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form of frontal instabilities ( Boccaletti et al. 2007 ; Fox-Kemper et al. 2008 ) or filaments arising from frontogenesis ( Capet et al. 2008 ; Badin et al. 2011 ; Zhong et al. 2012 ; Mensa et al. 2013 ). Dynamically, the controlling effects of geostrophy and strong stratification are no longer entirely dominant at the submesoscales and as such, these spatial and temporal scales are the resolution limit of current operational ocean models. In the Eulerian frame, active submesoscale motions
form of frontal instabilities ( Boccaletti et al. 2007 ; Fox-Kemper et al. 2008 ) or filaments arising from frontogenesis ( Capet et al. 2008 ; Badin et al. 2011 ; Zhong et al. 2012 ; Mensa et al. 2013 ). Dynamically, the controlling effects of geostrophy and strong stratification are no longer entirely dominant at the submesoscales and as such, these spatial and temporal scales are the resolution limit of current operational ocean models. In the Eulerian frame, active submesoscale motions
