Note: This document is for an older version of GRASS GIS that will be discontinued soon. You should upgrade, and read the current manual page.

**-t**- Time-series output
**--overwrite**- Allow output files to overwrite existing files
**--help**- Print usage summary
**--verbose**- Verbose module output
**--quiet**- Quiet module output
**--ui**- Force launching GUI dialog

**elevation**=*name***[required]**- Name of input elevation raster map
**dx**=*name***[required]**- Name of x-derivatives raster map [m/m]
**dy**=*name***[required]**- Name of y-derivatives raster map [m/m]
**rain**=*name*- Name of rainfall excess rate (rain-infilt) raster map [mm/hr]
**rain_value**=*float*- Rainfall excess rate unique value [mm/hr]
- Default:
*50* **infil**=*name*- Name of runoff infiltration rate raster map [mm/hr]
**infil_value**=*float*- Runoff infiltration rate unique value [mm/hr]
- Default:
*0.0* **man**=*name*- Name of Manning's n raster map
**man_value**=*float*- Manning's n unique value
- Default:
*0.1* **flow_control**=*name*- Name of flow controls raster map (permeability ratio 0-1)
**observation**=*name*- Name of sampling locations vector points map
- Or data source for direct OGR access
**depth**=*name*- Name for output water depth raster map [m]
**discharge**=*name*- Name for output water discharge raster map [m3/s]
**error**=*name*- Name for output simulation error raster map [m]
**walkers_output**=*name*- Base name of the output walkers vector points map
- Name for output vector map
**logfile**=*name*- Name for sampling points output text file. For each observation vector point the time series of sediment transport is stored.
**nwalkers**=*integer*- Number of walkers, default is twice the number of cells
**niterations**=*integer*- Time used for iterations [minutes]
- Default:
*10* **output_step**=*integer*- Time interval for creating output maps [minutes]
- Default:
*2* **diffusion_coeff**=*float*- Water diffusion constant
- Default:
*0.8* **hmax**=*float*- Threshold water depth [m]
- Diffusion increases after this water depth is reached
- Default:
*0.3* **halpha**=*float*- Diffusion increase constant
- Default:
*4.0* **hbeta**=*float*- Weighting factor for water flow velocity vector
- Default:
*0.5* **threads**=*integer*- Number of threads which will be used for parallel compute
- Default:
*4*

The module automatically converts horizontal distances from feet to metric system using
database/projection information. Rainfall excess is defined as rainfall intensity
- infiltration rate and should be provided in [mm/hr].
Rainfall intensities are usually available from meteorological stations.
Infiltration rate depends on soil properties and land cover. It varies in space and time.
For saturated soil and steady-state water flow it can be estimated using
saturated hydraulic conductivity rates based on field measurements or using
reference values which can be found in literature.
Optionally, user can provide an overland flow infiltration rate map
*infil* or a single value *infil_value* in [mm/hr] that control the rate of
infiltration for the already flowing water, effectively reducing the flow depth and
discharge.
Overland flow can be further controlled by permeable check dams or similar type of structures,
the user can provide a map of these structures and their permeability ratio
in the map *flow_control* that defines the probability of particles to pass
through the structure (the values will be 0-1).

Output includes a water depth raster map *depth* in [m], and a water discharge
raster map *discharge* in [m3/s]. Error of the numerical solution can be analyzed using
the *error* raster map (the resulting water depth is an average, and err is its RMSE).
The output vector points map *output_walkers* can be used to analyze and visualize
spatial distribution of walkers at different simulation times (note that
the resulting water depth is based on the density of these walkers).
The spatial distribution of numerical error associated with path sampling solution can be
analysed using the output error raster file [m]. This error is a function of the number
of particles used in the simulation and can be reduced by increasing the number of walkers
given by parameter *nwalkers*.
Duration of simulation is controlled by the *niterations* parameter. The default value
is 10 minutes, reaching the steady-state may require much longer time,
depending on the time step, complexity of terrain, land cover and size of the area.
Output walker, water depth and discharge maps can be saved during simulation using
the time series flag *-t* and *output_step* parameter
defining the time step in minutes for writing output files.
Files are saved with a suffix representing time since the start of simulation in minutes
(e.g. wdepth.05, wdepth.10).
Monitoring of water depth at specific points is supported. A vector map with observation points and
a path to a logfile must be provided. For each point in the vector map which is located in
the computational region the water depth is logged each time step in the logfile. The logfile is
organized as a table. A single header identifies the category number of the logged vector points.
In case of invalid water depth data the value -1 is used.

