InVEST 3.9.0.post249+invest.gf12cf86d documentation

Seasonal water yield

Summary

There is a high demand for tools estimating the effect of landscape management on the water supply service, for uses like irrigation, domestic consumption and hydropower production. While the InVEST Annual Water Yield model provides an estimate of total water yield for a catchment, many applications require knowledge of seasonal flows, especially during the dry season. This requires the understanding of hydrological processes in a catchment, in particular the partitioning between quick flow (occurring during or shortly after rain events) and baseflow (occurring during dry weather). In highly seasonal climates, baseflow is likely to provide greater value than quick flow, unless significant storage (e.g., a large reservoir) is available. The InVEST Seasonal Water Yield model seeks to provide guidance regarding the contribution of land parcels to the generation of both baseflow and quick flow. The model computes spatial indices that quantify the relative contribution of a parcel of land to the generation of both baseflow and quick flow. Currently, there are no quantitative estimates of baseflow, only the relative contributions of pixels; a separate tool is in development to address this question.

Introduction

Understanding the effect of landscape management on seasonal flow is of critical importance for watershed management. The contribution of a given parcel to streamflow depends on a number of environmental factors including climate, soil, vegetation, slope, and position along the flow path (determining if the pixel may receive water from upslope or if water recharged may later be evapotranspired).

Water flowing across the landscape is either evaporated, transpired, withdrawn by a well, or leaves the watershed as deep groundwater flow or streamflow. If we consider an individual pixel, and its value with respect to water yield, we can consider two approaches:

  • The first gives credit to the net amount of water generated on a pixel as equal to the incoming precipitation minus the losses to evapotranspiration on that pixel. In this scheme, it is possible for actual evapotranspiration to be greater than precipitation if water is supplied to the site from upslope. Thus, the net generation could be negative. This approach pays no heed to the eventual disposition of that water generated on that pixel; that is, it does not consider whether the water actually shows up as streamflow or is evaporated or withdrawn somewhere along its path.

  • The second approach gives credit to the water from a parcel that actually shows up as streamflow. Thus, if a parcel generates water that is later evaporated, the contribution is considered to be nil.

The former approach puts greater emphasis on the land-use and land-cover of a site, since the focus is on net generation from that pixel. It accounts for the subsidy of water from upslope pixels, but does not consider downslope effects. It represents the potential to generate streamflow (not an actual generation of flow).

The second approach puts more emphasis on the topographic position of a pixel, as that will determine the potential for water generated on that pixel to be consumed before becoming streamflow. It represents the actual streamflow generated by a pixel. Since actual streamflow cannot be less than zero, this approach, unlike the first, will result in indices that are greater than or equal to zero.

We use both of these concepts to develop a set of three indices, one for quickflow, one for recharge (which represents the ‘potential baseflow’), and one for actual baseflow. Here, baseflow is defined as the generation of streamflow with watershed residence times of months to years, while quick flow represents the generation of streamflow with watershed residence times of hours to days.

The Model

Quickflow

Quickflow (QF) is calculated with a Curve Number (CN)-based approach. Monthly rain events cause precipitation to fall on the landscape. Soil and land cover properties determine how much of the rain runs off of the land surface quickly (producing quickflow) versus infiltrating into the soil (producing local recharge.) The curve number is a simple way of capturing these soil + land cover properties - higher values of CN have higher runoff potential (for example, clay soils and low vegetation cover), lower values are more likely to infiltrate (for example, sandy soils and dense vegetation cover.)

To calculate quickflow, we use the mean event depth, \(\frac{P_{i,m}}{n_{i,m}}\) and assume an exponential distribution of daily precipitation depths on days with rain,

\[f\left( p \right) = \frac{1}{a_{i,m}}exp\left( - \frac{p}{a_{i,m}} \right)\]

Where \(a_{i,m} = \frac{P_{i,m}}{n_{m}}/25.4\) and

  • \(a_{i,m}\) is the mean rain depth on a rainy day at pixel i on month m [in],

  • \(n_{i,m}\) is the number of events at pixel i in month m [-],

  • \(P_{i,m}\) is the monthly precipitation for pixel i at month m [mm].

