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Talk presented at the Symposion "Climate Impact Research: Why, How and When?"
Berlin-Brandenburg Academy of Sciences and German Academy Leopoldina, Berlin, 28 October 1997

Ocean currents have a profound influence on climate
Ocean currents were different in the past
The thermohaline circulation is a strongly non-linear system
The ocean circulation may change in the future
References
How will man-made climate change affect the ocean circulation? Is the present system of ocean currents stable, and could it be disrupted if we continue to fill the atmosphere with greenhouse gases? These are questions of great importance not only to the coastal nations of the world. While the ultimate cause of anthropogenic climate change is in the atmosphere, the oceans are nonetheless a vital factor. They do not respond passively to atmospheric changes but are a very active component of the climate system. There is an intense interaction between oceans, atmosphere and ice. Changes in ocean circulation appear to have strongly amplified past climatic swings during the ice ages, and internal oscillations of the ocean circulation may be the ultimate cause of some climate variations.

Our understanding of the stability and variability of the ocean circulation has greatly advanced during the past decade through progress in modelling and new data on past climatic changes. I will not attempt to give a comprehensive review of all the new findings here, but rather I will emphasise four key points.

Ocean currents have a profound influence on climate

Covering some 71 per cent of the Earth and absorbing about twice as much of the sun's radiation as the atmosphere or the land surface, the oceans are a major component of the climate system. With their huge heat capacity, the oceans damp temperature fluctuations, but they play a more active and dynamic role as well. Ocean currents move vast amounts of heat across the planet - roughly the same amount as the atmosphere does. But in contrast to the atmosphere, the oceans are confined by land masses, so that their heat transport is more localised and channelled into specific regions.

The present El Niño event in the Pacific Ocean is an impressive demonstration of how a change in regional ocean currents - in this case, the Humboldt current - can affect climatic conditions around the world. As I write, severe drought conditions are occurring in a number of Western Pacific countries. Catastrophic forest and bush fires have plagued several countries of South-East Asia for months, causing dangerous air pollution levels. Major floods have devastated parts of East Africa. A similar El Niño event in 1982/83 claimed nearly 2,000 lives and global losses of an estimated US$ 13 billion.

Another region that feels the influence of ocean c?????eurrents particularly strongly is the North Atlantic. It is at the receiving end of a circulation system linking the Antarctic with the Arctic, known as 'thermohaline circulation' or more picturesquely as 'Great Ocean Conveyor Belt' (Fig. 1). The Gulf Stream and its extension towards Scotland play an important part in this system. The term thermohaline circulation describes the driving forces: the temperature (thermo) and salinity (haline) of sea water, which determine the water density differences which ultimately drive the flow. The term 'conveyor belt' describes its function quite well: an upper branch loaded with heat moves north, delivers the heat to the atmosphere, and then returns south at about 2-3 km below the sea surface as North Atlantic Deep Water (NADW). The heat transported to the northern North Atlantic in this way is enormous: it measures around 1 PW, equivalent to the output of a million power stations. If we compare places in Europe with locations at similar latitudes on the North American continent, the effect becomes obvious. Bodö in Norway has average temperatures of -2°C in January and 14°C in July; Nome, on the Pacific Coast of Alaska at the same latitude, has a much colder -15°C in January and only 10°C in July. And satellite images show how the warm current keeps much of the Greenland-Norwegian Sea free of ice even in winter, despite the rest of the Arctic Ocean, even much further south, being frozen.
 

Figure 1. Europe's heating system. This highly simplified cartoon of Atlantic currents shows warmer surface currents (red) and cold north Atlantic Deep Water (NADW, blue). The thermohaline circulation heats the North Atlantic and Northern Europe. It extends right up to the Greenland and Norwegian Seas, pushing ba?????eck the winter sea ice margin. Reproduced from Rahmstorf 1997.

