Thermohaline circulation - wikipedia Thermohaline circulation A summary of the path of the thermohaline circulation. Blue paths represent deep - water currents, while red paths represent surface currents. Play media Thermohaline circulation Thermohaline circulation ( THC ) is a part of the large - scale ocean circulation that is driven by global density gradients created by surface heat and freshwater fluxes. The adjective thermohaline derives from thermo - referring to temperature and - haline referring to salt content, factors which together determine the density of sea water. Wind - driven surface currents ( such as the Gulf Stream ) travel polewards from the equatorial Atlantic Ocean, cooling en route, and eventually sinking at high latitudes ( forming North Atlantic Deep Water ). This dense water then flows into the ocean basins. While the bulk of it upwells in the Southern Ocean, the oldest waters ( with a transit time of around 1000 years ) upwell in the North Pacific. Extensive mixing therefore takes place between the ocean basins, reducing differences between them and making the Earth 's oceans a global system. On their journey, the water masses transport both energy ( in the form of heat ) and matter ( solids, dissolved substances and gases ) around the globe. As such, the state of the circulation has a large impact on the climate of the Earth. The thermohaline circulation is sometimes called the ocean conveyor belt, the great ocean conveyor, or the global conveyor belt. On occasion, it is used to refer to the meridional overturning circulation ( often abbreviated as MOC ). The term MOC is more accurate and well defined, as it is difficult to separate the part of the circulation which is driven by temperature and salinity alone as opposed to other factors such as the wind and tidal forces. Moreover, temperature and salinity gradients can also lead to circulation effects that are not included in the MOC itself. Contents 1 Overview 1.1 Formation of deep water masses 1.2 Movement of deep water masses 1.3 Quantitative estimation 2 Gulf Stream 3 Upwelling 4 Effects on global climate 4.1 Shutdown of thermohaline circulation 5 See also 6 References 7 Other sources 8 External links Overview The global conveyor belt on a continuous - ocean map The movement of surface currents pushed by the wind is fairly intuitive. For example, the wind easily produces ripples on the surface of a pond. Thus the deep ocean -- devoid of wind -- was assumed to be perfectly static by early oceanographers. However, modern instrumentation shows that current velocities in deep water masses can be significant ( although much less than surface speeds ). In general, ocean water velocities range from fractions of centimeters per second ( in the depth of the oceans ) to sometimes more than 1 m / s in surface currents like the Gulf Stream and Kuroshio. In the deep ocean, the predominant driving force is differences in density, caused by salinity and temperature variations ( increasing salinity and lowering the temperature of a fluid both increase its density ). There is often confusion over the components of the circulation that are wind and density driven. Note that ocean currents due to tides are also significant in many places ; most prominent in relatively shallow coastal areas, tidal currents can also be significant in the deep ocean. There they are currently thought to facilitate mixing processes, especially diapycnal mixing. The density of ocean water is not globally homogeneous, but varies significantly and discretely. Sharply defined boundaries exist between water masses which form at the surface, and subsequently maintain their own identity within the ocean. But these sharp boundaries are not to be imagined spatially but rather in a T-S - diagram where water masses are distinguished. They position themselves above or below each other according to their density, which depends on both temperature and salinity. Warm seawater expands and is thus less dense than cooler seawater. Saltier water is denser than fresher water because the dissolved salts fill interstices between water molecules, resulting in more mass per unit volume. Lighter water masses float over denser ones ( just