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PERFECT GWlag  SRG
GWlag is both a rainfall runoff model and a constituent (salt) generation model. Descriptions of both these aspects of functionality are provided in this section.
Description and rationale
Catchment models have traditionally focused on estimating total stream flows with less emphasis on modelling the groundwater component. Greater pressure on water resources and the environment, as well as the need to better model constituent generation, has led to more interest in low flow conditions, particularly how these are impacted by groundwater  surface water interactions.
GWlag is a simple delay based model to explicitly simulate groundwater movement in catchments, improving both the contributions and timing of groundwater to the stream, especially at low flows. It estimates both slow and quick groundwater contributions to stream flow at the catchment outlet. It also estimates groundwater salt load contributions to the stream. GWlag is intended to be applied across upland areas composed mainly of local and intermediate groundwater flow systems.
Scale
GWlag operates at the catchment scale and daily timestep.
Principal developer
The principal developer is eWater building on earlier work as noted below.
Scientific provenance
GWlag builds on earlier models including 2CSalt (Stenson et al., 2005; Stenson et al., 2011) and the Biophysical Capacity to Change model (BC2C) (Dawes et al., 2004; Gilfedder et al., 2009) which were developed by CSIRO and the Cooperative Research Centre for Catchment Hydrology. In addition, GWlag incorporates the 1D PERFECT crop water balance model (Littleboy et al., 1992) developed by the Queensland Department of Primary Industries.
Version
Source v3.8.10
Dependencies
None
Availability/conditions
GWlag is a plugin, but is available in the plugin folder that accompanies Source installations.
Flow phase
The conceptual model used inisation of the GWlag builds on the structure of the 2CSalt model (Stenson et al. 2005; 2011) and BC2C (Gilfedder et al. 2009). A gauged catchment is subdivided into subcatchments using terrain analysis of surface topography and a knowledge of the scale of the underlying Groundwater Flow Systems (Coram et al. 2000).
Each subcatchment is further divided into Functional Units (FUs), which are defined as areas with the same combination of soil, landuse and climate. For each of these FUs, water balances are calculated using the 1D PERFECT crop water balance model (Littleboy et al. 1992). PERFECT (Productivity, Erosion, Runoff Functions to evaluate Conservation Techniques) considers climate, crop type, and soil parameters, and predicts surface runoff and deep drainage. The PERFECT results from all FUs are summed to the subcatchment level.
GWlag works at a subcatchment scale and accepts daily deep drainage which is split into recharge of groundwater (slow flow) and shallow lateralflow (quick flow) (using the approach of Rassam and Littleboy 2003) from each FU within the subcatchment. Groundwater and lateral flow response time scales are calculated for each subcatchment using linearstoragedischarge relationships. In addition to the groundwater and lateral flow delays, GWlag allows for losses of groundwater recharge to deep regional groundwater, and for losses from the stream itself due to prolonged dry periods and groundwater pumping. The delayed groundwater and lateral flows, losses, and surface runoff are combined to predict the daily stream flow at the outlet of the catchment (Figure 1).
Source catchments implementation
GWlag is in the form of a Rainfall Runoff model and includes the companion models SimpleGWSaltModel, PumpingImpactModel, and FlowScaledNodeLossModel.
The SimpleGWSaltModel uses estimated spatial representations of groundwater salinity to a subcatchment scale. Salt is treated as conservative and is tightly linked to slow flow discharge to the stream. It is designed to give an estimate of groundwater concentrations of salt to upland streams.
The PumpingImpactModel simulates the impact of groundwater extraction on stream flow and loads and is applied at a catchment scale through the implementation of one or many pumps within each subcatchment. Pumps can be either spatially implemented or behave as a simple abstract loss. Each pump has a series of pumping events where water and constituents are removed for a specified period of time at a specified rate. As each event may take many years to fully impact the stream, each event is tracked and combined with all other events for a particular subcatchment, giving an overall impact at each timestep. The PumpingImpactModel may be applied to one or many subcatchments within Source.
The FlowScaledNodeLossModel simulates losses from the stream that are flow weighted and constrained by actual flow in the stream. The modeller applies a single loss volume which is then scaled against flow in the stream. The scaled loss is removed at each timestep. The loss cannot be greater than the flow in the stream.
Process
GWlag generates daily time series inputs of surface runoff and deep drainage. These inputs can be scaled if required. The surface runoff contributes directly to stream flow. Deep drainage is split into a lateral (quick) and a vertical recharge (slow) component. The lateral flow pathway is delayed using a user parameterised exponential function before contributing to stream flow. The recharge component is delayed using a groundwater response time calculated from hydrogeology and topography (saturated hydraulic conductivity, storativity, aquifer thickness, aquifer flow length, and basement slope). This response time can then be scaled by a wholecatchment userdefined parameter. GWlag can deal with losses by removing groundwater and/or removing stream flow.
Rainfall scaling
There can be inconsistencies in the measured rainfall data used to drive the catchment runoff model. For example, this has been shown to be a specific issue in the Namoi River catchment (Croke et al. 2006; Herron and Croke 2007). This issue can be handled by changing rainfall in the 1D water balance model; although due to long run times this would need to be a separate exercise explored outside Source.
GWlag can allow for changes to catchment rainfall with a scaling parameter (P). GWlag uses P to scale deep drainage and runoff from the lumped 1D Water balance models.
Equation 1 