Quickflow for pixels located in streams is set to the precipitation on that pixel, which assumes no infiltration, only runoff.

\[\text{QF}_{stream,m} = \ P_{stream,m}\]

otherwise it can be shown from the exponential distribution that the monthly runoff \(\text{QF}_{i,m}\) is

(1)\[\text{QF}_{i,m} = n_{m} \times \left( \left( a_{i,m} - S_{i} \right)\exp\left( - \frac{0.2S_{i}}{a_{i,m}} \right) + \frac{S_{i}^{2}}{a_{i,m}}\exp\left( \frac{0.8S_{i}}{a_{i,m}} \right)E_{1}\left( \frac{S_{i}}{a_{i,m}} \right) \right) \times \left( 25.4\ \left\lbrack \frac{\text{mm}}{\text{in}} \right\rbrack \right)\]

where

  • \(S_{i} = \frac{1000}{\text{CN}_{i}} - 10\) [in]

  • \(\text{CN}_{i}\) is the curve number for pixel i [in-1], tabulated as a function of the local LULC, and soil type (see Appendix I for a template of this table),

  • \(E_{1}\) is the exponential integral function, \(E_{1}(x) = \int_{1}^{\infty}{\frac{e^{-xt}}{t}\text{dt}}\).

  • and \(25.4\) is a conversion factor from inches (used by the equation) to millimeters (used by the model)

Thus the annual quick flow \(\text{QF}_{i}\), can be calculated from the sum of monthly \(\text{QF}_{i,m}\) values,

(2)\[\text{QF}_{i} = \sum_{m = 1}^{12}{QF_{i,m}}\]

Local recharge

The local recharge, or potential contribution to baseflow, of a pixel is computed from the local water balance. Precipitation that does not run off as quickflow, and is not evapotranspired by the vegetation on a pixel, can infiltrate the soil to become local recharge. Local recharge can be negative if a pixel does not receive enough of its own water to satisfy its vegetation requirements (determined by its crop factor Kc), so it uses water generated upslope of the pixel as well (referred to as an “upslope subsidy”.) The local recharge index is computed on an annual time scale, but uses values derived from monthly water budgets.

For a pixel i, the local recharge derived from the annual water budget is (Figure 1):

(3)\[L_{i} = P_{i} - \text{QF}_{i} - \text{AET}_{i}\]

Where annual actual evapotranspiration AET is the sum of monthly AET:

(4)\[\text{AET}_{i} = \sum_{\text{months}}^{}\text{AET}_{i,m}\]

For each month, \(\text{AET}_{i,m}\) is either limited by the demand (potential evapotranspiration - PET) or by the available water (from Allen et al. 1998):

(5)\[\text{AET}_{i,m} = min(\text{PET}_{i,m}\ ;\ P_{i,m} - \text{QF}_{i,m} + \alpha_{m}\beta_{i}L_{sum.avail,i})\]

Where \(\text{PET}_{i,m}\) is the monthly potential evapotranspiration,

(6)\[\text{PET}_{i,m} = K_{c,i,m} \times ET_{0,i,m}\]

\(L_{sum.avail,i}\) is recursively defined by (Figure 2),

(7)\[L_{sum.avail,i} = \sum_{j \in \{ neighbor\ pixels\ draining\ to\ pixel\ i\}}^{}{p_{\text{ij}} \cdot \left( L_{avail,j} + L_{sum.avail,j} \right)}\]

where \(p_{\text{ij}}\ \in \lbrack 0,1\rbrack\) is the proportion of flow from cell i to j, and \(L_{avail,i}\) is the available recharge to a pixel, which is \(L_{i}\) whenever \(L_{i}\) is negative, and a proportion \(\gamma\) of \(L_{i}\) when it is positive (see below for definition of \(\gamma\)):

(8)\[L_{avail,i}\ = min(\gamma L_{i},L_{i})\]

In the above:

  • \(P_{i}\) and \(P_{i,m}\) are the annual and monthly precipitation, respectively [mm]

  • \(\text{QF}_{i}\) and \(\text{QF}_{i,m}\) are the quickflow indices, defined above [mm]

  • \(ET_{0,i,m}\) is the reference evapotranspiration for month m [mm]

  • \(K_{c,i,m}\) is the monthly crop factor for the pixel’s LULC

  • \(\alpha_{m}\) is the fraction of upslope annual available recharge that is available in month m (default is 1/12)

  • \(\beta_{i}\) is the fraction of the upslope subsidy that is available for downslope evapotranspiration (default is 1; see Appendix II for more information)

  • γ is the fraction of pixel recharge that is available to downslope pixels (default is 1)

Attribution of recharge

The total baseflow, \(Q_b\) (in mm), is the average of the contributing local recharges (negative or positive) in the catchment,

(9)\[Q_{b} = \frac{\sum_{k \in \left\{ \text{pixels in catchment} \right\}}^{}L_{k}}{n_{\text{pixels in catchment}}}\]

Attribution value to a pixel is the relative contribution of local recharge \(L\) on that pixel to the baseflow \(Q_b\):

(10)\[V_{R,i} = \frac{L_{i}}{{Q_{b} \times n}_{\text{pixels in catchment}}}\]

_images/fig1.png

Figure 1. Water balance at the pixel scale to compute the local recharge (Eq. 3).