as a piece of wood or ice will float on water, see buoyancy ). This is known as `` stable stratification '' as opposed to unstable stratification ( see Bruunt - Väisälä frequency ) where denser waters are located over less dense waters ( see convection or deep convection needed for water mass formation ). When dense water masses are first formed, they are not stably stratified, so they seek to locate themselves in the correct vertical position according to their density. This motion is called convection, it orders the stratification by gravitation. Driven by the density gradients this sets up the main driving force behind deep ocean currents like the deep western boundary current ( DWBC ). The thermohaline circulation is mainly driven by the formation of deep water masses in the North Atlantic and the Southern Ocean caused by differences in temperature and salinity of the water. The great quantities of dense water sinking at high latitudes must be offset by equal quantities of water rising elsewhere. Note that cold water in polar zones sink relatively rapidly over a small area, while warm water in temperate and tropical zones rise more gradually across a much larger area. It then slowly returns poleward near the surface to repeat the cycle. The continual diffuse upwelling of deep water maintains the existence of the permanent thermocline found everywhere at low and mid-latitudes. This model was described by Henry Stommel and Arnold B. Arons in 1960 and is known as the Stommel - Arons box model for the MOC. This slow upward movement is approximated to be about 1 centimeter ( 0.5 inch ) per day over most of the ocean. If this rise were to stop, downward movement of heat would cause the thermocline to descend and would reduce its steepness. Formation of deep water masses The dense water masses that sink into the deep basins are formed in quite specific areas of the North Atlantic and the Southern Ocean. In the North Atlantic, seawater at the surface of the ocean is intensely cooled by the wind and low ambient air temperatures. Wind moving over the water also produces a great deal of evaporation, leading to a decrease in temperature, called evaporative cooling related to latent heat. Evaporation removes only water molecules, resulting in an increase in the salinity of the seawater left behind, and thus an increase in the density of the water mass along with the decrease in temperature. In the Norwegian Sea evaporative cooling is predominant, and the sinking water mass, the North Atlantic Deep Water ( NADW ), fills the basin and spills southwards through crevasses in the submarine sills that connect Greenland, Iceland and Great Britain which are known as the Greenland - Scotland - Ridge. It then flows very slowly into the deep abyssal plains of the Atlantic, always in a southerly direction. Flow from the Arctic Ocean Basin into the Pacific, however, is blocked by the narrow shallows of the Bering Strait. Diagram showing relation between temperature and salinity for sea water density maximum and sea water freezing temperature. In the Southern Ocean, strong katabatic winds blowing from the Antarctic continent onto the ice shelves will blow the newly formed sea ice away, opening polynyas along the coast. The ocean, no longer protected by sea ice, suffers a brutal and strong cooling ( see polynya ). Meanwhile, sea ice starts reforming, so the surface waters also get saltier, hence very dense. In fact, the formation of sea ice contributes to an increase in surface seawater salinity ; saltier brine is left behind as the sea ice forms around it ( pure water preferentially being frozen ). Increasing salinity lowers the freezing point of seawater, so cold liquid brine is formed in inclusions within a honeycomb of ice. The brine progressively melts the ice just beneath it, eventually dripping out of the ice matrix and sinking. This process is known as brine rejection. The resulting Antarctic Bottom Water ( AABW ) sinks and flows north and east, but is so dense it actually underflows the NADW. AABW formed in the Weddell Sea will mainly fill the Atlantic and Indian Basins, whereas the AABW formed in the Ross Sea will flow towards the Pacific Ocean. The dense water masses