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Ocean gyre

From Wikipedia, the free encyclopedia
(Redirected fromGyre)
Any large system of circulating ocean surface currents
For other uses, seeGyre (disambiguation).
Map showing 5 circles. The first is between western Australia and eastern Africa. The second is between eastern Australia and western South America. The third is between Japan and western North America. Of the two in the Atlantic, one is in hemisphere.
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Map showing 5 circles. The first is between western Australia and eastern Africa. The second is between eastern Australia and western South America. The third is between Japan and western North America. Of the two in the Atlantic, one is in hemisphere.
World map of the five major ocean gyres

Inoceanography, agyre (/ˈdʒaɪər/) is any large system ofocean surface currents moving in a circular fashion driven bywind movements. Gyres are caused by theCoriolis effect; planetaryvorticity, horizontal friction and vertical friction determine the circulatory patterns from thewind stresscurl (torque).[1]

Gyre can refer to any type ofvortex in anatmosphere or asea,[2] even one that is human-created, but it is most commonly used in terrestrialoceanography to refer to the majorocean systems.

Gyre formation

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The largest ocean gyres are wind-driven, meaning that their locations and dynamics are controlled by the prevailingglobal wind patterns:easterlies at the tropics andwesterlies at the midlatitudes. These wind patterns result in a wind stress curl that drivesEkman pumping in the subtropics (resulting in downwelling) andEkman suction in subpolar regions (resulting in upwelling).[3] Ekman pumping results in an increased sea surface height at the center of the gyre and anticyclonicgeostrophic currents in subtropical gyres.[3] Ekman suction results in a depressed sea surface height and cyclonic geostrophic currents in subpolar gyres.[3]

Wind-driven ocean gyres are asymmetrical, with stronger flows on their western boundary and weaker flows throughout their interior. The weak interior flow that is typical over most of the gyre is a result of the conservation ofpotential vorticity. In theshallow water equations (applicable for basin-scale flow as the horizontal length scale is much greater than the vertical length scale), potential vorticity is a function ofrelative (local) vorticityζ{\displaystyle \zeta } (zeta),planetary vorticityf{\displaystyle f}, and the depthH{\displaystyle H}, and is conserved with respect to thematerial derivative:[4]

DDt(ζ+fH)=0{\displaystyle {D \over Dt}\left({\frac {\zeta +f}{H}}\right)=0}

In the case of the subtropical ocean gyre, Ekman pumping results in water piling up in the center of the gyre, compressing water parcels. This results in a decrease inH{\displaystyle H}, so by the conservation of potential vorticity the numeratorζ+f{\displaystyle \zeta +f} must also decrease.[5] It can be further simplified by realizing that, in basin-scale ocean gyres, the relative vorticityζ{\displaystyle \zeta } is small, meaning that local changes in vorticity cannot account for the decrease inH{\displaystyle H}.[5] Thus, the water parcel must change its planetary vorticityf{\displaystyle f} accordingly. The only way to decrease the planetary vorticity is by moving the water parcel equatorward, so throughout the majority of subtropical gyres there is a weak equatorward flow.Harald Sverdrup quantified this phenomenon in his 1947 paper, "Wind Driven Currents in a Baroclinic Ocean",[6] in which the (depth-integrated)Sverdrup balance is defined as:[7]

fVg=βρwE{\displaystyle fV_{g}=\beta \rho w_{E}}

Here,Vg{\displaystyle V_{g}} is themeridional mass transport (positive north),β{\displaystyle \beta } is theRossby parameter,ρ{\displaystyle \rho } is the water density, andwE{\displaystyle w_{E}} is the vertical Ekman velocity due to wind stress curl (positive up). It can be clearly seen in this equation that for a negative Ekman velocity (e.g., Ekman pumping in subtropical gyres), meridional mass transport (Sverdrup transport) is negative (south, equatorward) in the northern hemisphere (f>0{\displaystyle f>0}). Conversely, for a positive Ekman velocity (e.g., Ekman suction in subpolar gyres), Sverdrup transport is positive (north, poleward) in the northern hemisphere.