_images/fig2.png

Figure 2. Routing at the hillslope scale to compute actual evapotranspiration (based on each pixel’s climate variables and the upslope contribution, see Eq. 5) and baseflow (based on Bsum, the flow actually reaching the stream, see Eq. 11-14)



Baseflow

The baseflow index represents the actual contribution of a pixel to baseflow (i.e. water that reaches the stream). If the local recharge is negative, then the pixel did not contribute to baseflow so \(B\) is set to zero. If the pixel contributed to groundwater recharge, then \(B\) is a function of the amount of flow leaving the pixel and of the relative contribution to recharge of this pixel.

For a pixel that is not adjacent to the stream channel, the cumulative baseflow, \(B_{sum,i}\), is proportional to the cumulative baseflow leaving the adjacent downslope pixels minus the cumulative baseflow that was generated on that same downslope pixel (Figure 2):

(11)\[\begin{split}B_{sum,i} = L_{sum,i}\sum_{j \in \{\text{cells to which cell i pours}\}}^{}\begin{Bmatrix} p_{\text{ij}}\left( 1 - \frac{L_{avail,j}}{L_{sum,j}} \right)\frac{B_{sum,j}}{L_{sum,j} - L_{j}}\ \text{ if }j\text{ is a nonstream pixel} \\ p_{\text{ij}}\ \text{ if }j\text{ is a stream pixel} \\ \end{Bmatrix}\end{split}\]

At the watershed outlet (or at any pixel adjacent to the stream), the sum of baseflow generation \(B_{sum,i}\) over all upslope pixels is equal to the sum of local generation over the same pixels (because there is no further opportunity for the slow flow to be consumed before reaching the stream):

(12)\[B_{sum,outlet} = L_{sum,outlet}\]

where \(L_{sum,i}\) is the cumulative upstream recharge defined by

(13)\[L_{sum,i} = L_{i} + \sum_{j,\ all\ pixels\ draining\ to\ pixel\ i}^{}{L_{sum,j} \cdot p_{\text{ji}}}\]

and the baseflow, \(B_{i}\) can be directly derived from the proportion of the cumulative baseflow leaving cell i, with respect to the available recharge to the upstream cumulative recharge:

(14)\[B_{i} = max\left(B_{sum,i} \cdot \frac{L_{i}}{L_{sum,i}}, 0\right)\]

Limitations

Like all InVEST models, Seasonal Water Yield uses a simplified approach to estimating quickflow and baseflow, and does not include many of the complexities that occur as water moves through a landscape. Quickflow is primarily based on curve number, which does not take topography into account. For baseflow, although the model uses a physics-based approach, the equations are extremely simplified at both spatial and temporal scales, which significantly increases the uncertainty on the absolute numbers produced. So we do not suggest to use the absolute values, but instead the relative values across the landscapes (where we assume that the simplifications matter less, because they apply to the entire landscape).

Of course, this makes it harder to validate against observed results, which is always recommended. One possibility is to validate the relative values (i.e. the distribution of values across the landscape). This requires several (at least >3, more realistically >5) stream gauges, which can be compared with the baseflow generation output of the model. Alternatively, results may be compared to a different spatially-explicit model, if it is available.

Data needs

This section outlines the specific data used by the model. See the Appendix for additional information on data sources and pre-processing. Please consult the InVEST sample data (located in the folder where InVEST is installed, if you also chose to install sample data) for examples of all of these data inputs. This will help with file type, folder structure and table formatting. Note that all GIS inputs must be in the same projected coordinate system and in linear meter units.

  • Workspace (required). Folder where model outputs will be written. Make sure that there is ample disk space, and write permissions are correct.

  • Suffix (optional). Text string that will be appended to the end of output file names, as “_Suffix”. Use a Suffix to differentiate model runs, for example by providing a short name for each scenario. If a Suffix is not provided, or changed between model runs, the tool will overwrite previous results.

