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== Density, Salinity and Temperature of the Ocean ==
[[File:Hydrometer in test.jpg|thumb|A hydrometer measures the density of the water (or other liquid) by floating a standard weight.]]
[[w:density|Density]] is a measure of the substance’s mass per unit volume, or how compacted or dense a substance is. Specific density is a measure of whether a substance will float or sink relative to pure water, which has a specific density of 1. Liquids with a [[w:Relative density|specific density]] less than 1 will float, while liquids with a specific density of more than 1 will sink in a glass of pure water. Ocean water, because it contains a mixture of salts and dissolved particles averages a specific density between 1.020 to 1.029. Density in ocean water is measured using a [[w:Hydrometer|hydrometer]], which is a glass tube with a standard weight attached to a scale that indicates how far the weight sinks in the fluid. If you were to mix ocean water and freshwater, the two would likely mix, making it difficult to determine whether one floats above another. The greater density difference between fluids, the more likely you can get them to stack on top of each other, by floating the less dense fluid on top of the denser fluid. However, if you try to stack the denser fluid on top of a less dense fluid, the two fluids simply mix. A column of fluids of different densities is said to be stratified, strata means layers, so a stratified ocean is an ocean that is divided into unique layers based on differences in densities.

The density of water is not only related to how much salt is dissolved in the water, but also the water’s temperature. The colder the water, the denser it becomes, although between 4° C to 0° C near the freezing point water becomes less dense as it freezes to ice.
[[File:The effects of heat exchange and thermal advection on the rate of change of temperature at Ocean Weather Station November. (1974) (20999564969).jpg|thumb|left|The thermocline, halocline, and pycnocline (surface ocean water is warm and fresh; deeper ocean water is cold and salty).]]
The gradient between density and salinity of ocean water is called the [[w:Halocline|'''halocline''']]. In a vertical profile of the ocean, salinity increases with depth, because salty water is denser and will sink. The gradient between density and temperature of ocean water is called the [[w:Thermocline|'''thermocline''']]. In a vertical profile of the ocean, temperature decreases with depth, as colder water (above 4°C) is denser and will sink. The densest ocean water is both cold and salty, while the least dense ocean water is both hot and fresh. The gradient of density with depth is referred to as the [[w:Pycnocline|'''pycnocline''']]. ''Pycnos'' in ancient Greek means dense. The pycnocline is a graph showing density with depth of ocean water. If the ocean is stratified into layers of different densities, the graph will show a slope with steps at each layer of increasing density. However, if the ocean is well mixed, the pycnocline will be a straight line vertical of equal density with depth.
[[File:Stratified-Deep-Ocean-Waters.jpg|thumb|Stratified deep ocean waters, showing important gradients with water depth.]]
In the previous sections, surface ocean currents and upwelling and downwelling are influenced by [[w:Geostrophic wind|geostrophic winds]], and surface processes that result in shallow movement of the ocean waters. However, [[w:Ekman transport|Ekman’s research]] also showed that deep ocean water, deeper than 100 meters will remain less mobile, and will not be influenced by these forces that work only on the surface of the ocean. Deep ocean water moves very slowly, so slowly that oceanographers debate what the rate of movement of this deep ocean water truly is as it moves around the Earth.

Deep ocean water circulation of the planet is a slow and gentle process that involves most of the total volume of the oceans, and is a consequence of dynamic changes in ocean water density with depth. Such changes in density result in a mixing of surface and deep ocean waters.

==Stratified Water==
How do oceans or for that matter any large body of water on Earth become stratified into different layers of density?

