|Research||Teaching||WORLD OCEAN CLIMATOLOGY
Da Costa E. D., A.Colin de Verdiere, 2002, The 7.7 year North Atlantic Oscillation.
Quaterly Journal of the Royal Meteorological Society, 128, 797-817
Colin de Verdiere A.,
fluide lent entre deux spheres en rotation rapide: les
Verdiere A and R. Tailleux, 2004, The interaction of
a baroclinic mean flow with long
Verdiere A, M. Ben Jelloul, F. Sevellec, 2006,
Bifurcation structure of thermohaline millennial
oscillations, Journal of Climate, November 15 2006,
Verdiere A., 2007, A simple model of millennial
thermohaline oscillations, Journal of Physical
Ollitrault M. A. Colin de Verdiere, 2014, The World Ocean circulation near 1000 m depth.
de Verdiere A. and M.Ollitrault, 2016, A direct
determination of the World Ocean barotropic circulation.
Verdiere A., T. Meunier and M. Ollitrault, 2019,
Meridional overturning and heat transport from Argo floats
displacements and the Planetary Geostrophic Method.
graduate level for 2 nd year of a Physical Oceanography Master
degree lecture notes
A World Ocean Climatology based on World Ocean Atlas for
temperature, salinity and ANDRO for velocity from
Argo floats with a resolution of 1 deg x 1 deg. Data is stored in
a single file which contains T, S, geopotential (absolute), u, v,
w in a .mat Matlab format. The first step of the
method is to compute a geopotential at 1000 db, the displacement
float level from the relative vorticity float fields with the
equation of balance (a Poisson equation in the horizontal domain).
Given a density climatology such as WOA, hydrostatics allows then
to obtain the geopotential at all pressures. Finally geostrophy is
used to compute the u and v velocity. The whole procedure amounts
to get rid of the divergent part of the float velocities.
The reconstruction uses a staggered A grid for different variables. Hence there is a specific grid lat_p, lon_p for T, S, geopotential (and relative vorticity if needed), one grid lat_u, lon_u for u, one grid lat_v, lon_v for v and one grid lat_w, lon_w for w (where horizontal divergence is computed). I have included the Ekman transport from Large and Yeager's wind stress. When the Ekman velocities constant in a 50 m layer are added to the geostrophic velocities, the vertical velocity is obtained from continuity with w=0 at the surface. The above papers 2014, 2016 and 2019 explain the method and outline some of the potential for applications.
The end product is the result of many, still ongoing, efforts to generate a high quality float displacements data base ANDRO by C. Cabane, N. Kolodziejczyk, M. Ollitrault, JP. Rannou and the Altran Ouest team.
Click here to access the . mat climatology: DATA