SpringerImages - Time-series of forcings prescribed in the experiment. a Insolation (W/m2) at 60°N (Berger 1978), and b smoothed atmospheric concentrations of CH4 and CO2. The latter curves are obtained by fitting a 3rd order polynomial function through the ice core data presented in Raynaud et al. (2000)

Time-series of forcings prescribed in the experiment. a Insolation (W/m2) at 60°N (Berger 1978), and bsmoothed atmospheric concentrations of CH4 and CO2. The latter curves are obtained by fitting a 3rd order polynomial function through the ice core data presented in Raynaud et al. (2000)

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Time-series of forcings prescribed in the experiment. a Insolation (W/m²) at 60°N (Berger 1978), and b smoothed atmospheric concentrations of CH₄ and CO₂. The latter curves are obtained by fitting a 3rd order polynomial function through the ice core data presented in Raynaud et al. (2000)

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2000 ) for the 9–0 kyr BP period (Fig. 2 ).

7.7%) over the last 9 kyr (Fig. 2 a).

The atmospheric CH ₄ content decreases by about 70 ppbv until 5 kyr BP, but rises again by 130 ppbv during the last 4.5 kyr (Fig. 2 b).

The simulated long-term summer cooling over the continents north of 60°N follows the prescribed orbital forcing (Fig. 2 a).

To quantify the contribution of the variations in greenhouse gas concentrations, we performed an additional sensitivity experiment with ECBilt-CLIO-VECODE in which we prescribed only the long-term changes in atmospheric CH ₄ and CO ₂ content as shown in Fig. 2 .

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