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\[t = \frac{{\pi \cdot \left( {3.3 \times {{10}^{ - 4}} \cdot V - 0.5} \right)^2}}{{1 \times {{10}^{ - 6}}}}\]  Table 2 lists values of t for different values of V. The values of V were chosen corresponding to the volumes of fluid expelled from an overpressured 40km x 1000m thick sediment sequence at depth within the Edale basin with incremental changes in porosity of 0.1, 1 and 10\% on dewatering. The corresponding values of t are 16, 1723 and 173500 years respectively. These correspond to mean fluxes of 285, 26.5 and 0.26 litres.hr^{-1}. litres.m^{-1}.hr^{-1}. Such flow rates are not unrealistic. Very high rates of effusion for periods of several years have been observed following earthquakes e.g (add refs by Nur and Tsuneishi et al., 1970)  One can legitimately question the model details and parameter estimates but the point of this somewhat heuristic approach is not to be an accurate model. It is to give an indication of the likely flow rates that are needed to sustain the maximum observed thermal anomaly within the Dirtlow Rake fault system.