Property:Describe time scale and resolution
From CSDMS
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1 year time steps, good results up to 200-300 years +
D
1. Sediment transport time through a catchment
2. Exhumation time from a depth of a thermochronometric closure isotherm to the surface +
A
I
S
A parameter called the CFL number controls the time step in relation to the spatial scales. For boussinesq simulations, a CFL number of 0.2 is usually sufficient for code stability. However, for the non-boussinesq simulations, I usually have to lower the CFL number to around 0.05. It's really just a bit of trial and error though. +
I
S
T
C
Averaging time is on the order of annual averages so that individual storm events are not represented. Problems usually are scaled for years, to decades all the way up to millenia. +
P
CFL condition +
S
R
Code has been most commonly run at 1 year time steps for up to 6000 years. Time steps are constrained by rates of evolution of topography due to episodic sediment transport events and peat accretion and how quickly those processes affect the flow field. In the situation for which the model was developed, sediment accumulates at a mean rate of 1 mm/yr. +
G
Constraints:
* Time step - 1 - 50 years
* Duration - Hundreds to thousands of years +
Currently does not time-evolve. I would like to couple this to a 3D viscoelastic mantle at some point, but this hasn't happened yet. +
M
Daily timestep. +
R
Daily timesteps +
H
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C
Data covers 1901 to 2100.
It is processed from the original data to comprise a monthly timescale. +
S
Days or greater. Component processes can have much higher resolutions for numerical stability. +
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D
R
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Designed for time scales over which topography changes appreciably, which might be years for badlands, up to thousands or millions of years for other landscapes. +
A
Developed as a stratigraphic model, approach is event-based. Intended time scale ranges from several decades to Holocene (10-10.000yrs). +
T
Each process can have its own timestep. Typical timesteps are:
*Channel flow (seconds)
*Infiltration (seconds to minutes)
*Snowmelt (hours to days)
*Subsurface flow (hours to days), etc.
Model can be run for a full year or longer, if necessary. +
C
B
T
For typical application in a natural river as a prediction tool, the recommended resolution is annual, although it can be as high as hours for simulation of a specific known event. +
G
GENESIS is a long-term shoreline evolution model and is best applied to estimate shoreline change over time periods of 1 year to 10's of years. +
M
Generally runs with very large time steps (1 year)
Cannot resolve intra-tidal processes (i.e., ebb-flood variability) +
N
R
C
U
C
I am running the model with dynamical time steps of 1800 seconds, but it only computes the radiative transfer every 200 timesteps. +
Internal time step years to decades
Model chron resolution 1000 years
Total run time 1-10 My +
A
Internal timestep is determined by ANUGA for numerical stability (in seconds). Output timestep is set by the user. Simulations are realistically limited to a few model hours. +
M
It is applied for 90 years. The time step is ~0.7 days. +
G
It is typically run for times no less than 25 years and no greater than 700 years. +
W
It simulate at daily time-steps. Maximum available datasets time-span is between 1901-present. +
R
Limited by computational resources. +
N
Limited by computational resources. +
L
Long-term water balance can be simulated (using a daily time step), as can individual flood events (using hourly time intervals, or even smaller). The output of a “water balance run” can be used to provide the initial conditions of a “flood run”. +
G
D
Mapview at a given time +
B
H
Minimal runtime: 1yr; up to > 10kyrs
Daily discharge is the smallest output timestep +
R
L
Model needs daily (or smaller) timesteps. +
C
Morphological time steps can be on the order of years
Time steps shorter than one tidal period are not realistic +
G
Most forcings are required at hourly scale. Integration time step is what required by numerical algorithms to converge (depends actually on processes) +
D
N
B
No assimilation means it works best for simulations shorter than ~6months unless boundary conditions are carefully tuned to avoid model drift. +
D
No time resolution constraints as this software performs topographic analysis. +
S
No time resolution constraints as this software performs topographic analysis. +
H
No time resolution constraints as this software performs topographic analysis. +
None +
M
None except elapsed time and memory limits. +
A
Not applicable - the model generates static channel planforms. +
M
G
N
Radar sweeps every approx. 15 minutes +
S
SBEACH is a short-term storm processes model and is intended for the estimation of beach profile response to storm events. Typical simulation durations are limited to hours to days (1 week maximum). +
P
Sediment and water discharge come from some physical parameters and the number of parcels chosen for each timestep. Set the number of parcels for both water and sediment to 1000s for improved resolution and speed. +
See 'Description of Input and Examples for PHREEQC Version 3 - A computer program for speciation, batch-reaction, one-dimensional transport, and inverse geochemical calculations'. +
W
See WRF-Hydro Technical Description https://ral.ucar.edu/projects/wrf_hydro/technical-description-user-guide +
C
See above. +
S
F
See:
