In the survey area the geological structure in theoverburden is relatively flat as can be seen in thesurface seismic volumes and in the symmetry ofthe CRG gathers. This structural simplicityallows us to use the well-known method ofslowness curve construction through which thephase slowness at the receiver array can becomputed from direct arrival time picks (e.g.Horne et al., 2008). Since these phase slownessesare only related to the formation propertiesaround the receiver array, we can use these datato provide local estimates of the anisotropy. Anexample of this analysis is shown in Figure 2where the calculated slowness data are shown as the black squares and the modelled data for thebest fitting models are shown in red.