Imagine a large lake, which serves as a reservoir of water with inflowing rivers of fresh salt-free water. The flux of incoming freshwater into the lake from the surrounding rivers decreases in the late summer, but increases in the late winter and early spring from run off or the rainy seasons. During the summer the hot sun heats the top layers of the lake resulting in [[w:Evaporation|evaporation]], and the underlying layers of water become saltier, but remain warm. Over time such a lake will become stratified into different layers of density. In the summer, the surface water will become salty, but warmer, allowing it to float over the denser water below, however, as the fall temperatures drop, the salty water will increase in density. During the spring an influx of less dense freshwater from the rivers will float over this salty and colder water already in the lake. This adds a new layer of less dense freshwater, and stacks the water on top. Over time, the lake will become heavily stratified into cold/salty dense layers remaining deep in the lake, while warm/fresh less dense water remain at the top with each input of freshwater.
[[File:Artsy density column.png|thumb|150px|left|Layers of liquid with various densities. Such stratification of ocean water can occur, and does occur in many large bodies of water. These different color layers of liquid are not mixing, but forming layers, and hence are stratified.]]
What process can cause the two layers to mix? If during the winter months the lake is covered in [[w:Ice|ice]], the top layer of water will become both cold and salty. The salt originates from the fact that as ice forms on the top of the lake, the ice will contain no salts, leaving the layers just below the ice slightly saltier, and very cold. Ice coverage on the lake will cause this salty/cold dense water to lay on top of warm/fresh less dense water, which will ultimately cause the water at the surface to sink, and the deep water to rise. An ice-covered body of water contains a better mixture of waters compared to ice-free bodies of water. As a result, bodies of water in cold regions of Earth are less stratified than waters in warm tropical regions. Another thing that can happen to the lake is if the deep water is somehow warmed. This can occur when a volcano or magma heats the bottom waters. When these dense deep waters are heated, they become less dense and rise, this is likely what happened in the [[w:Lake Nyos disaster|Lake Nyos disaster]] in Cameroon Africa, when deep waters bubbled up releasing massive amounts of carbon dioxide gas killing many people.

Measurements of the pycnocline in various lakes around the world demonstrate that colder lakes covered in ice during the winter are better mixed than warmer lakes, which remain ice free. The same processes of mixing deep waters with surface waters can be applied to the entire ocean, which is more complex since the [[w:World Ocean|Worlds Ocean]] is more interconnected and spans the entire Earth’s surface. [[w:Oceanography|Oceanographers]] have mapped out differences in annual temperatures and salinity to help to understand this complex process.
[[File:NASA's Aquarius Sees Salty Shifts.jpg|thumb|NASA Aquarius measures the ocean’s surface salinity over the entire Earth.]]
[[File:SurfaceTemperature.jpg|thumb|Ocean Surface Temperatures, with warmest ocean waters near the equator, and coldest near the poles.]]
Annual surface temperatures measured across the entire ocean show that the warmest waters are found along the equator, with the coldest waters found near the poles. However, surface [[w:Salinity|salinity]] measured across the entire ocean shows that the saltiest surface waters are found within the large ocean gyres, such as the [[w:North Atlantic Gyre|North Atlantic]] and [[w:South Atlantic Gyre|South Atlantic gyres]], which are some of the saltiest regions of the open ocean. This is because these regions of the ocean are more stagnant, as well as being in drier regions that receive less rainfall. The [[w:Intertropical Convergence Zone|ITCZ]] around the equator contributes massive amounts of freshwater from rain, and limits evaporation along the equator. Large confided bodies of ocean water surrounded by land, like the [[w:Mediterranean|Mediterranean]] and [[w:Red Sea|Red Seas]], are some of the most saline regions of the ocean. Some of the least salty regions of the ocean are found near where there is a large input into the ocean of freshwater from rivers, particularly in [[w:Southeast Asia|Southeastern Asia]]. Regions near the poles also get input of freshwater from melt waters. [[w:Sea ice|Sea ice]] which expands during the winter months in polar regions of the [[w:Arctic Ocean|Arctic]] and [[w:Antarctic Ocean|Antarctic Oceans]] is important for the mixing of surface and deep ocean waters. If these waters are already salty from evaporation, mixing can be enhanced. In the North Atlantic the salty surface ocean waters trapped in the North Atlantic gyre are pushed northward toward Greenland with the Gulf Stream currents. If these salty warmer waters are subsequently cooled and covered in sea ice, these waters will sink, resulting in a mixing of surface and deep waters in the [[w:North Atlantic Deep Water|North Atlantic Ocean]]. This drives what is called the [[w:Thermohaline circulation|'''Thermohaline circulation''']] of deep ocean waters.