Two plots of velocity profile, the top of which depicts the flow velocity with a positive slope near the western boundary and the bottom of which depicts the flow velocity with a negative slope near the eastern boundary.
The velocity profile within the boundary layer calculated using Munk's boundary layer solution[8] for both the case of a western boundary (top) and eastern boundary (bottom) in a northern hemisphere subtropical gyre. Note that positive vorticity is input into the flow near the boundary only in the case of the western boundary current, meaning this is the only valid solution to gyre return flow.

Western intensification

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See also:Boundary current § Western intensification

As the Sverdrup balance argues, subtropical ocean gyres have a weak equatorward flow and subpolar ocean gyres have a weak poleward flow over most of their area. However, there must be some return flow that goes against the Sverdrup transport in order to preserve mass balance.[9] In this respect, the Sverdrup solution is incomplete, as it has no mechanism in which to predict this return flow.[9] Contributions by bothHenry Stommel andWalter Munk resolved this issue by showing that the return flow of gyres is done through an intensified western boundary current.[10][8] Stommel's solution relies on a frictional bottom boundary layer which is not necessarily physical in a stratified ocean (currents do not always extend to the bottom).[5]

Two plots: the left one showing a sinusoidal function that represents the winds over a subtropical gyre and the right one showing the resulting gyre circulation in a rectangular basin, which is clockwise around the basin and intensified to the west.
The normalizedstream functionψ{\displaystyle \psi } (right) computed using Munk's boundary layer solution[8] in a rectangular, flat-bottomed ocean gyre on a beta plane in the northern hemisphere centered at 30°N with horizontal length scaleL{\displaystyle L}. The applied windsτ{\displaystyle \tau } (left) are sinusoidal, which is an approximation of the typical winds driving a subtropical gyre. Flow is alongstreamlines (black dotted lines) and the stream function is negative throughout the gyre, indicating the gyre is rotating clockwise. The distance between streamlines is inversely proportional to the flow speed – note the much closer streamlines on the west side of the basin, indicating western intensification of the gyre.

Munk's solution instead relies on friction between the return flow and the sidewall of the basin.[5] This allows for two cases: one with the return flow on the western boundary (western boundary current) and one with the return flow on the eastern boundary (eastern boundary current). A qualitative argument for the presence of western boundary current solutions over eastern boundary current solutions can be found again through the conservation of potential vorticity. Considering again the case of a subtropical northern hemisphere gyre, the return flow must be northward. In order to move northward (an increase in planetary vorticityf{\displaystyle f}), there must be a source of positive relative vorticity to the system. The relative vorticity in the shallow-water system is:[11]

ζ=∂v∂x−∂u∂y{\displaystyle \zeta ={\partial v \over \partial x}-{\partial u \over \partial y}}

Herev{\displaystyle v} is again the meridional velocity andu{\displaystyle u} is thezonal velocity. In the sense of a northward return flow, the zonal component is neglected and only the meridional velocity is important for relative vorticity. Thus, this solution requires that∂v/∂x>0{\displaystyle \partial v/\partial x>0} in order to increase the relative vorticity and have a valid northward return flow in the northern hemisphere subtropical gyre.[5]

Due to friction at the boundary, the velocity of flow must go to zero at the sidewall before reaching some maximum northward velocity within the boundary layer and decaying to the southward Sverdrup transport solution far away from the boundary. Thus, the condition that∂v/∂x>0{\displaystyle \partial v/\partial x>0} can only be satisfied through a western boundary frictional layer, as the eastern boundary frictional layer forces∂v/∂x<0{\displaystyle \partial v/\partial x<0}.[5] One can make similar arguments for subtropical gyres in the southern hemisphere and for subpolar gyres in either hemisphere and see that the result remains the same: the return flow of an ocean gyre is always in the form of a western boundary current.

