California Academy of Sciences RECEIVED BY PURCHASE 23179 La} LY . NF il ‘L ' ; MI ( } ra uN by ‘3 \ \ Ke. i UNG tba AVY . ce aly Digitized by the Internet Archive — ee In 2011 with funding from te California Academy of Sciences Librar my ty ‘fe ' ‘ 14g cy TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. SECOND SERIES. VOLUME IV. Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque iis uti, sed ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientinarum filii, nobis (si videbitur) se adjungant. Novum Organum, Prefatio. LONDON: PRINTED BY RICHARD TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1836. a) = ‘ A sl ee 6 OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY OF LONDON. 1835. PRESIDENT. CHARLES LYELL, Jun., Esq. M.A. F.R.S. & FLL.S. VICE-PRESIDENTS. Sir PHILIP DE MALPAS GREY EGERTON, EDWARD TURNER, M.D. F.R.S. L.& E. Pro- Bart. M.P, F.R.S. fessor of Chemistry in the University of London. RODERICK IMPEY MURCHISON, Esq. F.R.S. HENRY WARBURTON, Esq. M.P. F.R.S. & & F.L.S. F.L.S. SECRETARIES. WILLIAM JOHN HAMILTON, Esq. | WOODBINE PARISH, Jun., Esq. F.R.S. FOREIGN SECRETARY. HENRY THOMAS DE LA BECHE, Esq. F.R.S. & F.L.S. TREASURER. JOHN TAYLOR, Esq. F.R.S. COUNCIL. GEORGE WILLIAM AYLMER, Esq. GEORGE BELLAS GREENOUGH, Esq. F.R.S. FRANCIS BAILY, Esq. F.R.S. & F.L.S. & F.L.S. ARTHUR K. BARCLAY, Esq. HENRY HALLAM, Esq. F.R.S. WILLIAM JOHN BRODERIP, Esq. F.R.S. & JOHN FORBES ROYLE, Esq. F.L.S. F.L.S. Rev. ADAM SEDGWICK, Woodwardian Professor Rey. WILLIAM BUCKLAND, D.D. F.R.S. & in the University of Cambridge, F.R.S, & F.L.S. F.L.S., Professor of Mineralogy and Geology in Lieut.-Col. W. H. SYKES, F.R.S. & F.L.S. the University of Oxford. JOHN HENRY VIVIAN, Esq. M.P. F.R.S. WILLIAM HENRY FITTON, M.D. F.R.S. & Sir RICHARD VYVYAN, Bart. M.P. F.R.S. F.L.S. Rev. JAMES YATES, F.L.S. CURATOR anv LIBRARIAN. WILLIAM LONSDALE, Esq. ADVERTISEMENT. THE Editors of the Transactions of the Geological Society ari directed to make it known to the Public, that the Authors alone are respon- sible for the facts and opinions contained in their respective papers. It is requested that all letters and communications to the Secretaries, and presents to the Society, may be addressed to the Apartments of the Geological Society, Somerset House, London. OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY OF LONDON. 1836. PRESIDENT. CHARLES LYELL, Jun., Esq. M.A. F.R.S. F.L.S. VICE-PRESIDENTS. Rey. WILLIAM BUCKLAND, D.D. F.R.S. GEORGE BELLAS GREENOUGH, Esq. F.R.S. F.L.S., Professor of Mineralogy and Geology in F.L.S. the University of Oxford. EDWARD TURNER, M.D. F.R.S. L.& E. Pro- Sir PHILIP DE MALPAS GREY EGERTON, fessor of Chemistry in the University of London. Bart. M.P. F.R.S. SECRETARIES. WILLIAM JOHN HAMILTON, Esq. | WOODBINE PARISH, Jun., Esq. F.R.S. FOREIGN SECRETARY. HENRY THOMAS DE LA BECHE, Esq. F.R.S. F.L.S. TREASURER. JOHN TAYLOR, Esq. F.R.S. COUNCIL. FRANCIS BAILY, Esq. V. P. & Treas. R.S. F.L.S. Viscount OXMANTOWN, F.R.S. WILLIAM JOHN BRODERIP, Esq. F.R.S. JOHN FORBES ROYLE, Esq. F.L.S. F.L.S, Rev. ADAM SEDGWICK, Woodwardian Professor WILLIAM CLIFT, Esq. F.R.S. in the University of Cambridge, F.R.S. F.L.S. Sir ALEXANDER CRICHTON, M.D. F.R.S. Lieut.-Col. WILLIAM HENRY SYKES, F.R.S. WILLIAM HENRY FITTON, M.D. F.R.S. F.L.S. F.L.S. HENRY WARBURTON, Esq. M.P. F.R.S. HENRY HALLAM, Esq. F.R.S. F.L.S. ROBERT HUTTON, Esq. Rev. WILLIAM WHEWELL, F.R.S. F.L.S. RODERICK IMPEY MURCHISON, Esq. V.P.R.S. F.L.S. CURATOR anv LIBRARIAN. WILLIAM LONSDALE, Esq. ADVERTISEMENT. THE Editors of the Transactions of the Geological Society are directed to make it known to the Public, that the Authors alone are respon- sible for the facts and opinions contained in their respective papers. It is requested that all letters and communications to the Secretaries, and presents to the Society, may be addressed to the “Apartments of the “ Geological Society, Somerset House, London.” CONTENTS. PART I. I. On the Geology of the Neighbourhood of Weymouth and the adjacent Parts of the Coast of Dorset. By the Rev. William Buckland, D.D. F.G.S. F.R.S. (Professor of Geology and Mineralogy in the University of Ox- Jord), and Henry Thomas De la Beche, Esq. F.G.S. F.R.S. §c. . p. 1 II. Introduction to the General Structure of the Cumbrian Mountains ; with a Description of the great Dislocations by which they have been sepa- rated from the neighbouring Carboniferous Chains. By the Rev. Adam Sedgwick, V.P.G.S. F.R.S. §c. (Woodwardian Professor in the Uni- versity of Cambridge) . : - ; ; 4 : : p. 47 Ill. Description of a Series of Longitudinal and Transverse Sections through a Portion of the Carboniferous Chain, between Penigent and Kirkby Stephen. By the Rev. Adam Sedgwick, V.P.G.S. F.R.S. $c. (Wood- wardian Professor in the University of Cambridge) : 3 : p. 69 PART II. IV. Observations on some of the Strata between the Chalk and the Oxford Oolite in the South-east of England. By William Henry Fitton, M.D. P.G.S. FLRS. §c. . ; . ° 2 p- 103 V. Zoological Observations on a New Fossil user of Chine from Cningen. By Thomas Bell, Esq. F.G.S. F.R.S. 5 ; . p. 379 VI. On the new Red Sandstone Series in the Basin of the Eden, and north- western Coasts of Cumberland and Lancashire. By the Rev. Adam Sedgwick, V.P.G.S. F. RS. §c. (Woodwardian Professor in the Uni- versity of Cambridge) . . : : : : : p. 383 VII. On a Portion of Dukhun, East Indies. By Lieut.-Colonel William Henry Sykes, /.G.S. F.RS. FDS. . : : : - p- 409 VII. On the Geology of the Environs of Bonn. By Leonard Horner, Esq. PIGS, NSS. bg E, . « . : 5 Pe ails : p. 433 vi CONTENTS. Index : : 2 - A 5 : , : : : ; ‘ p- 483 A List of Donations to the Library, to the Collection of Maps, Plans, Sections, and Models, and to the Museum; from the Close of the 26th Session in June, 1833, to the Close of the 29th Session in June 1836. Explanation of the Plates. Plates and Maps to the Volume. *.* The Binder is directed to place the Lists of Officers and Council immediately after the Title Page, in the order of their Dates ; and he is to place Plate X. b. before Plate X. a., that both may fold out, and be examined at the same time. ERRATA er CORRIGENDA. Page106, line 5, for No. 1.) illustrates read No. 1. and X. b. fig. 1. illustrate ——107, — 17, after No. 1. insert and Plate X. b. fig. 1. o —— 108, Note*, for Section, Plate X.a. No, 1. read Sections, Plate X.a. No. 1. and X. b. fig. 1. — 11], line 3 from bottom, for at read from — 112, — 23, for subcristatus read cristatus ; and add Plate XI. fig. 23.—See Appen- dix A. p. 337. 15, for Hamites aculeatus read Ha- mites spiniger 9 from bottom, add the words also at Blackdown, Devon, Plate XVIII. p. 242. 9 from bottom, for Siphonaria, read Si- phonia — 130, — 20, for XXI. f. 7. read XXIII. fig. 7. —— 131, — 14, for Trochus, read Pleurotomaria —— 188, The thickness of the beds represented in the Wood-cut differs in some respects from those of the List, p.139; the latter are the more correct. —— 143, line 22, dele is — ih See 11D. —— 153, — 3, for striata read gigantea —— 164, — 3, for fig. 2. read fig. 3. — — — 4, for No. 5. read No. 6. — 167, — 11 from bottom, for (b.) read (@.) —— — — 9 from bottom, for (b.) read (@.) — — — 9 from bottom, for fluviorum read vivi- para —— 168, — 1, for (2.b.and 2. e.) read 2. B. and 2. ¢. 8, for 12 read 10? — 11, for 2. a. read 2. a. —— — last line, add p. 186, read (95.) p. 186. —— 181, line 15, fe ppiuetond read Peppingford- ar —— — — 21, for Odontopteris read Sphenopteris —— 182, — 13 from bottom, for No. 6. read No. 7. —— 195, — 14, 15, 17, from bottom, for Gryphea read Exogyra —— 203, — 3, for Seligrimus read Selliguinus —— 204, — 2, insert“ Anomiaconvexa. Plate XIV. fig.7. Shore East of Shanklin Chine. See p. 338.” 25, after Ostrea carinata insert ‘‘ Ostrea retusa, Plate XIV. fig. 4.; from Atherfield, in the Lower green- sand.” — 214, last line, for VIII. read IX. —— 225, line 14, dele and —— 230, — 9, for XX. read XXII. Page 231, line 24, for tricristata read triserrata —— 234, — 6, after thus: insert “ (see Plate X. a. No. 11, and X. b. fig. 9.)” a eee | for Stutchburiensis read Stutchburianus 342, — 2, from bottom, and Descript. of PI. X VIII.fig.1. 242, — 9, first column, for megastrema read megatrema —— — — 5, secondcolumn, add the words ‘“‘also from Eastware Bay, in Kent; see p. 114, line 32.” —— 252, — 15, for 4 feet to 7 feet read 4 to7 — 259, — 19, for in read or — 260, — 8, for Berston read Benston —— 262, — 26, for South read North —.— — 382, for between Gin Cross read from Gore Cross —— 273, — 6 from bottom, for Aptychus read Trigonellites —— 292, — 23 and 30, for Aptychus read Trigo- nellites —— 297, — 10 from bottom, dele the semicolon after suboolitic —— 298, — 20, for Potamides carinatum read Pota- mides? (a new species.) —— 300, — 5 from bottom, for 286 read 206 —— 302, — 19, for Aptychus (Von Meyer),—read ‘* Trigonellites,(Parkinson); Ichthy- osiagones, (Riippell); Aptychus, (Von Meyer.)” — 303, — 5, for 206. read 286. —— 304, — 16 from bottom, for masses read matter — — — 24, for masses read matter — 305, — 9, dele the word “ chalk” — 309, — 4, note }, for R.C. read C. B. —— 316, — 6 from bottom, for Aptychus read Tri- gonellites —— 324, — 8, for (168.) p. 326. read (167.) and (168.) pp. 326. and 329. —— 339, — 9, for gigantea read striata — 352, Inthe reference connected with Pentacri- nites scalaris, for fig. 2. read fig. 4. Tables 353, After Gastrochena, insert ‘“ sp. doubtful.— In perforations in dicotyledonous (silicified) wood ;—Gault, east of Folkstone.” — 355, In the reference Cytherea subrotunda, for Pl. XXII. 2. read Plate XVII. 2. 355, After Cyclas media insert “ C media, a gibbose variety, Pl. X XI. fig. 11. (Hastings-said; Sussex, 177.—Pur- beck strata; S. Wilts, 259.}” — 358, note, dele ?? after the word adjective ¥ ay ups "se } iol ie tniones +h; Li saa i Whee Oe ae ty Wie Bins aes “i 72a ole eh Ta eels sik = (| sSRPRE Wiss of? epg ine ae pe m ? + le [ ea 2 ¢ ° 3 at Wee sees asta! yea woth Mhoedlh eget Y i iF MS ee Ae y Be ‘a. a Fas ae | a ot Pale ‘ar Tg eT ee 2 ‘ ' “ ; 1 | Lap See ‘he OM ey aby ae “| eet a ia Vie ee =) 0 ally Se velia talaaeel aa ry ae +6 deer Ie ee ony st vet Tae Pee. aged roar ‘ J i teed mee ate AK ig 3 ‘ } I t : I.—On the Geology of the Neighbourhood of Weymouth and the adjacent Parts of the Coast of Dorset. By tue Rev. W. BUCKLAND, D.D. F.G.S. F.R:S. (PROFESSOR OF GEOLOGY AND MINERALOGY IN THE UNIVERSITY OF OXFORD.) Ano H. T. De ra BECHE, Ese. F.G.S. F.R.S. &e. [Read April 2 and 16, 1830. ] FEW parts of the world present in a small compass so instructive a series of geological pheenomena as those which are displayed in the vertical cliffs of the south coast of England. An important portion of this coast, including the Isle of Wight and the Isle of Purbeck, has been well described by Mr. Webster*, and subsequently illustrated by Dr. Fitton+. In the Second Series of the Geological Transactionst, Mr. De la Beche has published sections of the coast from Bridport Harbour to Sidmouth; and in the same volume Dr. Buckland has given drawings of the cliffs from Sidmouth to Beer Head, and from Lyme Regis to the Isle of Portland§. The geological history of the neighbourhood of Weymouth has been partially illustrated by Prof. Sedgwick in the Annals of Philosophy || ; and it will be the object of this paper to supply its full details, illustrated by a map and sections ; beginning our observations at the point where Mr. Webster’s sections end, viz., at the Pro- montory of White Nore, about eight miles E.N.E. of the town of Weymouth, and continuing them to Weymouth and Portland, and thence westward along the Chesil Bank to the cliffs west of Lyme Regis. To our representations of the coast we shall add many inland sections of the adjacent district, including all the strata which occupy that portion of the south frontier of the county of Dorset which lies between the great south * See Sir H. Englefield’s History of the Isle of Wight; the Geological Transactions, First Series, vol. ii. p. 161—254; and Second Series, vol. ii. Part 1. p. 37 —44: also Annals of Philo- sophy, vol. xxv. p. 33—51. + Annals of Philosophy, Nov. 1824, vol. Ixiv. p. 376. t Geological Transactions, Second Series, vol. i. Part I. Pl. VIII. § Ibid. Plate XIV. || Annals of Philosophy, 1826, vol. xxvii. p. 346. VOL. IV.— SECOND SERIES. B 2 Prof. Bucktanp and Mr. De ta Becue on the escarpment of the chalk downs and the sea. We shall designate this tract by the general appellation of the Weymouth District: it is a tract of no small importance in the geological history of England :— 1. From its position near the south-western termination of several principal formations of this island, including tertiary strata, chalk, greensand, Purbeck and Portland beds, several members of the oolite formation, and lias. 2. As exhibiting a coast section which forms an interesting object of com- parison with the north-eastern terminations of the same strata on the coast of Yorkshire, which have recently been so well described by Mr. Phillips*, and with their appearance across the Channel on the coast of Normandy, the details of which have been described by Mr. De la Beche in the Geological Transactionst, and subsequently by M. de Caumont in his Essay on the Department of Calvados tf. 3. As affording remarkable examples of violent disturbances which have affected all these strata since the period of their consolidation ; producing elevations, depressions, fractures, and denudations, connected and continuous with those which have operated so extensively in Purbeck and the Isle of Wight, and through the wealds of Sussex and Kent. We shall take a short review of the general physical features of this district before we enter upon geological details. It will be seen by reference to our map§, which is on the same scale as the Ordnance Survey, that the physical features of the coast are:—I1. On the east a range of high cliffs extending from the chalk of White Nore to the flat marsh lands of Lodmore near Wey- mouth. 2. The marsh lands of Lodmore, divided only by a bank of pebbles from the waters of Weymouth Bay. 3. A low range of cliffs, extending from Weymouth Harbour to Portland Ferry. 4. The remarkable accumulation of pebbles called the Chesil Bank, extending from the northern extremity of Portland about sixteen miles north-westward to Burton Castle, and causing the sea to be separated from the main land along nearly half this district by a backwater called the Fleet. 5. A succession of cliffs rising gradually from Bur- ton towards the west till they attain their highest elevation of about 600 feet in the summit of the Golden Cap Hill, between Bridport and Charmouth. The physical features of the interior divide it into two distinct compart- ments, which we shall call the Vale of Weymouth and the Vale of Bredy. The Vale of Bredy is bounded on the north and east by lofty escarpments of * Tllustrations of the Geology of Yorkshire, by John Phillips, Esq. F.G.S. York, 1829. + Geological Transactions, Second Series, vol. i. Part I. p. 40—47. t Essai sur la Topographie Géognostique du Département du Calvados, par M. de Caumont. Caen, 1828. § Plate I. ‘‘iakar es a Geology of the Neighbourhood of Weymouth, &c. 3 the chalk downs; on the south by Abbotsbury Castle, and a lower range which slopes from thence continuously to Burton Castle ; on the west it is separated by some hills of moderate elevation from the valley of Bridport. Of the Vale of Weymouth the following are the three most prominent features :— Ist, The lofty escarpment of the Ridgeway which bounds it on the north, running nearly in a straight line about twelve miles from east to west. 2nd, The elevated and inclined plane of limestone which constitutes the Isle of Portland, and terminates this district towards the south. 3rd, Between this elevated Ridgeway and Portland is a space somewhat triangular, composed of an alternation of low and nearly parallel, narrow ridges and narrow valleys, which are terminated successively on the west by the Chesil Bank, and on the east by Portland Road and Weymouth Bay ; these all diminish in Jength successively, as their position is nearer to the south, until the most southerly of them terminates in the sea at Portland Ferry. These ridges and valleys constitute a series of narrow belts, which are crossed nearly at right angles by the road from Dorchester to Weymouth ; we shall therefore designate these belts by the names of the villages that stand upon or nearest to them: thus the names of Upway, Upway Street, Broad- way, Nottington, and Radipole, will indicate five successive belts, composed of five distinct and successive formations; namely, Portland stone, Kimmeridge clay, Oxford oolite, Oxford clay, and forest marble,—all dipping north towards the base of the escarpment of the Ridgeway chalk: nearly in the centre of this belt of forest marble the dip changes suddenly towards the south ; and the same succession of strata is repeated, dipping in an opposite direction southwards, and disposed in corresponding belts, which may be designated by the names of Melcombe, Wyke Regis, Portland Ferry, and Portland Island. The formations superior to the Portland beds, if they exist south of the island, are covered by the sea exterior to the Bill of Portland. At the Race of Portland the agitation of the water is caused by the obstruction which the subjacent mass of Portland stone offers to the tidal currents. The line of section fig. 1,* exhibits the general structure of this district. The forest marble{, with its clays and cornbrash, constituting the lowest strata which rise to the surface, forms a double, central belt, elevated, as Mr. * Plate Al: + The forest marble and cornbrash are so closely united throughout this district, that, except in cases of minute local description, it will be most convenient to include them and their subor- dinate clays under the common appellation of forest marble. B2 4 Prof. Bucktanp and Mr. De ta Becue on the Conybeare has stated*, into the form of an arch or saddle, on each side of which the superior strata repose in corresponding order of succession, having their dips respectively conformable to the north and south dips of the sides of the arch, whilst their direction or line of bearing is nearly east and west, and parallel to the axis of this central arch. Thus, on each side of our axis or anticlinal line of forest marble, the Oxford clay reposes conformably, and constitutes two parallel valleys, which extend from the sea in Weymouth Bay to the Chesil Bank. 'To these succeed two similar parallel ridges of the Oxford oolite formation, which are again overlaid by two parallel belts of Kimmeridge clay, on which are still further superimposed two distinctly cha- racterized deposits of Portland stone; and on the north side only, above the Portland stone we find strata belonging to the Purbeck series, to the green sand, the chalk, and plastic clay. The superficial breadth of the belts on each side of the anticlinal line is in the inverse ratio of their dip; and as this dip is most rapid on the north side, the surface of the northern belts is less broad than that of the corresponding belts on the south side. Having taken this general view of the structure of the coast of Dorset, we will again examine its component parts in a descending order, and point out in regular succession the history and peculiar circumstances of each forma- tion of which it is composed, beginning from the eastern extremity at White Nore, and thus connecting it immediately with the observations of Mr. Webster. Tertiary Deposits.—Plastic Clay, &c. It is well known from the maps of Mr. Webster f and Mr. Greenough {, that the tertiary strata which fill the chalk basin of Hants and Dorset find their western termination about three miles east of Dorchester. Between this ter- mination and the great south-western escarpment of the chalk, there occur in- sulated patches of the same tertiary deposits, and many large blocks of pudding- stone and of gray-wether sandstone, which show that the original limits of the tertiary formations extended far beyond their present outlines, and were pro- bably almost coextensive with the chalk. Thus near Came Down on the Ridge- way about four miles south of Dorchester, we have a deposit of rounded chalk- flint pebbles, resembling the round tertiary gravel of Blackheath, near Lon- * Outlines of the Geology of England and Wales, by the Rev. W. D. Conybeare, F.G.S. &c., and William Phillips, F.G.S. &c., pp. 182, 192. + Geological Transactions, First Series, vol. ii. Plate IX. + Geological Map of England and Wales, by G. B. Greenough, Esq. P. G. S. 1819. Geology of the Neighbourhood of Weymouth, &c. 5 don: and at the summit of Black Down, six miles south-west of Dorchester, which forms the highest hill within our district, we have a considerable series of beds of similar pebbles, sand, brick earth, and plastic clay*, analogous to the outlying fragments of the plastic clay formation which crown many of the highest summits of the downs of Wiltshire and Hampshire, and are described in Dr. Buckland’s paper on Valleys of Elevation f. Upon the high table land of chalk, also, on which this plastic clay of Black Down rests, we have numerous blocks of siliceous pudding-stone, scattered over the surface of the fields, and composed, like that of Hertfordshire, of a congeries of chalk flints imbedded in highly indurated siliceous sand: these blocks also contain occasionally, though rarely, a few angular fragments of chert from the greensand formation, and a few small pebbles of white quartz. The chalk flints which make up the greatest part of their substance are not all rounded, as in the Hertfordshire pudding-stone, but for the most part are angular, as in the case of similar insulated blocks which occur on the hills of greensand near Sidmouth ; and this angular condition deserves peculiar notice, as it seems to connect them with the next deposits we are about to mention, some of which may possibly be referred to the era of the plastic clay formation. In two deep and steep combs excavated in chalk on the west and south of Black Down Hill, viz. at Bride Bottom on the west, and at Por- tisham on the south, these blocks of angular breccia are accumulated as thickly as the gray-wethers in Clatford Bottom, near Kennet, on the Marlborough downs : their abundance in Bride Bottom has caused it to be called the Valley of Stones. This bottom forms the upper extremity of the Vale of Bredy, where it contracts into a deep and narrow comb, at the head of which the blocks are spread over a space of several acres, like a flock of sheep, often so close together that a man may leap successively from one to another of them. On the south side of the plain of Black Down we have another collection of huge blocks of the same breccia in the steep comb which descends the chalk escarpment into the village of Portisham: they are most abundant in the village itself, where they lie so thick that they partly obstruct the street, and when they occur in the line of the houses the walls are built upon them : their extreme hardness and bulk have hitherto prevented their removal or destruction by the hand of man. In the street at West Lulworth, also, similar * These strata supply materials to a manufactory of bricks, tiles, and coarse pottery that is established on this hill. The clay exhibits the same varieties of colour, viz. blood-red, yellow, white, and black, which are so characteristic of the plastic clay formation, and are so well shown in Alum Bay and at Reading. + Geological Transactions, Second Series, vol. ii. Part I., p- 119—130. 6 Prof. Buckianp and Mr. De ta Becue on the blocks of the same stone lie in the line of the tront of some cottages, and are built into the walls. In Dr. Kidd’s Geological Essay, p. 177, a similar col- lection of siliceous boulders is described as scattered over a dry valley, high up on the chalk downs of Berkshire, near Ashdown Park, on the south of Swindon, so thickly as to render the road inconvenient, even to a foot tra- veller. Although these blocks have been entirely separated from the matrix in which they were formed, they are very slightly rolled, and have been drifted but to a small distance from their native place. We think it right to refer to the action of water, probably in more than one period of the tertiary formations, certain deposits of angular gravel which occur on the summits of many hills within our district. A remarkable ex- ample of this kind, composed of an admixture of unrolled chalk flints with yellow clay and sand, is seen in the upper margin of the cliffs at White Nore, where it forms a continuous bed, varying in thickness from two to twenty feet, level at its upper surface, but extremely irregular below, and filling up deep holes and furrows (puts naturelles), which pervade the entire surface of the subjacent chalk. These deposits seem due to the effect of water dissolving the chalky matrix of the flints, but not sufficiently agitated to roll them into pebbles, nor to move them from the spot on which the dissolution of the chalk had taken place. The most instructive example we know of the effects of this dissolving operation is at Dunscombe Hill, on the east of Sidmouth, where, on the summit of a ridge of chalk, of which the surface is furrowed with pits and hollows that are evidently due to the action of water, we find an unstratified mass of chalk flints, which have not undergone the slightest rolling, piled on each other, and intermixed with Joose sand and clay; the outer portions of this mass, from which the rain has washed away the sand and clay, lie loose and hollow, like stones in an artificial barrow, or in a wall constructed without mortar. It is scarcely possible to explain the actual state and position of these flints but by supposing that the chalk in which they were formed has been gradually dissolved in a quiet sea. To the same operation of quiet solution we must also refer analogous deposits of angular chalk flints and yellow clay which fill the irregular and deep troughs and hollows that fringe the upper margin of the chalk in the cliffs from Lyme to Axmouth, in a manner similar to that we have described at White Nore. Cavities and projections of this kind appear to be universal on the surface of the chalk wherever it is covered up with any kind of tertiary strata, and has been protected by them from the levelling effects of atmospheric agents ; in all these cases the actual surface of the land affords no indications of the Geology of the Neighbourhood of Weymouth, &c. 7 irregularities which exist below: but however rugged be the subjacent surface of the chalk, its irregularities are all obliterated and filled up with breccias and gravel beds, presenting on their upper surface a smooth and continuous outline, whilst their lower surface is curved and dentated downwards, con- formably to the furrowed curvatures, and ridges and pinnacles that fringe the upper surface of the chalk on which they rest; the existence of these pits and cavities shows, that the chalk had not been exposed to the levelling effects of atmospheric agents before the deposition of these breccias and gravel beds. The water which formed these breccias must have been subject to very irre- gular currents and agitations ; for whilst in many places (such as those last mentioned) the solution has been conducted in perfect tranquillity, in other spots it has been attended or followed by agitations which have reduced the flints to perfect roundness, as in the Hertfordshire pudding-stone and Black- heath gravel; and again, in other cases, there is evidence of an intermediate state of action, where only a partial rounding of the fragments has taken place, as in the partly rounded and partly angular chalk flints which form a thick bed reposing on strata of greensand on the summit of Haldon, on the west of Exeter. Another variety of angular gravel occurs in many beds of shivered chert of the greensand formation, which seem to have undergone a certain degree of decomposition, causing them entirely to break to pieces and crack into angular fragments, and become converted into strata of loose and shivered gravel, on which no mechanical attrition seems to have been produced by the operation of water, but the fractures have resulted from the splitting to pieces of the beds of chert still resting in their natural position. A remarkable example of this kind may be seen in the cliffs that overhang the new road between Lyme and Charmouth, and also on the summit of Abbotsbury Castle. In the oolite formation also, about two miles west of Bridport, a similar dislo- cation and splitting of the stone has converted to loose breccia the upper beds of inferior oolite on part of the summit of Chideock Hill. This is the only case we have noticed of such an occurrence in the oolite of the coast of Dorset. It is not easy to distinguish between these undisturbed beds of shivered chert, and accumulations of the same chert which have been very slightly agitated by water, except in cases where the admixture of miscellaneous fragments of other strata shows that moving water has operated in bringing these frag- ments to their present position amongst the chert. There is also a difficulty in distinguishing the deposits of angular breccia, both of this chert and of the chalk formation, from deposits of diluvial gravel which have been removed. 8 Prof. Bucktanp and Mr. De 1a Becue on the to a small distance only from their native place. The cliffs at Axmouth and near Sidmouth exhibit deposits of such miscellaneous diluvial gravel, resting on red marl, and adjacent to beds of uniform and angular chalk-flint breccia that rest on the chalk. These deposits of breccia on the coast of Dorset seem analogous to those which are found in Normandy, reposing on the similarly corroded surfaces of the chalk, and which occur also on the surface of other formations in that part of France, each formation respectively being often covered with a cap- ping of loose angular fragments composed of the hardest materials of the sub- jacent strata. According to M. de Caumont, a breccia allied to the plastic clay formation, and composed of angular chalk flints imbedded in red clay, occasionally attaining the thickness of 80 and 100 feet, occurs in the valley of the Rille, and various adjacent parts of Normandy*. M. de Caumont speaks of all these breccias under the head of Diluvium,—falling into the same common error with many other Continental geologists, of including under the term Diluvium many pebble beds and breccias which belong to the tertiary, and to older formations. Chalk. The lofty escarpment of chalk which bounds our field of observation on the north, forms the margin of the chalk downs of the southern part of Dor- setshire, and is the direct continuation of the south frontier of the great chalk basin of Dorset and Hants. Along great part of this south frontier, from the east extremity of the Isle of Wight to the west extremity of Purbeck, and thence to the cliffs of White Nore, where we euter on its history, Mr. Web- ster has shown its position to be sometimes absolutely vertical, but for the most part dipping at a very high angle northwards towards the interior of the basin f. This high inclination ceases a little east of the promontory of White Nore, where the chalk suddenly sweeps round, and dips at an angle of a few degrees only to the north-east. Along the range of its escarpment westward, for nearly twenty miles from White Nore to its termination at Chilcomb Hill, on the east of Bridport, the dip is almost constantly towards the north, at angles varying from 10° to 40°. Its mean elevation along all this range may be taken at about 500 feet. The base of this escarpment appears throughout to be * See sections and description in M. de Caumont's Essai sur la Topographie Géognostique du Calvados ; and De la Beche on the Geology of the North Coast of France, from Fecamp to St. Vaast, in Geol. Trans. Second Series, vol. i. Part I. p. 73—89. + See Sir Henry Englefield’s History of the Isle of Wight, Plate 50; and the Geological Transactions, First Series, vol. i1. Plate XI. Geology of the Neighbourhood of Weymouth, &c. 9 composed of beds of the greensand formation ; but these are rendered invi- sible in the greater part of the Weymouth district, in consequence of a fault which runs along the escarpment for nearly ten miles, from Poxwell to Abbots- bury, and brings up strata, subjacent to the greensand, into immediate contact with the chalk: this fault we shall hereafter describe. The promontory of White Nore is the last point in the South-west of Eng- Jand at which the great bedy of the chalk touches the sea; those insulated por- tions of this formation which occur in the cliffs between Lyme and Sidmouth being only detached outlying masses, separated, by denudations of many miles in width, from the south-west termination of the great chalk basin of Dorset- shire*. The mineralogical character and organic remains of the chalk in this district present nothing unusual: the lower strata of the chalk pass into hard chalk, devoid of flints, and interspersed irregularly with green grains of sili- cate of iron. Greensand. The strata of the greensand formation, which at White Nore emerge from beneath the lowest chalk, dip conformably with it to the north-east, and attain a thickness of about 100 feet: their succession in a descending order is:—1. Chalky glauconite, composed of greensand interspersed with cal- careous cement. 2. Green, yellow, and brown sand, alternating with irre- gular calcareous concretions, and with thick beds of chert. 3. Dark argil- laceous greensand, with large nodular concretions, equivalent to the sandy concretions called cow-stone, at Lyme Regis: the upper subdivisions of this section also closely resemble some of those exhibited by the greensand for- mation near Lyme. We are unable to recognise distinctly in this district, or in any part of the coast west of Weymouth, those regular and extensive threefold subdivisions of fire-stone, gault, and lower greensand, which are so obvious in Hants, Sussex, and Kent; although an approximation to the character of fire-stone may be traced at White Nore, and still more decidedly in Devonshire, in the cliff and quarries of Beer already described by Mr. De la Bechet. For a considerable distance near White Nore and Osmington the green- sand is visible at the base of the chalk escarpments, dipping always conform- ably to the chalk; but along the great escarpment from Poxwell to Abbotsbury it is seen only in two places, namely, near Sutton Pointz, and at Bincombe, being elsewhere masked by the Portland stone, which the great fault that * See Map, Plate I. + Geological Transactions, Second Series, vol. ii. p. 109. VOL, IV.—SECOND SERIES. C 10 Prof. Buckianp and Mr. Dre 1a Becue on the runs along this escarpment brings up into absolute contact with the chalk. At these two places, however, its thickness is so great as to leave little doubt that it continues in its proper place beneath the chalk, to the west extremity of the fault near Abbotsbury, where it is again exposed, and forms a con- siderable feature in the escarpment of White Hill, overhanging the village of Abbotsbury, and projecting thence nearly two miles westward into the summit of the long and elevated ridge of Abbotsbury Castle. From Abbots- bury Castle it turns northward, still forming the sub-escarpment of the chalk, along the entire east and north frontier of the Vale of Bredy. It ap- pears also on the summit of Swyre Knoll, Hammerdon Hill, and Shipton Beacon, which form three remarkable outlying hills on the flanks of the Vale of Bredy, and in much greater force on the summits of the insulated hills of Golden Cap, Hadden Hill, Stonebarrow Hill, Coneygore, and Conig Castle near Charmouth ; and further north, on the lofty tops of Lewsdon Hill, Pillesdon Hill, and Black Down near Broadwindsor*. In the escarpment on the north of Abbotsbury we have a distinct section, displaying ledges of hard coarse limestone, loaded with grains of quartz and silicate of iron, and alter- nating with thick strata of chert; a little further west, at Abbotsbury Castle, the calcareous matter ceases, and is replaced by strata of chert. These cal- careous and cherty strata of the greensand at Abbotsbury, afford an interest- ing object of comparison with those in the neighbourhood of Lyme Regis, described by Mr. De la Beche f, as well as with those at White Nore. The occasional presence of so much calcareous matter in the greensand, seems to justify the appellation of crate chloritée, given by the French to the upper- most strata of the greensand formation. The greensand in our Weymouth district is found to overlie and repose successively on formations of different ages; thus, in the valley of Upton on the east of Osmington it rests on the Purbeck bedst ; in the south escarpment of Upton Hill towards Ringstead Bay, on Portland stone$ ; on the west of Osmington Mill, on Kimmeridge clay||; at Abbotsbury Common, on a clay which is probably the Oxford clay; at Golden Cap Hill, on inferior oolite**; near Lyme Regis, upon lias++; and at Axmouth and Beer, upon red marltt. The same overlapping disposition of the greensand has been ob- * See Map, Plate I. t Geological Transactions, Second Series, vol. ii. pp. 109, &c. + See Plate Il. fig. 2 & 3. § See Plate II. fig. 2. || See Plate ITI. fig. 9. G See Plate II. fig. 6 & 7. ** Geological Transactions, Second Series, vol. i. Part I. Plate VIII. and Plate XIV. No.1. In these sections the inferior oolite was omitted by mistake, but is inserted in a section of the same coast, in Pl. III. of Mr. De la Beche’s Sections and Views Illustrative of Geological Pheenomena. tt Ibid. Plate VIII. tt Ibid. Plate XIV. No. 2. Geology of the Neighbourhood of Weymouth, &c. 11 served by Mr. De la Beche* and M. de Caumont in Normandyf, where it overlaps successively the formations of Kimmeridge clay, coral rag, and Ox- ford clay. This circumstance derives an additional importance, at the present time, from the recent paper of M. Elie de Beaumontf, in which he observes that a connexion exists between the elevation of mountains and succeeding deposits of extensive overlapping strata, e. g. the greensand and chalk in the Jura mountains, filling the longitudinal valleys produced by the elevation of the oolites. On the coast of Dorsetshire no elevation of the strata appears to have taken place between the deposition of the lias and the plastic clay. Hastings Sand, and Purbeck Beds. Although the Wealden or Hastings sands do not enter the area of our actual observation, they approach very near to its eastern extremity, becoming gradually thinner in their progress westward through the Isle of Purbeck, until they terminate a little west of Lulworth: this has been already pointed out by Dr. Fitton and Mr. Webster$. The identity of this Hastings sand with that of Swanwich Bay, at the east extremity of Purbeck, has recently been further confirmed by the Rev. T. O. Bartlett’s discovery of the remains of the Iguanodon and other reptiles in the iron sandstone at Swanwich. Bones of this animal have also been recog- nised by Prof. Buckland and by Mr. Vine in the same sandstone at Sandown Fort, and other places on the south coast of the Isle of Wight. The Purbeck beds enter our district on the north-west of White Nore, but are seen only in two small insulated patches near the villages of Osmington and Upway. The details of the beds composing the Purbeck series are so fully given by Mr. Webster ||, that it is here superfluous for us to say anything respecting them, further than that several of their most remarkable varieties are recognised and wrought even to their final termination on the west of Upway. We trace also throughout this district the remarkable beds of fi- brous carbonate of lime that pervade the clay which alternates with the beds of limestone throughout the Isle of Purbeck. The fibres of this limestone, like those of satin spar, are at right angles to the planes of the beds which they compose, and which vary from two to six inches in thickness. From the resemblance of its small and parallel fibres to the fibres of animal muscle, this limestone is known among the workmen by the name of “Beef”: it * Geol. Trans. Second Series, vol. i. Part I. Pl. X. { Essai sur le Top. Geog. Pl. VI. t Ann. des Sciences Nat. vol. xvii. Sept. 1829. § Annals of Philosophy, 1824, New Series, vol. viii. p. 382: also Sir H. Englefield’s History of the Isle of Wight, p. 194. || Geological Transactions, Second Series, vol. ii. p. 36. c 2 12 Prof. Bucktanp and Mr. De ta Becue on the sometimes entirely occupies the place of the clay between the limestone beds of this formation. One of the most important points in the geological history of the Purbeck series, is the occurrence ofa bed of oyster-shells called the “cinder bed,” often many feet in thickness, and almost wholly composed of dark- coloured, small oyster-shells in the midst of a series of strata, some of which contain exclusively shells of freshwater formation, and others an admixture of freshwater shells with those which are marine: this circumstance has been duly noticed by Mr. Webster and Dr. Fitton ; and although we cannot infer from it the return of the sea for any long period in the middle of the Purbeck for- mation, yet it shows that the district it occupies could not have been a lake of pure fresh water, but was probably an estuary at the time when these oysters occupied its bottom, and were accumulated to the thickness of many feet over a distance of many miles*. We are disposed to agree with Mr. Webster, and to adopt more confidently than he has done the opinion he advances with respect to the propriety of referring to the lower region of the Purbeck series the beds of white cal- careous slate, usually destitute of organic remains, which occur between the undoubted Purbeck beds and the Portland stone; these beds resemble the compact varieties of Purbeck stone, which are devoid of shells, and which near Lulworth attain a thickness of from 60 to 100 feet. In Portland the * The following description of the actual state of the lake Menzalé at the mouth of the Nile, by a modern traveller, is highly illustrative of the mode in which living animals of a mixed character are associated together near the confluence of great rivers with the sea. “The lake Menzalé is only five miles distant from Damietta. I should judge it to be sixty-five miles long, and fifteen broad: it is not, properly speaking, a maritime lake, but formed by the increase of the Damietta branch of the Nile; the depth is from three to five feet, and on pushing an oar to the bottom I have observed it coated with the common mud of the Nile for about twenty inches deep. Along all the length of the lake a narrow tongue of land separates it from the sea, but not wholly: there are four passages through which it is possible for barks to sail; through two of them I passed with a good deal of difficulty. At the mouth of each there is a bar of sand, which makes the passage perilous from the sea. No sea or lake in the world can perhaps boast of the same quantity of fish in a given space as the lake of Menzalé. “‘The principal sorts of fish caught here are the Perca Luth, or Lot’s perch; another species called kescher ; the charamoot or Stilurus anguillaris,—the fin is said to be poisonous; the burra, or red mullet; the kelp el bahr, or sea-dog; the casheff, or Mormyrus anguilloides of Linnzeus ; this I have seen weighing thirty pounds. The salmon of the Nile is found in the upper part of Menzalé weighing from 80 to 100 pounds. The mixture of sea and river water in the lake causes it to be neither salt nor sweet ; so that both river and sea fish are to be found here in equal quantity: but both, in my opinion, of an inferior quality. The quantity of birds which cover the lake is pro- digious. Pelicans, cormorants, cranes, and herons live only on the fish.”