  • Precipitation Directory (required). Folder containing 12 rasters of monthly precipitation for each pixel. Raster file names must end with the month number (e.g. Precip_1.tif for January.) Only .tif files should be in this folder (no .tfw, .xml, etc files). [units: millimeters]

  • ET0 directory (required). Folder containing 12 rasters of monthly reference evapotranspiration for each pixel. Raster file names must end with the month number (e.g. ET0_1.tif for January.) Only .tif files should be in this folder (no .tfw, .xml, etc files). [units: millimeters]

  • Digital Elevation Model (required). Raster of elevation for each pixel. Floating point or integer values. [units: meters]

  • Land use/land cover (required). Raster of land use/land cover (LULC) for each pixel, where each unique integer represents a different land use/land cover class. All values in this raster MUST have corresponding entries in the Biophysical table.

  • Soil group (required). Raster of SCS soil hydrologic groups (A, B, C, or D), used in combination with the LULC map to compute the curve number (CN) raster. This is a raster of integers where values are entered as numbers 1, 2, 3, and 4, corresponding to soil groups A, B, C, and D, respectively.

  • AOI/Watershed (required). Shapefile delineating the boundary of the watershed to be modeled. Results will be aggregated within each polygon defined. The column ws_id is required, containing a unique integer value for each polygon.

  • Biophysical table (required). A .csv (Comma Separated Value) table containing model information corresponding to each of the land use classes in the LULC raster. All LULC classes in the LULC raster MUST have corresponding values in this table. Each row is a land use/land cover class and columns must be named and defined as follows:

    • lucode (required). Unique integer for each LULC class (e.g., 1 for forest, 3 for grassland, etc.) Every value in the LULC map MUST have a corresponding lucode value in the biophysical table.

    • CN_A, CN_B, CN_C, CN_D (required). Integer curve number (CN) values for each combination of soil type and lucode class. No 0s (zeroes) are allowed.

    • Kc_1, Kc_2… Kc_11, Kc_12 (required). Floating point monthly crop/vegetation coefficient (Kc) values for each lucode. Kc_1 corresponds to January, Kc_2 February, etc.

  • Rain events table (either this or a Climate Zone table is required). CSV (comma-separated value, .csv) table with 12 values of rain events, one per month. A rain event is defined as >0.1mm. The following fields are required:

    • month (required). Values are the integer numbers 1 through 12, corresponding to January (1) through December (12)

    • events (required). The number of rain events for that month, which are floating point or integer values

  • Threshold flow accumulation (required). The number of upstream cells that must flow into a cell before it is considered part of a stream, which is used to create streams from the DEM. Smaller values create more tributaries, larger values create fewer. Integer value. See Appendix 1 for more information on choosing this value. Integer value, with no commas or periods - for example “1000”.

  • alpha_m, beta_i, gamma (required). Model parameters used for research and calibration purposes. Default values are: alpha_m = 1/12, beta_i = 1, gamma = 1. alpha_m is type string; beta_i and gamma are type floating point.

Advanced model options

One model input is the number of rain events per month, which is entered as a .csv table with one number for each month of the year. This assumes that there is one such number for the whole watershed, which may not be true for large areas or areas with very spatially variable precipitation.

To represent variability in the number of rain events, it is possible to enter a map of climate zones, and associated number of rain events for each zone.

Inputs

  • Climate zone table (either this or a Rain Events table is required). CSV (comma-separated value, .csv) table with the number of rain events per month and climate zone, with the following required fields:

    • cz_id. Climate zone numbers, integers which correspond to values found in the Climate zone raster

    • jan feb mar apr may jun jul aug sep oct nov dec. 12 fields corresponding to each month of the year. These contain the number of rain events that occur in that month in that climate zone. Floating point.

  • Climate zone. Raster of climate zones, each uniquely identified by an integer (i.e. all pixels that are part of one climate zone should have the same integer value.) Must match cz_id values in the Climate zone table.


The model computes sequentially the local recharge layer, and then the baseflow layer from local recharge. Instead of InVEST calculating local recharge, this layer could be obtained from a different model (e.g, RHESSys.) To compute baseflow contribution based on your own recharge layer, it is possible to bypass the first part of the model and directly enter a map of local recharge.

Inputs

  • Local recharge. Raster with the local recharge obtained from a different model (in mm). Floating point values.


