Carbon Dioxide in the Ocean and Atmosphere
Carbon Dioxide in the Ocean and Atmosphere
Carbon dioxide (CO2) is considered a trace gas in the atmosphere because it is much less abundant than oxygen or nitrogen. However, this trace gas plays a vital role in sustaining life on Earth and in controlling the Earth's climate by trapping heat in the atmosphere.
The oceans play an important role in regulating the amount of CO2in the atmosphere because CO2 can move quickly into and out of the oceans. Once in the oceans, the CO2 no longer traps heat. CO2 also moves quickly between the atmosphere and the land biosphere (material that is or was living on land).
Of the three places where carbon is stored—atmosphere, oceans, and land biosphere—approximately 93 percent of the CO2 is found in the oceans. The atmosphere, at about 750 petagrams of carbon (a petagram [Pg] is 1015 grams), has the smallest amount of carbon.
Balances in Carbon Dioxide Levels
Approximately 90 to 100 Pg of carbon moves back and forth between the atmosphere and the oceans, and between the atmosphere and the land biosphere. Although these exchange rates are large relative to the total amount of carbon stored in the atmosphere, the concentration of CO2 was constant at 280 parts per million (ppm) by volume for at least 1,000 years prior to the industrial era. Atmospheric concentrations of CO2 were constant because the carbon being removed from the atmosphere in some places exactly matched the CO2 being added to the atmosphere in other places.
Today, CO2 concentrations in the atmosphere are increasing as a direct result of human activities such as deforestation and the burning of fossil fuels (e.g., coal and oil). Over the past 150 years, CO2 concentrations in the atmosphere have increased by as much as 30 percent (from 280 to 370 ppm).
All trees, nearly all plants from cold climates, and most agricultural crops respond to increasing atmospheric CO2 levels by increasing the amount of CO2 they take up for photosynthesis . It is believed that the increased uptake in land plants from rising atmospheric CO2 levels roughly counterbalanced the CO2 released from cutting down tropical rain forests and other agricultural practices in the decade of the 1980s. In the 1990s, the land biosphere was estimated to take up approximately 1 Pg more CO2 than it released each year.
Most of the CO2 released from the burning of fossil fuels and other human activities (e.g., cement manufacturing) is stored either in the atmosphere or in the oceans. The CO2 that remains in the atmosphere acts as a greenhouse gas, absorbing long-wavelength radiation (heat) in the atmosphere. CO2 taken up by the oceans does not affect the Earth's heat balance, so an understanding of the air-sea exchange of CO2 is an essential part of understanding the Earth's climate system and the potential impact of future CO2 emissions.
Regulating Carbon Dioxide Emissions.
The potential for anthropogenic (human-derived) CO2 to adversely affect the Earth's climate has resulted in attempts on the international level to regulate global CO2 emissions. The Kyoto Protocol, for example, was designed to reduce global CO2 emissions to 5 percent below 1990 levels. As of late 2002, the Protocol had not been ratified and global emissions have continued to rise. Global emissions in 2001 were roughly 11 percent higher than 1990 levels.
Natural Ocean Carbon Cycle
The oceans contain about 50 times more CO2 than the atmosphere and 19 times more than the land biosphere. CO2 moves between the atmosphere and the ocean by molecular diffusion when there is a difference between CO2 gas pressure (pCO2) between the atmosphere and oceans. For example, when the atmospheric pCO2 is higher than the surface ocean, CO2 diffuses across the air-sea boundary into the sea water.
The oceans are able to hold much more carbon than the atmosphere because most of the CO2 that diffuses into the oceans reacts with the water to form carbonic acid and its dissociation products, bicarbonate and carbonate ions . The conversion of CO2 gas into nongaseous forms such as carbonic acid and bicarbonate and carbonate ions effectively reduces the CO2 gas pressure in the water, thereby allowing more diffusion from the atmosphere.
The oceans are mixed much more slowly than the atmosphere, so there are large horizontal and vertical changes in CO2 concentration. In general, tropical waters release CO2 to the atmosphere, whereas high-latitude oceans take up CO2 from the atmosphere. CO2 is also about 10 percent higher in the deep ocean than at the surface. The two basic mechanisms that control the distribution of carbon in the oceans are referred to as the solubility pump and the biological pump.
The solubility pump is driven by two principal factors. First, more than twice as much CO2 can dissolve into cold polar waters than in the warm equatorial waters. As major ocean currents (e.g., the Gulf Stream) move waters from the tropics to the poles, they are cooled and can take up more CO2 from the atmosphere. Second, the high latitude zones are also places where deep waters are formed. As the waters are cooled, they become denser and sink into the ocean's interior, taking with them the CO2accumulated at the surface.
Another process that moves CO2 away from the surface ocean is called the biological pump. Growth of marine plants (e.g., phytoplankton) takes CO2 and other chemicals from sea water to make plant tissue. Microscopic marine animals, called zooplankton, eat the phytoplankton and provide the basis for the food web for all animal life in the sea. Because photosynthesis requires light, phytoplankton only grow in the nearsurface ocean, where sufficient light can penetrate.
Although most of the CO2 taken up by phytoplankton is recycled near the surface, a substantial fraction, perhaps 30 percent, sinks into the deeper waters before being converted back into CO2 by marine bacteria. Only about 0.1 percent reaches the seafloor to be buried in the sediments.
The CO2 that is recycled at depth is slowly carried large distances by currents to areas where the waters return to the surface (upwelling regions). When the waters regain contact with the atmosphere, the CO2 originally taken up by the phytoplankton is returned to the atmosphere. This exchange process helps to control atmospheric CO2 concentrations over decadal and longer time scales.