formed by these processes flow downhill at the bottom of the ocean, like a stream within the surrounding less dense fluid, and fill up the basins of the polar seas. Just as river valleys direct streams and rivers on the continents, the bottom topography constrains the deep and bottom water masses. Note that, unlike fresh water, seawater does not have a density maximum at 4 ° C but gets denser as it cools all the way to its freezing point of approximately − 1.8 ° C. This freezing point is however a function of salinity and pressure and thus - 1.8 ° C is not a general freezing temperature for sea water ( see diagram to the right ). Movement of deep water masses Formation and movement of the deep water masses at the North Atlantic Ocean, creates sinking water masses that fill the basin and flows very slowly into the deep abyssal plains of the Atlantic. This high - latitude cooling and the low - latitude heating drives the movement of the deep water in a polar southward flow. The deep water flows through the Antarctic Ocean Basin around South Africa where it is split into two routes : one into the Indian Ocean and one past Australia into the Pacific. At the Indian Ocean, some of the cold and salty water from the Atlantic -- drawn by the flow of warmer and fresher upper ocean water from the tropical Pacific -- causes a vertical exchange of dense, sinking water with lighter water above. It is known as overturning. In the Pacific Ocean, the rest of the cold and salty water from the Atlantic undergoes haline forcing, and becomes warmer and fresher more quickly. The out - flowing undersea of cold and salty water makes the sea level of the Atlantic slightly lower than the Pacific and salinity or halinity of water at the Atlantic higher than the Pacific. This generates a large but slow flow of warmer and fresher upper ocean water from the tropical Pacific to the Indian Ocean through the Indonesian Archipelago to replace the cold and salty Antarctic Bottom Water. This is also known as ' haline forcing ' ( net high latitude freshwater gain and low latitude evaporation ). This warmer, fresher water from the Pacific flows up through the South Atlantic to Greenland, where it cools off and undergoes evaporative cooling and sinks to the ocean floor, providing a continuous thermohaline circulation. Hence, a recent and popular name for the thermohaline circulation, emphasizing the vertical nature and pole - to - pole character of this kind of ocean circulation, is the meridional overturning circulation. Quantitative estimation Direct estimates of the strength of the thermohaline circulation have been made at 26.5 ° N in the North Atlantic since 2004 by the UK - US RAPID programme. By combining direct estimates of ocean transport using current meters and subsea cable measurements with estimates of the geostrophic current from temperature and salinity measurements, the RAPID programme provides continuous, full - depth, basinwide estimates of the thermohaline circulation or, more accurately, the meridional overturning circulation. The deep water masses that participate in the MOC have chemical, temperature and isotopic ratio signatures and can be traced, their flow rate calculated, and their age determined. These include Pa / Th ratios. Gulf Stream Main article : Gulf Stream Benjamin Franklin 's map of the Gulf Stream The Gulf Stream, together with its northern extension towards Europe, the North Atlantic Drift, is a powerful, warm, and swift Atlantic ocean current that originates at the tip of Florida, and follows the eastern coastlines of the United States and Newfoundland before crossing the Atlantic Ocean. The process of western intensification causes the Gulf Stream to be a northward accelerating current off the east coast of North America. At about 40 ° 0 ′ N 30 ° 0 ′ W ﻿ / ﻿ 40.000 ° N 30.000 ° W ﻿ / 40.000 ; - 30.000, it splits in two, with the northern stream crossing to northern Europe and the southern stream recirculating off West Africa. The Gulf Stream influences the climate of the east coast of North America from Florida to Newfoundland, and the west coast of Europe. Although there has been recent debate, there is consensus that the climate of Western Europe and