==Thermohaline Ocean Circulation of Deep Ocean Waters==
[[File:Thermohaline Circulation using Improved Flow Field.ogv|400px|thumb|center|Animation of the Thermohaline Circulation showing the process of downwelling ocean water in the North Atlantic Ocean, which starts the process of global deep water mixing ]]
The [[w:Thermohaline circulation|Thermohaline circulation]] is a broad deep water circulation of the entirety of the world’s ocean, although the precise process of this motion is highly debated among oceanographers. The North Atlantic serves as the region of sinking cold salty water, resulting from salty water in the Atlantic pushed northward, and subjected to coverage of sea ice, especially during the winter months in the Northern Hemisphere. This sinking cold salty ocean water churns the ocean over in the North Atlantic and helps to drive the [[w:Gulf Stream|Gulf Stream]], pulling more warm salty waters northward to cool and subsequently sink. The North Atlantic is the least stratified region in the worlds ocean, resulting in well-mixed waters that are enriched in oxygen.
[[File:Younger Dryas and Air Temperature Changes.jpg|thumb|The Younger Dryas Event, from ice cores on Greenland’s ice sheet, where temperatures warmed then cooled, then warmed again during the Late Pleistocene and beginning of the Holocene, 15 to 11 thousand years ago.]]
Ice core from Greenland records a period of time 12,000 years ago, when the Thermohaline circulation may have been altered dramatically. This period of time is called the [[w:Younger Dryas|'''Younger Dryas event''']], because sediments in lakes record the return of pollen of the cold-adapted [[w:Dryas octopetala|Dryas arctic flower]], which prefers colder climates. The flower grew across much of Northern Europe and Greenland during the last [[w:Ice age|Ice Age]] up to about 14,000 years ago, when the flower disappeared from these regions as the climate warmed. However, the flower’s pollen returns in the sediments of lakes around 12,000 years ago, signaling a return of cold climates for several hundred years, before again disappearing from these regions. This episode of colder climates in the North Atlantic is hypothesized to be a result of the thermohaline circulation being altered by an influx of freshwater from land. The idea holds that massive amounts of freshwater flooded into the North Atlantic, particularly from the [[w:Labrador Sea|Labrador Sea]] and [[w:Gulf of Saint Lawrence|Straits of Lawrence]], which drained the great ice sheets that covered the [[w:Great Lakes|Great Lakes]] and much of [[w:Canada|Canada]]. This influx of freshwater resulted in the [[w:Atlantic Ocean|North Atlantic Ocean]] becoming more stratified, and resulted in weakening [[w:Gulf Stream|Gulf Stream]], with less warm ocean water reaching Northern Europe. This resulted in colder climates to prevail, until the melt of the great ice sheets ended, at which time the Thermohaline circulation resumed, resulting in warmer climates in Northern Europe again.
[[File:Thermohaline Circulation 2.png|thumb|center|500px|The Earth’s Thermohaline Circulation of Deep Ocean Waters.]]
The [[w:Thermohaline circulation|thermohaline circulation]] is often depicted as a ribbon of flow that involves the entire world’s ocean, but oceanographers debate how this circulation pattern works in reality on a global scale. Recent research suggests that the deep ocean waters that encircle [[w:Antarctica|Antarctica]] are pulled up as a result of this churning in the North Atlantic. These Southern Ocean waters are warmest during December/January and rise with the warming temperatures, pulled by the North Atlantic which is at its coldest and saltiest levels during these months. In July/August, the North Atlantic Ocean returns to its warmest levels, while the ocean waters around Antarctica are at their coldest and covered by sea ice. [[w:Polynya|'''Polynyas''']] form in the sea ice around Antarctica, which are regions of thin ice mix with open water which are thinner than expected for the given temperature, because these regions frequently contain saltier water. This results in the cold/salty water to sink deeper around the coast of Antarctica in July/August. Like a teeter-totter, deep ocean water circulating around Antarctica rises and falls each year with the seasons. These [[w:Antarctic bottom water|Antarctic Bottom Waters]] are well mixed, and enriched in oxygen and nitrogen.
[[File:Antarctic bottom water.svg|thumb|Antarctic Bottom Waters]]
[[File:Balaenoptera musculus in American Museum of Natural History.jpg|thumb|A model of the largest animal on Earth, the Blue Whale (Balaenoptera musculus) at the American Museum in New York City.]]
[[w:Sea ice|Sea ice]] is of vital importance in the mixing of the World’s Oceans, and life has adapted to the annual rise and fall of deep ocean waters in these polar regions. When deeper ocean waters rise in these polar regions, they bring up nitrogen which benefits phytoplankton growing in the upper photic zone. Large blooms of phytoplankton occur during the summer months, which attract krill and fish that feed on the phytoplankton. These schools of fish and [[w:Krill|krill]] prosper in the oxygen enriched cold waters, and feed migrating [[w:Baleen whale|baleen whales]], which feed on the krill using baleen to filter them out of the water. The largest animal on Planet Earth, the blue whale (''Balaenoptera musculus'') evolved to exploit the deep ocean circulation patterns that have resulted from large portions of the ocean being covered in sea ice.

