Uvic ice dev #1
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Uvic ice dev #1
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Uvic ice jp
…izing in stim_variables and stim_flato, parameter to turn on and off winton in flato, functions, init_stim_winton and do_stim_winton in stim_flato
…jp' of github.com:juliaputko/stim into uvic_ice_jp
…f albedo_ice to albedo_ice_uvic
Uvic ice jp
changing vars to target for pointer
adding do_ice_uvic to stim_models
…o that vars are properly allocated
clean;removed pointers, more simple method of value passing;reorder s…
made qb public for access in register_all_variables file
…nted, bypassing error messages related to kb
removed no longer necessary var from yaml, nr_iterate no longer comme…
no longer bypassing salinity error
airseafluxes update and qe qh switch
Uvic ice jp
renamed ice_uvic_hmix to hmix
val for tmelts was off - fixed
This was referenced Aug 11, 2021
adding Qfluxes_uvic for calculation of surface fluxes
clean for compatibility with ford documentation
Uvic fabm jp
stim cleanup
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We implemented an ice model based on the 1-D thermodynamic sea ice model by Greg Flato (Flato and Brown, 1996) and modified to fit the GOTM structure, as well as containing the snow distribution and meltponds subgrid parametrization (Abraham et al. 2014). This is a transposition of the work done by Nadja Steiner for a previous version of GOTM.
It performs a surface energy budget calculation to get net flux at ice, snow or open water surface, solves the 1-D heat conduction problem using an implicit finite difference scheme with the ice/snow slab discretized into an arbitrary number of thickness layers (presently configured for only one snow layer). A Newton-Raphson iterative scheme is used to solve for the surface temperature which appears non-linearly in both surface and conductive fluxes. Surface melt is calculated to use up the net incoming energy flux at the surface with the surface temperature fixed at the melting point. Additional melt may occur to restore temperatures to the freezing point where it is exceeded. Under cooling conditions, the upper surface has a flux boundary condition with surface growth occurring only if snow load causes surface flooding. Growth at the ice underside is calculated so as to balance the flux at the bottom where the temperature remains at the freezing point of sea water. If ice melts completely, incoming heat is stored in the mixed layer which must cool to the freezing point before new ice can form. Initial growth of very thin ice is calculated assuming a linear temperature profile.