—Madden’s Travels in Egypt, §c. vol. ii. p. 171—175. Geology of the Neighbourhood of Weymouth, &c. 13 lowest of them form the surface of the island, and cover the true Portland stone with a deposit of freshwater formation. ‘This formation presents beds of chert containing freshwater sheils, near the Ridgeway fault, on the west side of the road from Weymouth to Dorchester ; and also beds of chert con- taining chalcedonic casts of minute freshwater shells, at the water’s edge, on the east side of Lulworth Cove. Section of the Dirt-bed in the Isle of Portland. Calcareous slate. £- os : c| Freshwater formation. re = ——— i a YY sxe a UY sf Ip Mf : Dirt-bed. My sinned lie P i HUM, Ancient forest. Marine formation. We consider a small stratum, called by the workmen “ Dirt-bed,” to be by far the most interesting and remarkable deposit in this district. It seems to be made up of black loam, mixed with the exuviz of tropical plants, accumulated on the spot on which they grew, and preserved during a series of years, in which the surface of the Portland stone had for a time become dry land, and accumulated a soil of about a foot in thickness, composed of an admixture of earth and black vegetable matter, interspersed with slightly rounded frag- ments of stone, which Mr. Webster ascertained to be from the lower part of the Portland series. ‘These fragments are found to be almost coextensive with the dirt-bed, and the fact that we have yet found with them no admix- ture of pebbles derived from the subjacent oolites, or from any other more ancient rocks, shows that no violent rush of water from any distant region took place during the period in which these pebbles of Portland stone were under the process of becoming slightly rounded. This dirt-bed, as Mr. Webster has stated, forms the matrix of the silicified trunks of very large coniferous trees, which are so abundant in the Isle of Port- land, and are found there coextensive with the upper surface of the Portland stone. Wherever the dirt-bed is laid open to extract the subjacent building- stone, it is found to contain these silicified trees laid prostrate, partly sunk into the black earth, and partly covered by the superjacent calcareo-siliceous slate: from this slate the silex, to which the trees are now converted, must 14 Prof. Bucktanp and Mr. De 1a BeEcue on the have been derived. A bed of snow falling on a modern peat-bog, and cover- ing the upper portion of prostrate trees, whose lower portion has been sunk by their weight into the substance of the peat, would represent the position of the calcareous slate which immediately covers these fossil trees in Portland : some of them extend to a length exceeding thirty feet, and bifurcate at their upper end; but the branches are not continuous to their extremities, and we find no traces of leaves. The leaves and small branches, and exterior parts of the trunks, had probably decayed, whilst they lay exposed to air on the surface of the peat. Amid these prostrate trees, many of which attain three and four feet in diameter, we find silicified stems of plants closely resembling the modern Cycas and Zamia: these have been described by Prof. Buck- land under the name of Cycadeoidez*, and are important, as indicating that the temperature in which they grew was much higher than that of our pre- sent climate. We find also, at nearly the same intervals at which trees are found growing in a modern forest, an assemblage of silicified stumps or stools of large trees, with their roots attached to the earth in which they grew. These stumps are from one to three feet long: they are mostly erect, whilst a few are slightly inclined. The black earth which contains their roots seldom exceeds one foot in thickness; the upper portions of the stumps, as represented by Mr. Webstert, project upwards into the substance of the superjacent stone (called “soft Burr’ and “ Aish’’), which gives indication of their presence by hemispherical concretions accumulated around the top of each stump of woodf. Section of the Cliff east of Lulworth Cove. er LE, See Ayreon Soft burr. as YES bas OE Zr Prag Ancient forest in the dirt-bed. Lower Purbeck beds ig Ze, A Te ipritier 4 composed of calca- ee Ae or reous slate of fresh-~ ~ water formation. Portland stone of marine formation. In the highly inclined strata of the cliff, about a furlong east of Lulworth Cove, and represented in the above sketch, we find a considerable number of these silicified stumps, some entirely laid bare by the washing of the sea, others partly exposed and partly covered, and others still wholly encased with * Geological Transactions, Second Series, vol. ii. Part III. p. 395. + Ibid. vol. ii. Part I. Pl. 6. fig. 3, 4. t See wood-cut at p. 13. Geology of the Neighbourhood of Weymouth, &c. 15 concretions of soft burr, and all having their roots fixed in the dirt-bed, which occurs here also of the same thickness, and in precisely the same relative place, and interspersed with the same rounded fragments of limestone which it contains in the Isle of Portland: the position of these stumps, at an angle nearly of 45° to the horizon, affords a striking proof of the elevation which the strata have undergone. We find the dirt-bed also on the top of the Portland stone, in the sections of some quarries along the Ridgeway, e. g. near Upway, on the north of Weymouth, and at the western termination of the Portland stone near Portisham, at the distance of twenty miles west from Lulworth. Dr. Buckland has found slight traces of this dirt-bed on the upper surface of a stratum of Portland stone in the quarries about two miles north of Thame, in Oxfordshire: it is here covered by a few feet of clay, in which he found no other animal remains than fragments of some Testudo, too small to point out the genus to which they belong. The recognition of this very remarkable bed in a locality so distant from Portland seems to indicate that it may be found to be nearly coextensive with the Portland formation throughout England; and it well merits the attention of future observers to search for it in the Vale of Aylesbury, and in the two localities of the Port- land stone intermediate between Oxford and Dorsetshire, namely, at Swindon and Tisbury. The probability of its occurrence at Tisbury is increased by the recent recognition of the Cycadeoidew at this place by Miss Benett*. We consider this dirt-bed as quite decisive in forming the barrier between the Portland and Purbeck formations: its deposition must have proceeded during a considerable period of time, antecedently to which the districts it occupies were entirely submerged beneath the sea, and subsequently to which the waters again returned to overwhelm them, first with a deposit of about 1000 feet of the semi-lacustrine sediments of a great estuary (in- cluding the united thickness of the Purbeck series and the Wealden sands * Dr. Fitton has discovered this deposit on the opposite side of the Channel in the Bou- lonnois, and has thus described it in the Annals of Philosophy, December, 1826. ‘ Some traces of the lowest members of the group to which these two strata (Weald clay and Hastings sand) belong, and which is remarkable from its containing throughout the remains of freshwater shells, are visible on the summit of the cliffs between Gris-nez and Equinen, where a thin bed occurs of somewhat bituminous clay, abounding in silicified wood, the cavities of which are coated with minute crystals of quartz. This bed corresponds precisely to that which exists on the top of the Isle of Portland, bearing there the name of ‘Dirt,’ and abounding in similar wood ; and on the French coast it is associated with beds of limestone, different from the stone beneath, and contain- ing shells in great numbers, apparently of the genera Cyclas and Ampullaria.” Dr. Fitton has also recognised thin fissile beds of Purbeck stone containing freshwater shells, e. g. Cyclas and Cypris, at Whitchurch in Bucks. 16 Prof. Bucktanp and Mr. De 1a Becue on the and clays), and afterwards with a series of marine deposits amounting to much more than 1000 feet of greensand and chalk. Throughout the entire succession of all these changes there is no evidence of any sudden and violent disturbance causing either elevation or depression of the Portland stone, or of the subjacent oolites. The present high incli- nation of all these beds is uniformly parallel to that of the beds of Purbeck stone, greensand, and chalk ; and these all seem to have been raised simul- taneously by the same convulsion which elevated the axis of the Weymouth district, together with all the inclined strata in Purbeck and the Isle of Wight. We have a measure of the duration of the period during which the surface of the Portland stone continued in the state of dry land, covered with forest, in the thickness of the “ Dirt Bed,’ which has accumulated more than a foot of black earth, loaded with the wreck of its vegetation. The regular and uniform preservation of this thin bed of black earth over a distance of so many miles, shows that the change from dry land to the state of a freshwater lake or estuary was not accompanied by any violent denudation or rush of water, since the loose black earth, together with the trees which lay prostrate on its surface, must inevitably have been swept away had any such violent catastrophe then taken place*. * Prof. Henslow in the summer of 1832 found in the top cap of the Portland stone, imme- diately beneath the dirt-bed, root-shaped cavities descending from the bottom of the dirt-bed into the subjacent solid stone ; this top cap should seem, therefore, to have been occupied by the roots of the trees which grew in the dirt-bed, and penetrated the Portland stone whilst it was yet soft and unconsolidated. He also noticed in Portland two partial and very thin seams of black earth; the uppermost at the distance of five feet, and the lowermost of seven feet, below the dirt- bed: these seams of black earth are important, as they mark two short intervals during which vegetable matter had begun to accumulate on the surface of the soft and gradually increasing ma- terials of the uppermost beds of the Portland stone, whilst they were just rising above the level of the sea. The incipient bed of vegetable matter was thus twice interrupted in its progress, and buried beneath an influx, first of two feet, and next of five feet, of earthy sediment, before the general surface on which the true dirt-bed rests had been raised entirely above the water. The above cut represents an example which in the summer of 1832 occurred to Prof. Henslow in the Isle of Portland, in a quarry where the surface of the burr had been laid bare, E49) Geology of the Neighbourhood of Weymouth, &c. 17 Portland Stone. As the details of the component beds and fossils of the Portland series have been sufficiently described by Mr. Webster and Mr. Conybeare, we shall of an erect stump protruding through the burr stone into the superior stratum called Aish, analogous to that represented by Mr. Webster in his section of the Portland beds (Geol. Trans. Second Series, vol. ii. p. 1. Plate VI. fig. 3 and 4.), and which the workmen stated to be of rare occurrence; this superior stratum exhibited to Prof. Henslow two or three of those conical and dome-shaped protuberances which so generally indicate the presence of stumps of trees imme- diately beneath them. In the case represented, the protruding stump being longer than the rest, the burr stone was not deposited in sufficient thickness to cover it, but was heaped around it in two circular ridges, with intermediate circular depressions. From these appearances we may infer that a state of great tranquillity attended the deposition of the calcareous sediment of which the dome-shaped caps that cover the shorter stumps were formed (See Section of the Dirt-bed, page 13.) The circular ridges and depressions which surround the taller stumps (see page 16,) seem to have been produced by an interruption of the undulations on the surface of water so shallow that the waves were caught and broken by a stump but four feet high, whilst they passed over the shorter stools immediately adjacent to them; these interrupted undulations being propa- gated first downwards and then outwards along and around the stump whose top was high enough to obstruct the ripple on the surface of the shallow lake, by which the dirt-bed was gradually inundated. Here, then, we have proofs of a tranquil state and gentle action of water in the period imme- diately succeeding, as well as in that which preceded, the formation of the dirt-bed, upon a sur- face that became dry land during a short time intermediate between the transition of the district which it covers from a submarine state to that of a freshwater lake. The rapid possession which in our modern tropics is taken by the Pandanus or Screw Pine and Cocca-nut Palm of the first banks and reefs of coral islands that emerge above the level of the sea, affords an example of the luxuriant growth of vegetables on the margin of land just rising above the water, analogous to the ancient juxtamarine forest the remains of which contributed to the formation of the dirt-bed, in the region which has now become the southern coast of Dorsetshire. With respect to the silicified trees Prof. Henslow makes the following observations :— “From what I saw I should think that all the erect stumps must have suffered considerable decay before they had become imbedded, or at least fossilized, in the burr. They consisted of no more than the central portion of the wood just above and below the neck of the trees, which had every appearance of having grown in the places which they still occupy. “In a quarry of very white and chalk-like Portland stone, at the base of Chalbury Hill, near Preston, I found a cylindrical mass of flint ten inches in diameter, reposing upon a soot-like mass of carbonaceous matter, probably resulting from the decomposition of leaves and bark, and forming an envelope to the lower part of the cylinder, but not extending beyond it. Upon crack- ing off as much of this cylinder as protruded from the side of the quarry, I perceived the central portions, of three inches in diameter, to consist of fossilized wood. It appears to me most pro- bable that the whole cylinder had occupied the space originally filled by the trunk or branch of a tree; but that during the process of its becoming silicified, the organic structure of the outer portions had not been impressed upon the flint. In the Isle of Portland the quarry-men collect a similar black vegetable substance, which they use for blacking.” VOL. IV.—SECOND SERIES. D 18 Prof. Buckianp and Mr. De 1a BeEcueE on the only refer to their account of them*, and to our own detailed section of Black Nore on the west cliff of the Isle of Portland. We have little to add to what these authors have published, except the occurrence of bones of Saurians which we discovered in the cliff of Black Nore, imbedded in compact Port- land stone. We have stated in our introduction that this district contains two distinct ranges of Portland stone; one constituting the table-land of the Isle of Portland, dipping southwards beneath the sea, and rising with an elevated escarpment northwards towards the bay and valley of Weymouth ; the other constituting a long and narrow line of elevated hills, parallel, and immediately subjacent, to the chalk escarpment of the Ridgeway, and presenting a con- tinuous and lofty escarpment towards the south. In fact, these hills occupy the position which in districts that have been less disturbed is usually held by the sub-escarpments of the greensand formation, where it emerges regularly from beneath the chalk: such are the escarpments of greensand which in Kent and Sussex extend from Folkstone, by Coxheath, Nutfield, and Leith Hill, to Godalming. A glance at our map will show that along the northern frontier of the Vale of Weymouth this ridge of Portland stone forms a con- tinuous band from the east extremity of our district near White Nore to Portisham, where it suddenly terminates in the great fault, and is found no- where further west in England. Along nearly the whole of this tract it attains a high elevation, rising near the central part at least 500 feet into the lofty eminences of Preston Hill, Charlbury, and Bincombe Hill: at these three places its elevation is little less than that of the chalk itself. On the west of Upway it forms a narrow ridge or hog’s back from Upway to Portisham, known by the name of Corton Hill and Waddon, dipping at an angle of about 45° to the north. Although these Portland beds dip thus rapidly to the north, through great part of the range now under consideration, yet such is the dislocation and elevation they have suffered along the line of the great fault, that their northern margin is seldom brought into contact with any other strata than the chalk. On the west of Upway this line of contact is marked by a longitudinal valley, flanked on its north side by the chalk escarpment, and on its south side by the upper Portland strata of Corton Hillt : thus, the Portland beds dipping to the north in Corton Hill, and south along the fault, form a trough in which reposes a long and narrow strip of Purbeck strata, extending more than a mile both on the east and west of Upway, and dipping conformably to the double dip of the subjacent Portland * Geological Transactions, Second Series, vol. ii. p. 37, &c. Outlines of the Geology of En- gland and Wales, p. 172. ¢ Plate III. fig. 3. t{ See Map, Plate I. Geology of the Neighbourhood of Weymouth, &c. 19 stone. The sudden and total disappearance and termination of the Portland formation at Portisham, seems not to result from its accidental intersection at that place by the great Ridgeway fault; but rather from the tendency which is common to this, with most other great formations, to terminate abruptly where they are accumulated to their fullest thickness; thus we find the full thickness of the chalk and oolite formations exhibited for many hundred miles along the line of their great escarpments throughout England, and in like manner the full Portland strata terminate abruptly in the Vale of Weymouth: they reappear and again terminate with equal abruptness in the Vale of Tisbury, and exhibit nearly the same features of sudden termination in the hills near Brill and Thame in Oxfordshire, and near Aylesbury and Whitchurch in Bucks. The fact of the interrupted deposition of the Portland formation in En- gland, occurring as it does only in the limited districts just mentioned, and in one other small spot at Swindon, is analogous to the interrupted deposits of other strata, particularly the most recent members of the oolite formation. We know not the cause of these irregularities ; the fact may be illustrated by the case of the Kimmeridge clay, which attains at Kimmeridge a thickness of 600 feet, is reduced to 70 feet near Oxford, disappears entirely in some places along its line of bearing, and again resumes its strength in the Vale of Pickering, and near the coast of Yorkshire. The Portland stone has not yet been identified on the opposite coast of Normandy, but M. Elie de Beaumont states that he has discovered it in Burgundy*, and M. Dufrénoy says that it occurs largely in the vicinity of Angoulesmeyt. We think it pro- bable that it will soon be recognised among the great calcareous formations of the Alps and Apennines. Portland Sand i The consolidated and calcareous beds of the Portland stone are separated from the Kimmeridge clay by the interposition of a deposit of sand and marly sandstone at least eighty feet thick, exceeding the total thickness of the Portland stone itself. This deposit is coextensive with the Portland stone throughout nearly the whole of the coast of Dorset, and is well exhibited by a vertical section near Black Nore, on the west cliff of the Isle of Portland, and along the west shore from Black Nore to the village of Chesilton. Its pre- vailing character is a siliceous sand, so abundantly mixed with grains of green earth, as to be scarcely distinguishable from the lower strata of the green- sand formation near Lyme and Seaton: it also contains large semicalcareous * Ann. des Sciences Nat., July 1829. + Annales des Mines, 1829, vol. ii. p. 434. i See Pl. IIL. fig. 1. n. 0. and fig. 3. 20 Prof. Bucktanp and Mr. De ta Becue on the concretions resembling the cow-stones in the lower greensand at these two places ; its fossils, however, are different, and more allied to those of the oolite ; and its position beneath the Portland stone is decisive in separating it totally from the greensand formation. We have adopted for this stratum the name of Portland Sand, being that suggested by Dr. Fitton, who had ascertained its relation in the Boulonnais and in Buckinghamshire*. This Portland sand is of sufficient importance to be marked on our map by a distinct colour along nearly the whole extent of the base of all the escarp- ments of Portland stone ; its mineralogical resemblance to the greensand of Lyme may be best seen at Corton, about two miles west of Upway, where nearly one half of its substance is made up of grains of green earth. The following list of fossils from the Portland sand has been prepared by Mr. James Sowerby, from specimens we collected at Black Nore and Chesil- ton, in the Isle of Portland, and at Corton. Black Nore. Serpula plexus, M. C. 598. f. 1. Pecten, with concentric lamine. Mya? (Pullastra of Phillips), only a cast. Exogyra (Gryphea) nana, M. C. 383. f. 3. Trigonia clavellata, M. C. 87. Ammonites triplex. M. C. 292, 293. Plicatula, a new species, occurs at Weymouth. Chesilton. Mya? same as at Black Nore. Exogyra nana. Venus, only a cast. Ammonites giganteus? young, M. C. 126. Ostrea Hemicyclus, new species. Corton. Lucina? a fragment. Plagiostoma rusticum? M. C, 381. Cardium, small fragment. Ostrea, new ? Avicula concentrica, new species, very abun- Anomia? one valve imperfect. dant. Belemnites, fragment. Pinna viminea, new species; found also at Ammonites giganteus? Young, or possibly 4. Down Cliff, Bridport, in inferior oolite. Vernoni of Phillips: it is much crushed. Pecten, with concentric lamine. Echinus spines. The prevailing character of this stratum, along the whole line coloured on the north side of our map, is a bed of siliceous sand and green earth. It is also sandy and full of green earth at the village of Chesil; but at the base of the high west cliff of Portland, under the promontory of Black Nore, where it attains a thickness of eighty feet}, it is mixed with marl, and exhibits subordinate concretions, and beds of sandy marl and sandstone, both contain- ing the same fossils that are found at Chesilton and Corton. Its lowest beds become more argillaceous as they approach nearer to the subjacent Kim- * See Phil. Mag. and Ann., May 1827, vol. i. p. 139. t+ See Pl. III. fig. 1 & 3. Geology of the Neighbourhood of Weymouth, &c. 2) meridge clay ; it seems to form a connecting link between the Portland stone and Kimmeridge clay ; and, as has been observed by Mr. Conybeare™*, is pro- bably identical with the beds of sand and green earth, full of large boulder- shaped semi-calcareous concretions, that occur in Shotover Hill, near Oxford, between Kimmeridge clay and the imperfect upper calcareous Portland beds, which extend from Shotover to Brill and Thame and Aylesbury, and which also are occasionally much loaded with grains of green earth. Dr. Fitton has recognised this sand beneath the calcareous Portland beds at Whitchurch in Bucks: it occurs also in the same position in the Quainton Hills; and Mr. Lonsdale considers the sand which forms the escarpment close on the north and west of the town of Swindon to be also identical with this Portland sand ; the calcareous or upper Portland beds occur also beneath and a little to the east of that town. In the Boulonnois, Dr. Fitton describes this forma- tion as consisting of calcareous concretions of great size, as in Oxfordshire and Bucks, abounding in petrifactions, and imbedded in yellowish somewhat ferruginous sand ; between Gris-nez and Audreselles the shore is covered with these enormous masses fallen from the sand f. Kimmeridge Clay. The general character and fossils of this formation have been already described by Conybeare and Phillips. It is chiefly composed of beds of slaty bituminous clay, interspersed with Septaria and beds of bituminous marlstone. Near its middle region, in Ringstead Bay, it contains thin beds of marly sandstone, full of well preserved organic remains, and through its whole extent it is loaded with deltoid oysters, which are well known to be its most characteristic shell in England ; it contains also the Gryphea Virgula, which is considered characteristic of this formation in France, and abounds in it at Shotover near Oxford. Mr. James Sowerby has prepared the following list of fossils from this marly sandstone in Ringstead Bay. A carinated Serpula. Pinna granulata? a small fragment, M. C. 347. Mya depressa, M. C. 418. Ostrea deltoidea, M. C. 148. Pholadomya, near Ph. obtusa. Terebratula inconstans, M. C. 277. f. 3, 4. Venus? Pleurotomaria reticulata (Trochus), M. C. 272. Cardium ? eae Trigonia elongata, M. C. 431. Ammonites, species between 4. decipiens and Modiola bipartita, M. C. 210. f. 3, 4. A. mutabilis. , a small boring species. Ammonites rotundus, M. C. 298. f. 3. * Outlines of the Geology of England and Wales, pp. 166, 173, &c. + Philosophical Magazine, 1827, New Series, vol. i. p. 139. 22 Prof. Buckianp and Mr. De ta Becue on the On the opposite side of the Channel the Kimmeridge clay occupies the cliffs of Havre and Honfleur, where it lies next beneath the greensand, and it has been further identified by M. Elie de Beaumont, and by M. de Dufrénoy in the South of France. This formation exhibits its best sections and highest elevation near the east extremity of our district in the cliffs of Ringstead Bay and Osmington, where it attains a thickness of about 300 feet. From Osmington Cliff it continues westward, without interruption, through Preston and Upway Street to Abbotsbury, forming the narrow north belt of clay which we have named from the village of Upway Street. Great part of this belt is marked by a valley parallel and subjacent to the ridge of Portland stone above described, and dividing it from the ridge of Oxford oolite which forms its southern frontier: this belt of clay terminates suddenly about one mile west of Abbotsbury. In the Vale of Bredy, the covered state of the country renders it almost impossible to distinguish the Kimmeridge clay among the different clay beds that occupy a large part of its surface ; but we have identified it at Litton Cheney, immediately on the south of that village, containing the Gryphea Virgula. The southern belt of Kimmeridge clay near Weymouth, occupies a very small portion of the surface, constituting a triangular area, the base of which extends about a mile from Sandsfoot Castle westward, to the Chesil Bank, whilst its apex is at Portland Ferry : but although so small a portion of this belt of clay is here visible on the surface, we have evidence of its submarine continuation from hence to Portland Island, in the clay bottom of the excel- lent anchorage of Portland Road, beyond which also it appears above the level of the sea in the base of the escarpment at the north extremity of the Isle of Portland, and along its west shore also immediately south of the village of Chesilton. Hence it is clear that the Kimmeridge clay forms the fundamental stratum of the whole island, separated, as we have shown, from the Portland stone by the Portland sand and sandstone last described. The rapid dip of all these strata towards the south, causes the Kimmeridge formations to sink below the level of the sea in the southern portion of the island; whilst that part of its western coast, whose base is composed of these perishable sands and clays, is defended from the tremendous south-western waves by a natural breakwater of enormous masses of Portland stone that have fallen from the summit, and form a barrier against any further encroachments *. At a point near Portland Ferry, extending over many yards of the shore, Dr. Buckland remembers to have seen, several years ago, a portion of Kim- * See Plate III. fig. 3. Geology of the Neighbourhood of Weymouth, &c. 23 meridge clay, which is now covered up with sand, and which at that time presented the appearance of slate burnt to the condition of red tiles ; we have now strong reason to presume that such combustion may have taken place, since we have at this moment before our eyes the pseudovolcanic phe- nomena that are exhibiting themselves in the same stratum of Kimmeridge clay near the east extremity of Ringstead Bay, at Holworth Cliff, adjacent to the promontory of White Nore. This pseudovolcanic combustion began in September 1826, and during a period of many months emitted considerable volumes of flame, probably originating in the heat produced by the decompo- sition of the iron pyrites with which this shale occasionally abounds ; in the same manner as in the year 1755, a spontaneous combustion arose and con- tinued during several years in the bituminous shale-beds of the lias in the cliffs at Charmouth ;—we have a description of this circumstance in the Che- mical Essays of Bishop Watson : it is probable that in each case rain-water acting on iron pyrites has set fire to the bituminous shale ; thus ignited, it has gone on burning at Holworth unto the present hour, and may still continue smouldering for a long series of years, the bitumen being here so abundant in some strata of the shale, that it is burnt as fuel in the adjoining cottages ; the same bituminous shale is used as fuel in the village of Kimmeridge, and is there called Kimmeridge coal. This pseudovolcano at Holworth commenced in the face of the cliffs about twenty feet above the sea; its combustion was proceeding feebly when we saw it in September 1829, and it emitted no flame ; there was no appearance of any crater, nor has there ever been any kind of explosion. The extent of the surface of clay which has been burnt does not exceed fifty feet square. Within this space are many small fumaroles that exhale bituminous and sul- phureous vapours, and some of which are lined with a thin sublimation of sulphur ; much of the shale near the central parts has undergone a perfect fusion, and is converted to a cellular slag. In the parts adjacent to this ignited portion of the cliff, where the effect of fire has been less intense, the shale is simply baked and reduced to the condition of red tiles, like that on the shore near Portland Ferry. Should a similar ignition ever take place in the cliffs at Kimmeridge, which are so much more abundantly impregnated with bitumen, the fire may be propagated there for centuries, until the whole of the bitumen is consumed. Coralline or Oxford Oolite, and Calcareous Grit. The general thickness of this formation near Weymouth is about 150 feet. It contains beds of oolitic limestone resembling the oolite of Heddington, o4 Prof. Buckianp and Mr. De ta Becue on the Calne, and Scarborough, and in the sandy beds of its lower region, the same huge semi-calcareous concretions that occur in the calcareous grit of Wilts and Oxon. The corals which abound in this formation, in the two last- named counties, and which there give it the name of Coral Rag, are rare on the coast of Dorsetshire, just as reefs of modern corals occur at unconnected intervals in our modern tropical seas. In the Annals of Philosophy * Prof. Sedgwick has published a list of the beds composing the cliffs between Portland Ferry and Weymouth Harbour, and of the principal organic remains which they contain: he divides the whole series into nine groups, which, in the following section, we have subdivided further into thirty-one beds, included between the Kimmeridge clay at the top, and the Oxford clay at the bottom, of the whole series. Section between Portland Ferry and Weymouth.—(Order descending.) 1. Considerable thickness of Kimmeridge clay, 9. Grit bed,—Trigonize and Melania Hed- containing an abundance of the Ostrea dingtoniensis abundant. deltoidea. At about fifteen feet above 10. Grit bed,—Trigoniz abundant: the Tri- No. 2, clay iron-stone two feet thick— partly in nodules. goniz fill more than half of the beds Nos. 7, 8, 9, & 10. 2. Brownish red bed, about six feet—lime- 11. Grey marl. stone with small vesicles at top, gritty at 12. More compact grit—few shells. bottom—cylindrical and round concre- 13. Same as No. 10. tions of iron—contains deltoid oysters, Serpule, Pectines, Belemnites, and lig- . Grit. . Grit, with Melaniz. nite. 16. Grey marl, about four feet. 8. Grey grit, full of concretions resembling 17. Sandy bed. the stalks of Alcyonia, and crossing one 18. Limestone full of broken shells. another horizontally like a mass of en- 19. Grit. tangled and inosculating roots; the ex- 20. Dark grey sandy clay, four or five feet. posed surface is ferruginous. 21. Light brown oolite,—jointed Ammonite 4. Grey marl-clay. —Joints filled by hornstone. 4mm. ver- 5. Ferruginous bed, with eagle-stones: at tebralis ? first about one foot thick, afterwards 22. Grey marl, five feet. swells out considerably under Sandsfoot 23. Oolite, three feet—marl parting. Castle. Lima rudis? abundant. 24. Oolite, one foot. 6. Sandy grey and green marl—contains a 25. Gritty marlstone. continuous bed of deltoid oysters—also 26. Grey marlstone and marl, tending to con- lignite. cretions, twenty-five feet. 7. Grit bed,—brown grey, Aleyonium-shaped 27. Fox-coloured sands, twelve feet. concretions —Trigoniz abundant—one 28. Grey marl, twenty feet. foot. Clay parting. 29. Alternations of calcareous grit and marls, . Grit bed,—Trigoniz abundant; clay part- ing. eighteen feet ;—Pectines, oysters, Nau- tii, Trigoniz, Serpule. * Annals of Philosophy, May 1826, p. 346. Geology of the Neighbourhood of Weymouth, &c. 25 $0. Oolitic grit, —Trochus, Pecten—three beds stems of Alcyonia. Prof. Sedgwick has alternating with marl. shown the resemblance of these beds to 31. Brown, reddish grit—oysters abundant,— those of the same formation near Filey Pectines, Ammonites, Gryphea dilatata, Bridge and Scarborough Castle, where G. bullata? Trigonie. the sandstone is similarly aggregated into 32. Yellow brown. sandy grit, forty feet,— irregularly branching cylindrical concre- Gryphea dilatata, oysters, sharp-keeled tions. Ammonite, other Ammonites, Pectines, 33. Oxford clay, abounding in Gryphea dila- Nautili: the hard beds contain concre- tata. tions resembling a mass of entangled It appears from this section, that the Oxford oolite formation is composed of alternations of imperfectly oolitic limestone and calcareous grit, with nume- rous partings of clay. The superior beds are loose and sandy, and may be considered analogous to the upper calcareous grit in Yorkshire, described by Mr. Phillips; they are best seen near Sandsfoot Castle, where the uppermost of them contain deltoid oysters, and become gradually more argillaceous until they pass into Kimmeridge clay : the central beds are the most oolitic, some- times loose and sandy, and at other times compact and in continuous beds: they are most oolitic at the village of Wyke Regis and in the cliffs near Osmington, at both which places they afford a light-coloured building-stone, which, but for the vicinity of Portland, might have been applied to purposes of architec- ture. In the cliffs west of Wyke Regis, they show the same oblique cleavage which isso common in oolitic strata. Thus = — M. Boblaye, in his paper on the Jura . oe 0 SOS Formation in the North of France*, no- tices that in the great oolitic quarries of Ballon near Stenay, lines of false division cross the true stratification at angles of 45° or 50°. Examples of the same kind are seen in the Oxford oolite quarries at Heddington, and in the forest marble and great oolite along the road from Cirencester to Bath ; similar parting occur also in the new red sandstone at Bridgenorth, but in a manner much more complicated, and crossing the true strata in all possible directions. Beneath these central oolitic beds, strata of semi-calcareous sand and cal- careous grit prevail, and display alternations of sand and sandy loam, with continuous beds of calcareous grit and beds of large concretions lodged in strata of sand. The entire thickness of these calcareous grit beds with their largest concretions, is best exhibited in Ham Cliff, about three miles north- east of Weymouth}. In the hill immediately on the west of Weymouth, the * Ann. des Scien. Nat., Mai 1829. + See Plate II. fig. 8. VOL. IV. SECOND SERIES. E 26 Prof. Buckianp and Mr. De 1a Becue on the sandy loam beds of this formation afford an useful brick earth. The passage of the lowest strata into Oxford clay is indicated by the presence of the Gry- phea dilatata in the beds of grit, and this passage is analogous to that which occurs at Heddington Hill near Oxford; but the presence of an upper cal- careous grit and gradual passage of the superior strata at Weymouth into Kimmeridge clay, show a more perfect development of this part of the oolite formation in Dorset than in Oxfordshire. In the sections at Heddington the upper grit is wanting, and the Kimmeridge clay reposes immediately on the oolitic building-stone: the surface of this stone is also guttered over and furrowed with water-worn cavities and small rock-basins, marking a destruc- tive action of the sea before the deposition of the Kimmeridge clay : this water-worn surface of the oolite is also decomposed and become rusty to the depth of about a foot, in a manner unusual where the series of depositions has been regularly continuous, and its decomposition seems to have resulted from long exposure to water before the laying on of the Kimmeridge clay. These circumstances are duly noticed by Conybeare and Phillips *. All the beds of the Oxford oolite formation near Weymouth are loaded with shells similar to those found in the same formation in Wiltshire, Oxford- * Outlines of the Geology of England and Wales, p. 189, note. Prof. Sedgwick, in his comparison of the appearance of the coral rag formation near Scar- borough and Weymouth with that of Oxford (Ann, of Phil., May 1826), conjectures that the upper portions of the Scarborough and Weymouth sections may be wanting near Oxford, and that the coral rag and freestone of Heddington together, represent the central group of the Weymouth and Steeple Ashton sections: thus, at its two extremities in the coast of Dorset and Yorkshire, the superior members of this formation are most fully developed, whilst they are wanting, and have been apparently removed from the central part of their range near Oxford. We entirely agree with Prof. Sedgwick in these remarks, and in the consequences which he draws as to the imperfection of the type of this formation near Oxford: the whole of this subject has been fully illustrated by Mr. Phillips in his excellent work on the Coast of Yorkshire, and still more recently by Mr. Lonsdale in his valuable paper on the Oolite District near Bath (Geol, Trans. vol. ui. Part II. p. 262), in which he gives a section of the Oxford oolite formation at Highworth, where the upper members are represented by about seven feet of alternating beds of sand and rubbly oolite, or oolitic calcareous grit: he also shows that near Steeple Ashton the superior beds appear under the form of ten feet of sand, resting on ten feet of ferruginous clay interspersed with oolitic grains of hydrate of iron. Some bones of a Plesiosaurus have been found in this clay by Mr. Mead. According to M. de Caumont, a similar alternation of strata of sand and calcareous sandstone, with beds of clay and of imperfect oolitic limestone, affords, on the coast of Normandy, a group corresponding with the upper calcareous grits of Weymouth and the coast of Yorkshire, interposed between the Kimmeridge clay and the coral rag. (See M. de Caumont’s Sectional Lists of the Clif at Hennequeville; of the Hill of Glos near Lisieux ; and of St. Julien-sur-Calone near Pont VEvéque. pp. 113, 114, 115.) , Geology of the Neighbourhood of Weymouth, &c. i shire, and Yorkshire. The T'rigonia clavellata and Melania Heddingtoniensis are among the most abundant. Another feature which is wanting in Oxfordshire, is the highly ferruginous character which this oolitic formation assumes near Weymouth, particularly in its upper beds immediately below the Kimmeridge clay; the same fer- ruginous character prevails also in other parts of its course through this district, and very remarkably in the hills near Abbotsbury. In a ravine called the Red Lane, immediately north of that village, the oolitic grains are com- posed of a rich hydrate of iron, which, if the country afforded fuel, might be wrought as an ore of the same quality with that which supplies so many iron-foundries in France, from a similar granular ore in the oolite formation. The extent of surface occupied by the Oxford oolite and its subordinate grits in the valley of Weymouth, will best be seen on the Map ; it forms two parallel belts of unequal breadth and length, subjacent to the two beds of Kimmeridge clay before described, and reposing on two other parallel belts of Oxford clay ; these oolitic belts terminate in two ridges, overhanging the Oxford clay, with two escarpments that face towards each other ; the most southerly of them extends nearly two miles west, from the town of Weymouth to the Fleet at Linch, and is about one mile broad; the northern ridge and its escarpment occupies a length of twelve miles, from the cliffs of Osmington to the sea at Abbotsbury, terminating in an escarpment towards the south, which presents its highest inland elevation in Linton Hill near Abbotsbury. In no part of its course does it much exceed half a mile in breadth, excepting at its western termination near Abbotsbury, where it widens to about a mile, from the effect of the great fault hereafter to be described ; here also it changes its dip from north, first to east, and then to south, bending round and enlarging itself like the bowl of a spoon, whose handle is represented by the long ridge of Linton Hill, just mentioned. ‘The towers of St. Catherine’s Chapel at Abbotsbury, and of Wyke Regis Church, are two remarkable land- marks, placed respectively near the western termination of the northern and southern belts of oolite just described, and serve as points by which their course may be recognised from the Dorchester road and hills adjacent to it near Weymouth. In the Vale of Bredy, the oolite occurs only in a very narrow band, extending about a mile from east to west, from Kingston House to the village of Litton Cheney ; it is seen only in a few old quarries near these two places, and in a hollow way at Litton Cheney, where it appears much disturbed by a fault, and brought, as at Abbotsbury, almost into close contact with the base of the escarpment of the chalk. E 2 28 Prof. BuckLanp and Mr. De 1a Becue on the Oxford Clay. The Oxford clay in this district attains a thickness of about 300 feet, and reposes immediately, and with conformable dip, on the central arch of corn- brash and forest marble; on the south side of this arch it forms a belt of low ground about a mile broad, extending from Melcombe Regis and Weymouth Bay to East Fleet. It winds round the eastern extremity of the forest marble at the Barracks, and the marsh of Lodmoor, and thence extends westward along the north side of the central arch, forming a valley of less than half a mile in width, to the Decoy and Swanery at Abbotsbury, where it terminates in the Chesil Bank, Its eastern termination is seen in the lowest strata at the base of Jordon Hill and Ham Cliff, about three miles north-east of Weymouth *. A distinct section of this stratum occurs in a low cliff under the Barracks at Radipole, where it dips south at about 20°, and where, till lately, it pre- sented, at low water, a pavement of large and beautiful Septaria, known pro- vincially by the name of Turtle Stones. The veins of these Septaria are filled with yellow semi-transparent calcareous spar, often passing into a rich deep brown colour: their beauty, when polished, has, within these few years, caused the greater part of them to be taken up and manufactured into slabs and tables. In this same section at Radipole Barracks large Ammonites and other shells abound. The most characteristic shell is the Gryphaa dilatata, which is as universally abundant in the Oxford clay throughout this district, as the deltoid oyster is in the Kimmeridge clay. In consequence of the want of sections, we have not attempted to trace the minute details of this clay in its windings through the Vale of Bredy, in which it forms a marginal band round the eastern and northern frontier of the forest marble. On the opposite coast of Normandy this same Oxford clay occurs at Vaches Noires, and abounds with the Gryph@a dilatata, and many other fossil shells. Forest Marble. The formations, which, for convenience of description we have united under the name of Forest marble, and which are the lowest that occur in the Vale of Weymouth, admit of a three-fold division ;—1. Cornbrash; 2. Forest marble ; 3. Clay, and marlstone. 