Improvement of coastal and mesoscale observation from space: Application to the northwestern Mediterranean Sea
Version of Record online: 26 MAY 2013
©2013. American Geophysical Union. All Rights Reserved.
Geophysical Research Letters
Volume 40, Issue 10, pages 2148–2153, 28 May 2013
How to Cite
2013), Improvement of coastal and mesoscale observation from space: Application to the northwestern Mediterranean Sea, Geophys. Res. Lett., 40, 2148–2153, doi:10.1002/grl.50324., , , , and (
- Issue online: 1 JUL 2013
- Version of Record online: 26 MAY 2013
- Accepted manuscript online: 8 MAR 2013 12:00AM EST
- Manuscript Revised: 5 MAR 2013
- Manuscript Accepted: 5 MAR 2013
- Manuscript Received: 22 JAN 2013
Additional supporting information may be found in the online version of this article.
|grl50324-sup-0001-2013GL055278A01.doc||Word document||25K||The Rossby radius is given by the formula: (Feliks 1985). As X0 (the boundary condition) is a constant, the three parameters that influence the Rossby radius are then the Brunt Vaisala frequency at the surface (N0), the scale height D, and f the Coriolis frequency. In the Mediterranean Sea, f is relatively high, the surface stratification (N0) is little stronger than other part in the global ocean but the depth of the thermocline is quite small and therefore D is too. Therefore the Rossby radius of deformation is small. Using the values of Pascual et al (2004), we can calculate R with the typical profile of N2. With N0=1.4e-2 s-1, D=200m, f=1e-4 s-1 and X0=2.8, we obtain R=10 km.|
|grl50324-sup-0002-2013GL055278fA02.tiff||TIFF image||126K||Histogram of the normalized absolute differences between the probability density function (pdf) of the drifters’ norm of geostrophic velocities and the different satellite products pdf. Similar results were obtained for the zonal and meridional components (not shown). The geostrophic velocities were computed without any filter because they are calculated from the maps resulting of the OI which has a spatial scale greater than the Rossby radius of deformation.|
|grl50324-sup-0003-2013GL055278pA03.tiff||TIFF image||3105K||(a) Satellite sea surface temperatures (SSTs) on 5 December 2010 for the area north of Mallorca, which were obtained through the GODAE High Resolution SST effort (GHRSST; www.ghrsst-pp.org). The ADT overlapped by the derived geostrophic currents from the (b) AVISO, (c) HR and (d) HR+bathy fields linearly interpolated on the same date.|
|grl50324-sup-0004-2013GL055278pA04.tiff||TIFF image||1831K||Maps of the error (in cm) of the second optimal interpolation at 2 different dates. (a) and (c) are taken on 14 May 2009 (SINOCOP experiment, cf Figure 3) whereas (b) and (d) are taken on 18 May 2009. Top panel is the whole area and bottom panel represent a zoom on the SINOCOP eddy region. On (c) the track 70 of Jason-1 has been indicated in red and the trajectory of a SINOCOP drifter is shown in dark blue. The error color bar is saturated at 2.5 cm because it corresponds approximately to the SSH value associated to the SINOCOP eddy signature (see to Fig 3).|
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