Kinematic wave

Surface routing

The main flow routing scheme available in Wflow.jl is the kinematic wave approach for channel and overland flow, assuming that water flow is mostly controlled by topography. The kinematic wave equations are (Chow, 1988):

\[ \begin{gathered} \dfrac{\partial Q}{\partial x} + \dfrac{\partial A}{\partial t} = q,\\ A = \alpha Q^{\beta}. \end{gathered} \]

These equations can then be combined as a function of streamflow only:

\[ \dfrac{\partial Q}{\partial x} + \alpha \beta Q^{\beta - 1} \dfrac{\partial Q}{\partial t} = q. \]

Here $\SIb{Q}{m^3 s^{-1}}$ is the surface runoff in the kinematic wave, $\SIb{x}{m}$ is the length of the runoff pathway, $\SIb{A}{m}$ is the cross-section area of the runoff pathway, $\SIb{t}{s}$ is the integration timestep and $\alpha$ and $\beta$ are unitless coefficients.

These equations are solved with a nonlinear scheme using Newton’s method and can also be iterated depending on the model space and time resolution. By default, the iterations are performed until a stable solution is reached ($\epsilon < 10^{-12}$). For larger models, the number of iterations can also be fixed for to a specific sub-timestep (in seconds) for both overland and channel flows to improve simulation time. To enable (fixed or not) iterations of the kinematic wave the following lines can be inserted in the TOML file of the model:

[model]
# Enable iterations of the kinematic wave
kin_wave_iteration = true
# Fixed sub-timestep for iterations of channel flow (river cells)
kw_river_tstep = 900
# Fixed sub-timestep for iterations of overland flow (land cells)
kw_land_tstep = 3600

The $\alpha$ parameter of the kinematic wave is fixed. To estimate the wetted perimeter for the calculation of the $\alpha$ parameter a bankfull river depth map (default value is $\SI{1.0}{m}$) for the river can be provided as follows:

[input.lateral.river]
bankfull_depth = "wflow_riverdepth"

The wetted perimeter of the river is based on half bankfull river depth. For the land part the wetted perimeter is based on the flow width.

Simplified reservoir and lake models can be included as part of the river kinematic wave network.

Inflow

External water (supply/abstraction) inflow $\SIb{}{m^3 s^{-1}}$ can be added to the kinematic wave for surface water routing, as a cyclic parameter or as part of forcing (see also Input section).

Abstractions

Abstractions from the river through the variable abstraction $\SIb{}{m^3 s^{-1}}$ are possible when water demand and allocation is computed. The variable abstraction is set from the water demand and allocation module each time step. The abstraction is divided by the length of the runoff pathway and subtracted from the lateral inflow of the kinematic wave routing scheme for river flow.

Subsurface flow routing

In the SBM model the kinematic wave approach is used to route subsurface flow laterally. Different vertical hydraulic conductivity depth profiles are possible as part of the vertical SBM concept, and these profiles (after unit conversion) are also used to compute lateral subsurface flow. The following profiles (see SBM for a detailed description) are available: - exponential (default) - exponential_constant - layered - layered_exponential

For the profiles exponential and exponential_constant, the saturated store S is drained laterally by saturated downslope subsurface flow for a slope with width \SIb{w}{m} according to:

\[ Q = K_0\tan(\beta)w\begin{cases} \frac{1}{f}\left(e^{-fz_i}-e^{-f\subtext{z}{exp}}\right) + e^{-f\subtext{z}{exp}}(z_t-\subtext{z}{exp}) & \text{if $z_i < \subtext{z}{exp}$}\\ \\ e^{-f\subtext{z}{exp}}(z_t - z_i) & \text{if $z_i \ge \subtext{z}{exp}$}, \end{cases} \]

where $\beta$ is element slope angle, $\SIb{Q}{m^3 d^{-1}}$ is subsurface flow, $\SIb{K_0}{m d^{-1}}$ is the saturated hydraulic conductivity at the soil surface, $\SIb{z_i}{m}$ is the water table depth, $\SIb{z_{t}}{m}$ is the total soil depth, $\SIb{f}{m^{-1}}$ is a scaling parameter that controls the decrease of $K_0$ with depth and $\SIb{\subtext{z}{exp}}{m}$ is the depth from soil surface for which the exponential decline of $K_0$ is valid. For the exponential profile, $\subtext{z}{exp}$ is equal to $z_t$.

