S. V. Wood, Jan. — Sequence of the Glacial Beds. 63 



to show that none of thorn can havo any connexion in timo with 

 tho Middle Glacial of East Anglia ; l)ut if, on tho other hand, they 

 be not identical, tho question then arises, how far this middle sand 

 of Cheshire and Lancashire offers grounds of identity with tho East 

 Anglian Middle Glacial. 



In the first place it behoves us to bear in mind that when we find 

 at Kelsea a gravel and sand whose fauna, as a group, offers nothing 

 that, on the one hand, would serve to identify it with the Middle 

 Glacial, or, on the other, with the Moel Tryfaen and Cheshire 

 fossiliferous sands, overlaid in actual section by a clay (that of 

 Hessle) Avhich, though containing Boulders (and striated ones, too), 

 is, as it seems to me, obviously unconnected with the Glacial series, 

 that is, with the beds belonging to the great subsidence, there is no 

 prima facie reason that sands should be identical with the Middle 

 Glacial of East Anglia merely because they intervene between two 

 Boulder-clays, or are intercalated in a Boulder-clay, as the case may 

 be. Beyond its bearing on any such prima facie assumption, there 

 is no need to allude further to the Hessle clay, for I have seen no 

 reason as yet to suppose that it is represented in the north-west of 

 England, though such may be the case. 



If it be the case, however, as Mr. Mackintosh represents,' that 

 the Lower Boulder-clay of Lancashire reaches up to elevations of 

 1,200 feet, then it is difficult to conceive that there can be any 

 identity between this clay and the beds, g and h, forming the East 

 Anglian Lower Glacial, for the following reasons : — The organic 

 remains occurring in, as well as the structure and distribution of the 

 beds, Ji. indicate that the little elevated counties of Norfolk and 

 Suffolk were only partially submerged during their accumulation ; 

 while the bed^ g, nowhere reaches higher than 250 feet. The marly 

 portion of this bed, g, being formed of the material of the soft chalk 

 of Norfolk, Suffolk, and the adjoining counties, ground down by ice, 

 and spread out in a nearly pure state under water, and the brick- 

 earth portion of it enclosing huge masses of the same marl, intro- 

 duced by the agency of bergs, proves that such chalk was not 

 sufficiently submerged at this time to be beyond the reach of the 

 degrading action of the icy envelope. The principal part of the 

 chalk so supplying the material of g does not lie at one-fifth of the 

 elevation thus reached by the lower clay of Lancashire, and even 

 its highest eminences fall hundreds of feet short of that elevation ; 

 and we can, therefore, scarcely suppose such a deposit as g to be 

 coeval with the lower clay of Lancashire, possessing the range in 

 elevation which is assigned to it. To suppose this Lancashire clay to 

 have been formed by land ice would not help the matter ; because 

 the 1,200 feet elevation must have been reached by th ' sea before 

 such ice as that to which the Glacial beds are due could be arrested, 

 so as to form a moraine. But, indeed, the difference between 

 GlaciaP clays, due to land ice, and those due to marine deposit, is 



^ Quart. Journ. Geol. 8oc., vol. xxv., p. 430. 



2 With Post-c/lacial beds, when the Glaciers were arrested before they reached the 

 sea, the case is different ; and beds due to land ice, in their true sjuse, may then'h.a.ie 

 accumulated, and at high elevations. 



