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start:hype_model_description:hype_land [2018/10/15 14:07]
cpers [Glaciers]
start:hype_model_description:hype_land [2024/02/21 10:05] (current)
cpers [Overview of flow paths]
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 ====== Land routines ====== ​ ====== Land routines ====== ​
  
-This section explains the computations in the land routines of HYPE. If you want an interactive overview of how the routines simulates runoff please have a look at [[http://​vattenweb.smhi.se/​hypeexplorer|the HYPE Runoff Explorer]].+This section explains the computations in the land routines of HYPE. 
  
 ===== Basic assumptions ===== ===== Basic assumptions =====
Line 31: Line 31:
 ==== Overview of flow paths ==== ==== Overview of flow paths ====
  
-|{{:​start:​hype_model_description:​overviewflowpaths.png?​600|}}|+|{{:​start:​hype_model_description:​HYPE_box_picture_v3_soilclasses.png?​600|}}|
 |Figure 5: Illustration of flowpaths in the soil in the HYPE model.| |Figure 5: Illustration of flowpaths in the soil in the HYPE model.|
 +
 +
 +==== Recharge - discharge model ====
 +
 +In the basic model of HYPE the land classes are calculated in parallell and have no interaction with each other. The recharge - discharge model is a modeloption to introduce a crude representation of flow of water between classes within a subbasin. Some classes are chosen to represent recharge area, and other classes represent discharge area within the subbasin. The glacier class and surface water classes cannot be included in the recharge-discharge model. Another limitation is that the model does not work with classes using rootzone leakage and travel-time soilmodels as recharge or discharge classes.
 +
 +In this model a part of the (originally calculated) runoff from the recharge classes are redirected to the discharge classes where it is spread equally over their area. This means that the model is sensitive to the relative fraction of area of recharge and discharge classes in the subbasin. The water is added to the bottom soillayers of the discharge classes and can there cause upwelling of water to above soil layers. The actual runoff of the recharge classes are reduced from the originally calculated value with the part going to the discharge area. The discharge classes will have a larger runoff due to the incoming water. ​
 +
 +The part of the runoff from a recharge class that will go the the discharge class(es) are determined by a fraction given per class, and a maximum catchment area of the discharge classes. The latter is determined by a factor (general parameter //​wetdisca//​) of the the area of the the discharge classes, a maximum ratio between recharge area and discharge area.
 +
  
 ==== Diagnostic variables ==== ==== Diagnostic variables ====
Line 38: Line 48:
 Some additional output variables are calculated from the soil state variables. ​ Some additional output variables are calculated from the soil state variables. ​
  
-=== Ground water level ===+=== Groundwater ​level ===
  
-A water table is calculated for each soil layer (//gwat//from the proportion ​of water-filled pores of effective porosity. If the ground water reaches above the surface, the water is calculated with 100% porosity.+The groundwater level is measured negative from surface ​(0mto bottom ​of the soil layers. A positive groundwater level means that the soil surface is below water. If the ground water table reaches above the surface, the water is calculated with 100% porosity.
  
-  IF(soil(k)-wp(k)-fc(k)>​0.0) +The water table is found in the lowest ​soil layer that is not completely filled with water. Soil layers above this layer may have water in its effective porosity, but that is not included in the groundwater level output variable.  
-    ​gwat(k) = (soil(k)-wp(k)-fc(k)-ep(k))/​ep(k) * soillayerthick(k) –  +The water table for a soil layer is calculated linearly from the proportion of water-filled pores of effective porosity part of the soil pore volume. If the soil moisture of a soil layer is at field capacity ​(or below), the groundwater level of that soil layer is at the bottom of the layer. If the pore volume is filled, the groundwater level of that soil layer is at the top of the layer
-               ​soillayerdepth(k-1) +
-  IF(gwat(1) > 0) gwat(1) = (soil(1)-wp(1)-fc(1)-ep(1))/​1000.+
  
-The water table measured as a negative from ground surface to bottom. A positive ground water table means that the land is under water. ​ 
-The lowest soil layer that is not completely filled with water is defined as the "​official"​ ground water table layer and is the one being printed. Soil layers above this may have water in its effective porosity. ​ 
  
 === Soil moisture deficit === === Soil moisture deficit ===
Line 63: Line 69:
 <m> frostdepth = frost * sfrost * soiltemp * (fc+wp) / soil </m> <m> frostdepth = frost * sfrost * soiltemp * (fc+wp) / soil </m>
  
-There are two parameters in order to be able to choose if you want the frost depth to be land use dependent or soil dependent. The not used parameter ​is set to one.+There are two parameters in order to be able to choose if you want the frost depth to be land use dependent or soil dependent. The parameter for the not used dependence ​is set to one.
  
