village of Thorpe. The spread of these sands generally obscures the subjacent rocks, but by a valley-denudation the Norwich Crag is exposed at the one spot described; and I believe the top of the Chillesford Clay to be also exposed for a short distance. To the presence of this clay I attribute the water which is found in the pit close by the shell-pit. The sands would not support water.

The stratification of the district strongly favours the view I have taken of the superposition of the Norwich Crag upon the Chillesford Clay. On the other hand, it would be quite possible to conceive that the Mya-bed might be here expanded into a thick bed of Crag, and this is what has been generally assumed to be the case. think, however, that the evidence rather supports my suggestion.

I

In the first place, the assemblage of species as seen at the shellpit differs from that of the Mya-bed. As strongly as I felt convinced on the spot that the Crag above Ferry-farm was derived from the Mya-bed, so strongly did I feel that the Crag at Thorpe was not derived from it.

In the second place, the pebbles of indurated clay found at the bottom of the shell-pit exactly correspond in composition and colour with the Chillesford Clay, wherever it is weathered brown, as, instance, at Chillesford itself.

for

In the third place, I have always noticed a porous sand underlying the Mya-bed, which would not support water. Indeed, in the clay pit near Sudbourn Park I have mentioned that a run of water from a field-drain is conducted to this sand and immediately lost in it. If, therefore, the Thorpe Crag were on the horizon of the Myabed, I do not think that we should have a spring at its base, nor a pond close by in the subjacent stratum.

The conclusion then appears to be correct, that the Fluvio-marine Crag at Thorpe near Aldborough rests on the Chillesford Clay, and that the descending sequence in that district is—

1. Fluvio-marine or Norwich Crag.

2. Chillesford Clay.

3. Mya-bed resting on sands, which, as at Aldborough Gasworks, are occasionally fossiliferous.

4. Red Crag.

Let us now see whether this sequence is borne out by other exposures of these beds.

It has long been known that a formation containing, as Sir Charles Lyell tells us, "lamellibranchiate shells with their valves united, mixed with land and freshwater Testacea, and with the bones and teeth of Elephant, Rhinoceros, Horse, and Deer"*, occurs

* Elements, 1855, p. 156. Since this paper was read I have been favoured with the sight of a letter written in 1864 by Col. Alexander to Mr. Searles V. Wood. Putting the contents of this letter by the side of the information I have received from Mr. Ewen, I gather that four Mastodon teeth have been obtained on this coast. That which is figured by Professor Owen in his 'Fossil Mammals' was found on the beach at Sizewell Gap, near Thorpe. Another, which Mr. Ewen now possesses, was found under the cliff after a fall at Easton Bavent. A third, with part of the jaw attached, was seen by Col. Alexander in the talus

at Easton Bavent Cliff near Southwold. I visited this spot in October, and was at once convinced, by the identity of the lithological character, that we here have the Chillesford Clay underlain by the Mya-bed.

Yet at this spot, as at Chillesford Brick-pit, I found no Myas in situ, though single valves occur. Tellina lata, with its valves united, is extremely common, as is also Tellina prætenuis.

Immediately beneath the Chillesford Clay we come upon a band of drifted shells, two or three inches thick, containing flints and fragments of bone imbedded in a coarse sand, and, beneath this, sand with Tellina as they lived. The bed occurs, where I saw it, at the very bottom of the second cliff north of the farm-house, and was only visible for a few feet, the rest being obscured by talus. The following species occur at this spot :

Tellina lata.
obliqua.
prætenuis.

Mya truncata.
Leda myalis.

Mactra ovalis.

Pecten opercularis.
Cyprina Islandica.
Litorina litorea.
Paludina lenta.

Mr. Ewen of Southwold, a friend of the late Col. Alexander, informed me that this band used to occur twenty-five years ago higher up in the cliff, and to the south of the spot where I found it, but that it had, through the wasting of the cliff, descended beneath the beach at the old locality, owing to the dip of the bed. This is important for my theory, as will appear in the sequel.