Northern Europe is warmer than it would otherwise be due to the North Atlantic drift, one of the branches from the tail of the Gulf Stream. It is part of the North Atlantic Gyre. Its presence has led to the development of strong cyclones of all types, both within the atmosphere and within the ocean. The Gulf Stream is also a significant potential source of renewable power generation. Upwelling Main article : Upwelling All these dense water masses sinking into the ocean basins displace the older deep water masses that were made less dense by ocean mixing. To maintain a balance, water must be rising elsewhere. However, because this thermohaline upwelling is so widespread and diffuse, its speeds are very slow even compared to the movement of the bottom water masses. It is therefore difficult to measure where upwelling occurs using current speeds, given all the other wind - driven processes going on in the surface ocean. Deep waters have their own chemical signature, formed from the breakdown of particulate matter falling into them over the course of their long journey at depth. A number of scientists have tried to use these tracers to infer where the upwelling occurs. Wallace Broecker, using box models, has asserted that the bulk of deep upwelling occurs in the North Pacific, using as evidence the high values of silicon found in these waters. Other investigators have not found such clear evidence. Computer models of ocean circulation increasingly place most of the deep upwelling in the Southern Ocean, associated with the strong winds in the open latitudes between South America and Antarctica. While this picture is consistent with the global observational synthesis of William Schmitz at Woods Hole and with low observed values of diffusion, not all observational syntheses agree. Recent papers by Lynne Talley at the Scripps Institution of Oceanography and Bernadette Sloyan and Stephen Rintoul in Australia suggest that a significant amount of dense deep water must be transformed to light water somewhere north of the Southern Ocean. Effects on global climate The thermohaline circulation plays an important role in supplying heat to the polar regions, and thus in regulating the amount of sea ice in these regions, although poleward heat transport outside the tropics is considerably larger in the atmosphere than in the ocean. Changes in the thermohaline circulation are thought to have significant impacts on the Earth 's radiation budget. Insofar as the thermohaline circulation governs the rate at which deep waters are exposed to the surface, it may also play an important role in the concentration of carbon dioxide in the atmosphere. While it is often stated that the thermohaline circulation is the primary reason that Western Europe is so temperate, it has been suggested that this is largely incorrect, and that Europe is warm mostly because it lies downwind of an ocean basin, and because of the effect of atmospheric waves bringing warm air north from the subtropics. However, the underlying assumptions of this particular analysis have likewise been challenged. Large influxes of low - density meltwater from Lake Agassiz and deglaciation in North America are thought to have led to a shifting of deep water formation and subsidence in the extreme North Atlantic and caused the climate period in Europe known as the Younger Dryas. Shutdown of thermohaline circulation Main article : Shutdown of thermohaline circulation See also : Deglaciation and Cold blob ( North Atlantic ) In 2005, British researchers noticed that the net flow of the northern Gulf Stream had decreased by about 30 % since 1957. Coincidentally, scientists at Woods Hole had been measuring the freshening of the North Atlantic as Earth becomes warmer. Their findings suggested that precipitation increases in the high northern latitudes, and polar ice melts as a consequence. By flooding the northern seas with lots of extra fresh water, global warming could, in theory, divert the Gulf Stream waters that usually flow northward, past the British Isles and Norway, and cause them to instead circulate toward the Equator. If this were to happen, Europe 's climate would be seriously impacted. Downturn of AMOC ( Atlantic meridional