 ==== Links to file reference ==== ==== Links to file reference ====
Line 82: Line 88:
 |::: | calculate_soil_moisture_deficit | soil moisture deficit | |::: | calculate_soil_moisture_deficit | soil moisture deficit |
 |::: | calculate_frostdepth | frost depth | |::: | calculate_frostdepth | frost depth |
 +
 +===== Snow routines =====
 +
 +The basic simulation of snow is accumulation of snowfall to a snow pack and snow melt that releases the water to infiltration. Other processes may be included dependent on model options and parameters set. These include liquid fraction of snow simulating snow water holding capacity, evaporation and sublimation,​ snow heat content, refreezing of liquid water in snow. 
 +
 +==== Snow melt ====
 +For the simplest snow model, snow melt is calculated by temperature index. Snow melting occurs proportionally to temperature,​ when the temperature is greater than a threshold temperature. Other options are to considers the effect of radiation and snow cover. ​
 +
 +
 +The alternative snowmelt models are not fully described here yet. 
 +
 +=== Model 0 (default) ===
 +The default model is a temperature index model, with or without snow cover scaling. Snow melting occurs when the temperature is greater than a threshold temperature. The potential snow that melts (//pmelt//) depends on the snowmelt parameter //cmlt//, threshold temperature parameter //ttmp// and air temperature (//temp//). Additionally snow melt may be adjusted by the snow cover (//​effcover//​). The parameter //fsceff// determine how large effect the snow cover scaling should have, between zero and one. The actual snow melt is limited by the amount of snow (//snow// in mm). 
 +
 +<m> effcover = 1-(1-fsceff)*snowcov </m>
 +
 +<m> pmelt = cm*(temp-ttmp)*effcover </m>
 +
 +<m> cm = cmlt*(1+cmltcorr) </m>
 +
 +<m> melt = MIN(pmelt,​snow) </m>
 +
 +The parameters //cmlt// and //ttmp// are related to land use and cmltcorr depend on parameter region, while //fsceff// is general.
 +
 +=== Model 2 ===
 +the second model is a temperature and radiation index model, with or without snow cover scaling. The temperature index potential snow melt is calculated the same way as the default model (//​pmelt//​). In addition potential snow melt by radiation index (//​rpmelt//​) is calculated from shortwave radiation (//swrad//) and albedo of the snow (//​albedo_snow//​). Additionally snow melt may be adjusted by the snow cover (//​effcover//​),​ see model 0. 
 +
 +<m> rpmelt = cmrad * swrad * (1.-albedo_snow) * effcover </m>
 +
 +The parameter //cmrad// is related to land use. Snow albedo is calculated as decreasing with the age of snow (//​snowage//​),​ and depend on land use specific parameters (//albmax, albmin// and //​albkexp//​).
 +
 +<m> albedo_snow = albmin+(albmax-albmin)*EXP(-albkexp*snowage) </m>
 +
 +The two potential melting parts are added for this model. Snow melt routine consider also that snow melt (and liquid content of snow) can refreeze for temperatures below the threshold (//ttmp//). The refreezing resuces the snow melt. The refreezing occur when temperature is below the threshold (//ttmp//) and is a fraction of the (negative) potential temperature index "snow melt". The fraction is given by the general model parameter //cmrefr//.
 +
 +<m> refreeze = cmrefr*cmlt*(ttmp-temp) </m>
 +
 +<m> melt = MIN(pmelt+rpmelt-refreeze,​snow) </m>
 +
 +
 +=== Snow heat ===
 +A model option for snow heat delays the snow melt until the temperature of snow is zero. Snow temperature is calculated from snow heat and snow water equivalent. Snow heat model uses general parameters //sdnsnew// and //snkika//.
 +
 +
 +
 +==== Snow cover ====
 +
 +Normally snow is assumed to cover the whole class if present.
 +Alternatively if parameters are given, snow cover fraction (//fsc//) within a class is calculated based on snow water equivalent (//snow//). The formulation is based on Samuelsson et al. (2006). During snow build up the snow cover increase as a function of snow water equivalent until a maximum value (general parameter //fscmax//) is reached.
 +
 +<m> fsc=fscmax*tanh(0.1*snow) </m>
 +
 +It is also possible to specify a minimum snow cover (general parameter //​fscmin//​). ​
 +As soon as the fractional snow cover area reaches above a certain threshold (//​fscmax-fsclim//​),​ the snow cover area is determined by another relation that represents the redistribution of snow during winter. In this case snow cover is dependent on maximum snow pack during the winter (//​snowmax//​) and a snow cover redistribution factor that is dependent on variation in elevation (//​stdelev//,​ the standard deviation of elevation within the subbasin) and land use.
 +
 +<m> fsc= snow / {snowmax*fscdist} </m>
 +
 +<m> fscdist=fscdist0+fscdist1*stdelev </m>
 +
 +The snow distribution factor (//​fscdist//​) is determined by three land use dependent parameters; //​fscdist0//​ and //​fscdist1//​ in the linear equation and a maximum value (//​fscdistmax//​). Also in this case the snowcover is limited by the maximum and minimum value parameters. When the end of the snow season approaches (defined by general parameter //fsck1//) the //snowmax// variable is gradually decreased in order to be reset before next winter season:
 +
 +<m> snowmax=snowmax-(fsck1*snowmax-snow)*{(1-e^{-fsckexp*ts})}/​{fsck1} </m>
 +
 +<m> {snow}/​{snowmax}<​fsck1 </m>
 +
 +The equation depends on two general parameters, //fsck1// and //​fsckexp//,​ where //fsckexp// depend on time (//ts// is seconds per timestep of simulation).
 +
 +For winters when the snow pack does not reach the definition of large snow pack, the first equation is used during the whole season. For winters when the snow does not melt completely, the second equation is continued to be used.
 +
 +==== Snow depth ====
 +
 +There are two alternative snow depth models implemented in HYPE. Both use the snow density of fresh snow. Snow density for fresh snow is set by a general parameter (//​sdnsnew//​ ~0.1). If there is wind and a wind scale parameter is given, then the fresh snow density (<​m>​sdnsnew_{scaled}</​m>​) is scaled with the wind factor (//​sdnswscale//​ and maximum snow density (//​sdnsmax//​). ​
 +
 +<​m> ​ sdnsnew_{scaled} = sdnsnew + (max(0.5,​sdnsmax)-sdnsnew)*(1 - exp({-wind*sdnswscale})) </m>
 +
 +In the default snow depth model, snow density (//​snowdens//​) depends on the snow's age in days (//​snowage//​). The increase of density with snow age (//​snowdensdt//​) is a general parameter (~0.002 g/cm3/d). The snow's age increases by one every time step, but are weighted with age (0) for any new snow.
 +
 +<​m> ​ snowage = (snowage + 1)*oldsnow/​(oldsnow+snowfall) </m>
 +
 +<​m> ​ snowdens = sdnsnew_{scaled} + snowdensdt * snowage/​timesteps_perday </m>
 +
 +<​m> ​ snowdepth = 0.1 * snow/​snowdens </m>
 +
 +In the alternative snow depth model, snow density is calculated by a compacting factor. Maximum snow density (//​sdnsmax//​),​ compactation rate for low temperatures (//​sdnsrate//​) and additional compactation for high temperature (//​sdnsradd//​) are all general parameters used for this model. The change in snowdensity due to snowfall is calculated from the updated snow depth (snowfall added with density <​m>​sdnsnew_{scaled}</​m>​) and snow pack. The change in snowdensity (//​densdt//​) due to compactation each time step is calculated as:
 +
 +<​m> ​ densdt = sdnsrate*(sdnsmax-snowdens) </m>
 +
 +for cold days (temperature is below threshold temperature parameter //ttmp//), and 
 +
 +<​m> ​ densdt = (sdnsrate+sdnsradd)*(sdnsmax-snowdens) </m>
 +
 +for warm days.
 +
 +==== Links to file reference ====
 +
 +^Section ^Symbol ^Parameter/​Data ^File ^
 +|Snow| |//​whcsnow//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 +|Snow melt|//​ttmp,​ fcseff//​|//​ttmp,​ fcseff//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 +|:::​|//​cm//​|//​cmlt,​ cmltcorr//​|:::​|
 +|:::​|//​albmin,​albmax,​albkexp,​cmrad//​|//​albmin,​albmax,​albkexp,​cmrad//​|:::​|
 +|:::| |//sdnsnew, snkika//​|:::​|
 +|:::​|//​T//​|calculated from|[[start:​hype_file_reference:​tobs.txt|Tobs.txt]]|
 +|Snow cover|//​stdelev//​|//​elev_std//​|[[start:​hype_file_reference:​geodata.txt|GeoData.txt]]|
 +|:::​|//​fscmax,​ fscdist0, fscdist1, fsck1, fsckexp//​|//​fscmax,​ fscdist0, fscdist1, fsck1, fsckexp//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 +|:::| |//​fscmin,​fsclim,​fscdistmax//​|:::​|
 +|Snow depth| ​ |//sdnsnew, snowdensdt, sdnsmax, sdnsrate, sdnsradd, ttmp, sdnswscale//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 +|:::​|//​wind//​|calculated from|[[start:​hype_file_reference:​uobs.txt|Uobs.txt]] or [[start:​hype_file_reference:​uwobs.txt|UWobs.txt]] and [[start:​hype_file_reference:​vwobs.txt|VWobs.txt]]|
 +
 +
 +==== Links to relevant procedures in the code ====
 +
 +^ Modules (file) ^ Procedures ^ Section ^
 +| [[http://​hype.sourceforge.net/​doxy-html/​namespacesoil__processes.html|soil_processes (soil_proc.f90)]]| calculate_snow | snow melt |
 +| ::: | calculate_snowmelt | ::: |
 +| ::: | snowalbedo_function | ::: |
 +| ::: | calculate_snowheat_processes| ::: |
 +| ::: | snow_thermal_conductivityfunction| ::: |
 +| ::: | calculate_fractional_snowcover | snow cover |
 +| ::: | calculate_snowdepth | snow depth |
 +
  