The western boundary current must transport on the same order of water as the interior Sverdrup transport in a much smaller area. This means western boundary currents are much stronger than interior currents,[5] a phenomenon called "western intensification".

Gyre distribution

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Subtropical gyres

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There are five major subtropical gyres across the world's oceans: the North Atlantic Gyre, the South Atlantic Gyre, the Indian Ocean Gyre, the North Pacific Gyre, and the South Pacific Gyre. All subtropical gyres are anticyclonic, meaning that in the northern hemisphere they rotate clockwise, while the gyres in the southern hemisphere rotate counterclockwise. This is due to theCoriolis force. Subtropical gyres typically consist of four currents: a westward flowing equatorial current, a poleward flowing, narrow, and strong western boundary current, an eastward flowing current in the midlatitudes, and an equatorward flowing, weaker, and broader eastern boundary current.

North Atlantic Gyre

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TheNorth Atlantic Gyre is located in the northern hemisphere in the Atlantic Ocean, between theIntertropical Convergence Zone (ITCZ) in the south and Iceland in the north. TheNorth Equatorial Current brings warm waters west towards the Caribbean and defines the southern edge of the North Atlantic Gyre. Once these waters reach the Caribbean they join the warm waters in the Gulf of Mexico and form theGulf Stream, a western boundary current. This current then heads north and east towards Europe, forming theNorth Atlantic Current. TheCanary Current flows south along the western coast of Europe and north Africa, completing the gyre circulation. The center of the gyre is theSargasso Sea, which is characterized by the dense accumulation ofSargassum seaweed.[12]

South Atlantic Gyre

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TheSouth Atlantic Gyre is located in the southern hemisphere in the Atlantic Ocean, between the Intertropical Convergence Zone in the north and theAntarctic Circumpolar Current to the south. TheSouth Equatorial Current brings water west towards South America, forming the northern boundary of the South Atlantic gyre. Here, the water moves south in theBrazil Current, the western boundary current of the South Atlantic Gyre. The Antarctic Circumpolar Current forms both the southern boundary of the gyre and the eastward component of the gyre circulation. Eventually, the water reaches the west coast of Africa, where it is brought north along the coast as a part of the eastern boundaryBenguela Current, completing the gyre circulation. The Benguela Current experiences theBenguela Niño event, an Atlantic Ocean analogue to the Pacific Ocean'sEl Niño, and is correlated with a reduction in primary productivity in the Benguela upwelling zone.[13]

Indian Ocean Gyre

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TheIndian Ocean Gyre, located in the Indian Ocean, is, like the South Atlantic Gyre, bordered by the Intertropical Convergence Zone in the north and the Antarctic Circumpolar Current to the south. TheSouth Equatorial Current forms the northern boundary of the Indian Ocean Gyre as it flows west along the equator towards the east coast of Africa. At the coast of Africa, the South Equatorial Current is split by Madagascar into theMozambique Current, flowing south through the Mozambique Channel, and theEast Madagascar Current, flowing south along the east coast of Madagascar, both of which are western boundary currents. South of Madagascar the two currents join to form theAgulhas Current.[14] The Agulhas Current flows south until it joins the Antarctic Circumpolar Current, which flows east at the southern edge of the Indian Ocean Gyre. Due to the African continent not extending as far south as the Indian Ocean Gyre, some of the water in theAgulhas Current "leaks" into the Atlantic Ocean, with potentially important effects forglobal thermohaline circulation.[15] The gyre circulation is completed by the north flowingWest Australian Current, which forms the eastern boundary of the gyre.