1, The uppermost region, or cornbrash, is composed of a loose rubbly limestone, alternating with thin beds of clay and marl, and is so absolutely * See Plate II. fig. 8. Geology of the Neighbourhood of Weymouth, &c. 29 identical, both in its mineral characters and abundant organic remains, with the cornbrash of Wiltshire, that no further description need be given of it than may be found in Conybeare and Phillips’s account of Cornbrash*. 2. The middle region, consisting of the usual well-known varieties of forest marble, sometimes constituting thick beds of stone composed of comminuted shells, at other times passing into oolitic and sandy slate. The most perfect condition of this forest marble is exhibited in the quarries of Bothenhampton, one mile south of Bridport, where it contains that remarkable fossil the Brad- ford Encrinite, Apiocrinites rotundus, together with fragments of Pentacrinite, palates of fish, and fragments of lignite, all imbedded in indurated masses of broken shells; it contains also the same Apiocrinite in the under-cliff between Abbotsbury Castle and the sea, and in the cliffs immediately west of Bridport Harbour. 3. The lower region is composed principally of strata of blue clay and grey marl and marlstone, containing subordinate beds of imperfect stone. The best section of this grey marl is seen in the cliff at Watton Hill, close on the west of Bridport Harbour, attaining a thickness of about 150 feet ; it is here capped by an outlying summit of forest marble, being the extreme south-western termination of this rock on the coast of England+. The base of this marl reposes on the sands of the inferior oolite. This grey marl also forms a cap on the summit of the inferior oolite in Burton Cliff, on the east of Bridport Harbour: it may probably be the equivalent of the Fuller's earth in the vicinity of Bath. The predominating character of these three deposits, which we have grouped together as forest marble, is clay; the amount of their united thickness may be about 400 feet. The extent of this forest marble formation in the Vale of Weymouth is con- siderable ; it occupies a tract near six miles long, and from two to three miles broad, constituting the lowest strata and central belt of that district. This central belt emerges at Radipole from beneath the Oxford clay, and is less elevated than the parallel belts of Oxford oolite and Portland stone, whose escarpments overhang it on the north and south, rising towards each other as if they once had been continuous, and had been separated by the elevation of the central axis of forest marble, over which, if reunited, they would form a continuous ridge. It is not of sufficient importance to trace separately the extent of the individual beds of cornbrash and forest marble throughout this central belt. The cornbrash occupies the uppermost place along the lines of its junction with the Oxford clay, and occurs also on many summits and minor * Outlines of the Geology of England, p. 202. + See Plate II. fig. 13 and 14. 30 Prof. Bucktann and Mr. De ta Becue on the hills within its area. The valleys are usually cut down to the slaty forest marble beds and their associated clays. On the north, and east, and south, it is entirely surrounded by, and dips beneath, the Oxford clay ; on the west it is terminated by the back-water of the Fleet, cutting it in an oblique line for about four miles, from the village of East Fleet to the Swanery of Abbotsbury. It has been already stated, that it constitutes the axis or central arch of the Weymouth district, upon each side of which, as on a saddle, all the more recent formations successively repose. After a slight depression beneath the surface at Abbotsbury, the forest marble and its clays, or in most cases the clays without the marble, reappear in strength in the Vale of Bredy, occupying an extent of surface about eight miles long and four miles broad ; bounded en the east and north by the over- hanging escarpments of chalk and greensand ; on the south by the sea and Chesil Bank, and on the west by the subjacent strata of inferior oolite near Burton Bradstock and Bridport. Throughout all this Vale of Bredy, the main dip of this strata is towards the north. Inferior Oolite. Along the whole coast of Dorset, and indeed the whole south coast of En- gland, there is a total absence of Bath oolite ; but the inferior oolite occurs in the vicinity of Bridport, attaining a thickness of about 300 feet, and occupying the cliffs for two miles east, aud three miles west, of Bridport Harbour. The summits of the highest hills around the town are composed of the superior strata of this formation, consisting of coarsely oolitic yellow limestone, resem- bling that of Dundry Hill near Bristol, irregularly interspersed with oolitic grains of hydrate of iron, as at Bayeux in Normandy : the most extensive quarries in these upper strata of the inferior oolite, are at the summit of Chideock Hill, on the west of Bridport ; these are wrought in a light brown limestone full of large and small ferruginous grains ; a few beds also abound in minute veins and cells lined with hydrate of iron. One stratum on this hill is in great measure composed of fragments of Pentacrinite, others contain a variety of organic remains,—Ammonites, Nautili, Belemnites, several Pectens, a large Lima, Cucullea, Plagiostoma, Modiola, several species of Terebratula, and fossil wood™. Beneath this coarse limestone is a series of brown and yellow Joam and sands, highly micaceous, and containing, in their upper region, strata of cal- * The oolite of Chideock Hill contains caverns, but no bones have yet been noticed in them ; in the same oolite beds at Burton Cliff, there are inaccessible fissures filled with diluvium. Geology of the Neighbourhood of Weymouth, &c. 31 careo-siliceous sandstone, and in the lower region interrupted strata of large concretions of coarse sandstone; the lowest strata of this formation become gradually more blue and marly, and at length pass imsensibly into the upper marl beds of the lias. We observed a remarkable fact in some stony masses from the middle region of the inferior oolite at Down Cliff on the west of Bridport, namely, that some of these masses contained an oolitic breccia or conglomerate of rolled fragments of coarse oolite, not differing in character from the strata of which they form a part. The fragments in this breccia are not concretions, but afford unequivocal evidence of having been rolled by water, in the fact that many of them are perforated on all sides by the holes of small Lithodomi, of which holes the lower extremities alone remain, their tops having been worn away by the attrition which has reduced the fragments in which they occur to the state of large subangular pebbles; these fragments must have lain loose in the sea at the time when the Lithodomi perforated their surface, for one side only could have been perforated before they were detached from their native rock ; and the perforation of the lower side at least, if not of the other sides, must have taken place in a period intermediate between such separation and the completion of that moderate degree of rounding which they have since undergone. We see at this time on the ledges of the shore at Lyme, between high and low water mark, loose angular slabs of lias recently torn from the subjacent strata, and perforated on all sides by boring Mollusc, after the manner of the fragments in our oolitic breccia. This perforated breccia at Down Cliff shows a lapse of time to have intervened, in which there was apparently a suspension of the deposition of the inferior oolite ; a time in which fragments were torn by the waters from the earlier beds and became inhabited by Lithodomi, and subsequently rolled on the shores, or at the bottom of the then existing seas ; they further show that the lower strata of the inferior oolite were at once consolidated to the condition of stone, hard enough to protect Lithodomi and to be rolled to pebbles, before the upper strata of this same inferior oolite formation had been laid over them. Lias. The western extremity of our Map includes the upper marl beds only of the lias formation ; these are exposed at the bottom of the valleys of denudation round Golden Cap Hill, and on the sea-shore along its base : they are cha- racterized by enormous deposits of Belemnites, and correspond with the Cal- caire & Belemnite of the French geologists, as the lower and more stony beds of lias at Lyme agree with the French Calcaire a Gryphite. One bed at the ae Prof. Bucktanp and Mr. De ta Becue on the base of Golden Cap presents an almost continuous pavement of Belemnites, running for some distance along the shore; these marl beds also contain the remains of Saurians. A detailed description of this lias formation at Lyme having been published by Mr. De la Beche*, we deem it sufficient to refer our readers to that paper. VALE OF BREDY. We have already pointed out details of the leading formations of the Vale of Bredy in our description of the westward terminations of the strata that occur in the Vale of Weymouth; we here sum them up in a few words. The structure of the Vale of Bredy is much less complicated than that of the Vale of Weymouth ; its strata do not, as there, dip in opposite directions from an anticlinal line, but emerge regularly from beneath the chalk and greensand escarpments of its eastern and northern frontiers, rising to the west and south, until at their western termination they rest on the inferior oolite of Burton Cliff and the hills near Bridport. Around the eastern and northern frontiers, the greensand constitutes a sub- escarpment to the chalk, and also forms the outlying summits of Abbotsbury Castle, Swyre Knoll, Shipton Beacon, and Hammerdon Hill already men- tioned : its southern frontier next the sea, is composed of forest marble and thick beds of clay connected with it; its middle region also (constituting the bed of the river Bredy,) is made up of these same clays, interspersed occa- sionally with thin stony beds of forest marble. The entire face of this Vale of Bredy is so destitute of roads and sections, and so covered up with grass from the bottom of the valley to the escarpment of the hills, that it is extremely dificult to trace the separation between these extensive clay beds of the forest marble formation, and those which may be made up of the continua- tions of Kimmeridge and Oxford clays, interposed between the forest marble and the greensand. EFFECTS OF DISTURBING FORCES. Having thus far considered the character and extent of each formation which occurs on the coast of Dorset, it remains only to examine the effects that have been produced on them by disturbing forces: these may be divided into five heads; namely,—1J. Elevation ;—2. Depression ;—3. Contortion ;—4. Faults ; —5}5. Denudation. I. Evevation. The most important feature which pervades the whole Vale of Weymouth * Geol. Trans. Second Series, vol. ii. Part I. p. 21. Plate II. Geology of the Neighbourhood of Weymouth, &c. 33 is, the arch-like disposition of all the formations it contains ; the axis of this arch passes east and west from Weymouth Bay to the Chesil Bank, forming an anticlinal line, on each side of which all the successive strata dip respec- tively to the north and south. This dip of the strata in opposite directions from the anticlinal line, is represented in the general section, Plate ITI. fig. 1. It affords, on a larger scale, an example of the same kind of valleys of eleva- tion with those which have been described by Professor Buckland*. 'The details of these arched strata in the Vale of Weymouth have already been sufficiently set forth. We think there is evidence enough to show that the strata were once nearly continuous and horizontal, and have been elevated to their present position by a force acting from beneath in a line nearly east and west, forming a continuation of the same line of elevation that extends through Purbeck and the Isle of Wight, and parallel to that of the axis of elevation of the Weald of Sussex and Kent. The period of elevation in all these cases was apparently the same, viz. subsequent to the deposition of the London clay, if not of the most recent tertiary strata in the Isle of Wight. With respect to the analogous axis of elevation, which extends with certain interruptions from the eastern extremity of the Mendip Hills along the coast of South Wales to Milford Haven, it has been shown by Dr. Buck- land and Mr. Conybeare that this elevation took place before the deposition of the new red sandstone formation +; the direction of this line deviates from east and west several points towards the north-west. In these comparatively small instances, as in the elevation of the highest mountains in the world, noticed by M. Elie de Beaumont{, it seems that the operating forces have been exerted usually in straight lines, and that these straight lies were often parallel to one another; and the fact that the greatest mountain chains are for the most part thus disposed, more especially those which are volcanic, as in the case of the Andes, leads us to refer the elevation of them all to one and the same common cause,—namely, the expan- sion of elastic vapours bursting upwards in longitudinal cracks along the lines where the least resistance was presented by the incumbent strata§. The comparative insignificance of the elevations we are considering in the South of England, makes no difference in the principles we would apply to explain their origin ; they appear to us to be faithful models, representing on a smaller * Geol. Trans. Second Series, vol. ii. Part I. p. 119. + Ibid. vol. i. p. 210, et seq. { Annales des Sciences Naturelles, 1829—1830. § The movement of modern earthquakes along straight lines, added to the frequent rectilinear ii of volcanic chains, adds still further probability to these conjectures.—See Hall’s South merica. VOL. IV.—SECOND SERIES. y 34 Prof. Bucktanp and Mr. De ta BeEcueE on the scale, the self-same phenomena, which, in more gigantic magnitude, pervade the highest Alps. In the eastern part of our Weymouth district, we have examples of valleys of elevation, on a small scale, in the three little circus-shaped valleys of Moignes Down, Poxwell, and Sutton Pointz*. All these three valleys are of an elongated oval shape, and so nearly resemble the interior of a Roman circus, that if the basset ends of the strata were cut into benches, the central area would be visible to persons seated on every part of them. These three small valleys of elevation are on the same straight line, running east and west, parallel to the grand axis of the Weymouth district, and also parallel to two great faults adjacent to them, and immediately to be described +. The western extremity of the first valley touches the eastern extremity of the second, and the second is separated from the third, only for a small space, by a ridge of Portland stone: each of these valleys has only one small lateral outlet for the discharge of its waters ; the area of the Moignes Down Circus scarcely descends below the Portland stone: those of the Poxwell Circus and Sutton Pointz Circus descend into the Portland sand and Kimmeridge clay. In the circus of Moignes Down and of Poxwell, the circumference is chiefly composed of the basset edges of strata of Portland stone dipping outwards in every direction ; but the circus of Sutton Pointz, which is much longer and wider than the other two, is surrounded by Portland stone on three sides only, the remaining north side being partially occupied by greensand and chalk, in consequence of its being intersected by the great Ridgeway faultt. Although the elevation of these circus-shaped valleys must have produced vast piles of fractured strata on the line of elevation, there is no accumulation of such fragments, nor any perceptible quantity of gravel of any kind within their area; the clearing out of all the rubbish which must have encumbered them at the time of their elevation, can only be referred to the contempo- raneous or subsequent operations of very powerful denudation. II. Depression. Elevations of strata, such as we have been tracing, can scarcely have arisen without simultaneous depressions in the spaces intermediate between * See Plate II. fig. 2, 3, 4. + See Map, Plate I. + The circus-like inclosure of the Valley of Sutton Pointz is best seen from its eastern extremity at the top of Osmington Hill, at a point on the old road near the western extremity of the Poxwell Circus ; the new turnpike road from Poxwell to Osmington, enters the Poxwell Circus by the outlet on its north side, and crossing its shorter diameter, cuts through the Portland stone on its south side, and there enters upon the Purbeck beds, reposing on the back of the Portland stone, and dipping towards Upton. See Plate II. fig. 3. Geology of the Neighbourhood of Weymouth, &c. 35 the lines of elevation ; and accordingly our district affords examples of troughs and depressions thus produced in the case of the Purbeck beds lying upon a trough of Portland stone at Upway, and of Kimmeridge clay in a trough of Oxford oolite at Abbotsbury *. ILI. Conrortion. At Upway in the quarries west of the Church, we have examples of con- tortion produced by the elevation of the strata, similar to those represented by Mr. Webster in his drawings of Lulworth Cove and the coves adjacent to it, in the Isle of Purbeck. Throughout the whole Weymouth district, and particularly along the lines of fault, which we shall next describe, contortions of greater or less amount are too numerous to require individual speci- fication. IV. Fautrs. In a district which has been so much dislocated, the elevations and depres- sions just described lead us to expect still further disturbances in the occur- rence of faults; and accordingly we find two very extensive faults on the northern and north-eastern frontier of the Vale of Weymouth, and also two others on the north-west of the Vale of Bredy and near Bridport, besides many minor local fractures. The two great faults in the Vale of Weymouth, run nearly in a straight line from east to west, parallel to the general axis of elevation of the whole district, and were probably produced by the same forces and at the same time with this general elevation. We shall call the most northerly of them the great Ridgeway Fault, the other the Osmington Fault. Wherever we examine these faults, we find double evidence of the movement that has taken place ; Ist, In the non- accordance of the strata that form the opposite sides of the faults ; 2ndly, In the fine parallel lines and vertical furrows resembling the lines and grooves on Slikensides, and often also in the highly polished surfaces of the materials that form the side walls of the fault, showing that these ponderous masses have ground each other with prodigious violence in the act of separation and movement from their original position. The great Ridgeway fault is an upcast fault, elevating, on its south side, into contact with the escarpment of the chalk strata that would otherwise have dipped beneath it, particularly the Portland stone, nearly along the whole line which this fault traverses. The Osmington fault is a downcast fault, throwing down, on its south side, strata * See Plate II. fig. 1, 6. F2 36 Prof. Bucktanp and Mr. De ta Becue on the of chalk, greensand, and Portland stone, to a position lower than the strata from whose extremities they have been snapped off*. 1. Great Ridgeway Fault. The most important of these, the great Ridgeway fault, extends, without interruption, nearly fifteen miles, from the eastern extremity of our district at Moignes Down, to the sea near Abbotsbury, passing along the great escarp- ment of the chalk at various elevations, from the top to the bottom of it; the Osmington fault we could trace only about three miles, from South Holworth near White Nore, to Ham Cliff on the north-east of Weymouth. The first or great Ridgeway fault is one of the most curious and important we have ever seen, in consequence of the variety of instructive sections afforded along its course; these sections we shall describe in the order of their occurrence, beginning at the eastern extremity f. The fault emerges from the chalk formation at Moignes Down Farm, on the north side of the circus of Moignes Down, and brings the truncated lower ends of strata of Portland stone into contact with the truncated upper ends of strata of chalk, both dipping to the northt. Here a valley of denudation runs exactly along the line of fault, having its north side composed of chalk, and its south side entirely of Portland stone. The strata have been raised on both sides of this fault, but raised unequally ; whence it results, that on the north side the chalk rises towards the fault, whilst on the south side the Portland stone dips towards it, as if plunging beneath the chalk; whereas the Portland stone has been elevated from its original position, relatively, though not absolutely, much higher than the chalk: yet, notwithstanding this fracture of the strata and dissimilarity of substances on the two sides of the valley, the effect of denudation has been so equable, and the removal of the fractured materials so total, that no other features are presented by the surface than those of an ordinary valley of denudation on horizontal chalk. Our next section§ is taken at Poxwell Hill, less than one mile west of Moignes Down Farm. Here the circumstances of the fault on the north of Poxwell Circus are similar to those at Moignes Down Farm, excepting that at Poxwell there has been no denudation on the line of fault. Two miles west of Poxwell in the valley of Sutton Pointz||, the exact line of the fault is scarcely to be recognised, from the circumstance of the strata on both sides of it being perpendicular. At fig. 5. in Sutton Valley, one mile west of *® See Plate II. fig. 2, 3. + See Plate II. fig. 1, 2, 3, 4, 5, 6, 7, 12. t See Plate II. fig. 2. § Plate II. fig. 3. || Plate II. fig. 4. Geology of the Neighbourhood of Weymouth, &c. 37 fiz. 4, the Portland stone forms the south side of the fault; and greensand, surmounted by chalk, the north side,—both dipping rapidly to the north. The theoretical figure (Plate II. No. 12.) is intended to represent by the dotted lines aa. bb. cc., effects that would be produced by denudation extended to different depths along the line of a fault, traversing such strata as occur along this part of the Ridgeway ; thus a denudation descending to aa. would leave chalk and greensand on the north side of the valley so denuded, and Portland stone on the south ; a denudation to bb. would give the same section on the north side of the valley, and Portland sand on the south ; and in this case it would be difficult to distinguish between these two sands, without the aid of organic remains. A denudation to cc. would give again the same beds on the north side, and Kimmeridge clay on the south: examples of all these three theoretical representations are visible in the course of the Ridgeway fault ; e. g. On the high crest which separates the valley of Bineombe from that of Sutton Pointz, the Portland stone touches the chalk; the surfaces of both rocks at the line of fault presenting a uniform appearance, and uniformly level line, like the surface of fig. 12. Plate II. Near the north-western extre- mity of Sutton Valley, a denudation, analogous to that represented by aa. fig. 12. Plate II., shows the Portland stone touching greensand; a lower point of the same denudation exhibits the Portland sand in contact with the greensand, as represented at 5b. in the same figure; and on the north of Sutton village the Kimmeridge clay also is brought into contact with the greensand, as represented at cc. At Upway, on the northern extremity of the general section, and near the summit of the hill*, the Portland stone, covered by Purbeck beds, occupies the south side of the fault, and nearly horizontal chalk its north side, the Pur- beck and Portland beds rising at a high angle northwards towards the fault. From Upway, for four miles westward, to the final termination of the Port- land stone at Portisham, the Portland stone is continued on the south side, and the chalk on the north side of this fault ; it is exposed by no section, but the junction can be traced on the surface of the fields. Near the village of Portisham, precisely at the western termination of the Portland stone, the fault deviates to a south-western direction for about a quarter of a mile, traversing the bottom of a deep and narrow dry valley or comb, by which the road from Portisham leads up to Black Down; the east side of this valley is composed of Portland stone, and the west side of chalk, both attaining a considerable elevation above the bottom of the valley. In the village of * Plate II. fig. 1. 38 Prof. Buckianp and Mr. De ta Becue on the Portisham, the fault again resumes its westerly direction, and at the same time brings up the Kimmeridge clay into immediate contact with the base of the escarpment of the chalk; this contact continues for some distance towards Abbotsbury. At Abbotsbury*, the Oxford oolite occupies the south side of the fault; and greensand, resting upon clay, the north side; the two latter are nearly horizontal, whilst the oolite rises to the north. The irregularities of structure occasioned by this fault on the west of Abbotsbury are considerable, and not totally made out by us. A compound disturbance, similar to that which has produced the trough-shaped disposition of the Purbeck and Portland stone at Upway, has caused an analogous derangement near Abbotsbury, along a tract of about a mile in length, from east to west, and nearly a mile in breadth+. This tract occupies the slope and under-terrace, between the summit of Abbotsbury Common and the sea, and is composed chiefly of ferruginous Oxford oolite, dipping regularly to- wards the north, on that side of Abbotsbury which is nearest to the sea, until it terminates abruptly in a hill called Zoles (immediately above the mansion of the Countess of IIchester). In this hill it suddenly trends round, changing its dip towards the east, and rising with an escarpment to the west, for a short distance, until the dip again turns suddenly to the south, and so continues along the line of fault, running east and west more than a mile from Zoles to the town of Abbotsbury. By these three dips, the oolite is thrown, at its termination, into the form of a spoon, rising outwards in three directions from the lowest central line of depression, and terminated by high escarpments on the south and west, and on the north partly by a false escarp- mentt, and partly by abutting against the fault§. The existence of this false escarpment (fig. 7.) is due to the agency of the upcast fault, which has elevated, not only these Oxford oolite beds, but even the subjacent beds of Oxford clay and forest marble irregularly along the under-terrace, between the false escarpment of oolite, and the true south escarpment of the lofty ridge of greensand and chalk composing Abbotsbury Common ; so that beneath and parallel to this true escarpment, at a distance varying from one to two furlongs, the false escarpment forms a broken under- terrace || facing the true escarpment, with opposite dip; and between these two escarpments a narrow band of forest marble is thrown up in great con- fusion for about a mile, from the town of Abbotsbury west to Zoles. The confusion is increased by land slips, which have brought down heaps of rubbish from the greensand escarpment of Abbotsbury Common and Abbots- * Plate II. fig. 6. + See Plate II. fig. 6 & 7. + Plate II, fig. 7. § Plate II. fig. 6. || See Plate II. fig. 7. Geology of the Neighbourhood of Weymouth, &c. 39 bury Castle Hill, and spread them over the various broken beds of the oolite formation, along the under-terrace and line of fault; and have also so com- pletely masked and covered up all the lower beds of the true escarpment below the greensand, that not one of them can be distinctly seen: and although this great escarpment is at least 400 feet above the sea, none of its lower strata are exposed to view, except a bed of clay, which, by casting out a line of springs along its junction with the incumbent greensand, affords a perpetual cause of the Jand slips which obscure the entire base of this escarp- ment, and prevent our tracing distinctly the great Ridgeway fault at its western termination into the sea*, The depth of the dislocations occasioned by this great Ridgeway fault along the escarpment of the chalk appears to vary to the amount of several hundred feet. 2. Osmington Fault. The range of the Osmington fault is east and west, and parallel to the great Ridgeway fault we have just described, at the distance of about one mile and a half to the south: its eastern extremity is lost in the chalk downs near South Holworth, and its western termination is seen in Ham Cliff, three miles north-east of Weymouth. Plate II. fig. 2% exhibits its most eastern section at Upton Hill, in which horizontal chalk beds form the north side of the fault, and subsided chalk, greensand, and Portland stone, the south side : a lime-kiln excavated exactly on the line of fracture, exhibits the disposition here represented. Ina section of the hill and water-course, one mile further west, at Osmington Mill, the south side of this fault is formed of subsided chalk and greensand, dipping north; and the north side formed of chalk, resting on greensand, both inclined slightly to the south. Plate II. fig. 8. shows the western extremity of this fault at Ham Cliff, where the Oxford oolite on its south side has subsided to the level of the Oxford clay on its north side. 3. Ringstead Bay Fault. Plate I]. fig. 11. represents a third and very local small fault, produced apparently by a fracture in the cliffs, and bringing a subsided mass of Port- land stone and Portland sand into contact with Kimmeridge clay. This fault is more oblique than any part of the two great faults we have been describing ; like them it ranges east and west, but can be traced only toa © On the north side of Abbotsbury Common, immediately below the Castle, a series of land slips, similar to those on the south side, is indicated by a long range of narrow ponds, supported by the bed of clay, across which the land slips have taken place. + Plate II. fig. 3. AO Prof. Buckianp and Mr. De ta Becue on the very short distance: the pseudovolcano we have described is in the Kim- meridge clay which forms the base of this subsided mass. Another minor fault is seen at Boat Cove, on the west of Osmington Mill*, where an apparently false dip of the Oxford oolite has been produced by a recent slip of the cliffs; it isso small and partial that it would be unworthy ~ of notice were it not that it is prominently exposed in the profile of the coast, and gives an erroneous impression of the position of the strata in the cliff from which it has fallen. Near this spot, also, at the cascade of Osmington Mill, we have another small fault, exposed on the shore traversing the Oxford oolite, and running outwards into the sea, just along the anticlinal line, where the strata turn at this part of the coast. 4. Bothenhampton Fault. Pl. IT. fig. 14. represents a downcast fault at Bothenhampton, one mile south-east of Bridport. We believe that this fault was first noticed by Prof. Sedgwick : it is of considerable depth, bringing the forest marble on its south side into contact with inferior oolite on the north side, the forest marble dipping at a considerable angle towards the fault; its general range, like that of the rest, is nearly east and west, and although, from the similarity of the clays which it intersects, we have not traced its uninterrupted con- nexion, we think it continues eastward to Shipton Gorge, Litton Cheney, and Long Bredy. At each of these three places, lying as they do nearly ona straight line, there has been much dislocation and disturbance. 5. Bridport Harbour Fault. At Pl. II. figures 13 and 14 represent the western termination of another downcast fault in the cliffs about a mile west of Bridport Harbour, being the last we have to mention. Its amount is considerable: on its north side are beds of inferior oolite based on lias; on its south side are beds of forest marble based on more than 150 feet of grey clay, and these are suddenly and violently turned up when they come into immediate contact with the fault. We believe this clay to be the same that occurs in such thickness in the Vale of Bredy ; and although we have there considered it as subordinate to the forest marble formation, we have no evidence to show that it may not also represent the Fuller’s earth beds that occur between the great oolite and in- ferior oolite of the neighbourhood of Bath. The eastern extremity of this fault { presents a complicated double fracture, causing the lower beds of the * See Plate Il. fig. 9. + See Plate II. fig. 9. + Plate II. fig. 13. a. Geology of the Neighbourhood of Weymouth, &c. Al grey marl and marlstone to assume a position partly vertical and partly tor- tuous, between horizontal beds of grey marlstone on the one side, and of inferior oolite on the other. These appearances may in part be due to sub- sidence superadded to the fault; the point of the cliff in which they occur is so much exposed to the action of the waves, that it may ere long be totally removed, and the appearances represented in our section be entirely changed. It should be observed that not one of all these faults appears to have been produced during the formation of the strata : not one is covered at its summit by any overlying substance except diluvium ; and that those in the eastern part of our district were evidently not produced until the time at which the chalk and all the strata subjacent to it, in this district, underwent a simulta- neous elevation. V. DENUDATION PRODUCING VALLEYS. In a country that has been the scene of such tremendous convulsions and subterranean disturbances, it was probable that we should find on the surface abundant ruins, and dislocated fragments of the rocks that have been sub- mitted to such violence ; we should expect to discover masses of rubbish such as we see in the wreck of modern land slips, and which cannot but have been created in prodigious quantity along the line of the elevations and fractures we have been tracing: but on examination we find that all this wreck has vanished, and been so totally swept away, that scarce a trace of it can be recognised throughout the whole district which it must once have covered. It is obvious, from a mere glance at the Map, that the strata originally occupied larger areas than they cover at present; and that if no further opera- tions had taken place in the Vale of Weymouth beyond the elevation and frac- tures we have described, we should have had little more than a series of arches piled successively on one another, and extending over a large portion of the whole district; the angle at which the strata rise being in many parts so small that no very distant separation of the fractured parts could have attended their elevation ; and thus the central cornbrash of the Vale of Weymouth would have been arched over with bending strata of Oxford clay, coral rag, Kimmeridge clay, and Portland stone; and the Vale of Bredy and the Brid- port district would have been covered by nearly horizontal beds of greensand and chalk, connecting the great greensand escarpment of the north and east of the Vale of Bredy and Abbotsbury Castle with the outlying summits of Swyre Knoll, Shipton Beacon, Eype Down, Golden Cap Hill, Lewsdon Hill, Lambert’s Castle, and the entire group of insulated caps and ridges of green- VOL. IV.