Data laboriously extracted from an Antarctic ice core provide an unprecedented view of temperature, and levels of atmospheric carbon dioxide and methane, over the past 800,000 years of Earth's history.
Palaeoclimatologists are scientific detectives. Using indirect clues from concentrations of stable isotopes and trace elements, and from fossils and other components of the geological record, they infer changes in climate long before they themselves were on the scene. Direct evidence of past environmental conditions is rare, which makes it all the more valuable where it does occur. In this issue1,2, members of the EPICA (European Project for Ice Coring in Antarctica) collaboration present the latest, and longest, record from perhaps the most valuable of these archives: the atmospheric gases trapped and preserved in ice cores extracted from Earth's polar regions.
Polar ice cores provide us with the long view of the cycling of greenhouse gases such as carbon dioxide and methane. Their potential is being realized by a relatively small band of international scientists who are gradually drilling further down into the ice cap and progressively analysing older ice cores. Until recently, the Vostok ice core from eastern Antarctica set the benchmark3 — an iconic 440,000-year data set that became a central backdrop for discussions about modern climate change.
That ante was upped in 2005 by a 650,000-year record4,5 from EPICA's 'Dome C', another drilling site in eastern Antarctica where much older ice could be extracted. An 800,000-year reconstruction of temperature change from the core already existed6. Now, after years of careful work and collaboration, Dome C has yielded a complete reconstruction of the history of atmospheric carbon dioxide (Lüthi et al., page 379)1 and methane (Loulergue et al., page 383)2 over the past 800,000 years.
The fundamental conclusion that today's concentrations of these greenhouse gases have no past analogue in the ice-core record remains firm. The general long-term behaviour of methane and carbon dioxide, following patterns driven ultimately by slow changes in Earth's orbit, continues throughout the older sections of the records. The remarkably strong correlations of methane and carbon dioxide with temperature reconstructions also stand (Fig. 1, overleaf).
The data further reinforce the tight link between greenhouse gases and climate, a link maintained by as-yet only partially understood feedbacks in the Earth system. Variations in methane levels are most probably caused by variations in the influence of temperature and rainfall on wetlands in the tropics and boreal (high-northern-latitude) regions. Carbon dioxide variability is almost universally viewed as an oceanic phenomenon, a consequence of the large pools of carbon sequestered there. Changes in ocean circulation, biological productivity, carbon dioxide solubility and other aspects of ocean chemistry have been implicated, but the exact mix of mechanisms is not clear.
In considering these extended records1,2 in detail, intriguing nuances emerge. Their most prominent feature is a sawtooth-shaped variability on 100,000-year timescales. As reported last year6, the amplitude of the 100,000-year temperature cycle reconstructed at Dome C seems to have changed fundamentally about 450,000 years ago (Fig. 1). Warm phases (interglacials) in the later period have been warmer, whereas cold phases (glacials) seem similar throughout the record. The carbon dioxide record generally shares this pattern, with muted cycles in its older part. Methane also follows the trend, though not as strongly: relatively high methane maxima in the oldest interglacial cycle approach those of later warm periods.
A curious facet of the extended carbon dioxide record is unusually low levels of the gas during the two earliest glacial–interglacial cycles. Lüthi et al. speculate1 that, taken as a whole, the carbon dioxide record is hinting at a longer-term cycle in mean levels of the gas that takes 400,000–500,000 years to complete. The eccentricity of Earth's orbit — its deviation from a perfect circle — does vary with a 413,000-year period. But whether this or some other mechanism explains any variation awaits the retrieval of an even older ice core.
The extended records also provide information about shorter-term, millennial-scale climate change taking place within the longer cycles. Data from ice cores in Greenland covering the past 110,000 years show that variations in methane levels were extremely closely coupled to episodes of abrupt warming and cooling in the mid-to-high latitudes of the Northern Hemisphere7,8. No older records from Greenland exist at present; indeed, records extending back further than about 200,000 years are not expected to be found there owing to high accumulation rates and the flow of older ice towards the margins of the ice sheet. But assuming that the close coupling between Greenland's temperature and levels of atmospheric methane holds before 110,000 years ago, jumps in the Dome C methane record provide a Southern Hemisphere proxy for abrupt warming in the Northern Hemisphere. Loulergue et al.2 identify 74 such jumps in their data and, following this logic, conclude that abrupt warming and cooling in Greenland and the Northern Hemisphere has been a characteristic of the climate system over at least the past 800,000 years.
Again using methane as a proxy for Greenland's temperature patterns, it can be shown that on millennial timescales carbon dioxide concentrations rose during times when Greenland was cold. At the same time, Antarctica warmed9. This pattern has been attributed to the effect of changes in ocean circulation on the carbon cycle and climate10. Lüthi et al.1 identify examples of this kind of variability in ice as old as 750,000 to 780,000 years, another indication that these millennial patterns pervade the palaeoclimate record.
These new benchmark data1,2 for greenhouse-gas variability pose questions as to what a much longer record might show. One such question is whether the 400,000–500,000-year cycle speculated on by Lüthi et al.1 is a real effect. Another is whether the 100,000-year cycles in carbon dioxide and methane, now so clearly established, give way to 40,000-year cycles before about 900,000 years ago; such behaviour might be predicted by comparison with climate reconstructions from ocean sediments11. If that is the case, what caused the shift? Was it a reduction in mean concentrations of greenhouse gases 900,000 years ago? This commonly cited theory12 is just one of many competing hypotheses11.
The international community of ice-core scientists, under the auspices of the umbrella group IPICS (International Partners in Ice Core Sciences), has set itself the immediate target of establishing a continuous 1.5-million-year record to attempt to answer these questions. The search for the right sites is beginning, and is likely to take several years. The best places are undoubtedly in eastern Antarctica, most probably in remote, high regions where snowfall rates and temperatures are extremely low. Meeting the challenge of drilling those cores should open up a further window on goings-on in the greenhouse.
Lüthi, D. et al. Nature 453, 379–382 (2008).
Loulergue, L. et al. Nature 453, 383–386 (2008).
Petit, J. R. et al. Nature 399, 429–436 (1999).
Spahni, R. et al. Science 310, 1317–1321 (2005).
Siegenthaler, U. et al. Science 310, 1313–1317 (2005).
Jouzel, J. et al. Science 317, 793–796 (2007).
Severinghaus, J. P., Sowers, T., Brook, E. J., Alley, R. B. & Bender, M. L. Nature 391, 141–146 (1998).
Huber, C. Earth Planet. Sci. Lett. 243, 504–519 (2006).
Ahn, J. & Brook, E. J. Geophys. Res. Lett. 34, L10703 (2007).
Schmittner, A., Brook, E. J. & Ahn, J. in Ocean Circulation: Mechanisms and Impacts (eds Schmittner, A., Chiang, J. C. H. & Hemming, S.) 315–334 (AGU, Washington DC, 2007).
Clark, P. U. et al. Quat. Sci. Rev. 25, 3150–3184 (2006).
Berger, A., Li, X. S. & Loutre, M.-F. Quat. Sci. Rev. 18, 1–11 (1999).
MacFarling Meure, C. et al. Geophys. Res. Lett. 33, L14810 (2006).
About this article
Cite this article
Brook, E. Windows on the greenhouse. Nature 453, 291–292 (2008). https://doi.org/10.1038/453291a