Overland flow is routed based on partial derivatives of elevation
field or other landscape features influencing water flow. Simulation
equations include a diffusion term (*diffusion_coeff* parameter) which enables
water flow to overcome elevation depressions or obstacles when water depth exceeds
a threshold water depth value (*hmax)*, given in [m]. When it is reached,
diffusion term increases as given by *halpha* and advection term
(direction of flow) is given as "prevailing" direction of flow computed
as average of flow directions from the previous *hbeta* number of grid cells.

**Green's function stochastic method of solution.**

The Saint Venant equations are solved by a stochastic method called Monte Carlo
(very similar to Monte Carlo methods in computational fluid dynamics or to
quantum Monte Carlo approaches for solving the Schrodinger equation (Schmidt
and Ceperley, 1992, Hammond et al., 1994; Mitas, 1996)). It is assumed
that these equations are a representation of stochastic processes with
diffusion and drift components (Fokker-Planck equations).

The Monte Carlo technique has several unique advantages which are becoming even more important due to new developments in computer technology. Perhaps one of the most significant Monte Carlo properties is robustness which enables us to solve the equations for complex cases, such as discontinuities in the coefficients of differential operators (in our case, abrupt slope or cover changes, etc). Also, rough solutions can be estimated rather quickly, which allows us to carry out preliminary quantitative studies or to rapidly extract qualitative trends by parameter scans. In addition, the stochastic methods are tailored to the new generation of computers as they provide scalability from a single workstation to large parallel machines due to the independence of sampling points. Therefore, the methods are useful both for everyday exploratory work using a desktop computer and for large, cutting-edge applications using high performance computing.

g.region raster=elevation.10m -p r.slope.aspect elevation=elevation.10m dx=elev_dx dy=elev_dy # synthetic maps r.mapcalc "rain = if(elevation.10m, 5.0, null())" r.mapcalc "manning = if(elevation.10m, 0.05, null())" r.mapcalc "infilt = if(elevation.10m, 0.0, null())" # simulate r.sim.water elevation=elevation.10m dx=elev_dx dy=elev_dy \ rain=rain man=manning infil=infilt \ nwalkers=5000000 depth=depth

ERROR: nwalk (7000001) > maxw (7000000)!

North Carolina State University

Jaroslav Hofierka

GeoModel, s.r.o. Bratislava, Slovakia

*hofierka@geomodel.sk*

Chris Thaxton

North Carolina State University

*csthaxto@unity.ncsu.edu*

- Mitasova, H., Thaxton, C., Hofierka, J., McLaughlin, R., Moore, A., Mitas L., 2004, Path sampling method for modeling overland water flow, sediment transport and short term terrain evolution in Open Source GIS. In: C.T. Miller, M.W. Farthing, V.G. Gray, G.F. Pinder eds., Proceedings of the XVth International Conference on Computational Methods in Water Resources (CMWR XV), June 13-17 2004, Chapel Hill, NC, USA, Elsevier, pp. 1479-1490.
- Mitasova H, Mitas, L., 2000, Modeling spatial processes in multiscale framework: exploring duality between particles and fields, plenary talk at GIScience2000 conference, Savannah, GA.
- Mitas, L., and Mitasova, H., 1998, Distributed soil erosion simulation for effective erosion prevention. Water Resources Research, 34(3), 505-516.
- Mitasova, H., Mitas, L., 2001, Multiscale soil erosion simulations for land use management, In: Landscape erosion and landscape evolution modeling, Harmon R. and Doe W. eds., Kluwer Academic/Plenum Publishers, pp. 321-347.
- Hofierka, J, Mitasova, H., Mitas, L., 2002. GRASS and modeling landscape processes using duality between particles and fields. Proceedings of the Open source GIS - GRASS users conference 2002 - Trento, Italy, 11-13 September 2002. PDF
- Hofierka, J., Knutova, M., 2015, Simulating aspects of a flash flood using the Monte Carlo method and GRASS GIS: a case study of the MalĂˇ Svinka Basin (Slovakia), Open Geosciences. Volume 7, Issue 1, ISSN (Online) 2391-5447, DOI: 10.1515/geo-2015-0013, April 2015
- Neteler, M. and Mitasova, H., 2008, Open Source GIS: A GRASS GIS Approach. Third Edition. The International Series in Engineering and Computer Science: Volume 773. Springer New York Inc, p. 406.

Available at: r.sim.water.mp source code (history)

Latest change: Monday Jun 03 21:35:37 2024 in commit: dcdac0d0eea604c982fe76531804a55ff1bb4322

Note: This document is for an older version of GRASS GIS that will be discontinued soon. You should upgrade, and read the current manual page.

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