 ===== Soil water ===== ===== Soil water =====
 +
 +==== Soil temperature and frozen soil ====
 +
 +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 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}{
 + ​\matrix{2}{2}
 +    {deepmem {for\ deeptemp}
 +    surfmem*e^{-depthrel*depth(k)} {for\ soil\ layer\ k} }} </m>
 +
 +<m> weigth_{air}={1}/​{soilmem+10*snowdepth} </m>
 +
 +<m> deeptemp=weight_{air}*T+(1-weight_{air})*deeptemp </m>
 +
 +<m> soiltemp=weight_{air}*T+(1-weight_{air}-weight_{deep} )*soiltemp+weight_{deep}*deeptemp </m>
 +
 +Negative soil temperature will freeze part of the soil water and affect evaporation,​ percolation and runoff. It was used by Stadnyk et al (2020). The effect of frozen soil can be included in simulation by a model option. The model option come in two variants.
 +
 +A fraction of the soil water is assumed in liquid phase for each soil layer (//​liqfrac//​). It is assumed equal in the different “pores”,​ i.e the same fraction frozen in water below wilting point, in water in field capacity and in water available for runoff. The fraction of liquid water for a soil layer is calculated from the temperature of the soil layer (//​soiltemp//,​ degree Celsius), soil water (//​water//​),​ porosity (//pw//) and two soil type dependent parameters (//​par<​sub>​logsatm</​sub>,​ par<​sub>​bcosby</​sub>//​): ​
 +
 +<m> liqfrac=1 , soiltemp>​0 </m>
 +
 +<m> liqfrac={pw/​water}*{({-334000*soiltemp}/​{9.81*(soiltemp+273.16)*10^{par_logsatm}*{1/​100}})^{-1/​par_bcosby}} , soiltemp<​0 </m>
 +
 +An alternative model for calculation of liquid fraction is available. In the alternate model each soillayer is divided into three equal thick temporary layers and a soil temperature for each of these are determined. Then the fraction of liquid phase is calculated for the temporary layers based on their soil temperatures. The average of the liqfrac for the temporary layers is then applied to the soil layer in the following calculations.
 +
 +Frozen soil affects evapotranspiration,​ percolation,​ soil layer runoff and tile runoff. Actual evapotranspiration is decreased by the fraction of frozen water in soil. Percolation is only acting on the liquid water of the soil. For runoff the frozen soil influences in two ways; one, the water available for runoff is reduced with the frozen fraction, and two the frozen water is assumed to expand.
 +
 +The expansion of ice decreases pore volume for liquid water. In HYPE this is assumed to affect soil layer runoff by increasing the pressure level in the soil layers. Since the ice is assumed equally divided between pores, this can actually force water to fill ep-pores and have some water available for runoff even though //​water<​wp+fc//​. Expansion is set with a general parameter, //​fzsexpand//,​ and could be up to 10% (i.e. parameter value 0.1).
 +
 +==== Evapotranspiration ==
 +
 +Evaporation from soil is assumed to occur from the two upper layers. The potential evaporation is assumed to decrease exponentially with depth (depending on the parameter //​epotdist//​). The potential evaporation is divided between the two layers (//​epotfrac//​) with the distribution depending on the potential evaporation in the midpoint of each soil layer (figure 6). This is then used by approximating to a rectangle. Since soil layers differ between classes, the evaporation distribution do to.
 +
 +<m> epot1 = EXP(- epotdist*soillayerdepth(1){/​}2) </m>
 +
 +<m> epot2 = EXP(- epotdist*(soillayerdepth(1)+{soillayerdepth(2)-
 +          soillayerdepth(1)}/​2)) </m>
 +          ​
 +<​m> ​ area1 = soillayerdepth(1)*epot1 </m>
 +
 +<​m> ​ area2 = (soillayerdepth(2)-soillayerdepth(1))*epot2 </m>
 +
 +<m> epotfrac1 = area1 / {area1 + area2} </m>
 +
 +<​m> ​ epotfrac2 = area2 / {area1 + area2} </m>
 +
 +
 +
 +|{{:​start:​hype_model_description:​potentialevaporation.png?​400|}}|
 +|Figure 6 The distribution of potential evaporation between the top two soil layers.|
 +
 +
 +The actual evaporation from a soil layer (//evap//) is limited by the availability of water in the soil (//soil//) above the wilting point (//wp//, mm). Evaporation is at potential rate only if the water exceeds field capacity (//fc//, mm) or a (large) proportion (general parameter //lp//) of field capacity. In between these limits evaporation increase linearly.
 +
 +<m> evapp= {lbrace}{
 + ​\matrix{3}{2}
 +    {0 {soil-wp<​0}
 +    epot*epotfrac {soil-wp>​lp*fc}
 +    epot*epotfrac*{{soil-wp}/​{lp*fc}} {else} }} </m>
 +
 +<m> evap = MAX(evapp,​soil-wp) </m>
 +
 +
 +|{{:​start:​hype_model_description:​evap.png?​400|}}|
 +|Figure 7 Evaporation as a function of soil water.|
 +
 +The actual evaporation may also depend on soil temperature (//​soiltemp//​). It is then reduced for temperatures above land use parameter //ttrig// and depend on two other land use parameters (//tredA//, //tredB//) as well (Figure 3). 
 +
 +| {{:​start:​hype_model_description:​pet_soiltemp.png?​400}} ​                                                                                   |
 +| Figure 8 Soil temperature factor for reduction of soil evapotranspiration. \\ Parameter values: //​ttrip//​=1,​ //​tredA//​=0.5,​ //​tredB//​=1. ​ |
 +
 +The soil temperature evapotranspiration reduction is calculated as:
 +
 +<m> factor = 1-e^( - tredA*(soiltemp-ttrig)^tredB) </m>
 +
 +<m> evapp = evapp*factor </m>
 +
 +The actual soil evaporation is set to zero for temperatures below the threshold temperature and for negative potential evaporation estimates (condensation). It may also be affected by frozen soil model, which then limit evaporation to the liquid part of soil water.
 +
 +
  