Equation 2 

where:
DD_{1D} lumped deep drainage output from 1D water balance models (m^{3}/day)
DD deep drainage used by GWlag (m^{3}/day)
P use defined scaling parameter (0<P<2)
RO_{1D} lumped runoff used by GWlag (m^{3}/day)
RO lumped runoff used by GWlag (m^{3}/day)
It is likely that P will be set to 1 in most catchments but if calibration/optimisation leads to a value of P which is not close to unity, it is likely that the rerunning of the 1D Water balance model with modified rainfall would be required to be undertaken.
Subsurface portioning factor
DD is split into lateral flow, and groundwater recharge using a partitioning fraction (PF). PF is determined using the method of Rassam & Littleboy (2003) (ie. calculated, not user defined), which was also used in the 2CSalt model (Stenson et al. 2005; 2011). The partitioning can also be scaled using γ (calibration parameter) if desired:
Equation 3 

Equation 4 

where:
R groundwater recharge (m^{3}/day)
DD deep drainage (m^{3}/day)
LF lateral flow (shallow subsurface) (m^{3}/day)
PF partitioning factor (0<PF<1) (Rassam and Littleboy, 2003)
γ calibration parameter (0 < γ <2)
Groundwater delay
A linearstoragedischarge relationship is used to predict groundwater response at a subcatchment level. A groundwater storage term (V) is calculated for each timestep but this is used to provide the response only, and is not meant to be considered explicitly.
Equation 5 

Equation 6 

where:
t is time (days)
DGW is the groundwater discharge to stream (m^{3}/day)
α is a calibration parameter (1 < α < 500)
R is Recharge (m^{3}/day)
VGW is a storage term (m^{3})
ts is the groundwater time scale (days)
The groundwater time scale is determined in a similar manner to the BC2C model (Gilfedder et al. 2009). This uses the idealised groundwater analogue that was developed by Walker et al. (2005) which captures some of the features of real, sloping aquifer systems (see Figure 2). It provides a simple approach for estimating the response of aquifers to changes in recharge, and for predicting the timescale between changes in recharge and subsequent changes in discharge.
Much of the literature on groundwater flow over sloping beds have a fullthickness seepage face as the downstreamend boundary condition (eg. Schmid and Luthin 1964; Childs 1971; Towner 1975; Verhoest and Troch 2000). This leads to a convex groundwater profile. The method in Walker et al. (2005) maintains a constant head boundary at the aquifer outlet, with the head at the elevation of the land surface  mimicking a stream overlying a thick and saturated zone. This boundary condition tends to result in a concave groundwater profile.
While the extended DupuitForchheimer assumption of streamlines parallel to the bed is typically used for modelling flow over sloping beds (eg. Wooding and Chapman 1966; Childs 1971). Chapman (1980) considered that the horizontal streamline assumptions remained satisfactory up to a bedslope of at least 10 degrees. Henderson and Wooding (1964) provided a solution for groundwater discharge from a steeply sloping aquifer using the classical DupuitForchheimer assumption of horizontal streamlines. In Walker et al. (2005) the mathematics is modified to allow for the inclusion of much flatter aquifers  with a focus on estimating changes in groundwater flux to a stream.
Groundwater time scale, ts, in equation 5 is calculated as follows.
Equation 7 