North Pacific Gyre

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TheNorth Pacific Gyre, one of the largest ecosystems on Earth,[16] is bordered to the south by the Intertropical Convergence Zone and extending north to roughly 50°N. At the southern boundary of the North Pacific Gyre, the North Equatorial Current flows west along the equator towards southeast Asia. TheKuroshio Current is the western boundary current of the North Pacific Gyre, flowing northeast along the coast of Japan. At roughly 50°N, the flow turns east and becomes theNorth Pacific Current. The North Pacific Current flows east, eventually bifurcating near the west coast of North America into the northward flowingAlaska Current and the southward flowingCalifornia Current.[17] The Alaska Current is the eastern boundary current of the subpolar Alaska Gyre,[18] while the California Current is the eastern boundary current that completes the North Pacific Gyre circulation. Within the North Pacific Gyre is theGreat Pacific Garbage Patch, an area of increasedplastic waste concentration.[19]

South Pacific Gyre

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TheSouth Pacific Gyre, like its northern counterpart, is one of the largest ecosystems on Earth with an area that accounts for around 10% of the global ocean surface area.[20] Within this massive area isPoint Nemo, the location on Earth that is farthest away from all continental landmass (2,688 km away from the closest land).[21] The remoteness of this gyre complicates sampling, causing this gyre to be historically under sampled in oceanographic datasets.[22][23] At the northern boundary of the South Pacific Gyre, the South Equatorial Current flows west towards southeast Asia and Australia. There, it turns south as it flows in theEast Australian Current, a western boundary current. The Antarctic Circumpolar Current again returns the water to the east. The flow turns north along the western coast of South America in theHumboldt Current, the eastern boundary current that completes the South Pacific Gyre circulation. Like the North Pacific Gyre, the South Pacific Gyre has an elevated concentration of plastic waste near the center, termed theSouth Pacific garbage patch. Unlike the North Pacific garbage patch which was first described in 1988,[19] the South Pacific garbage patch was discovered much more recently in 2016[24] (a testament to the extreme remoteness of the South Pacific Gyre).

Subpolar gyres

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Subpolar gyres form at high latitudes (around60°). Circulation of surface wind and ocean water is cyclonic, counterclockwise in the northern hemisphere and clockwise in the southern hemisphere, around alow-pressure area, such as the persistentAleutian Low and theIcelandic Low. The wind stress curl in this region drives the Ekman suction, which creates anupwelling of nutrient-rich water from the lower depths.[25]

Subpolar circulation in the southern hemisphere is dominated by theAntarctic Circumpolar Current, due to the lack of large landmasses breaking up theSouthern Ocean. There are minor gyres in theWeddell Sea and theRoss Sea, theWeddell Gyre andRoss Gyre, which circulate in a clockwise direction.

North Atlantic Subpolar Gyre

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The distribution of the North Atlantic Subpolar Gyre shown above the North Atlantic Gyre to the South.

The North Atlantic Subpolar Gyre, located in the North Atlantic Ocean, is characterized by a counterclockwise rotation of surface waters. It plays a crucial role in the global oceanic conveyor belt system, influencing climate and marine ecosystems.[26] The gyre is driven by the convergence of warm, salty waters from the south and cold, fresher waters from the north. As these waters meet, the warm, dense water sinks beneath the lighter, colder water, initiating a complex circulation pattern. The North Atlantic Subpolar Gyre has significant implications for climate regulation, as it helps redistribute heat and nutrients throughout the North Atlantic, influencing weather patterns and supporting diverse marine life. Additionally, changes in the gyre's strength and circulation can impact regional climate variability and may be influenced by broader climate change trends.[26]

TheAtlantic Meridional Overturning Circulation (AMOC) is a key component of the global climate system through its transport of heat and freshwater.[26] The North Atlantic Subpolar Gyre is in a region where the AMOC is actively developed and shaped through mixing and water mass transformation. It is a region where large amounts of heat transported northward by the ocean are released into the atmosphere, thereby modifying the climate of northwest Europe.[27] The North Atlantic Subpolar Gyre has a complex topography with a series of basins in which the large-scale circulation is characterized by cyclonic boundary currents and interior recirculation. The North Atlantic Current develops out of the Gulf Stream extension and turns eastward, crossing the Atlantic in a wide band between about 45°N and 55°N creating the southern border of the North Atlantic Subpolar Gyre. There are several branches of the North Atlantic Current, and they flow into an eastern intergyral region in theBay of Biscay, theRockall Trough, the Iceland Basin, and theIrminger Sea. Part of the North Atlantic Current flows into the Norwegian Sea, and some recirculate within the boundary currents of the subpolar gyre.[26]

