start:hype_model_description:hype_land
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start:hype_model_description:hype_land [2020/02/07 12:52] cpers [Infiltration] |
start:hype_model_description:hype_land [2020/03/31 13:49] cpers [Soil temperature and snow depth] |
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| - | Surface runoff due to limitation in infiltration capacity and macropore flow are calculated from the sum of snow melt and rainfall; the water available for infiltration (//infilt0//). | + | Surface runoff due to excess infiltration and macropore flow are calculated from the sum of snow melt and rainfall; the water available for infiltration (//infilt0//). |
| If the current infiltration rate is greater than a threshold (//mactrinf//, mm/timestep) then macropore flow (//macroflow//) and surface runoff (//infoverflow//) may occur. In addition, the water in the upper soil layer needs to be larger than another threshold (//mactrsm//) for surface runoff and macropore flow to occur. The two flows are calculated as a percentage (//macrate// respective //srrate//) of the infiltration above the first threshold; | If the current infiltration rate is greater than a threshold (//mactrinf//, mm/timestep) then macropore flow (//macroflow//) and surface runoff (//infoverflow//) may occur. In addition, the water in the upper soil layer needs to be larger than another threshold (//mactrsm//) for surface runoff and macropore flow to occur. The two flows are calculated as a percentage (//macrate// respective //srrate//) of the infiltration above the first threshold; | ||
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| Thus water does not flow up into the layer above when macropore flow is larger than the empty space in the soil layer with the water table, as in the case of groundwater inflow. Instead the excess flow stays in the soil layer above before reaching the soil layer of the water table. This distinction is important for the substances following the macropore flow. | Thus water does not flow up into the layer above when macropore flow is larger than the empty space in the soil layer with the water table, as in the case of groundwater inflow. Instead the excess flow stays in the soil layer above before reaching the soil layer of the water table. This distinction is important for the substances following the macropore flow. | ||
| - | ==== References ==== | ||
| - | |||
| - | Zhao, L., and D.M. Gray 1999. Estimating snowmelt infiltration into frozen soils, Hydrological Processes, 13:1827-1842. | ||
| ==== Links to file reference ==== | ==== Links to file reference ==== | ||
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| ==== Soil temperature and snow depth ==== | ==== Soil temperature and snow depth ==== | ||
| - | Soil layer temperature (//soiltemp//) is calculated as a balance of three temperatures; previous time step soil layer temperature, soil temperature at deep depth (//deeptemp//) and air temperature (//T//). The weight of the deep soil is constant (0.001), while the weight of the air temperature (//weightair//) depends on snow depth (//snowdepth//) and parameters. The soil memory (//soilmem//) depends on depth and land use, with parameters //surfmem// and //depthrel//. The memory of deep soil temperature is a general parameter (//deepmem//). | + | Soil layer temperature (//soiltemp//) is calculated as a balance of three temperatures; previous time step soil layer temperature, soil temperature at deep depth (//deeptemp//) and air temperature (//T//). The model is based on the work in Lindström et al. (2002). The weight of the deep soil is constant (0.001), while the weight of the air temperature (//weightair//) depends on snow depth (//snowdepth//) and parameters. The soil memory (//soilmem//) depends on depth and land use, with parameters //surfmem// and //depthrel//. The memory of deep soil temperature is a general parameter (//deepmem//). |
| <m> soilmem = {lbrace}{ | <m> soilmem = {lbrace}{ | ||
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| ===== References ===== | ===== References ===== | ||
| + | |||
| + | Lindström, G., K. Bishop, and M. Ottosson Löfvenius, 2002. Soil frost and runoff at Svartberget, northern Sweden - measurements and model analysis, Hydrological Processes, 16:3379-3392. | ||
| Samuelsson, P., S. Gollvik, and A. Ullerstig, 2006. The land-surface scheme of the Rossby Centre regional atmospheric climate model (RCA3), SMHI Report Meteorologi Nr 122, 25 pp. | Samuelsson, P., S. Gollvik, and A. Ullerstig, 2006. The land-surface scheme of the Rossby Centre regional atmospheric climate model (RCA3), SMHI Report Meteorologi Nr 122, 25 pp. | ||
| Radic, V. and Hock, R., 2010. Regional and global volumes of glaciers derived from statisti-cal upscaling of glacier inventory data, J. Geophys. Res., 115, F01010, doi:10.1029/2009JF001373. | Radic, V. and Hock, R., 2010. Regional and global volumes of glaciers derived from statisti-cal upscaling of glacier inventory data, J. Geophys. Res., 115, F01010, doi:10.1029/2009JF001373. | ||
| + | |||
| + | Zhao, L., and D.M. Gray 1999. Estimating snowmelt infiltration into frozen soils, Hydrological Processes, 13:1827-1842. | ||
| + | |||
start/hype_model_description/hype_land.txt · Last modified: 2024/02/21 10:05 by cpers
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