Property:Extended model description
From CSDMS
This is a property of type Text.
D
The delta-building model DeltaRCM expanded to included vegetation effects. Vegetation colonizes, grows, and dies, and influences the delta through increasing bank stability and providing resistance to flow. Vegetation was implemented to represent marsh grass type plants, and parameters of stem diameter, carrying capacity, logistic growth rate, and rooting depth can be altered. +
H
The development of the HAMSOM coding goes back to the mid eighties where it emerged from a fruitful co-operation between Backhaus and Maier-Reimer who later called his model 'HOPE'. From the very beginning HAMSOM was designed with the intention to allow simulations of both oceanic and coastal and shelf sea dynamics.
The primitive equation model with a free surface utilises two time-levels, and is defined in Z co-ordinates on the Arakawa C-grid. Stability constraints for surface gravity waves and the heat conduction equation are avoided by the implementation of implicit schemes. With a user defined weighting between future and presence time levels a hierarchy of implicit schemes is provided to solve for the free surface problem, and for the vertical transfer of momentum and water mass properties. In the time domain a scheme for the Coriolis rotation is incorporated which has second order accuracy. Time- and space-dependent vertical exchange and diffusivity coefficients are determined from a simple zero-order turbulence closure scheme which has also been replaced by a higher order closure scheme (GOTM). The resolution of a water column may degenerate to just one grid cell. At the seabed a non-linear (implicit) friction law as well as the full kinematic boundary condition is applied. Seabed cells may deviate from an undisturbed cell height to allow for a better resolution of the topography. The HAMSOM coding excludes any time-splitting, i.e. free surface and internal baroclinic modes are always directly coupled. Simple upstream and more sophisticated advection schemes for both momentum and matter may be run according to directives from the user.
Successful couplings with eco-system models (ECOHAM, ERSEM), an atmospheric model (REMO), and both Lagrangian and Eulerian models for sediment transport are reported in the literature. For polar applications HAMSOM was coupled with a viscous-plastic thermo-hydrodynamic ice model of Hibler type. Since about 15 years in Hamburg, and overseas in more than 30 laboratories, HAMSOM is already being in use as a community model.
N
The fault can have an arbitrary trace given by two points (x1, y1) and (x2, y2) in the fault_trace input parameter. These value of these points is in model-space coordinates and is not based on node id values or number of rows and columns. +
F
The grid contains the value 1 where fractures (one cell wide) exist, and 0 elsewhere. The idea is to use this for simulations based on weathering and erosion of, and/or flow within, fracture networks. +
W
The hydrodynamic module of WWTM solves the shallow water equations modified through the introduction of a refined sub-grid model of topography to deal with flooding and drying processes in irregular domains (Defina, 2000). The numerical model, which uses finite-element technique and discretizes the domain with triangular elements, has been extensively tested in recent years in the Venice lagoon, Italy (D’Alpaos and Defina, 2007, Carniello et al., 2005; Carniello et al., 2009).
For the wind wave modulel the wave action conservation equation is used, solved numerically with a finite volume scheme, and fully coupled with the hydrodynamic module (see Carniello et al. 2005). The two modules share the same computational grid. +
H
The hydromad (Hydrological Model Assessment and Development) package provides a set of functions which work together to construct, manipulate, analyse and compare hydrological models. +
M
The mizuRoute tool post-processes runoff outputs from any distributed hydrologic model or land surface model to produce spatially distributed streamflow at various spatial scales from headwater basins to continental-wide river systems. The tool can utilize both traditional grid-based river network and vector-based river network data. +
O
The model accounts for glacier geometry (including contributory branches) and includes an explicit ice dynamics module. It can simulate past and future mass-balance, volume and geometry of (almost) any glacier in the world in a fully automated and extensible workflow. Publicly available data is used for calibration and validation. +
G
The model calculates a unique regression equation for each grid-cell between a the relative area of a specific land use (e.g. cropland) and global population. The equation is used to extrapolate that land use are into the future in each grid cell with predicted global population predictions. If the relative area of a land use reach a value of 95%, additional expansion is migrated to neighboring cells thus allowing spatial expansion. Geographic limitations are imposed on land use migration (e.g. no cropland beyond 60 degree latitude).
