WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 103 



break and on the same horizon into the f ossiliferous Chillesford Clay. 

 At Pakefield we have an expansion of the seam e with rootlets 

 traversing the clay, and occupying the position of / in the Easton 

 Bavant section. Is it therefore that in the interval between Cove- 

 hithe and Pakefield that this ' Pebbly Clay ' sets in between d and f, 

 or is it a continuation, modified by altered conditions, of the bed/? 



At Alderby, 6 miles inland, the dark clay, which there overlies 

 the riuvio-marine Crag, also contains angular flints, and the late 

 Mr. Rose had in his collection remains of the Elephant, Deer, and 

 two species of Cetaceans from this same bed. Though it is not 

 there overlain by the Westleton Beds, it was found to be so in 

 a deep well sunk at Beccles on the other side of the valley, and is 

 therefore generally held to be the Chillesford Clay-bed. There are 

 again traces of the Porest Bed at the cliff" at Corton with an under- 

 lying clay, of the same character as at Kessingland and with rootlets. 



If this Suffolk bed is to be considered the equivalent of the Chil- 

 lesford Clay, then the so-called Eorest Bed of Happisburgh, Bacton, 

 and Mundesley, which occupies the same position and contains the 

 same remains, must also be referred to that age ; but the peculiar 

 character of its Mammalian remains — its numerous large Deer, 

 its special Elephants, and other Mammalia, all so different from 

 those of the Crag — the absence of Mastodon, which occurs both at 

 Norwich and at Easton Bavant, together with the evident local 

 and exceptional character of the Eorest Series, renders it difficult 

 to accept that solution of the problem. 



Whatever may be the solution, it does not directly affect the par- 

 ticular question upon which we are engaged, as the Westleton 

 Shingle is newer than the Forest Bed, and passes indiscriminately 

 oyer it and over the Chillesford Beds. At the same time at the 

 junction of the two former on the Norfolk coast there is to a certain 

 extent a passage between them, land-conditions there alternating 

 with marine during the accumulation of the Westleton Shingle. I 

 shall therefore only refer incidentally to the Forest Bed, which is 

 the less necessary as it has often been well and fully described, and 

 will confine myself to following the range of the Westleton Beds. 



The Shingle, which is displaced by the Glacial Sands at Kessing- 

 land, resumes its place in the neighbourhood of Pakefield and 

 Lowestoft, where it exists in considerable force, consisting of the 

 usual pebbles of flint and white quartz, with subangular fragments 

 of flint, ragstone, and chert, and an unusually large proportion of 

 other rocks, such as fragments of a rnica-schist, of a dark green 

 quartzosc rock, and of yellow, green, and brown sandstones. In 

 this part of the cliffs clay pebbles are common at the base of the 

 Westleton Beds, arising probably from the i)artial destruction cither 

 of the Chillesford Clay or of one of the Forest Beds. Glacial sands 

 again occupy much of the Corton and Gorlcston clifts. As the broad 

 estuary of the Yare then intervenes, the Westleton Shingle is not 

 met with again until we reach the Happisburgh Cliffs ; and even 

 there little is seen of it, although the Forest Bed with its multitude 