Version 2.0: Cohen et al. (2019), The Floodwater Depth Estimation Tool (FwDET v2.0) for Improved Remote Sensing Analysis of Coastal Flooding. Natural Hazards and Earth System Sciences (NHESS)
Version 1.0: Cohen, S., G. R. Brakenridge, A. Kettner, B. Bates, J. Nelson, R. McDonald, Y. Huang, D. Munasinghe, and J. Zhang (2017), Estimating Floodwater Depths from Flood Inundation Maps and Topography. Journal of the American Water Resources Association (JAWRA):1–12. +
C
S
Simulated meander evolution timesteps are typically 0.1 year to a few years. If downstream sediment transport is modeled, subiterations of ~0.01 year are required. +
T
Simulations are run at daily time step
Total simulation duration is typically over 100's of years. +
R
C
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F
Temporal scale and resolution determined by user. Model adjusts process and output to the temporal increment chosen by user. +
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The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
The basic stability condition is: dt < (dx / u_min), where dt is the timestep, dx is the grid cell size and u_min is the smallest velocity in the grid. This ensures that flow cannot cross a grid cell in less than one time step. Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
S
The component has been tested on event to annual time scales, on a range of resolutions (1 m to 100 m) but would likely run efficiently on even longer time scales and finer resolutions). +
T
The flow should be run to be fully developed, and this time scale depends on the time scale of sediment settling time, and flow periods. the time step should be fine enough not to cause numerical instability, and also capture the varying the flow forcing. +
S
The model assumes continuous discharge; assuming flow intermittency of 0.01, the model can represent tens of thousands of years of surface evolution. +
W
The model can be run for a single storm (minutes to hours), and can also be run in continuous simulation mode for any number of years (1 - 100+). +
K
The model explicitly runs on an individual tidal cycle time step, which we scale up to 2 months. But, results most meaningful at timescales greater than a couple years. +
C
The model has simulated periods from 1 day to 9000 years.
The length of run is largely contingent on the number of grid cells, thus a balance between resoltion and area of study. A small catchment with a coarse resolution will run very fast. Increase the area or make grid cells smaller and run times will increase. +
W
The model is abstract. Time given in iterations, relating iterations to real time depends strongly on the climate of the area simulated. +
S
E
S
The model is typically driven by hourly wind data (speed and angle) and models coastal change over a period of 10 to 100 years. +
W
The model takes about 4-6 model years to reach equilibrium. The modeled time period is from the Archean Earth (3.8 - 2.5 Ga) +
O
The model works best for event to decadal time scales on a personal machine. +
C
The steady flow assumption used by most (not all) hydrology sub-models restricts time scale to periods significantly longer than a single storm. The model has been mostly used to address time scales relevant to significant topographic evolution, though in the case of rapidly changing landscapes (e.g., gully networks) this can be as short as decades. +
A
The time scale constraints usually comes from the input meteorological data: each time step must be provided with a set of input data. +
M
The time scale is of the order of 10-1000 years, since the migration of meandering rivers is usually very slow, (e.g. 1 meter/year). +
1
The time scale over which the simulation occurs is specified in zrp.m as an input parameter. Since the module is computationally lightweight, millions of time steps can be simulated quickly.
Translating between discrete steps of the particle model and continuous, real-world time may be inferred during the dimensionalization process. +
S
The typical time scale is on the order of 100 second, and the time step should satisfy the Courant number (<0.3) +
B
There is no conservation of mass on adjacent hillslopes, which presents a natural time limitation of ~10^6 years. +
L
There is no explicit time, every time step is a bankfull event. With the parameters published here, vertical incision rates correspond to rates on the order of cm/yr. +
I
O
This is a point model and not dependent on time scale or resolution. +
T
C
M
S
Time scale is essentially set by the Courant condition: practially by P-wave velocity or maxwell time according to the constitutive model being considered. However, the mass scaling technique allows significantly increased time steps values from the usual dynamic one. +
H
W
Time scale ranges to seconds (for example, dam break problems) to tens of years (for example real time simulations of large watersheds). +
S
Time scale will be set by discharge calculation method. The model is in general intended for annual to geological time scales, but shorter time scales may be used if Landlab dynamic flow routing components are employed. +
E
Time scale: Days to millions of years +
T
Time scales should be long compared to the time scales of short-term bed elevation changes, i.e. changes in instantaneous bed elevation associated with bedload transport and bedform migration (Blom et al., 2003, Wong et al., 2007). In other words, model results are averages over short-term bed elevation changes. For applications at field scales, the time resolution should be at least of one year because the model runs with formative conditions representative of mean annual values.