Equation 8 

where:
S is storativity (volume of water released from storage in an aquifer per unit decline in hydraulic head, per unit area of the aquifer. Storativity is a dimensionless quantity, and ranges between 0 and the effective porosity of the aquifer)
L is the groundwater flow length (m)
K is the saturated hydraulic conductivity (m/day)
a is the aquifer basement slope
Δh is the change in elevation of land surface (m)
d is the aquifer thickness
The calibration parameter, α (in equation 5), is applied globally, while the groundwater time scale, ts, is calculated for each individual subcatchment. Thus, the variability of groundwater responses across the catchment is maintained, but can be adjusted to provide a better fit to gauged information.
Lateral flow delay
GWlag uses a linearstoragedischarge relationship to predict lateral flow response. A storage term (V_{LF}) is calculated for each timestep but this is used to provide the response only, and is not considered explicitly.
Equation 9 

Equation 10 

where:
D_{LF} is the lateral flow discharge to stream (m^{3}/day)
β is a calibration parameter (1 ≤ β < 30)
LF is a lateral flow input (m^{3}/day)
V_{LF} is a storage term
Losses
In addition to the groundwater and lateral flow delays, GWlag can allow for three different types of "loss".
 Recharge to deep regional groundwater;
 Fixed losses from streams; and
 Variable groundwater pumping losses from streams.
Recharge to deep regional groundwater (D)
Not all recharge appears as stream flow, for example, some recharge provides water to the regional groundwater system which may discharge outside the catchment or directly to the ocean.
Recharge to deep regional groundwater is handled by removing a fixed daily volume from the groundwater store (VGW). In other words, Equation 6 is modified to include recharge to deeper groundwater (D):
Equation 11 

Fixed losses from the stream (L)
Incorporation of fixed losses can be used to improve the modelling of zero flow periods, in areas where streams are losing. It provides the capacity to model losing streams, including noflow periods that are likely to occur after prolonged dry periods.
Loss of water from the stream is calculated using:
Equation 12 

where:
L is the amount of water lost from the stream (m^{3}/day)
REMOVE is an input/calibration parameter
Q is the stream flow (prior to loss) (m^{3}/day)
If L is calculated as being less than zero it is set to zero.
Variable groundwater pumping losses
Variable groundwater pumping losses are additional losses that occur in areas with extensive groundwater development. These losses are calculated using classical stream depletion models (Glover and Blamer, 1954) which require knowledge of pumping rates, distance from stream/gauge and aquifer parameters (see also, Evans, 2007). GWlag will recognise both local and regional impacts of pumping, depending on the depth of the bore.
Explicit groundwater pumping capacity is included in GWlag for two reasons: (1) if significant changes in groundwater development occur in the middle of a long simulation, then the depletion losses will be timevariant and hence a constant loss term will result in inferior calibration, and (2) to allow for scenario modelling to predict the impacts of proposed groundwater development on flows.
Pumping impacts are modelled as follows:
Equation 13 

where:
Q_{P} is the impact of pumping (m^{3}/day)
P is the pumping rate (m^{3}/day)
Erfc is the complementary error function
a is the distance of pump from subcatchment outlet (m)
D is the aquifer diffusivity (m^{2}/day)
K is the saturated conductivity (m/day)
d is the aquifer thickness (m)
S is the storativity
t is the time since start of pumping.
The impacts of groundwater pumping are calculated for each bore (or borefield). These impacts are estimated and their effect is to remove water from the gauged catchment outflow. For each pump (ie. individual bore, or borefield), the following inputs are required:
 Location (latitude/longitude); and
 Pumping regime (volume and timestep; dates of operation (eg. 1 ML/day between 1 Oct 2010  31 Mar 2011).
The result is that for each timestep, the sum of the impacts of pumping (ΣQ_{p}) from all pumping events is calculated and this amount is then removed from the groundwater discharge to stream volume at the subcatchment level. (ie the "removed volume" will be at the groundwater salinity, not stream salinity). The impact of groundwater pumping can reduce groundwater discharge to zero thus depleting stream flow from upstream catchments. The losses due to groundwater pumping will capture the groundwater discharge (base flow) and can deplete stream flow. In those situations surface flow (quick runoff) will only be available for a short period of time. Flow will soon drop to zero, when the quick runoff disappears but the flow is prevented from being negative.
Modelled stream flow
The modelled stream flow will be:
Equation 14 