==Deep Ocean Water Mixing Without Sea Ice==
[[File:Salt fingers.png|thumb|Salt fingers, where salty warm water cools, and sinks.]]
There have been periods of time that Earth’s ocean remained ice free, particularly during periods of enriched carbon dioxide in the atmosphere. Deep ocean water mixing without sea ice formation is possible, and occurs when salty water from warm seas that are confined and subjected to enhanced evaporation enter colder open ocean waters. An example of where this happens is near the [[w:Strait of Gibraltar|Straits of Gibraltar]] where the salty warm waters of the Mediterranean enter into the colder Atlantic Ocean. Heat diffuses faster than salt, and the relatively faster transfer of heat compared to salt results in the salty water cooling more quickly than the salt can disperse, and hence becomes unstable near the surface of the ocean. This salty/cold water is denser and sinks, forming “salt fingers,” which are a mix of deep and surface waters churning the waters vertically. These regions are enriched in nitrogen, phosphorus, as well as being fairly well oxygenated ocean waters. During Earth’s long history, such regions where responsible for biologically rich ocean life, despite periods of time when the oceans remained ice free year-round. One example of this is found in the rocks of Eastern Utah. During the [[w:Pennsylvanian (geology)|Pennsylvanian]] and [[w:Permian|Permian]] Periods about 270 million years ago, a land-restricted sea existed in present day [[w:Moab|Moab]], which was extremely salty, but opened out into the larger open ocean to the northwest. The influx of salty water from this sea resulted in a well-mixed ocean despite the much warmer climate of the time. Fossils are found abundantly in marine rocks of this age, as well as thick deposits of [[w:Phosphorus| phosphorus]] mined for agricultural fertilizers.

==The Danger of Highly Stratified Oceans==
[[File:GulfofMexico3D.jpg|thumb|The Gulf of Mexico]]
If the Earth’s oceans remain ice-free year-round, and there is no influx of salty surface waters from land-restricted seas, like the Mediterranean Sea, then the oceans can quickly become highly stratified. A highly stratified ocean means that deep and surface ocean waters never mix, and oxygen levels become highly restricted to only the surface of the ocean. Such periods of time happened on Earth, particularly during the [[w:Mesozoic|Mesozoic Era]], when dinosaurs roamed a much warmer Earth. These oceans are prone to [[w:Anoxic event|anoxia]], the absence of oxygen, which results in [[w:Dead zone (ecology)|“dead zones”]] where fish and other animals that need oxygen for respiration perish. An example of ocean water that is susceptible to anoxia is the [[w:Gulf of Mexico|Gulf of Mexico]]. During the heat of the late summer, the surface waters in the Gulf of Mexico evaporate resulting in salty surface waters, which sink as winter begins, but remains ice-free. The spring brings large amounts of freshwater from the [[w:Mississippi River|Mississippi River]], which floats on top of the denser ocean water, resulting in a highly stratified ocean. Deep ocean waters in the Gulf of Mexico often lack oxygen because they cannot mix with the surface ocean water (and oxygen atmosphere), and these deep anoxic waters remained locked deep in the basin of the Gulf of Mexico, with the annual influx of spring freshwater and evaporation in late summer warm temperatures.
[[File:Aquatic Dead Zones.jpg|thumb|Areas prone to anoxia or “Dead Zones.”]]

