,000 sq mi). It is the Earth's fifth-largest plate.

The Antarctic Plate's movement is estimated to be at least 1 cm (0.4 in) per year towards the Atlantic Ocean


The asthenosphere (from Greek ἀσθενής asthenḗs 'weak' + "sphere") is the highly viscous, mechanically weak and ductilely deforming region of the upper mantle of the Earth. It lies below the lithosphere, at depths between approximately 80 and 200 km (50 and 120 miles) below the surface. The Lithosphere–asthenosphere boundary is usually referred to as LAB. The asthenosphere is almost solid, although some of its regions could be molten (e.g., below mid-ocean ridges). The lower boundary of the asthenosphere is not well defined. The thickness of the asthenosphere depends mainly on the temperature. However, the rheology of the asthenosphere also depends on the rate of deformation, which suggests that the asthenosphere could be also formed as a result of a high rate of deformation. In some regions the asthenosphere could extend as deep as 700 km (430 mi). It is considered the source region of mid-ocean ridge basalt (MORB).

British Mid-Ocean Ridge Initiative

The British Mid-Ocean Ridge Initiative (the BRIDGE Programme) was a multidisciplinary scientific investigation of the creation of the Earth’s crust in the deep oceans. It was funded by the UK’s Natural Environment Research Council (NERC) from 1993 to 1999.

Central Indian Ridge

The Central Indian Ridge (CIR) is a north-south-trending mid-ocean ridge in the western Indian Ocean.

Explorer Ridge

The Explorer Ridge is a mid-ocean ridge, a divergent tectonic plate boundary located about 241 km (150 mi) west of Vancouver Island, British Columbia, Canada. It lies at the northern extremity of the Pacific spreading axis. To its east is the Explorer Plate, which together with the Juan de Fuca Plate and the Gorda Plate to its south, is what remains of the once-vast Farallon Plate which has been largely subducted under the North American Plate. The Explorer Ridge consists of one major segment, the Southern Explorer Ridge, and several smaller segments. It runs northward from the Sovanco Fracture Zone to the Queen Charlotte Triple Junction, a point where it meets the Queen Charlotte Fault and the northern Cascadia subduction zone.

Fracture zone

A fracture zone is a linear oceanic feature—often hundreds, even thousands of kilometers long—resulting from the action of offset mid-ocean ridge axis segments. They are a consequence of plate tectonics. Lithospheric plates on either side of an active transform fault move in opposite directions; here, strike-slip activity occurs. Fracture zones extend past the transform faults, away from the ridge axis; seismically inactive (because both plate segments are moving in the same direction), they display evidence of past transform fault activity, primarily in the different ages of the crust on opposite sides of the zone.

In actual usage, many transform faults aligned with fracture zones are often loosely referred to as "fracture zones" although technically, they are not.

Gakkel Ridge

The Gakkel Ridge (formerly known as the Nansen Cordillera and Arctic Mid-Ocean Ridge) is a mid-oceanic ridge, a divergent tectonic plate boundary between the North American Plate and the Eurasian Plate. It is located in the Eurasian Basin of the Arctic Ocean, between Greenland and Siberia, and has a length of about 1,800 kilometers. Geologically, it connects the northern end of the Mid-Atlantic Ridge with the Laptev Sea Rift.

