Arctic polar regions are not included in this experiment. Meridionally
the model extends from
to
.
Vertically the model is configured with fifteen layers with the
following thicknesses
(here the numeric subscript indicates the model level index number, ; note, that the surface layer has the highest index number 15) to give a total depth, , of . In pressure, this is Pa. The implicit free surface form of the pressure equation described in Marshall et al. [39] with the nonlinear extension by Campin et al. [8] is employed. A Laplacian operator, , provides viscous dissipation. Thermal and haline diffusion is also represented by a Laplacian operator. Wind-stress forcing is added to the momentum equations in (3.56) for both the zonal flow, and the meridional flow , according to equations (3.50) and (3.51). Thermodynamic forcing inputs are added to the equations in (3.56) for potential temperature, , and salinity, , according to equations (3.52) and (3.53). This produces a set of equations solved in this configuration as follows:
where and are the zonal and meridional components of the flow vector, , on the sphere. As described in MITgcm Numerical Solution Procedure 2, the time evolution of potential temperature, , equation is solved prognostically. The full geopotential height, , is diagnosed by summing the geopotential height anomalies due to bottom pressure and density variations. The integration of the hydrostatic equation is started at the bottom of the domain. The condition of at the sea surface requires a time-independent integration constant for the height anomaly due to density variations , which is provided as an input field.
Next: 3.11.3 Experiment Configuration Up: 3.11 P coordinate Global Previous: 3.11.1 Overview Contents mitgcm-support@dev.mitgcm.org |
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