 ==== Groundwater runoff ==== ==== Groundwater runoff ====
Line 108: Line 315:
            ​({soillayerdepth(k)} - streamdepth) </m>            ​({soillayerdepth(k)} - streamdepth) </m>
   ​   ​
 +If the frozen soil model is used, it influences in two ways; one, the water available for runoff is reduced to the liquid fraction, and two, the frozen water is assumed to expand possibly increasing the water level in the soil.
 +
 |{{:​start:​hype_model_description:​runofffromthird_layer.png?​400|}}| |{{:​start:​hype_model_description:​runofffromthird_layer.png?​400|}}|
-|Figure ​6: Runoff from the third soil layer with a stream.|+|Figure ​9: Runoff from the third soil layer with a stream.|
  
 Soil layers that lye entirely below the stream depth have no groundwater runoff. Soil layers that lye entirely below the stream depth have no groundwater runoff.
Line 150: Line 359:
 ==== Runoff through drainage pipes ==== ==== Runoff through drainage pipes ====
  
-Runoff in the drainage pipes occurs when the water table (the percentage of filled pores of the effective porosity) rises above the pipe's depth (figure ​7). Runoff depends on the groundwater surface elevation over the pipe (//​deltah//,​ m), and a recession coefficient //trrcs//. Recession parameter //trrcs// depends on soil type, while drainage pipe level depends on the class. The recession parameter is adjusted with the correction parameter //​rrcscorr//​ for different parameter regions (//​parreg//​). It is defined as an increase.+Runoff in the drainage pipes occurs when the water table (the percentage of filled pores of the effective porosity) rises above the pipe's depth (figure ​10). Runoff depends on the groundwater surface elevation over the pipe (//​deltah//,​ m), and a recession coefficient //trrcs//. Recession parameter //trrcs// depends on soil type, while drainage pipe level depends on the class. The recession parameter is adjusted with the correction parameter //​rrcscorr//​ for different parameter regions (//​parreg//​). It is defined as an increase.
  
 <m> trrcs = trrcs*(1+rrcscorr) </m> <m> trrcs = trrcs*(1+rrcscorr) </m>
 +
 +In addition the tile drainage can be adjusted if not the whole class is assumed to be drained by ditches. The fraction of drain area for the class is allowed to affect the recession parameter to reduce the effect of tile drainage.
 +
 +<m> trrcs=trrcs*tilefrac </m>
 +
 +where tilefrac is given per subbasin and class, or a group of classes called ''​tilegroup''​.
  
 Depending on which soil layer drainage pipe is in, the runoff will be calculated for water in that soil layer. For the soil layer //k// (//​soil(k)//​ is the water content in soil layer //k//) runoff is calculated as the parameter //trrcs// times the water found in the effective porosity of the layer and of the overlying soil layers if it is full.  Depending on which soil layer drainage pipe is in, the runoff will be calculated for water in that soil layer. For the soil layer //k// (//​soil(k)//​ is the water content in soil layer //k//) runoff is calculated as the parameter //trrcs// times the water found in the effective porosity of the layer and of the overlying soil layers if it is full. 
Line 163: Line 378:
     runoffd = trrcs * deltah / soillayerthick(k) * ep(k)     runoffd = trrcs * deltah / soillayerthick(k) * ep(k)
     ​     ​
 +If the frozen soil model is used, it influences in two ways; one, the water available for runoff is reduced to the liquid fraction, and two, the frozen water is assumed to expand possibly increasing the water level in the soil. 
  
 |{{:​start:​hype_model_description:​runoffthorughdrainagepipes.png?​400|}}| |{{:​start:​hype_model_description:​runoffthorughdrainagepipes.png?​400|}}|
-|Figure ​7: Illustration for calculation of runoff through the drainage pipes.|+|Figure ​10: Illustration for calculation of runoff through the drainage pipes.|
  
-==== Infiltration ==== +==== Infiltration ​and surface runoff ​==== 
-Infiltration is calculated from the sum of rain and snowmelt (//​infilt0//​) .+Infiltration is calculated from the sum of rain and snowmelt (//​infilt0//​, mm/time step) .
  