The alpha parameter represents the temporal variability in the contribution of upslope available water to evapotranspiration on a pixel. In the default parameterization, its value is set to 1/12, assuming that the soil buffers water release and that the monthly contribution is exactly 1\12th of the annual contribution.

To allow upslope subsidy to be temporally variable instead, the user can enter monthly alpha values, in the same table as the rain events table.

Inputs

  • Rain events table. The rain events table is a CSV (comma-separated value, .csv) model input (see above). Along with the required month field, one additional column named alpha is required to run this advanced option. Values for alpha are floating point.

Running the model

To launch the Seasonal Water Yield model navigate to the Windows Start Menu -> All Programs -> InVEST [version] -> Seasonal Water Yield. The interface does not require a GIS desktop, although the results will need to be explored with any GIS tool such as ArcGIS or QGIS.

Interpreting outputs

The following is a short description of each of the outputs from the Seasonal Water Yield model. Final results are found within the user defined Workspace specified for this model run. “Suffix” in the following file names refers to the optional user-defined Suffix input to the model.

The resolution of the output rasters will be the same as the resolution of the DEM that is provided as input.

  • [Workspace] folder:

  • Parameter log: Each time the model is run, a text (.txt) file will be created in the Workspace. The file will list the parameter values and output messages for that run and will be named according to the service, the date and time. When contacting NatCap about errors in a model run, please include the parameter log.

  • B_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of baseflow \(B\) values, the contribution of a pixel to slow release flow (which is not evapotranspired before it reaches the stream)

  • B_sum_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of \(B_{\text{sum}}\)values, the flow through a pixel, contributed by all upslope pixels, that is not evapotranspirated before it reaches the stream

  • CN_[Suffix].tif (type: raster): Map of curve number values

  • L_avail_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of available local recharge \(L_{\text{avail}}\)

  • L_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of local recharge \(L\) values

  • L_sum_avail_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of \(L_{\text{sum.avail}}\) values, the available water to a pixel, contributed by all upslope pixels, that is available for evapotranspiration by this pixel

  • L_sum_[Suffix].tif (type: raster; units: mm, but should be interpreted as relative values, not absolute): Map of \(L_{\text{sum}}\) values, the flow through a pixel, contributed by all upslope pixels, that is available for evapotranspiration to downslope pixels

  • QF_[Suffix].tif (type: raster; units: mm): Map of quickflow (QF) values

  • Vri_[Suffix].tif (type: raster; units: mm): Map of the values of recharge (contribution, positive or negative), to the total recharge

  • aggregated_results_swy_[Suffix].shp: Table containing biophysical values for each watershed, with fields as follows:

    • qb (units: mm, but should be interpreted as relative values, not absolute): Mean local recharge value within the watershed

  • [Workspace]\intermediate_outputs folder:

  • aet_[Suffix].tif (type: raster; units: mm): Map of actual evapotranspiration (AET)

  • qf_1_[Suffix].tif…qf_12_[Suffix].tif (type: raster; units: mm): Maps of monthly quickflow (1 = January… 12 = December)

  • stream_[Suffix].tif (type: raster): Stream network generated from the input DEM and Threshold Flow Accumulation. Values of 1 represent streams, values of 0 are non-stream pixels.

Appendix 1: Data sources and guidance for parameter selection

This is a rough compilation of data sources and suggestions about finding, compiling, and formatting data, providing links to global datasets that can get you started. It is highly recommended to look for more local and accurate data (from national, state, university, literature, NGO and other sources) and only use global data for final analyses if nothing more local is available.

Monthly precipitation

Global monthly precipitation data can be obtained from the WorldClim dataset: http://www.worldclim.org/ or Climatic Research Unit: http://www.cru.uea.ac.uk.

Alternatively, rasters can be interpolated from rain gauge points with long-term monthly data. When considering rain gage data, make sure that they provide good coverage over the area of interest, especially if there are large changes in elevation that cause precipitation amounts to be heterogeneous within the study area. Ideally, the gauges will have at least 10 years of continuous data, with no large gaps, around the same time period as the land use/land cover map used.

Monthly reference evapotranspiration

Reference evapotranspiration, \(ET_0\), is the energy (expressed as a depth of water, e.g. mm) supplied by the sun (and occasionally wind) to vaporize water. Reference evapotranspiration varies with elevation, latitude, humidity, and slope aspect. There are many methodologies, which range in data requirements and precision.

Global monthly reference evapotranspiration may be obtained from the CGIAR CSI dataset (based on WorldClim data): http://www.cgiar-csi.org/data/global-aridity-and-pet-database.