overturning circulation ), has been tied to extreme regional sea level rise. In 2013, an unexpected significant weakening of the THC led to one of the quietest Atlantic hurricane seasons observed since 1994. The main cause of the inactivity was caused by a continuation of the spring pattern across the Atlantic basin. See also Atlantic Multidecadal Oscillation ( AMO ) ( in regard to `` sea surface temperature '' ) Climate change Contourite Downwelling Halothermal circulation Hydrothermal circulation Shutdown of thermohaline circulation Upwelling References Jump up ^ Rahmstorf, S ( 2003 ). `` The concept of the thermohaline circulation '' ( PDF ). Nature. 421 ( 6924 ) : 699. Bibcode : 2003Natur. 421... 699R. doi : 10.1038 / 421699a. PMID 12610602. Jump up ^ Lappo, SS ( 1984 ). `` On reason of the northward heat advection across the Equator in the South Pacific and Atlantic ocean ''. Study of Ocean and Atmosphere Interaction Processes. Moscow Department of Gidrometeoizdat ( in Mandarin ) : 125 -- 9. Jump up ^ The global ocean conveyor belt is a constantly moving system of deep - ocean circulation driven by temperature and salinity ; What is the global ocean conveyor belt ? Jump up ^ Primeau, F ( 2005 ). `` Characterizing transport between the surface mixed layer and the ocean interior with a forward and adjoint global ocean transport model ''. Journal of Physical Oceanography. 35 ( 4 ) : 545 -- 64. Bibcode : 2005JPO... 35... 545P. doi : 10.1175 / JPO2699. 1. Jump up ^ Wunsch, C ( 2002 ). `` What is the thermohaline circulation ? ''. Science. 298 ( 5596 ) : 1179 -- 81. doi : 10.1126 / science. 1079329. PMID 12424356. Jump up ^ Wyrtki, K ( 1961 ). `` The thermohaline circulation in relation to the general circulation in the oceans ''. Deep - Sea Research. 8 ( 1 ) : 39 -- 64. Bibcode : 1961DSR... 8... 39W. doi : 10.1016 / 0146 - 6313 ( 61 ) 90014 - 4. Jump up ^ Schmidt, G., 2005, Gulf Stream slowdown ?, RealClimate Jump up ^ Eden, Carsten ( 2012 ). Ocean Dynamics. Springer. p. 177. ISBN 978 - 3 - 642 - 23449 - 1. Jump up ^ Stommel, H., & Arons, A.B. ( 1960 ). On the abyssal circulation of the world ocean. -- I. Stationary planetary flow patterns on a sphere. Deep Sea Research ( 1953 ), 6, 140 - 154. Jump up ^ United Nations Environment Programme / GRID - Arendal, 2006, ( 1 ). Potential Impact of Climate Change Jump up ^ `` RAPID : monitoring the Atlantic Meridional Overturning Circulation at 26.5 N since 2004 ''. Jump up ^ National Environmental Satellite, Data, and Information Service ( 2009 ). Investigating the Gulf Stream Archived 3 May 2010 at the Wayback Machine... North Carolina State University Retrieved 6 May 2009 Jump up ^ Hennessy ( 1858 ). Report of the Annual Meeting : On the Influence of the Gulf - stream on the Climate of Ireland. Richard Taylor and William Francis. Retrieved 6 January 2009. Jump up ^ `` Satellites Record Weakening North Atlantic Current Impact ''. NASA. Retrieved 10 September 2008. Jump up ^ The Institute for Environmental Research & Eductation. Tidal. pdf Archived 11 October 2010 at the Wayback Machine. Retrieved on 28 July 2010. Jump up ^ Jeremy Elton Jacquot. Gulf Stream 's Tidal Energy Could Provide Up to a Third of Florida 's Power Retrieved 21 September 2008 Jump up ^ Marshall, John ; Speer, Kevin ( 26 February 2012 ). `` Closure of the meridional overturning circulation through Southern Ocean upwelling ''. Nature Geoscience. 5 ( 3 ) : 171 -- 180. Bibcode : 2012NatGe... 5... 171M. doi : 10.1038 / ngeo1391. Jump up ^ Trenberth, K ; Caron, J ( 2001 ). `` Estimates of Meridional Atmosphere and Ocean Heat Transports ''. Journal of Climate. 14 ( 16 ) : 3433 -- 43. Bibcode : 2001JCli... 14.3433 T. doi : 10.1175 / 1520 - 0442 ( 2001 ) 014 < 3433 : EOMAAO > 2.0.CO ; 2. Jump up ^ Seager, R., 2006, The Source of Europe 's Mild Climate, American Scientist Jump up ^ Rhines and Hakkinen, 2003, Is the Oceanic Heat Transport in the North Atlantic Irrelevant to the Climate in Europe ? Archived 16 July 2007 at the Wayback Machine. ASOF Newsletter Jump up ^ Broecker, WS ( 2006 ). `` Was the Younger Dryas Triggered by a Flood ? ''. Science. 312 ( 5777 ) : 1146 -- 8. doi : 10.1126 / science. 