 <m> infilt0 = rainfall + melt </​m> ​ <m> infilt0 = rainfall + melt </​m> ​
  
-If the sum is greater than the infiltration capacity, a part of the water will not infiltrate into the soil. The calculation of actual infiltration will consider effects of surface runoff, macropore flow and frozen soil. If the calculated infiltration is greater than zero, it is added to the upper layer soil water. This is done regardless of whether there is space in the soil pores there or not. If the water exceeds the water pore volume it is assumed to lie on the ground, but it still belongs to the upper soil layer, is totally mixed and thus has the same concentrations.+Part of the available ​water for infiltration (//​infilt0//​) may not infiltrate into the soil, due to limitations by the soil's infiltration capacity and other properties of the soil. The calculation of actual infiltration will consider effects of surface runoff, macropore flow and frozen soil. If the finally ​calculated infiltration is greater than zero, it is added to the upper layer soil water. This is done regardless of whether there is space in the soil pores there or not. If the water exceeds the water pore volume it is assumed to lie on the ground, but it still belongs to the upper soil layer, is totally mixed and thus has the same concentrations.
  
 HYPE has an option for alternative calculation order of soil processes during a timestep. As default it calculates and add infiltration (and let the soil water percolate) before runoff and evaporation is calculated and removed from the soil water. Alternatively runoff and evapotranspiration is calculated before infiltration and percolation to slow the response of soil runoff. These options is tested during development of the soil routine. HYPE has an option for alternative calculation order of soil processes during a timestep. As default it calculates and add infiltration (and let the soil water percolate) before runoff and evaporation is calculated and removed from the soil water. Alternatively runoff and evapotranspiration is calculated before infiltration and percolation to slow the response of soil runoff. These options is tested during development of the soil routine.
Line 179: Line 395:
    
  
-Surface runoff due to limitation ​in infiltration ​capacity ​and macropore flow are calculated from the sum of snow melt and rainfall, and are withdrawn from actual infiltration.+There are alternative models for diversion of flow from water available for infiltration (//​infilt0//​) ​to be chosen from. All model options result ​in a division of available water into three flow paths; surface runoff to the nearest stream, ​infiltration ​to top soil layer, ​and macropore flow to the soil layer where the groundwater table is currently located.
  
-If the sum is greater than the infiltration ​capacity ​(a threshold parameter, ​//mactrinf//), and the water in the upper soil layer is larger ​than another ​threshold (//mactrsm//) then macropore flow (//​macroflow//​) and surface runoff (//​infoverflow//​) may occur. ​These runoffs are caused by an inadequate infiltration capacity of the soil. Both these two flows are calculated as a percentage (//​macrate//​ respective //srrate//) of the infiltration above the infiltration capacity ​threshold;+The original and default model is based on runoff coefficients and thresholds for infiltration and soil moisture. 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 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. This threshold is determined by a soil type dependent parameter (//​mactrsm//​) multiplied by the water not available for runoff (i.e. //​fc//​+//​wp//​)The two flows are calculated as a percentage (//​macrate//​ respective //srrate//) of the infiltration above the first threshold;
  
 <m> macroflow = macrate * (infilt0 - mactrinf) </m> <m> macroflow = macrate * (infilt0 - mactrinf) </m>
Line 195: Line 413:
 The actual infiltration is calculated by subtracting the macropore flow and surface runoff from the sum of snow melt and rain. The actual infiltration is calculated by subtracting the macropore flow and surface runoff from the sum of snow melt and rain.
  
-<m> infilt = infilt0 - macroflow ​– infoverflow </m>+<m> infilt = infilt0 - macroflow ​infoverflow </m> 
 + 
 +An alternative flow diversion model calculates surface runoff and macroporeflow from a surface runoff coefficient based on current (//S//) and maximum soil moisture (//Smax//). The soil moisture can be based on one, two or all three soil layers. 
 +<m> S=SUM(soil(j)) j=1,nlayer </​m>​ 
 +<m> Smax=SUM(pw(j) J=1,nlayer </​m>​ 
 +where  //soil(j)// is soil water of soil layer //j// (mm), //pw(j)// is pore volume of soil layer //j// (mm) and calculated from the model parameters for water holding capacity (//wcwp//, //wcfc// and //wcep//), //nlayer// is set by a general model parameter (//​srnlayer//​). 
 +The surface runoff coefficient (//​srratio//​) is a "​beta-function",​ with the general parameter //srbeta// as exponent //beta// 
 +<m> srratio = (S/​Smax)^beta </​m>,​ 
 +but limited to one. A fraction of the diverted flow goes to macropore flow (//​macroflow//​),​ while the rest become surface runoff (//​infoverflow//​). The infiltration (//​infilt//​) is the rest of the available water. 
 +<m> macroflow = macfrac*srratio*infilt0 </​m>​ 
 +<m> infoverflow = (1-macfrac)*srratio*infilt0 </​m>​ 
 +<m> infilt = (1. - srratio)*infilt0 </​m>​ 
 + 
 +Another alternative flow diversion model calculates surface runoff and macroporeflow from a surface runoff coefficient based on current (//S//) and maximum soil moisture (//Smax//) and from current available water for infiltration. This model is similar to the one above but the exponent of the surface runoff coefficient (//beta//) is calculated from two general parameters and //​infilt0//​. 
 +<m> beta = sralpha / infilt0^srgamma </​m>​ 
  
 === Additional infiltration limitation by frozen soil === === Additional infiltration limitation by frozen soil ===
  
-An optional model for infiltration limitation and diversion of flow considers the effect of frozen soil. It is developed based on Zhao and Gray (1999). This model redirects all or part of the remaining infiltration,​ after calculating the diversion of surface runoff and macropore flow as described above. ​+An optional model for infiltration limitation and diversion of flow considers the effect of frozen soil. It is developed based on Zhao and Gray (1999) and tried by Stadnyk et al (2020). This model redirects all or part of the remaining infiltration,​ after calculating the diversion of surface runoff and macropore flow as described above. Note that this is not part of the frozen soil model option described above ([[:​start:​hype_model_description:​hype_land#​soil_temperature_and_frozen_soil|Soil temperature and frozen soil]]).
  
-If the minimum daily temperature is less than 10 degrees and the infiltration is larger than 5mm/d an icelens ​is created in the soil. In this case, and as long as the maximum daily temperature is below zero, the icelens ​redirect all infiltration to surface runoff and macropore flow.+If the minimum daily temperature is less than 10 degrees and the infiltration is larger than 5mm/d an ice lens is created in the soil. In this case, and as long as the maximum daily temperature is below zero, the ice lens redirect all infiltration to surface runoff and macropore flow.
  