We now have computer models that give fairly realistic simulations of the ocean circulation, and these models can be used to examine the effects of the currents on climate. For the Atlantic 'conveyor belt' this task is made particularly straightforward by a peculiarity of the climate system: there are two stable climate states, one with the Atlantic conveyor, one without it. Just by using different initial conditions, all else remaining the same, the models can come up with either of these two different climates. This makes it easy to compare what the world would look like without the ocean circulation that warms Europe. Manabe and Stouffer 1988 were the first to analyse what happens when the familiar conveyor circulation is absent in an ocean-atmosphere circulation model. They found that the sea surface temperatures in the northern North Atlantic dropped up to 7°C in this case. Air temperatures dropped even more, up to 10°C over the Arctic seas near Scandinavia, even though the root cause for the atmospheric cooling was the lower sea surface temperatures. The reason for this amplification of the cooling was the advance of sea ice, which reflects sunlight back into space and thus led to further cooling. The air temperature changes in the model are roughly consistent with the observed difference between Bodö and Nome, confirming that this difference is indeed mainly caused by the warmth brought north by the Atlantic ocean currents in the present climate.

Ocean currents were different in the past

Painstaking detective work involving sediments of the deep sea has enabled scientists to derive a wealth of information on ocean currents of the distant ?????epast. What is just mud to a lay-person, provides a valuable archive of past climate data to the expert. Like tree rings or the annual layers of snow accumulated on glaciers, the sediments at the sea bottom preserve information on the environmental conditions from the time they were formed. It is even possible to distinguish between conditions at the sea surface and at the bottom, as the prime source of data are the shells of tiny organisms. Under the microscope, the abundance of different species can be counted and identified as surface or bottom dwellers. The chemical composition of their shells has been determined by the temperature, salinity and nutrient content of the waters the organisms lived in, which in turn reveals information on the ocean currents of the time.

Looking back over the oceanic records of the past 100,000 years or so, it is striking how variable the currents must have been. Only the last 8,000 years, i.e. most of the Holocene, were a relatively stable period. Before then, throughout the last ice age, sudden jumps and jolts occur in the record roughly every 1,000 years. These are consistent between different sediment cores, and what is more, most of the spikes in the oceanic conditions correspond to synchronous climate shifts on land as recorded in the Greenland ice cap (Bond et al. 1993). Some cold climate episodes started with a temperature drop over Greenland of 5°C happening over a few decades or even less. The most plausible explanation for these sudden climatic changes are rapid shifts or breakdowns in the ocean currents of the North Atlantic. The exact timing and sequence of events and the ultimate causes are still under investigation, but there is widespread agreement that the 'conveyor belt' circulation of the Atlantic played an active and dynamic role in the climatic roller coaster of the past.

Fairly detailed reconstructions of the Atlantic ocean circulation (Labeyrie et al. 1992; Sarnthein et al. 1994) at the height of last Ice Age, the Last Glacial Maximum (LGM) around 21,000 years before present, show that North Atlantic Deep Water (NADW) then formed south of Iceland (today much of it forms by convection to the north of Iceland). It sank to intermediate depths only, and Antarctic Bottom Water (AABW), which comes in from the south below the NADW, pushed further north than it does today, filling most of the abyssal North Atlantic. Recently the first coupled ocean-atmosphere simulation of glacial climate was performed at the Potsdam Institute (Ganopolski et al. 1998), accurately reproducing these features of the glacial ocean circulation (Fig. 2). Through a sensitivity experiment using the present-day ocean heat transports (instead of taking the glacial circulation changes into account), the authors were able to demonstrate that the change in Atlantic ocean currents played a major role in surface climate, amplifying the glacial cooling of the Northern Hemisphere by 50%. In the North Atlantic the southward shift of deep water formation sites and the corresponding advance of sea-ice led to an air temperature drop of 20°C.
 

Figure 2. Stream functions of meridional ocean transport in the Atlantic, for the present climate (left) and for the last glacial maximum (right), from the coupled ocean-atmosphere model simulation of Ganopolski et al. 1998.

Both model experiments and paleo-data thus demonstrate that the ocean circulation has undergone important change?????es in the past, and that these have led to major perturbations of the climate, at least in the North Atlantic region. It is possible that there are other regions of the globe, such as the Southern Ocean, in which the dynamic ocean caused major climate variations, but until now they have not been studied nearly as well as the North Atlantic.