Ross Gyre

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TheRoss Gyre is located in theSouthern Ocean surroundingAntarctica, just outside of the Ross Sea. This gyre is characterized by a clockwise rotation of surface waters, driven by the combined influence of wind, the Earth's rotation, and the shape of the seafloor. The gyre plays a crucial role in the transport of heat, nutrients, and marine life in the Southern Ocean, affecting the distribution ofsea ice and influencing regional climate patterns.

TheRoss Sea,Antarctica, is a region where the mixing of distinct water masses and complex interactions with thecryosphere lead to the production and export of dense water, with global-scale impacts.[28] which controls the proximity of the warm waters of the Antarctic Circumpolar Current to the Ross Sea continental shelf, where they may drive ice shelf melting and increase sea level.[29] The deepening of sea level pressures over the Southeast Pacific/Amundsen-Bellingshausen Seas generates a cyclonic circulation cell that reduces sea surface heights north of the Ross Gyre via Ekman suction. The relative reduction of sea surface heights to the north facilitates a northeastward expansion of the outer boundary of the Ross Gyre. Further, the gyre is intensified by a westward ocean stress anomaly over its southern boundary. The ensuing southward Ekman transport anomaly raises sea surface heights over the continental shelf and accelerates the westward throughflow by increasing the cross-slope pressure gradient. Thesea level pressure center may have a greater impact on the Ross Gyre transport or the throughflow, depending on its location and strength. This gyre has significant effects on interactions in the Southern Ocean between waters of the Antarctic margin, the Antarctic Circumpolar Current, and intervening gyres with a strong seasonal sea ice cover play a major role in the climate system.[30]

The Ross Sea is the southernmost sea on Earth and holds the United States'McMurdo Station and ItalianZuchelli Station. Even though this gyre is located nearby two of the most prominent research stations in the world for Antarctic study, the Ross Gyre remains one of the least sampled gyres in the world.[31]

Locations of the Weddell & Ross Gyre's and their distribution in the Southern Ocean.

Weddell Gyre

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TheWeddell Gyre is located in the Southern Ocean surrounding Antarctica, just outside of the Weddell Sea. It is characterized by a clockwise rotation of surface waters, influenced by the combined effects of winds, the Earth's rotation, and the seafloor's topography.[32] Like the Ross Gyre, the Weddell Gyre plays a critical role in the movement of heat, nutrients, and marine life in the Southern Ocean. Insights into the behavior and variability of the Weddell Gyre are crucial for comprehending the interaction between ocean processes in the southern hemisphere and their implications for the global climate system.[32]

This gyre is formed by interactions between theAntarctic Circumpolar Current and theAntarctic Continental Shelf.[33] The Weddell Gyre (WG) is one of the main oceanographic features of the Southern Ocean south of the Antarctic Circumpolar Current which plays an influential role in global ocean circulation as well as gas exchange with the atmosphere.[33] The WG is situated in the Atlantic sector of the Southern Ocean, south of 55–60°S and roughly between 60°W and 30°E (Deacon, 1979). It stretches over the Weddell abyssal plain, where theWeddell Sea is situated, and extends east into the Enderby abyssal plain.[33]

Beaufort Sea Gyre

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Image of the distribution of the Beaufort Sea Gyre and its relationship with the transpolar drift

