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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.)
Model:TopoFlow-Channels-Kinematic Wave + (The kinematic wave method for flow routing in the channels of a D8-based river network.)
Model:RASCAL + (The main source code calls sub-modules tha … The main source code calls sub-modules that simulate the following processes:- Vegetation community colonization as a function of local water depth. Colonization is deterministic over some ranges and stochastic in others.- Solution of flow field in two dimensions using a cellular automata algorithm (see Larsen and Harvey, 2010, Geomorphology, and Larsen and Harvey, 2010 in press, American Naturalist). The flow field is only simulated during high-flow events that entrain sediment.- Sediment transport by flow according to an advection-dispersion equation. Within each high-flow pulse, steady conditions are assumed.- Evolution of the topography through sediment transport, peat accretion (which is based on Larsen et al., Ecological Monographs, 2007), diffusive erosion of topographic gradients, vegetative propagation, and below-ground biomass expansion.- Adjustment of water levels and high-flow discharge to satisfy a water balance and compensate for the growth of vegetation patches.sate for the growth of vegetation patches.)
Model:Frost Model + (The mean annual temperature of the warmest and coldest months at a given location gives a first-order estimate of distribution of permafrost.)
Model:Kirwan marsh model + (The model calculates changes in elevation … The model calculates changes in elevation and vegetation growth for a hypothetical salt marsh. In each cell, elevation change is calculated as the difference between accretion and erosion. Accretion rates are a function of inundation depth, vegetation growth, and suspended sediment concentration. Water routed according to Rinaldo et al. (1999) scheme. Erosion rates calculated according to excess sheer stress. Channels widen according to a diffusion-like routine where downslope transport is inversely proportional to vegetation. Vegetation grows according to Morris et al. (2002) where biomass is proportional to inundation depth up until an optimum depth. Episodic vegetation disturbance is simulated by removing vegetation from randomly selected cells (Kirwan et al., 2008). Another version of the model treats wave erosion in a simplistic manner (Kirwan and Murray, 2008).mplistic manner (Kirwan and Murray, 2008).)
Model:ESCAPE + (The model computes flow accumulation using … The model computes flow accumulation using multiple flow direction over unstructured grids based on + an adaptation of the implicit approach proposed by Richardson & Perron (Richardson, Hill, & Perron, 2014). + an extension of the parallel priority-flood depression-filling algorithm from (Barnes, 2016) to unstructured mesh is used to simulate sedimentation in upland areas and internally drained basins. + marine sedimentation is based on a diffusion algorithm similar to the technique proposed in pybadlands (Salles, Ding, & Brocard, 2018).sed in pybadlands (Salles, Ding, & Brocard, 2018).)
Model:HBV + (The model consists of subroutines for mete … The model consists of subroutines for meteorological interpolation, snow accumulation and melt, evapotranspiration estimation, a soil moisture accounting procedure, routines for runoff generation and finally, a simple routing procedure between subbasins and in lakes. It is possible to run the model separately for several subbasins and then add the contributions from all subbasins. Calibration as well as forecasts can be made for each subbasin.s forecasts can be made for each subbasin.)
Model:D'Alpaos model + (The model describes the tidal-network init … The model describes the tidal-network initiation and development, and the vertical accretion of the adjacent marsh platform. Tidal network development is driven by the exceedance of a local hydrodynamic bottom shear stress, controlled by water surface gradients. Marsh vertical growth is modeled by using a sediment balance equation acconting for erosion and deposition terms. The deposition terms account for sediment settling, trapping and organic production.settling, trapping and organic production.)
Model:FUNDY + (The model is forced by tidal or other barotropic boundary conditions, wind, and/or fixed baroclinic pressure gradient, all acting at a single frequency (including zero) and specified by the user.)
