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\begin{equation}\label{eq:1}  \delta_E = \bigg[\frac{\alpha_e\delta_L - h\delta_a - \epsilon_e - \Delta\epsilon}{(1 - h)}\bigg]  \end{equation}  The evaporation model describes how the  isotopic fractionationcauses the isotope ratio to change  between the liquid water surface and the water vapor transported to 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. The kinetic fractionation term ($\Delta\epsilon$), includes the parameterisation of the relative importance of turbulence and molecular diffusion for the transport from the diffusive sub-layer to the free atmosphere above (turbulent transport is assumed to be non-fractionating and molecular diffusion is). 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 \cite{Dubbert_2013}.  \item The height of $\delta$_a - normally just assumed to be the measurement height