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\[\delta_E = \bigg[\frac{\alpha_e\delta_L - h\delta_a - \epsilon_e - \Delta\epsilon}{(1 - h)}\bigg]\]   The evaporation model describes how isotopic fractionation causes the isotope ratio to change between the liquid water surface and the free atmosphere. It includes equilibrium effects at the water surface (reflects the temperature at the evaporating surface) and the kinetic effects related to the diffusion of water vapour from the liquid surface to the atmosphere above. For modeling the isotope ratios of ET fluxes, there are number areas of uncertainty in the parameterisation of the model:  \begin{itemize}  \item temperature of the evaporating surface - hard to measure and can have a large effect on attempts to partition ET using isotopes. isotopes \cite{Dubbert_2013}.  \item The height of $\delta$_a - normally just assumed to be the measurement height   \item The $\delta$_L definition - where is the evaporating surface in the soil. What is the isotopic composition of the evaporating leaf water.  \item the parameterisation of kinetic fractionation factor  \item steady state vs non-steady state plant transpiration  \begin{itemize}