The anti-cyclonicBeaufort Gyre is the dominant circulation of theCanada Basin and the largest freshwater reservoir in theArctic Ocean's western and northern sectors.[34] The Gyre is characterized by a large-scale, quasi-permanent, counterclockwise rotation of surface waters within theBeaufort Sea. This gyre functions as a critical mechanism for the transport of heat, nutrients, and sea ice within the Arctic region, thus influencing the physical and biological characteristics of the marine environment. Negativewind stress curl over the region, mediated by the sea ice pack, leads to Ekman pumping,downwelling of isopycnal surfaces, and storage of ~20,000 km3 of freshwater in the upper few hundred meters of the ocean.[35] The gyre gains energy from winds in the south and loses energy in the north over a mean annual cycle. The strong atmospheric circulation in the autumn, combined with significant areas of open water, demonstrates the effect that wind stress has directly on the surface geostrophic currents.[36] The Beaufort Gyre and theTranspolar Drift are interconnected due to their relationship in their role in transporting sea ice across the Arctic Ocean. Their influence on the distribution of freshwater has broad impacts for global sea level rise and climate dynamics.

Biogeochemistry of Gyres

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An animation of a year in organism density on Earth. The South Pacific Gyre is visibly low (purple) in organism density.

Depending on their location around the world, gyres can be regions of highbiological productivity or low productivity. Each gyre has a unique ecological profile but can be grouped by region due to dominating characteristics. Generally, productivity is greater for cyclonic gyres (e.g., subpolar gyres) that drive upwelling through Ekman suction and lesser for anticyclonic gyres (e.g., subtropical gyres) that drive downwelling through Ekman pumping, but this can differ between seasons and regions.[37]

Subtropical gyres are sometimes described as "ocean deserts" or "biological deserts", in reference toarid landdeserts where little life exists.[38] Due to theiroligotrophic characteristics, warm subtropical gyres have some of the least productive waters per unit surface area in the ocean.[37] The downwelling of water that occurs in subtropical gyres takes nutrients deeper in the ocean, removing them from surface waters. Organic particles can also be removed from surface waters through gravitational sinking, where the particle is too heavy to remain suspended in the water column.[39] However, since subtropical gyres cover 60% of the ocean surface, their relatively low production per unit area is made up for by covering massive areas of the Earth.[40] This means that, despite being areas of relatively low productivity and low nutrients, they play a large role in contributing to the overall amount of ocean production.[41][42]

In contrast to subtropical gyres, subpolar gyres can have a lot of biological activity due to Ekman suction upwelling driven by wind stress curl.[43] Subpolar gyres in the North Atlantic have a "bloom and crash" pattern following seasonal and storm patterns. The highest productivity in the North Atlantic occurs in boreal spring when there are long days and high levels of nutrients. This is different to the subpolar North Pacific, where almost no phytoplankton bloom occurs and patterns of respiration are more consistent through time than in the North Atlantic.[37]

Nutrient availability

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The distribution of nitrate throughout the global ocean.

Primary production in the ocean is heavily dependent on the presence of nutrients and the availability of sunlight. Here, nutrients refers to nitrogen, nitrate, phosphate, and silicate, all important nutrients in biogeochemical processes that take place in the ocean.[44] A commonly accepted method for relating different nutrient availabilities to each other in order to describe chemical processes is the Redfield, Ketchum, and Richards (RKR) equation. This equation describes the process of photosynthesis and respiration and the ratios of the nutrients involved.[45]

The RKR Equation for Photosynthesis and Respiration:

106CO2+16HNO3+H3PO4+122H2O⟶(CH2O)106(NH3)16H3PO4+138O2{\displaystyle {\ce {106CO2 +16HNO3 +H3PO4 +122H2O ->(CH2O)106(NH3)16H3PO4 +138O2}}}[45]
This plot shows the relationship to nitrogen and phosphorus availability throughout different areas of the global ocean. Nitrogen is most often more limiting than phosphorus for photosynthesis.

