Figure 11.12: Global average sea level rise 1990 to 2100 for the SRES scenarios. Thermal expansion and land ice changes were calculated using a simple climate model calibrated separately for each of seven AOGCMs, and contributions from changes in permafrost, the effect of sediment deposition and the long-term adjustment of the ice sheets to past climate change were added. Each of the six lines appearing in the key is the average of AOGCMs for one of the six illustrative scenarios. The region in dark shading shows the range of the average of AOGCMs for all 35 SRES scenarios. The region in light shading shows the range of all AOGCMs for all 35 scenarios. The region delimited by the outermost lines shows the range of all AOGCMs and scenarios including uncertainty in land-ice changes, permafrost changes and sediment deposition. Note that this range does not allow for uncertainty relating to ice-dynamical changes in the West Antarctic ice sheet. See 220.127.116.11 for a full discussion. The bars show the range in 2100 of all AOGCMs for the six illustrative scenarios
Warrick et al. (1996) made projections of thermal expansion and of loss of mass from glaciers and ice-sheets for the 21st century for the IS92 scenarios using two alternative simple climate models. Since the SAR, time-dependent experiments have been run with several AOGCMs (Chapter 9.1.2, Table 9.1) following the IS92a scenario (Leggett et al., 1992) for future concentrations of greenhouse gases, including the direct effect of sulphate aerosols. In Section 18.104.22.168, we use the AOGCM IS92a results to derive estimates of thermal expansion and land ice melt, employing methods from the literature as described in Section 11.2, and we add contributions from thawing of permafrost, sediment deposition, and the continuing adjustment of the ice sheets to climate changes since the LGM. The choice of scenario is not the principal consideration; the main point is that the AOGCMs all follow the same scenario, so the range of results reflects the systematic uncertainty inherent in the modelling of sea level changes. The use of IS92a also facilitates comparison with the result of Warrick et al. (1996).
To quantify the uncertainty resulting from the uncertainty in future emissions, and to obtain results consistent with the global-average temperature change projections of Section 9.3.3, in Section 22.214.171.124 we derive projections for thermal expansion and land ice melt for the scenarios of the IPCC Special Report on Emissions Scenarios (SRES) (Nakic´enovic´ et al., 2000) (see also Box 9.1 in Chapter 9, Section 9.1). The results are given as sea level change relative to 1990 in order to facilitate comparison with previous IPCC reports, which used 1990 as their base date.
Over the hundred years 1990 to 2090, the AOGCM experiments for IS92a including sulphate aerosols (GS experiments – see Chapter 9, Table 9.1) show global-average sea level rise from thermal expansion in the range 0.09 to 0.37 m (Figure 11.1, Table 11.11). There is an acceleration through the 21st century; expansion for 2040 to 2090 is greater than for 1990 to 2040 by a factor of 1.4 to 2.1. Since the models experience the same forcing, the differences in the thermal expansion derive from differences in the physical behaviour of the models. Broadly speaking, the range of results reflects the systematic uncertainty of modelling in three factors: the size of the surface warming, the effectiveness of heat uptake by the ocean for a given warming (Gregory and Mitchell, 1997) and the expansion resulting from a given heat uptake (Russell et al., 2000). The separation of the first two factors parallels the distinction made in Section 126.96.36.199 between the effects of climate feedback and heat uptake on the rate of climate change. Since models differ in regard to the second and third factors, experiments with a similar temperature change do not necessarily have a similar thermal expansion, as the results demonstrate.
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