—SECOND SFRIES. G 42 Prof. Bucktanp and Mr. De ta Becue on the sand and chalk near Charmouth, Lyme, and Axminster. But as no such arches exist in the Vale of Weymouth, nor any such continuity of the green- sand strata in the vales of Bredy and Bridport, we cannot but infer that some adequate cause has produced the removal of the vast masses of materials which apparently must once have filled the spaces that are now left void ; and we see no cause adequate to the production of such an effect, except the denuding power of a mass of moving waters; a power which has removed more than it has left of the entire bulk of nearly all the strata that appear on the surface of this district, excepting the chalk. Again, if we look for traces of ruin and violence on the surface along the lines of fault, we find no such indications presented to us ; but however great may have been the dislocation and subterraneous changes of level, the out- lines of the surface are little affected by these changes: thus, our sections Pl. II. fig. 1, 2, 3, 4, 5, and 6, afford examples of the summits and sides of hills where we should be utterly unconscious, from the external form of the land, that the least derangement or fracture has ever affected the subjacent strata ; the general outlines are regular and rounded, as if no violent move- ments had ever occurred below, and all the ruins and piles of rubbish that must have been produced along the lines of elevation and fracture are swept clean, clear, and smooth away. If we traverse the great Ridgeway fault for fifteen miles, from one extre- mity to the other, we see along the whole surface scarcely an indication of its existence. Near Upway we have an obvious example of this fact, at the point where the road from Bridport passes down the chalky escarpment of the Ridgeway through one of those broad and sweeping dry combs which are so common in escarpments of chalk: having descended nearly to the bottom of the hill, where we should expect the outcrop of inferior chalk or greensand, we are surprised to find Portland stone rising to the north, and abutting against the chalk ; yet we see not the slightest change in the outline of the surface on either side of this line of fault, nor is there upon its south side a single remain- ing fragment of all the masses of greensand and chalk that must have been elevated into a new and high position on that side of the fault when the frac- ture took place; all traces of the enormous ruins that attended this great convulsion have utterly vanished and been swept away ; so that scarcely the residuum of an outlying fragment remains to attest the catastrophe that has taken place: the sloping sides of the combs glide regularly and gently down, as if they had been excavated in one undisturbed and uniform mass of con- tinuous chalk. Nor is this outclearing and total removal of the broken frag- ments peculiar to this comb on the north-west of Upway ; it is equally ap- Geology of the Neighbourhood of Weymouth, &c. AS parent in many others along the whole extent of the fault, particularly in the deep combs of Elwell, Bincombe, and Sutton Pointz, that lie successively adjacent to Upway on the east. The deep and numerous dry valleys on the surface of the chalk hills that bound our district partake of the general character of such valleys on the surface of the chalk formation throughout England; and have no peculiar features beyond those which they have derived from enormous volumes of water, retiring in all directions from the higher to the lower levels, and acting at all elevations and on all points to modify the previous forms of the surface of the earth. If we look for the cause of all this removal in any natural operations now proceeding within the district, we find not the shadow of any satisfactory explanation of that vast destruction of which it has been the scene. It is vain to appeal to the action of rivers, for in many parts where the denudation has been greatest, there is not even a streamlet, or a single spring. The greatest streams we have in the district are the two insignificant rivulets of the Wey and Bredy*. It is equally vain to appeal to meteoric agents, for we have a measure of the total amount of their effects in the fragments accumulated in the form of talus and land slips at the bottom of certain slopes and precipices, and in a few small accumulations of mud and sand in the low grounds. The only satisfactory solution we can find is in the waters of a violent inundation, and in these we think we see a cause that bears a due ratio to the effects that have been produced. * The only river in the Vale of Weymouth is the small stream of the Wey, which, rising suddenly at Upway, from a cross fracture in the Portland beds, runs about five miles from north to south, into the sea at Weymouth, crossing nearly at right angles all the different formations, as well as the hills and valleys that occur along its course, and receiving only a few tributary confluents from the west. The Vale of Bredy is traversed by the small river of that name, running west from the village of Little Bredy to the sea at Burton Bradstock. It is impossible to refer the excavation of these deeply denuded valleys and the removal of the broken strata to the flood waters of such streamlets, or to the agency of their waters accumulated into lakes by any imaginable series of barriers, which the bursting of such lakes may be supposed to have removed. The east and west portions of the elliptical valley of Sutton Pointz offer a good example of denudation, independent of rivers. The only stream within this valley rises on its northern side, upon the line of the great fault at the base of the chalk escarpment, and running direct across the shorter diameter of the valley, escapes through a broad denudation, which intersects the Portland stone that forms the south side of the ellipse. (See Map, and Pl. II. fig. 4.5.) We have a measure of the small amount of the excavating power of this streamlet cooperating with meteoric agents in a ravine five or six feet deep, and a few yards long, which the water has cut in a talus of chalk rubble, in which it begins its course. A similar ravine of much greater length, and about twenty feet deep, which occurs at the base of the chalk escarpment, on the south of Wantage, is there cut through G2 44 Prof. Bucktanp and Mr. De 1a Becue on the How far the causes of this inundation may be connected with the elevation of the strata in the immediate neighbourhood or in distant regions, is a sub- ject which at present we conceive it premature to enter into, further than to suggest that the relation of the one to the other may possibly be nearer than has been hitherto apprehended. DILuviumM. Although the excavation of valleys of denudation, and removal of broken strata has been so considerable in all this district, we have no proportionate accumulation of extensive and continuous beds of gravel. ‘The power and rapidity of the currents which could excavate the materials that filled such enormous spaces must have been too great to allow these materials to subside so near the spots from which they have been torn away, and must have drifted them far forwards into the prolongation of these valleys in the bottom of the English Channel, whence perhaps many of them may have been cast up again, and have contributed to form the Chesil Bank. The largest deposit of dilu- vium we have noticed is at Upway Street, four miles north of Weymouth; but in smaller quantities and irregular patches it is disposed over the whole surface of the country, on the summits and slopes of the hills as well as in the valleys. We have not heard of many organic remains in the diluvium of this district, but the following are sufficient to show their identity with those found in diluvial gravel in other parts of England. A few years ago a large rolled molar tooth of an elephant was cast upon the Chesil Bank, from the diluvium the chalk-marl with such regularity as to present the uniform width and uniform grassy slopes of the deep foss of a military fortification, and affords a similar measure of the amount of the power of existing agents on a substance of such uniform and perishable materials as soft chalk-marl. The following list of the temperature of springs in the neighbourhood of Weymouth was taken by Professor Henslow, with a good thermometer, in the year 1832 :— 20th August. Well at Chesilton, in Portland stone, near the middle of the ascent in the yard of the Portland Arms. A pump was used ......... sic feted he te ees 54° O! 24th August. Spring at Preston, by the road side, in the Portland sand ..........+. 53° of 28th September. Large spring at Upway, the source of the river Wey, rising suddenly in great force from a cross fracture of the Portland rock .........++- se ecenee 51° o! 20th Septemper. Pump at Corfe Castle ......... o, »(sielnae Cielo wr sinhy whine tene 52° 5! 20th September. Hill side (vertical strata), half way between Corfe and Worbarrow Bay, junction of chalk and sands ............e0e0- + olosntetetere, «exec ioadheleRedencrniete 52° 0! 4th September. Top of Headon Hill, Isle of Wight: spring from the upper freshwater formation, a few feet from the summit ........ eo ehente Stele cletete eked: neler Omar 5th September. Spring issuing from the sand rock under the fire-stone at Knighton... .51° 0! Where the temperature was taken in pump-water, it was not done until all the water that had filled the pipes was removed by long pumping. Geology of the Neighbourhood of Weymouth, §c. 45 beneath the sea, and is preserved at Abbotsbury by the Countess of Ilchester. Near Bridport also, at the villages of Burton Bradstock and Loders, the gravel has afforded the remains of elephants and other terrestrial quadrupeds. In the gravel that crowns the cliffs of lias, near the church of Lyme Regis, many teeth of rhinoceros have been found, and portions of the tusks of elephants ; and lastly, the cliff at the south termination of the valley of Char- mouth, where, as at Lyme, the lias is covered with a cap of diluvium, has afforded several nearly perfect tusks of elephants which tumble from the summit and get mixed with the debris of lias, when masses of the cliff are undermined, and fall down on the sea shore. A tusk nine feet eight inches long, from the gravel of this cliff, was some years ago in the collection of Mr. De la Beche, and is now in the Museum of the Geological Society *. Two molar teeth of elephant, one weighing twelve the other thirteen pounds, were found in this same cliff, in December 1832. ConcLusion. ‘ We shall conclude with pointing out the following general results that appear deducible from the facts we have been considering. We conceive that we have before us sufficient evidence of the following succession of changes in the state of that small portion of England which occupies the coast of Dorsetshire. ‘They are analogous to those deduced by Mr. Mantell from the phenomena he has described in the weald of Sussex. Ist, We have a succession of marine deposits, continuous from the lias up- wards through the oolites, and terminating in the deposition of the Portland stone ; during the period of all these formations our district must have been the bottom of an ancient sea: the presence of the remains of trees in the oolite and lias shows that land existed probably at no great distance from this sea; it is also probable that the waters were not very deep, in which Plesiosauri were so abundant as they must have been, to supply such numerous remains as we find imbedded in the lias at Lyme. 2ndly, The bottom of this sea appears for a certain time to have become dry land, and whilst in this state, to have been covered with a forest of large coniferous trees, and of Cycadeoideous plants that indicate a warm climate. We have a measure of the duration of this forest, in the thickness of decayed vegetable matter and soil, which has accumulated more than a foot of black earth around the roots of these trees. The regular and uniform preservation of this thin bed of black earth over a distance of so many miles, shows that * See Geological Transactions, Second Series, vol. i. p. 421—422. 46 Prof. Bucktanp and Mr. De 1a Becue on the Geology of Weymouth, &c. the change to the next state of things was quiet and gradual ; since the trees that lie prostrate on this black earth would have been swept away had there been any violent agitation, or sudden irruption of water. 3rdly, The dry land on which this forest grew became converted to some- thing like an estuary, in which the lowest deposits contain freshwater shells ; these are succeeded by a thick bed of oyster shells, and above the oyster bed are strata containing an admixture of freshwater shells with shells that are marine. We have evidence that this formation extended eastward from what is now the coast of Dorset, through the Isle of Wight to the eastern extremity of the weald of Kent; but of the boundaries of this supposed estuary we have not the slightest indication beyond that which is afforded by the existing deposits of Purbeck and Wealden freshwater formations. The occurrence of the Purbeck strata reposing on the Portland stone at Lady Down near Tisbury, on the west of Salisbury, in a position directly north of the [sle of Purbeck, at the distance of about thirty miles, renders it probable that the breadth of the estuary in this part extended over the inter- mediate portions of Dorset and Wilts, which are now covered up with chalk. Athly, We have a return of the sea over our estuary; and in this sea an accumulation of the successive and thick marine deposits which constitute the greensand and chalk formations. 5thly, We have in the Isle of Wight a reappearance of freshwater deposits mixed and alternating with others that are marine, through the next great periods of the tertiary formations. 6thly, All these deposits appear to have been succeeded by a tremendous catastrophe, producing elevations, depressions, and contortions of the strata ; and intersecting them with enormous faults. 7thly, These movements of the land have been succeeded by inundations, competent to excavate the valleys of denudation, and partially to overspread the country with diluvial gravel. Sthly, This denudation has been followed by a state of tranquillity, which has remained undisturbed to the present hour. 11.—Introduction to the general Structure of the Cumbrian Mountains ; with a Description of the great Dislocations by which they have been separated from the neighbouring Carboniferous Chains. By tHe Rev. ADAM SEDGWICK, V.P.G.S. F.R.S. &c. (WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. ) [Read January 5, 1831. ] § 1. Introduction. I HOPE, in a series of communications, of which this may be considered the introduction, to lay before the Society the results of observations made principally during the summers of 1822, 1823, and 1824, among the Cumbrian mountains, and the neighbouring districts of the North of England. All the central portions of the region, I propose hereafter to describe in detail, is composed of rocks of a date anterior to the old red sandstone, but its outskirts are covered by deposits chiefly of the carboniferous order. On the west side it is washed by the Irish Sea; and on the east it presses against, and, in part, blends itself with, the great calcareous chain which forms the separation of the waters descending to the coasts of Lancashire and Yorkshire. To the north it is prolonged, through an unbroken zone of mountain limestone, into the plain of the new red sandstone, stretching down the vale of the Eden ; to the south it sinks towards the shores of Morecombe Bay, and terminates in a succession of flat-topped elevations, crowned with precipices of mountain limestone—the remains of a calcareous ridge, once undoubtedly continuous from the higher part of the valley of the Kent to the southern extremity of Cumberland. It follows, from this description, and will be still more clearly seen by a glance of the eye over the north-west part of the geological map of England*, that the circular cluster of the mountains here described, presents, through the greater portion of its circumference, a nearly unbroken band of mountain limestone ; and on whatever side it is approached, we are struck with the tameness of the outline of every portion of the calcareous zone, when con- trasted with the fine serrated peaks of the loftier and more central elevations. * A new edition of Mr. Greenough’s Geological Map of England is now in progress, and will be shortly published. 48 Prof. Sepewick on the general Structure From some of the ridges in the range of Cross Fell, the eye takes in, at one view, the greatest part of the northern calcareous zone. Seen from that distance, all its minor inequalities disappear, and I have often fancied that it resembled a portion of a great semicircular redoubt formed near the base of the older hills, and presenting a long, sweeping, irregular glacis towards the valley of the Eden. On a nearer approach, an illusion of this kind must ne- cessarily vanish, and I only mention it in this place to convey a general idea of the external characters of the district, and of the relations of the great formations to each other. On the eastern side of the region, where the older rocks abut, as above described, against the great central calcareous chain, the contrast of external forms is perhaps still more striking. The calcareous mountains, though some- times cut down into mural precipices, and having individual features of the greatest beauty, and, though rising to such an elevation as to overlook the more ancient formations in their immediate neighbourhood, seldom exhibit any grandeur of outline, and in consequence of the horizontal position of their beds, often terminate in great featureless and somewhat tabular masses. On the contrary, the greywackeé hills on the confines of Yorkshire and West- moreland have their sides worn down into deep combes and irregular sinuosi- ties, and sometimes rise into sharp angular crests, forming outlines of great variety and beauty. Within the calcareous zone above described are several extensive masses of granite, syenite, and porphyry ; but the greatest part of the region is occu- pied by stratified deposits of a slaty texture, which may be subdivided into four distinct formations. Ist, Various crystalline slates, resting immediately on the granite of Skiddaw Forest, and forming the base of the whole stratified series. 2nd, Black glossy clay-slate, sometimes passing into greywacké, but containing no calcareous beds, and no organic remains. 3rd, Green quartzose roofing slate, associated, in every variety of complication, with felspathic rocks of porphyritic structure. This formation contains many beds effervescing briskly when first plunged in acids ; but it contains no continuous bed de- serving the name ef limestone, and no organic remains. 4thly, Greywacke slate, often more or less calcareous, and having subordinate beds passing into impure limestone, full of organic remains. We owe our first accurate knowledge of these subdivisions to Mr. J. Otley of Keswick, who not merely described them in general terms, but gave their geographical distribution with a very near approximation to accuracy*. * See an early Number of the “ Lonsdale Magazine,” and “ A Guide to the English Lakes,” by Jonathan Otley of Keswick. of the Cumbrian Mountains. 49 In subsequent communications I hope to prove: Ist, That the crystalline unstratified masses form the true geological centres of the mountain groups ; and that by their protrusion the schistose formations have been elevated into the position they now occupy. 2ndly, That a true mineralogical axis may be traced through the inferior divisions of the slate rocks on each side of which the successive formations, as far as they are clearly developed, are arranged symmetrically. 3rdly, That the beds of these formations, when we exclude irregularities arising from local causes, have a nearly constant strike from a few degrees north of magnetic east to a few degrees south of magnetic west. And, lastly, That all these peculiarities of structure and position originated in causes brought into action at a period anterior to the existence of the old red sandstone. On these several subjects I wish, for the present, to avoid any further de- tails: I may, however, be permitted so far to anticipate the materials of a future communication as to describe the range of the remarkable calcareous beds, interposed between the green quartzose roofing slate and the greywacké slate. Such a description will place in a clear point of view the kind of evi- dence by which we determine the strzke of the slaty masses, and will at the same time make us acquainted with a succession of dislocations which have considerably modified the external forms of the Cumbrian mountains. It will also form a natural introduction to the description of a second system of dis- locations, by which, at a later geological epoch, these older mountain groups were snapped off from the central carboniferous chain, and brought into their present almost insulated position. § 2. Range of a band of Limestone and Calcareous Slate, between the Quartzose Green Slate and the Greywacké Slate, &c. &c.* This band is full of organic remains, and is separated by masses of enor- mous thickness from all other caicareous strata with which it could possibly be confounded: moreover, it occupies, as before stated, a place intermediate between two entirely distinct formations. Hence, although varying in thick- ness from 30 or 40 to 200 or 300 feet, it can be easily followed ; and in the places where its continuity has been broken by great internal movements, we can generally, in imagination, reunite the disjointed portions, and calculate the amount of their dislocation, without running the very common risk of mis- taking one bed for another. The most western appearance of the limestone is at Beck, a farm in the * See Plate IV. VOL. IV.—SECOND SERIES. H 50 Prof. Sepawick on the general Structure division of Cumberland called Millam. Thence it ranges through Corn Park, over the Knot, into the Low House grounds; and, after crossing a marsh, reappears in the same range above Water Blain, and terminates at the foot of the village called Hill,—the mean bearing of the beds in the whole of this range being about north-east by east, and the dip south-east by south. Here we lose all trace of the limestone ; but after ascending several miles up a rivulet, we find, immediately above Graystone House, among the hills to the east of Duddon Bridge, a bed of limestone, identical in dip and range with the one we had left behind. Moreover, the Graystone House limestone is very nearly in the exact prolongation of the band of transition limestone on the other side of the Duddon. Hence we may conclude that the Graystone House and Water Blain limestones belong to the same formation, and have been severed by an enormous fault, descending nearly in the direction of the valley of Hallthwaite. ‘The quantity of dislocation estimated in the direction of a perpendicular to the two parallel lines of bearing cannot be less than two miles*. Such a disruption of great mountain masses is not a little startling to the imagination; but I may state, by way of explanation, that many of the neigh- bouring mountains are penetrated by dykes of porphyry and syenite, probably of the date of the eruption of the Bootle granite, and that the whole region of Black Comb, which belongs to the oldest slate formation, has probably at the same period been thrust out of the bowels of the earth, and elevated into a position out of all symmetry with the structure of the neighbouring region. The country between Millam and Duddon Bridge is, therefore, one where we ought to look for the evidence of enormous dislocations ; and this evidence is placed before us in the most impressive manner by that break in the con- tinuity of the limestone, and that great lateral movement which I have just described. The beds of the Graystone House limestone would, in their prolongation, * It is right to state that there is a difficulty in identifying the Graystone House and Water Blain limestone, arising out of the mineral character of the overlying slates. In general we can easily separate, even by hand specimens, the greywacké slate of the highest group from the green slate under the limestone. But at Graystone House this is not possible, as the overlying slates are in structure almost identical with those of the inferior group. Hence some one might conclude that the Graystone House limestone formed no part of the calcareous band described above, but was an accidental mass subordinate to the series of the lower green slate. There is not, J think, much force in the objection; for there are other places where portions of the two slate groups cannot be mineralogically distinguished: and, after all, it merely shifts the difficulty, as we shall have (on this supposition) to interpolate an enormous fault, somewhere on the line of the Duddon, in order to explain the position of the corresponding calcareous bands on the opposite sides of the river. of the Cumbrian Mountains. 51 strike the south end of the range of hills on the north-east side of the Duddon ; the limestone is not, however, found in those hills, but appears, with its usual characters, and the same mean line of dip and sérake, in the lowlands on the east side of the ridge. From this I conclude that a break of the strata passes down the valley of the Duddon, accompanied with a lateral movement, not however comparable in extent to the one last noticed. The further range of the limestone is well defined by the following localities, viz. Hartley Ground, Lum Holm, Broughton Mill, and thence up the bed of the river to Stock- beck*. The limestone preserves an undeviating strike and dip; and in consequence of the sinuosities of the channel, is seen, here and there, above the mill, on different sides of the river. At Stockbeck the river bifurcates, and the limestone runs along the north-west side of the eastern branch, close to Appletreethwaite, where there is a transverse fault, throwing the pro- longation of the limestone, about a hundred yards further to the north. ‘This apparently lateral movement has no effect on the direction of the beds, which preserve an almost perfect parallelism ; but it produces a slight deviation in the direction of the rivulet. From Appletreethwaite the limestone continues its course (about 70° or 75° east of magnetic north), and making a very slight deflection to the north- east, passes on that side of Ash Gill quarries. Thence ranging over Torver Fell, and across the rivulet, it passes along the line of the Seathwaite road, and reaches one of the flanks of Coniston Old Man; up which it rises to a considerable elevation, and in a plane nearly parallel to the steep side of the mountain. On reaching the north side of Broadway Beck (one of the streams descending from the mountain), the limestone is again cut off by a great transverse fault, which appears to throw it to a point about 300 yards south- east of its line of bearing. After reappearing in Scrow pastures, it ranges through a wood, descends down the north side of Mealy Gill, passes close to Old Mill, south of Silverbank, and thence close to the road, and at the foot of a great precipice, to Low Yew Dale, from which place it is prolonged across the low grounds to a point close to Yew Tree. Here it is cut off by the great precipice of Raven Crag, and a vast transverse fault has pushed whole mountain masses of green slate * There can be no doubt of the identity of the Millam limestone with that which ranges through the places enumerated in the text. Hence (though the Graystone House limestone, in consequence of the difficulty alluded to in the preceding note, be excluded from the range), we must at least suppose that the Water Blain and Hill limestone bands were once continuous with that of Hartley Ground. But this supposition is quite incompatible with the general strike of the beds, unless, as stated in the preceding note, we interpolate an enormous fault along the line of the Duddon. H 2 52 Prof. Srepewick on the general Structure and felspathic rock so far out of their line of bearing, that we are compelled to make a southern traverse to a knoll above Coniston Hall (a distance of more than a mile), before we can discover the broken ends of the beds of lime- stone. The line of fault appears to be prolonged down the valley, nearly in the direction of Coniston Water Head. From the knoll above mentioned the limestone ranges, with a slight devia- tion from its mean direction, through the hills which overlook the Tarns, and descends to a point, close to the separation of the Skelwith and Ambleside roads. Here the great masses of green slate, which had before encroached on the strike of the beds, are suddenly thrown back at Pool Beck Scar, and the limestone beds are cast, at a single heave, about a mile and a half to the north of their former line of direction. This enormous fault, though it pro- duces a considerable influence on the configuration of the neighbouring country, is in one respect an exception to a general rule, inasmuch as its di- rection is not marked by any valley. In this part of the range the country is much covered with alluvial matter ; but the continuation of the line is nearly defined by the lime quarries of Holmes House, the beds under Pool House, and the old limeworks on the north shore of Pool Wyke. Seen from Pool Wyke the quarries of transition lime- stone on the east shore of Windermere are not more than 10° north of true east; but had they been on the prolongation of the mean line of range, they would have appeared about 35° north of the same point. From this we may, I think, conclude, that there has been a break between the opposite shores of the lake—that the beds, on the east side, have had a considerable movement towards the south—and that the valley of Windermere, like all the other great valleys cutting through the limestone range, has been scooped out upon a line of fracture. From the quarries about 400 yards above Low Wood Inn, on the east shore of Windermere, the limestone beds range through the woods, and pass just under Dove Nest, and on the north side of High Skelgill, near which place they are expanded over a considerable surface, the rise of the mountain side being nearly parallel to the plane of stratification. They are prolonged in a direction a few degrees north of magnetic east, through the extreme ramifications of the rivulet which runs down to Low Wood, and thence to the top of the hill overhanging the village of Troutbeck. From this point the range of the limestone on the opposite side of the valley, near the high pass leading to Kentmere, is distinctly visible, and bears about 15° south of mag- netic east. Now this change of bearing is exactly the opposite to that which might have been expected ; especially after remarking the great elevation of of the Cumbrian Mountains. 53 the pass before mentioned : for the beds being all inclined at a great angle, and rising to the north-west, we have reason to look for the most northern portions of their range at the points of highest elevation. This fact makes the change of bearing above mentioned still more striking, and convinced me, before I descended from the hill, that there was a great fault ranging down the valley of Troutbeck. On this subject we are not left to mere inference, for the limestone beds descend the hill on the north side of the village, range through a point about 150 yards above the junction of the two roads, and are traced to a small coppice near the river side, called Intake Wood. Near that place they are cut off by a fault ranging down the river, which has caused a great movement towards the south in the whole system of beds on the opposite side of the valley. We are therefore compelled to descend about three quarters of a mile before we can catch the broken ends of the beds we have left behind. After being concealed in the alluvion of the valley, the beds again break out behind Line Foot, and, ascending rapidly towards the north, with the inclination of the hill, pass for some way on the north side of the Kentmere road. At the top of the hill they range on the south side of the road, in a direction difficult to ascertain in such uneven ground, but approaching mag- netic east. In descending the hill towards Kentmere Hall they appear to be dislocated, and shattered by a complication of faults, and one great mass ranges down the brow, in a direction about 45° east of magnetic south. This very anomalous bearing is accounted for partly by the movements of dislocation, and partly by the great angle of dip and inclination of the surface. Another disjointed mass of limestone ranges nearly in the mean bearing behind the Hall, but is cut off by a fault before it reaches the chapel. Lastly, the beds in regular order, beyond the faulty ground, cross the rivulet (with their usual dip and strike) about 400 yards above the bridge, through the fields of Head Lane farm. From this place the beds rise into a ravine in the edge of Pike How, and thence over the top of the hill, through a point about 200 yards south of the mountain road. to Long Sleddale, and so down the hill to a place called Till’s Hole. By taking, from Till’s Hole, the bearing of the corresponding beds on the other side of Long Sleddale, we find that the limestone strikes the oppo- site hills at a point several degrees out of its previous bearing ; which fact pro- bably indicates the passage of a fault also down this valley. Everything is however obscured by alluvion near the banks of the river; and if there be any shift of position among the mineral masses in their strike across the valley, it must be of comparatively small extent. 5A Prof. Sepewick on the general Structure On the east side of Long Sleddale the beds of limestone are seen crossing a rivulet, about 200 yards above the houses called Little London; and from that place they may be traced up the southern branch of the same rivulet (called Tron Crow Gill), for nearly half a mile, in a direction about north-east by east. They then disappear under great accumulations of turf-bog, and alluvial mat- ter, and are not again seen. Some peculiar felspathic rocks on which they rest, and some thick beds of blue flagstone, by which they are surmounted, may however be traced through a morass on the top of the mountain: there can, therefore, be little doubt that the limestone beds are also continued past the north side of a hill called Lord’s Seat, and thence into the turf-bogs on the east side of Yarlside Crag, to a place not more than a mile and a half from Wastdale Head. Had this system of strata met with no interruption, it would, after a further range of about four miles, have abutted against the zone of mountain lime- stone. It is, however, cut off by a great boss of granite, which has deranged the relative position, and changed the mineral structure of all the neighbour- ing rocks: from which we may, I think, safely conclude, that the granite of Wastdale Head (commonly called Shap granite), did not assume its present position till some period after the formation of the transition limestone. I have been the more minute in these details because they enable us clearly to establish a series of important facts in the geological history of the Cum- brian mountains. First. They prove, that at a very ancient epoch, and probably during the principal period of elevation, great cracks were formed, diverging from the centre of the mountains, accompanied by great changes in the relative posi- tion of the mineral masses on the opposite sides; and further, that these cracks prepared the way for future valleys*. Now the principal valleys of these mountains diverge towards all parts of the circumference, from a centre near the high crests of Sca-Fell. Is it not, therefore, probable (though in the absence of beds of limestone, like those above described, we cannot establish the fact on direct evidence), that great lines of dislocation pass down the greatest number of these valleys? In making this supposition we merely * The usual appearance, on the opposite sides of the faults above described, is exactly that of a great horizontal lateral movement, and is not, I believe, by any means entirely deceptive; for expansive forces of elevation acting on oblique planes, might easily produce such a movement. The effect was probably of a compound kind. When beds are highly inclined, a mere subsidence on one side of a fault will, however, produce on the surface the exact appearance of a horizontal slide. It is not, therefore, always possible, especially in the absence of underground workings, to determine the exact direction of the movements which have accompanied a fault. of the Cumbrian Mountains. 55 assume that similar effects have been produced by similar causes acting within a very limited region. And, if this hypothesis be admitted, we can advance a step further, and point to the probable origin of these great diverging fissures: for the valleys start from a central region, which is violently broken, where the dip and range of the stratified masses is unsymmetrical, and which is marked by protruding mountains of granite and syenite. Secondly. Notwithstanding the great dislocations of the masses of green slate and porphyry, forming the support of the limestone, there is hardly any instance in which they are bent and contorted. After seeing the violent contor- tions of some portions of the other slate systems of the region, this fact might appear inexplicable ; but we find a solution of our difficulty in the enormous irregular masses of hard unbending felspathic and porphyritic rocks, im- bedded in, and so intimately mixed with, the green quartzose slate, that we in vain seek to separate the formations from each other. If, then, we admit the igneous origin of the porphyries, in what way can we account for the accompanying, and apparently almost contemporaneous, deposits of stra- tified chloritic slate? I know no explanation so probable as that which sup- poses igneous and aqueous causes to have acted together—the porphyries to have been produced by some modification of submarine igneous action— and the chloritic slates to have been deposited from the waters in the same region, and in the same periods of time: the first operation supplying, at least in part, the materials for the second, and similar operations being many times repeated. Thirdly. The previous details enable us clearly to determine the mean line of bearing of the whole system of stratified rocks associated with the lime- stone; and this line makes the schistose masses, one after the other, to abut against the carboniferous zone. ‘This fact alone proves that the older and newer systems are entirely unconformable—a conclusion confirmed by all the sections which connect the slate rocks with the calcareous zone. Again: There is no gradation between the two systems ; their position is not only unconformable, but the transition from one system to the other is instantaneous. Masses of red conglomerate are found here and there, near the base of the older mountains, resting upon the edges, and filling up the inequalities of the component strata, and upon these conglomerates are depo- sited the lower beds of the carboniferous limestone. These facts seem to prove, that the elevation of the cluster of mountains of Cumberland was sud- den (which seems to be almost implied by the great faults and dislocations above described, as well as by the regularity of the lines of bearing), and that all those causes which produced the elevation of the older strata, and deter- 56 Prof. Sepawick on the general Structure mined their line of bearing, had ceased to act before the completion of the old red conglomerates. In the region above described there is no connexion between the direction of the valleys and the mean line of bearing of the formations ; and one of the means successfully used by M. Elie de Beaumont in grouping together distant mountain chains, would, in this instance, entirely fail us. I do, however, think that the leading doctrine of the Essay on the Epochs of Elevation (viz., that mountain chains elevated at the same period of time have, even when widely separated from each other, a general parallelism in the bearing of their com- ponent strata), receives a strong confirmation from the position of the older formations of the British Isles. It is now generally allowed that the old chains of mountains, mainly com- posed of clay-slate and greywacké, which give so great an impress to the physical character of this island (viz., the chains of Cornwall, of North Wales, of the Isles of Man and Anglesea, of Cumberland, of Lannermuir, including the whole range from St. Abb’s Head to the Mull of Galloway, &c. &c.), are nearly of the same age, and were probably all elevated before or during the period of the old red sandstone. Now if a line be drawn along the axis of the Cornish chain ; a second parallel to the prevailing ranges of the higher Welsh mountains, as laid down in Mr. Greenough’s map; a third in the direc- tion of the strata of Anglesea ; a fourth in the axis of the greywacké chain of the Isle of Man; anda fifth from St. Abb’s Head to the Mull of Galloway ; all these lines will make a near approach to parallelism with the line of bearing in the system of the Cumbrian mountains, as established by the previous details. Is this parallelism accidental? I am unwilling to believe it; and although there are even in England some remarkable exceptions to this arrangement, I think that the facts here stated afford, as far as they go, a confirmation of that principle on which are founded many of the bold generalizations of the extraordinary essay of M. Elie de Beaumont, to which I have alluded. § 3. On the Great Dislocations by which the Cumbrian Mountains became separated from the Central Carboniferous Chain, &c. The internal movements which produced the derangement of the groups of strata described in the preceding section were succeeded by a long period of comparative repose, during which our whole carboniferous series was elabo- rated. Had our island been laid dry immediately after that period, without any change of relative position among the great formations, the Cumbrian moun- tains would have appeared as a cluster of ancient rocks rising out of a great carboniferous plain; extending north and south from the border of Scotland to of the Cumbrian Mountains. 57 the very heart of England, and in a transverse line from the Gerinan Ocean to the Irish Sea, and as far west perhaps as the Isle of Man. The remains of the carboniferous strata in the northern and central parts of England, not- withstanding the manner in which they have been dislocated, and afterwards covered up by newer deposits, justify us in giving them this great original ex- tent, and thus bringing them almost to the confines of the carboniferous system of the Bristol Channel. This carboniferous period (during which we have no indications of great internal movements producing mountain masses with their strata in discordant positions), was immediately succeeded by some of the most remarkable convul- sions which have affected our island. During these convulsions, took place some of those extraordinary dislocations of the coal measures on the confines of the Bristol Channel (so admirably described in former memoirs read before this Society *), and also the elevation of the great northern central chain, extend- ing from the neighbourhood of Derby to the mouth of the Tweed: and during the same period the calcareous zone surrounding the Cumbrian mountains was torn off from that part of the great northern chain, which, after deflecting a little to the north-west, is prolonged through the crests of Cross Fell to the confines of Scotland. I only mention the carboniferous system of the Bristol Channel for the pur- pose of founding upon it one or two general remarks, and of contrasting it with the northern chain of the same period. First. The axes of the different coal basins on the Bristol Channel seem to form a striking exception to the rule above quoted, viz., that regions of contemporaneous elevation are marked by parallel lines of bearing. Among the axes of these basins there is certainly no such parallelism. Secondly. As the calcareous slates of North Devon and of a part of South Wales do not conform to the rule which appears to govern the range of the greatest number of our greywackeé chains; but, on the contrary, run nearly east and west, in a direction parallel to the axis to the great elliptical coal basin of South Wales ; is it not highly probable that the anomaly was caused by the extension to North Devon and a part of South Wales of the same forces which produced the actual configuration of that basin? Or, in other words, may we not conclude, that the great elevatory movements of the grey- wacké series of North Devon and of a part of South Wales took place after the completion of the carboniferous series ; and, therefore, many ages after the * See the sections accompanying the Memoir by Messrs. Buckland and Conybeare, Geol. Trans., New Series, vol. i. p- 210, &c. VOL. I1V.