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Central to understanding how cloud feedback is produced is a thermodynamic equilibrium, commonly referred to in the literature as the Earth’s radiative equilibrium temperature. The Stefan-Boltzmann Law calculates this value as 255K, and two observations have been shown to determine its value: (i) incoming and outgoing SW and LW radiative flux (figure 1) (ii) the greenhouse effect (Wells, 2012). By recourse to observational data from the CERES satellite, the net forcing this radiative flux produces when interacting with clouds can be quantified by reducing the climate into two simple (though reductive) states: a cloudy and non-cloudy sky (Ramanathan et al., 1987). In the first state, a cloudy sky reflects incoming SW radiative flux away from the Earth, thus reducing ECS by producing a forcing of - 50. In the second state, the absence of clouds in a non-cloudy sky produces a forcing of + 30, as the greenhouse effect can absorb more incoming SW radiative flux at the TOA. Owing to the large magnitude of this forcing, it could be argued that clouds can cause significant feedback (Stephens, 2005). The greenhouse effect, therefore, can be thought of as a conduit through which this radiative flux mediates Earth’s radiative equilibrium, and for reasons hereafter discussed, cloud feedbacks and ECS.