where:
Q is the stream flow (m^{3}/day)
DLF is discharge to stream flow from ‘lateral flow’ (m^{3}/day)
DGW is discharge to stream from groundwater (m^{3}/day)
RO is the runoff (m^{3}/day)
L is the amount of water lost from the stream (m^{3}/day)
ΣQ_{p} is the sum of the impacts of groundwater pumping (m^{3}/day)
If Q, in equation 14 is calculated to be less than zero, it is set to zero.
Modelled salt export
Note that this section is related to GWlag as a constituent generation model rather than as a rainfall runoff model. The explanation of this functionality is included here for completeness.
GWlag is a capable of modelling salt generation from subcatchments and salt exports in stream flow.
Equation 15 

Equation 16 

where:
SALT_{gen} is the salt generated from subcatchments (kg/day)
DLF is the discharge to stream from ‘lateral flow (m^{3}/day)
D_{GW} is the discharge to stream from groundwater (m^{3}/day)
LATPER is the ‘lateral flow’ salinity as a proportion of groundwater salinity
GW_{SAL} is the groundwater discharge salinity (kg/m^{3})
RO is the runoff (m^{3}/day)
RAIN_{SAL} is the rainfall salinity (kg/m^{3})
SALT is the salt export from catchment in stream flow (kg/day)
L is the amount of water lost from the stream (m^{3}/day)
ΣQ_{p} is the sum of the impacts of groundwater pumping (m^{3}/day)
Assumptions
The model makes the following assumptions:
 Contribution of water and constituents are calculated at a FU level and accumulated to a subcatchment level.
 Stream losses are calculated at the catchment outlet, not at a subcatchment level.
 Each subcatchment is modelled as a predominantly gaining system (stream losses are only calculated for the whole catchment).
 There is no feedback between the groundwater and the 1D Water balance models.
 All runoff makes it to the stream within the timestep.
 All deep drainage becomes recharge at the saturated zone within the timestep.
 The subcatchment is parameterised with a single set of hydrogeological values (area weighted average).
 The groundwater response assumes that aquifers are unconfined.
 Groundwater discharge can only occur to a stream (not to the land surface).
 Salt mass balance is conserved in the surface water.
Limitations
GWlag is not applicable in areas with regulated surface flow. It is suitable for local and intermediate groundwater flow systems and is intended for areas which are drained by surface water streams.
Input data
GWlag requires the following data sets:
 Spatial representations of soil type, land use type, climate zone (based on rainfall and ET), and initial conditions including proportion of field capacity (dimensionless), crop residue (kg/ha).
 Rainfall and ET time series. These are used for climate inputs for the GWlag model that is specified for each FU.
 Spatial representations of aquifer thickness (m), aquifer hydraulic conductivity (m/day) and aquifer storativity (dimensionless).
 Information on groundwater pumping to parameterise the pumping impacts model
 distance to local and regional impacts (m)
 aquifer diffusivity (m^{2}/day)
 pumping regimes (start and end dates and pumping rate (m^{3}/day)).
 Spatial representation of groundwater salinity (kg/m^{3}) and rainfall salinity (kg/m^{3}).
 Daily loss volume from the stream at the catchment outlet.
Parameters or settings
Model parameters are summarised in Table 1 and Table 2.
Table 1. Model parameters (PERFECT)
Parameter  Description  Units  Default  Range 
Covm  Percent surface residue cover based on the crop residue value    n.a.   
Cres  Crop residue – initial condition    n.a.   
PAWCFactor  Plant available water capacity factor    n.a.   
 Crop factor parameters 
 n.a. 

Ddwe  Daily root growth  mm  n.a.  ≥0 
Dwemax  Maximum root depth  mm  n.a.  ≥0 
Cf  Crop factor    n.a.   
EtPanWUE  Water use efficiency    n.a.   
HI  Harvest index    n.a.   
EtPanDays  Days from crop planting to harvest    n.a.  ≥0 
MaxResidCover  Maximum residual cover    n.a. 