—SECOND SERIES. I 58 Prof. Sepewicx on the general Structure movements which produced the strike and dip of the Cumbrian mountains as above described ? Thirdly. The form and direction of the dislocations in the coal fields on the Bristol Channel bear little resemblance to those of the northern carboni- ferous chain—a circumstance probably originating, partly in the local nature of the disturbing forces themselves, and partly in the fact that the application of these forces in the two carboniferous regions was not contemporaneous. After the first elevation of the central carboniferous chain of the north, the lowest division of the new red sandstone group (rothe-todte-legende) was immediately deposited. The movements of elevation were not merely followed by, but were probably the mechanical causes of, this deposit ; which is com- posed of sand, small pebbles, and other incoherent materials, drifted to the outer and lower edges of the coal-fields ; even at this day is in many places but imperfectly cemented; and contains, though rarely, a few drifted coal plants*. In some districts it is perfectly conformable to the upper coal strata on which it immediately rests, and seems to form a regular connecting link between them and the overlying formations ; but, considered on the whole, its position, as far as regards the inferior strata, is discordant. It was followed, and perhaps interrupted, by movements of elevation, producing a considerable derangement in its component beds, and, of course, also affecting the lower formations ; and these movements were succeeded in several parts of York- shire, and of the Cumbrian mountains, by deposits of magnesian conglo- merate and magnesian limestone—unconformable both to the lower division of the new red sandstone (rothe-todte-liegende) and to the coal measures +. Now the overlying deposits of the Bristol coal-fields are perfectly analogous to the series in the North of England, which commences with the magnesian conglomerate ; but they appear to contain no representative whatsoever of the lower division of the new red sandstone. Hence we may, I think, conclude (not hypothetically, but on direct physical evidence), 1. That the movements which gave the final configuration to the coal-fields on the Bristol Channel took place after the deposition of the lower red sandstone, and were probably contemporaneous with the second system of movements in the North of En- gland, before alluded to. 2. That the movements (prior to the existence of the lower red sandstone or rothe-todte-liegende) which gave the chief impress * See Geol. Trans., Second Series, vol. iii. p. 64. Traces of vegetable fossils occur in this deposit, on the coast of Cumberland, near Whitehaven. Stems of Equiseta and other vegetable impressions have also been found in it at Hickleton in Yorkshire, by the Rev. W. Thorp of Don- caster. I was unacquainted with these facts at the time the Memoir just quoted was composed. + See Geol. Trans., Second Series, vol. iii. Pl. VI. figs. 3. 4. 5. 6. of the Cumbrian Mountains. 59 to the carboniferous chains of the North, took place during a time long an- terior to the principal dislocations of our south-western coal-fields*. Fourthly. Though the contortions of the carboniferous system of the Bristol Channel are so very extraordinary, the actual elevation of the beds is much less than that of the northern chain. This is perhaps the reason why the secondary rocks, from the new red sandstone to the chalk, have in their range from the south coast to the latitude of Derby, a direction nearly parallel to the mean bearing of the greywacké chains—that is, the very direction they would have had, provided they had been deposited immediately on the flanks of the greywacké chains, without the intervention of the carboniferous series. Thus, for example, the principal line of transition limestone in South Wales is nearly parallel to the direction of the great oolitic terrace in the corre- sponding latitudes. In making this observation (which must not be pushed too far), all minor inequalities are, of course, left out of account, as well as the changes of bearing produced by much more recent disturbing forces—such, for instance, as the great saddle of the wealds of Kent, and the east and west range of the vertical chalk through the Isle of Wight and a part of Dorsetshire. Now if we follow the same secondary beds beyond the latitude of Derby, we find a sudden change in their direction, bringing them nearly into paral- lelism with the great central carboniferous chain of the North. From which . it appears, that this chain was of sufficient magnitude to produce, by its eleva- tion, a great change in the bottom of the neighbouring seas, and, conse- quently, to produce an immediate influence upon the direction of all the strata afterwards deposited, by the same seas, upon its flanks. Leaving the consideration of subjects which may appear remote and hy- pothetical, I now proceed to describe the nature of some of the greater dislo- cations produced by the elevation of the northern carboniferous chain. The disturbing forces, acting with their greatest intensity in a direction nearly north and south, commenced in the latitude of Derby, and produced their first effects towards the north in elevating the High Peak limestone and the coal-fields on its eastern flank. They are marked by a system of great lon- gitudinal faults ranging on the west side of this limestone region ft. * I am aware that this conclusion has been objected to by some of our best geologists, but I do not believe that they have personally examined the whole evidence on which it rests. t See Pl. V. fig. 1. Some interesting phenomena connected with these faults are described in Farey’s Geological and Agricultural Survey of Derbyshire. The accompanying section is not intended to convey any details of stratification, but only a general notion of the position of the great mineral masses. The toadstone beds of the High Peak limestone are intentionally omitted. 12 60 Prof. Sepewick on the general Structure Continuing the range towards the north, the elevatory forces seem to have operated more feebly, as the limestone is not brought up to the surface. But their line of action is, in some places, marked by an irregular saddle of mill- stone grit, forming the water-shed between our eastern and western coasts. The great saddle of millstone grit at Blackstone Edge, flanked by the Lanca- shire and Yorkshire coal-fields, is a good example of this arrangement*. A few miles further towards the north the mountain limestone is again pro- truded: the chain gradually arises to a commanding elevation, and is continued as far as Stainmoor, preserving throughout a great similarity in its external forms, and an almost perfect identity in its internal structure. Near that part of this range where the carboniferous mountains begin to present a decided escarpment towards the west, commences a great longi- tudinal fault (or perhaps a system of faults), which has been traced by Mr. Phillips from the heart of Craven to the hills near Kirkby Lonsdale, and ex- cellently described in a paper published in a former volume of our Trans- actions}. I must refer to this paper for the proof that the great Craven fault has rent asunder a part of the carboniferous chain, and produced such a down- cast on the west side, that mountain masses of limestone are tumbled into the neighbouring regions with an inverted dip ; and that a coal-field which ought to appear above the top of Ingleborough, has sunk below the level of its base f. From beneath this coal-field the limestone beds again rise up, and after passing in the form of a great arch over Farlton Knot, recover their hori- zontal position, and are prolonged into those tabular hills mentioned above, which form the south-western skirt of the Cumbrian mountains. From which it appears, that the southern calcareous zone of the Cumbrian system, is cut off from the central chain by the intervention of the great Craven fault. I once imagined that this great fault ranged through the neighbourhood of Kirkby Lonsdale and Farlton Knot, and there terminated. It is unques- tionable that lines of dislocation do range in the direction here indicated (as is proved by the position of the limestone of Kirkby Lonsdale bridge; and the still more remarkable position of the limestone between Casterton and Bar- bon); but after several subsequent visits to the neighbourhood, I found that the leading branch of the Craven fault ranged along the line of junction of the central chain with the skirts of the Cumbrian system, passing along the south flank of Casterton Low Fell, up Barbondale, thence across the valley of Dent, through the upper part of the valley of Sedbergh, and along the flanks * See Pl. V. fig. 2. + See Geol. Trans., Second Series, vol. iii. p. 5—15. t See Pl. V. fig. 3. of the Cumbrian Mountains. 61 of Bawfell and Wildboar Fell, to the ridge between Mollerstang and Raven- stone dale ; and that along the whole of this line there are enormous and most complex dislocations. Some of these phenomena I hope to describe more at length in a future communication ; and for the present I only observe, that a great upheaving force acting at once upon the two contiguous and uncon- formable systems, produced a great strain and separation of parts, accompanied with fractures and dislocations, principally along the line of their junction*. In a part of the range between Mollerstang and Ravenstonedale the cluster of the older mountains, by deflecting to the north-west, quits the central car- boniferous chain ; and it becomes a question of some consequence to deter- mine the further range and nature of the great Craven fault. The ruptures produced by it are fortunately on a scale too great to be overlooked or mis- understood. It ranges through Mollerstang into the hills immediately south- east of Kirkby Stephen, and thence skirting the escarpments which trend towards Stainmoor, finally stops near the foot of the mountain-pass. Its pro- gress is marked by a lofty ridge of carboniferous limestone, which has been upheaved from the very base of the whole system, contorted and shattered, and then sent headlong into the valley, where it is to be seen on edge for many miles ; and where its lower extremities lie buried under accumulations of alluvial matter and the horizontal conglomerates of the new red sandstone f. In following these dislocated ridges in the opposite direction, we may trace them into the calcareous hills of Ravenstone dale, where they expand them- selves and assume a more horizontal position, and in this way gradually pass into the unbroken calcareous zone which skirts the north side of the Cum- brian mountains as far as Egremont. Thus, it appears that the northern and southern calcareous zones of the Cumbrian mountains are cut off from the central chain by the same fault, which, both in the neighbourhood of Ingle- ton and Kirkby Stephen, has produced a great downcast on the western side of its rangef. So far it appears that we have a clear and consistent explanation of the re- * See Pl. V. figs. 4. 5. T See the southern extremity of the section, Pl. V. fig. 7. t See Pl. V. figs. 3.7. The effects produced along the line of dislocation on the lower beds of the carboniferous system vary with the circumstances of the case. Where the beds abut against the steep sides of the greywacké chain, their broken ends have undergone a movement of elevation. Under such circumstances a depression like that at Ingleton, or the still more eom- plex derangement of the strata, like that in the valley above Kirkby Stephen, was obviously im- possible. See Pl. V. figs. 4, 5. These two figures are ideal ; the former being intended to repre- sent the undisturbed, and the latter the disturbed, position of the greywacké and carboniferous series. 62 Prof. Sepewick on the general Structure lations of the central carboniferous chain to the secondary zones of the great cluster of the Cumbrian mountains. But there is still one difficulty to be explained. Beyond Stainmoor, the western border of the central chain de- flects, as before stated, considerably towards the north-west, and rises into an escarpment, partly made up of mural precipices, which overlooks the plain of the new red sandstone in the vale of the Eden, and in the crest of Cross Fell reaches the elevation of 2900 feet. On the contrary, the northern calcareous zone of the Cumbrian system dips under the plain of the new red sandstone, and along the course of the Eden, lies buried probably many hundred feet below the surface. This relative position is explained in a transverse section from the central mountains to the ridge of Cross Fell: and it seems impossible to account for the collocation of the two carboniferous systems without the intervention of a faudt ranging somewhere near the base of the chain of Cross Fell, and producing an enormous upcast to the north-east*. ‘The misappre- hension of this fault formerly introduced a great error into certain published sections, in which the new red sandstone of the Eden was placed wnder the whole system of Cross Fell t. Fortunately in this, as in the former case, we have better evidence than a mere inference ; for in following the escarpment from any portion of the Cross Fell chain to the foot of Stainmoor (the key of the whole position), we have a manifestation of the true nature of the fault, and on a scale hardly to be rivalled in any other part of our islandf{. A little before we reach Brough, there commences a steep craggy mountain ridge, ranging parallel to the prin- cipal escarpment; from which it is separated by a ravine several hundred feet in depth. On entering this ravine, we find ourselves on the very line of an ancient convulsion, by which the whole craggy ridge has been torn off from the escarpment, and tumbled over into the valley, in which it now stands on edge; every part of it being inclined at a very great angle. It is of vast thickness, and probably includes nearly the whole calcareous system of Cross Fell: but its upper beds are buried under the alluvion of the new red sand- stone. These inclined beds (on a part of which stands the town of Brough) are prolonged to the foot of Stainmoor, and thus brought into contact with the dislocated beds thrown down from the opposite side of the valley by the great * See’ Pl. V. fig. 6, { See a paper by Professor Buckland (Geol. Trans., First Series, vol. iv. p. 105), in which this mistake is rectified. { There are some other places near the base of the carboniferous chain where we meet with in- dications of the‘nature of the Cross Fell fault. (See Geol. Trans., First Series, vol. iv. Pl. V. figs. 2 and 3.) But in none of them is the evidence comparable to that exhibited in the Brough section. of the Cumbrian Mountams. 63 Craven fault. The transverse section from the hills above Brough to the hills above Kirkby Stephen, shows the singular relations of these dislocated masses™*. It thus appears, that during the elevation of the central carboniferous chain of the North, there were great changes of level among the component strata, —and that the points of greatest stress not being upon the same straight line, the fractures were sometimes inclined to each other—that the great Craven fault and the great Cross Fell fault, intersecting each other at a considerable angle near the centre of the chain, shattered and cut off from it a great trian- gular mass of the component strata—and that this triangular mass, being thus cut off by the disruptive forces of elevation, underwent a change in its rela- tive level, and was at the same moment affected by a great downcast move- ment; of which we have a most convincing proof in the present extraordinary position of the mineral masses at the foot of Stainmoor, and on the line of section. I am far from supposing that in the preceding details I have pointed out all the great movements whereby our northern mountain chains have been af- fected. All I have attempted to do has been to explain the nature of certain great dislocations of which we have direct evidence, and of which we can determine the geological epoch ; and thence to show the general effects they have produced on certain mountain groups in the North of England. If I wished to speculate on the causes of these great movements among the integuments of the mountains, I should point to the porphyries of the Cheviots and the syenite of Charnwood Forest, rising at the two extremities of the carboniferous chain. I should also point to the granitoid rocks near Dufton Pike; and perhaps also to the Whin Sill, and the other masses of augitic trap, associated so largely with the calcareous system of Cross Fellt. If it were objected, that the porphyry of the Cheviots sometimes resembles the old felspathic rocks of Cumberland, and sometimes passes into syenite and granite ; and further that we have proofs of its existence before the conglo- merates of the old red sandstone: we might on the other hand reply, that such facts throw no difficulties in the way of supposing, that the Cheviot por- phyry (like some of the other crystalline formations of Scotland), was elevated en masse at some period subsequent to its first formation ; especially as we can show, to the north of the Tweed, derangements exactly answering to such an elevation. We might further reply, that the red porphyries of the Scotch Border, however like each other in mineral structure, are not all of the same * See.Pl. V. fig, 7. + See Geol. Trans,, First Series, vol. iv. p. 109, &c. 64 Prof. Sepewick on the general Structure age ; inasmuch as some of them are unequivocally posterior to a portion of the coal measures. The discussion of these subjects would, however, lead me too far from the direct object of this paper*. Many of the great movements above described, appear to have been pro- duced by an action both violent and of short duration. The nature of the fractures leads us to this conclusion, as well as the nature of the mineral masses resting immediately upon the dislocated beds. In some portions of our coal-fields there may be indications of a passage into the next superior order of formations. But in the neighbourhood of the great faults above described, there is certainly no such indication, or anything whatever which could mark the slow progress from one system of things to the other. That these great fractures were produced by some modification of volcanic action is, to say the least of it, a very probable hypothesis. But, granting this hypothesis, what proper measure can we set up for the intensity of vol- canic power during any one geological period of the earth, except that which is defined by the effects produced? Guided by this rule we assume nothing : and though we fall into error from hasty generalizations, our conclusions, unfettered by theory, are ever open to correction ; and as observations are multiplied, gradually approximate nearer and nearer to the truth. Of the cause of volcanic action we know nothing ; but we know enough of * At Rodham, a few miles from Wooler, the carboniferous series is separated from the Cheviot porphyry by an old red conglomerate forming the base of the stratified rocks. The conglomerate contains many pebbles identical in structure with the porphyry, which must therefore have existed before the carboniferous series: and the conclusion is confirmed by similar phenomena in Roxburgh- shire. Judging, however, from the inclination of the stratified masses, we should, I think, be led to infer, that the porphyry had undergone some movement since their deposition. A porphyry perfectly identical with that of the Cheviots, in the same range, and sometimes passing into a true granite, breaks out in Lamberton Hills, a few miles north of Berwick ; and near Shiels runs down close to the coast. At this point the red sandstone (subordinate to the old carboniferons formation of the Tweed), which forms the sea cliff, suddenly becomes vertical, and in some places is moved more than 90° from its undisturbed position. ‘The phenomena are correctly described in a paper published by Mr. Witham in the Newcastle Transactions: but the important fact of the close approach of the granitoid porphyry appears to have escaped his notice. It seems to prove, unequivocally, that the Lamberton porphyry assumed its present position after the epoch of the carboniferous system of the Tweed. 1 mention these apparently contradictory facts for the purpose of showing, how difficult it is to prove the age of igneous rocks by any single set of phenomena. Trappean rocks are very abundant in the higher parts of the Tweed, and have a great simila- rity of mineral structure ; yet it is generally impossible to come to any certain conclusion respect- ing their epoch. At Cowdenknows (a few miles north-east of Melrose), a red porphyry distinctly overlies a red sandstone similar to that in the lower course of the river. of the Cumbrian Mountains. 65 the effects of this action to be certain, that it cannot be ever brought under the mechanical laws of any constant force. ‘To assume therefore, indepen- dently of an incomparably wider induction from facts than has yet been made, that volcanic forces have acted on the earth during all geological periods with equal intensity, is so far from being sound philosophy, that it is a mere gratuitous assumption—founded, it may be, upon a mistaken analogy be- tween the calculated effects of constant forces, and the effects of other forces, which are not only not constant, but which are unknown in their origin and undefined in their power. Judging from facts alone, and independently of all hypothesis, I adopt some of the leading principles of the Essay on the Epochs of Elevation by M. Elie de Beaumont, to which I before referred. They are certainly cpen to nu- merous exceptions ; especially in low geological regions like many of those in our Island. But among mountain chains which are well defined and of considerable elevation, they are, I believe, of very extensive application and of unquestionable importance. The two systems of dislocations, described in the second and third sections of this paper, mark two epochs of elevation which have had a great effect in modifying the structure of this Island. Note.—1 hope I may be excused in very briefly anticipating some of the conclusions which seem to follow from a detailed examination of the Cumbrian mountains. 1, The crystalline structure of some of the slates appears to have been superinduced after their deposit by an action from below. This seems to be certain, as far as regards a zone of indurated slates which surrounds the boss of Shap granite; and it is at least a probable explanation of the crystalline structure of the lowest group of slate rocks in Skiddaw Forest. 2. There are, in many large tracts of the Cumbrian system, slate beds with a decided transverse cleavage, alternating with coarse flagstone and grey- wacké, and not associated with any igneous or unstratified rocks. Similar facts are repeated in North and South Wales on a more extended scale, where the slates sometimes pass into true chlorite slate, alternating with other unal- tered slaty masses. In such cases we have no right to assume that the crystal- line structure has been produced by any modification of igneous action. Hence it appears to be a rash generalization to attribute the crystalline structure of all primary slate rocks to direct igneous action. This negative conclusion is further confirmed when we consider that secondary deposits, by the mere chemical action of their particles, unaided by any igneous cause, sometimes assume a perfectly crystalline structure. For example; many beds of moun- VOL, IV.—SECOND SERIES, K 66 Prof. Sepewick on the general Structure tain limestone are perfectly crystalline ;—and the large globular structure of magnesian limestone has occasionally been superinduced on masses originally deposited in thin lamine; as is demonstrated by the fact, that the lines of the original lamine may still, in some instances, be traced through a congeries of balls mutually compressing each other. ‘These peculiarities of structure are found in places where there is not the least indication of any igneous action. 3. The highest greywacké group of the Cumbrian mountains contains beds with numerous organic remains. The next inferior group (composed of green slate and porphyry), and the third group in the descending order (composed of fine, black clay slate and greywacké slate, &c.), contain no organic remains. How can we account for the absence of organic remains in this third group, except on the supposition that they did not exist in the seas where it was de- posited? It is developed through large mountain tracts, and is, with very few exceptions, composed of rocks unaltered by igneous action. Had there been any organic beings where it was deposited, we should, I think, have found their remains imbedded in it. We arrive at precisely the same conclusions in traversing the whole slate system of Devonshire and Cornwall. The upper part contains organic remains; the lower part does not. Yet in the lower part there are large tracts where the rocks are unaltered, and contain beds of limestone and calcareous slate, not more crystalline than ordinary beds of mountain limestone. The same positive and negative conclusions are strengthened by the phenomena of North and South Wales. I may state generally, as the result of my own observations on the older strata of this Island, that there is a line in the descending series where organic remains seem entirely to disappear ; and that this line is by no means coordinate with mineral changes superinduced by igneous action. It is true that igneous action has in many cases produced a crystalline structure in stratified masses, and obliterated their organic remains : but it is not by any means true that this action always accounts for the absence of organic remains from the older strata. 4. 'The ancient separation of the old schistose deposits into two great groups (the upper containing organic remains, and the lower not,) appears, therefore, to be borne out by the phenomena of our Island. This separation is, how- ever, on two accounts, of very little importance. First, Because the two groups almost entirely interchange mineralogical characters. Secondly, Be- cause, between the two extremes, there appears to be an enormous develop- ment of rocks, in which organic remains (though appearing here and there) are very rare. Hence it must always be difficult, and oftentimes impossible, to draw any precise line between the two groups in question. 5. I believe, however, that there is a broad mineralogical distinction be- tween the primary stratified rocks (including under that term all stratified rocks inferior to the old red sandstone,) and the secondary,—and a still broader, of the Cumbrian Mountains. 67 between the primary stratified groups and the deposits superior to the chalk. In some instances secondary rocks have put on the exact appearance of the primary: but is there a tertiary deposit in any country yet examined, which could for a moment be confounded with the greywacké systems of Cumberland or Devonshire? Through large regions of the earth, the epoch of many deposits is not less defined by the mineral structure of the rocks than by their organic contents. Accurate mineralogical distinctions, and an order of superposition determined by natural sections, must form the first foundations of the geology of every country. Organic remains often help us to unite together disconnected base lines. They also enable us to subdivide the successive de- posits of one epoch, in cases where all other means fail; and in speculating on the former conditions of the earth they are invaluable: but they can in no instance supersede the necessity of studying in detail the structure and superposition of the great mineral masses composing the crust of the globe. 6. In the Cumbrian system, the elevation of the old slate rocks appears to have been produced by the protrusion of mountain masses of granite and syenite. In the higher parts of North Wales, the strata are thrown into vast undulations ranging parallel to the principal mountain chain; but we find no obvious centre of dislocation. This fact however throws no difficulty in the way of the igneous hypothesis of elevation ; as we know that the most violent volcanic action is often felt at a great distance from the focus of eruption. The parallelism of the undulations seems however to prove, that they were not produced by different shocks of earthquakes succeeding each other after long intervals of time. As the earth has apparently diminished in temperature, we have a right to look for some indication of a contraction of its dimensions. May not some of the great parallel corrugations of the older systems of strata have been pro- duced by such a partial contraction ? 7. In stating that volcanic action could not be brought under the laws of any constant force, I merely made a reference to the irregular and undefined nature of its effects. The degradation of the solid portions of the earth by aqueous action may in a certain sense be considered constant ; because there is a demonstrable provision in the laws of nature for the perpetual circulation of water over the surface of the globe. But who can point out, compatibly with the known laws of chemical action, a provision for the eternal and uni- form circulation of volcanic fire through all parts of the crust of the globe— to go its rounds with regularity, and, during given periods of time, neither to increase or diminish in intensity? If such a supposition be started, it can only be regarded as a mere gratuitous and most complicated hypothesis ; and ought not ever to be assumed as the basis of @ priori reasoning. K 2 68 Prof. Sepewicx on the general Structure of the Cumbrian Mountains. Every case of volcanic combustion may be only an instance of chemical combination on a great scale ; in which case, after it ceases, the particles acted on are held together by new affinities more powerful than those which existed among them before, and are in a new condition of chemical equilibrium. Each successive instance of volcanic action must bring the crust of the earth nearer and nearer to a state of ultimate chemical quiescence: volcanic fires like all other fires must exhaust themselves; and must cease entirely, when the whole crust of the earth has reached its highest state of oxidation, or when the solid parts are in that state of combination which represents the highest order of chemical affinities compatible with the physical constitution of the earth. Whether the earth is ever actually to reach that state, is a question not affecting the hypothesis, and, of course, admits of no reply. Or we may argue on another hypothesis—that volcanic action is produced by the penetration of water through the surface of the earth, to a liquid mass of highly heated matter far below. Even in this case there must be some che- mical action: for we know that unoxidized bodies are always present ; and if these produce some influence on volcanic products, they must also produce some influence, however small, on the intensity of volcanic force. Let us, however, exclude the effect of chemical action altogether ; still, volcanic action must diminish in frequency and intensity, during the evolution of the succes- sive geological periods, by the mere refrigeration of the earth (a fact implied in the terms of the hypothesis), and by the greater difficulties offered to the penetration of water through the parts which have gradually become solid. Perhaps, however, it is best to exclude all hypotheses, and to acknowledge our entire ignorance of the cause of volcanic action. In that case we have no right to assume, that it either is, or is not, of the nature of a constant force. To assume either the one side of the question or the other is perfectly gra- tuitous ; as it can only be decided by induction from the geological pheno- mena of every known epoch. As a matter of observation, modern volcanic forces appear to have modified the earth in two ways. First, by violent paroxysms, splitting up the crust of the earth, and producing lines of volcanic vent (such as those described in the works of Humboldt and Von Buch), generally of small curvature, and extend- ing through great geographical regions. Secondly, by local action on the great lines of vent, producing all the ordinary phenomena of volcanic cones and eruptions of lava. To the former kind of action, the forces which have produced the elevation of some of our mountain chains appear to have been most nearly assimilated. Walton, May 18233. Appendix to Professor Sepawick’s Paper entitled “An Introduction to the General Structure of the Cumbrian Mountains.” [Read November 6, 1833.] IN the preceding paper, p. 49 et seq., describing in detail the range of a band of limestone and calcareous slate separating the upper from the middle division of the schistose rocks of the Cumbrian mountains, I have mentioned two great faults, between Coniston-water Head and Windermere; one throwing the calcareous beds to the south, and the other to the north, of their line of bearing. Both these faults are of enormous magnitude, and the calcareous slate between them, ranging about 40° north of true east, past two or three small mountain tarns, terminates in some broken masses, just where a cross road strikes off from the Ambleside turnpike to Skelwith bridge; being there cut off by the most northern of the two great faults above mentioned. This part of the range is about a mile and a half in extent; and the calcareous bands, commencing in a low hill north-east of Coniston Hall, exhibit some disloca- tions which, although of comparatively small extent, deserve notice. About one third of a mile from their commencement, the calcareous bands are cut through by a fault, throwing them fifty or sixty feet towards the south- east. The line of dislocation is marked by a small watercourse, and by some masses of calcareous slate thrown out of their bearing. The beds then regain their strike (about 15° north of magnetic east), and run to a round hill, due south of the lowest tarn. There they are again cut off, and shifted about 150 or 200 yards, to a point south-east of the tarns. Thence they range (nearly with the same strike as before) uninterruptedly for more than half a mile; increasing, however, gradually in dip as they approach a mountain mass of green slate and porphyry, called Pool Brow. Immediately beyond a mountain road leading to Arnside, there is a third dislocation, throwing the beds about 120 paces to the south-east. Beyond this interruption the limestone is again continued, but is soon after (in consequence, I believe, of a number of small dislocations), spread over the brow of a hill (Lemestone Hill), and descends to the angle of the Skelwith bridge road, the extreme point being marked by a kiln on the Knipe Fold estate. Here the limestone bands are again cut off, being thrown (as stated in p. 52) more than a mile to the north of their bearing. 68* Appendix. Such details as these may be considered of small importance, but they belong to the history of the formation I am describing. There are, however, other phenomena of more importance, and extremely well exhibited along the line just described. The calcareous slates sometimes pass into strong beds of limestone: but without exception they exhibit true cleavage planes, which often almost obliterate the lines of stratification ; and the calcarecus beds (even where they pass into a pure subcrystalline limestone), when struck with the hammer, break into tabular masses, having their faces parallel to the cleavage of the slates. These calcareous beds abound with Corals, Bivalves, Trilobites, &c., and have a south-easterly dip, varying from 30° to 60°. The planes of cleavage generally dip toward the north-west, at a great angle. They sometimes strike with the beds, and sometimes cut obliquely through them; but I could not find any instance where the planes of cleavage and the true beds coincided. I stated (in the paper before mentioned, p. 54) that the calcareous bands were cut off by the Shap granite, and the assertion was, I believe, true: but during the past summer I ascertained that these bands reappear, in their line of strike, on the north side of the granite boss, in the new road cut through the morass; from Shap Wells to the turnpike leading to the village of Shap. The same calcareous bands appear also in the rivulet, about a quarter of a mile north of the wells, nearly with the strike and dip above mentioned, and so pass under the horizontal beds of the old red sandstone and conglomerates which form the base of the mountain limestone ridges, stretching out on the north side of the district. It deserves remark, that the calcareous slates are broken through by porphyritic masses, but reappear in the form of calcareous conglomerates imbedded in the greywacké. These conglomerates are im- pregnated with pyrites, and give rise to the mineral waters of Shap Wells. It appears, therefore, probable, from what has been already stated, that the Shap granite interrupts the continuity of the calcareous bands, and is there- fore of an origin posterior to them. The same truth is rendered probable by the extreme induration of the upper greywacké series, where it approaches the granite. The conclusion is, however, put out of all doubt by a fact I observed for the first time, this summer; viz. that near the farm-house called Wasdale Head, the granite is in two places seen to send veins into the greywacké; which near its contact with the granite passes into a rock, very much resembling the more crystalline varieties of the Cornish killas. ‘These phenomena, taking place among the upper fossiliferous divisions of the slate series, are of considerable theoretical importance ; but I shall not dwell upon them, as I shall have to return to the subject in a subsequent paper. {1].—Description of a Series of Longitudinal and Transverse Sections through a Portion of the Carboniferous Chain between Penigent and Kirkby Stephen. By tHe Rev. ADAM SEDGWICK, V.P.G.S. F.R.S. &c. (WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. ) [Read March 2 and 16, 1831.] § 1. Introduction. HAVING in the preceding communication pointed out some peculiarities in the position of the great central carboniferous chain (which extends from the neighbourhood of Derby to the Scotch Border), with the view of connecting it with the calcareous zone of the Cumbrian mountains ; I now proceed to describe in detail the composition of a very remarkable portion of it, forming a mineralogical link between the High Peak of Derbyshire and the region of Cross Fell. ‘The facts adduced will serve to explain some of the changes the chain undergoes in its range between one extremity and the other; and will also supersede the necessity of many details respecting the carboniferous zone of the Cumbrian mountains, which once formed, beyond doubt, a continuous part of the same system, and is now only separated from it by the great breaks and dislocations described in the preceding paper. The principal section * about to be described, commences at Penigent in Horton parish, and, passing through the highest mountains of the range, ends in the plain of Kirkby Stephen. T'wo other sections} connect this line with the ridge of mountains on the west side of Swaledale. Nearly at right angles to the same line are drawn a series of transverse sections+, prolonged across the breaks connected with the great Craven fault. They will, I hope, place in a striking point of view some of the internal movements which took place when the chain was elevated, just before the period of the new red sandstone. The old red conglomerates do not appear in any part of the longitudinal section, but they are exposed in one of the transverse sections§, and are seen * See Plate VI. fig. 2. + Fig. 3. and 4. t Fig. 5. 6. 7. 8. and 9. § Fig. 8. 70 Prof. Sepe@wick on the Carboniferous Chain in several other places, at the junction of the carboniferous chain with the unconformable greywacké mountains of Westmoreland. ‘There can, there- fore, be no doubt that the lowest beds of the carboniferous system of this region rest upon an irregular surface of unconformable greywacke slate, from which they are separated, here and there, by great irregular masses of old red conglomerate. | The whole overlying series is essentially composed of alternating masses of limestone, sandstone, and carbonaceous shale, terminating in a great system of beds connected with the millstone grit. The limestone groups are incom- parably the most continuous and the best defined, and form a kind of frame- work by which all the other component parts are held together. They are six in number, and will be referred to in the several sections, under the fol- lowing names :—Ist, Great scar limestone. 2nd, Black marble limestone. 3rd, Strong post limestone. 4th, Wold or Mosdale Moor limestone. 5th, Four- fathom limestone. 6th, Main, or twelve-fathom limestone. The names given to the Ist, 5th, and 6th groups are in common use in, the North of England, and on that account ought not to be changed. The other three groups might be conveniently designated in the section by the names 2nd, 3rd, and 4th limestones: but these names would cease to have any propriety if applied to remote parts of the same chain, and therefore ought not to be made use of, except in local description. To prevent a frequent repetition of nearly similar details, I shall commence with an enumeration and description, in the ascending order, of all the re- markable groups of strata which appear upon different parts of the lines of section. § 2. General Section of the whole System, in the ascending order*. 