Combining with the following continuity equation: \[ (\theta_s-\theta_r)w\frac{\partial h}{\partial t} = -\frac{\partial Q}{\partial x} + wr \]

where $\SIb{h}{m}$ is the water table height, $\SIb{x}{m}$ is the distance downslope, and $\SIb{r}{m d^{-1}}$ is the net input rate to the saturated store. Substituting for $h (\frac{\partial Q}{\partial h})$, gives:

\[ \frac{\partial Q}{\partial t} = -c\frac{\partial Q}{\partial x} + cwr \]

where celerity $c$ is calculated as follows: \[ c = \frac{K_0 \tan(\beta)}{\theta_s-\theta_r}\begin{cases} e^{-fz_i} + e^{-f\subtext{z}{exp}} & \text{if $z_i < \subtext{z}{exp}$}\\ \\ e^{-f\subtext{z}{exp}} & \text{if $z_i \ge \subtext{z}{exp}$}. \end{cases} \]

For the layered and layered_exponential profiles the equivalent horizontal hydraulic conductivity $\SIb{K_h}{m d^{-1}}$ is calculated for water table height $\SIb{h = z_t-z_i}{m}$ and lateral subsurface flow is calculated as follows:

\[ Q = K_h h \tan(\beta) w, \]

and celerity $c$ is given by:

\[ c = \frac{K_h \tan(\beta)}{\theta_s-\theta_r}. \]

The kinematic wave equation for lateral subsurface flow is solved iteratively using Newton’s method.

Note

For the lateral subsurface flow kinematic wave the model timestep is not adjusted. For certain model timestep and model grid size combinations this may result in loss of accuracy.

Multi-Threading

The kinematic wave calculations for surface - and subsurface flow routing can be executed in parallel using multiple threads. In the model section of the TOML file, a minimum stream order can be provided to define subbasins for the river (default is 6) and land domain (default is 5). Subbasins are created at all confluences where each branch has a minimal stream order. Based on the subbasins a directed acyclic graph is created that controls the order of execution and which subbasins can run in parallel.

[model]
min_streamorder_river = 5 # minimum stream order to delineate subbasins for river domain, default is 6
min_streamorder_land = 4  # minimum stream order to delineate subbasins for land domain, default is 5

Subcatchment flow

Normally the the kinematic wave is continuous throughout the model. By using the pits entry in the model and input sections of the TOML file all flow is at the subcatchment only (upstream of the pit locations, defined by the netCDF variable wflow_pits in the example below) and no flow is transferred from one subcatchment to another. This can be convenient when connecting the result of the model to a water allocation model such as Ribasim.

[input]
# these are not directly part of the model
pits = "wflow_pits"

[model]
pits = true

Limitations

The kinematic wave approach for channel, overland and lateral subsurface flow, assumes that the topography controls water flow mostly. This assumption holds for steep terrain, but in less steep terrain the hydraulic gradient is likely not equal to the surface slope (subsurface flow), or pressure differences and inertial momentum cannot be neglected (channel and overland flow). In addition, while the kinematic wave equations are solved with a nonlinear scheme using Newton’s method (Chow, 1988), other model equations are solved through a simple explicit scheme. In summary the following limitations apply:

Channel flow, and to a lesser degree overland flow, may be unrealistic in terrain that is not steep, and where pressure forces and inertial momentum are important.
The lateral movement of subsurface flow may be very wrong in terrain that is not steep.

External inflows

External inflows, for example water supply or abstractions, can be added to the kinematic wave via the inflow variable. For this, the user can supply a 2D map of the inflow, as a cyclic parameter or as part of forcing (see also Input section). These inflows are added or abstracted from the upstream inflow qin before running the kinematic wave to solve the impact on resulting q. In case of a negative inflow (abstractions), a minimum of zero is applied to the upstream flow qin.

References

Chow, V., Maidment, D. and Mays, L., 1988, Applied Hydrology. McGraw-Hill Book Company, New York.