The existence and approximate location of the Gakkel Ridge were predicted by Soviet polar explorer Yakov Yakovlevich Gakkel, and confirmed on Soviet expeditions in the Arctic around 1950. The Ridge is named after him, and the name was recognized in April 1987 by SCUFN (under that body's old name, the Sub-Committee on Geographical Names and Nomenclature of Ocean Bottom Features).The ridge is the slowest known spreading ridge on earth, with a rate of less than one centimeter per year. Until 1999, it was believed to be non-volcanic; that year, scientists operating from a nuclear submarine discovered active volcanoes along it. In 2001 two research icebreakers, the German Polarstern and the American Healy, with several groups of scientists, cruised to the Gakkel Ridge to explore it and collect petrological samples. Among other discoveries, this expedition found evidence of hydrothermal vents. In 2007, Woods Hole Oceanographic Institution conducted the "Arctic Gakkel Vents Expedition" (AGAVE), which made some unanticipated discoveries, including the unconsolidated fragmented pyroclastic volcanic deposits that cover the axial valley of the ridge (whose area is greater than 10 km2). These suggest volatile substances in concentrations ten times those in the magmas of normal mid-ocean ridges. Using "free-swimming" robotic submersibles on the Gakkel ridge, the AGAVE expedition also discovered what they called "bizarre 'mats' of microbial communities containing a half dozen or more new species".The Gakkel ridge is remarkable in that is not offset by any transform faults. The ridge does have segments with variable orientation and varying degrees of volcanism: the Western Volcanic Zone From the Lena trough, 7° W, to 3° E longitude), the Sparsely Magmatic Zone (from 3° E to 29° E longitude), and the Eastern Magmatic Zone (from 29° E to 89°E). The gaps of volcanic activity imply very cold crust and mantle, probably related to the very low spreading rate, but it is not yet known why some parts of the ridge are more magmatic than others. Some earthquakes have been detected from the mantle, below the crust, which is very unusual for a mid-ocean ridge. It confirms that the mantle and crust of Gakkel ridge, like some segments of the Southwest Indian Ridge, are very cold.

John M. Edmond

John Marmion Edmond FRS (April 27, 1943 – April 10, 2001) was a professor of marine geochemistry and oceanography at the Massachusetts Institute of Technology, who did pioneering work on oceanic particulate matter, the oceanic carbon dioxide cycle, trace elements, and radioisotopes. He explored and analyzed water chemistry from environments as diverse as the mid-ocean ridge hydrothermal vents to the polar oceans to remote rivers and lakes in South America, Africa, Siberia, and Tibet. He and his students and colleagues in his lab measured more chemical elements at lower concentrations in water than had ever been done before.

Kula-Farallon Ridge

The Kula-Farallon Ridge was an ancient mid-ocean ridge that existed between the Kula and Farallon plates in the Pacific Ocean during the Jurassic period. There was a small piece of this ridge off the Pacific Northwest 43 million years ago. The rest of the ridge has since been subducted beneath Alaska.

In its early stages of development, the Kula-Farallon Ridge sheared pieces of oceanic rock off the coast of California. When the Kula–Farallon Ridge was in the area where Washington and Oregon are now, basaltic lava erupted there. Some of the basaltic lava is now part of the Olympic Peninsula.

Mid-Atlantic Ridge

The Mid-Atlantic Ridge (MAR) is a mid-ocean ridge, a divergent tectonic plate or constructive plate boundary located along the floor of the Atlantic Ocean, and part of the longest mountain range in the world. In the North Atlantic, it separates the Eurasian and North American plates, and in the South Atlantic, it separates the African and South American plates. The ridge extends from a junction with the Gakkel Ridge (Mid-Arctic Ridge) northeast of Greenland southward to the Bouvet Triple Junction in the South Atlantic. Although the Mid-Atlantic Ridge is mostly an underwater feature, portions of it have enough elevation to extend above sea level. The section of the ridge that includes Iceland is known as the Reykjanes Ridge. The ridge has an average spreading rate of about 2.5 centimetres (0.98 in) per year.

Mid-Labrador Ridge

The Mid-Labrador Ridge was a mid-ocean ridge in the Labrador Sea that represented a divergent boundary between the Greenland and North American plates during the Paleogene. The ridge extended from the South Greenland Triple Junction in the southeast to the Davis Strait area in the northwest. Seafloor spreading along the Mid-Labrador Ridge discontinued about 40 million years ago when the mid-ocean ridge became essentially extinct.The Mid-Labrador Ridge is now mostly buried under sediment, exposed only as a northwesterly trend of seamounts in the southeastern part of the Labrador Basin.

Pacific-Kula Ridge

The Pacific-Kula Ridge is a former mid-ocean ridge that existed between the Pacific and Kula plates in the Pacific Ocean during the Paleogene period. Its appearance was in an east-west direction and the Hawaiian-Emperor seamount chain had its attribution with the ridge. The Pacific-Kula Ridge lay south of the Hawaii hotspot around 80 million years ago, moving northward relative to the hotspot.

