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Study Finds That Plankton Blooms Do Not Send Atmospheric Carbon to the Deep Ocean; Weakens Iron Fertilization as Geo-Engineering Approach

Carbonexplorer
Bishop and Wood with a recent version of the Carbon Explorer float. Photo: Roy Kaltschmidt, Lawrence Berkeley National Laboratory. Click to enlarge.

Oceanographers Jim Bishop and Todd Wood of the US Department of Energy’s Lawrence Berkeley National Laboratory have measured the fate of carbon particles originating in plankton blooms in the Southern Ocean, using data that deep-diving Carbon Explorer floats collected around the clock for well over a year. Their study reveals that most of the carbon from lush plankton blooms never reaches the deep ocean.

The results weaken the applicability of the simplest version of the Iron Hypothesis as a geo-engineering approach to climate change. Iron Hypothesis adherents suggest global warming can be slowed or even reversed by fertilizing plankton with iron in regions that are iron-poor but rich in other nutrients like nitrogen, silicon, and phosphorus. The Southern Ocean is one of the most important such regions.

Bishop and Wood report their results in a forthcoming issue of the journal Global Biogeochemical Cycles. (Preprints are available online to subscribers at http://www.agu.org/journals/gb/papersinpress.shtml, using doi:10.1029/2008GB003206.)

Just adding iron to the ocean hasn’t been demonstrated as a good plan for storing atmospheric carbon. What counts is the carbon that reaches the deep sea, and a lot of the carbon tied up in plankton blooms appears not to sink very fast or very far.

—Jim Bishop

The reasons, while complex, are most likely due to the seasonal feeding behavior of planktonic animal life, and specifically to the effects of the dark Antarctic winter on plant and animal growth and the mixing of surface and deep waters by winter storms. Phytoplankton blooms in the spring may indicate that much of the zooplankton (animal) population essential for carbon sedimentation has starved during the winter.

The Carbon Explorers involved in the study were launched in January, 2002, as part of the Southern Ocean Iron Experiment (SOFeX), a collaboration led by scientists from Moss Landing Marine Laboratory and the Monterey Bay Aquarium Research Institute. The Carbon Explorers can descend to a kilometer beneath the surface, measure particulate carbon (and other forms of carbon), and resurface to send data by satellite.

SOFeX was meant to test the Iron Hypothesis in waters between New Zealand and Antarctica during the Antarctic summer. The Berkeley Lab Carbon Explorers were originally intended to monitor the iron-fertilization experiment for 60 days, but they continued to report by satellite throughout the Antarctic fall and winter and on into the following year.

The Iron Hypothesis. In the 1980s, oceanographer John Martin of the Moss Landing Marine Laboratories, who died in 1993, proposed that iron added to regions of the ocean that are otherwise rich in nutrients but poor in iron (so-called high-nutrient, low-chlorophyl, or HNLC, regions) can stimulate the growth of phytoplankton—a bold scientific hypothesis that has since been proven correct.

Martin went further, however, when he suggested that artificial iron fertilization of the oceans could change the climate. “Give me half a tankerful of iron and I’ll give you an Ice Age,” he said in 1988.

In testing the Iron Hypothesis, SOFeX’s investigators acknowledged that matters were not quite that simple, and that the crucial question was not whether plankton blooms could be induced but whether the carbon they captured was removed to the deep sea.

The SOFeX research vessels fertilized and measured two regions of ocean, one in an HNLC region at latitude 55 degrees south and another at 66 degrees south. Carbon Explorers were launched at both these sites; a third Carbon Explorer was launched well outside the iron-fertilized region at 55°S as a control. Berkeley Lab scientists Todd Wood, Christopher Guay, and Phoebe Lam were members of the expedition, while Bishop monitored and communicated with the Carbon Explorers from Berkeley over a computer link to communications satellites.

One question was whether the relatively silicate-poor waters of the more northerly 55° region would allow plankton known as diatoms to form silicon skeletons. If large diatoms could not grow in this HNLC region, the SOFeX researchers theorized, enhanced carbon sinking would not occur. Partly for this reason, most of the effort by the ships was at 66°S, where silicon wasn’t considered a limiting factor.

