Property:Describe processes
From CSDMS
This is a property of type Text.
R
G
See the GEOMBEST++ Users Guide, section 4.
Equilibrium profile
Sea Level Change
Depth-Dependant Shoreface Response Rate
Backbarrier Deposition
Bay and Marsh Infilling (including wave edge erosion) +
W
See the WRF-Hydro Technical Description https://ral.ucar.edu/projects/wrf_hydro/technical-description-user-guide
"First the 1-dimensional (1D) column land surface model calculates the vertical fluxes of energy (sensible and latent heat, net radiation) and moisture (canopy interception, infiltration, infiltration-excess, deep percolation) and soil thermal and moisture states. Infiltration excess, ponded water depth and soil moisture are subsequently disaggregated from the 1D LSM grid, typically of 1–4 km spatial resolution, to a highresolution, typically 30–100 m, routing grid using a time-step weighted method (Gochis and Chen, 2003) and are passed to the subsurface and overland flow terrain-routing modules. In typical U.S. applications, land cover classifications for the 1D LSMs are provided by the USGS 24-type Land Use Land Cover product or MODIS Modified IGBP 20-category land cover product (see WRF/WPS documentation); soil classifications are provided by the 1-km STATSGO database (Miller and White, 1998); and soil hydraulic parameters that are mapped to the STATSGO soil classes are specified by the soil analysis of Cosby et al. 20 (1984). Other land cover and soil type classification datasets can be used with WRF-Hydro but users are responsible for mapping those categories back to the same categories as used in the USGS or MODIS land cover and STATSGO soil type datasets. The WRF model pre-processing system (WPS) also provides a fairly comprehensive database of land surface data that can be used to set up the Noah and Noah-MP land surface models. It is possible to use other land cover and soils datasets.
Then subsurface lateral flow in WRF-Hydro is calculated prior to the routing of overland flow to allow exfiltration from fully saturated grid cells to be added to the infiltration excess calculated by the LSM. The method used to calculate the lateral flux of the saturated portion of the soil column is that of Wigmosta et al. (1994) and Wigmosta and Lettenmaier (1999), implemented in the Distributed Hydrology Soil Vegetation Model (DHSVM). It calculates a quasi-3D flow, which includes the effects of topography,
saturated soil depth, and depth-varying saturated hydraulic conductivity values. Hydraulic gradients are approximated as the slope of the water table between adjacent grid cells in either the steepest descent or in both x- and y-directions. The flux of water from one cell to its down-gradient neighbor on each timestep is approximated as a steady-state solution. The subsurface flux occurs on the coarse grid of the LSM while overland flow occurs on the fine grid.
Next, WRF-Hydro calcuates the water table depth according to the depth of the top of the saturated soil layer that is nearest to the surface. Typically, a minimum of four soil layers are used in a 2-meter soil column used in WRF-Hydro but this is not a strict requirement. Additional discretization permits improved resolution of a time-varying water table height and users may vary the number and thickness of soil layers in the model namelist described in the Appendices A3, A4, and A5.
Then overland flow is defined. The fully unsteady, spatially explicit, diffusive wave formulation of Julien et al. (1995-CASC2D) with later modification by Ogden (1997) is the current option for representing overland flow, which is calculated when the depth of water on a model grid cell exceeds a specified retention depth. The diffusive wave equation accounts for backwater effects and allows for flow on adverse slopes (Ogden, 1997). As in Julien et al. (1995), the continuity equation for an overland flood wave is combined with the diffusive wave formulation of the momentum equation. Manning’s equation is used as the resistance formulation for momentum and requires specification of an overland flow roughness parameter. Values of the overland flow roughness coefficient used in WRF-Hydro were obtained from Vieux (2001) and were mapped to the existing land cover classifications provided by the USGS 24-type land-cover product of Loveland et al. (1995) and the MODIS 20-type land cover product, which are the same land cover classification datasets used in the 1D Noah/Noah-MP LSMs.