 <m> redirect = infilt </m> <m> redirect = infilt </m>
  
-If there is no icelens, but the soil temperature of the upper soil layer (//​soiltemp//​) is below zero the infiltration is restricted but not blocked. The infiltration is restriced by a potential infiltration adapted from Zhao and Gray (1999). The potential infiltration (//​potinfilt//​) depends on a model parameter (//​bfroznsoil//​) that is soil type dependent. It also depend on the "​opportunity time" (//t0//), which is an estimate of the time with possible infiltration in hours;+If there is no ice lens, but the soil temperature of the upper soil layer (//​soiltemp//​) is below zero the infiltration is restricted but not blocked. The infiltration is restriced by a potential infiltration adapted from Zhao and Gray (1999). The potential infiltration (//​potinfilt//​) depends on a model parameter (//​bfroznsoil//​) that is soil type dependent. It also depend on the "​opportunity time" (//t0//), which is an estimate of the time with possible infiltration in hours;
  
  
Line 234: Line 467:
 ==== Percolation ==== ==== Percolation ====
  
-The flow of water downward through the soil layers is only done by water over field capacity (water in the effective porosity). A maximum percolation (mm/d) limits the flow between soil layers. For the upper soil layer it is //mperc1//, and for the second soil layer it is //mperc2//. These parameters are soil type dependent. Flow is also limited by how much water the lower layer can receive.+The flow of water downward through the soil layers is only possible for water over field capacity (water in the effective porosity ​part of the pore volume). For a frozen soil, percolation is only acting on the liquid water of the soil. A maximum percolation (mm/d) limits the flow between soil layers. For the upper soil layer it is //mperc1//, and for the second soil layer it is //mperc2//. These parameters are soil type dependent. Flow is also limited by how much water the lower layer can receive.
  
 Drainage from soil layer 1 to soil layer 2 is Drainage from soil layer 1 to soil layer 2 is
Line 268: Line 501:
 ==== Saturated surface runoff ==== ==== Saturated surface runoff ====
    
-Surface runoff due to a high ground water table (//satoverflow//) occurs when the water table in the upper soil layer reaches above the surface. It depends on a parameter //srrcs// which is dependent on land use. The recession parameter is corrected with the correction factor //​rrcscorr//​ for different parameter regions (parreg). It is defined as an increase.+Surface runoff due to a high ground water table (//q//, mm/time step) occurs when the water table in the upper soil layer reaches above the surface. It depends on a parameter //srrcs// which is dependent on land use. The recession parameter is corrected with the correction factor //​rrcscorr//​ for different parameter regions (parreg). It is defined as an increase.
  
 <m> srrcs = srrcs*(1+rrcscorr) </m> <m> srrcs = srrcs*(1+rrcscorr) </m>
  
-<​m> ​satoverflow ​= MAX(srrcs * (soil(1)-wp(1)-fc(1)-ep(1)),​0.) </m>+<​m> ​= MAX(srrcs * (soil(1)-wp(1)-fc(1)-ep(1)),​0.) </m>
  
 Runoff is removed from the uppermost soil layer. The total surface runoff (due to high ground water table and low infiltration capacity) is calculated and printed. Runoff is removed from the uppermost soil layer. The total surface runoff (due to high ground water table and low infiltration capacity) is calculated and printed.
Line 283: Line 516:
 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 ====
  
 ^Section ^Symbol ^Parameter/​Data ^File ^ ^Section ^Symbol ^Parameter/​Data ^File ^
-|Groundwater runoff|//​wp,​ fc, ep//​|calculated from //​wcwp,​wcfc,​wcep,​wcwp1-3,​wcfc1-3,​wcep1-3//​|[[start:​hype_file_reference:​par.txt|par.txt]]|+|Soil temperature and frozen soil|//T//| |[[start:​hype_file_reference:​tobs.txt|Tobs.txt]]| 
 +|:::​|//​deeptemp//​|//​init2//​|[[start:​hype_file_reference:​par.txt|par.txt]]| 
 +|:::​|//​par<​sub>​logsatmp</​sub>,​ par<​sub>​bcosby</​sub>//​ |//​logsatmp,​ bcosby//​|:::​| 
 +|:::| |//deepmem, surfmem, depthrel, fzsexpand//​|:::​| 
 +|:::|//pw// | //​pw=wp+fc+ep//​ and calculated from //wcwp, wcfc, wcep, wcwp1-3, wcfc1-3, wcep1-3//​|:::​| 
 +|Groundwater runoff|//​wp,​ fc, ep//​|calculated from //wcwp, wcfc, wcep, wcwp1-3, wcfc1-3, wcep1-3//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |:::| |//rrcs1, rrcs2, rrcs3, rrcscorr//​|:::​| |:::| |//rrcs1, rrcs2, rrcs3, rrcscorr//​|:::​|
 |:::| |//​soillayerdepth,​ streamdepth,​ tiledepth//​|[[start:​hype_file_reference:​geoclass.txt|GeoClass.txt]]| |:::| |//​soillayerdepth,​ streamdepth,​ tiledepth//​|[[start:​hype_file_reference:​geoclass.txt|GeoClass.txt]]|
Line 297: Line 532:
 |:::| |//​parreg//​|:::​| |:::| |//​parreg//​|:::​|
 |Runoff through drainage pipes| |//​trrcs//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |Runoff through drainage pipes| |//​trrcs//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
-|Infiltration| |//​mactrinf,​ mactrsm, macrate, srrate, bfroznsoil//​|[[start:​hype_file_reference:​par.txt|par.txt]]|+|:::| |//​tilegroup//​|[[start:​hype_file_reference:​classdata.txt|ClassData.txt]]| 
 +|:::​|//​tilefrac//​|//​tilefrac_1,​ tilefrac_2,​...,​tilefrac_10//​|[[start:​hype_file_reference:​geodata.txt|GeoData.txt]]| 
 +|Infiltration| |//​mactrinf,​ mactrsm, macrate, srrate, bfroznsoil, macfrac//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |:::​|//​pw//​|calculated from //​wc+fc+wp//​|:::​| |:::​|//​pw//​|calculated from //​wc+fc+wp//​|:::​|
 +|:::​|//​beta//​|//​srbeta//​ or calculated from //sralpha, srgamma//​|:::​|
 +|:::​|//​nlayer//​|//​srnlayer//​|:::​|
 |Percolation| |//mperc1, mperc2//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |Percolation| |//mperc1, mperc2//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |Saturated surface runoff| |//​srrcs//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |Saturated surface runoff| |//​srrcs//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
Line 306: Line 545:
  