The thermohaline circulation is a strongly non-linear system

Understanding the role of the ocean in climate change requires an understanding of the dynamics of ocean circulation changes. Systematic computer simulations have led to important advances in our knowledge of circulation dynamics in recent years. We have found that there are two distinct mechanisms that can cause non-linear transitions in the state of the Atlantic ocean circulation, a 'fast' and a 'slow' mechanism. The slow mechanism is quite well understood, and can be described by a simple stability diagram (discussed below).

The modelling studies have confirmed Stommel's 1961 idea that there are two states which are stable under present climatic conditions, namely with and without deep water formation in the North Atlantic (see section 1). Stommel described the positive salt advection feedback responsible for this strange behaviour: salinity in the high latitudes needs to be high enough for deep water to form, but it is only high enough because the thermohaline circulation continually brings in salty water from the south. The system is therefore self-maintaining.The flow depends on precariously balanced forces: cooling pulls in one direction, while the input of freshwater from rain, snow, melting ice and rivers pulls in the other. This freshwater threatens to reduce the salinity, and therefore the density, of the surface waters; only by a conti?????enuous flushing away of the freshwater and replenishing with salty water from the south does the conveyor survive. If the flow slows down too much, there comes a point where it can no longer keep up at all and the conveyor breaks down. This 'spin-down' takes many decades or even centuries: this is the 'slow' transition mechanism.
 

Figure 3. Stability diagram showing how the meridional transport in the Atlantic ('strength of the conveyor') depends on the amount of freshwater (precipitation and river run-off minus evaporation) entering the Atlantic. Note the bifurcation point S, beyond which no North Atlantic Deep Water formation can be maintained. For a detailed discussion, see Rahmstorf 1996.

A look at a simple stability diagram shows how it works (Fig. 3). The key feature is that there is a definite threshold for how much freshwater input the conveyor can cope with. Such thresholds are typical for complex, non-linear systems. The diagram is based on Stommel's theory, adapted for the Atlantic conveyor, but experiments with global circulation models also show the same behaviour (Rahmstorf 1996). Different models locate the present climate at different positions on the stability curve - for example, models with a rather strong conveyor are located further left in the graph, and require a larger increase in precipitation to push the conveyor 'over the edge'. The stability diagram is a unifying framework that allows us to understand and compare different computer models and experiments.

The model st?????eudies also revealed another kind of threshold where the conveyor flow can change or break down (Rahmstorf 1995). While the vulnerability in Stommel's theory arises from the large-scale transport of salt by the conveyor, this second type of threshold depends on the vertical mixing in the convection areas (e.g. the Greenland Sea and the Labrador Sea). If the mixing is interrupted, then the conveyor may break down completely in a matter of years, or the locations of the convection sites may shift. This process is known as 'convective instability', and is the 'fast' transition mechanism. We do not yet know where the critical limits of convection are, nor what it would take to set off such an event. Current climate models are not powerful enough to resolve such regional processes accurately. Convective instability could be the mechanism responsible for some of the very fast climatic changes seen in the paleo-climate records. Both mechanisms are summarised in table 1.
 

Advective Spindown Convective Instability
Time Scale gradual (~100 y) rapid (~10 y)
Mechanism large-scale salt advection local convection physics
Cause (forcing) basin-scale heat and freshwater budget/td> local forcing in convection region
Effects conveyor winds down shift of convection locations or complete breakdown of conveyor
Equilibria conveyor 'on' or 'off' several equilibria with different convection patterns
Modelling modelled quite well by climate models large uncertainty in forcing and response

Table 1: Overview over properties of the two instability mechanisms relevant to the Atlantic ocean circulation.

The ocean circulation may change in the future

Given the past instability of ocean currents and our understanding of their non-linear behaviour, the future of the Atlantic circulation in the changing climate of the next century is a natural concern. Manabe and Stouffer 1993 published scenario simulations with a coupled ocean- atmosphere model in which the carbon dioxide content of the atmosphere was gradually increased to both twice and four times the pre-industrial value and then kept constant (Fig.4). With a doubling of CO2, the Atlantic conveyor circulation declined strongly but subsequently recovered. If the CO2 content was increased fourfold, h?????eowever, the thermohaline circulation in the model was interrupted completely. Other model scenarios for a greenhouse world generally show a reduction in thermohaline circulation between 20% and 50% for a carbon dioxide doubling in the atmosphere (Rahmstorf 1997). A systematic sensitivity study with a simpler model revealed that not only the total amount of carbon dioxide, but also its rate of increase determines the effects on the ocean (Stocker and Schmittner 1997).
 