On examining other spots in the neighbourhood of Southwold, I found a pit at a place called Yarn Hill, near Potter's Bridge. Here is a bed of shells, chiefly Tellina in sand. It is covered by a brown loam, which I believe to be weathered Chillesford Clay, a band of flints in sand intervening; I have no doubt of its being a continuation of the Mya-bed seen in the cliff.

The species found at Yarn Hill were:—

Tellina obliqua (common).
lata (common).

prætenuis (common).

Mactra subtruncata (common).

ovalis (not common).

Cardium edule (common).
Cyprina Islandica (fragments).
Mytilus edulis.

Litorina litorea.

Buccinum undatum.
Natica catena.

Guillemini.

Ringicula buccinea.
Paludina lenta.
Succinea oblonga.

On the hills above this pit are pits of Chillesford loam and clay, extensive brick-works being carried on in the latter at Manor House, Frostenden, and other places. At Frostenden brick-kiln the sand is dry beneath the clay, but the Mya-bed appears to be absent. Draw

of the same cliff, and appears to have come from some position above the Myabed. It fell to pieces. A fourth, now in the possession of Mr. Ewen, was taken from the Mya-bed. It is the tooth of a very young animal.

Col. Alexander speaks of the occurrence of Crag shells in the talus of Easton Cliff to the south of the outcrop of the Mya-bed. The impression left on my mind is that some patches of Norwich Crag were then existing in the cliff in the position I have assigned to it above the Chillesford Clay, but hidden by talus.

ing a line from the spot where the Mya-bed occurs on the beach to the pit at Yarn Hill, which is scarcely raised above the sea-level, and bearing in mind that the outcrop on the coast has been carried beneath the beach towards the south by the encroachment of the sea, we obtain a dip towards the south-west.

Proceeding to Wangford, we meet with pits in the true Norwich Crag, exactly resembling the deposit at Thorpe, near Aldborough, and at the pits about Norwich. It is a gravelly deposit of considerable thickness; how thick the section does not show, because the upper part is denuded, but about 9 feet remains. The shells are not grouped as in the Mya-bed, the proportion of univalves being greater. None of the bivalves are in pairs. Here I found an antler of a deer, but too much decayed for removal.

I dug in the floor of this pit and found the Crag to rest on a laminated sandy loam, closely agreeing with the upper part of the Chillesford Clay at Easton Bavent Cliff. The dip of the beds to the southwest, as determined above, agrees well with this identification.

There is another pit, which I had not time to visit, at Bulcham Workhouse. I am told by Mr. Wood, jun., that it is in the Norwich Crag. Its position would agree very well with the view I take of its superposition on the Chillesford Clay.

Thus the observations I was enabled to make in the neighbourhood of Southwold confirm my former view, that the descending order of sequence is

1. Norwich Crag,

2. Chillesford Clay,
3. Mya-bed;

while they give the additional fact that the Mastodon and other Mammalia have been procured from the Mya-bed at Easton Cliff. We cannot, then, hesitate to include the Chillesford Clay in the Norwich Crag series.

I am not aware whether the Chillesford Clay occurs in the Norfolk district of the Crag, where it rests immediately upon the Chalk.

There can be no doubt about the Chillesford Clay being a marine deposit, for I found in it a lenticular patch of sand containing shells similar to those of the Mya-bed; and Mr. Prestwich and Mr. Wood found marine shells in it at Chillesford. The character of the deposit might otherwise have led one to suppose that it was lacustrine.

There are still some problems of considerable complexity to be solved respecting the sequence between the Mya-bed and the Red Crag, and again from the Norwich Crag upwards.

