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Fig.
. 1.
Hydrological dynamics at cell level
When distanceTransfer is c
according to the lowest al
possibility to represent stoc
each cell the quantity of w
residence in the cell. Any
cell through decreasing the
from each water pack is pr
cell, with constraint of the t
quantity of water available
Underground flow betw
attribute for Cell, deepTr
deepTransfer * (c1 saturati
c2 is the cell with the low
computed as the difference
groundwater compartment
groundwater compartment w
average from one year to
this leakage parameter at
because there is no outflow
Model handles specifica
boundary cell goes through
cell with the rules explain
unsuccessful, the target cel
Each boundary cell goes thr
omputed, the transfer path of the water pack is determin
ltitudes. A key benefit of this modelling approach is
cks and flows at the same time, since we can compute
water going through it during the time step and its time
withdrawing along the flow can also be computed in
e quantity of water flowing through it. Quantity withdra
roportional to time of residence of this water pack on
total quantity of water withdrawn during the time step
for each water pack.
ween cells is adapted from [23]. It features an additio
ransfer, such that a cell c1 will transfer to a cell
ion - c2 saturation), if c1 saturation > c2 saturation an
west saturation in c1 neighbourhood. A cell saturation
e between its groundwater compartment capacity and
t content. Further each cell has a leakage from
which is calibrated so that this compartment stays stable
another without withdrawals. Calibration has determi
1.6mm for each cell. Adding this parameter is nee
from ground water.
ally boundary cells to prevent from boundary effects. E
h the same surface flow process if it can identified a tar
ned above for non boundary cells. If this identification
ll is a virtual cell, assumed to be 1 m below emitting c
rough the same underground transfer as explained abov
ned,
the
for
e of
any
awn
the
and
onal
c2
nd if
n is
d its
its
e in
ned
ded
Each
rget
n is
cell.
ve if
