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Model:GOLEM + (Runoff, hillslope and channel sediment transport.)
Model:SBEACH + (SBEACH is an empirically based numerical m … SBEACH is an empirically based numerical model for estimating beach and dune erosion due to storm waves and water levels. The magnitude of cross-shore sand transport is empirically related wave energy dissipation per unit water volume in the main portion of the surf zone. Direction of transport is dependent on deep water wave steepness and sediment fall speed.er wave steepness and sediment fall speed.)
Model:STWAVE + (STWAVE simulates depth-induced wave refrac … STWAVE simulates depth-induced wave refraction and shoaling, current- induced refraction and shoaling, depth- and steepness-induced wave breaking, diffraction, wind-wave growth, and wave-wave interaction and whitecapping that redistribute and dissipate energy in a growing wave field. dissipate energy in a growing wave field.)
Model:SWAN + (SWAN accounts for the following physics: * … SWAN accounts for the following physics:* Wave propagation in time and space, shoaling, refraction due to current and depth, frequency shifting due to currents and non-stationary depth.* Wave generation by wind.* Three- and four-wave interactions.* Whitecapping, bottom friction and depth-induced breaking.* Wave-induced set-up.* Propagation from laboratory up to global scales.* Transmission through and reflection (specular and diffuse) against obstacles.* Diffraction.diffuse) against obstacles. * Diffraction.)
Model:SWMM + (SWMM accounts for various hydrologic proce … SWMM accounts for various hydrologic processes that produce runoff from urban areas. These include:* time-varying rainfall* evaporation of standing surface water* snow accumulation and melting* rainfall interception from depression storage* infiltration of rainfall into unsaturated soil layers* percolation of infiltrated water into groundwater layers* interflow between groundwater and the drainage system* nonlinear reservoir routing of overland flow.linear reservoir routing of overland flow.)
Model:Auto marsh + (Salt marsh erosion by wind waves. The pre … Salt marsh erosion by wind waves. The presence of natural heterogeneities is an integral characteristic of salt marshes and needs to be account for, as local feedbacks could influence the large scale morphodynamic evolution of these wetlands. Herein, we use field data and a cellular automata model to investigate salt marsh response to wave action under different wave energy conditions and frequency of extreme events.onditions and frequency of extreme events.)
Model:Barrier Inlet Environment (BRIE) Model + (Sea-level rise, alongshore sediment transport, and tidal-driven sediment transport on barrier islands, resulting in storm-overwash, tidal inlet formation, migration, and closure, and barrier transgression)
Model:MCPM + (Sediment advection/diffusion Sediment settling Bed erosion Soil creep Organic sediment production Increase in effective settling due to vegetation Increase in drag due to vegetation)
Model:Sun fan-delta model + (Sediment routing in alluvial channels, deposition, erosion, avulsion)
Model:Erode + (Sediment transport (parameterized with slope and contributing area grids), rainfall, uplift, base-level lowering.)
Model:TwoPhaseEulerSedFoam + (Sediment transport under steady channel flow, oscillatory flow (sinusoidal and Stokes 2nd order waves))
Model:River Erosion Model + (Sediment transport, channel bed aggradatio … Sediment transport, channel bed aggradation/degradation, fluvial bank erosion (excess shear stress) and bank failure (mass wasting). See Lammers and Bledsoe (2018) and Lammers and Bledsoe (2019) for more information: https://www.sciencedirect.com/science/article/pii/S0022169418307303https://www.sciencedirect.com/science/article/pii/S0301479718314968.com/science/article/pii/S0301479718314968)
Model:Marsh column model + (Sedimentation, compaction, root growth and death, carbon deposition, carbon decay)
Model:PHREEQC + (See See 'Description of Input and Examples for PHREEQC Version 3 - A computer program for speciation, batch-reaction, one-dimensional transport, and inverse geochemical calculations'.)
Model:FUNWAVE + (See manual)
Model:SPHYSICS + (See manual)
Model:REF-DIF + (See manual version3)
Model:GEOMBEST++ + (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))
Model:WRF-Hydro + (See the WRF-Hydro Technical Description ht … 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."on of options in the model namelist file.")
Model:RiverMUSE + (See the associated published paper: https://doi.org/10.1086/684223)
Model:TOPOG + (See website, too many to describe: http://www-data.wron.csiro.au/topog/)
Model:Meanderpy + (Simple linear relationship between the nominal migration rate and curvature)
Model:SoilInfiltrationGreenAmpt + (Soil infiltration, as calculated using the Green-Ampt equation.)
Model:Hogback + (Soil production from to different lithologies; weathering and transport of discrete rock blocks; transport of soil using linear diffusion; boundary incision)
Model:AeoLiS + (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.)