1. Great Scar Limestone. otal thickness about 600+ feet.—The term scar, in the dialects of the North, means any bare precipice on the face of a mountain, and is applied with great propriety to this limestone, which in all parts of its range is marked by grey precipices and mural escarpments. The grey scars near the base of Ingleborough, of Penigent, and of Whernside ; the mural precipices above Giggleswick and Malham, and the magnificent cavernous gorge of Gordale, are among the striking exhibitions of this de- posit, and present a nearly exact counterpart to the features of the same lime- stone in the High Peak of Derbyshire. * See Pl. VI. fig. 1. + This number is merely approximate, and there are only a few places where the whole thick- ness is visible. It is probably very variable, as the deposit has taken place upon an uneven, un- conformable surface. from Penigent to Kirkby Stephen. va Like the Peak limestone, the group, here described, is full of fissures and clefts (often of unknown depth), in which the mountain torrents are engulfed ; and, after running in subterranean channels, and uniting with the waters of other sources, emerge in copious streams in the lower regions of the neigh- bouring valleys. But of all the phenomena connected with the drainage of the waters through the scar limestone, the beautiful reciprocating well above Giggleswick is the most remarkable, and even to this may be found a counter- part among the limestone hills of Derbyshire. It contains, like the limestone of the Peak, many caverns of consider- able extent ; some partly open to the surface, others only to be approached through a narrow horizontal entrance. In some of these great subterranean recesses we find waterfalls of no common grandeur; in others we see no waters, but we hear them roaring among the inaccessible chambers of the rock. Asa general rule, these caverns have perpendicular walls, and often nearly flat roofs. However greatly modified, they have, therefore, not been formed by the mere long-continued erosion of the waters passing through them. When the conformation is such as I have pointed out, the opposite walls are portions of the same stratum, and the flat roof is composed of the superincumbent stratum ; and the cavern has the exact appearance of having been formed by one of the beds sliding off horizontally from the side of a ver- tical joint. Ido not think such a movement impossible. The component strata, when first lifted up, were perhaps in a very unequal state of solidifica- tion, so that one part would offer a greater resistance in any given direction than another. The points of greatest stress might also be very unequally dif- fused ; and, in consequence, the strata may have started among themselves, and undergone considerable relative movements, not unlike those we may observe among the timbers of a ship which has been wrecked, and thrown violently on her beam ends. In this way some caverns may have been formed by the sliding of solid beds upon each other, some by the gradual removal of incoherent or imperfectly solidified portions of the rock, and others by both causes combined. The subject is one of considerable difficulty, and I wish to exclude no agent from its proper share in producing the existing appearances. All I contend for is, that in such cases as I have alluded to, the slow erosion of the waters flowing through the interior chambers of the scar limestone is not the kind of action by which its great caverns have been scooped out. The mineral characters of the scar limestone are too well known to be detailed at any length. The great bottom shales found in so many parts of England are almost entirely wanting in the line of section, and in the neigh- bouring country. Perhaps they are represented, in a very obscure form, by some dark-coloured beds of impure limestone, separated by bands of shale, Wes Prof. Sepewick on the Carboniferous Cham which occur here and there at the base of the series. In the same position are rarely found some dark and nearly compact beds, resembling the black marble series, but unfit for use; and in the prolongation of the longitudinal section towards the north (for example, near Ravenstonedale and Kirkby Stephen), beds of reddish sandstone alternate with the lower portion of the sear limestone, and the whole group begins to approximate to the type of the Cross Fell chain*. There are no bands of coal subordinate to the limestone on the sectional lines ; but carbonaceous and bituminous matter are the colouring principle of all the darker beds. In some instances this colouring matter is so unequally diffused, that after a recent fracture, or on a polished surface, it appears in the form of dark cloudy blotches upon a light grey base. It is this arrange- ment of colours, arising out of the irregular diffusion of the bituminous matter, which constitutes the beauty of some marbles in the North of England f. Near the line of section, however, no beds appear in this limestone which are fit for polishing, and very few indeed which are well suited to the commonest domestic architecture. In general they have an irregular fissured or shaken texture, which unfits them for such uses. It is, perhaps, hardly necessary to add—that their prevailing colours are light grey or bluish grey, from which they change, through every variety of shade, into dark blue, or biuish black —that their mineral characters are such as link them to transition limestone —and that they contain in great abundance corallines, encrinites, and all the ordinary well-known fossils of the carboniferous limestone f. The highest beds of this group often become impure, and, for about thirty or forty feet, alternate with beds of sandstone and calcareous shale; in this way forming a gradual passage into the next superior group. 2. Group of Sandstone and Shale. Greatest thickness 150 feet. The thickness of this group is extremely variable, being in some places not more than twenty or thirty feet: but when it is best developed, it appears to admit of the following subdivisions :— (a.) Dark-coloured shale, with nodules of clay iron-stone. * In various parts of the North of England, where the bottom beds of the scar limestone rest immediately upon greywacké, they contain rolled pebbles of the inferior rock, and occasionally pass into a coarse conglomerate form. (See Geol. Trans., Second Series, vol. iii. p- 10, &e. &e.) This structure seems to have originated in the last feeble efforts of those causes which in other places produced the great masses of old red conglomerate. t The Beetham Fell marble, near Milnthorpe in Westmoreland, is the most remarkable instance of this kind, and it is subordinate to the great scar limestone. { Some of the rare corallines, described by the late Mr. Parkinson, were collected from loca- lities near the line of section. See “ Organic Remains,” vol. ii. Pl. VI. fig. 9. &c. &c. from Penigent to Kirkby Stephen. 73 (b.) Alternations of sandy, micaceous shale, and brown, micaceous sandstone, generally of a coarse, flaggy, or slaty structure. (c.) Strong beds of hard, micaceous gritstone, alternating with similar masses of slaty texture, and generally surmounted by a few beds of meagre, sandy shale. Wherever the shale beds abound, the thickness of the whole group is ex- tremely variable. The micaceous flagstones of the middle portion are some- times wanting, and the group is then composed of carbonaceous shale, iron- stone, and gritstone. One of the finest exhibitions of this group is at the waterfall of Hardraw Scar near Hawes. It is also well exposed by the many torrents which descend from the mountains on both sides of the valley of Dent. 3. Second Limestone, or Black Marble Group. Greatest thickness about 45 feet; average thickness about 30 feet. This group is distinguished from all the rest by the regularity of its strati- fication, which often makes it look, on the face of a precipice, like a rude work of masonry ; also by its dark-coloured, compact beds with a conchoidal fracture*. Some of these beds take a beautiful polish ; and when they can be raised in large slabs free from white spots, and without seams or cross joints, are of considerable value. Unfortunately many of the quarries are almost spoilt by the cracks and fissures which traverse all the component strata: and many of the more solid masses are injured by the imbedded or- ganic remains (such as Encrinites, Caryophylliz, Producte, Spirifers, &c. &c.), replaced by pure white carbonate of lime containing little of the carbon and bitumen which form the dark colouring matter of the rock. The thin bands of bituminous shale, separating these limestone beds, also contain organic remains ; and, among the rest, innumerable specimens of the Producta latissima and P. Scotica, which may be almost considered as charac- teristic of this group. Nearly all the quarries, in the neighbourhood of the lines of section, from which the black marble has been exported, are found in the valley of Dent. I have however traced them, in the exact position here indicated, through Horton parish, on both sides of Chapel Je Dale, in Kingsdale, and in Gars- dale. They may be also traced through a part of Wensleydale, and appear at the top of the precipice of Hardraw, over which tumble the waters of a mountain torrent, forming one of the grandest waterfalls in the North of England. They are there however so much changed in structure, that they * Most of the beds before polishing have a bluish tinge, and their weathered surfaces are of a greyish colour. On being burnt, they are reduced to a beautiful white calx, all the colouring bi- tuminous matter being driven off. VOL. IV.— SECOND SERIES. L (C3 Prof. Sepewick on the Carboniferous Chain are only identified by their relation to the other groups, and by beds of the Producta latissima and P. Scotica which follow them. 4. Group of Sandstone, Shale, and Calcareous Grit, &c. Maximum thick- ness 150 feet; average thickness about 60 or 70 feet. The arrangement of the subordinate parts of this group is extremely vari- able, as the different masses frequently seem to replace each other. In an approximate way the group may be subdivided as follows. (a.) Dark-coloured shale, with one or two bands of crow-limestone or cal- hard. (6.) Hard beds of brownish, siliceous grit, generally of a somewhat slaty texture ; containing subordinate, strong, hard beds of a calciferous grit, some- times ferruginous. (c.) Alternating bands of hard, brown, flaggy grit and shale. The beds of calciferous grit are extremely characteristic of this group, and are sometimes so expanded as to form a prominent part of it. Within they are of a greyish colour; but their weathered surfaces are generally brown, from the presence of iron. The quantity of calcareous matter contained in them is very variable, as they pass at one extreme into pure, close-grained, siliceous grit; and at the other, where organic remains are abundant (which is however rarely the case), into a nearly pure limestone. The crow-limestone or calliard is not so characteristic, as it is, here and there, subordinate to all the great masses which alternate with the six groups of limestone. It may however be proper to explain these synonymous pro- vincial terms, as they will be frequently used in the following details. They are applied to a very impure variety of shelly limestone which is sometimes associated with gritstone, and then passes irregularly into calciferous grit, but most frequently is subordinate to the beds of dark-coloured shale. In the latter position it sometimes appears in the form of concretions ; but more fre- quently in irregular bands, seldom more than one or two feet in thickness. The outer surface of this crow-limestone is very irregular, and is generally covered with a thin, earthy coat of hydrate of iron. It is very ponderous, in parts reaching the specific gravity of the nodules of argillaceous iron ore. It is difficult of fracture ; but when broken almost always shows a bluish, cal- careous interior; and rarely has a core of nearly pure limestone. It contains innumerable organic remains, especially large specimens of a species of Producta ; and from the crescent-shaped impressions of that shell, the miners sometimes designate it by the name of horse-shoe limestone*. It * The specific characters are generally obscure; but I believe the large Productz belong chiefly to the species Producta Scotica. from Penigent to Kirkby Stephen. 75 is obvious, that it owes its existence to the accidental presence of beds of shells (chiefly of the genus Producta), during the deposits of the great masses of shale—that these shells supplied a considerable portion of the calcareous matter—and that they also caused the precipitation or separation of the ferru- ginous and pyritous matter, and of the other constituents commonly found together in these calliards. In the upper division (c.) of the group here described, there is in some places a band of coal: but as it is in general not more than a few inches in thickness, it has never been worked to any profit*. 5. Strong Post Limestone. 'Thickness nearly the same as the black marble series (No. 3.), averaging about 30 feet. This group, in its mode of bedding, in its colour, and in the dark bands of shale which alternate with the strata, nearly resembles the black marble system. The beds are however stronger, thicker, and coarser ; and though generally unfit for polishing, afford a beautiful material for the construction of door- posts, small pillars, coignes, coping-stones, &c.+ I have traced this group in the position here indicated, through the flanks of Ingleborough, Penigent, and Whernside; all round the valley of Dent; through the upper part of Garsdale ; and through a part of the chain of hills between Wensleydale and Swaledale. There can, therefore, be no doubt of its continuity through all the country bordering on the southern and central part of the principal section. 6. Alternations of Fissile Gritstone and Carbonaceous Shale. Greatest thickness 150 feet ; average thickness about 120 feet. The alternations are indefinite ; but on the whole the group may be conveniently separated as follows. . (a.) Alternations of gritstone and shale; the gritstone sometimes rising in strong beds ; but more frequently micaceous and of a flaggy structure. (6.) Carbonaceous shale and gritstone with a band of coal ; also with two thin bands of crow-limestone or calliard. (c.) Hard, brown, and light grey, micaceous grit, with bands of shale ; the micaceous grit in some places highly fissile, and forming a good roofing slate. The most important bed in this group is the coal in division (5). It is ex- * TI have been informed that works were formerly opened in this bed at Load Gill on the south side of Dent, and also on the north side of Garsdale, but with very little success. + Attempts have, I believe, been made, but without success, to polish some of the darker beds containing many very small encrinital stems. A small, dark-coloured, encrinital marble, found in Derbyshire, and other parts of the carboniferous chain, is provincially called bird’s-eye marble ; and is occasionally found subordinate to the black marble group. i be 76 Prof. Sepewick on the Carboniferous Cham tensively worked in the Barbon and Casterton liberties, where it is about fourteen inches thick. The lower part of this bed is however so impure, as to be unfit for domestic use, and is chiefly consumed in lime-works*. An attempt is now making to work the same bed in the adjoining liberty of Dent. It is also worked at Stoth pits near Hawes, in Baw Fell above Sedbergh, and at Kitchen Gill on the side of Naitby Fell near Kirkby Stephen ; and there are many traces of old works in the same bed near Garsdale Head{. Iam certain that in all these places the coal is very nearly on the same geological parallel. It must therefore have been very widely extended. But it was by no means continuous, as is proved by innumerable sections through this group, which perpetually varies in its composition, and in which there is often no indication whatsoever of the coal-bed. It deserves remark that the two thin calliard beds appear to be continuous for many miles. The slate-beds in division (c.) are next in importance. They have been extensively worked in several places ; especially at Wydern and Kirkbank in the valley of Dent: but the most beautiful example of these beds is in Cow Gill, about five miles above the village, where there is a quarry of hard, white, siliceous grit capable of being split into very thin flags, coated with silvery mica, and forming the most beautiful roofing slate I have seen in the carboni- ferous chain. 7. Mosdale Moor or Wold Limestone§. Average thickness from 30 to 40 feet. * Section, in descending order, from the shaft of the Barbon coal-pits :— Feet. Inch. Feet. Inch. ils ANIME Roll, 85 coooa0gado0e 52 5. Alternations of gritstone and shale 12 0 2. Plate (calcareous shale) ...... 1 6 Goo haley. icis .sareieierietete svccssvees 30: 0 3. Limestone (the fourth, or Mosdale 7. Crow-limestone....... sieroieietels 20 Moor limestone, of the general 8. Plate, with a three-inch crow-coal 1 6 SECION) Wiatelsienerehcitaieues oe ielele 21240 OF IGritstonewlrcmi siete ieleis = 27.0 10: UC Galle isia epetetotekioteeiieir: Po Oi Ly G2 The crow-limestone (No. 7.) more commonly appears in the form of two distinct bands sepa- rated by a bed of impure, pyritous shale. In this section, the beds seem to have run together ; probably by the partial disappearance, or thinning out of the pyritous shale. + The attempt was unsuccessful, and the works have been deserted since the above passage was written. { I have been informed that the coal of Kitchen Gill is eighteen inches thick; but I have seen no accurate sections of the works. In the places where it has been most worked the average thickness of the bed is not much more than a foot. § The group is known in some of the valleys under the name of Wold-limestone: as, however, this word designates any tract of dry green pasture land rising out of the morasses of the carboni- ferous chain; and as this kind of soil marks, more or less, the range of all the calcareous groups; the term wold is a bad distinctive name for any one of them. from Penigent to Kirkby Stephen. ig This limestone is less regularly bedded than the two preceding groups (Nos. 3. and 5.). The bottom beds are generally of a grey colour and of an open, shaken texture. They are frequently surmounted by two or three coarse, strong beds of a grey colour, not to be mineralogically distinguished from the most ordinary varieties of the great scar limestone, containing various fossils, apparently distributed without regularity. The higher beds become thinner, more compact, and sometimes contain many encrinital stems, and are occasionally of a dark colour. In the highest part of the series, the beds alternate with bands of dark shale, become impure and ferruginous, and frequently pass into the state of crow-limestone or calliard, with many large Product. Detailed sections of this division would, no doubt, offer many modifications ; but few quarries have been opened in it, since it contains no beds of any pe- culiar value, and many parts of it are obscured by alluvial accumulations. It may, however, be tracked without any difficulty, wherever it rises to the day, along the sides of all the mountains which range near the lines of section ; as well as in all the various systems of valleys which branch among the moun- tains between Askrigg and Kirkby Stephen. It has indeed been important to make out its continuity, as it forms the roof of a series of beds to which the Barbon coal seam is subordinate (No. 6. (5.)) 8. Alternations of Sandstone, Fissile Gritstone, and Shale. 'This is by much the most remarkable of all the groups alternating with the beds of lime- stone. Its greatest thickness is perhaps as much as 350 feet; and its average thickness in the central and southern parts of the section is about 200 feet. Like all the other masses composed of sandstone and shale, it is extremely variable in its structure, the subordinate parts either disappearing or replacing each other. In some places the alternations are indefinite: but on the whole it admits of the following approximate subdivisions. (a.) Alternations of slaty, micaceous gritstone and shale, sometimes con- taining bands of crow-limestone. (b.) Shale with bands of gritstone. (c.) Micaceous, fissile gritstone with thin bands of shale, and with subordi- nate masses of coarse gritstone. There are very fine quarries in the lower division (a.), especially at Raw- thay Gill (between Ravenstone Dale and Sedbergh), where in colour the gritstone somewhat resembles the Pennant stone of Bristol; but is more micaceous and fissile, and generally of a more open grain. In the higher part of the upper division (c.), the fissile beds have been extensively worked 78 Prof. Sepewick on the Carboniferous Chain for roofing slate and flagstone, (e. g. Garsdale Hall pastures, High Pike in Dent, and all round the upper precipices of Ingleborough, &c. &c.) They are generally of a dark bluish grey colour, and are liable to decomposition. Round Ingleborough they are however of a brownish grey colour, and of a closer texture. Strong beds of grey sandstone occur in the lower part of this division (c.); which sometimes, though very rarely, become of so coarse a texture as to resemble millstone grit. Two thin bands of bright coal have been found (at Rawthay Gill and Ingle- borough), one in the lower (a.) and the other in the upper division (c.) of this group: and between Brough and Stainmoor (to the north of the line of section) it contains a bed of coal, which has been worked to a considerable extent. In some of the hills near the head of Wensley Dale (e.g. Stag’s Fell near Hawes, &c.) the shale-beds almost disappear; and the group passes into a complex deposit of hard, grey, micaceous gritstone, some parts of which afford a good building-stone, and other more fissile parts, a material for flagstone and roofing slate. 9. Four-fathom Limestone. Notwithstanding the name by which it is de- signated in the mining districts of the North of England, this limestone group is of much more variable thickness than any of the three preceding (Nos. 3. 5. 7.): but I believe that it in no instance entirely disappears. In some places it is not more than ten or twelve feet in thickness; in others it is much more ex- panded, and is not less than thirty or forty feet thick. Changes ranging within these limits are several times repeated, as may be proved by tracing these beds through the mountains at the head of Dent and Garsdale. Its average thick- ness in these regions is perhaps less than that which is indicated by its name. The bottom of the series, as usual, is impure, and is deposited in irregular, grey beds with traces of fossils. "The middle portion is much more regularly bedded, and contains innumerable fossils, especially encrinital stems. Indeed, where the middle and upper portions of this group are largely developed, we find that large encrinital stems form the greater part of the substance of the successive beds; and where the same portions are ill developed, the stems are fewer in number and less in size *—a fact, which shows the large share these extraordinary fossils had in the formation of the several beds. At the top of this group we here and there find cherty, siliceous beds, with casts of encrinital stems (like the well-known Derbyshire screw-stones) alter- nating with bands of calcareous shale, containing innumerable, flattened Pro- ducte. These beds, though unimportant in themselves, offer us a valuable * In the hills south of Dent the variety called bird’s-eye marble abounds in this group.—See above, Note + to page 75. from Penigent to Kirkby Stephen. 99 analogy by help of which we compare them with the cherty beds in the four- fathom limestone of the mining districts of Swaledale and Arkendale. The strongest masses of this group (in which the fossils are all more or less white and crystalline, and imbedded in a dull grey, nearly compact limestone), are, on the north side of Garsdale, extensively quarried for the Kendal marble works ; and works were opened on the corresponding strata in the valley of Dent, but are now deserted; a better material having been there discovered in the twelve-fathom limestone. 10. Gritstone, Coal, and Shale. Thickness varying from 50 to 80 feet. The prevailing order appears to be nearly as follows : (a.) Thin-bedded gritstone, sometimes coarse-grained. (b.) Coal and carbonaceous shale. (c.) Bands of light-coloured, micaceous grit. The lowest division (a.) is of very variable structure. It is in some places very coarse-grained ; but in Uldale, between Swath Fell and Baw Fell, it passes into a dark, compact, siliceous mass, exactly like the metalliferous chert of Swaledale. Along the line of section this cherty form is, however, an ex- ception to the prevailing structure. The coal varies in thickness from a mere trace to two feet, and is in many places of excellent quality*. When it reaches its maximum thickness, it is, however, generally mixed with shale and other impurities. 'To the north of Ingleborough, no member of the whole series is more continuous than this coal-bed and its superincumbent shale ; and it has been worked, more or less, in almost every mountain near the lines of section. But in Ingleborough and Penigent the whole group here described thins out to such a degree, that the four-fathom and twelve-fathom limestones become confounded, and present a single unbroken escarpment. ‘T’o the north of the line of section the same coal is now extensively worked in the neighbourhood of Brough. 11. Twelve-fathom Limestone. 'This system of beds makes a striking fea- ture in many parts of the carboniferous chain of the North, beg the highest limestone group of sufficient thickness to give any character to the soil or to produce a distinct escarpment. In some districts it forms the crown of a long * This coal was formerly worked to a considerable extent, by means of horizontal drifts, under Great Colm, on the south side of the valley of Dent, though not more than five or six inches in thickness. It was of excellent quality, and in such request, that about seventy or eighty years since, it was sent on pack-horses over the mountains as far as Kendal for the use of the black- smiths’ forges, &c. I know of no fact which places in a more striking point of view the great im- provements in internal communication within the period above mentioned, A supply like this would now be utterly worthless. The extensive manufactories of Kendal have long been supplied with fuel from the great Lancashire coal-fields. 80 Prof. Sep@wick on the Carboniferous Chain succession of tabular hills; in others, it forms a terrace on the sides of the mountains terminating a succession of green pastures, which rise in inter- rupted slopes from the neighbouring valleys. Above it the strata often lie concealed under accumulations of black turf bog ; and the highest summits of the mountains terminate in great irregular masses of tabular millstone grit. Near the line of section its greatest thickness is about eighty feet ; but in one or two places it thins off and almost comes to an edge ; and its average thick- ness is under twelve fathoms. The mineral characters of the group are so nearly the same with those of the four-fathom limestone, that the same description may almost serve for both. Its prevailing colours are grey, and some of the beds exactly resemble ordinary specimens of the great scar limestone. Most commonly this group is distin- guished by the abundance of encrinital stems, which in some rare instances so nearly constitute the whole mass of the strata, that the cementing principle is almost wanting, and the weathered surfaces of the blocks rapidly disinte- grate and fall into innumerable cylindrical fragments*. In general, however, the encrinital fragments are held firmly together by a grey, subcrystalline, cal- careous cement, and form hard beds, the most regular of which admit of a good polish. The most beautiful variety of this fossil marble, is obtained from one or two of the upper beds of this group, and is quarried at Snays-wold Fell, between Dent and Garsdale. The dull grey base in which the fossils are commonly imbedded, is there enlivened by many dark cloudy blotches, arising out of the irregular distribution of the colouring bituminous matter. The group appears to terminate in a few, thin, impure beds of dark bluish lime- stone alternating with slaty gritstone and carbonaceous shale f. So far the relations of the successive groups may be ascertained with a near * Beds of this kind burn to a pure lime very readily: but on extracting it from the kilns, in- stead of coming out in such lumps as are convenient for transport, the lime frequently falls at once into a fine impalpable powder. Some beds of this kind overlie the coal-seam (No. 10 (0.)) at a hill called The Cross in the valley of Dent. + Section of the marble quarry of Snays-wold Fell, in the descending order :— Feet. Inches. Feet. Inches. 1. Carbonaceous shale............ 4 0 5. Hard, dark blue limestone, and a Oe Mlagey, brown Grit cece. cle = ier 40 thin band of shale ......... wa T a6 3. Hard, dark blue, impure limestone 2 4 6. Fine, compact bed, with crystalline 4, Shale and gritstone irregularly mix- stems of Encrinites....... » 00 leg LO, ed together, and containing much 7. Shattered beds and shale....... » 046 calcareous matter in nodular 8. Strong Encrinite bed...... Soca whe masses, with large stems of En- 9. Lower calcareous bed, not exposed CEIMITES .ce ee cere ews essences O10 in the section. Nos. 6, and 8. are the only beds used in the marble works. Srom Penigent to Kirkby Stephen. 81 approach to accuracy, as the various limestone deposits offer a series of good base lines to which all the distant observations may be referred. But in the remaining part of the ascending series we lose all our lines of verification ; and the sections, as might have been expected, differ very widely in their details. Out of much apparent confusion, we may, however, make out an approximate order, and divide a great thickness of strata into groups suf- ficiently extended to admit of a general comparison among themselves. 12. Great upper Shale. Thickness varying from 40 or 50 tonearly 200 feet. This group is complex, containing, here and there, a band of crow-limestone, and having many subordinate masses of grit, generally of a thin, slaty texture. On the whole, however, it is characterized by a dark-coloured shale, and makes a remarkable feature in the higher parts of many of the mountains, being often laid bare by the deep water-channels which intersect the boggy region between the first millstone grit and the twelve-fathom limestone. On the south side of Baw Fell (in the brow above the marble quarry men- tioned above (p.79.)), a five-inch coal is, I believe, subordinate to this group ; and, on the west side of the mountain, it contains a strong band of crow-lime- stone. In apart of Swaledale it contains the main chert, black beds, red beds, iron beds, &c. enumerated in the detailed sections of the miners in that district. 13. First Millstone Grit. Thickness varying from 20 to 60 feet. The term is here used with considerable latitude, being applied to a group of strata, a part only of which has the true character of millstone grit. When used more strictly, it designates a coarse, open-grained, siliceous gritstone very irregularly bedded, often subdivided by lines not parallel to the planes of stra- tification, and usually containing a considerable quantity of kaolin, and small rounded pieces of opaque quartz interspersed irregularly through its mass. The prevailing colour of the group, here described, is light grey ; but this is by no means constant. The characteristic millstone grit is sometimes found associated with all parts of this group ; sometimes only with the upper part ; in which case the lower beds generally consist of a hard, light grey, thin-bedded sandstone. Sometimes the millstone bands are entirely wanting, and then the group (especially when the beds alternate with shale) cannot be easily sepa- rated from that which is next superior to it. It is finely exposed in the last precipice of Penigent, and in the strata which form the crown of Ingleborough. It also forms a part of the higher escarp- ment of Whernside and of Great Colm*. * The open-grained varieties of gritstone in this group sometimes decompose into a sharp sili- ceous sand, which is much used in the saw-mills where the marble blocks are divided into thin slabs fit for polishing. VOL. IV.——SECOND SERIES. M 82 Prof. Sepewicx on the Carboniferous Chain 14. Alternations of hard, thin-bedded, brown gritstone, and dark-coloured carbonaceous shale, with two or three beds of coal. Average thickness along the principal line of section about 60 feet. In some of the neighbouring regions (for example among the mountains of Swaledale Head), this group contains two or three thin beds of crow-lime- stone, and its aggregate thickness is about 200 feet. The only bed of coal which has been much worked, is in the lower part of the group, and varies from eighteen inches to nearly four feet in thickness. At Tan Hill near the highest part of the road from Brough to Arkendale, and at Turna Fell near Hawes, this coal is of good quality, and is extensively worked. Near the top of Penigent, of Whernside, and of Great Colm, horizontal drifts have been carried into this bed ; but it is of bad quality, and not fit for domestic use, being mixed with ferruginous and pyritous shale*. The hard, brown beds of grit alternating with the carbonaceous shale, are provincially termed szll-stones. 15. Second Millstone Grit. The limits of this group are very ill defined, and its thickness varies from 40 or 50 to 120 feet. At the top of Penigent and Whernside it is represented by an open-grained, thin-bedded, siliceous grit, no part of which has the appearance of millstone. But at the top of Baw Fell, Wildboar Fell, and some of the Swaledale hills, it passes into great, thick heds of the finest millstone grit. 16. Alternations of gritstone and shaie, with traces of a thin bed of coal. Thickness about 100 feet. The band of coal is found, here and there, near the bottom of this division. In general the subordinate shales are meagre, sandy, and micaceous; and the alternating beds of grit are thin and open-grained, like certain bands associated with the groups of millstone grit. There is just a trace of this group at the top of Wildboar Fell, and perhaps at the highest point of Whernside, under the soil and morass. It is best ex- posed under the highest summit of Shunner Fell, and near the top of a part of the high ridge between Mollerstang and Swaledale Head. 17. Upper Millstone Grit. Thickness 120 feet. * As not less than three beds of coal are found, here and there, subordinate to this group, it would be impossible to prove that in all the above-mentioned places the coal is precisely upon the same parallel. It is, however, so considered by the miners of the neighbouring districts. Near Kirkby Stephen it generally passes under the name of the Tan Hill seam, that being the locality of the most valuable coal work, established upon the bed in question. There, however, the re- lations of the coal to the neighbouring groups are somewhat obscure ; and in a general description the Turna Fell seam is perhaps the best name which can be given to it. from Penigent to Kirkby Stephen. 83 __A most characteristic exhibition of this group is seen at Shunner Fell top, and on some other of the highest eminences of Swaledale ; but it does not appear anywhere upon the longitudinal line of section. Like the other groups (Nos. 13. and 15.), it varies in structure; but it contains, and passes into, masses of the most characteristic millstone grit. Here terminate the details of the general section; and with one limited exception, no higher beds appear among the mountain ridges extending from Penigent to Stainmoor, and to the mining districts of Arkendale and Swale- dale. Before commencing the description of the longitudinal section, it may be expedient, for the purpose of easy reference, to give a tabular view of the preceding detailed general section. Carboniferous limestone series, &c., in the descending order*. Greatest thickness in Feet, PPO pper WUlIstONe Grit, GLC. 66s soe sic cic.c cence ccce as nowtne cine daveceecescevcs 120 16. Gritstone and shale, with traces of a thin bed of coal .....eeecceeee siteieees. LOO 15. Second millstone grit, &c. ...... Daikiehis tale ae Li apSele's el dint oele siecle oblesiee De 4120 14, Alternations of hard gritstone, shale, and two or three beds of coal. Mean thick- MessHADOULTOOVOL 10 ACCEL | is aialelerniejei$,9 eTep0,sse,0 soy epsieuesss Aoosécnacoddnoood. LO 13. First millstone grit, &c. .......... aielorevetele aietarereierote eqeilo.estrepecereteqereysie.a) S10:8 -- 60 12. Great upper shale..... rae aterete ste SWeicfo/atars Se oie e¥e' vlald wie arellshaa Raval oes ees - 200 er Pieleic-fathone HmestOnen cro sie sere oasis ec cscccdvececserene Silas « oats Sales |) «00 Be eiemiastOneNCoaly Aid Shalesh ASS «Jk win able bald vn bobo pide Wb wiescie ciele wees | 80 c. Bands of grey, micaceous grit. 6, Coal and shale. a. Thin-bedded grit. Be hOmr- fai hom ImeStONe | dele «,o,00> sins c\0r0.0i06.0.0 0 o0 2108 Anan pOGe coo UF Sogont Z tin aA 8. Sandstone, fissile gritstone, and shale ........eeeeeseecees APGSHOBSOOS setsistene OD c. Micaceous, slaty grit, with bands of shale and a trace of coal. 6. Shale with bands of gritstone. a. Slaty, micaceous grit and shale, sometimes with a trace of coal. 7. Mosdale Moor or Wold limestone ........ HE SANS FM Bh a Ad Wea Slelenarere ices veleft Seid. 45 6. Fissile gritstone, and carbonaceous shale, with a bed of coal........++eeeeee+- 150 c. Hard, micaceous, slaty grit. 6. Shale, coal, and grit. a. Grit and shale. 5. Strong post limestone ....... piateraters vocédocnotme sHeoocu eon doco cdospoptio: Ze BeeaNGSrone, SHAlG;aNd CAICACCOMS OTE: stiscls cus cs cecccevvetetensecene pietaten 50 c. Hard, brown grit, shale, and a trace of coal. 6. Siliceous and calciferous grit. a. Dark shale. 3. Second limestone or black marble group ...+++ssseeeee0% piv}s 6's © ele) oleleid o dzeie's «) / (45 2. Sandstone and shale ......... Se oadeticnoe se joo SbDOr sidalsis)sielewshets\slelelitisieien 4.10.0) ce. Hard micaceous grit and shale, &c. 6. Sandy, micaceous shale and brown sand- stone. a. Dark shale and iron-stone. iF Ra CPMNSC OT TUUSTLCSLUTIC eter tot totale) oan rel cia sick Blea ciel ai'es ot lovelose'c¥ slamsile. tisioveiehteSitwidkcke 600 otalesc dace (2060 PV ES hig. 1. mM 2 S4 ‘Prof. Srpewicx on the Carboniferous Chain The thickness from the bottom of the whole system to the top of the twelve- fathom limestone is 1735 feet, as determined by these numbers ; and from the top of the great Scar limestone to the top of the twelve-fathom limestone, is 1135 feet. But asmall correction must be made on account of dip; anda more considerable correction on account of over-estimate, all the beds being taken at the maximum thickness, which is never the case in any one section. After all the deductions, there must remain a thickness of about 1000 feet for the alternating beds between the top of the great Scar limestone and the top of the twelve-fathom limestone ; and as far as regards the mountains of Gars- dale and Dent, 1 do not think that this is an over-estimate. It is, however, right to state, that very few of the numbers in the preceding details are from actual measurement. I wish them to be considered only as the average results of a great many independent approximate observations. § 3. Longitudiual section from Penigent to the plains of the Eden near Kirkby Stephen, &c. &c.* This section might have been extended many miles further towards the south, through a region which, though of less elevation than the one here described, has nearly the same external characters, and is composed of similar groups of strata: but I wish to confine it to the part of the chain I have per- sonally and repeatedly examined. Commencing at the top of Penigent, it passes just above the village of Horton, and thence nearly in a straight line to the top of Ingleborough. The summit of Penigent is, I believe, composed of beds subordinate to the second millstone grit (Group 15.) ; and immediately below, the highest slope, Nos. 14. 13. 12, are finely exposed, and the coal bed of No. 14. has been worked in horizontal drifts. Then comes a great limestone precipice representing Nos. 11. 10. and 9.—No. 10. having nearly disappeared, and the twelve-fathom and four-fathom limestones (Nos. 11. and 9.) making but one precipice. The remaining part of the great escarpment is composed of No. 8. From the swallow holes at the base of No. 8. to the level of Horton Beck, all the successive beds (No. 7. to No. 1.) may be traced without a single omission. The black marble beds (No. 3.) have been quarried above Hull Pot, but are not of good quality ; and the group (No. 2.) is not more than twenty or thirty feet thick+. The great Scar limestone is magnificently ex- hibited ; and in it are Hull Pot and Hunt Pot. The former a great roofless * Plate VI..fig.. 2. + Both in Ingleborough and Penigent the groups between the Scar limestone and the tnelve- fathom limestone, are of less aggregate thickness than in many other parts of the principal section. from Penigent to Kirkby Stephen. 