It is important that the precipitation data used for calculating reference evapotranspiration is the same as the precipitation data used as input to the model.

You can calculate reference ET by developing monthly average grids of precipitation, and maximum and minimum temperatures (also available from WorldClim and CRU) which need to incorporate the effects of elevation when interpolating from observation stations. Data to develop these monthly precipitation and temperature grids follow the same process in the development of the ‘Monthly Precipitation’ grids.

A simple way to determine reference evapotranspiration is the ‘modified Hargreaves’ equation (Droogers and Allen, 2002), which generates superior results than the Pennman-Montieth when information is uncertain.

\[ET_0 = 0.0013\times 0.408\times RA\times (T_{avg}+17)\times (TD-0.0123 P)^{0.76}\]

The ‘modified Hargreaves’ uses the average of the mean daily maximum and mean daily minimum temperatures (\(T_{avg}\) in degrees Celsius), the difference between mean daily maximum and mean daily minimums (\(TD\)), \(RA\) is extraterrestrial radiation (\(RA\) in \(\mathrm{MJm^{-2}d^{-1}}\) and precipitation (\(P\) in mm per month), all of which can be relatively easily obtained. Temperature and precipitation data are often available from regional charts or direct measurement. Radiation data, on the other hand, is far more expensive to measure directly but can be reliably estimated from online tools, tables or equations. FAO Irrigation Drainage Paper 56 provides radiation data in Annex 2.

The reference evapotranspiration could be also calculated using the Hamon equation (Hamon 1961, Wolock and McCabe 1999):

\[PED_{Hamon} = 13.97 d D^2W_t\]

where \(d\) is the number of days in a month, \(D\) is the mean monthly hours of daylight calculated for each year (in units of 12 hours), and \(W_t\) is a saturated water vapor density term calculated by:

\[W_t = \frac{4.95e^{0.062 T}}{100}\]

where \(T\) is the monthly mean temperature in degrees Celsius. Reference evapotranspiration is set to zero when mean monthly temperature is below zero.

A final method to assess ETo, when pan evaporation data are available, is to use the following equation.

\(ETo = pan ET *0.7\) (Allen et al., 1998)

Digital elevation model

DEM data is available for any area of the world, although at varying resolutions.

Free raw global DEM data is available from:

Alternatively, it may be purchased relatively inexpensively at sites such as MapMart (www.mapmart.com).

The DEM resolution may be a very important parameter depending on the project’s goals. For example, if decision makers need information about the impacts of roads on ecosystem services then fine resolution is needed. The hydrological aspects of the DEM used in the model must be correct. Most raw DEM data has errors, so it’s likely that the DEM will need to be filled to remove sinks. The QGIS Wang & Liu Fill algorithm (SAGA library) or ArcGIS Fill tool have shown good results. Look closely at the stream network produced by the model (stream.tif.) If streams are not continuous, but broken into pieces, the DEM still has sinks that need to be filled. If filling sinks multiple times does not create a continuous stream network, perhaps try a different DEM. If the results show an unexpected grid pattern, this may be due to reprojecting the DEM with a “nearest neighbor” interpolation method instead of “bilinear” or “cubic”. In this case, go back to the raw DEM data and reproject using “bilinear” or “cubic”.

Land use/land cover

A key component for all water models is a spatially continuous land use/land cover (LULC) raster, where all pixels must have a land use/land cover class defined. Gaps in data will create missing data (holes) in the output layers. Unknown data gaps should be approximated.

Global land use data is available from:

Data for the U.S. is provided by the USGS and Department of the Interior via the National Land Cover Database: https://www.mrlc.gov/finddata.php

The simplest categorization of LULCs on the landscape involves delineation by land cover only (e.g., cropland, forest, grassland). Several global and regional land cover classifications are available (e.g., Anderson et al. 1976), and often detailed land cover classification has been done for the landscape of interest.

A slightly more sophisticated LULC classification involves breaking relevant LULC types into more meaningful types. For example, agricultural land classes could be broken up into different crop types or forest could be broken up into specific species. The categorization of land use types depends on the model and how much data is available for each of the land types. You should only break up a land use type if it will provide more accuracy in modeling. For instance, only break up ‘crops’ into different crop types if you have information on the difference in evapotranspiration rates (Kc) and soil characteristics (CN) between crop management values.

