96
3 Basics of Nonhydrostatic Modelling
On the other hand, with disappearance of the evaporative forcing, inertia leads to
rapid levelling out of the sea level while lateral density gradients remain. Baroclinic
pressure gradients are left behind and now can create the outflow of hypersaline
bottom water into the ambient sea (Fig. 3.56, bottom panel). The sea level in the
estuary drops owing to this outflow and triggers an intensified inflow in the surface
layer. Findings of this exercise indicate that the circulation in inverse estuaries is
intermittent and responds rapidly to variations in evaporation rates.
3.25.4 Additional Exercise for the Reader
Describe a temporally varying evaporation rate according to:
E(t) = E o [1 − cos (2π t/T )]
where E o = 5 cm/day. Vary the period T between 1 and 10 days and explore the
resultant exchange circulations.
3 Basics of Nonhydrostatic Modelling
On the other hand, with disappearance of the evaporative forcing, inertia leads to
rapid levelling out of the sea level while lateral density gradients remain. Baroclinic
pressure gradients are left behind and now can create the outflow of hypersaline
bottom water into the ambient sea (Fig. 3.56, bottom panel). The sea level in the
estuary drops owing to this outflow and triggers an intensified inflow in the surface
layer. Findings of this exercise indicate that the circulation in inverse estuaries is
intermittent and responds rapidly to variations in evaporation rates.
3.25.4 Additional Exercise for the Reader
Describe a temporally varying evaporation rate according to:
E(t) = E o [1 − cos (2π t/T )]
where E o = 5 cm/day. Vary the period T between 1 and 10 days and explore the
resultant exchange circulations.