Pangaea Ultima

Pangaea Ultima (also called Pangaea Proxima, Neopangaea, and Pangaea II) is a possible future supercontinent configuration. Consistent with the supercontinent cycle, Pangaea Ultima could occur within the next 100 million to 200 million years. This potential configuration, hypothesized by Christopher Scotese, earned its name from its similarity to the previous Pangaea supercontinent. Scotese later changed Pangaea Ultima (Last Pangaea) to Pangaea Proxima (Next Pangaea) to alleviate confusion about the name Pangaea Ultima which could imply that it would be the last supercontinent. The concept was based on examination of past cycles of formation and breakup of supercontinents, not on current understanding of the mechanisms of tectonic change, which are too imprecise to project that far into the future. "It's all pretty much fantasy to start with," Scotese has said. "But it's a fun exercise to think about what might happen. And you can only do it if you have a really clear idea of why things happen in the first place."Supercontinents describe the merger of all, or nearly all, of the Earth's landmass into a single contiguous continent. In the Pangaea Ultima scenario, subduction at the western Atlantic, east of the Americas, leads to the subduction of the Atlantic mid-ocean ridge followed by subduction destroying the Atlantic and Indian basin, causing the Atlantic and Indian Oceans to close, bringing the Americas back together with Africa and Europe. As with most supercontinents, the interior of Pangaea Proxima would probably become a semi-arid desert prone to extreme temperatures.

Phoenix Ridge

The Phoenix Ridge (also called the Aluk Ridge) was an ancient mid-ocean ridge that existed between the Phoenix Plate and the Pacific Plate. The Phoenix Ridge consisted of three ridges and had a spreading rate of 18–20 cm per year until around 84 Ma. A major decrease in spreading rate, and the convergence rate with the Antarctic Plate occurred around 52.3 Ma. The Phoenix Ridge has since been subducted under the Antarctic Peninsula in the Miocene period.

Prehnite-pumpellyite facies

The prehnite-pumpellyite facies is a metamorphic facies typical of subseafloor alteration of the oceanic crust around mid-ocean ridge spreading centres.

It is a metamorphic grade transitional between zeolite facies and greenschist facies representing a temperature range of 250 to 350 °C and a pressure range of approximately two to seven kilobars. The mineral assemblage is dependent on host composition.

In mafic rocks the assemblage is chlorite, prehnite, albite, pumpellyite and epidote.

In ultramafic rocks the assemblage is serpentine, talc, forsterite, tremolite and chlorite.

In argillaceous sedimentary rocks the assemblage is quartz, illite, albite, and stilpnomelane chlorite.

In carbonate sediments the assemblage is calcite, dolomite, quartz, clays, talc, and muscovite.

Seafloor spreading

Seafloor spreading is a process that occurs at mid-ocean ridges, where new oceanic crust is formed through volcanic activity and then gradually moves away from the ridge.

Slab window

In geology, a slab window is a gap that forms in a subducted oceanic plate when a mid-ocean ridge meets with a subduction zone and plate divergence at the ridge and convergence at the subduction zone continue, causing the ridge to be subducted. Formation of a slab window produces an area where the crust of the over-riding plate is lacking a rigid lithospheric mantle component and thus is exposed to hot asthenospheric mantle (for a diagram of this, see the link below). This produces anomalous thermal, chemical and physical effects in the mantle that can dramatically change the over-riding plate by interrupting the established tectonic and magmatic regimes. In general, the data used to identify possible slab windows comes from seismic tomography and heat flow studies.

Undersea mountain range

Undersea mountain ranges are mountain ranges that are mostly or entirely underwater, and specifically under the surface of an ocean. If originated from current tectonic forces, they are often referred to as a mid-ocean ridge. In contrast, if formed by past above-water volcanism, they are known as a seamount chain. The largest and best known undersea mountain range is a mid-ocean ridge, the Mid-Atlantic Ridge. It has been observed that, "similar to those on land, the undersea mountain ranges are the loci of frequent volcanic and earthquake activity".

Mid-ocean ridges
Ocean zones
Sea level


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