Sample Land Use/Land Cover Table

lucode

Land Use/Land Cover

1

Evergreen Needleleaf Forest

2

Evergreen Broadleaf Forest

3

Deciduous Needleleaf Forest

4

Deciduous Broadleaf Forest

5

Mixed Cover

6

Woodland

7

Wooded Grassland

8

Closed Shrubland

9

Open Shrubland

10

Grassland

11

Cropland (row Crops)

12

Bare Ground

13

Urban and Built-Up

14

Wetland

15

Mixed evergreen

16

Mixed Forest

17

Orchards/Vineyards

18

Pasture

Soil group

Two global layers of hydrologic soil group are available, 1) from FutureWater (available at: http://www.futurewater.eu/2015/07/soil-hydraulic-properties/) and 2) ORNL-DAAC’s HYSOGs250m (available at https://daac.ornl.gov/SOILS/guides/Global_Hydrologic_Soil_Group.html.)

The FutureWater raster provides numeric group values 1-4 14, 24 and 34. The Seasonal Water Yield model requires only values of 1/2/3/4, so you need to convert any values of 14, 24 or 34 into one of the allowed values.

HYSOGs250m provides letter values A-D, A/D, B/D, C/D and D/D. For use in this model, these letter values must be translated into numeric values, where A = 1, B = 2, C = 3 and D = 4. Again, pixels with dual values like A/D, B/D etc must be converted to a value in the range of 1-4.

If desired, soil groups may also be determined from hydraulic conductivity and soil depths. FutureWater’s Soil Hydraulic Properties dataset also contains hydraulic conductivity, as may other soil databases. Table 1 below can be used to convert soil conductivity into soil groups.


Table 1: Criteria for assignment of hydrologic soil groups (NRCS-USDA, 2007 Chap. 7)

Group A

Group B

Group C

Group D

Saturated hydraulic conductivity of the least transmissive layer when a water impermeable layer exists at a depth between 50 and 100 centimeters

>40 μm/s

[40;10] μm/s

[10;1] μm/s

<1 μm/s (or depth to impermeable layer<50cm or water table<60cm)

Saturated hydraulic conductivity of the least transmissive layer when any water impermeable layer exists at a depth greater than 100 centimeters

>10 μm/s

[4;10] μm/s

[0.4;4] μm/s

<0.4 μm/s

Watersheds / subwatersheds

To delineate watersheds, we provide the InVEST tool DelineateIT, which is relatively simple yet fast and has the advantage of creating watersheds that might overlap, such as watersheds draining to several dams on the same river. See the User Guide chapter for DelineateIt for more information on this tool. Watershed creation tools are also provided with GIS software, as well as some hydrology models. It is recommended that you delineate watersheds using the DEM that you are modeling with, so the watershed boundary corresponds correctly to the topography.

Alternatively, a number of watershed maps are available online, e.g. HydroBASINS: http://hydrosheds.org/. Note that if watershed boundaries are not based on the same DEM that is being modeled, results that are aggregated to these watersheds are likely to be inaccurate.

Exact locations of specific structures, such as reservoirs, should be obtained from the managing entity or may be obtained on the web:

Some of these datasets include the catchment area draining to each dam, which should be compared with the area of the watershed(s) generated by the delineation tool to assess accuracy.

Biophysical table

It is recommended to do a literature search to look for values for CN and Kc that are specific to the area you’re working in. If these are not available, look for values that correspond as closely as possible to the same types of land cover/soil/climate. If none of these more local values are available, several general sources are recommended.

  • Curve numbers (fields CN_A, CN_B, CN_C, CN_D) can be obtained from the USDA handbook: (NRCS-USDA, 2007 Chap. 9)

  • Monthly Kc values (fields Kc_1 through Kc_12) can be obtained from the FAO guidelines: (Allen et al., 1998)

For water bodies and wetlands that are connected to the stream, CN can be set to 99 (i.e. assuming that those pixels rapidly convey quickflow.)

When the focus is on potential flood effects, CN may be selected to reflect wet antecedent runoff conditions: CN values should then be converted to ARC-III conditions, as per Chapter 10 in NRCA-USDA guidelines (2007).

