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Climate of the Past An interactive open-access journal of the European Geosciences Union
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Volume 5, issue 4 | Copyright
Clim. Past, 5, 683-693, 2009
https://doi.org/10.5194/cp-5-683-2009
© Author(s) 2009. This work is distributed under
the Creative Commons Attribution 3.0 License.

  11 Nov 2009

11 Nov 2009

The importance of Northern Peatlands in global carbon systems during the Holocene

Y. Wang1,2, N. T. Roulet2, S. Frolking3, and L. A. Mysak4 Y. Wang et al.
  • 1Department of Geography, University of Sussex, Falmer, Brighton, BN1 9SJ, UK
  • 2Dept. of Geography and McGill School of Environment, McGill Univ., 3534 Univ., Montreal, Quebec H3A 2A7, Canada
  • 3Institute for the Study of Earth, Oceans, and Space, University of New Hampshire, Durham, NH 03824, USA
  • 4Dept. of Atmospheric and Oceanic Sciences, McGill University, 805 Sherbrooke Street West, Montreal, Quebec H3A 2K6, Canada

Abstract. We applied an inverse model to simulate global carbon (C) cycle dynamics during the Holocene period using atmospheric carbon dioxide (CO2) concentrations reconstructed from Antarctic ice cores and prescribed C accumulation rates of Northern Peatlands (NP) as inputs. Previous studies indicated that different sources could contribute to the 20 parts per million by volume (ppmv) atmospheric CO2 increase over the past 8000 years. These sources of C include terrestrial release of 40–200 petagram C (PgC, 1 petagram=1015 gram), deep oceanic adjustment to a 500 PgC terrestrial biomass buildup early in this interglacial period, and anthropogenic land-use and land-cover changes of unknown magnitudes. Our study shows that the prescribed peatland C accumulation significantly modifies our previous understanding of Holocene C cycle dynamics. If the buildup of the NP is considered, the terrestrial pool becomes the C sink of about 160–280 PgC over the past 8000 years, and the only C source for the terrestrial and atmospheric C increases is presumably from the deep ocean due to calcium carbonate compensation. Future studies need to be conducted to constrain the basal times and growth rates of the NP C accumulation in the Holocene. These research endeavors are challenging because they need a dynamically-coupled peatland simulator to be constrained with the initiation time and reconstructed C reservoir of the NP. Our results also suggest that the huge reservoir of deep ocean C explains the major variability of the glacial-interglacial C cycle dynamics without considering the anthropogenic C perturbation.

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