Model:Plume + (Steady-state river generated hypopycnal sediment plume)

Model:Avulsion + (Stream avulsion over a delta)
Model:Bing + (Submarine debris flow generated by slope failure)
Model:CarboCAT + (Subsidence Depth dependent carbonate production Lithofacies spatial distribution based on number of neighoubrs of same facies type)
Model:Cyclopath + (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)
Model:TISC + (TISC is a geodynamic numerical model combi … 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 repositorySee 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.ing first results of this numerical model.)
Model:TOPMODEL + (TOPMODEL is defined as a variable contribu … 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.index derived from a topographic analysis.)
Model:ThawLake1D + (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.)
Model:TopoFlow-Snowmelt-Degree-Day + (The Degree-Day method for modeling Snowmelt.)
Model:TopoFlow-Snowmelt-Energy Balance + (The Energy Balance method for modeling snowmelt.)
Model:TopoFlow-Evaporation-Energy Balance + (The Energy Balance method of estimating losses due to evaporation.)
Model:TopoFlow-Infiltration-Green-Ampt + (The Green-Ampt method for modeling infiltration.)
Model:PIHM + (The Penn State Integrated Hydrologic Model … The Penn State Integrated Hydrologic Model (PIHM) is a fully coupled multiprocess hydrologic model. Instead of coupling through artificial boundary conditions, major hydrological processes are fully coupled by the semi-discrete finite volume approach. For those processes whose governing equations are partial differential equations (PDE), we first discretize in space via the finite volume method. This results in a system of ordinary differential equations (ODE) representing those procesess within the control volume. Within the same control volume, combining other processes whose governing equations are ODE’s, (e.g. the snow accumulation and melt process), a local ODE system is formed for the complete dynamics of the finite volume.he complete dynamics of the finite volume.)
Model:QUAL2K + (The QUAL2K framework includes the followin … The QUAL2K framework includes the following new elements:*Software Environment and Interface. Q2K is implemented within the Microsoft Windows environment. Numerical computations are programmed in Fortran 90. Excel is used as the graphical user interface. All interface operations are programmed in the Microsoft Office macro language: Visual Basic for Applications (VBA). *Model segmentation. Q2E segments the system into river reaches comprised of equally spaced elements. Q2K also divides the system into reaches and elements. However, in contrast to Q2E, the element size for Q2K can vary from reach to reach. In addition, multiple loadings and withdrawals can be input to any element.*Carbonaceous BOD speciation. Q2K uses two forms of carbonaceous BOD to represent organic carbon. These forms are a slowly oxidizing form (slow CBOD) and a rapidly oxidizing form (fast CBOD).*Anoxia. Q2K accommodates anoxia by reducing oxidation reactions to zero at low oxygen levels. In addition, denitrification is modeled as a first-order reaction that becomes pronounced at low oxygen concentrations. *Sediment-water interactions. Sediment-water fluxes of dissolved oxygen and nutrients can be simulated internally rather than being prescribed. That is, oxygen (SOD) and nutrient fluxes are simulated as a function of settling particulate organic matter, reactions within the sediments, and the concentrations of soluble forms in the overlying waters.*Bottom algae. The model explicitly simulates attached bottom algae. These algae have variable stoichiometry.*Light extinction. Light extinction is calculated as a function of algae, detritus and inorganic solids.*pH. Both alkalinity and total inorganic carbon are simulated. The river’s pH is then computed based on these two quantities.*Pathogens. A generic pathogen is simulated. Pathogen removal is determined as a function of temperature, light, and settling.*Reach specific kinetic parameters. Q2K allows you to specify many of the *Weirs and waterfalls. The hydraulics of weirs as well as the effect of weirs and waterfalls on gas transfer are explicitly included.s on gas transfer are explicitly included.)
Model:TopoFlow-Infiltration-Richards 1D + (The Richards 1D method for modeling infiltration.)
Model:TopoFlow-Infiltration-Smith-Parlange + (The Smith-Parlange 3-parameter method for modeling infilteration.)
Model:TopoToolbox + (The TopoToolbox 2 is a Matlab based softwa … The TopoToolbox 2 is a Matlab based software for Digital Elevation Model (DEM) analysis. It uses an object oriented programming (OOP) approach to represent and work with geoferenced raster data, flow directions, stream networks and swath profiles in Matlab. TopoToolbox offers a wide range of tools to analyse DEMs, flow and stream networks, that allow for interactive and automated workflows.w for interactive and automated workflows.)