==Catastrophic Mixing of Deep and Surface Ocean Waters==
[[File:NZL orthographic NaturalEarth.svg|thumb|left|New Zealand, including its territorial claim to parts of Antarctica.]]
In 1961, James P. Kennett raced across the mountainous landscape of the [[w:South Island of New Zealand|South Island of New Zealand]] on a motorcycle on a mission. He was searching for rocks. Ever since he was a child growing up in [[w:Wellington|Wellington, New Zealand]], Kennett was collecting rocks, shells and fossils from the beaches and mountains of New Zealand. At 18 he went off to college, having learned all he could about the field of geology from books, but since the subject was not offered at his local school he was eager to learn more at the university. Once enrolled in college classes, he begun working in the geology laboratory at the age of 18. Unlike a biology or chemistry lab, a geology lab is a messy dirty place, where rocks are sliced and cut on saws; boxes of heavy rocks collect dust in cases and drawers; lab coats and beakers are replaced with rock grinders, hammers and chisels.
[[File:Foraminifera hg.jpg|thumb|A planktic fossil foraminifera under magnification.]]
Kennett became interested in tiny marine fossils known as [[w:Foraminifera|foraminifera]], which are studied from either sliced or grounding up rocks. Foraminifera are single celled organisms that live on the ocean floor by feeding on organic detritus that sinks down from the photic zone. They form their protective outer skeleton or shell (test) from [[w:Calcium carbonate|calcium carbonate]]. As common fossils, these tiny fossils accumulate thick deposits on the ocean floor that form marine [[w:Limestone|limestones]]. Limestones such as those used to build the [[w:Giza pyramid complex|Pyramids in Giza]] are actually filled with fossils of these single celled animals. Each rock sample could yield thousands of these tiny fossils, and reveal important clues about the ocean in the past, such as temperature, salinity, acidity, and water depth over long periods of time. As Kennett zoomed down the winding roads of New Zealand, he was on a quest to collect marine deposited rocks that bracket the time of the major climate transition that led to the formation of the great ice sheets in Antarctica. With its close proximity to Antarctica, New Zealand was a good place to study this changing climate, and its effects on the ocean in the ancient marine rocks that now eroded out of the mountains. Kennett was young, and not yet even a graduate student, yet his experiences in the lab made him see the world completely differently. He was eager for his own research, and spent his days hunting new rocks from new periods of time documenting the expansion of the Antarctic sea ice during the late [[w:Miocene|Miocene Epoch]]. His enthusiasm got the attention of his mentors and instructors and was invited to join the crew of the [[w:Antarctic Research Centre#Antarctic Expeditions|Victoria University of Wellington Antarctic Expedition]] in 1962–1963. The expedition was to map the frozen [[w:Transantarctic Mountains|Transantarctic Mountain range]] south of the [[w:Ross Sea|Ross Sea]] and collect rock samples. For Kennett the expedition changed his life, but he continued to document how changes in the ocean over millions of years resulted in an inhospitable cold climate for Antarctic that he experienced firsthand. In 1966 Kennett and his wife moved to the United States, as a pioneer of a new field of research, [[w:Paleoceanography|paleoceanography]], a word he coined for the study of ancient oceans. Kennett was excited over the new research coming from sediment cores that were being drilled offshore. These rock cores contained detailed records of tiny fossil foraminifera spanning millions of years, which unlocked the ancient record of the ocean at each location.
[[File:Joides resolution odp.jpg|left|thumb|Drillship JOIDES Resolution, the U.S. oceanography research vessel.]]
In the 1970s, Kennett began working with [[w:Nicholas Shackleton|Sir Nicholas Shackleton]], the great-nephew of the Antarctic Explorer [[w:Ernest Shackleton|Ernest Shackleton]]. Both were focused on a better understanding of the development of the [[w:Antarctic Circumpolar Current|Antarctic Circumpolar Current]] and how it had resulted in the freezing of the Antarctic Continent, over the last 40 million years. Like Kennett, Shackleton also studied ocean floor sediments, measuring oxygen isotopes of the tiny foraminifera to infer ancient ocean floor temperatures from the past, using a scientific method developed by [[w:Harold Urey|Harold Urey]] in the 1940s. Getting samples drilled off the shore of Antarctica was a challenge affair, but unlike the individual rock samples collected while traveling around New Zealand on motorcycle, a drilled core reveals a more complete record of the sediments laid down over millions of years on the ocean floor. In the 1980s, both men became involved in the [[w:JOIDES Resolution|JOIDES Resolution drilling program]], funded by the United States National Science Foundation, which also funds Antarctic exploration for the United States Government. The drilling program successfully drilled through millions of years of worth of sediment on the ocean floor, retrieving cores that would unlock a 90-million-year long history of ocean floor sedimentation off the coast of Antarctica.