With the correct ratios of nutrients on the left side of the RKR equation and sunlight, photosynthesis takes place to produce plankton (primary production) and oxygen. Typically, the limiting nutrients to production are nitrogen and phosphorus with nitrogen being the most limiting.[45]

Lack of nutrients in the surface waters of subtropical gyres is related to the strong downwelling and sinking of particles that occurs in these areas as mentioned earlier. However, nutrients are still present in these gyres. These nutrients can come from not only vertical transport, but also lateral transport across gyre fronts. This lateral transport helps make up for the large loss of nutrients due to downwelling and particle sinking.[46] However, the major source of nitrate in the nitrate-limited subtropical gyres is a result of biological, not physical, factors. Nitrogen in subtropical gyres is produced primarily bynitrogen-fixing bacteria,[47] which are common throughout most of the oligotrophic waters of subtropical gyres.[48] These bacteria transform atmospheric nitrogen into bioavailable forms.

High-nutrient, low-chlorophyll regions

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The Alaskan Gyre and Western Subarctic Gyre are an iron-limited environment rather than a nitrogen or phosphorus limited environment. This region relies on dust blowing off the state of Alaska and other landmasses nearby to supply iron.[49] Because it is limited by iron instead of nitrogen or phosphorus, it is known ashigh-nutrient, low-chlorophyll region.[50][51] Iron limitation in high-nutrient, low-chlorophyll regions results in water that is rich in other nutrients because they have not been removed by the small populations of plankton that live there.[52]

Seasonality in the North Atlantic Subpolar Gyre

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The North Atlantic Subpolar Gyre is an important part of the ocean's carbon dioxide drawdown mechanism. The photosynthesis of phytoplankton communities in this area seasonally depletes surface waters of carbon dioxide, removing it through primary production.[53] This primary production occurs seasonally, with the highest amounts happening in summer.[54] Generally, spring is an important time for photosynthesis as the light limitation imposed during winter is lifted and there are high levels of nutrients available. However, in the North Atlantic Subpolar Gyre, spring productivity is low in comparison to expected levels. It is hypothesized that this low productivity is because phytoplankton are less efficiently using light than they do in the summer months.[54]

Trophic levels

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Ocean gyres typically contain 5–6trophic levels. The limiting factor for the number of trophic levels is the size of thephytoplankton, which are generally small in nutrient limited gyres. In low oxygen zones,oligotrophs are a large percentage of the phytoplankton.[55]

At the intermediate level, small fishes and squid (especiallyommastrephidae) dominate thenektonic biomass. They are important for the transport of energy from low trophic levels to high trophic levels. In some gyres,ommastrephidae are a major part of many animals' diets and can support the existence of largemarine life.[37]

Indigenous knowledge of ocean patterns

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Indigenous Traditional Ecological Knowledge recognizes that Indigenous people, as the original caretakers, hold unique relationships with the land and waters. These relationships make TEK difficult to define, as Traditional Knowledge means something different to each person, each community, and each caretaker. The United Nations Declaration on the Rights of Indigenous Peoples begins by reminding readers that “respect for Indigenous knowledge, cultures and traditional practices contributes to sustainable and equitable development and proper management of the environment”[56] Attempts to collect and store this knowledge have been made over the past twenty years. Conglomerates such as The Indigenous Knowledge Social Network (SIKU)https://siku.org/, the Igliniit project,[57] and the Wales Inupiaq Sea Ice Directory have made strides in the inclusion and documentation of indigenous people's thoughts on global climate, oceanographic, and social trends.

One example involves ancient Polynesians and how they discovered and then travelled throughout the Pacific Ocean from modern day Polynesia to Hawaii and New Zealand. Known aswayfinding, navigators would use the stars, winds, and ocean currents to know where they were on the ocean and where they were headed.[58] These navigators were intimately familiar with Pacific currents that create the North Pacific gyre and this way of navigating continues today.[59]

Another example involves theMāori people who came from Polynesia and are an indigenous group in New Zealand. Their way of life and culture has strong connections to the ocean. The Māori believe that the sea is the source of all life and is an energy, called Tangaroa. This energy could manifest in many different ways, like strong ocean currents, calm seas, or turbulent storms.[60] The Māori have a rich oral history of navigation within the Southern Ocean and Antarctic Ocean and a deep understanding their ice and ocean patterns. A current research project is aimed at consolidating these oral histories.[61] Efforts are being made to integrate TEK with Western science in marine and ocean research in New Zealand.[62] Additional research efforts aim to collate indigenous oral histories and incorporate indigenous knowledge into climate change adaptation practices in New Zealand that will directly affect the Māori and other indigenous communities.[63]