 ^ Modules (file) ^ Procedures ^ Section ^ ^ Modules (file) ^ Procedures ^ Section ^
-| [[http://​hype.sourceforge.net/​doxy-html/​namespacesoil__processes.html|soil_processes (soil_proc.f90)]] | initiate_soil_water | groundwater runoff |+| [[http://​hype.sourceforge.net/​doxy-html/​namespacesoil__processes.html|soil_processes (soil_proc.f90)]] ​| calculate_soiltemp | soil temperature and frozen soil | 
 +| ::: | calculate_weigthed_temperature | ::: | 
 +| ::: | calculate_unfrozen_soil_water| ::: | 
 +| ::: | calculate_three_soil_temperature| ::: | 
 +| ::: | calculate_liquid_water_fraction| ::: | 
 +| ::: | initiate_soil_water | groundwater runoff |
 | ::: |calculate_soil_runoff| ::: | | ::: |calculate_soil_runoff| ::: |
 | ::: |calculate_tile_drainage| runoff thorugh drainage pipes | | ::: |calculate_tile_drainage| runoff thorugh drainage pipes |
-| ::: |infiltration ​| diversion of surface runoff and macropore flow, infiltration |+| ::: |calculate_infiltration_flow_diversion ​| diversion of surface runoff and macropore flow, infiltration ​
 +| ::: |add_infiltration | ::: |
 | ::: |percolation | percolation | | ::: |percolation | percolation |
 | ::: |add_macropore_flow | macropore flow | | ::: |add_macropore_flow | macropore flow |
 | [[http://​hype.sourceforge.net/​doxy-html/​namespacegeneral__water__concentration.html|general_water_concentration (general_wc.f90)]] | inflow_lowest_soillayer | upwelling | | [[http://​hype.sourceforge.net/​doxy-html/​namespacegeneral__water__concentration.html|general_water_concentration (general_wc.f90)]] | inflow_lowest_soillayer | upwelling |
- 
-===== Snow routines ===== 
- 
-==== Snow melt ==== 
-As default, snow melting occurs when the temperature is greater than the threshold temperature. The amount of snow (in mm) that melts (//melt//) depends on the snowmelt parameter //cmlt//, threshold temperature parameter //ttmp// and air temperature (//temp//). 
- 
-<m> melt = MIN(cmlt*(temp-ttmp),​snow) </m> 
- 
-The parameters //cmlt// and //ttmp// are related to land use.  ​ 
- 
-=== Snow melt models === 
-Alternative snowmelt models exist, but are not fully described here yet.  
- 
-== Model 0 (default) == 
-Temperature index model, without snow cover scaling 
- 
-<m> melt = MIN(cmlt*(temp-ttmp),​snow) </m> 
- 
-== Model 1 == 
-Temperature index model, with snow cover scaling 
- 
-<m> melt = MIN(cmlt*(temp-ttmp),​snow)*snowcover </m> 
- 
-== Model 2 == 
-Temperature and radiation index model, with snow cover scaling 
- 
- 
- 
- 
-==== Snow cover ==== 
- 
-Normally snow is assumed to cover the whole class if present. 
-Alternatively if parameters are given, snow cover fraction (//fsc//) within a class is calculated based on snow water equivalent (//snow//). The formulation is based on Samuelsson et al. (2006). During snow build up the snow cover increase as a function of snow water equivalent until a maximum value (general parameter //fscmax//) is reached. 
- 
-<m> fsc=fscmax*tanh(0.1*snow) </m> 
- 
-It is also possible to specify a minimum snow cover (general parameter //​fscmin//​). ​ 
-As soon as the fractional snow cover area reaches above a certain threshold (//​fscmax-fsclim//​),​ the snow cover area is determined by another relation that represents the redistribution of snow during winter. In this case snow cover is dependent on maximum snow pack during the winter (//​snowmax//​) and a snow cover redistribution factor that is dependent on variation in elevation (//​stdelev//,​ the standard deviation of elevation within the subbasin) and land use. 
- 
-<m> fsc= snow / {snowmax*fscdist} </m> 
- 
-<m> fscdist=fscdist0+fscdist1*stdelev </m> 
- 
-The snow distribution factor (//​fscdist//​) is determined by three land use dependent parameters; //​fscdist0//​ and //​fscdist1//​ in the linear equation and a maximum value (//​fscdistmax//​). Also in this case the snowcover is limited by the maximum and minimum value parameters. When the end of the snow season approaches (defined by general parameter //fsck1//) the //snowmax// variable is gradually decreased in order to be reset before next winter season: 
- 
-<m> snowmax=snowmax-(fsck1*snowmax-snow)*{1-e^{-fsckexp*ts}}/​{fsck1} </m> 
- 
-<m> {snow}/​{snowmax}<​fsck1 </m> 
- 
-The equation depends on two general parameters, //fsck1// and //​fsckexp//,​ where //fsckexp// depend on time (//ts// is seconds per timestep of simulation). 
- 
-For winters when the snow pack not reach the definition of large snow pack, the first equation is used during the whole season. ​ 
- 
-==== 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 (//temp//). 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}{ 
- ​\matrix{2}{2} 
-    {deepmem {for\ deeptemp} 
-    surfmem*e^{-depthrel*depth(k)} {for\ soil\ layer\ k} }} </m> 
- 
-<m> weigth_{air}={1}/​{soilmem+10*snowdepth} </m> 
- 
-<m> deeptemp=weight_{air}*temp+(1-weight_{air})*deeptemp </m> 
- 
-<m> soiltemp=weight_{air}*temp+(1-weight_{air}-weight_{deep} )*soiltemp+weight_{deep}*deeptemp </m> 
- 
-In the default snow depth model, snow density (//​snowdens//​) depends on the snow's age in days (//​snowage//​). Snow density for fresh snow (//​sdnsnew//​) and the increase of density with snow age (//​snowdensdt//​) are general parameters (~ 0.1 and ~0.002). The snow's age increases by one every time step, but are weighted with age (0) for any new snow. 
- 
-<​m> ​ snowage = (snowage + 1)*oldsnow/​(oldsnow+snowfall) </m> 
- 
-<​m> ​ snowdens = sdnsnew + snowdensdt * snowage </m> 
- 
-<​m> ​ snowdepth = 0.1 * snow/​snowdens </m> 
- 
-In the alternative snow depth model, snow density is calculated by a compacting factor. Snow density for fresh snow (//​sdnsnew//​),​ maximum snow density (//​sdnsmax//​),​ compactation rate for low temperatures (//​sdnsrate//​) and additional compactation for high temperature (//​sdnsradd//​) are all general parameters. The change in snowdensity (//​densdt//​) due to compactation each time step is calculated as: 
- 
-<​m> ​ densdt = sdnsrate*(sdnsmax-snowdens) </m> 
- 
-for cold days (temperature is below threshold temperature parameter //ttmp//), and  
- 
-<​m> ​ densdt = (sdnsrate+sdnsradd)*(sdnsmax-snowdens) </m> 
- 
-for warm days. 
- 
-==== Links to file reference ==== 
- 
-^Section ^Symbol ^Parameter/​Data ^File ^ 
-|Snow melt|//​cmlt,​ ttmp//​|//​cmlt,​ ttmp//​|[[start:​hype_file_reference:​par.txt|par.txt]]| 
-|:::​|//​temp//​|calculated from|[[start:​hype_file_reference:​tobs.txt|Tobs.txt]]| 
-|Snow cover|//​stdelev//​|//​elev_std//​|[[start:​hype_file_reference:​geodata.txt|GeoData.txt]]| 
-|:::​|//​fscmax,​ fscdist0, fscdist1, fsck1, fsckexp//​|//​fscmax,​ fscdist0, fscdist1, fsck1, fsckexp//​|[[start:​hype_file_reference:​par.txt|par.txt]]| 
-|:::| |//​fscmin,​fsclim,​fscdistmax//​|:::​| 
-|Soil temperature and snow depth|//​deeptemp//​|//​init2//​|[[start:​hype_file_reference:​par.txt|par.txt]]| 
-|:::| |//deepmem, surfmem, depthrel, sdnsnew, snowdensdt, sdnsmax, sdnsrate, sdnsradd, ttmp//|:::| 
- 
-==== Links to relevant procedures in the code ==== 
- 
-^ Modules (file) ^ Procedures ^ Section ^ 
-| [[http://​hype.sourceforge.net/​doxy-html/​namespacesoil__processes.html|soil_processes (soil_proc.f90)]]| calculate_snow | snow melt | 
-| ::: | calculate_snowmelt | ::: | 
-| ::: | snowalbedo_function | ::: | 
-| ::: | calculate_fractional_snowcover | snow cover | 
-| ::: | calculate_snowdepth | soil temperature and snow depth | 
-| ::: | calculate_soiltemp | ::: | 
-| ::: | calculate_weigthed_temperature | ::: | 
- 
  
