Project Team Moise

Overall Objectives
Scientific Foundations
Application Domains
New Results
Contracts and Grants with Industry
Partnerships and Cooperations
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Section: New Results

Mathematical Modelling of the Ocean Dynamics

Beyond the traditional approximation on the Coriolis force

Participant : Antoine Rousseau.

Formerly, A. Rousseau has performed some theoretical and numerical studies around the derivation of quasi-hydrostatic models. With C. Lucas, he proved that it is sometimes necessary to take into account the cosine part of the Coriolis force (which is usually neglected, leading to the so-called Traditional Approximation).

They have also shown that the non-traditional terms do not raise any additional mathematical difficulty in the primitive equations: well-posedness for both weak and strong solutions.

In 2011, A. Rousseau and J. McWilliams (UCLA) proposed in [62] a mathematical justification of the tilt of convective plumes in the quasi-geostrophic regime, thanks to the account of the complete Coriolis force in the so-called quasi-hydrostatic quasi-geostrophic (QHQG) model. The new model has been presented in several international conferences [26] , [49] .

Coupling Methods for Oceanic and Atmospheric Models

Participants : Eric Blayo, David Cherel, Laurent Debreu, Antoine Rousseau, Manel Tayachi.

Interface conditions for coupling ocean models

Many physical situations require coupling two models with not only different resolutions, but also different physics. Such a coupling can be studied within the framework of global-in-time Schwarz methods. However, the efficiency of these iterative algorithms is strongly dependent on interface conditions. As a first step towards coupling a regional scale primitive equations ocean model with a local Navier-Stokes model, a study on the derivation of interface conditions for 2-D x-z Navier-Stokes equations is currently underway (D. Cherel's PhD thesis). It has been shown theoretically that several usual conditions lead to divergent algorithms, and that a convergent algorithm is obtained when using transmission conditions given by a variational calculation. Moreover the impact of two numerical schemes (a projection method, and a direct method [67] ) on the implementation of the domain decomposition method has been discussed.

Using the direct method in a 2D x-z Navier-Stokes model, D. Cherel has implemented a Schwarz-based domain decomposition method, for which he used the so-called transmission boundary conditions that mix the velocity and pressure variables on an Arakawa-C grid. The numerical results confirm the rate of convergence that has been obtained theoretically, thanks to a Fourier analysis of the semi-discretized problem. A paper is in preparation.

Coupling dimensionally heterogeneous models

The coupling of different types of models is gaining more and more attention recently. This is due, in particular, to the needs of more global models encompassing different disciplines (e.g. multi-physics) and different approaches (e.g. multi-scale, nesting). Also, the possibility to assemble different modeling units inside a friendly modelling software platform is an attractive solution compared to developing more and more global complex models. More specifically one may want to couple 1D to 2D or 3D models, such as Shallow Water and Navier Stokes models: this is the framework of our partnership with EDF in the project MECSICO. In her PhD, M. Tayachi is aimed to build a theoretical and numerical framework to couple 1D, 2D and 3D models for river flows.

This year, she obtained both numerical and theoretical results on a Laplace equation in a domain that suggests a domain decomposition method with two sub-domains that do not have the same space dimension (see Figure 1 ). A paper is in preparation.

Figure 1. Numerical solution of a coupled 1D-2D system in a specific domain

Numerical schemes for ocean modelling

Participants : Laurent Debreu, Jeremie Demange.

Reducing the traditional errors in terrain-following vertical coordinate ocean models (or sigma models) has been a focus of interest for the last two decades. The objective is to use this class of model in regional domains which include not only the continental shelf, but the slope and deep ocean as well. Two general types of error have been identified: 1) the pressure-gradient error and 2) spurious diapycnal diffusion associated with steepness of the vertical coordinate. In a recent paper [78] , we have studied the problem of diapycnal mixing. The solution to this problem requires a specifically designed advection scheme. We propose and validate a new scheme, where diffusion is split from advection and is represented by a rotated biharmonic diffusion scheme with flow-dependent hyperdiffusivity satisfying the Peclet constraint.

In 2011, in collaboration with F. LemariƩ at UCLA, this work has been extended in order to render the biharmonic diffusion operator scheme unconditionaly stable (paper submitted to ocean modelling). This is particularly needed when the slopes between coordinates lines and isopycnals surfaces are important so that the rotation of the biharmonic leads to strong stability condition along the vertical coordinate where the grid size is relatively small. This work also extends more classical results on the stability of laplacian diffusion with mixed derivatives.

In his Ph'D, Jeremie Demange begins a work on advection-diffusion schemes for ocean models (Supervisors : L. Debreu, P. Marchesiello (IRD)). His work will focus on the link between tracers (temperature and salinity) and momentum advection and diffusion in the non hyperbolic system of equations typically used in ocean models (the so called primitive equations with hydrostatic and Boussinesq assumptions).

Salinity at 1000 m in the Southwest Pacific ocean is shown in figure 2 . The use of traditional upwind biased schemes (middle) exhibits a strong drift in the salinity field in comparison with climatology (left). The introduction of high order diffusion rotated along geopotential surfaces prevents this drift while maintaining high resolution features (right).

Figure 2. Salinity at 1000m in the Southwest Pacific ocean.