REFERENCES
Blom, A., Ribberink, J. S. & de Vriend, H. (2003). Vertical sorting in bed forms: Flume experiments with a natural and a trimodal sediment mixture. Water Resources Research, 39 (2), 1025.
Wong, M., Parker, G., DeVries, P., Brown, T. M. & Burges, S. J. (2007). Experiments on dispersion of tracer stones under lower-regime plane-bed equilibrium bedload transport. Water Resources Research, 45, W03440. +
G
Time step - 1 - 50 years
Duration - Hundreds to thousands of years +
H
Time step and simulation period are determined from the auxiliary data and meteorological forcing +
C
Time step is limited by Courant stability criteria (CFL < 1). Typical time step for open-ocean propagation: 15 s; near the coast: 0.5-5 s. Typical simulation time for geophysical tsunamis: few to 36 hours. +
G
Time step: 2-50 years (typically 10 years)
Duration: Centuries to millennia +
B
Time step: one year, with multiple storms occurring within each year
Duration: years to centuries +
Time step: one year, with multiple storms occurring within each year
Duration: years to millennia +
G
Time steps are limited by CFL condition based on depth of fluid. Finer grids can automatically refine to use finer resolution in time than the underlying coarse grids. +
W
Time steps from seconds to 1h. Time length of runs can be up to years. +
Q
Time steps of 10 – 1000 years depending on output range. Total range up to Millions of years. +
G
Time to create the model domain increases with the number of intersections between segments, catchment sub-basins, and the MODFLOW grid. +
C
Timestepping is usually annual, extending over 1000 years. However the model is capable of doing finer and longer runs. +
B
Timesteps in the range of 1-10 years are generally stable, can run for as long as desired until the memory runs out. +
C
Topographic analysis so no time scale constraints. +
S
Total time scale is merely dependant on computing time, typically on the order of several thousands to 100,000 years. Time steps are restricted to 1 year. +
E
B
Typical time scale of order tens to hundreds of thousands of years. +
I
T
Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
Typical timesteps are on the order of seconds to minutes. Model can be run for a full year or longer, if necessary. +
D
Typically millions of years to tens of millions of year +
M
F
Wave-current BL: timescale ~10 min; time step ~0.01 sec; Tidal BL: timescale days and time step 10 s +
E
We present an equilibrium solution that may or may not be reached. The fundamental assumption is that in the absence of subsidence, uplift and change of downstream water surface base level, an alluvial river will evolve toward an equilibrium state in which overbank and bar deposition (floodplain construction) are perfectly balanced by the removal of floodplain sediment due to channel migration (floodplain shaving) (Lauer & Parker, 2006). This equilibrium state can be reached if hydrologic regime, sediment supply and caliber do not vary in time.
Reference
Lauer, J. W. & Parker, G. (2006). Net local removal of floodplain sediment by river meander migration, Geomorphology 96, 123-149. +
Q
We use the ‘basin equilibrium timescale’ (Paola 2000), defined as the length scale square divided by the fluvial diffusivity. In field settings, this time scale can range from centennial to millennia up to millions of years. +
M
Yearly time steps are appropriate +
C
G
C
Years to millenia. Typically, the model is run with timesteps on the order of a day. However, the assumptions that the shoreface progrades or erodes while maintaining its cross-shore shape prevents model results from being interpreted as meaningful over time scales shorter than years to decades. (Storm and post storm cross-shore shifting of sediment within the shoreface causes shoreline fluctuations on event timescales that are implicitly averaged out in this model.) +
W
C
days- years +
M
default settings represent a 3 hour time step for larger scale dynamics, and 1 hour time step for water volume flux subdivided into smaller iterations based on localized grid cell parameters (can get as small as ~12 minutes for some cells) +
Z
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I
G
D
F
mean annual conditions +
D
M
D
n/a +
C
T
none +
B
none +
sea-level rise timescales (decades to millennia). Parameterizations not suitable for short-timescale analyses +
G
T
see the discussion of limitations in Beven et al., 1995 and Beven, 1997.
Variable, from 1 to 24 hours +
B
D
C
time scale: decades
resolution constraints: day +
F
W
typically 30-minute time steps +
X
K
yearly +
O