Figure 4. Time series of meridional transport in the Atlantic for two greenhouse scenarios of Manabe and Stouffer 1993. Top panel: carbon dioxide forcing of the runs. For the scenario leading to a quadrupling of carbon dioxide in the atmosphere, the thermohaline ocean circulation winds down almost completely.

The circulation changes in all these experiments happen on the slow, advective time scale over one or two centuries; rapid changes as seen during the last glacial were not triggered in these scenarios. This is the main reason why the effects on regional temperatures are only moderate in these models; the reduced ocean heat transport then falls in a time of strong greenhouse warming and is partly cancelled by this. The effects of such circulation changes on marine ecosystems are largely unexplored and will probably be serious. Furthermore, a weakened circulation reduces the ability of the ocean to absorb carbon dioxide, making the climate system even less forgiving of human emissions (Sarmiento and Le Quéré 1996).

The lack of rapid circulation changes ?????e in the model scenarios does not rule out that they could happen. Due to poor resolution, present climate models cannot capture the fast convective instability very well; this process depends on regional details. The latest report of the Intergovernmental Panel on Climate Change (Houghton et al. 1995) concluded: "Future climate changes may also involve 'surprises'. (...) Examples of such non- linear behaviour include rapid circulation changes in the North Atlantic." This is still a valid conclusion today.

References

Bond, G., W. Broecker, S. Johnsen, J. McManus, L. Labeyrie, J. Jouzel and G. Bonani, 1993: Correlations between climate records from North Atlantic sediments and Greenland ice. Nature, 365, 143-147.

Ganopolski, A., S. Rahmstorf, V. Petoukhov and M. Claussen, 1998: Simulation of modern and glacial climates with a coupled global model of intermediate complexity. Nature, 391, 350-356.

Houghton, J. T., L. G. Meira Filho, B. A. Callander, N. Harris, A. Kattenberg and K. Maskell, 1995: Climate Change 1995. Cambridge University Press, Cambridge, 572 pp.

Labeyrie, L. D., J. C. Duplessy, J. Duprat, A. Juillet-Leclerc, J. Moyes, E. Michel, N. Kallel and N. J. Shackleton, 1992: Changes in the vertical structure of the North Atlantic ocean between glacial and modern times. Quaternary Science Review, 11, 401-413.

Manabe, S. and R. J. Stouffer, 1988: Two stable equilibria of a coupled ocean-atmosphere model. J. Clim., 1, 841-866.

Manabe, S. and R. J. Stouffer, 1993: Century-scale effects of increased atmospheric CO2 on the ocean-atmosphere system. Nature, 364, 215-218.

Rahmstorf, S., 1995: Bifurcations of the Atlantic thermohaline circulation in response to changes in the hydrological cycle. Nature, 378, 145-149.

Rahmstorf, S., 1996: On the freshwater forcing and transport of the Atlantic thermohaline circulation. Clim. Dyn., 12, 799-811.

Rahmstorf, S., 1997: Risk of sea-change in the Atlantic. Nature, 388, 825- 826.

Sarmiento, J. L. and C. Le Quéré, 1996: Oceanic carbon dioxide uptake in a model of century-scale global warming. Science, 274, 1346-1350.

Sarnthein, M., K. Winn, S. J. A. Jung, J. C. Duplessy, L. Labeyrie, H. Erlenkeuser and G. Ganssen, 1994: Changes in east Atlantic deepwater circulation over the last 30,000 years: Eight time slice reconstructions. Paleoceanography, 9, 209-267.

Stocker, T. and A. Schmittner, 1997: Influence of CO2 emission rates on the stability of the thermohaline circulation. Nature, 388, 862-865.

Stommel, H., 1961: Thermohaline convection with two stable regimes of flow. Tellus, 13, 224-230.

 


   
       
 
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