Additional modules have also been implemented to represent stream channel flow processes, lakes and reservoirs, and stream baseflow. In WRF-Hydro v5.0 inflow into the stream network and lake and reservoir objects is a one-way process. Overland flow reaching grid cells identified as ‘channel’ grid cells pass a portion of the surface water in excess of the local ponded water retention depth to the channel model. This current formulation implies that stream and lake inflow from the land surface is always positive to the stream or lake element. There currently are no channel or lake loss functions where water can move from channels or lakes back to the landscape. Channel flow in WRF-Hydro is represented by one of a few different user-selected methodologies described below. Water passing into and through lakes and reservoirs is routed using a simple level pool routing scheme. Baseflow to the stream network is represented using a conceptual catchment storage-discharge bucket model formulation (discussed below) which obtains “drainage” flow from the spatially-distributed landscape. Discharge from buckets is input directly into the stream using an empirically-derived storage-discharge relationship. If overland flow is active, the only water flowing into the buckets comes from soil drainage. This is because the 21 overland flow scheme will pass water directly to the channel model. If overland flow is switched off and channel routing is still active, then surface infiltration excess water from the land model is collected over the pre-defined catchment and passed into the bucket as well. Each of these process options are enabled through the specification of options in the model namelist file."
R
T
D
M
S
Soil infiltration, as calculated using the Green-Ampt equation. +
H
Soil production from to different lithologies; weathering and transport of discrete rock blocks; transport of soil using linear diffusion; boundary incision +
A
Spatiotemporal varying sediment availability through simulation of the process of beach armoring.
A 1-D advection scheme.
Multifraction Erosion and Deposition.
Hydraulic Mixing, Infiltration, and Evaporation. +
P
A
B
C
Subsidence
Depth dependent carbonate production
Lithofacies spatial distribution based on number of neighoubrs of same facies type +
Subsidence and uplift
Eustatic oscillations
Water depth dependent in-situ carbonate production
Spatial variations in sediment production rate
Depth dependent sediment transport
Diffusional sediment transport +
T
TISC is a geodynamic numerical model combining computer modeling techniques to investigate the interplay between lithospheric-scale tectonics and erosion/sedimentation at the Earth's surface. TISC is a code that integrates the calculation of lithospheric flexure, kinematic fault deformation, and surface mass transport (erosion/transport/sedimentation) along drainage networks. In other words, TISC is a software that simulates the evolution of 3D large-scale sediment transport together with tectonic deformation and lithospheric isostatic movements on geological time scales. TISC stands for Tectonics, Isostasy, Surface transport, and Climate.
Take a look at the documentation wiki and download TISC at GitHub. TISC is available for Linux / OS X platforms only.
Download TISC from the github repository
See also the Open Forum.
The Landscape Evolution Model (LEM) component of TISC can deal with closed (internally-drained, endorheic) basins and finds the equilibrium between precipitation in drainage basins and evaporation in terminal lakes. Orographic precipitation is also calculated. Relative to other existing LEMs (Child, Cascade, Eros, ...), TISC explicitly handles lakes forming in local topographic minima, finding the outlet of such water bodies, and accounting for their role as hydrological and sedimentary sinks. It also accounts for internal drainage (endorheism) depending on the collected runoff and the lake's surface evaporation, explicitly calculating the extension of the resulting closed-drainage lakes. It also tracks sediment horizons in the sedimentary basins. TISC uses a fixed rectangular mesh for the finite-difference method. Water flow is at steady state.
Particular attention is given to the formation of sedimentary basins, with a full track of the source-to-sink balance between erosion and sedimentation. Further information in these papers (G-C, 2002, Basin Res., G-C et al., 2003) showing first results of this numerical model. +
TOPMODEL is defined as a variable contributing area conceptual model in which the dynamics of surface and subsurface saturated areas is estimated on the basis of storage discharge relationships established from a simplified steady state theory for downslope saturated zone flows. The theory assumes that the local hydraulic gradient is equal to the local surface slope and implies that all points with the same value of the topographic index, a/tan B will respond in a hydrologically similar way. This index is derived from the basin topography, where a is the drained area per unit contour length and tan B is the slope of the ground surface at the location. Thus the model need make calculations only for representative values of the index. The results may then be mapped back into space by knowledge of the pattern of the index derived from a topographic analysis. +
ThawLake1D Model couples a permafrost thermal model, a lake ice model and a subsidence model. It models heat conductio through a lake-permafrost system, evaluating temperature with depth. +
The Degree-Day method for modeling Snowmelt. +
The Energy Balance method for modeling snowmelt. +