1123253. PMID 16728622. Jump up ^ Garrison, Tom ( 2009 ). Oceanography : An Invitation to Marine Science ( 7th ed. ). Cengage Learning. p. 582. ISBN 9780495391937. Jump up ^ Bryden, H.L. ; H.R. Longworth ; S.A. Cunningham ( 2005 ). `` Slowing of the Atlantic meridional overturning circulation at 25 ° N ''. Nature. 438 ( 7068 ) : 655 -- 657. Bibcode : 2005Natur. 438... 655B. doi : 10.1038 / nature04385. PMID 16319889. Jump up ^ Curry, R. ; C. Mauritzen ( 2005 ). `` Dilution of the northern North Atlantic in recent decades ''. Science. 308 : 1772 -- 1774. Bibcode : 2005Sci... 308.1772 C. doi : 10.1126 / science. 1109477. PMID 15961666. Jump up ^ Jianjun Yin ; Stephen Griffies ( 25 March 2015 ). `` Extreme sea level rise event linked to AMOC downturn ''. CLIVAR. Other sources Apel, JR ( 1987 ). Principles of Ocean Physics. Academic Press. ISBN 0 - 12 - 058866 - 8. Gnanadesikan, A. ; R.D. Slater ; P.S. Swathi ; G.K. Vallis ( 2005 ). `` The energetics of ocean heat transport ''. Journal of Climate. 18 ( 14 ) : 2604 -- 16. Bibcode : 2005JCli... 18.2604 G. doi : 10.1175 / JCLI3436. 1. Knauss, JA ( 1996 ). Introduction to Physical Oceanography. Prentice Hall. ISBN 0 - 13 - 238155 - 9. `` Potential Impact of Climate Change ''. United Nations Environment Programme / GRID - Arendal. 2006. Rahmstorf, S ( 2006 ). `` Thermohaline Ocean Circulation '' ( PDF ). In Elias, S.A. Encyclopedia of Quaternary Sciences. Elsevier Science. ISBN 0 - 444 - 52747 - 8. External links Ocean Conveyor Belt THOR FP7 projects http://arquivo.pt/wayback/20141126093524/http%3A//www.eu%2Dthor.eu/ investigates on the topic `` Thermohaline overturning - at risk ? '' and the predictability of changes of the THC. THOR is financed by the 7th Framework Programme of the European Commission. Atmospheric, oceanographic and climate models Model types Atmospheric model Climate model Numerical weather prediction Tropical cyclone forecast model Atmospheric dispersion modeling Chemical transport model Upper - atmospheric models Ensemble forecasting Model output statistics Meteorological reanalysis Parametrization Specific models Climate IGCM HadCM3 HadGEM1 GFDL CM2. X CGCM CCSM CESM CFSv2 ECHAM MPAS Global weather IFS ( ECMWF ) FIM GEM / GDPS GFS NAEFS NAVGEM UM JMA - GSM GME / ICON ARPEGE Regional and mesoscale atmospheric NAM RR / RAP RAMS WRF RAQMS HIRLAM LAPS RPM Regional and mesoscale oceanographic HyCOM ROMS POM MOM FVCOM MITgcm FESOM Atmospheric dispersion ADMS AERMOD ATSTEP AUSTAL2000 CALPUFF DISPERSION21 ISC3 MEMO MERCURE NAME OSPM PUFF - PLUME RIMPUFF SAFE AIR Chemical transport CLaMS MOZART GEOS - Chem Land surface parametrization JULES CLASS ISBA Discontinued AVN / MRF / GSM Eta LFM MM5 NGM NOGAPS RUC Mathematical model Statistical model Scientific modelling Computer simulation Ocean currents and gyres Currents Arctic Ocean East Greenland North Icelandic Norwegian Transpolar Drift Stream Atlantic Ocean Angola Antilles Azores Baffin Island Benguela Brazil Canary Cape Horn Caribbean East Greenland East Iceland Falkland Florida Guinea Gulf Stream Irminger Labrador Lomonosov Loop North Atlantic North Brazil North Equatorial Norwegian Portugal Slope Jet South Atlantic South Equatorial West Greenland West Spitsbergen Indian Ocean Agulhas Agulhas Return East Madagascar Equatorial Counter Indian Monsoon Indonesian Throughflow Leeuwin Madagascar Mozambique North Madagascar Somali South Australian South Equatorial West Australian Pacific Ocean Alaska Aleutian California Cromwell Davidson East Australian East Korea Warm Equatorial Counter Humboldt Indonesian Throughflow Kamchatka Kuroshio Mindanao North Equatorial North Korea Cold North Pacific Oyashio South Equatorial Tasman Front Southern Ocean Antarctic Circumpolar Tasman Outflow Gyres Major gyres Indian Ocean Gyre North Atlantic Gyre South Atlantic Gyre North Pacific Gyre South Pacific Gyre Other gyres Beaufort Gyre Ross Gyre Weddell Gyre Related Atmospheric circulation Boundary current Coriolis force Ekman transport Marine debris Marine garbage patches Great Pacific Indian Ocean North Atlantic South Pacific Thermohaline circulation Physical oceanography Waves Airy wave theory Ballantine scale Benjamin -- Feir instability Boussinesq approximation Breaking wave Clapotis Cnoidal wave Cross sea Dispersion