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The Southern Ocean moves carbon both into and out of the ocean interior. Surface waters can absorb atmospheric carbon dioxide, phytoplankton can turn dissolved carbon into organic matter, and circulation can carry both forms downward. But the region is a gateway, not a one-way sink: upwelling and mixing also return carbon-rich deep water toward the surface, and air–sea exchange shifts with season and location.
Why the Southern Ocean matters to the ocean carbon cycle
The Southern Ocean is a major connection between the atmosphere, the ocean surface, and the intermediate, deep, and bottom waters that circulate through the global ocean. Carbon that crosses the sea surface or is fixed by marine life can be redistributed by this circulation; carbon already in the interior can also be brought back up. The NOAA-hosted 2023 review of the Southern Ocean Carbon and Climate Observations and Modeling project (SOCCOM) calls the region “the primary gateway through which the intermediate, deep, and bottom waters of the ocean interact with the surface ocean (and thus the atmosphere).” Read the SOCCOM review.
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This two-way exchange is why the Southern Ocean cannot be described accurately as a simple drain that pulls carbon down and keeps it there. The net result is shaped by several linked processes: carbon dioxide crosses the surface in both directions; biology moves carbon into organic matter; sinking, mixing, and animal activity transport material vertically; and overturning circulation moves water masses between depths and regions. A large amount of organic matter is broken down before it reaches the deepest ocean, while some carbon remains in deeper waters for longer periods before circulation returns it toward the surface.
For climate, the distinction between a transfer and long-term storage matters. Carbon moving below the surface is no longer in immediate exchange with the atmosphere, but not every downward transfer is permanent. How long it remains isolated depends in part on where it goes, how it changes form, and how circulation reconnects that water with the surface.
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How atmospheric carbon dioxide enters surface water
Carbon dioxide (CO2) moves across the air–sea boundary in both directions. The direction at a particular place and time depends on the conditions affecting the surface and the difference in CO2 between air and water. When surface water takes up CO2, the carbon becomes part of the ocean’s dissolved inorganic carbon pool rather than remaining in the atmosphere.
Cold water can absorb CO2. In the Southern Ocean, upwelling brings deep water toward the surface; after exposure to the atmosphere, surface water can absorb CO2 and later move downward again. Winds and other conditions affect the exchange. Upwelling can also expose carbon-rich water to the atmosphere and create the possibility of outgassing. Thus, the same broad circulation system can support uptake in one circumstance and release in another. NASA’s account of aircraft observations describes these interacting processes and their seasonal variation. NASA’s 2021 explanation of the study.
What the seasonal signal does—and does not—show
NASA’s December 2, 2021 account reports that aircraft observations from field campaigns spanning 2009–2018 found a drawdown of CO2 in the lower atmosphere over the Southern Ocean surface during summer, indicating ocean uptake. The study found stronger Southern Hemisphere summer uptake and less winter outgassing than some earlier estimates based on ocean acidity had suggested. Matthew Long, the study’s lead author and a scientist at the National Center for Atmospheric Research, described the finding this way: “Airborne measurements show a drawdown of carbon dioxide in the lower atmosphere over the Southern Ocean surface in summer, indicating carbon uptake by the ocean.”
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That result is evidence about the campaigns and period studied, not a universal rate for every part of the Southern Ocean or every year. Seasonal changes in exchange do not imply that the entire region acts uniformly: different basins and conditions can have different fluxes, and a regional net balance combines areas and times with differing directions of exchange.
How phytoplankton move carbon into organic matter
Phytoplankton use photosynthesis to take dissolved inorganic carbon from surface water and make organic carbon. That carbon enters living cells and can become particulate or dissolved organic matter. It is a separate route from direct CO2 absorption: air–sea exchange transfers carbon between atmosphere and water, while biological production changes its form within the ocean. Both routes can contribute to carbon being transported below the surface.
Organic matter may sink under gravity when cells die or are packaged into particles, and it can also be transported by animal migration and mixing. The biological pump therefore is not limited to a simple rain of dead plankton. Organisms consume organic matter; microbes and animals remineralize much of it in intermediate waters, converting organic carbon back into inorganic forms. That process raises dissolved inorganic carbon and returns nutrients to the surrounding water. Some material is transported farther down before it is broken down.
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The biological pump also includes biogenic calcium carbonate particles. NOAA’s 2025–2035 Ocean Carbon Observing Science Plan describes organic matter transport and the export of these particles, which dissolve at depth. Biological export thus changes both where carbon is found and the chemical form in which it is carried. It does not mean that all carbon fixed at the surface reaches the deep sea: much is recycled at shallower depths, where its carbon and nutrients remain in the ocean interior until later physical transport may move them again.
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Overturning circulation connects surface waters with the ocean interior and redistributes carbon vertically and between regions. Surface exchange and biological activity alter the carbon content and form of upper-ocean water. Water-mass transport then carries that carbon into intermediate, deep, or bottom waters, where it can be stored away from immediate contact with the atmosphere. The same circulation system also brings dissolved inorganic carbon and regenerated nutrients back toward the surface.