Rain events table

The average number of monthly rain events can be obtained from local climate statistics (Bureau of Meteorology) or online resources:

Climate zones are available from: http://koeppen-geiger.vu-wien.ac.at/present.htm

Threshold flow accumulation

There is no one “correct” value for the threshold flow accumulation (TFA). The correct value for your application is the value that causes the model to create a stream layer that looks as close as possible to the real-world stream network in the watershed. Compare the model output file stream.tif with a known correct stream map, and adjust the TFA accordingly - larger values of TFA will create a stream network with fewer tributaries, smaller values of TFA will create a stream network with more tributaries. A good value to start with is 1000, but note that this can vary widely depending on the resolution of the DEM, local climate and topography. Also note that streams delineated from a DEM generally do not exactly match the real world, so just try to come as close as possible. If the modelled streams are very different, then consider trying a different DEM. This is an integer value, with no commas or periods - for example “1000”.

A global layer of streams can be obtained from HydroSHEDS: http://hydrosheds.org/, but note that they are generally more major rivers and may not include those in your study area, especially if it has small tributaries. You can also try looking at streams in Google Earth if no more localized maps are available.

alpha_m

Default=1/12. See Appendix 2

beta_i

Default=1. See Appendix 2

gamma

Default =1. See Appendix 2



Appendix 2: \({\mathbf{\alpha},\mathbf{\beta}}_{\mathbf{i}},\)and \(gamma\) parameters definition and alternative values

\(\alpha\) and \(\beta_{i}\) represent the fraction of annual recharge from upslope pixels that is available to a downslope pixel for evapotranspiration in a given month. The product \(\alpha \times \beta_{i}\) is expected to be <1 since some water from upslope may be unavailable, either when it follows deep flowpaths or when the timing of supply and (evapotranspiration) demand is not right.

\(\alpha\) is a function of precipitation seasonality: recharge from a given month can be used by downslope areas during later months, depending on the subsurface travel times. In the default parameterization, its value is set to 1/12, assuming that the soil buffers water release and that the monthly contribution is exactly one 12th of the annual contribution. An alternative assumption is to set values to the antecedent monthly precipitation values, relative to the total precipitation: Pm-1/Pannual

\(\beta_{i}\) is a function of local topography and soils: for a given amount of upslope recharge, the amount of water used by a pixel is a function of the storage capacity. It also depends on the characteristics of the upslope area: the use of the upslope subsidy is conditioned by the shape and area of the contribution area (i.e. the recharge from the pixel just above the pixel of interest is less likely to be lost than the pixels much further away)

In the default parameterization, \(\beta\) is set to 1 for all pixels. One alternative is to set \(\beta_{i}\) as TI, the topographic wetness index for a pixel, defined as \(ln(\frac{A}{\text{tan}\beta}\)) (or other formulation including soil type and depth).

γ represents the fraction of pixel recharge that is available to downslope pixels. It is a function of soil properties and possibly topography. In the default parameterization, γ is constant over the landscape and plays a role similar to \(\alpha\).

In practice

The options above are provided mainly for research purposes. In practice, we suggest that for highly seasonal climates, alpha should be set to the antecedent monthly precipitation values, relative to the total precipitation: Pm-1/Pannual

Then, we offer two options to address the uncertainty around the parameter values:

  1. Verification of actual evapotranspiration with observations

The model outputs the actual evapotranspiration at the annual time scale: users can adjust parameters to meet observed actual evapotranspiration (e.g. from MODIS, http://www.ntsg.umt.edu/project/mod16). In the following, “_mod” stands for modeled AET, “_obs” stands for observed AET.

  • If AET_mod > AET_obs, the model overpredicts evapotranspiration, which can be corrected by: reducing Kc values, or reducing gamma values, and/or beta values (so less water is available for each pixel).

  • If AET_mod < AET_obs, the model underpredicts evapotranspiration, which can be corrected by: increasing Kc values (and increasing gamma or beta values if they are not at their maximum of 1).

If monthly values of AET are available, a finer calibration can be performed by changing the seasonal parameter alpha.

  1. Ensemble modeling

The model can be run under different assumptions and the outputs compared to estimate the effect of parameter error. Parameter ranges can be determined from assumptions about the proportion of upslope subsidy available to a given pixel; they can be set to the maximum bounds (0 and 1) for preliminary results.

References

Allen, R.G., Pereira, L.S., Raes, D., Smith, M., 1998. Crop evapotranspiration - Guidelines for computing crop water requirements, FAO Irrigation and drainage paper 56. Rome, Italy.

NRCS-USDA, 2007. National Engineering Handbook. United States Department of Agriculture, http://www.nrcs.usda.gov/wps/portal/nrcs/detailfull/national/water/?cid=stelprdb1043063.

© Copyright 2019, The Natural Capital Project.