  
Line 471: Line 608:
 Glacier melting, snow melting on snowfield and/or rain are added to the soil. Thus the soil represents the whole glacier class area. The concentrations in the glacial melt water are zero. This means that any atmospheric deposition of nutrients is lost on the glacier. Glacier melting, snow melting on snowfield and/or rain are added to the soil. Thus the soil represents the whole glacier class area. The concentrations in the glacial melt water are zero. This means that any atmospheric deposition of nutrients is lost on the glacier.
  
 +The soil water is calculated as described above.
 ==== Links to file reference ==== ==== Links to file reference ====
  
Line 481: Line 619:
 |//​c//​|//​logvolcorr//​|[[start:​hype_file_reference:​glacierdata.txt|GlacierData.txt]]| |//​c//​|//​logvolcorr//​|[[start:​hype_file_reference:​glacierdata.txt|GlacierData.txt]]|
 | |//​glactype//​|:::​| | |//​glactype//​|:::​|
-|//T//|see needed data in [[start:​hype_model_description:​processes_above_ground#​links_to_file_reference|temperature]]| |+|//T//|see needed data in [[start:​hype_model_description:​processes_above_ground#​links_to_file_reference|Links for temperature]]| |
 |//​swrad//​|calculated or from|[[start:​hype_file_reference:​swobs.txt|SWobs.txt]]| |//​swrad//​|calculated or from|[[start:​hype_file_reference:​swobs.txt|SWobs.txt]]|
-|//coef0//​|//​glacvcoef//​ or //​glacvcoef1//​|[[start:​hype_file_reference:​par.txt|par.txt]]|+|//coef//​|//​glacvcoef//​ or //​glacvcoef1//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |//​exp//​|//​glacvexp//​ or //​glacvexp1//​|:::​| |//​exp//​|//​glacvexp//​ or //​glacvexp1//​|:::​|
 |//cmlt, ttmp//​|//​glaccmlt,​ glacttmp//​|:::​| |//cmlt, ttmp//​|//​glaccmlt,​ glacttmp//​|:::​|
 |//​albedo<​sub>​snow</​sub>//​|calculated from //snalbmin, snalbmax, snalbkexp//​|:::​| |//​albedo<​sub>​snow</​sub>//​|calculated from //snalbmin, snalbmax, snalbkexp//​|:::​|
-| |//glacalb, glacdens, glac2arlim, crefr, cmrad, ​fepotglac//|:::|+| |//glacalb, glacdens, glac2arlim,fepotglac//​|:::​| 
 +|//crefr, cmrad//​|//​glaccrefrglaccmrad//|:::|
  
 ==== Links to relevant procedures in the code ==== ==== Links to relevant procedures in the code ====
Line 499: Line 638:
  
 ===== 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.
 +
 +Radic, V. and Hock, R., 2010. Regional and global volumes of glaciers derived from statistical upscaling of glacier inventory data, J. Geophys. Res., 115, F01010, doi:​10.1029/​2009JF001373.
  
 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. 
  
-RadicV. and HockR.2010. Regional and global volumes of glaciers derived from statisti-cal upscaling of glacier inventory dataJGeophysRes., 115, F01010, ​doi:10.1029/2009JF001373.+StadnykTAMK MacDonaldA TefsSJ Déry, K Koenig, D Gustafsson, K Isberg, and B Arheimer2020Hydrological modeling of freshwater discharge into Hudson Bay using HYPEElem Sci Anth8: 43. doi:10.1525/elementa.439 
 + 
 +Zhao, L., and D.M. Gray 1999. Estimating snowmelt infiltration into frozen soils, Hydrological Processes, 13:​1827-1842. 
  
  
start/hype_model_description/hype_land.1539605226.txt.gz · Last modified: 2023/11/16 14:28 (external edit)