Thermohaline circulation (from Britannica)
The general circulation of the oceans consists primarily of the wind-driven
currents. These, however, are superimposed on the much more sluggish circulation driven by
horizontal differences in temperature and salinity—namely, the thermohaline circulation. The
thermohaline circulation reaches down to the seafloor and is often referred to as the deep, or
abyssal, ocean circulation. Measuring seawater temperature and salinity distribution is the chief
method of studying the deep-flow patterns. Other properties also are examined; for example, the
concentrations of oxygen, carbon-14, and such synthetically produced compounds as
chlorofluorocarbons are measured to obtain resident times and spreading rates of deep water.
In some areas of the ocean, generally during the winter season, cooling or net evaporation causes
surface water to become dense enough to sink. Convection penetrates to a level where the
density of the sinking water matches that of the surrounding water. It then spreads slowly into
the rest of the ocean. Other water must replace the surface water that sinks. This sets up the
thermohaline circulation. The basic thermohaline circulation is one of sinking of cold water in
the polar regions, chiefly in the northern North Atlantic and near Antarctica. These dense water
masses spread into the full extent of the ocean and gradually upwell to feed a slow return flow to
the sinking regions. A theory for the thermohaline circulation pattern was proposed by Stommel
and Arnold Arons in 1960.
In the Northern Hemisphere, the primary region of deep water formation is the North Atlantic;
minor amounts of deep water are formed in the Red Sea and Persian Gulf. A variety of water
types contribute to the so-called North Atlantic Deep Water. Each one of them differs, though
they share a common attribute of being relatively warm (greater than 2° C) and salty (greater
than 34.9 parts per thousand) compared with the other major producer of deep and bottom water,
the Southern Ocean (0° C and 34.7 parts per thousand). North Atlantic Deep Water is primarily
formed in the Greenland and Norwegian seas, where cooling of the salty water introduced by the
Norwegian Current induces sinking. This water spills over the rim of the ridge that stretches
from Greenland to Scotland, extending to the seafloor to the south as a convective plume. It then
flows southward, pressed against the western edge of the North Atlantic. Additional deep water
is formed in the Labrador Sea. This water, somewhat less dense than the overflow water from the
Greenland and Norwegian seas, has been observed sinking to a depth of 3,000 metres within
convective features referred to as chimneys. Vertical velocities as high as 10 centimetres per
second have been observed within these convective features. A third variety of North Atlantic
Deep Water is derived from net evaporation within the Mediterranean Sea. This draws surface
water into the Mediterranean through the Strait of Gibraltar. The mass of salty water formed
within the Mediterranean exits as a deeper stream. It descends to depths of 1,000 to 2,000 metres
in the North Atlantic Ocean, forming the uppermost layer of North Atlantic Deep Water. The
outflow in the Strait of Gibraltar reaches as high as 2 metres per second, but its total transport
amounts to only 5 percent of the total North Atlantic Deep Water formed. The outflow of the
Mediterranean plays a significant role in boosting the salinity of North Atlantic Deep Water.
The blend of North Atlantic Deep Water, with a total formation rate of 15 to 20 × 106 cubic
metres per second, quickly ventilates the Atlantic Ocean, resulting in a residence time of less
than 200 years. The deep water spreads away from its source along the western side of the
Atlantic Ocean and, on reaching the Antarctic Circumpolar Current, spreads into the Indian and
Pacific oceans. The sinking of North Atlantic Deep Water is compensated for by the slow
upwelling of deep water, mainly in the Southern Ocean, to replenish the upper stratum of water
that has descended as North Atlantic Deep Water. North Atlantic Deep Water exported to the
other oceans must be balanced by the inflow of upper-layer water into the Atlantic. Some water
returns as cold, low-salinity Pacific water through the Drake Passage in the form of what is
known as Antarctic Intermediate Water, and some returns as warm salty thermocline water from
the Indian Ocean around the southern rim of Africa.
Remnants of North Atlantic Deep Water mix with Southern Ocean water to spread along the
seafloor into the North Pacific Ocean. Here, it upwells to a level of 2,000–3,000 metres and
returns to the south lower in salinity and oxygen but higher in nutrient concentrations as North
Pacific Deep Water. This North Pacific Deep Water is eventually swept eastward with the
Antarctic Circumpolar Current. Modification of deep water in the North Pacific is the direct
consequence of vertical mixing, which carries into the deep ocean the low salinity properties of
North Pacific Intermediate Water. The latter is formed in the northwestern Pacific Ocean.
Because of the immenseness of the North Pacific and the extremely long residence time (more
than 500 years) of the water, enormous quantities of North Pacific Deep Water can be produced
by vertical mixing.
Considerable volumes of cold water generally of low salinity are formed in the Southern Ocean.
Such water masses spread into the interior of the global ocean and to a large extent are
responsible for the anomalous cold, low-salinity state of the modern oceans. The circumstances
leading to this role for the Southern Ocean are related to the existence of a deep-ocean
circumpolar belt around Antarctica that was established some 25 million years ago by the
shifting lithospheric plates which make up the Earth’s surface (see below Ocean basins). This
belt establishes the Antarctic Circumpolar Current, which isolates Antarctica from the warm
surface waters of the subtropics. The Antarctic Circumpolar Current does not completely sever
contact with the lower latitudes. The Southern Ocean does have access to the waters of the north,
but through deep- and bottom-water pathways. The basic dynamics of the Antarctic Circumpolar
Current lifts dense deep water occurring north of the current to the ocean surface south of it.
Once exposed to the cold Antarctic air masses, the upwelling deep water is converted to the cold
Antarctic Bottom Water and Antarctic Intermediate Water. The southward and upwelling deep
water, which carries heat injected into the deep ocean by processes farther north, is balanced by
the northward spread of cooler, fresher, oxygenated water masses of the Southern Ocean. It is
estimated that the overturning rate of water south of the Antarctic Circumpolar Current amounts
to 35 to 45 million cubic metres per second, most of which becomes Antarctic Bottom Water.
The primary site of Antarctic Bottom Water formation is within the continental margins of the
Weddell Sea, though some is produced in other coastal regions, such as the Ross Sea. Also, there
is evidence of deep convective overturning farther offshore. Antarctic Bottom Water, formed at a
rate of 30 million cubic metres per second, slips below the Antarctic Circumpolar Current and
spreads to regions well north of the equator. Slowly upwelling and modified by mixing with less
dense water, it returns to the Southern Ocean as deep water.
The remaining upwelling of deep water spreads near the surface to the north, where it forms
Antarctic Intermediate Water within the Antarctic Circumpolar Current zone and spreads along
the base of the thermoclines farther north. This water mass forms a sheet of low-salinity water
that demarcates the lower boundary of the subtropical thermocline. It upwells into the
thermocline, partly compensating for the sinking of North Atlantic Deep Water.
Arnold L. Gordon