e. the possible shifting north of the convection regions). The signal in the eastern North Atlantic is described in Swingedouw et al. (2013) where the authors show that the leakage (i.e. removal of freshwater that then does not re-circulate) relates to the meridional tilt of the separation between the sub-polar and the sub-tropical gyre. The leakage via the Canary current (the eastern branch of the pattern) diminished the amount of freshwater that is transported to the convection sites in the Labrador Sea and Nordic Seas and could then affect the intensity of deep convection if the leakage is sufficiently large. This also occurs in EC-Earth. The long-term pattern of freshwater in our forcing

field as shown in Fig. 7 resembles the observed anomaly in sea-level rise near the Antarctic ice shelves shown in Fig. 1 in Rye et al. Anti-infection Compound Library purchase (2014). The only conspicuous difference is that we have a somewhat larger melt in the northern peninsula region. The gross Antarctic sea-level rise pattern in Rye et al. (2014) is also present in our simulation. In the Southern Hemisphere, the freshwater released along the coast of Antarctica spreads northward and is thereafter taken up Selleckchem BIBW2992 by the Antarctic Circumpolar Current (ACC), spreading it in a band around Antarctica. The same pattern around Antarctica can

be seen in the simulation described in Lorbacher et al., where the fast response to Antarctic melt occurs on a timescale of mere days. This is remarkable because the fast response is due to barotropic waves and not directly related to the long-term response. In Fig. 3 in Rye et al. (2014) the sea-level rise in a model output indicates locally larger relative rise than is in our simulation. Recent experiments with high resolution, eddy-resolving, models (Weijer et al., Spence et al., 2013 and den Toom et al., 2014) indicate qualitative differences in large-scale circulation compared with coarse-resolution ones (∼1°∼1°) like EC-Earth. The circulation shows different

ventilation pathways (Spence et al., 2013) of North Atlantic Deep Water (NADW), which is not surprising given the finer topography and different diffusion value needed. Also, deep convection regions persist longer at higher resolution (Weijer et al. and Spence et al., 2013). The entrainment along the western boundary lasts longer compared to a low-resolution Leukocyte receptor tyrosine kinase model which favours a more immediate transport to the deep convection zones (Spence et al., 2013). The short-term response in a high-resolution model can be different, but this does not necessarily mean a significant difference in behaviour on decadal timescales (Weijer et al.). Caveats like these suggest that a significant improvement in realism can be expected when high-resolution models are coupled with atmospheric models (den Toom et al., 2014), which has not been feasible so far. Nevertheless, our run does show similarities with higher-resolution (den Toom et al., 2014).