85 cavern, with perpendicular walls, from which may be heard the roaring of subterranean waters. The latter, an open crevice of unknown but great depth, as is proved by the long-continued rumbling noise of the stones which descend after many rebounds from its projecting ledges towards the foun- dations of the mountain. Below Dowgill Scar is a beautiful junction of the horizontal limestone and inclined greywacké without the intervention of any conglomerate*. In the prolongation of the section through Moulton Fell, the Scar limestone presents no features deserving peculiar notice; but a little to the east of the line, above the village of Selside, is an open chasm called Alum Pot, of enormous but unknown depth. It is surrounded by grassy shelving banks, and many animals tempted towards its brink have fallen down and perished in itt. Further up the hill (at Moor Syke, &c.) are the black marble beds (No. 3.), and after passing in succession all the intervening beds, we have, at the top of Simon Fell, the slate quarries of No. 8.c. The upper portion of this group makes a magnificent precipice on the north side of Ingleborough, and its slate quarries may be traced all round the mountain. Over this group comes a precipice of limestone, in which (as at Penigent) the twelve-fathom and the four-fathom limestones are united, the intervening shale and coal (No. 10.) having nearly disappeared. Over these comes the upper shale (No. 12.); and then the first millstone grit (No. 13.), forming a great tabular mass on the top of Ingleborough. The two highest groups of the Penigent section are therefore wanting. In descending from the great precipice of slaty grit and shale to the river of Chapel le Dale, we pass in regular succession over every group from No. 8. to the bottom of the Scar limestone. 'The upper groups are much concealed by morass, but they break out, here and there, and are laid bare in the water- courses on the sides of the mountain. In the bottom of the valley (about half a mile below the Chapel) there is a beautiful junction of the horizontal limestone and the inclined greywacké ; and just at that point all the mountain streams, which in the higher part of the valley had been engulfed in the cavernous Scar limestone, burst out in one copious spring, and form the river which descends to Ingleton. Following the line of section, we have at the base of Whernside some of * The greywacké dips about south by west, at an angle of 45°. + The approach of cattle is now prevented by a strong, lofty wall; but there can be little doubt, that during the last two or three thousand years, great masses of bony breccia must have accumu- lated in the lower parts of this great fissure, which probably descends through the whole thickness of the Scar limestone. 86 Prof. Sepewick on the Carboniferous Chain the most characteristic features of the Scar limestone. It is traversed by fissures, and hollowed out into caverns; in one of which (Weathercoat Cave) is a waterfall of no common beauty, and doubly striking from the extraordinary nature of the objects which are about it. Ascending thence to the top of the mountain, we cross the groups in regular succession, and end with a series of thin-bedded, coarse grits, nearly on the same parallel with the beds on the top of Penigent, and therefore pro- bably subordinate to No. 15. of the general section *. The first millstone grit (No. 13.) makes a feature on all sides of the mountain top, and the coal bed in No. 14. has been partially opened on its north face. The coal bed in No. 10. (b.) has been worked in three or four different places, and the group to which it is subordinate becomes regularly expanded (though probably of rather less than its mean thickness) between the twelve-fathom and the four-fathom limestones. Here, therefore, ceases the anomaly of the Ingleborough and Penigent sections already noted ; and it is, as far as I know, the only great anomaly in the structure of the districts through which the lines of section range. ‘There is, however, a peculiarity (and it is repeated on the east side of Great Colm) which deserves notice. The four- fathom limestone all round this mountain is thicker than the ¢welve-fathom limestone, one group being developed much beyond its average thickness, and apparently at the expense of the other. From Whernside the line deflects nearly due west (without producing any confusion in the details, as all the groups are very nearly horizontal), and ranges by High Pike across the pass from Dent to Ingletent. The four- fathom limestone, and the slate quarries (No. 8. c.), form the top of the ridge ; and on the north-east side of it, is a succession of waterfalls over the bare escarpments of all the groups, from the fourth limestone (No. 7.) down to the beds above the black marble series. Through the middle portion of these falls, runs a north and south vein (partly filled with calc-spar), producing a downcast of eight or ten yards on its west side. I mention this for the pur- * The natural section is not good near the top of Whernside, the highest mountain of the whole range; but the top beds may possibly represent a portion of the 16th group of the general section. + This fact has sometimes induced me to suppose that the great calcareous escarpment near the top of Ingleborough and Penigent was chiefly composed of the four-fathom limestone ; and that some bands of shale and thin beds of limestone near its top, might represent the two superior groups (Nos. 10. and 11.) in a very degenerate form. I mention this only as a mere conjecture. { In the southern and central portions of the principal line of section, the beds, though nearly horizontal, incline on the whole a little to the north-east. The part of the section deflecting nearly due west, from the top of Whernside over High Pike to Great Colm, is omitted in the accom- panying figure (Pl. VI. fig. 2.). from Penigent to Kirkby Stephen. 87 pose of remarking the almost entire absence of great faults or veins in theneigh- bouring mountains, and their consequent sterility in all metalliferous minerals. From High Pike to the top of Great Colm, all the groups succeed each other in regular order; but on that side of the mountain the twelve-fathom limestone is still in a degraded form, and the four-fathom limestone has more than its average thickness. On following them to the eastern side of the mountain we may, however, remark, that one gradually increases and the other diminishes in thickness till they assume their average proportions. Over the twelve-fathom limestone (No. 11.) the three superior groups are well exhibited ; and a bad two-foot coal has been partially worked in the group No. 14, which is here about 60 feet in thickness. On the highest summit is a trace of the second millstone grit (No. 15.), which, though rather thin-bedded, has here the mineral structure indicated by its name. I do not, however, think that these beds are so high in the series as those which form the highest peaks of Penigent and Whernside. Here the section again deflects to the north, and in the remaining part of its range is very nearly in a straight line*. Descending from Great Colm top to the valley of Dent we commence, as above stated, in the lower portion of the second millstone grit (No. 15.), and cross in succession every group till we meet the upper strata of the great Scar limestone, about 200 feet above the level of the river. We may remark, during this traverse, the old coal-works in No. 10. (b.) +,—the slate quarries of Little Colm in No. 8. (c.),—the old slate quarries and the Barbon coal-works in No. 6. (0. c.),{—and the various quarries which have been opened in the black marble beds (No. 3.). In the higher part of the valley of Dent the river runs for several miles among the upper beds of the Scar limestone, and we meet with a succession of objects highly characteristic of the formation. The mountain-streams are engulfed, and the strata interrupted by numberless grotesque caverns and open fissures, resembling, on a miniature scale, the striking features of Chapel le Dale. From Dent, the sectional line ranges over the top of Risell to the Garsdale river, close to the chapel. On the ascending line, all the beds are laid bare up to the Wold or Mosdale Moor hmestone, in a great ravine called Scotchergill. On the eastern brow of Risell are quarries in the fowr-fathom and twelve- fathom limestones ; and from the upper quarry is obtained a very beautiful variety of fossil marble already noticed. On the western brow of the same hill, the coal-bed (No. 10. 6.) has been partially worked ; and the summit is composed of the lower beds of the first millstone grit (No. 13.). * See Pl. VI. fig. 2. continued. + See above, Note to p. 79. } See above, Note to p. 76. $8 Prof. Sepawick on the Carboniferous Chain On the descending line there is a fine exhibition of the slate quarries in No. 8. c. Close to the chapel the river runs in the grit bands (No. 2. c.) under the black marble ; but in ascending to Garsdale Head (where the road turns off to Kirkby Stephen), all the beds up to the fourth Mosdale Moor lime- stone (No. 7.) may be observed to cross the channel in succession. Both sides of Risell are much covered with alluvial matter and vegetation ; but independently of the localities above indicated, the position of the respec- tive groups is defined by the rows of inverted green cones, provincially called swallow-holes, which often mark the presence of the limestone bands when no rock is visible at the surface. From many places, on the line of section, five rows of these inverted cones, each indicating the presence of one of the cal- careous groups above the Scar limestone, may be seen on the sides of the neighbouring mountains *. In ascending from Garsdale chapel to the top of Baw Fell we may find, by the sides of various torrents, good sections of all the groups, from the black marble to the twelve-fathom limestone. A thin coal band breaks out, here and there, in the group (No. 4.) above the black marble beds. On the west flank of this mountain, the coal bed (No. 6. b.) under the Mosdale Moor limestone has been worked extensively ; and on the same flank the coal bed under the twelve-fathom limestone has been attempted+. The quarries in the four- fathom limestone, from which large encrinital blocks are extracted for the use of the Kendal marble works, also deserve notice. The groups of strata above the twelve-fathom limestone are of the aggre- gate thickness of 500 or 600 feet, and terminate at the top of the mountain in fine, horizontal, tabular masses of millstone grit, subordinate, if I mistake not, to the second group of that rock (No. 15.). All the upper parts of the * The origin of these cones is very clear. The several limestone groups abound in crevices and fissures, through which the waters, descending from the higher regions, immediately sink, and trickle down among the lower strata, till they meet some impervious bed which throws them out again to the surface. Now on the sloping sides of the mountains these groups generally form long horizontal terraces, more or less buried under masses of alluvial, incoherent matter: and through this covering the waters freely percolate, till they meet the surface of the limestone beds; when they sink, as above described, through some of the crevices, and carry along with them the finely comminuted portions of the superincumbent materials. In this way the alluvial beds are slowly undermined, and sink down into inverted cones—the inferior portions of which, being sheltered from the elements, and kept dry by the action of the crevices below, become covered with a fine green sward abound- ing in such plants as are commonly found only in the lower regions of the mountains. t Not far below the works in No. 6. 6. a trial was made, a few years since, in some highly in- clined, carbonaceous shales, probably subordinate to No. 4. of the general section. The coal was abundant, but of very bad quality, and difficult to work ; being close to the disturbance produced by the passage of the great Craven fault. See the preceding Memoir, p. 60. from Penigent to Kirkby Stephen. 89 section are extremely obscured by morass ; but we have, I think, evidence enough to show—that a five-inch coal (breaking out about 100 feet above the twelve-fathom limestone) is subordinate to the great upper shale (No. 12.), which is here very largely developed,—and that a second bed of four-inch coal, about 200 feet above the preceding, is subordinate to the alternating beds (No. 14.) above the first millstone grit. ‘The evidence for this arrange- ment may be considered obscure; but it is at least made probable by the struc- ture of the nearest mountains of the chain. Descending from Baw Fell top to the head of Uldale (after crossing a region of thick morass), we meet with magnificent sections of a great series of beds commencing with the twelve-fathom limestone. Under this limestone the coal bed (No. 10. 5.) has been partially worked. We then cross a series of cherty beds, analogous to those on the same parallel in the Arkendale and Swaledale sections: and further down the torrent is a great precipice (com- posed of the four-fathom limestone, resting on the gritstone bands and thick shales of No. 8.), over which the waters shoot in a single plunge, and form one of the grandest falls in the carboniferous chain*. Below the fall is one of the finest gritstone quarries of the chain (No 8. a.); and a few hundred yards further down the valley we find great masses of highly inclined and dislocated limestone, connected with the range of the Craven fault. The phenomena, last described, are a little to the west of the line of section, which at Uldale Head makes its nearest approach to the greywacké region. Thence it ranges over Swath Fell, to the top of Wildboar Fell, through a country almost buried under turf bog and alluvial soil. The top of Swath Fell appears to belong to the same group (No. 15.) as the top of Baw Fell, but it does not quite reach the same elevation. At the top of Wildboar Fell we have just a trace of the group (No. 16.) ; but * Tn all chains of mountains composed, like those I am describing, of horizontal strata in very different degrees of induration, waterfalls are necessarily abundant. The harder groups have an obvious tendency to form terraces over which the waters break with a violence proportioned to the nature of the descent. The steep sides of the hills are, however, often composed of solid beds of sandstone or limestone, resting on thick masses of soft, incoherent shale: and when such combina- tions cross the direction of a mountain stream, they almost always produce an overshot fall. For, had the inferior shales ever projected so far as to produce a gradual descent, they must soon have given way to the friction of the water, till they arrived in such a position as to be protected from its action. And even when removed from the direct effects of erosion, they often continue to ex- foliate so rapidly, that the hard superincumbent beds form a projecting ledge, over which the waters leap at once into an inferior basin. In this way the great waterspout of Hardraw Scar commences in the black marble group, and plunges into a basin of the shales subordinate to No, 2. These appearances are so very common and obvious as perhaps hardly to require notice. VOL. IV.—SECOND SERIES. N 90 Prof. Sepewick on the Carboniferous Chain the magnificent tabular escarpment overlooking Mollerstang is composed ex- clusively of the second millstone grit (No. 15.) ; and on the same face of the mountain we have a succession of the finest sections, exposing all the groups down to the twelve-fathom limestone. They are, perhaps, of as great a thick- ness as at Baw Fell; but in consequence of the degenerate form of the first mill- stone grit (which is here an ordinary, open-grained, whitish sandstone), they are not well defined. Subordinate to No. 14. is a bed of coal about eighteen inches thick, which has been partially worked, but hitherto without profit. Descending from the crown of the hill, along the edge of its eastern escarp- ment, to the level of the white grit beds representing the first millstone (No. 13.), we cross (close to a place called Dolphin Sty) the line of a great vein or fault, which throws all the beds on its north side about 150 feet below their level. In consequence, the coal-bed (No. 14.) and the accompanying grits and shales are once again repeated. ‘This vein strikes the opposite hills (producing the same northern downcast), and is prolonged into the mining district of Swaledale. After reaching the level of the twelve-fathom limestone, we cross the bearings of one or two other veins, which have partially deranged the position of the groups. I have attempted to convey only a general notion of them in the accompanying section, for the country is so much covered with alluvion that their exact effects cannot be easily ascertained. Continuing to descend, we come upon the edges of the dislocated masses thrown up by the great Craven fault. The horizontal beds of the great Scar hmestone lie far below the bottom of the neighbouring valley*: but the broken ends of the whole mass have been torn up from the foundations of the mountain, and jammed against the edges of the upper horizontal groups. The vast force of elevation is indicated by the enormous extent and contor- tions of the dislocated masses ; and the line of greatest stress is indicated by an anticlinal axis, on the north side of which the Scar limestone, after many breaks and undulations, gradually falls down to the level of the Eden, and is buried under the conglomerates of the new red sandstone, where the longi- tudinal section ends. * The Mosdale Moor limestone (No. 7.) is, I believe, the lowest calcareous group to be seen in the deep valley at the eastern base of Wildboar Fell. + It deserves remark, that in some places near Kirkby Stephen the direction of the anticlinal axis is traced by a small vein, which, here and there, has been worked for lead. ‘This seems to prove that, at least, some of the lead veins of the carboniferous chain originated in fissures pro- duced by the great elevatory movements before the period of the new red sandstone. I believe, partly on the evidence afforded by the details of this paper, that many of the lead veins of Arken- dale and Swaledale had their origin during the same period. SJrom Penigent to Kirkby Stephen. 91 Such are the striking phenomena along the line of section. In order to make the structure of the region still more clear, and to connect it with the mountain tract at the head of Swaledale, I proceed to describe, very briefly, two other sections—one commencing at the top of Penigent—and the other at the top of Whernside, and both diverging considerably from the bearing of the principal line. Section from Penigent to the top of Stags Fell, near Hawes ; mean bearing about N.N.E.* The strata of Penigent have been already described. If the line of section be made to range along the south side of the valley, above the village of Horton, we shall arrive at the great vertical chasm called Ling Gill, which gives a series of fine, bare sections, through almost every part of the Scar limestone. Continuing the section nearly in a straight line, over the summit of Cam Fell, we first cross the outgoings of all the groups up to the twelve-fathom limestone, forming the great plateau above Cam Houses, and find that the three groups (Nos. 9. 10. 11.) which were confounded together in Penigent, are here exhibited with their true relations. We then cross the great wpper shale and the first millstone grit (No. 12. 13.), and rise to the summit of Cam Dod, which is buried under peat moss ; and from that point may see the pro- longation of the twelve-fathom limestone down Wensleydale, forming on both sides of the valley the crown of a long range of flat-topped elevations +. Descending to Hawes, which stands upon the upper part of the Scar limestone, we cross all the successive groups in regular order. The coal (No. 10. b.) has been worked both on the east and west sides of Cam, and the lower coal seam (No. 6. 0.) is still worked near the village of Gale. In the range of the sectional line, on the other side of the valley, over Stags Fell, we again cross the same successive groups, in the ascending order, till we reach the great overhanging plateau of the twelve-fathom lime- stone; and we may remark, by the way, that it is traversed by a cross vein, with a downcast of several fathoms towards the south-east. Rising from this plateau to the top of the mountain ridge, between Wensleydale and Swale- dale, we first cross the upper shale (No. 12.) and the first millstone grit (which is not far from the highest level of the road from Hawes to Muker) : * Plate VI. fig. 3. + The summit of Cam Dod is probably composed of beds subordinate to the group (No. 14.) over the first millstone grit. Nn 2 92 Prof. Sepewick on the Carboniferous Chain above them are the grits, shales, and coal bands of No. 14*; and the series, though almost lost among the accumulations of peat earth, terminates, I be- lieve, in the beds of the second millstone grit (No. 15.). Notwithstanding the constancy in the position of the several groups, there are changes of mineral structure which, had we not so many terms of com- parison, might lead to some confusion. Near the eastern end of this sec- tion, the black marble beds (No. 3.) lose that mineral character which gives them their chief value, and resemble the beds of the higher group (No. 5.); and with these beds they might easily be confounded, as, in some places near Hawes, the shales of No. 4. are wanting, and the sandstone beds of the group are not more than twenty or thirty feet in thickness+. Near the same place the shales of No. 8. become insignificant, but the micaceous, slaty beds are well developed. Section from the top of Whernside to the top of Shunner Fell ; mean bearing about N.N.E.t The line here ranges from Whernside into the higher part of the valley of Dent, about five miles above the village (where the river runs upon the top beds of the Scar limestone); thence over the Cross to Mosdale, and over Cotter Fell to the top of Shunner Fell, without making any very great devia- tions in its course §. The strata of Whernside have been already noticed, and the same groups succeed each other in regular order on the side of the next mountain, where however we may remark, that the four-fathom limestone is of less, and the twelve-fathom limestone of greater, than their average thickness; just the con- trary of what was observed among the groups of Whernside ; and another instance of what was remarked before,—viz., that each of these two limestone * This coal bed is not worked, as it is only about eighteen inches thick, and is inferior in qua- lity to the thirty-inch coal of Turna Fell, in the same range of hills, and only at a short distance towards the north. - + Further down Wensleydale these three groups of the general section (viz. Nos. 3. 4. and 5.) probably lose all distinctive character, and appear as one group: for I have remarked, that in the hills below Askrigg there are only five, instead of six, distinct limestone groups, from the Scar lime- stone (which is partially expanded in the lowest parts of the valley) to the twelve-fathom limestone inclusive. Between Askrigg and Bolton Castle the whole system is intersected by metalliferous veins, producing (like ordinary faults) contortions, upcasts or downcasts, and other disturbances of the component strata. t Plate VI. fig. 4. § The Cross (a mountain of which the summit is sometimes called Naughtberry Hill) must not be confounded with Cross Fell, the highest mountain of the carboniferous chain north of the Eden. Jrom Penigent to Kirkby Stephen. 93 groups is of variable thickness, and that each of them appears to be sometimes developed at the expense of the other*. Above the twelve-fathom limestone, the upper shale and the first millstone (Nos. 12. and 13.) are in their characteristic form, and over them are the car- bonaceous shales, coal bands, and grits of No. 14. and perhaps a trace of No. 15; but the summit of the hill is buried in morass. Following the sectional line, we find in Mosdale all the beds denuded, down to the Mosdale Moor limestone (No. 7.) ; and on the east side of the valley we have an extensive tract of green pastures, crowned with a plateau of the twelve-fathom limestone, under which are many traces of old coal works in the group (No. 10. 5.). From this plateau to the top of Shunner Fell there are strata more than 100 fathoms in thickness ; but all of them are buried under the peat mosses, till we reach the grey crags of millstone grit, on the last ascent towards the crest of the mountain. We there cross the outgoings of the second millstone grit (No. 15.); of the shale and gritstone (No. 16.); and we reach the highest plateau after passing the rugged escarpment of the upper millstone grit, the last group of the general section f. * There is a very fine natural section of all the groups, from the upper beds of the Scar lime- stone to the four-fathom limestone inclusive, in the sides of a torrent called Artingill, near the old pass over the Cross between Dent and Hawes. Immediately above the highest point of this pass, are extensive coal works (in No. 10. b.) reached by shafts sunk through the twelve-fathom lime- stone. ¢ As the strata from the plateau of the twelve-fathom limestone to Shunner Fell top are not, on the whole, well exposed along the sectional line, I subjoin a more detailed, ascending section through the same series, as exhibited near the Turna Fell coal works, a little further to the south. Feet. Inches, Feet. Inches. 1. Twelve-fathom limestone. 7. Hard; brown git oi. aa )s oi0s)es 7 2. Shale, with bands of grit........ 20 0 See UIANO | a cnia eh lola iayisimsinsnybia’ #60.) itollte 3. Quarry grit, with bandsof shale40or50 0 9. Hard, brown grit ........-. 4. Sill stone (hard brownish grit) with 10. Shale,with bands of soft, tough grit bands of dark shale...... 200r 30 0 11. Bands of open, coarse grit, passing BMA sie. o's) o0'sin/ aes vies) sii eaiere coon @ 6 into the upper group ...... 20 or 30 0 6. Shale with bands of brown gritstone, 12. Millstone grit, &c. ......... as 120.0 and a three-inch coal near the 13. Coarse, thin-bedded grit and shale .100 0 EOP oi a:e a's di0ininjciniain sas oe /0.0r 80.0 14. Upper millstone grit, &c. ...... 120 0 The thickness of the beds from the coal, No. 5. to No. 10. inclusive, is very nearly thirty-three fathoms, as determined from the sinkings of an air-shaft. The other numbers are only approxi- mate. Nos. 2. and 3. represent, in a degraded form, the upper shale and the first millstone grit. All the beds from No. 4. to No. 10. inclusive may be considered as one group, representing No. 14. of the general section: and the remaining groups represent the three highest divisions of the general section in their most characteristic form. 94 Prof. Sepewick on the Carboniferous Chain I could have wished to extend the two diverging sections, just described, as far as the metalliferous hills between Arkendale and Swaledale ; but I am not sufficiently acquainted with that region to represent the prolongation correctly. I may, however, state in general terms, that the four-fathom limestone and the twelve-fathom limestone range through the hills on both sides of Arken- dale, and are among the best lead-bearing beds of the country. ‘They are known by the miners under the names wnderset lime and main lime, and are immediately surmounted by a group about 100 feet in thickness (composed of shale, chert, and gritstone, with some peculiar masses called red beds and iron beds), which, on the whole, may be considered to represent. the upper shale of the general section (No. 12.). Over this group is a strong deposit of coarse grit, upwards of sixty feet in thickness, which probably represents the first millstone grit (No. 13.). The coarse gritstone last mentioned is surmounted by a very complex succes- sion of deposits about 160 feet in thickness. In the lower part of this series we have alternations of gritstone and shale, with a subordinate twelve-inch coal— over these are alternations of chert and shale, with a bed of crow-limestone of the extraordinary thickness of twelve feet—and the system terminates in a mass of shale about eighty feet thick, containing three subordinate bands of impure limestone. It has been stated above, that bands of crow-limestone are found, here and there, subordinate to all the great shales of the carboniferous chain. But their number, and the thickness of one of them, in so high a division of the Arkendale section, must be considered anomalous. I have, however, little hesitation in identifying this complex group (especially as it is immediately surmounted by a deposit of mzllstone grit nearly 100 feet thick) with the 14th division of the general section. The preceding details of this paper explain the structure of a part of the carboniferous chain. ‘Those which follow show the effects produced by the prolongation of the great Craven fault, and the movements which took place among some of the mineral masses when the chain was elevated. § 4. Transverse Sections, from five points of the Longitudinal Section, through the dislocated strata on the line of the Craven Fault*. The first transverse section (fig. 5.) commences from the top of Penigent, and ranges (about south-west by west) through the village of Horton, over Moughton Fell; and thence over a second plateau of the Scar limestone, to the calcareous hills immediately north-east of Clapham. * Plate VI. Transverse Sections (fig. 5. 6. 7. 8. 9.). Jrom Penigent to Kirkby Stephen. 95 The successive groups of strata on the side of Penigent have been noticed above* ; and the various phenomena exhibited at the junction of the carboni- ferous system with the greywacké have been very clearly explained by Mr. Phillips in a preceding memoir of our 'Transactions+. My object is to con- nect the longitudinal section above described, with section (D.) of that me- moir f. From Clapham to the hills north of Ingleton, the range of the Craven fault is marked by an anticlinal line or break, apparently formed by the pro- trusion of the slate rocks during the elevation of the limestone chain. This line passes through Clapham Beck about a mile above the village, as is indi- cated in the section. The second transverse section (fig. 6.) commences at the top of Great Colm, passes in a direction nearly due south over Gragreth ; thence, deflecting a little towards the east, crosses the foot of Kingsdale and becomes united with section (A.) in Mr. Phillips’s paper$. The strata of Great Colm have been described above|| ; but in consequence of their gradual rise towards the south-west, some of the lower groups are brought out in the Gragreth range, the top of which is composed of the fissile gritstone (No. 8. c. of the general section){. In descending from the top of Gragreth to the waterfall called Thornton Force, at the foot of Kingsdale, we cross all the groups from No. 8. down to the great Scar limestone. On crossing the line of the great fault, the dislocation is precisely of the same kind as in Clapham Beck ; but is incomparably more striking. The whole Scar limestone has been tumbled into the valley, and seems to pass under the Burton coal-field. Some of the dislocated masses may be considered, in their prolongation, to reappear in the inclined beds of Kirkby Lonsdale and Farlton Knot. The principal line of fault passes however (as stated in a former paper)** by Ease Gill and Barbondale, and thence in a direction about north by east to the foot of Stainmoor. And in all this portion of its range, the nature of the dislocations of the carboniferous strata are modified by the immediate contact of a lofty greywacké chain, as will be seen in the three next transverse sec- tions. The third transverse section (fig. 7.) commences at the top of Crag or Cas- terton High Fell (the north-western extremity of the ridge of Great Colm), * Supra, p. 84. + Geological Transactions, Second Series, vol. iii. p. 5—15. £ Ibid. Plate I. (D.) p. 12. § Ibid. Plate I. (A.) p. 9. || Supra, p. 87. {| Some of the grits (subordinate to No. 8. of the general section) along this line are of coarse texture, and have been used for millstones. ** Supra, p. 60. 96 Prof. Sepewick on the Carboniferous Chain and ranging in a direction about west by north, cuts through the junction of the carboniferous and greywacké chains. The highest strata of Casterton High Fell are of millstone grit; and desending in the direction above indicated, we cross every bed in regular succession down to the strong post limestone (No. 5. general section). But at a place called Short Gill, on traversing the line of the great fault, we find that all the lower groups, including the Scar limestone, have been torn up from the foundations of the mountain, bent into a saddle, and afterwards jammed between the edges of the horizontal beds and the steep face of the neighbouring greywacké ridge. In order to explain this appearance, we must remember—that the grey- wacké chains existed in some form or other before the deposit of the carbo- niferous system—and that the beds of this system, before their elevation, must have abutted against a series of inclined planes presented by the submarine portions of the old greywacké chain. During a subsequent elevation, both the greywacké and carboniferous systems appear to have been violently acted on at the same moment, and a great strain, accompanied by a relative vertical movement, to have taken place all along the plane of their junction. Buta relative vertical movement of the inclined flanks of the older mountains might not only break off the ends of the carboniferous strata abutting against them ; but would also necessarily produce a great horizontal thrust, which may, I think, account for such a curvature of the dislocated masses as is indicated in this section. This example has been selected on account of its complexity. There are many places along the line of dislocation, where the lower groups have been torn off, by the pressure of the greywacké hills, from the horizontal’ system, and tilted up at a great angle, without undergoing any flexures or contortions like those at Short Gill. The fourth transverse section (fig. 8.) presents still more complex disloca- tions. It ranges nearly east and west, from the top of Baw Fell to Hebble- thwaite Hall Gill, and thence across the upper part of the valley of Sedbergh to the Howgill Fells. The west end of Baw Fell top is, if I mistake not, composed of the second millstone grit (No. 15. general section) ; the inferior groups along the line of section are much concealed under morass ; but several of them may be dis- covered by ascending the different water-courses. ‘The fowr-fathom limestone and the Mosdale Moor limestone are both well exposed, and the horizontal system terminates with flaggy gritstone and carbonaceous shale, containing a subordinate bed of coal which has been extensively worked. (General Section from Penigent to Kirkby Stephen. 97 No. 6. b.) After crossing on the descending line (immediately below the coal shale) about fifty feet of micaceous slaty gritstone (No. 6. a.), we suddenly come to the great fault, beyond which the beds dip at a high angle about west-north-west. They now seem to succeed each other in a regular ascend- ing order ; but on the contrary we find a succession of groups representing, if I mistake not, Nos. 4. 3. and 2. of the general section ; and at length reach the great Scar limestone (No. 1.), the beds of which have a fan-shaped ar- rangement: the first portion dipping at a great angle in the direction above indicated,—the middle portion being elevated into broken vertical masses,— while the lowest strata gradually acquire an opposite dip (about east-north- east), and rest on the conglomerates of the old red sandstone. Descending by Hebblethwaite Hall Gill, we have masses of old red conglo- merate resting unconformably upon irregular, protruding beds of greywacke ; and in the lower part of the valley these conglomerates become of very great thickness. From beneath them on the opposite side of the valley of Sedbergh rise the steep escarpments of the greywacké ridges in which various tributary branches of the Lune have their source*. By comparing this description with the accompanying section, it appears,— Ist, That by the prolongation of the Craven fault under Baw Fell, all the groups below No. 6. were cut off from the horizontal system.—2ndly, That forces of elevation, acting irregularly upon the dislocated masses, pushed a portion of the great Scar limestone above them all into a vertical position.— 3rdly, That by this movement a portion of the Scar fimestone, and three or four superior groups were actually inverted. It is obvious, from this section, that great masses of old red conglomerate were formed on the flanks of the nearest greywacké hills before the existence of the carboniferous series ; and the beds of this series may perhaps never have abutted against the neighbouring greywacké chain. The first effect of elevation seems to have been exactly the same with that which is indicated in the preceding section at Short Gillf. ‘The lower groups were torn off from the base of the mountain ; but not being exposed to the same horizontal thrust from the greywacké chain, they had more room to expand themselves, and fell into the remarkable position just described. 5. The last transverse section (fig. 9.)is drawn from the top of Wild Boar Fell (in a direction about west-north-west) through some dislocated masses, forming * The beds in many parts of the greywacké chains, near the lines of section, are violently con- torted. The lines drawn through the greywacké in the accompanying sections are ideal, and merely intended to contrast the inclined position of its strata with that of the horizontal carboni- ferous system. + Plate VI. (Transverse Section, fig. 7.) VOL. IV.—SECOND SERIES. 0 98 Prof. Sepewick on the Carboniferous Chain bare hills called the Clouds*, and thence to the greywacke chain of Raven- stonedale. The phenomena are here less complex than in the preceding section, though the dislocated beds have undergone a greater movement of elevation. The top of Wild Boar Fell is chiefly composed of the second millstone grit (General Section No. 15.), and along the descending line we cross all the groups to the fowr-fathom limestone (No. 9.). The line of the great fault crosses the section in a deep morass very near the outcrop of the last-men- tioned group (No. 9.); and at a very short distance the highly inclined beds of the Scar limestone rise into the bare hills, called the Clouds, and are con- tinued (sometimes in a vertical position and sometimes contorted) to the rivulet where they are cut off by the greywacké chain. It is possible that some of the groups above the Scar limestone may be con- cealed among the dislocated masses under the morass : but it is at least evident, that a portion of the Scar limestone has been broken off from the bottom of the carboniferous system, and lifted up to its present position over the edges of all the groups of the general section from No. 2. to No. 8. inclusive. The first and second of these five transverse sections (Fig. 5. & 6.) connect the facts described in this paper with those already published by Mr. Phillips + ; and the last three sections (Fig. 7. 8. & 9.) show the very complex nature of the movements along the line of fault, where it ranges close to the junction of the carboniferous and greywacké chains.—By combining these details with those given at the end of the preceding paper, ‘‘ On the general Structure of the Cumbrian Mountains, &c. &c.”’ ¢ we shall have a sufficiently minute account of the whole northern range of the great Craven fault, and of the structure of the neighbouring carboniferous chain. § 5. Conclusion. 1. I will not repeat what I have so recently stated on the changes of the carboniferous system in its range from Derbyshire to the valley of the ‘Tweed§: but I may observe, that the region above described seems by its structure to form a natural link between the northern and southern portions of the chain. * The hills are probably so called from the light grey colour of the dislocated rocks of Scar limestone. + Geol. Trans., Second Series, vol. iii. pp. 12. and 9. t Supra, p. 60. § See Anniversary Address, Feb. 18, 1851. Proceedings of the Geological Society, No. 20. p. 286—288. , from Penigent to Kirkby Stephen. 99 The whole series of strata composing the mountains along the line of sec- tion may be divided into three great natural groups: Ist, The Scar limestone. 2nd, All the alternating subordinate groups (from No. 2. to No 12. inclusive), ending with the great upper shale over the twelve-fathom limestone. 3rd, All the various deposits (from No. 13. to No. 17. inclusive) associated with mill- stone grit*. The lowest of these groups is almost identical with the formation of moun- tain limestone at the base of the carboniferous series of Derbyshire and the Bristol Channel. The middle group has, on the contrary, little in common with the carboniferous series of Derbyshire, and, perhaps, still less with that of the Bristol Channel: but it conforms very nearly to a portion of the car- boniferous system in the chain of Cross Fell. The third group appears in some form or other through the whole extent of the carboniferous chain ; and, though by no means constant in its characters, undergoes perhaps less modi- fication in its long range than either of the other two. A fourth great group might include all the richest deposits of our northern, midland, and south-western coal-fields ; and the analogies they present both in structure and position are obvious; but they belong not to the subjects considered in this paper. In the North of England the deposit of mountain limestone was exposed to many interruptions, arising from drift, mud and sand, mixed with the wreck of numerous trees and plants. Upon such masses as these, encrinites and corals would obviously refuse to grow, till the incoherent sediment became compacted by calcareous matter, upon which they would again find an appro- priate resting-place. ‘The calcareous beds would then go on increasing till they were again interrupted by a new incursion of mud and sand. Effects like these were many times repeated. In the valley of the Tweed these disturbing forces were in full action from the first commencement of the deposit of mountain limestone ;—in Yorkshire (as appears from the previous details) they produced very considerable effects long before the complete development of the formation ;—in Derbyshire, and in the south-western coal-fields, on the contrary, they produced but a small modification of the carboniferous system before the deposit of mountain lime- stone was completed. I hope in a subsequent paper to describe several similar modifications of structure in the northern calcareous zone of the Cumbrian mountains. 