Days0 … Days12 
   n.a.  0366 
Gcov0 … Gcov12 
   n.a.  0100 
Ccov0 … Ccov12 
   n.a.  0100 
NumberOfSoilHorizons  The number of soil horizons in the soil profile    1.0  1.03.0 
Cona  Stage II soil evaporation    n.a.   
Uritch  Upper limit of Stage I soil evaporation  mm  n.a.   
Cn2b  Runoff curve number for average antecedent moisture conditions and bare soil    n.a.   
Cnred  Reduction in curve number at 100% cover    n.a.   
Cracklimit  Limit of infiltration due to cracking  mm  n.a.  ≥0 
Cracking  Does cracking occur (0  no, 1  yes)    n.a.   
Cnrough  Maximum reduction in curve number due to tillage    n.a.   
Cnrain  Cumulative rainfall to remove roughness  mm  n.a.  ≥0 
Kusle  MUSLE K factor    n.a.   
Pusle  MUSLE P factor    n.a.   
Slope  Field slope  %  n.a.  0100 
Length  Slope length or bank spacing  m  n.a.  ≥0 
Beta  Rill/interrill ratio    n.a.  01 
Bd  Bulk density  cm  n.a.  0.010.0 
SoilHorizon1TotalDepth  Depth of soil horizon 1  mm  n.a.  ≥0 
SoilHorizon1AirDry 
 %  n.a.  ≥0 
SoilHorizon1LowerLimit  Lower limit for soil horizon 1  %  n.a.  0100 
SoilHorizon1UpperLimit  Upper limit for soil horizon 1  %  n.a.  0100 
SoilHorizon1Saturation  Saturation limit for soil horizon 1  %  n.a.  0100 
SoilHorizon1KSat  Saturated hydraulic conductivity of soil horizon 1  mm/h  n.a.  ≥0 
SoilHorizon2TotalDepth  Depth of soil horizon 2  mm  n.a.  ≥0 
SoilHorizon2AirDry 
 %  n.a.  ≥0 
SoilHorizon2LowerLimit  Lower limit for soil horizon 2  %  n.a.  0100 
SoilHorizon2UpperLimit  Upper limit for soil horizon 2  %  n.a.  0100 
SoilHorizon2Saturation  Saturation limit for soil horizon 2  %  n.a.  0100 
SoilHorizon2KSat  Saturated hydraulic conductivity of soil horizon 2  mm/h  n.a.  ≥0 
SoilHorizon3TotalDepth  Depth of soil horizon 3  mm  n.a.  ≥0 
SoilHorizon3AirDry 
 %  n.a.  ≥0 
SoilHorizon3LowerLimit  Lower limit for soil horizon 3  %  n.a.  0100 
SoilHorizon3UpperLimit  Upper limit for soil horizon 3  %  n.a.  0100 
SoilHorizon3Saturation  Saturation limit for soil horizon 3  %  n.a.  0100 
SoilHorizon3KSat  Saturated hydraulic conductivity of soil horizon 3  mm/h  n.a.  ≥0 
ModifyFluxesRatio  Fluxes modification ratio    n.a.  01 
Table 2. Model parameters (GWlag)
Parameter  Description  Units  Default  Range 

