Property:Describe key physical parameters
From CSDMS
This is a property of type Text.
B
Shear stress-driven fluvial erosion, primarily modulated by bed erodibility, critical bed shear stress, block delivery, and block size. +
A
Snow settling, temperature diffusion, snow saltation and suspension, snow metamorphism, terrain radiation. +
D
Soil flux is calculated at the product of diffusivity, a characteristic transport depth, and an exponential velocity profile based on total soil depth. +
2
Solves the non-linear, depth-averaged conservation equations, using finite difference scheme of Koutitas (1988) +
T
Species specific, logistic growth equation for individual trees.
Sediment flux for each tree fall a function of sediment volume, transport distance, and hillslope angle.
Sediment volume and transport distance a function of tree diamter. +
W
Spectral action balance equation. +
I
Standard flow routing and uniform sampling principles are used to govern the processes of this model. +
C
H
Terrain analysis.
One equation is the resolution of a hexagon can be estimated using its area instead of edge length. +
W
The WRF-ARW core is based on an Eulerian solver for the fully compressible nonhydrostatic equations, cast in flux (conservative) form, using a mass (hydrostatic pressure) vertical coordinate. Prognostic variables for this solver are column mass of dry air (mu), velocities u, v and w (vertical velocity), potential temperature, and geopotential. Non-conserved variables (e.g. temperature, pressure, density) are diagnosed from the conserved prognostic variables. The solver uses a third-order Runge-Kutta time-integration scheme coupled with a split-explicit 2nd-order time integration scheme for the acoustic and gravity-wave modes. 5th-order upwind-biased advection operators are used in the fully conservative flux divergence integration; 2nd-6th order schemes are run-time selectable. +
B
The dynamics of erosion and deposition are schematized with a relationship, which represents a diffusion scheme that changes the bottom elevation at a rate linearly proportional to the difference between the current and the equilibrium profile, defined by the Dean's equation, and then redistributes the removed or deposited material in equal parts between the contiguous inshore and offshore locations.<br>
The phenomenon of overwash is schematized assuming that the first shoreface element of the barrier island is eroded of a quantity, which is related to the frequency of hurricanes and severe storms and to the difference between the maximum elevation of the barrier and the mean sea level. +
D
C
The evolution of the coastline is governed by a continuity equation; the rate of horizontal shoreline change in the local cross-shore direction is proportional to the divergence of alongshore sediment flux. Alongshore sediment transport is computed via the common CERC formula, which relates alongshore sediment flux to breaking-wave approach angle and breaking wave height. Breaking-wave characteristics in each shoreline location are calculated by starting with the deep-water height and propagation direction (obtained for each time slice from the input wave file), and refracting and shoaling the waves over assumed shore-parallel contours until breaking occurs. The CERC equation also involves an empirical constant K, which can be configured by the model user. Other equations for sediment flux can easily be substituted. See Ashton and Murray (2006a) for details. +
A
The geometry of a channel centerline is represented as a direction series using a second-order autoregressive formulation. The governing equation is
theta(i) = b_1*theta(i-1) + b_2*theta(i-2) + epsilon(i)
where theta is the channel direction, i is the centerline node index, b_1 and b_2 are coefficients, and epsilon is a random disturbance drawn from a normal distribution with a mean of zero. +
O
The key algorithms and parameters are described in length the Geoscientific Model Development paper by Adams et al., (2017). +
S
The key equations and parameters are described in Shobe et al (2017, Geoscientific Model Development). +
D
The key methods used are:
1) Feature normalization and principal component analysis
2) Spatial clustering using GEOSOM algorithm
3) Hierarchical agglomerative clustering to built nested clusters +
C
The key parameters are temperature; density; heat capacity; thermal conductivity; porosity; volume fractions of ice, unfrozen water, and air; degree of water saturation; pore-water solute type and concentration; particle radii. +
1
The key physical parameters are the hillslope length and height, as well as a parameter which specifies the underlying asymmetry in the particle dynamics. The process of determining these parameters is described in the simulation section of a corresponding paper (which can be accessed here: https://arxiv.org/abs/1801.02810). +
Q
The key physical parameters are: (1) the sediment unit-flux, defined as the sediment input from the river network in units of volume per unit width. (2) The average water discharge per unit width. (3) The basement slope on top of which the delta develops. (4) The base-level curve.
The key equations are a sediment mass balance and the boundary conditions dictated by diffusive transport (i.e., the sediment flux is proportional to the local bed slope through the fluvial diffusivity). To first order calculations, we assume the fluvial diffusivity to be half the water discharge per unit width (they both have the same units). More accurate expressions for the fluvial diffusivity can be found in Paola 2000 and Lorenzo-Trueba et al.2009. +