Model:Equilibrium Calculator + (The model predicts bankfull geometry of si … The model predicts bankfull geometry of single-thread, sand-bed rivers from first principles, i.e. conservation of channel bed and floodplain sediment, which does not require the a-priori knowledge of the bankfull discharge. Building on previous work on the equilibrium of engineered rivers, i.e. rivers with fixed banks and sinuosity (Blom et al., 2016, 2017, Arkesteijn et al., 2019), as well as formulations for floodplain morphodynamics (Lauer & Parker, 2008, Viparelli et al., 2013, Lauer et al., 2016) and bank migration (Parker et al., 2011, Eke et al., 2014, Davidson & Eaton, 2018, De Rego et al., 2020), we derive equilibrium solutions for channel geometry (width, depth, slope), floodplain sediment size distribution, bankfull discharge, channel migration and overbank deposition rates. ReferencesArkesteijn, L., Blom, A., Czapiga, M. J., Chavarrias, V. & Labeur, R. J. (2019). The quasi-equilibrium longitudinal profile in backwater reaches if the engineered alluvial river: A space-marching method, Journal of Geophysical Research: Earth Surface 124, 2542-2560.Blom, A., Viparelli, E. & Chavarrias, V. (2016). The graded alluvial river: Profile concavity and downstream fining, Geophysical Research Letters 43 (12), 6285-6293.Blom, A., Arkesteijn, L., Chavarrias, V. & Viparelli, E. (2017). The equilibrium alluvial river under variable flow and its channel-forming discharge, Journal of Geophysical Research: Earth Surface 122, 1924-1948.Davidson, S.L. & Eaton, B. C. (2018). Beyond Regime: A stochastic model of floods, bank erosion, and channel migration. Water Resources Research, 54, 6282-6298. De Rego, K., Lauer, J. W., Eaton, B. & Hassan, M. (2020). A decadal-scale numerical model for wandering, cobble-bedded rivers subject to disturbance, Earth Surface Processes and Landforms 45, 912-927. Eke, E., Parker, G. & Shimizu, Y. (2014). Numerical modeling of erosional and depositional bank processes in migrating river bends with self-formed width: Morphodynamics of bar push and bank pull, Journal of Geophysical Research: Earth Surface 119, 1455-1483.Lauer, J. W. & Parker, G. (2008). Modeling framework for sediment deposition, storage, and evacuation in the floodplain of a meandering river: Theory, Water Resources Research 44, W04425, doi: 10.1029/2006WR005528.Lauer, J. W., Viparelli, E. & Piegay, H. (2016). Morphodynamics and sediment tracers in 1-D (MAST-1D): 1-D sediment transport that includes exchange with an off-channel sediment reservoir, Advances in Water Resources 93, 135-149.Parker, G., Shimizu, Y., Wilkerson, G. V., Eke, E. C., Abad, J. D., Lauer, J. W., Paola, C., Dietrich, W. E. & Voller, V. R. (2011). A new framework for modeling the migration of meandering rivers, Earth Surface Processes and Landforms 36, 70-86.Viparelli, E., Lauer, J. W., Belmont, P. & Parker, G. (2013). A numerical model to develop long-term sediment budgets using isotopic sediment fingerprints, Computers & Geosciences 53, 114-122.ediment budgets using isotopic sediment fingerprints, Computers & Geosciences 53, 114-122.)
Model:Tracer dispersion calculator + (The model represent the streamwise and vertical dispersal of a patch of tracer stones in an equilibrium gravel bed.)
Model:SWEHR + (The model simulates infiltration, fluid flow, and sediment transport. Fluid behavior is influenced by sediment concentration.)
Model:Meander Centerline Migration Model + (The model simulates the lateral migration of a meandering rivers, allowing the formation of oxbow lakes and scroll bars which may have a different erosional resistance with respect to the pristine floodplain.)
Model:PyDeCe + (The model simulates transport and deposition from the dense endmember of a pyroclastic density currents generated either by impulsive column collapse or sustained fountaining eruptions.)
Model:1DBreachingTurbidityCurrent + (The model solves both Gary Parker's three … The model solves both Gary Parker's three and four equation models for sediment mixtures. A condition was incorporated in the model to solve the equation of conservation of turbulent kinetic energy (fourth equation) and to decide how to estimate the friction coefficients. See also: Eke, E., Viparelli, E., and Parker, G., 2011. Field-scale numerical modeling of breaching as a mechanism for generating continuous turbidity currents. Geosphere, 7, 1063-1076. Doi: 10.1130/GES00607.1ents. Geosphere, 7, 1063-1076. Doi: 10.1130/GES00607.1)
Model:UEB + (The model uses physically-based calculations of radiative, sensible, latent and advective heat exchanges.)