| 11 | | [=#averaging_interval '''averaging_interval'''] |
| 12 | | }}} |
| 13 | | {{{#!td style="vertical-align:top; text-align:left;style="width: 50px" |
| 14 | | R |
| 15 | | }}} |
| 16 | | {{{#!td style="vertical-align:top; text-align:left;style="width: 100px" |
| 17 | | 0.0 |
| 18 | | }}} |
| 19 | | {{{#!td |
| 20 | | Averaging interval for all output of temporally averaged data (in s).\\\\ |
| 21 | | This parameter defines the time interval length for temporally averaged data (vertical profiles, spectra, 2d cross-sections, 3d volume data). By default, data are not subject to temporal averaging. The interval length is limited by the parameter |
| 22 | | [[#dt_data_output_av dt_data_output_av]]. In any case, '''averaging_interval <= dt_data_output_av''' must hold.\\\\ |
| 23 | | If an interval is defined, then by default the average is calculated from the data values of all timesteps lying within this interval. The number of time levels entering into the average can be reduced with the parameter [#dt_averaging_input dt_averaging_input].\\\\ |
| 24 | | If an averaging interval can not be completed at the end of a run, it will be finished at the beginning of the next restart run. Thus for restart runs, averaging intervals do not necessarily begin at the beginning of the run.\\\\ |
| 25 | | Parameters [#averaging_interval_pr averaging_interval_pr] and [#averaging_interval_sp averaging_interval_sp] can be used to define different averaging intervals for vertical profile data and spectra, respectively. |
| | 11 | [=#ocean '''ocean'''] |
| | 12 | }}} |
| | 13 | {{{#!td style="vertical-align:top; text-align:left;style="width: 50px" |
| | 14 | L |
| | 15 | }}} |
| | 16 | {{{#!td style="vertical-align:top; text-align:left;style="width: 100px" |
| | 17 | ''.F.'' |
| | 18 | }}} |
| | 19 | {{{#!td |
| | 20 | Parameter to switch on ocean runs.\\\\ |
| | 21 | By default PALM is configured to simulate atmospheric flows. However, starting from version 3.3, '''ocean''' = ''.T.'' allows simulation of ocean turbulent flows. Setting this switch has several effects:\\\\ |
| | 22 | * An additional prognostic equation for salinity is solved. |
| | 23 | * Potential temperature in buoyancy and stability-related terms is replaced by potential density. |
| | 24 | * Potential density is calculated from the equation of state for seawater after each timestep, using the algorithm proposed by Jackett et al. (2006, J. Atmos. Oceanic Technol., 23, 1709-1728). |
| | 25 | So far, only the initial hydrostatic pressure is entered into this equation. |
| | 26 | * z=0 (sea surface) is assumed at the model top (vertical grid index k=nzt on the w-grid), with negative values of z indicating the depth. |
| | 27 | * Initial profiles are constructed (e.g. from pt_vertical_gradient / pt_vertical_gradient_level) starting from the sea surface, using surface values given by pt_surface, sa_surface, ug_surface, and vg_surface. |
| | 28 | * Zero salinity flux is used as default boundary condition at the bottom of the sea. |
| | 29 | * If switched on, random perturbations are by default imposed to the upper model domain from zu(nzt*2/3) to zu(nzt-3). |
| | 30 | |
| | 31 | Relevant parameters to be exclusively used for steering ocean runs are [#bc_sa_t bc_sa_t], [#bottom_salinityflux bottom_salinityflux], [#sa_surface sa_surface], [#sa_vertical_gradient sa_vertical_gradient], [#sa_vertical_gradient_level sa_vertical_gradient_level], and [#top_salinityflux top_salinityflux].\\\\ |
| | 32 | |
