Abstract
The atmospheric concentration of CO2 increased from 190 to 280 ppm between the last glacial maximum 21,000 years ago and the pre-industrial era1,2. This CO2 rise and its timing have been linked to changes in the Earth’s orbit, ice sheet configuration and volume, and ocean carbon storage2,3. The ice-core record of δ13CO2 (refs 2,4) in the atmosphere can help to constrain the source of carbon, but previous modelling studies have failed to capture the evolution of δ13CO2 over this period5. Here we show that simulations of the last deglaciation that include a permafrost carbon component can reproduce the ice core records between 21,000 and 10,000 years ago. We suggest that thawing permafrost, due to increasing summer insolation in the northern hemisphere, is the main source of CO2 rise between 17,500 and 15,000 years ago, a period sometimes referred to as the Mystery Interval6. Together with a fresh water release into the North Atlantic, much of the CO2 variability associated with the Bølling-Allerod/Younger Dryas period ∼15,000 to ∼12,000 years ago can also be explained. In simulations of future warming we find that the permafrost carbon feedback increases global mean temperature by 10–40% relative to simulations without this feedback, with the magnitude of the increase dependent on the evolution of anthropogenic carbon emissions.
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Change history
06 September 2016
The original version of this Letter contained a typographical error in the final sentence of the first paragraph in the main text. This sentence should have read 'The ratio, described by its δ13CO2 value7, is strongly affected by the exchange of carbon between the biosphere and the atmosphere because photosynthesis preferentially takes up 12C, resulting in a low δ13C in biosphere-derived carbon, at a mean value around –25‰ (ref. 8).' This has been corrected in all the online versions of this Letter.
References
Lüthi, D. et al. EPICA Dome C Ice Core 800 KYr Carbon Dioxide Data. IGBP PAGES/World Data Center for Paleoclimatology Data Contribution Series # 2008–055. NOAA/NCDC Paleoclimatology Program (2008).
Lourantou, A. et al. Constraint of the CO2 rise by new atmospheric carbon isotopic measurements during the last deglaciation. Glob. Biogeochem. Cycles 24, GB2015 (2010).
Sigman, D. M., Hain, M. & Haug, G. H. The polar ocean and glacial cycles in atmospheric CO2 concentration. Nature 446, 47–55 (2010).
Schmitt, J. et al. Carbon isotope constraints on the deglacial CO2 rise from ice cores. Science 336, 711–714 (2012).
Bouttes, N. et al. Impact of oceanic processes on the carbon cycle during the last termination. Clim. Past 8, 149–202 (2012).
Denton, G. H., Broecker, W. S. & Alley, R. B. The mystery interval 17.5 to 14.5 kyrs ago. PAGES News 14, 14–16 (2006).
Craig, H. Isotopic standards for carbon and oxygen and correction factors for mass-spectrometric analysis of carbon dioxide. Geochim. Cosmochim. Acta 12, 133–149 (1957).
Maslin, M. A. & Thomas, E. Balancing the deglacial global carbon budget: the hydrate factor. Quat. Sci. Rev. 22, 1729–1736 (2003).
Ciais, P. et al. Large inert carbon pool in the terrestrial biosphere during the Last Glacial Maximum. Nat. Geosci. 5, 74–79 (2012).
Zech, R., Huang, Y., Zech, M., Tarozo, R. & Zech, W. High carbon sequestration in Siberian permafrost loess-paleosols during glacials. Clim. Past 7, 501–509 (2011).
Zimov, N. S. et al. Carbon storage in permafrost and soils of the mammoth tundra-steppe biome: role in the global carbon budget. Geophys. Res. Lett. 36, L02502 (2009).
Hugelius, G. et al. Estimated stocks of circumpolar permafrost carbon with quantified uncertainty ranges and identified data gaps. Biogeosciences 11, 6573–6593 (2014).
Crichton, K. A., Roche, D. M., Krinner, G. & Chappellaz, J. A simplified permafrost-carbon model for long-term climate studies with the CLIMBER-2 coupled Earth system model. Geosci. Model Dev. 7, 3111–3134 (2014).
