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2). Salinity reaches a maximum �C remnants of high-salinity water from the Atlantic Ocean tuclazepam �C along the ��n=28.05kg/m3 contour, this high-salinity water is also known as Lower Circumpolar Deep Water (LCDW) (Rintoul and Bullister, 1999). The bottom water ��n>28.3kg/m3 is fresh (SCabozantinib nmr for dense water masses from the ventilation sites to the hydrographic section. In order to accurately estimate the transit time, we performed a tracer release experiment with an ocean general circulation model. MRI.COM is a level model with a quasi-global domain (78��S to 90��N) and a grid size of 1/11�� in latitude, 1/10�� in longitude, and 51 vertical level. It uses biharmonic horizontal diffusion with a coefficient of 1012?m4/s. Background vertical viscosity of 10?4?m2/s and vertical diffusivity that depends on the bottom topography (Decloedt and Luther, 2010) are used. A generic length scale model (Umlauf and Burchard, 2003) is used for the mixed layer. The sea ice component is implemented with a thermodynamics model of Mellor and Kantha (1989) with thickness categorisation, ridging and rheology (Hunke and Dukowicz, 2002?and?Hunke and Lipscomb, 2010). The model was spun up from the 1970 state with CORE.v2 forcing (Large and Yeager, 2003). The 1970 state was estimated from a coarse (1�� longitude by 0.5�� latitude) model spun up from Polar Science Centre Hydrographic Climatology version 3 (Steele et al., 2001) for 922 years under repeated CORE.v2 (1948�C2008) forcing. The spatial distribution of the modelled salinity along 62��S (Fig. 3) showed a reasonable resemblance to the observed salinity Selleck Tofacitinib distribution (Fig. 2) despite a low salinity bias of about 0.02. The stronger bias around 90��E suggests that the LCDW salinity carried by the modelled ACC might be too fresh closer to Antarctica. On the other hand, the fresh near-surface water, which probably originates from sea ice melt-water, is much saltier in the model than in the observation. Possible reasons for this include errors in the model surface freshwater flux or in the melting parameterisation of the model?s sea ice component. The fact that the spatial distribution of the bias roughly follows that of the water masses implies that the model performs reasonably well in reproducing flow (i.e. advection and diffusion) but that the water mass characterisation processes (i.e.