To the researchers’ surprise, the iron-augmented region at 55°N did form a vigorous plankton bloom. Dubbed the North Patch, Carbon Explorers tracked this bloom throughout the Antarctic summer, measuring carbon particles, including waste from grazing zooplankton and other aggregates, sinking beneath the bloom and carrying 10 to 20% of the fixed carbon out of the surface layer—at least to below 100 meters. The initial results of the SOFeX experiment, published in Science in April, 2004, seemed to support the Iron Hypothesis in an unexpected way.

Instead of stopping after 60 days, however, the Carbon Explorers kept operating. The two North Patch floats operated for over 14 months, diving, recording, and surfacing to report data in the world’s stormiest waters, traveling almost to South America before falling silent. The Carbon Explorer launched at 66° south lasted 18 months, spending much of its first winter recording at 800 meters depth and surfacing at weekly intervals to report, although occasionally prevented by bumping into the underside of the sea ice. The Carbon Explorer data accumulated, awaiting analysis.

In 2007 Bishop and Lam published measurements from shipboard instruments deployed during SOFeX which suggested that the picture of plankton blooms sending carbon to the deep ocean wasn’t so simple after all. Carbon reaching the deep ocean depended partly on particle size and weight; more important, there seemed to be much less particulate matter reaching depth where the biomass was highest, e.g., in plankton blooms.

This paper was criticized on the grounds that it was based on limited shipboard observations. So Todd Wood and I turned to the treasure-trove of virtually continuous observations in the records of the Carbon Explorers.

—Jim Bishop

The Carbon Explorers’ records through the Antarctic summer and fall of 2002 and the winter and spring of 2003 (and in the case of the float at 66° south, much longer) not only confirmed the limited shipboard observations in greater detail but opened up a complex picture of life in the Southern Ocean.

The Carbon Explorer at 66°S recorded data never before observed or reported. During the SOFeX experiment, the float had measured the demise of a plankton bloom rich in particulate organic carbon. Particulate carbon levels were severely reduced with the onset of perpetual darkness and sea ice formation, then modestly increased again with the return of light and the melting of the ice. Strong sedimentation—the sinking of large numbers of carbon particles to the deep ocean—was never observed.

Data from the two floats deployed farther north at 55°S produced a startling picture. As noted above, the Explorer launched inside the original SOFeX iron-amended region, dubbed 55A, had recorded a long-lasting bloom immediately following iron fertilization, with sedimentation to 100 meters. 55A found an equally strong bloom the next spring in the same region—long after the SOFeX iron was gone—with equally strong sedimentation down to 100 meters.

And while it was unsurprising that the original control float, dubbed 55C, did not see a bloom, a bigger surprise came at depth: a rain of particulate organic carbon at 800 meters down. Carbon Explorer 55C had measured sedimentation beneath a region with no plankton bloom much greater than the 55A float measured under the bloom itself.

To explain this counterintuitive “High Biomass, Low Export” result the researchers considered a number of ideas. Perhaps current shears had separated the plankton blooms from their sedimentation; or perhaps there were “large rare particles” of organic carbon that the Carbon Explorers had failed to observe; or perhaps differences in mixing of surface and deep waters during winter storms had brought sequestered iron back to the surface. The first two hypotheses were rejected, and the third, even if true, would imply that iron-stimulated blooms still lead to reduced carbon sedimentation at kilometer depths.

A fourth hypothesis, taking into account the lighting conditions that encourage or limit the growth of microscopic plants and zooplankton, emerged as the most convincing. Latitude 55°S is far enough north for light to reach into the water year round (although in winter it is much reduced). But mixing between near-surface and deeper waters can carry phytoplankton too deep to grow—out of the light, beneath the critical depth where growth is sufficient to meet the energy demands of the whole plant and animal community. The latitudes where the Explorers operated are infamously stormy; in wintertime the mixed layer can reach 400 or 500 meters deep.

To survive the winter, zooplankton have to stay deep, where it’s too dark for the phytoplankton they live on to survive. Storms and deep mixing keep the zooplankton alive. “Mixing is the dumbwaiter that brings food down,” says Bishop. “The question is whether the dumbwaiter is empty or full.”