Petoukhov, V. et al. CLIMBER-2: a climate system model of intermediate complexity. Part 1: model description and performance for present climate. Clim. Dynam. 16, 1–17 (2000).
Ganopolski, A. et al. CLIMBER-2: a climate system model of intermediate complexity. Part II: model sensitivity. Clim. Dynam. 17, 735–751 (2001).
Brovkin, V., Ganopolski, A., Archer, D. & Rahmstorf, S. Lowering of glacial atmospheric CO2 in response to changes in oceanic circulation and marine biogeochemistry. Paleoceanography 22, PA4202 (2007).
Brovkin, V., Hofmann, M., Bendtsen, J. & Ganopolski, A. Ocean biology could control atmospheric δ13C during glacial-interglacial cycle. Geochem. Geophys. Geosyst. 3, 1–15 (2002).
Bouttes, N., Paillard, D., Roche, D. M., Brovkin, V. & Bopp, L. Last glacial maximum CO2 and δ13C succesfully reconciled. Geophys. Res. Lett. 38, L02705 (2011).
Oliver, K. I. C. et al. A synthesis of marine sediment core 13C data over the last 150 000 years. Clim. Past 6, 645–673 (2010).
Kageyama, M., Paul, A., Roche, D. M. & Van Meerbeeck, C. J. Modelling glacial climatic millennial-scale variability related to changes in the Atlantic Meridional Overturning Circulation: a review. Quat. Sci. Rev. 29, 2931–2956 (2010).
Tarasov, L. & Peltier, W. R. Arctic freshwater forcing of the Younger Dryas cold reversal. Nature 435, 662–665 (2005).
Lambeck, K., Rouby, H., Purcell, A., Sun, Y. & Sambridge, M. Sea level and global ice volumes from the Last Glacial Maximum to the Holocene. Proc. Natl Acad. Sci. USA 111, 15296–15303 (2014).
Yu, Z., Loisel, J., Brosseau, D. P., Beilman, D. W. & Hunt, S. J. Global peatland dynamics since the Last Glacial Maximum. Geophys. Res. Lett. 37, L12402 (2010).
Kleinen, T., Brovkin, V., von Bloh, W., Archer, D. & Munhoven, G. Holocene carbon cycle dynamics. Geophys. Res. Lett. 37, L02705 (2010).
Brovkin, V. et al. Carbon cycle, vegetation, and climate dynamics in the Holocene: experiments with the CLIMBER-2 model. Glob. Biogeochem. Cycles 16, 1139 (2002).
Ruddiman, W. F., Kutzbach, J. E. & Vavrus, S. J. Can natural or anthropogenic explanations of late-Holocene CO2 and CH4 increases be falsified? Holocene http://dx.doi.org/10.1177/0959683610387172 (2011).
Berger, A. Long-term variations of daily insolation and Quaternary climatic changes. J. Atmos. Sci. 35, 2362–2367 (1978).
Waelbroeck, C. et al. Sea-level and deep water temperature changes derived from benthic foraminifera isotopic records. Quat. Sci. Rev. 21, 295–305 (2002).
Shakun, J. D. et al. Global warming preceded by increasing carbon dioxide concentrations during the last deglaciation. Nature 484, 49–54 (2012).
Curry, W. B. & Oppo, D. W. Glacial water mass geometry and the distribution of δ13C of ΣCO2 in the western Atlantic Ocean. Paleoceanography 20, PA1017 (2005).
Acknowledgements
The research leading to these results has received funding from the European Community’s Seventh Framework Programme (FP7 2007-2013) under Grant 238366 (GREENCYCLES II) and under grant GA282700 (PAGE21, 2011-2015). D.M.R. is supported by INSU-CNRS and by NWO under project no. 864.09.013.
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K.A.C. carried out the study and interpreted data, building on work from N.B. and D.M.R. for the deglaciation period, K.A.C. designed the fresh water forcing experiments. All authors contributed to writing the paper.
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Crichton, K., Bouttes, N., Roche, D. et al. Permafrost carbon as a missing link to explain CO2 changes during the last deglaciation. Nature Geosci 9, 683–686 (2016). https://doi.org/10.1038/ngeo2793
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DOI: https://doi.org/10.1038/ngeo2793