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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.m^{-1}.hr^{-1}. Such flow rates are not geologically  unrealistic. Very The highest rates associated with the smallest fluid pulses are on the order of the  high rates of effusion from springs that have been monitored  for periods of several yearshave been observed  following moderate  earthquakes e.g (add refs by Nur and Tsuneishi et al., 1970) 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 thelikely  flow rates that are needed to sustain the maximum observed thermal anomaly within the Dirtlow Rake fault system. system assuming a physical system that couples fluid overpressure and faulting.