When mixing is consistently below the critical level, phytoplankton are carried out of the light and can’t grow; the dumbwaiter stays empty and the zooplankton starve. When mixing stops in the spring, the fast growing phytoplankton rebound, but there aren’t enough surviving zooplankton population to keep up with the growth and resulting bloom, and also less production of the sinking carbon particles other zooplankton species depend on. With fewer animals to intercept the material as it falls between 100 and 800 meters, Carbon Explorer 55A observed a low carbon export to the deep ocean beneath the lush bloom.

Continual deep mixing can starve zooplankton, but if the mixing is regularly interrupted, more phytoplankton grow during the winter to supply the zooplankton lurking at depth. In the region where Carbon Explorer 55C spent the winter, storms were intermittent and mixing below 400 meters was interrupted on a daily basis. When phytoplankton growth began in the spring, the healthy zooplankton were there to “mow the lawn,” as it were—probably accounting for the modest phytoplankton growth near the surface, with increased carbon sedimentation from the zooplankton.

Bishop says these observations point to an important lesson: “Iron is not the only factor that determines phytoplankton growth in HNLC regions. Light, mixing, and hungry zooplankton are fundamentally as important as iron.

The Iron Hypothesis isn’t wrong, but it’s much more subtle than usually stated. Achieving optimum carbon sedimentation from plankton growth may require the right “recipe” of iron and other trace nutrients to grow the right kind of phytoplankton. Says Bishop, “You can grow a lot of Brussels sprouts, but kids won’t eat it. The same appears to be the case with diatom phytoplankton and zooplankton. It’s the zooplankton community that determines carbon sedimentation.”

The new study brings one other important lesson say the researchers: two Carbon Explorers deployed under similar circumstances experienced subtle differences in ocean physical conditions that resulted in very distinct biological responses. A fleet of Carbon Explorers could yield essential data on the workings of the ocean’s biological pump at far less cost than a shipborne expedition, and answer questions that cannot be answered now—such as how much man-made atmospheric carbon the ocean can absorb, and how much longer we can depend on it to soak up our excesses—and most important, how the biological carbon pump will respond to changing ocean conditions.

This research was funded by the Biological and Environmental Research Program of the US Department of Energy’s Office of Science, and by the National Oceanographic Partnership Program administered by the Office of Naval Research.

Comments

danm

If this is true it's really too bad. In a worse case scenario of global warming, i always thought we could start dumping iron and begin sucking up some carbon.
Back to the drawing board.

clett

I can't believe they assumed the sedimentation would occur in the same geographic area directly underneath the location where the bloom first started.

How far can a sediment-carrying near surface current travel in one year? Several thousand miles anyway.

Rick

On the one hand, this sounds like a promising way to scale up oceanographic research. Maybe ocean and space-faring research can learn from each other: once the mechanics of research-platform survival are worked out, a lot of productive survey work could be done with small teams of humans tending fleets or networks of survey stations (ocean buoys, etc; space satellites, rovers, static-sites, etc.) In other words, we should expect field-research in all the "fields" (ocean, space, atmospheric, geology) to go through the same sorts of production-strategies seen in more prosaic industries. Oceanography sounds as if it's ripe to enter "flexible-mass-production" of data, with the attendant budget requirements (but also knowledge-development opportunities).

On the other hand: the idea of simple carbon sequestration has always struck me as wrong-headed. Carbon seems to have some promising technological possibilities: just two possibilities are carbon fibers and algae-based chemicals production. How much carbon could be productively "sequestered" in long-term capital goods?

For comparison's sake, how much iron-based fertilizer would have to be used to tie up how many tons of carbon in molecular forms capable of sequestration -- and how would those tonnages compare with current industrial processes? How much would have to be used to have a strategic effect?

One last thought: if this proves to work, can climatologists predict where this could be most strategically deployed -- not just in terms of efficiency of the process, but where the effects on the climate would be maximized? This is a question where scale will matter: not just the global effects, but effects on specific regions. In fact, if some nations believe they can spot areas where the preponderance of good effects would be concentrated on their territories, they may find it worth doing for their own sakes, even without international agreements on global strategy. Any researchers shopping for grants to scale up research might want to consider that angle in their scale-up strategies.

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