It is well known that in the district of the Red Crag there are thick beds of reddish-brown sand overlying the fossiliferous Red Crag. These have been called "the unproductive sands of the Crag"*. Mr. Wood, jun., considers them to belong to his "middle drift," and thinks that the Chillesford beds are a local modification of them. I am not prepared to deny that the Chillesford beds, and therefore also the Norwich Crag, may be a local modification of these sands; but I

* Prestwich, Quart. Journ. Geol. Soc. vol. x. p. 93, note.

question their bearing any relation to the sands which usually underlie the Boulder-clay, and which Mr. Wood has called "middle drift." Indeed, I believe that he feels that difficulty himself, for he is unable to make a separation between these unproductive sands and the phosphatic nodule-band, and yet he evidently shrinks from dissociating that peculiar band from the general deposit of the Red Crag. He says, "I incline strongly to a belief that this horizontal Crag is merely the redeposit of the material of the Red Crag beach, washed up on the submergence of the Crag beneath the middle-drift sea;" though further on he adds, "but in the case of the horizontal Crag or nodule-band, this dissociation"-of the nodule-band from the Red Crag-" seems difficult to arrive at”*.

My own impression is that the mass of sands met with between the Boulder-clay and the Red Crag belongs to several deposits of different ages. The unproductive sands of the Crag, which are of a peculiar unctuous character, are one deposit. The laminated brown and yellow sands seen, for instance, about Aldringham Common, in which I found Mytili abundant, are another, and I suspect belong to the "laminated beds" of Mr. Gunn, which underlie the Norfolk Till. We have still a third deposit of sand in the "middle drift," overlying these, and containing those beds of rounded pebbles which have contributed chiefly to form the beach of the Suffolk coast.

I believe that all these sands may be seen emerging from beneath the Boulder-clay in the interval between Westerfield and Bealings stations on the East Suffolk railway.

* Remarks, &c., pp. 5 & 6.

OF

THE GEOLOGICAL SOCIETY.

POSTPONED PAPER.

On the CARBONIFEROUS ROCKS of the VALLEY of KASHMERE. By Capt. H. GODWIN-AUSTEN. With NOTES on the BRACHIOPODA collected by Capt. GODWIN-AUSTEN in THIBET and KASHMERE, by T. DAVIDSON, Esq., F.R.S., F.G.S.

[Communicated by R. A. C. Godwin-Austen, Esq., F.R.S., For. Sec. G.S.]

(Read partly on May 25, 1864, and partly on June 21, 1865*.)

THE district or Pergunah of Vihi is situated on the right bank of the Jhelum, above Srinagar, and is bounded on the N.W. by Zebanwan (8813 feet), on the S.E. by Wasterwan.

The rough panoramic sketch (fig. 2) of the hills which surround this valley, as seen from the line of the river looking east, indicate the positions of the several places at which the following sections were taken. The distance from Zéwan to Reshpur is about 8 miles. The level plain consists of the lacustrine and alluvial deposits of the Kashmere valley, through which the streams from the hills have cut deep courses. The Jhelum flows between high banks of the same formation.

Everywhere, both in Kashmere and Thibet, a Palæozoic series underlies the Mesozoic formations. The age of the Palæozoic rocks is that of the Carboniferous series of Europe, but as yet fossils have not occurred to enable me to distinguish any formations of older date. As, however, Lower Silurian fossils from the Khyber Hills were found by Dr. Falconer in the gravel of the Cabul River, as also by Colonel Strachey on the Niti Pass, the great masses of slaty and metamorphosed rocks, which in this part of the Himalayan chain underlie the Carboniferous beds, may be referred to a Lower Palaozoic series.

The Carboniferous formation may be traced all along the range of mountains on the north side of the Kashmere valley, where, in conjunction with Dr. Vercher, I met with its characteristic fossils in great abundance.

Fig. 3 is a section along a spur from Wasterwan, between Barus and Reshpur, in a direction from S. to N. At the base are the metamorphosed hornblende-slates of Wasterwan Peak. Next comes the quartz-rock, followed by beds of limestone (fig. 3, p. 31).

Beyond Zéwan, to the east, near Khoonmoo, is an outlying or projecting spur of limestone(fig. 4); the strike is S.W. N.E., and the dip. 30° S.E.

*For the abstracts of these communications already published, and for the other communications read at these evening-meetings, see Quart. Journ. Geol. Soc. vol. xx. p. 383, and vol. xxi. p. 492.