IN THE ANGLO-PARIS BASIN 83 



up as a hard-ground on the spathi Subzone sea floor for their upper surfaces are 

 strongly eroded (text-fig. 35) . The currents had scoured out the sandy matrix from 

 around the nodules, and, subsequently, phosphatic fragments from a later spathi 

 Subzone period of erosion accompanied by a gritty clay sediment were forced into the 

 crevices between and even underneath the nodules of ptizosianus age. J. -P. & P. 

 Destombes record ' Protohoplites raulinianus ' from this bed (1938a ; 102). 



In the foreshore to the NE. up to Strouanne, these puzosianus Subzone phosphatic 

 nodules are still present but are scattered and much more rolled : they have not 

 yielded fossils. In the reef on the foreshore in front of Petit Blanc Nez a few putty- 

 coloured gritty well-rolled smaller phosphatic nodules of puzosianus Subzone type 

 still occur mixed in with the predominantly spathi Subzone debris. It can be seen, 

 therefore, that the degree of reworking increases north-eastwards from the cliff 

 section near Wissant. In this respect it is important to note that the Palaeozoic 

 floor rises sharply off-shore (J. -P. & P. Destombes 1963 ; 53 text-fig. 3). 



There is no evidence of the presence of an eodentatus or lyelli Subzone element in 

 Bed 7, and the spathi element is strongly reminiscent of the fauna in Division A in 

 the Maidstone By-Pass (p. 38) which indicates that the earliest part of the spathi 

 Subzone may not be represented either. The equivalent of the Greensand Seam and 

 the basal spathi Subzone element of the dentatus nodule bed at Folkestone is, there- 

 fore, absent at Wissant. 



It is not easy to make out the complete sequence between Bed 7 and Bed 11 and it 

 is possible that these clays might be somewhat thicker than has been previously 

 recorded. Nonetheless, for the purpose of this account, the general sequence given 

 by P. & J. -P. Destombes will be the one considered. Hopiites (H.) occurs crushed in 

 the matrix of Bed 7 and in the lower 3 inches of Bed 8 (i), and these sediments are 

 classified with the spathi Subzone. The base of the intermedius Subzone has not been 

 satisfactorily defined but probably commences at the base of 8 (ii). Scattered 

 crushed examples of Anahoplites intermedius & A. praecox occur throughout the bulk 

 of 8 (ii) and P. Destombes records Falciferella in the uppermost 8 inches (20 cms) 

 (1962 ; 196-7). Bed 8 (ii) is, therefore, classified with the intermedius Subzone, 

 however, as can be seen from the section and the general nature of the fauna it differs 

 greatly from the upper part of Bed I and Bed II at Folkestone. P. Destombes (1962) 

 classifies the bed later numbered 9 with the niobe Subzone and this must also include 

 Bed 10. 



Bed 11 has yielded a remanie fauna of ammonites including Mojsisovicsia sub- 

 delaruei & M. remotum indicating the subdelaruei Subzone, Euhoplites of the mean- 

 drinus group indicating that Subzone, and also fragments of Euhoplites lautus and 

 E. nitidus indicating the nitidus Subzone. The degree of condensation at Wissant is, 

 therefore, greater than that represented by Bed IV at Folkestone and includes mater- 

 ial also found in the nitidus Subzone sediments of Bed V. 



The nitidus Subzone is well developed in Bed 12 (i-iv) and the preservation of the 

 fossils particularly in 12 (iii) is identical to that of Bed V-VI at Folkestone. It is 

 possible that 12 (iv) may represent the equivalent of the lower part of Bed VII below 

 the base of the daviesi Subzone but there is no certain evidence for this. However, 

 it is certain that there is an important break in the sequence between 12 (iv) and (v), 