The team was driven as much in seeking to understand the record of the more recent glaciation of Antarctica, as they were in finding the deep layer in the ocean core, that represented the moment when large dinosaurs became extinct. As an expert in foraminifera, Kennett and his colleague Lowell Stott, discovered a point in the recovered sediment core, where the foraminifera underwent a dramatic change. The large healthy foraminifera suddenly disappear in the core, replaced by a reddish mud, nearly absent of foraminifera. This layer also did not correspond with the extinction event that killed off the dinosaurs, but millions of years later at the end of the [[w:Paleocene|Paleocene Epoch]]. Isotopes of oxygen from the sediment indicated that the ocean floor became very warm at this point in time. Kennett and Stott wrote a quick paper describing this catastrophic warming of the deep ocean waters around 56 million years ago near Antarctica in 1991, but soon other scientists observed the same features in rocks and core from around the world. In [[w:Luxor|Luxor, Egypt]], from the same limestone rocks that were used to build the pyramids, geologists observed the same extinction event in rocks dated to 56 million years old and in Northern Wyoming geologists described a global warming event recorded in the Bighorn Basin of the same time affecting the mammals and plants. Something happened 56 million years to dramatically warm the deep ocean waters. The event was named the PETM ([[w:Paleocene–Eocene Thermal Maximum|Paleocene-Eocene Thermal Maximum]]). In the 30 years since the publication by Kennett and Stott, oceanographers have come to the dramatic realization that there can be periods of time when there is catastrophic mixing of deep and surface ocean waters.
[[File:65 Myr Climate Change.png|thumb|Oxygen isotopes from foraminifera in sediment core drilled on the sea floor reveals a history of past warmer ocean waters during the Paleocene and Eocene Epochs, when Antarctica was ice free, the sudden warming event (a spike) at the boundary between the Paleocene and Eocene is the PETM (Paleocene-Eocene Thermal Maximum). ]]

The theory goes like this; 56 million years ago, the [[w:Arctic Ocean|Arctic Ocean]] was only narrowly connected to the North Atlantic. The climate was much warmer today, so warm that the Arctic Ocean remained ice free throughout the year, despite the winter months being dark with the short days due to the high latitude at the North Pole. Rivers would drain into the Arctic Ocean during the spring, bringing freshwater. Since the climate was relatively cold, given its geography, evaporation was minimal. The yearly cycle of freshwater would stack on the colder saltier water each year, resulting in a highly stratified body of water. An example of this type of highly stratified body of water today is the [[w:Black Sea|Black Sea]], but this was on a much larger scale. Each year the North Pole would pass through long summer days, with plenty of sunlight for photosynthesizing phytoplankton, then very short winter days, with little to no sunlight. Each year these blooms of algae and other photosynthesizing organisms would accumulate on the stratified deep ocean seafloor in the Arctic Ocean. Scavenging bacteria would convert this organic matter into [[w:Methane|methane]], which would be trapped on the cold sea floor. This was a ticking bomb.

Around 56 million years ago, a massive set of [[w:Types of volcanic eruptions#Submarine|underwater volcanic eruptions]] exploded on the ocean floor around present day [[w:Iceland|Iceland]] and north into the [[w:Arctic Ocean|Arctic Ocean]]. Warming deep ocean water caused these waters to rise, as warm water is less dense. Methane also undergoes sublimation at warmer temperatures. Sublimation is the transition of a substance directly from a solid to a gas phase. This methane gas bubbled up from the deep ocean floor of the Arctic Ocean, releasing massive amounts of methane into the atmosphere, a strong greenhouse gas. Very quickly the atmosphere became enriched in [[w:Carbon dioxide|carbon dioxide]] as the methane reacted to the oxygen in the atmosphere. Suddenly the global climate became hotter and hotter, and the oceans warmed further. This run-away global warming event began to turn the global ocean acidic, killing off most of the tiny carbonate-shelled animals Kennett has spent his life studying.

Such inversions of the ocean, where the deep ocean waters rise up to the surface, appears to have resulted in widespread anoxia (dead zones), methane release, and major extinctions of marine life due to acidic ocean waters. Such deep-water inversion events can be a consequence of run-away global warming, and the destabilization of the vast amounts of solid methane stored on the ocean floor, and often triggered by massive volcanic events. The heating of deep ocean water, results in the water rising to the surface, which can profoundly affect Earth over short spans of time. The current thermohaline circulation of the World’s Ocean keeps this from happening today (by moving surface ocean water downward in the North Atlantic), but many oceanographers worry about recent [[w:Global warming|anthropogenic global warming]], which could result in another inversion of the ocean, with deep ocean water rising to the surface. Comparable to the short horror story, [[w:The Call of Cthulhu|The Call of Cthulhu]] by [[w:H. P. Lovecraft|Lovecraft]], the deep ocean is a frightful mysterious place, that in a sense, could destroy the world if it so wished.

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