in tJie South English Chalk. 361 



effect of the anticline as to prevent any further chalk of the zone of 

 Marstipites from coming into the cliff. After about half a mile the 

 beds begin to dip eastwards again, and the whole thickness of the 

 subzone passes out of the cliff into the foreshore in the course of 

 a quarter of a mile at Old Nore Point. The syncline into which the 

 beds are here passing is a very gentle one and culminates just west 

 of the miniature rifle butts under Castle Hill, but the gentle westerly 

 dip which prevails from this point to Newhaven harbour is just as 

 likely to be due to the change of direction of the cliff giving a section 

 along the general dip oft' the Wealden axis as to the approach of 

 another anticline transverse to the general coastline. It certainly 

 does not bring the subzone iip into the cliff again. There may well 

 be an anticline bringing up the subzone in the middle of the Ouse 

 Valley ; but in any case when the chalk reappears on the coast at 

 the Buckle Inn, near Seaford, this subzone has sunk far below beach 

 level and is only seen again in Seaford Head. 



[The various folds Avhich have been indicated may be labelled from 

 west to east as — Rottingdean syncline, Saltdean anticline, Telscombe 

 syncline. Friars Bay anticline. Castle Hill syncline, Seaford syncline, 

 and Seaford Head anticline. They are obviously capable of being 

 referred to just such a system, if not a continuation of the same 

 system, of folds, oblique and secondary to the Wealden axis, as 

 I have suggested in Hants. The Seaford syncline has been shown 

 by Dr. Elsden to run inland obliquelj- to the coastline, and Meeching 

 Quarry, Newhaven, almost certainly gives a similarly oblique line of 

 prolongation for the Friars Bay anticline.] 



The subzone varies very little lithologically in these exposures. It 

 is 60 feet thick between Brighton and Rottingdean and again in 

 Friars Bay and 64 feet in the Saltdean anticline, and the minute 

 lithological details correspond so closely that it can hardly be doubted 

 that the marl beds treated in the following section as corresponding 

 are actually continuous over the intervening areas. Even at Seaford 

 Head there appears to be an exact correspondence bed by bed and 

 marl seam by marl seam, though the thicknesses of the individual beds 

 are uniformly reduced, perhaps owing to local compression in the 

 course of folding. 



This subzone reproduces very accurately in Sussex the features 

 ascribed to it in Hants. The lower 25 feet or so are characterized 

 by E. scutatus, var. iectiformis, Bonrgueticrimis Form 6, and 

 0. Wegmanniana and 0. incurva in abundance. The next 25 feet 

 or so are characterized by E. scutatus, var. depressus, and Bourgueti- 

 crinus Form 5, while in the upper 10 feet or so E. scutatus passes 

 rapidly into the var. tnoicatus, which becomes fully established before 

 the subzone ends. The section indicates the lowest bed in which 

 I have yet found 0. pilula. It occurs in all higher beds. 



It is necessary to deal with the grounds on which I have fixed my 

 base of the subzone. As I have found normal (small and smooth) 

 Marsupites plates in the cliff at Friars Bay, immediately below the 

 lowest marl seam shown in my sections, it is clear that the zone of 

 Marsupites is properly carried up to that seam, and the only question 

 is as to the 7 ft. baud of chalk separating it from the one I have 