Anthropogenic CO2 Uptake
The constant atmospheric CO2 concentrations in the centuries prior to the Industrial Revolution suggest that the oceans released a small amount of CO2 to the atmosphere to balance the carbon input from rivers. Today, this trend is reversed and the oceans must remove CO2 added to the atmosphere from human activities, known as anthropogenic (humanderived) CO2.
In the 1980s, the oceans removed an estimated 2.0±0.6 Pg of anthropogenic CO2 each year. Because humans are producing CO2 at an everincreasing rate, the average ocean removal rate increased to 2.4±0.5 Pg of carbon each year in the 1990s.
The uptake of anthropogenic CO2 by the oceans is driven by the difference in gas pressure in the atmosphere and in the oceans and by the air–sea transfer velocity. Because the pCO2 is increasing in the atmosphere, CO2 moves into the ocean in an attempt to balance the oceanic and atmospheric gas pressures.
The mechanisms that control the speed with which the CO2 gas can move from the atmosphere to the oceans (air–sea transfer velocity) are not well understood today. Recent technological advances are helping scientists to better understand these mechanisms.
The transfer velocity is related to the surface roughness of the ocean and the wind speed. The difference in pCO2 is related to the amount of carbon that is converted from CO2 gas to other nongaseous carbon species in the sea water, like bicarbonate and carbonate ions. This so-called "buffer capacity" is what allows the oceans to hold so much carbon.
The relative concentrations of CO2 (1%), bicarbonate ion (91%) and carbonate ion (8%) control the acidity (pH) of the oceans. Since CO2 is an acid gas, the uptake of anthropogenic CO2 uses up carbonate ions and lowers the oceanic pH. The carbonate ion concentration of surface sea water will decrease by an estimated 30 percent with a doubling of atmospheric CO2 from preindustrial levels (280 to 560 ppm). As the carbonate ion concentration decreases, the buffer capacity of the ocean and its ability to take up CO2 from the atmosphere is reduced.
Over the long term (millennial timescales), the ocean has the potential to take up approximately 85 percent of the anthropogenic CO2 that is released to the atmosphere. As long as atmospheric CO2 concentrations continue to rise, the oceans will continue to take up CO2. However, this reaction is reversible. If atmospheric CO2 were to decrease in the future, the oceans will start releasing the accumulated anthropogenic CO2 back out into the atmosphere.
The ultimate storage place for anthropogenic CO2 must be reactions that bind the CO2 in a manner that is not easily reversed. Dissolution of calcium carbonate in the oceans, for example, is a long-term storage place for CO2. As the oceans continue to take up anthropogenic CO2, it will penetrate deeper into the water column, lowering the pH and making the waters more corrosive to calcium carbonate. The problem is that carbonate dissolution typically occurs in the deep ocean, well removed from the anthropogenic CO2 taken up in the surface waters. In portions of the North Atlantic and North Pacific Oceans, however, anthropogenic CO2 may have already penetrated deep enough to influence the dissolution of calcium carbonate in the water column.
Burial of plant and animal material into the sediments can also provide long-term storage of anthropogenic CO2. Interestingly, almost no phytoplankton seem to grow faster in higher CO2 environments, unlike many land plants. This is because phytoplankton growth in the oceans is generally limited by the availability of light and chemicals other than CO2, principally nitrogen and phosphorus but also smaller amounts of iron, zinc, and other micronutrients.
One proposed approach for enhancing carbon removal from the atmosphere is to enhance phytoplankton growth by fertilizing specific regions of the ocean with a relatively inexpensive biologically limiting chemical like iron. The hypothesis is that the resulting bloom of oceanic plants would remove CO2 from the atmosphere then transport that carbon into the deep ocean or sediments, effectively removing it from the short-term budget. The effectiveness of the "iron hypothesis" is being tested with several research efforts attempting to scale up iron fertilization experiments.
Other carbon sequestration approaches, including direct injection of liquefied CO2 into the deep ocean, are also being examined. Further research is necessary to determine whether any of these techniques will be effective or economically feasible. Implementation of these approaches may depend, in large part, on policy decisions made at national and international levels.
see also Algal Blooms in the Ocean; Ecology, Marine; Global Warm in and the Ocean; Global Warming: Policy-Making; Microbes in the Ocean; Ocean Biogeochemistry; Ocean Chemical Processes; Ocean Currents; Ocean-Floor Sediments; Plankton; Sea Water, Gases in.
Christopher L. Sabine
Broecker, Wallace S., and Tsung-Hung Peng. Tracers in the Sea. Palisades, NY: Eldigio Press, 1982.
Falkowski, Paul G., Richard T. Barber, and Victor Smetacek. "Biogeochemical Controls and Feedbacks on Ocean Primary Production." Science 281 (1998): 200–206.
Prentice, I. Colin et al. "The Carbon Cycle and Atmospheric Carbon Dioxide." In Climate Change: The Scientific Basis—Contribution of Working Group I to the Third Assessment Report of the Intergovernmental Panel on Climate Change, eds. John T. Houghton et. al., Cambridge, U.K.: Cambridge University Press, (2001):183–237.
Trends Online: A Compendium of Data on Global Change Carbon Dioxide Information Analysis Center. Oak Ridge National Laboratory, U.S. Department of Energy. <http://cdiac.esd.ornl.gov/trends/trends.htm>.
In 1997, a United Nations meeting was held in Kyoto, Japan to establish legally binding commitments for reducing future emissions of CO2 and other greenhouse gases. The goal was for each member country to commit to reducing emissions to 5 percent below 1990 levels by the period 2008–2012. The timeframe 2008–2012 was set for compliance so that member nations could transition to efficient loweremitting carbon technologies. The Kyoto Protocols will not be binding until 3 months after they have been ratified by at least 55 member nations, including a sufficient number of the developed countries so as to account for 55 percent of the 1990 global emissions.