FN Archimer Export Format
PT J
TI Three-dimensional reconstruction of oceanic mesoscale currents from surface information - art. no. C09005
BT 
AF ISERN-FONTANET, Jordi
   LAPEYRE, Guillaume
   KLEIN, Patrice
   CHAPRON, Bertrand
   HECHT, M
AS 1:1;2:3;3:1;4:1;5:2;
FF 1:PDG-DOP-DCB-OPS-LOS;2:PDG-DOP-DCB-OPS-LPO;3:;4:PDG-DOP-DCB-OPS-LOS;5:;
C1 IFREMER, Dept Oceanog Phys & Spatiale, F-29280 Plouzane, France.
   Los Alamos Natl Lab, Computat Phys Grp, Comp & Computat Sci Div, Los Alamos, NM 87545 USA.
   Ecole Normale Super, Lab Meteorol Dynam, F-75005 Paris, France.
C2 IFREMER, FRANCE
   LOS ALAMOS NATL LAB, USA
   ENS, FRANCE
SI BREST
SE PDG-DOP-DCB-OPS-LOS
   PDG-DOP-DCB-OPS-LPO
IN WOS Ifremer jusqu'en 2018
   copubli-france
   copubli-int-hors-europe
IF 3.147
TC 87
UR https://archimer.ifremer.fr/doc/2008/publication-4620.pdf
LA English
DT Article
DE ;3D dynamics reconstruction;SST;Surface Quasi Geostrophy
AB The ability to reconstruct the three-dimensional (3D) dynamics of the ocean by an effective version of Surface Quasi-Geostrophy (eSQG) is examined. Using the fact that surface density plays an analogous role as interior potential vorticity (PV), the eSQG method consists in inverting the QG PV generated by sea-surface density only. We also make the extra assumption that sea-surface temperature (SST) anomalies fully represent surface density anomalies. This approach requires a single snapshot of SST and the setup of two parameters: the mean Brunt-Vaisala frequency and a parameter that determines the energy level at the ocean surface. The validity of this approach is tested using an Ocean General Circulation Model simulation representing the North Atlantic in winter. It is shown that the method is quite successful in reconstructing the velocity field at the ocean surface for mesoscales (between 30 and 300 km). The eSQG framework can also be applied to reconstruct subsurface fields using surface information. Results show that the reconstruction of velocities and vorticity from surface fields is reasonably good for the upper 500 m and that the success of the method mainly depends on the quality of the SST as a proxy of the density anomaly at the base of the mixed layer. This situation happens after a mixed-layer deepening period. Therefore the ideal situation for the application of this method would be after strong wind events.
PY 2008
PD SEP
SO Journal of Geophysical Research - Oceans
SN 0148-0227
PU American Geophysical Union
VL 113
IS C9
UT 000259001900005
DI 10.1029/2007JC004692
ID 4620
ER

EF