Climate change

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Ocean circulation re-distributes the heat and water-resources, therefore determines the regional climate. For example, the western branches of the subtropical gyres flow from the lower latitudes towards higher latitudes, bringing relatively warm and moist air to the adjacent land, contributing to a mild and wet climate (e.g., East China, Japan). In contrast, the eastern boundary currents of the subtropical gyres streaming from the higher latitudes towards lower latitudes, corresponding to a relatively cold and dry climate (e.g., California).

Currently, the core of the subtropical gyres are around 30° in both Hemispheres. However, their positions were not always there. Satellite observational sea surface height andsea surface temperature data suggest that the world's major ocean gyres are slowly moving towards higher latitudes in the past few decades. Such feature show agreement with climate model prediction under anthropogenic global warming.[64] Paleo-climate reconstruction also suggest that during the past cold climate intervals, i.e., ice ages, some of the western boundary currents (western branches of the subtropical ocean gyres) are closer to the equator than their modern positions.[65][66] These evidence implies that global warming is very likely to push the large-scale ocean gyres towards higher latitudes.[67][68]

Pollution

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This section is an excerpt fromGarbage patch.[edit]
Trash washed ashore inHawaii from theGreat Pacific Garbage Patch

Agarbage patch is a gyre ofmarine debris particles caused by the effects ofocean currents and increasingplastic pollution by human populations. These human-caused collections of plastic and other debris are responsible for ecosystem and environmental problems that affect marine life, contaminate oceans with toxic chemicals, and contribute togreenhouse gas emissions. Once waterborne, marine debris becomes mobile. Flotsam can be blown by the wind, or follow the flow of ocean currents, often ending up in the middle ofoceanic gyres where currents are weakest.

Within garbage patches, the waste is not compact, and although most of it is near the surface of the ocean, it can be found up to more than 30 metres (100 ft) deep in the water.[69] Patches contain plastics and debris in a range of sizes frommicroplastics and small scaleplastic pellet pollution, to large objects such asfishing nets and consumer goods and appliances lost from flood and shipping loss.

Garbage patches grow because of widespread loss of plastic from human trash collection systems. TheUnited Nations Environmental Program estimated that "for every square mile of ocean" there are about "46,000 pieces of plastic".[70] The 10 largest emitters of oceanic plastic pollution worldwide are, from the most to the least, China, Indonesia, Philippines, Vietnam, Sri Lanka, Thailand, Egypt, Malaysia, Nigeria, and Bangladesh,[71] largely through the riversYangtze,Indus,Yellow,Hai,Nile,Ganges,Pearl,Amur,Niger, and theMekong, and accounting for "90 percent of all the plastic that reaches the world's oceans".[72][73] Asia was the leading source of mismanagedplastic waste, with China alone accounting for 2.4 million metric tons.[74]

The best known of these is theGreat Pacific Garbage Patch which has the highest density of marine debris and plastic. The Pacific Garbage patch has two mass buildups: the western garbage patch and the eastern garbage patch, the former off the coast ofJapan and the latter betweenCalifornia andHawaii. These garbage patches contain 90 million tonnes (100 million short tons) of debris.[69] Other identified patches include theNorth Atlantic garbage patch between North America and Africa, theSouth Atlantic garbage patch located between eastern South America and the tip of Africa, theSouth Pacific garbage patch located west of South America, and theIndian Ocean garbage patch found east of South Africa listed in order of decreasing size.[75]

See also

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Wikimedia Commons has media related toOceanic gyres.

References

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  1. ^Heinemann, B. and the Open University (1998)Ocean circulation, Oxford University Press: Page 98
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