P  Rainfall scaling parameter    n.a.  0  2 
γ  Calibration parameter for subsurface partitioning    n.a.  0  2 
α  Calibration parameter for groundwater delay    n.a.  1  500 
β  Calibration parameter for lateral flow delay    n.a.  1  30 
D  Recharge to deep regional groundwater  m^{3}/day  n.a.  ≥0 
REMOVE  Calibration parameter for loss from the stream    n.a.  ≥1 
LATPER  ‘Lateral flow’ salinity as a proportion of the groundwater salinity    n.a.  0  1 
Output data
A time series of total stream flow at the catchment outlet (Q), salt export from the catchment in stream flow (SALT), discharge to the stream from lateral flow (D_{LF}), discharge to the stream from groundwater (DGW), and runoff from the water balance model (RO).
In addition, the variables listed in Table 3 can be recorded.
Table 3. Recorded variables from PERFECT
Variable  Parameter  Frequency 
Tsevap  Daily soil evaporation  time step 
Ttrans  Total daily transpiration  time step 
PreRassamLittleboyRecharge  Recharge before RassamLittleboy split  time step 
PostRassamLittleboyRecharge  Recharge after RassamLittleboy split  time step 
PostRassamLittleboyLateralFlow  Lateral flow after RassamLittleboy split  time step 
Swtot  Daily total soil water  time step 
Tse  Daily PERFECT evapotranspiration  time step 
GreenCover  Green cover proportion  time step 
TotalCover  Total cover proportion  time step 
Reference list
Chapman, TG (1980). Modelling groundwaterflow over sloping beds. Water Resources Research, 16(6):11141118.
Childs, EC (1971) Drainage of groundwater resting on a sloping bed’, Water Resources Research 7(50): 12561263.
Coram, JE, Dyson PR, Houlder, PA & Evans, WR (2000) Australian groundwater flow systems contributing to dryland salinity. Report by the Bureau of Rural Sciences for the Dryland Salinity Theme of the National Land and Water Resources Audit, Canberra.
Croke, BFW, Letcher, RA & Jakeman, AJ (2006) Development of a distributed flow model for underpinning assessment of water allocation options in the Namoi River Basin, Australia’, Journal of Hydrology 319: 5171.
Dawes,W.R., Gilfedder, M.,Walker, G.R., Evans,W.R., (2004). Biophysical modelling of catchmentscale surface water and groundwater response to landuse change. Math. Comput. Simul. 64(1): 312.
Evans, R. (2007). The impact of groundwater use on Australia’s Rivers, Land & Water Australia, Sinclair Knight Merz (SKM): 127.
Gilfedder, M, Walker, GR, Dawes, WR & Stenson, MP (2009) Prioritisation approach for estimating the biophysical impacts of landuse change on streamflow and salt export at a catchment scale, Environmental Modelling and Software 24(2): 262269.
Glover, RE & Balmer, GG (1954) River depletion resulting from pumping a well near a river, Transactions of the American Geophysical Union 35(3): 468470.
Henderson, FM & Wooding, RA (1964) Overland flow + groundwater flow from steady rainfall of finite duration, Journal of Geophysical Research 69(8) 15311540.
Herron, NF & Croke BWF (2007) Including the influence of groundwater exchanges in a lumped rainfallrunoff model, Proceedings of MODSIM07 Congress, December 2007, Christchurch, pp. 14361442.
Littleboy, M, Silburn, DM, Freebairn, DM, Woodruff, DR, Hammer, GL & Leslie, JK (1992) Impact of soil erosion on production in cropping systems, I. Development and validation of a simulation model, Australian Journal of Soil Research 30:757774.
Rassam, D & Littleboy, M (2003) ‘Identifying the lateral component of drainage flux in hill slopes’, Proceedings of MODSIM03 Congress, July 2003, Townsville, pp 183188.
Schmid, P & Luthin J (1964) Drainage of sloping lands’, Journal of Geophysical Research 69(8) 15251529.
Stenson, M, Littleboy, M & Gilfedder, M (2005) Modelling water and salt export from unregulated upland catchments: The 2CSalt model, Proceedings of International Water Conference, NZHSIAHNZSSS, Auckland, November, 2005.
Stenson, M. P., M. Littleboy and M. Gilfedder (2011) Estimation of water and salt generation from unregulated upland catchments. Environmental Modelling and Software 26(11): 12681278.
Towner, GD (1975) Drainage of groundwater resting on a sloping bed with uniform rainfall, Water Resources Research 11(1) 144147.
Verhoest, NEC & Troch, PA (2000) Some analytical solutions of the linearized Boussinesq equation with recharge for a sloping aquifer, Water Resources Research 36(3): 793800.
Walker GR, Gilfedder, M, & Dawes WR (2005) Idealised analogue for predicting groundwater response times from sloping aquifers. Technical Report 14/05, CSIRO Land and Water, Adelaide, 21pp.
Wooding, RA & Chapman, TG (1966) Groundwater flow over a sloping impermeable layer. 1. Application of DupuitForchheimer assumption’, Journal of Geophysical Research 71(1):28952902.
Bibliography
Gilfedder, M, Rassam, DW, Stenson, MP & Littleboy, M 2009, ‘Groundwater component of the WaterCAST catchment modelling framework’, Proceedings of 18th World IMACS/MODSIM Congress, July 2009, Cairns, [published as CDROM].