Digital Elevation Model based Hydrologic Modeling Topography and Physical runoff generation processes (TOPMODEL) Raster calculation of wetness index Raster.
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Presentation on theme: "Digital Elevation Model based Hydrologic Modeling Topography and Physical runoff generation processes (TOPMODEL) Raster calculation of wetness index Raster."— Presentation transcript:
Digital Elevation Model based Hydrologic Modeling Topography and Physical runoff generation processes (TOPMODEL) Raster calculation of wetness index Raster calculation of TOPMODEL runoff Extendability of ArcGIS using Visual Basic Programming Outline
Physical Processes involved in Runoff Generation From http://snobear.colorado.edu/IntroHydro/geog_hydro.html
Runoff generation processes Infiltration excess overland flow aka Horton overland flow Partial area infiltration excess overland flow Saturation excess overland flow P P P qrqr qsqs qoqo P P P qoqo f P P P qoqo f f
Map of saturated areas showing expansion during a single rainstorm. The solid black shows the saturated area at the beginning of the rain; the lightly shaded area is saturated by the end of the storm and is the area over which the water table had risen to the ground surface. [from Dunne and Leopold, 1978] Seasonal variation in pre-storm saturated area [from Dunne and Leopold, 1978]
Runoff generation at a point depends on Rainfall intensity or amount Antecedent conditions Soils and vegetation Depth to water table (topography) Time scale of interest These vary spatially which suggests a spatial geographic approach to runoff estimation
TOPMODEL Beven, K., R. Lamb, P. Quinn, R. Romanowicz and J. Freer, (1995), "TOPMODEL," Chapter 18 in Computer Models of Watershed Hydrology, Edited by V. P. Singh, Water Resources Publications, Highlands Ranch, Colorado, p.627-668. “TOPMODEL is not a hydrological modeling package. It is rather a set of conceptual tools that can be used to reproduce the hydrological behaviour of catchments in a distributed or semi- distributed way, in particular the dynamics of surface or subsurface contributing areas.”
TOPMODEL and GIS Surface saturation and soil moisture deficits based on topography –Slope –Specific Catchment Area –Topographic Convergence Partial contributing area concept Saturation from below (Dunne) runoff generation mechanism
Numerical Evaluation with the D Algorithm Upslope contributing area a Stream line Contour line Topographic Definition Specific catchment area a is the upslope area per unit contour length [m 2 /m m] Tarboton, D. G., (1997), "A New Method for the Determination of Flow Directions and Contributing Areas in Grid Digital Elevation Models," Water Resources Research, 33(2): 309-319.) (http://www.engineering.usu.edu/cee/faculty/dtarb/dinf.pdf)http://www.engineering.usu.edu/cee/faculty/dtarb/dinf.pdf
Hydrological processes within a catchment are complex, involving: Macropores Heterogeneity Fingering flow Local pockets of saturation The general tendency of water to flow downhill is however subject to macroscale conceptualization
TOPMODEL assumptions The dynamics of the saturated zone can be approximated by successive steady state representations. The hydraulic gradient of the saturated zone can be approximated by the local surface topographic slope, tan . The distribution of downslope transmissivity with depth is an exponential function of storage deficit or depth to the water table -T o is lateral transmissivity [m 2 /h] -S is local storage deficit [m] -z is local water table depth [m] (=S/n e ) -n e is effective porosity -m is a storage-discharge sensitivity parameter [m] -f =n e /m is an alternative storage-discharge sensitivity parameter [m -1 ]
Topmodel - Assumptions The soil profile at each point has a finite capacity to transport water laterally downslope. e.g. or S DwDw D
Topmodel - Assumptions The actual lateral discharge is proportional to specific catchment area. Specific catchment area a [m 2 /m m] (per unit contour length) S DwDw D R is –Proportionality constant –may be interpreted as “steady state” recharge rate, or “steady state” per unit area contribution to baseflow.
Relative wetness at a point and depth to water table is determined by comparing q act and q cap Specific catchment area a [m 2 /m m] (per unit coutour length) S DwDw D Saturation when w > 1. i.e. Topmodel - Assumptions
Topmodel Specific catchment area a [m 2 /m m] (per unit coutour length) S DwDw D z
Slope Specific Catchment Area Wetness Index ln(a/S) from Raster Calculator. Average, = 6.91
Numerical Example Given K o =10 m/hr f=5 m -1 Q b = 0.8 m 3 /s A (from GIS) n e = 0.2 Raster calculator -( [ln(sca/S)] - 6.90)/5+0.46 Compute R=0.0002 m/h =6.90 T=2 m 2 /hr
Calculating Runoff from 25 mm Rainstorm Flat area’s and z <= 0 –Area fraction (81 + 1246)/15893=8.3% –All rainfall ( 25 mm) is runoff 0 < z rainfall/effective porosity = 0.025/0.2 = 0.125 m –Area fraction 546/15893 = 3.4% –Runoff is P-z*0.2 –(1 / [Sat_during_rain ]) * (0.025 - (0.2 * [z])) –Mean runoff 0.0113 m =11.3 mm z > 0.125 m –Area fraction 14020/15893 = 88.2 % –All rainfall infiltrates Area Average runoff –11.3 * 0.025 + 25 * 0.083 = 2.47 mm –Volume = 0.00247 * 15893 * 30 * 30 = 35410 m 3
GIS estimation of hydrologic response function Amount of runoff generated Travel time to outlet Distance from each grid cell to outlet along flow path (write program to do this) Distance from each point on contributing area –overlay grid to outlet distances with contributing area.
Steps for distance to outlet program Read the outlet coordinates Read the DEM flow direction grid. This is a set of integer values 1 to 8 indicating flow direction Initialize a distance to outlet grid with a no data value Convert outlet to row and column references Start from the outlet point. Set the distance to 0. Examine each neighboring grid cell and if it drains to the current cell set its distance to the outlet as the distance from it to the current cell plus the distance from the current cell to the outlet.
1 2 3 1 2 3 Distances to outlet Programming the calculation of distance to the outlet 5 1 8 7 6 3 2 4 5 6 5 6 7 7 6 7 7 Direction encoding 42.4 72.4 0 30 72.4 102.4