Fig. 2: Splitting and inversion of summer low tends to occur for \({{\boldsymbol{p}}}_{{{\bf{CO}}}_{{\bf{2}}}}^{{\prime} }\) but not its drivers. | Nature

Fig. 2: Splitting and inversion of summer low tends to occur for \({{\boldsymbol{p}}}_{{{\bf{CO}}}_{{\bf{2}}}}^{{\prime} }\) but not its drivers.

From: Arctic Ocean annual high in \({{\boldsymbol{p}}}_{{{\bf{CO}}}_{{\bf{2}}}}\) could shift from winter to summer

Fig. 2

a–h, Arctic domain averages for decadal climatologies of 1996–2005 (a,c,e,g) and 2091–2100 (b,d,f,h) are shown for nine CMIP5 models (historical and RCP8.5) for surface ocean \({p}_{{{\rm{CO}}}_{2}}^{{\prime} }\) (a,b), fractional ice concentration (c,d), NPP (e,f) and surface ocean temperature (g,h). The line colours represent individual models, the black dots represent the model mean and the shaded region is the uncertainty (±1 s.d., n = 9). The red dashes are for modern observational estimates (gridded data products) for \({p}_{{{\rm{CO}}}_{2}}\), ice fraction and sea surface temperature (Methods). Extended Data Fig. 1 shows analogous results from CMIP6 (SSP5-8.5). Models fall into three groups for simulated \({p}_{{{\rm{CO}}}_{2}}^{{\prime} }\) in 2091–2100 but may share a common evolution pathway (Fig. 3).

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