Edge wave Equatorial waves Fetch Gravity wave Green 's law Infragravity wave Internal wave Iribarren number Kelvin wave Kinematic wave Longshore drift Luke 's variational principle Mild - slope equation Radiation stress Rogue wave Rossby wave Rossby - gravity waves Sea state Seiche Significant wave height Soliton Stokes boundary layer Stokes drift Stokes wave Swell Trochoidal wave Tsunami megatsunami Undertow Ursell number Wave action Wave base Wave height Wave power Wave radar Wave setup Wave shoaling Wave turbulence Wave -- current interaction Waves and shallow water one - dimensional Saint - Venant equations shallow water equations Wind wave model Circulation Atmospheric circulation Baroclinity Boundary current Coriolis force Coriolis -- Stokes force Craik -- Leibovich vortex force Downwelling Eddy Ekman layer Ekman spiral Ekman transport El Niño -- Southern Oscillation General circulation model Geostrophic current Global Ocean Data Analysis Project Gulf Stream Halothermal circulation Humboldt Current Hydrothermal circulation Langmuir circulation Longshore drift Loop Current Modular Ocean Model Ocean dynamics Ocean gyre Princeton Ocean Model Rip current Subsurface currents Sverdrup balance Thermohaline circulation shutdown Upwelling Whirlpool World Ocean Circulation Experiment Tides Amphidromic point Earth tide Head of tide Internal tide Lunitidal interval Perigean spring tide Rip tide Rule of twelfths Slack water Tidal bore Tidal force Tidal power Tidal race Tidal range Tidal resonance Tide gauge Tideline Landforms Abyssal fan Abyssal plain Atoll Bathymetric chart Coastal geography Cold seep Continental margin Continental rise Continental shelf Contourite Guyot Hydrography Oceanic basin Oceanic plateau Oceanic trench Passive margin Seabed Seamount Submarine canyon Submarine volcano Plate tectonics Convergent boundary Divergent boundary Fracture zone Hydrothermal vent Marine geology Mid-ocean ridge Mohorovičić discontinuity Vine -- Matthews -- Morley hypothesis Oceanic crust Outer trench swell Ridge push Seafloor spreading Slab pull Slab suction Slab window Subduction Transform fault Volcanic arc Ocean zones Benthic Deep ocean water Deep sea Littoral Mesopelagic Oceanic Pelagic Photic Surf Swash Sea level Deep - ocean Assessment and Reporting of Tsunamis Future sea level Global Sea Level Observing System North West Shelf Operational Oceanographic System Sea - level curve Sea level rise World Geodetic System Acoustics Deep scattering layer Hydroacoustics Ocean acoustic tomography Sofar bomb SOFAR channel Underwater acoustics Satellites Jason - 1 Jason - 2 ( Ocean Surface Topography Mission ) Jason - 3 Related Argo Benthic lander Color of water DSV Alvin Marginal sea Marine energy Marine pollution Mooring National Oceanographic Data Center Ocean Ocean exploration Ocean observations Ocean reanalysis Ocean surface topography Ocean thermal energy conversion Oceanography Pelagic sediment Sea surface microlayer Sea surface temperature Seawater Science On a Sphere Thermocline Underwater glider Water column World Ocean Atlas Commons Retrieved from `` https://en.wikipedia.org/w/index.php?title=Thermohaline_circulation&oldid=821758743 '' Categories : Physical oceanography Chemical oceanography Climate change Climate forcing agents Hidden categories : Webarchive template wayback links Use dmy dates from September 2015 Wikipedia articles needing clarification from October 2017 Articles containing video clips Talk Contents About Wikipedia Беларуская Català Čeština Dansk Deutsch Eesti Español فارسی Français Gaeilge Galego 한국어 Hrvatski Italiano עברית Lietuvių Bahasa Melayu Nederlands 日本 語 Norsk Polski Português Русский Српски / srpski Srpskohrvatski / српскохрватски Suomi Svenska Taqbaylit Türkçe Українська 中文 Edit links This page was last edited on 22 January 2018, at 13 : 20. Text is available under the Creative Commons Attribution - ShareAlike License ; additional terms may apply. By using this site, you agree to the Terms of Use and Privacy Policy. Wikipedia ® is a registered trademark of the Wikimedia Foundation, Inc., a non-profit organization. About Wikipedia

Question: where does wind move from during thermohaline circulation
Answer: global density gradients