Model:Mrip + (The bed is represented by a 2-D matrix. At … The bed is represented by a 2-D matrix. At this time the bed is 250 x 250. Each block (i,j) is taken to be a slab of sediment 10cm x 10cm x 1cm deep. A second matrix represents the flow. This is the same everywhere in the domain at each time point, except for a random spatial fluctuation representing turbulence.The user-defined flow picks up (or puts down) sediment according to a transport law. Three transport laws have been tested: Bailard (1981), Ribberink (1998) or simple rules. The simple rules are simply thresholds: (if flow greater than 70cm/sec pick up one block).Once sand block have been picked up, they are moved forward with the flow. Generally, I have used a fraction of the distance that the water would travel (jump_frac). So, with a flow of 100cm/sec, in one second that water goes 100 cm. The sand in this case would go 50 cm (half the distance). At the extremes, the model is sensitive to this parameter, but at intermediate values, it is not.Tested flows have consisted of combined sinusoidal flow+steady flow, purely osc, purely steady, and natural flow time series taken from current meter measurements. All flows have a random spatial fluctuation added at each time point. Once bedforms are generated, feedback rules are employed by altering the flow over the bedform. Once a bedform gets tall, the flow over the top accelerates, increasing transport at that location. In the steep lee of a bedform, a shadow zone forms where flow goes to ~zero, therefore transport goes to zero. These mechanisms destroy or build bedforms.hese mechanisms destroy or build bedforms.)
Model:Pllcart3d + (The code models the evolution of a diffusive interface and the instabilities that arises when a less viscous fluid pushes a more viscous one in a confined rectangular geometry.)
Model:TopoFlow-Channels-Diffusive Wave + (The diffusive wave method for flow routing in the channels of a D8-based river network.)
Model:TopoFlow-Channels-Dynamic Wave + (The dynamic wave method for flow routing in the channels of a D8-based river network.)
Model:CoAStal Community-lAnDscape Evolution (CASCADE) model + (The effects of individual storm events and … The effects of individual storm events and SLR on shoreface evolution; dune dynamics, including dune growth, erosion, and migration; overwash deposition by individual storms; large-scale coastline evolution arising from alongshore sediment transport processes; and human management activities.rocesses; and human management activities.)
Model:CVFEM Rift2D + (The four primary components of our multi-p … The four primary components of our multi-physics code include geomechanical, hydrologic, solute transport and heat transfer modules. The geomechanical module calculates displacement of an elastic lithosphere disturbed by an ice sheet load. Transient geomechanical deformation is represented by one-dimensional (lateral) viscous asthenosphere flow. Our geomechanical module is partially coupled to the hydrologic module by providing the rate of change in the mean normal stress. Mean normal stress change rate is included as a source term in the groundwater flow equation driving flow. Flow is also influenced by changes in the top specified hydraulic head boundary condition. We implement two-way coupling between fluid flow, solute transport and heat transfer module via density and viscosity equations of state. Three additional modules in our multi-physics code calculate changes to the upper hydraulic and thermal boundary conditions or alter the hydraulic transport properties (permeability) due to hydrogeomechanical failure. These include ice sheet evolution, permafrost, and failure analysis modules. Ice sheet thickness determines both the vertical load in the geomechanical module as well as the hydraulic head boundary condition at the land surface in the hydrologic module. In this study we adopted a simple parabolic polynomial equation to represent the idealized geometry of an ice sheet’s cross section in the ice sheet evolution module. We solved for permafrostformation at and below the land surface using a suite of one-dimensional heat transfer models. We allowed for grid growth within the permafrost module to account for changes in ice sheet thickness. A failure analysis module was used to modify permeability due to hydromechanical failure. We adopted the effective Coulomb’s Failure Stress change criterion from Ge et al.(2009) to assess regions of failure during glaciations.ess regions of failure during glaciations.)
Model:MODFLOW + (The ground-water flow equation is solved u … The ground-water flow equation is solved using the finite-difference approximation. The flow region is subdivided into blocks in which the medium properties are assumed to be uniform. In plan view the blocks are made from a grid of mutually perpendicular lines that may be variably spaced. Model layers can have varying thickness. A flow equation is written for each block, called a cell. Several solvers are provided for solving the resulting matrix problem; the user can choose the best solver for the particular problem. Flow-rate and cumulative-volume balances from each type of inflow and outflow are computed for each time step.d outflow are computed for each time step.)
Model:WASH123D + (The integrated multi-processes include: # … The integrated multi-processes include:# hydrological cycles (evaporation, evapotranspiration, infiltration, and recharges);# fluid flow (surface runoff in land surface, hydraulics and yydrodynamics in river/stream/canal networks;# interflow in vadose zones, and groundwater flow in saturated zones);# salinity transport and thermal transport (in surface waters and groundwater);# sediment transport (in surface waters);# water quality transport (any number of reactive constituents);# biogeochemical cycles (nitrogen, phosphorous, carbon, oxygen, etc.); and# biota kinetics (algae, phyotoplankton, zooplakton, caliform, bacteria, plants, etc.).lakton, caliform, bacteria, plants, etc.).)
Model:CellularFanDelta + (The key processes are 1) topographically-d … The key processes are 1) topographically-driven overland flow and 2) bedload transport by this flow. Through these processes the model self-organizes channels which incise, back-fill, and avulse. Processes are similar to alluvial fans. There are no marine processes besides bedload dumping. marine processes besides bedload dumping.)