For more information:
Haney, N., Cohen, S. (2015), Predicting 21st century global agricultural land use with a spatially and temporally explicit regression-based model. Applied Geography, 62: 366-376. +
C
The model calculates the surface energy balance in order to represent energy transfer processes between the atmosphere and the ground. These processes include the radiation balance, the exchange of sensible heat, as well as evaporation and condensation. For a realistic representation of the thermal dynamics of the ground, the model includes processes such as the phase change of soil water and an insulating snow cover during winter. +
S
The model couples the shallow water equations with the Green-Ampt infiltration model and the Hairsine-Rose soil erosion model. Fluid flow is also modified through source terms in the momentum equations that account for changes in flow behavior associated with high sediment concentrations. See McGuire et al. (2016, Constraining the rates of raindrop- and flow-driven sediment transport mechanisms in postwildfire environments and implications for recovery timescales) for a complete model description and details on the numerical solution of the governing equations. +
1
The model evolves a 1D hillslope according to a non-linear diffusion rule (e.g. Roering et al. 1999) for varying boundary conditions idealised as a gaussian pulse of baselevel fall through time. A Markov Chain Monte Carlo inversion finds the most likely boundary condition parameters when compared to a time series of field data on hillslope morphology from the Dragon's Back Pressure Ridge, Carrizo Plain, CA, USA; see Hilley and Arrowsmith, 2008. +
M
The model is developed to simulate the sediment transport and alluvial morphodynamics of bedrock reaches. It is capable of computing the alluvial cover fraction, the alluvial-bedrock transition and flow hydrodynamics over both bedrock and alluvial reaches. This model is now validated against a set of laboratory experiment. Field scale application of the model can also be done using field parameters. +
S
The model is related to the numerical solution of the shallow water equations in spherical geometry. The shallow water equations are used as a kernel for both oceanic and atmospheric general circulation models and are of interest in evaluating numerical methods for weather forecasting and climate modeling. +
Q
The model is three-dimensional and fully nonlinear with a free surface, incorporates advanced turbulence closure, and operates in tidal time. Variable horizontal and vertical resolution are facilitated by the use of unstructured meshes of linear triangles in the horizontal, and structured linear elements in the vertical +
E
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. +
A
The model reproduce the effect of a variability in soil resistance on salt marsh erosion by wind waves.
The model consists of a two-dimensional square lattice whose elements, i, have randomly distributed resistance, r_i. The critical soil height H_ci for boundary stability is calculated from soil shear strength values and is assumed as representative of soil resistance, as it is a convenient way to take into account general soil and ambient conditions. The erosion rate of each cell, E_i, which represents the erosion of an homogeneous marsh portion, is defined as:
E_i=〖αP〗^β exp (-H_ci/H)
Where α and β are non-dimensional constants set equal to 0.35 and 1.1 respectively, P is the wave power, and H is the mean wave height.
The model follows three rules: i) only neighbors of previously eroded cells can be eroded. Therefore, only cells having at least one side in common with previously eroded elements are susceptible to erosion; ii) at every time step one element is eroded at random with probability p_i=E_i/(∑E_i ); iii) A cell is removed from the domain if it remains isolated from the rest of the boundary (no neighbors). +
W
The model simplifies the geometry of a backbarrier tidal basin with 3 variables: marsh depth, mudflat depth, mudflat width. These 3 variables are evolved by sediment redistribution driven by wave processes. Sediment are exchanged with the open ocean, which is an external reservoir. Organic sediments are produced on the marsh platform. +
S
The model simulates the formation, drift, and melt of a population of icebergs utilizing Monte Carlo based techniques with a number of underlying parametric probability distributions to describe the stochastic behavior of iceberg formation and dynamics. +
M
The model simulates the long-term evolution of meandering rivers above heterogeneous floodplain surfaces, i.e. floodplains that have been reworked by the river itself through the formation of oxbow lakes and point bars. +
