Abstract. Understanding what controls the water vapor isotopic composition of
the sub-cloud layer (SCL) over tropical oceans (δD0) is
a first step towards understanding the water vapor isotopic composition
everywhere in the troposphere. We propose an analytical model to predict
δD0 motivated by the hypothesis that the altitude from
which the free tropospheric air originates (zorig) is an important
factor: when the air mixing into the SCL is lower in altitude, it
is generally moister, and thus it depletes the SCL more efficiently.
We extend previous simple box models of the SCL by prescribing the
shape of δD vertical profiles as a function of humidity profiles
and by accounting for rain evaporation and horizontal advection effects.
The model relies on the assumption that δD profiles are steeper
than mixing lines, and that the SCL is at steady state, restricting
its applications to timescales longer than daily. In the model, δD0
is expressed as a function of zorig, humidity and temperature
profiles, surface conditions, a parameter describing the steepness
of the δD vertical gradient, and a few parameters describing
rain evaporation and horizontal advection effects. We show that δD0
does not depend on the intensity of entrainment, in contrast to several
previous studies that had hoped that δD0 measurements
could help estimate this quantity. Based on an isotope-enabled general circulation model simulation,
we show that δD0 variations are mainly controlled by mid-tropospheric
depletion and rain evaporation in ascending regions and by sea surface
temperature and zorig in subsiding regions. In turn, could δD0
measurements help estimate zorig and thus discriminate between
different mixing processes? For such isotope-based estimates of zorig
to be useful, we would need a precision of a few hundred meters in
deep convective regions and smaller than 20 m in stratocumulus regions.
To reach this target, we would need daily measurements of δD
in the mid-troposphere and accurate measurements of δD0
(accuracy down to 0.1 ‰ in the case of stratocumulus clouds,
which is currently difficult to obtain). We would also need information
on the horizontal distribution of δD to account for horizontal
advection effects, and full δD profiles to quantify the uncertainty
associated with the assumed shape for δD profiles. Finally,
rain evaporation is an issue in all regimes, even in stratocumulus
clouds. Innovative techniques would need to be developed to quantify
this effect from observations.