When carbon-rich water rises, some of its CO2 can return to the atmosphere; some can remain dissolved, and nutrients can support new biological production. Whether carbon is absorbed, retained, or released depends on the interaction of circulation, biology, and conditions at the surface. This coupling explains why a description of sinking particles alone misses an important part of the story: physical transport moves dissolved carbon as well as organic material, and the upward limb can reconnect interior carbon with the air–sea exchange zone.
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Regional averages also hide important variation. Alison R. Gray’s 2024 review emphasizes the Southern Ocean carbon cycle’s four-dimensional character, including basin-scale differences, mixed-layer depth, eddies, and high-frequency atmospheric variability. A zonal-mean view—averaging conditions around a latitude band—can smooth over those local and short-lived effects. Read Gray’s 2024 review.
How the main storage pathways differ
The routes are distinct, but they operate together. Direct uptake first changes the exchange of carbon between the atmosphere and surface water. Biological fixation first changes the form of carbon in seawater. Circulation can transport either dissolved or biologically produced carbon, while remineralization can turn exported organic matter back into dissolved inorganic carbon at depth.
| Pathway | What moves carbon | What happens below the surface | Important qualification |
|---|---|---|---|
| Air–sea exchange and water-mass transport | CO2 crosses the ocean surface; circulation moves dissolved carbon in water. | Water transported downward can carry dissolved inorganic carbon into the interior. | Exchange can be uptake or outgassing. The direction varies with season, location, and conditions. |
| Biological fixation and export | Phytoplankton turn dissolved inorganic carbon into organic matter; sinking, animal migration, and mixing transport some of it downward. | Much organic matter is remineralized in intermediate waters, returning carbon to inorganic form and adding nutrients; some material goes deeper. Biogenic calcium carbonate particles also dissolve at depth. | Production and export are variable, and not all carbon fixed near the surface reaches deep water. |
Why scientists still have difficulty measuring the net sink
The Southern Ocean is remote and environmentally extreme, and sustained observations are sparse in places. Estimating net carbon uptake requires measurements that resolve differences by depth, region, and time. Aircraft can track atmospheric CO2 patterns over the sea; ship measurements and autonomous floats sample ocean conditions; and models help connect observations and processes. These methods do not measure the same thing in the same way, so regional estimates should be read with their method and observation period in view.
The NOAA Ocean Carbon Observing Science Plan notes that biological production and export can vary rapidly with plankton communities, mixed-layer depth, grazing, nutrients, eddies, and other conditions. It identifies sparse sustained observations of the biological pump and undersampling in the Southern Ocean as challenges for understanding carbon movement and comparing observations with models. Read NOAA’s FY25–FY35 Ocean Carbon Observing Science Plan.
These limits matter when interpreting a claim that the Southern Ocean is a major sink. That broad role is well recognized, but the estimated magnitude and variability of uptake depend on the observation method and time period. NASA’s 2021 account reports a finding from aircraft campaigns spanning 2009–2018; Gray’s 2024 review discusses persistent uncertainty tied to remote conditions and small-scale processes; NOAA’s 2025 plan says uncertainty remains about how circulation and biological changes affect the ocean sink’s magnitude and variability. None of those points supports treating one regional estimate as timeless or method-independent.
How SOCCOM improved observations of the region
SOCCOM was implemented in 2014 to help address gaps in Southern Ocean observations. Its autonomous profiling floats carry oxygen, nitrate, pH, and bio-optical sensors. They provide year-round observations from the surface to a maximum depth of 2,000 meters, making it possible to track multiple aspects of ocean conditions rather than relying only on occasional ship visits.
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How to read a claim about Southern Ocean carbon
A useful estimate or headline should make clear what kind of carbon movement it describes. A measurement of atmospheric drawdown, for example, addresses air–sea exchange during a particular period; it is not by itself a complete accounting of biological export or long-term storage at depth. Likewise, evidence that particles sink does not establish how much carbon remains isolated from the atmosphere or for how long.
- Identify the pathway: Is the claim about dissolved CO2 uptake, water-mass transport, biological fixation, or sinking and remineralization?
- Check direction and depth: Does it describe surface uptake or outgassing, export into intermediate water, or carbon carried into deeper layers?
- Look for time and place: Is the result seasonal, tied to specific field campaigns, or averaged over a basin or broader region?
- Read the evidence method: Aircraft observations, profiling floats, ship measurements, and models have different coverage and constraints. The measurement period and what it actually sampled matter.
Those distinctions prevent a seasonal uptake signal, a biological-export observation, or a broad circulation description from being mistaken for a complete, permanent carbon-storage estimate. The best-supported picture is a dynamic one: atmospheric exchange, biological transformations, and overturning continually redistribute carbon between the air, surface ocean, and deep interior.
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