2. Many of the coal-beds above described must have been deposited under * The three longitudinal sections, fig. 2. 3. and 4, are coloured on this principle, the detailed subdivisions appearing only in fig. 1. 0 2 100 Prof. Sepewick on the Carboniferous Chain the waters of a sea of considerable depth ; and I never saw any shells of decided freshwater genera in the carbonaceous shales alternating with the mountain limestone*; but these shales sometimes contain thin beds of ma- rine shells, chiefly producte. I am of course aware that freshwater shells occur abundantly in some of our rich coal-fields; and in such cases the de- posits may have taken place in lakes, or more probably in shallow bays and estuaries. It is, perhaps, in very few instances necessary to consider them of purely lacustrine origin ; especially when we remember, that in a part of the great Yorkshire coal-field (far above any of the groups represented in the preceding sections) there are beds abounding in pectens and am- monites. 3. Certain species of marine fossils abound in particular groups of the lime- stone strata, and so far become in some measure characteristic of them; but 1 am not sure that any one species is actually confined to one limestone group. Most of the fossils of the Scar limestone may be found, here and there, in the twelve-fathom limestone, and vice versdt. Wherever there is a sudden change of mineral character, we may, however, remark an equally sudden change in the fossil species. Thus, for example, very few of the corallines, encrinites, bivalves, &c. (abounding in the limestone) are found in the alternating beds of shalef ; and impressions of coal-plants hardly ever occur in the limestone groups, though they abound in the alternating groups of sandstone and shale. This distribution obviously originated, partly in the habits of the animals above- mentioned, and partly in the mechanical causes by which the beds themselves were produced. 4. The several groups of limestone, so remarkable above all the other strata for their regularity and continuity, were evidently the result of a slow. tranquil deposit, assisted by the action of organic bodies ; and most of the * Some geologists have contended, not merely that all coal-beds are lacustrine, but that they once existed as turf bogs,—a supposition surely inapplicable to the carboniferous chains of Northumberland and Yorkshire. To bring such a theory into action, we must suppose that the chains in question were elevated, and again submerged under the ocean, at least as many times as there are beds of coal alternating with beds of encrinite limestone ;—-a most cumbrous, and, I think, an incredible hypothesis, which never could have been started by any one who had examined the coal-fields in the basin of the Tweed, or even the carboniferous chains of the North of England. + T may, however, remark, that I have never seen trilobites, ammonites, orthoceratites, and perhaps some other rare fossils of the mountain limestone, in any part of the series above the great Scar limestone. + The bands of calliard or crow-limestone, above described, may seem an exception to this rule; but the number of species they contain is, if I mistake not, very limited. from Penigent to Kirkby Stephen. 101 fossil remains subordinate to them have lived and died on the spots where they are now found. On the contrary, some of the other alternating strata have originated in an action decidedly mechanical, and their imbedded ligneous fossils have been drifted from a distance. Hence it is that these strata are in general much less regularly continuous than the groups of limestone. The observation must not, however, be strained too far; as some of the thin bands of coal above described are, on any hypothesis, of astonishing regularity and continuity *. 5. The bottom beds of each calcareous group are often impure, and contain very few traces of organic remains, and do not generally alternate to any con- siderable extent with shale and sandstone. We may also remark, that the corallines, zoophytes, &c. found in such positions are commonly of small size. At the top of each limestone group, on the contrary, the alternations of shale and sandstone are universal, and the fossils are numerous and full-grown. From all which it seems to follow—that each limestone group commenced at the beginning of a period of repose—that the marine animals which assisted its growth were at first few in number and ill-developed—that they gradually became vigorous and full-grown; and were at length destroyed only after repeated irruptions of mud and sand. 6. The valleys in the carboniferous chain, near the longitudinal sections, are not generally excavated on any lines of fault; and are, in the severest sense of the term, valleys of denudation. Yet the actual erosion on the ledges of solid rock at the numerous waterfalls (of which I have attempted to point out the origin), is in general so small as almost to demonstrate, that there must have been a great change in the distribution of the water-channels at some period, very recent when compared with that of the first elevation of the carboniferous chain, before the deposit of the new red sandstone. * As an example of this, I may state that at Cross Pits, in the valley of Dent, the coal-seam under the twelve-fathom limestone is divided by a band of clay, half an inch thick, into two parts, with distinct mineral characters; and that the same coal-seam, with exactly the same subdivisions, has been found in the mountain on the opposite side of the valley, at the distance of three or four miles measured in a straight line. This seems to prove that a bed, not more than a fraction of an inch thick, was originally continuous through an area, probably several miles in diameter. Ay OR iia) Fon re ata i , ‘s 1V.—Observations on some of the Strata between the Chalk and the Oxford Oolite, in the South-east of England. By WILLIAM HENRY FITTON, M.D., F.R.S. P.G.S., &c. [Read June 15, 1827.] a.) IN a paper published in the Annals of Philosophy for November and December 1824*, I gave an account of the order and characters of the strata which occur beneath the chalk on the coast of part of the Isle of Wight and of Dorsetshire, and stated some reasons for supposing that a similar arrange- ment would be found to exist in the interior of England. The principal objects of that paper were; First, to distinguish as a separate group, the series of strata now called the Lower Green-sand ;—which had pre- viously been confounded either with the beds containing green particles immediately below the chalk, or with the sandy and ferruginous strata conspi- cuously exhibited on the coast at Hastings, and then called “ Iron-sand.’’ Secondly, to indicate more clearly than had been done before, the peculiar characters of the group, which succeeds in a descending order to that just mentioned, and is remarkably distinguished by its fossils from the strata imme- diately in apposition with it, both above and below. For this latter group, which includes the Weald clay, the sand of Hastings, and the Purbeck lime- stone, and is well entitled toa separate denomination, I have adopted the name of “Wealden,” proposed by Mr. Martin, in his valuable memoir on the West of Sussex. (2.) The objects of the inquiries which have produced the following pages were, to compare some portions of the series of strata between the chalk and the Oxford oolite, in different parts of the South-east of England ; to ascer- tain the existence of the Wealden in the interior; and, if possible, to deter- mine its boundaries. * Annals of Philosophy; New Series, 1824, vol. viii. pp. 365, 458, &c. + “ Memoir on a Part of Western Sussex”: 4to, London, 1828. 104 Dr. Frrton on the Strata below the Chalk. In stating the result of this investigation, I shall give a series of sections of the strata below the chalk, at places which I have myself examined *, beginning on the coast near Folkstone, and following the outline of the chalk thence to the sea on the N. West of Norfolk. The relative situation of these places is shown in the map annexed to this papert. The intermediate country, in general, I have not examined in detail, and some points of importance I have never seen; but those who may have opportunities of continuing the inquiry, will find, I hope, no difficulty in connecting their observations with mine. (3.) The series of strata about to be described extends from the Chalk down to the Oxford oolite or coral-rag, and is composed of alternating but irre- gularly distributed beds of Sand, Clay, and Stone. Among the sandy strata, it is important to discriminate not only between the Lower green-sand and that of Hastings, but to distinguish both from a third group, consisting principally of sand abounding in green particles, which lies beneath the Portland stone. Clay, of several varieties, occurs in all parts of this series; but three groups, constituting the Gault, the Weald-clay, and the Kimmeridge-clay, derive pe- culiar importance from their generally occupying valleys, or depressions, at the foot of the escarpments of the Chalk, the Lower green-sand, and the Port- land stone, respectively, and thus producing conspicuous natural features in the tracts where this succession is observable. The stone of the tracts under consideration is either limestone; indurated sand-rock; chert; or siliceous matter intimately mixed with carbonate of lime, in the form of grit,—which has commonly a concretional structure, and seems to pass into continuous beds only by the approach and ultimate union of the concretions. But the most remarkable distinction, in the suite described in this paper, arises from the great difference of character in the organized remains which the principal groups include. The fossils of the chalk and green-sands and those of the Portland stone, are all marine, and the species numerous. But in the Wealden, between the lower green-sand and the Portland stone, although the fossils are abundant as to quantity, the species are comparatively few, and by far the greater part of them belongs to fresh water. The whole of the phe- nomena, in short, presented by this remarkable assemblage of beds, are such as to accord with the hypothesis of their having been deposited in fresh water communicating with the sea. * Plates X. a, and X. b. - + Plate IX.—The detail, upon a larger scale, will appear in the new edition of Mr. Greenough’s Geological Map of England. Dr. Firron on the Strata below the Chalk. 105 (4.) Combining these sources of distinction, the following arrangement and subdivisions may be adopted, the nomenclature of which, however exposed to criticism, is now probably too well established to be changed without incon- venience™. { Upper. 7 Cuarx.... < Lower. L Marly. Fossils, marine: species nu- Upper green-sand. e merous. Green-sanp < (Gault. | L Lower green-sand. J ( Weald-clay. 7 WEALDEN.. Q Hastings sands. > of fresh water: species L Purbeck strata. j few. A Portland stone. Fossils, for the greater part, Part of the Portland sand. Fossils, marine: species nu- Ooxrtic Surtees ) Kimmeridge and Weymouth clay and sand. merous. Oxford oolite (Coral rag). (5.) I proceed now to describe the Sections of these strata, beginning with the coast of Kent; and I shall connect with each section a list of such fossils as I have either found myself, or obtained on good authority from the places men- tioned. The whole of the shells in these lists have been examined and named by Mr. James Sowerby, by whom also the drawings of the supposed new species were made, and the annexed engravings executed}. It is right to mention this explicitly, both that I may take the opportunity of expressing my acknowledgments for Mr. Sowerby’s valuable and assiduous cooperation,— and that, being myself but very slightly acquainted with Conchology, I may place the portion of the following pages which relates to that subject on better authority than my own. Vicinity of Fouxstone, Kent. (6.) The small map, (Plate VII. fig. 1.,) reduced from the Ordnance Survey, represents the country in the immediate neighbourhood of Folkstone and * | have stated in another place (Annals of Philosophy, vol. viii. pp. 461, 462,) some objections to the employment of names for geological strata, which refer to characters not essentially con- nected with the structure or position of the objects to be designated. But the term green-sand, however faulty, besides the universal use of it in England, has been adopted both in Germany and France ;—where, however, it may be regarded, in some measure, as free from the disadvantages of a significant name. } Plates XI., et seq. VOL. IV.—SECOND SERIES. P 106 Dr. Firton on the Strata below the Chalk. Sandgate,—the relative position of this tract being shown on the general map, (Plate IX.). The View (Plate VIII.), for which I am indebted to the kind- ness of my friend the Rev. J. D. Glennie of Sandgate, shows the actual appear- ance of the coast from Eastware Bay to Hythe; and the section (Plate X a No. 1.) illustrates the succession of the strata, on a part of the shore which is not distinctly visible in the more direct view from the sea. (7.) The chalk cliffs in the vicinity of Dover have been described in detail by the late Mr. William Phillips* ; and the presence of the upper green-sand which had escaped the notice of Mr. Phillips, has been pointed out by Mr. De Basterot}. These, with Mr. Conybeare’s more general description {, and Mr. William Smith’s coloured map of Kent, are the only modern geolo- gical illustrations of this part of England with which I am acquainted. But there is a publication of much earlier date,—Packe’s “Chart of East Kent,” with its explanatory memoir entitled ATKOTPA®IA, printed in 1743, which, though not strictly geological in its immediate object, points out very correctly the connexion between the external features and the disposition of the strata in the tract to which it relates, and contains such excellent views in physical geography as to demand especial notice in this place§. (8.) As the chalk rises, in proceeding from Dover towards Folkstone, the upper beds disappear ; the cliffs represented in the view and section consist- ing entirely of the lower members of that stratum. The rise of the marly chalk above the sea level occurs about a mile and a half to the east of the escarp- ment of Folkstone hill, and the place is well marked by the breaking out of a very copious and perennial spring, called ‘“Lydden Spout,” which issues from the top of these marly beds|| ;—a situation probably corresponding to that of the springs which everywhere appear in the interior, along the foot of the chalk range. Near the “Spout” the cliff is about 450 feet high; the upper part consisting of very white chalk, with a bed of flint nodules, the rest of chalk without flints, gradually assuming a greyer hue as it descends. About the middle of the cliff'a thick bed has acquired by exposure a rough and darker surface, by the aid of which it can be traced towards the west ; * Geol. Trans., First Series, vol. v. p. 16. + Geol. Trans., Second Series, vol. ii. p. 334. * Outlines of England and Wales, p. 119—184. § A more full account of this valuable work, which had been previously mentioned by Mr, Co- nybeare, will be found in a tract on the Progress of Geology in England, by the author of the present paper :—London and Edinburgh Philosophical Magazine for 1832, vol. i. p. 447, &e. || A new species of Tornatella, named by Mr. Sowerby elongata, was found in the chalk marl at this place, by the Rev. G. E. Smith. See Plate XI. fig. 1. Dr. Firron on the Strata below the Chalk. 107 and on the shore there are numerous detached masses, composed of round portions of grey marly chalk united by a yellowish-brown cement. The shore itself, at this place, is a firm floor of light bluish grey marl, the beds beneath being of a still darker hue. The vertical face of the cliff retires from the sea about 2000 paces west of Lydden Spout ; and the intermediate shore, thence to Copt Point, is occupied by a mass of ruin, which has fallen from above, in consequence of the rise and erosion of the soft argillaceous beds beneath. The sudden transition to this ruinous under-cliff from the vertical face of chalk is very remarkable. A stratum abounding in green particles, intimately mixed with marl, appears at low water, in several detached places on the shore west of Lydden Spout, and is succeeded by the blue clay of the gault, which continues to Copt Point, where it rests upon the sand and grit of lower green-sand :—the prominence of the Point itself, and of the shore to the west of it, being evidently produced by the greater firmness and durability of the latter stratum. The succession of the beds is best seen in the retiring portion of the shore, immediately on the north of Copt Point, (see Plate Xa. No.1.) A small outlier of the lowest chalk, with green-sand beneath it, is there exposed at the summit of the rounded hill on which stands the Martello Tower No. 3. Copt Point itself consists almost entirely of gault, which tops the low cliff thence to the village of Folkstone. The lower green-sand, rising gradually from the Point, occupies the whole cliff west of the village ; and being continued without in- terruption, through Sandgate and in the heights above Hythe, its outcrop turns from the coast into the interior, at Aldington Corner. Finally, the Weald- clay, rising on the shore beneath Shorn Cliff, occupies the greater part of the heights and sloping ground on which the town of Hythe is placed, and ex- tends about four miles farther to the west, where it gives place to the Hastings-sands. | In my obervations on this part of the coast, I shall confine myself to the beds below the chalk; referring for a detailed account of that stratum to Mr. W. Phillips’s paper, already mentioned. (9.) Upper Green-sand. The upper green-sand near Folkstone, is but a scanty representative of the formation, as it occurs in the Isle of Wight, Surrey, Western Sussex, and some other places in the interior; its total thickness probably not exceeding five-and-twenty or thirty feet, and the stony strata and concretions of chert being altogether wanting. Its rise upon the shore is concealed; and the stratum is first seen in its proper situation be- neath the Martello Tower No.2. A small outlying portion about fourteen feet in thickness, occurs beneath a cap of grey chalk marl about eight feet P2 108 Dr. Firron on the Strata below the Chalk. thick, at the top of the hill on which the Tower No. 3. is placed*; and in this place the stratum consists of a soft marly sand, traversed in every direction by stem-like cylinders, which have within them cores of darker green matter. It also contains some irregular masses of a bright brown or orange hue; but the greater part is composed of grey calcareous marl, like the lowest chalk, so thickly interspersed with green particles as to exhibit only their colour. The fossils which I found in this stratum were few in number, and in- distinct: the only species that could be ascertained was the Pecten orbicu- laris}, one of the characteristic shells of the lower chalk and upper green- sand in Hampshire and Western Sussex. . (10.) The green matter, which abounds in this stratum near Wissant, on the opposite coast of France, has been examined by M. Berthier{ ; who found it to consist principally of silica and protoxide of iron, with ten per cent. of potash. For the purpose of comparing the green-sands of different places and forma- tions, my friend Dr. Turner, Professor of Chemistry in the London Univer- sity, was good enough to examine some specimens from the upper and lower green-sands of Folkstone, of the Vale of Wardour, and the Boulonnois, and also particles of the same kind which abound in the sand and concretions beneath the Portland stone, in the Boulonnois, and in England. I subjoin the result of this examination§, whence it appears that in all these cases the * See Plate VIII. and the Section, Plate Xa. No. 1. + Mineral Conchology, tab. 186. + Cuvier and Brongniart, Environs de Paris, 2nd edit. 1822, p. 249. See also Annales des Mines, iv. 1819, p. 625.; and v. 1820, p. 197. § The following passages are transcribed from the notes with which Dr. Turner has favoured me upon this subject. “The colouring matter of green-sand sometimes appears in the rock of its ordinary green tint, and sometimes in grains of so deep a green that they seem black. The former generally occurs in sand, or where the sandstone is porous, and in this state an ochreous appearance is often observed, due to the green particles being partially decomposed, and their iron having passed into a higher state of oxidation; whereas the black-looking grains are met with in highly calcareous sand- stone, where the texture is too firm to admit of the percolation of water. From either kind of rock the green matter may be obtained by washing with water and subsidence, since the colouring matter subsides less readily than grains of quartz, and more readily than calcareous and argillaceous sub- stances. For the purpose of analysis it is best procured from those calcareous sandstones where the cement predominates, as in the neighbourhood of Hythe and Folkstone in Kent. On reducing such samples to powder, washing away the finer particles with pure water, and separating any adhering carbonates by dilute muriatic acid, the colouring matter is left, mixed only with small grains of quartz. It then always appears in the form of earthy particles of a deep green tint. “ The green matter, when not previously weathered, is very feebly attacked by concentrated acids, Dr. Firton on the Strata below the Chalk. 109 green matter is of the same nature. A slight examination of the green par- ticles, which Sir John Herschel had previously the goodness to make for me, intimated the same results. (11.) Gault. The rise of this stratum on the shore is also obscured by ruins of the superior beds; but it is visible in detached points, at low water, in Eastware Bay, and forms the greater part of the cliff at Copt Point, where many of the more beautiful specimens of the Gault fossils, seen in collections, have been obtained. It appears also below the outlier of the upper green- sand already mentioned (Plate X a. No. 1.); and occupies nearly the whole of the grassy and ruinous cliff between the base of the Martello Tower No. 2, and the sea. Its total thickness is about 130 feet, and it may be divided into even by the nitro-muriatic. It gives out water when heated, and becomes brown from its iron passing into the state of peroxide. As it has been supposed to owe its green colour to the pre- sence of phosphoric acid, it was carefully examined, with the view of detecting that acid, if present. It was accordingly fused with carbonate of soda, the alkaline filtered solution neutralized by nitric acid, and evaporated to dryness, and the neutral solution tested by nitrate of silver and nitrate of lead. Of two samples of green-sand, thus examined, one was found to be quite free from phosphoric acid, and traces only were detected in the other. The former was also free from lime, and the latter contained but a small portion. It is hence obvious, that neither lime nor phosphoric acid are essential constituents of the colouring matter of green-sand, and their presence must be regarded as casual. In order to determine the chemical constitution of the colouring matter, I collected some green particles from the calcareous sand of Eastware-bay, near Folkstone, removing all foreign matter as far as possible, by washing with water and dilute acid. The only impurity which I could detect after this treatment consisted of small grains of quartz, the quantity of which varied in different samples. “A portion of green particles thus purified, very free from oxidation, and dried at 212° Fahr. lost 7-0 per cent. of water when heated to redness. “Another portion of the same sample was fused with carbonate of soda, and the earthy ingredients subsequently separated and weighed in the manner usual in such analyses. ‘A third portion was heated with carbonate of baryta, and examined for potash, traces of which were readily found. According to the total result, the green particles consist of [M. Berthier’s analysis of the green particles from near Havre gave the following proportions ;:— CO SHC Wae She ania ae eA co OT Oe 48°5 SiliGaitectate ic steve afets oterelere ae Heats 50°0 Black Oxide of Tron). ...065.0..0 22°0 Protoxig@e Of [LOM sie'e)e)=/eleraieiere 21:0 AMINA’... se. sleatetearete ole Sette ee moll AD PATTATTITTIANs of cies sree) si sicietel skexelel ets 1 (U MARNESIA. ». 2s see's vise Seniesa SE iepeeiolS Speman Sait, MSTA sheild sate Go eA TO Wiaterierracie css, crecicheisiviecie sine clkcO PMs) sts onic ickteale os via «'e sles! tFaces Potash Uae(a)./ece ACOUDOUOO BNET 10°0 “ 98-3 99°0.] “Tt is superfluous to speculate on the precise atomic constitution of the green particles, since they were not obtained in a state of perfect purity. The ingredients which appear to be essential, 110 Dr. Fitton on the Strata below the Chalk. two portions. ‘The upper part immediately succeeding the upper green-sand contains green particles; and thence, for some feet downwards, it is harsh and sandy. The lower portion consists of a smooth, uniform, very plastic clay, of a light bluish grey colour, much in request for the fabrication of tiles and common pottery. It is in this part of the cliff at Copt Point, that the perfect and beautifully iridescent Ammonites, Inocerami, Hamites, and other fossils, have been obtained. From the Point the stratum rises gradually to the west, forming the summit of the hill, about 108 feet in height, on the east of the town of Folkstone; and some traces of it also exist at the top of the next cliff, on which the church stands. From the coast the gault can be traced in a corresponding situation in the interior, along the foot of the chalk escarpment ; its presence being everywhere indicated by a depression of the surface, and by the marshy aspect of the soil, which generally produces rushes and is strongly contrasted with that both of the chalk above, and of the lower green-sand beneath. It is not improbable that in the Isle of Wight and some other situations where the fossils of the gault are rare, the upper and more sandy portion only of this stratum may exist. At Cheriton Tile-works near Folkstone, the workmen expressly state that it is the lower part only of their pits which affords the shells. (12.) Throughout the gault, but chiefly in the inferior portion, concretions of iron pyrites are found, generally approaching to a globular or cylindrical figure, and of a radiated crystalline structure within, or in long thin vermi- cular rods, which at first sight might be taken for vegetable stems. On the opposite coast of France, near Wissant, the pyrites is so abundant in the gault as to have given origin, some years since, to a manufactory of sulphate of iron*; but near Folkstone the quantity is comparatively inconsiderable. hoth from the quantity in which they occur, and their constancy in the colouring matter of green-sand from different localities, are silica, alumina, oxide of iron, magnesia, and water. I should hence consider the green matter as a hydrated silicate of alumina, magnesia, and black oxide of iron, and as being, in all probability, the true green earth, or earthy chlorite of mineralo- gists. The analyses of chlorite hitherto published are so discordant as to prove, either that dif- ferent compounds have been examined under the same name, or that the specimens under exami- nation were very impure. The essential ingredients, however, appear to have been the same as in the subject of my analysis. “Though the foregoing description applies more immediately to the colouring matter of the green-sand from the vicinity of Folkstone, I have obtained similar results on examining that from Hythe and several other places. Indeed, from the examination of many samples of green-sand collected by Dr. Fitton from various localities in England and France, I believe the colouring matter to be precisely the same in all.” * See Annales des Mines, 1819, p. 623. Dr. Fitton on the Strata below the Chalk. lil (13.) Other nodules and irregular masses are also found throughout this stratum, which resemble coprolite in their chemical composition, though no traces of animal structure are apparent in them. These are often associated with pyrites, and traversed by veins of that substance, as in septaria. Inter- nally they are in general of a dark brownish hue, and the fracture is even or splintery, like that of some varieties of chert. The form of these nodules is sometimes very like that of coprolites; but though portions of shells are sometimes found within them, I have not detected any fragments of bone or scales of fishes. The surface of some of the detached masses is eroded, as if by worms ; to the action of which, therefore, they were probably exposed be- fore they were enveloped in the clay. In other cases they are of a very irre- gular figure, surrounding or incorporated with fossil remains, especially of Ammonites, the interior of which is filled with matter of the same kind. Concretions of this description occur not only in the gault of different places, but are also numerous in the bottom of the lower green-sand at Ather- field in the Isle of Wight; and a mass found by Mr. Lyell in the crag at Southwold in Suffolk, which is mentioned by Dr. Buckland*, appears to have been of similar character. The concretions of the gault in Kent evidently agree with those of Havre and Wissant, analysed by M. Berthier, and found to contain about 57 per cent. of phosphate of lime, with a considerable portion also of carbonate of limet. It can hardly be doubted that they are derived from the remains of animals, though no traces of bony texture are now per- ceptible ; and it is not improbable that they may have been the contents of the intestines of marine animals, which fed upon each other, though not in all cases moulded into the form of coprolite. The abundance of phosphate of lime, especially in submarine strata, will not appear surprising, when it is recollected that not only the bones, spicule and scales of fishes afford that substance in large quantities, but also the covering of the Echinodermata, and of crustaceous animals, in a smaller proportion f. * Geological Transactions, Second Series, vol. iii. p. 234, note. t Dr. Prout, soon after his examination of the Coprolites, of which Dr. Buckland has given an account in the Geological Transactions (Second Series, vol. iii. p. 237 &c.), was good enough to examine some of the concretions from the gault of Kent and the Vale of Wardour, and from Ather- field, and found them all to contain phosphate of lime, united with carbonate of lime and oxide of iron, in different proportions, the dark-coloured varieties containing the largest proportions of the phosphate. They all, likewise, yielded, more or less, the peculiar smell given out by coprolites when dissolved in muriatic acid. Dr. Turner has since examined other specimens, from the gault beneath Blanc-nez, and at Lottinghen on the east of the Lower Boulonnois, and finds them to indi- cate 2 similar chemical composition. { Hatchett “On Shell and Bone, &¢.”; Philosophical Transactions 1799, p. 323, and 1800, p. 373. 2 Dr. Frrron on the Strata below the Chalk. (14.) The following is a list of the fossils of the gault in this neighbourhood, in my own collection, and in those of Mr. Hills, of Court-at-street near Lympne, of Mr. Sowerby, and some other of my friends. I take the present oppor- tunity of expressing my obligation, especially to the Rev. Gerard E. Smith and Mr. Hills, for their kindness in supplying me with all the new species of their collections, many of which are figured in the plates annexed to this paper. Lord Greenock also has been so good as to allow me to have drawings taken from some specimens collected by himself. List of Fossils from the Gavuut, in the vicinity of Fotkstone, Kent*. Ammonites auritus. Fleur de Luce pits near Folkstone. F. A. Benettiz. Leacon Dill, about two miles S.W. of Charing, Kent. S. A. Beudantii. (Brongniart; Env. de Paris, tab. vii. fig. 2.) Cheriton. F, A.? circularis. PJ]. XI. f.20. Burham near Maidstone. So. A.crenatus. Pl. XI. f.22. Tile-works at Cheriton. F. A. dentatus. (Syn. A. serratus, Parkinson.) Leacon Hill. S. Fleur de Luce. F. A. inflatus. Folkstone. F. A. lautus. Leacon Hill. S. Folkstone. Min. Conch. A. minutus. Folkstone. Min. Conch. A. proboscideus. Folkstone. Min. Conch. A. Selliguinus. (Brongniart; Env. de Paris, tab. vii. f.1.) (Syn. A. levigatus ? Min. Conch.) Cheriton, near Folkstone. F. A. splendens. (Syn. A. planus? Mantell.) Leacon Hill. S. Tile-works, Cheriton. F. A. subcristatus. (Brongniart; Env. de Paris, tab. vii. f. 10.) Fleur de Luce near Folkstone. F. A, symmetricus. Pl. XJ. f.21 and 23. Clay-pits near the Fleur de Luce, Folk- stone. F. A. tuberculatus. Weacon Hill. S. Fleur de Luce pits, near Folkstone. F. A. varicosust+. Folkstone. M. C. * In this and the subsequent lists of fossils, the names are disposed in alphabetical order, for facility of reference. The new species are in Roman type, the rest in Italics. A systematic list of all the genera and species of the several lists will be given at the close of these pages. In the statement of localities, the capital letters after the names of places denote the persons to whose authority the occurrence of the several species is referred ; H. signifying Mr. Hills, of Court- at-street near Lympne; S., the Rev. G. E. Smith, A.M.; So., Mr. Sowerby; G., Henry H. Good- hall, Esq.; F., the Author of this paper. The letters M. C., or Min. Conch., denote the Mineral Conchology of Messrs. Sowerby; Geol. Soc., the Museum of the Geological Society. + Mr. Parkinson has mentioned other species of Ammonites; 4. ornatus, from Folkstone and Cambridge, 4. pansus, from Folkstone and West Malling, Kent (Geol. Trans., First Series, vol. v. pp. 57 and 58). The A. serratus of Parkinson is 4. dentatus of Sowerby. Dr. Firron on the Strata below the Chalk. 113 Auricula inflata. PI. XI. f.11. Copt Point? S. Belemnites alttenuatus. Weacon Hill. S. Near Folkstone. F. B. minimus. (Syn. B. Listeri.) Folkstone. F. Cardium? decussatum. Copt Point. S. C. (species doubtful). Indistinct specimens, apparently different from C. decussa- tum. Caryophyllaa. Folkstone. F. Corbula striatula. Folkstone. Min. Conch. Corystes? Mantell, Sussex. Pl. 29. fig. 13. Near Folkstone. S. Cytherea parva. (Syn. Venus parva; M.C.) Eastware Bay and Leacon Hill. S. Dentalium ellipticum. Copt Point. S. Exogyra conica. Near Hythe. H. Gastrochena (species doubtful). Found in perforations of dicotyledonous wood. Kast of Folkstone. S. and F. Hamites aculeatus. Pl. XII. f.4. Copt Point. H. and S. The Rey. G. E. Smith’s observations on the new points in the structure of this genus will be found hereafter, with Mr. Sowerby’s description of the species figured in the Plates annexed to this paper. The figures in Pl. XII. are from drawings by Mr. Smith. HT. armatus. Near Folkstone. F. Hi. attenuatus. Pl. XII. f. 3. Copt Point. HI. compressus. Fleur de Luce near Folkstone. F. Hi. gibbosus. Fleur de Luce near Folkstone. F. H. elegans. (Parkinson, Geol. Trans. v. p. 58.) Folkstone. S. Hi. intermedius. Leacon Hill, and Fleur de Luce pits. F. H, maximus. Leacon Hill. S. Fleur de Luce. F. H nodosus. Near Bythe. H. HI. rotundus. Pl. XII. f.1 &2. Copt Point. S. HI. tenuis. Near Folkstone. F. Inoceramus concentricus. Beautiful specimens of I. concentricus and sulcatus, with va- rious Ammonites, retaining the pearly lustre of the shell, are found in great num- bers about the middle of the cliffat Copt Point. F. Folkstone; W. Malling, Kent; and Cambridge : (Parkinson, Geol. Trans. v. p. 57, 58.) Also at Leacon Hill. S. I. Cripsii?’ Mantell, Geol. Sussex, P]. 27. f. 11. Near Sandgate. I. sulcatus. Folkstone; W. Malling, Kent; and Cambridge: Parkinson. Modiola bella. Pl. XI. f. 9. Near Hythe. (Lower Green-sand?) H. and F. _ Murex calcar. Folkstone? F. Natica canaliculata. (Syn, Ampullaria canaliculata, Mantell,) Pl. XI. f.12. Near Folkstone. S. and F. The specimen a, } is filled with brownish (coprolitic ?) phosphate of lime. Nucula bivirgata. Pl. XI. f.8. Eastware Bay. H. and G. Leacon Hill. S. N. ovata. Mant., Geol. Sussex, Pl. 19. f. 26.27. Folkstone. Mantell. N, pectinata, Copt Point and Leacon Hill. S. Fleur de Luce pits and Cheriton. F. W. Malling, Kent; and Cambridge: (Parkinson, Geol. Trans. v. p. 59.) VOL. IV.—SECOND SERIES, Q 114 Dr. Fitton on the Strata below the Chalk. Nucula? undulata. Copt Point? S. Ostrea macroptera? Fleur de Luce near Folkstone. M. C. and F. Panopeaa plicata. (Mya plicata, Min. Conch.) Near Folkstone. M. C. Pentacrinus. P\. XI. f. 4. Copt Point. H. Plagiostoma elongatum. Folkstone. Specimens have been found 1; in. wide, # in. deep, and 3 in. thick. G. Pleurotomaria Gibsii. (Trochus Gibsit of Min. Conch.) Copt Point and Leacon Hill. S. Plicatula pectinoides. East of Folkstone. S.? Pollicipes levis. Pl. XI. f. 5. Copt Point, Folkstone. H.; with the following species :— P. rigidus. Pl. XI. f.6*. Copt Point. H. P.unguis. Pl]. XI. f.5*. Copt Point. H. Pyrula?}+ Smithii. Pl. XI. f. 15. Copt Point. S. Rostellaria buccinoides. Pl. XI. f.17. Eastware Bay. G. . calcarata. Near Folkstone. S. .carinata. Pl. X1.f.19. Eastware Bay. S. . elongata. Pl. XI. f. 16. Copt Point, Folkstone. H. .-marginata. Pl. XI. f.18. Copt Point. H. R. Parkinsonii. Copt Point and Leacon Hill. S. Serpula antiquata. Near Beachborough, Folkstone. M.C. (Upper Green-sand ?) S. articulata. Folkstone. M. C. S. rustica. Eastware Bay. M.C. (Upper Green-sand ?) Solarium conoideum. (Min. Conch.) Pl. XI. f. 14. Near Folkstone. S. and F. S. ornatum. Pl. XI. f.13. Fleur de Luce near Folkstone. S. and F. Spatangus argillaceus. (Phillips, Geol. of Yorkshire, Pl. II. f. 4.) East of Folkstone. Teredo? In fossil Dicotyledonous wood, Leacon Hill. S. Kolkstone, and Cam- bridge: (Parkinson, Geol. Trans. v. p. 58.) Terebratula biplicata. Folkstone (in gault?). S. T. sella. Near Folkstone (in gault?). S. T. sulcata. Folkstone, and Cambridge: (Parkinson, Geol. Trans. y. p. 59.) Tornatella? affinis. Plate XVIII. fig. 9. Eastware Bay. S. Trochus Gibsii? See Pleurotomaria Gibsii. Turbinolia Kenigii. Weacon Hill. Very abundant. S. Turritella (species doubtful). Folkstone. S. Venericardia tenuicosta. Pl. XI. f.7*. Eastware Bay. H. Venus parva. See Cytherea. V.?tenera. Pl. XI. f.7. Copt Point near Folkstone. H. OU t In naming this genus, and some others mentioned in this paper, respecting which doubts may be entertained, Mr. Sowerby appears to have been influenced by a desire to produce all the infor- mation which the specimens could afford, conceiving that even if the names be erroneous, the figures may still have some value as objects of future comparison. Dr. Firron on the Strata below the Chalk. 115 Wood, dicotyledonous. East of Folkstone. Perforated by Gastrochena; near Folk- stone. S. Sometimes surrounded with pyrites. Mr. Parkinson states that “fossil “ wood occurs plentifully in the marl (gault) of Folkstone; lying chiefly at the “ bottom of the stratum, on the green-sand.”’ Geol. Trans. vy. p. 59. (15.) Lower Green-sand.—T he uniform surface of this stratum, extensively shooting out beyond the chalk, forms a conspicuous feature of the country, which is well seen from the ascent of Folkstone Hill on the road to Dover*. The analogy in this respect to the appearance of the sands at the Black- down Hills in Devonshire, is obvious and striking. The Bagshot sands, above the chalk in Surrey, also exhibit long and uniform platforms, the section of which presents a linear and almost horizontal top, with a rapid escarpment at both extremities. (16.) One of the principal circumstances in the internal structure of the Lower Green-sand at Folkstone, is the distinctness with which it is divided into three groups ; and this subdivision probably occurs wherever the formation is fully developed in the South-east of England. It is clearly seen in Surrey ; I have evidence from Mr. Martin of its existence in the West of Sussex ; Mr. Lonsdale believes it to hold also near Devizes in Wiltshire ; and though I did not become acquainted with it till after 1 had examined the Isle of Wight, I have little doubt that it will be found there also. a. The first of these subdivisions may be characterized as consisting prin- cipally of sand, white, yellowish, or ferruginous, with concretions of limestone and of chert, frequently in false stratification. It forms commonly a flat, but sometimes an irregular hilly surface, rising from the valley of the gault, and bearing a dry, barren soil. b. The second member abounds in green matter, is retentive of moisture, and contains comparatively little stone: it occupies a flat and marshy tract, between the first and third divisions. c. The third and lowest member contains a greater proportion of calca- reous matter, and includes some of the principal beds of stone bearing the name of “Kentish Rag”; which commonly form a prominent ridge at its outcrop, adjoining the valley of the Wealdt. * From Folkstone Hill the ridge of Fairlight Down, near Hastings, is a very striking object : its range is evidently parallel to that of the chalk outcrop, as might be expected in the axis of elevation of the tract by which it is surrounded. + In Mr. William Smith’s Geological Map of Kent, two ranges are indicated, by darker co- lours, in the tract between the coast and Maidstone; one running parallel to the chalk, from Sandgate through Ashford and Bursted to Penenden-Heath, on the N.E. of Maidstone; the lower, less regularly, from Hythe along the verge of the WealdClay. These lines, I have no doubt, indi- cate a subdivision like that mentioned in the text: but in the explanatory table of the map, the stone of the tract thus coloured is said to be the Portland-rock. Q 2 116 Dr. Frrton on the Strata below the Chalk. The situation and relative space occupied by these subdivisions near Folk- stone, are shown in the small Map, Plate VII. fig. 1., and in the View, Plate VIII. (17.) a. The uppermost subdivision is about seventy feet thick. It rises upon the shore on the west of Eastware Bay ; and some of the firm siliceous beds which it includes near the top, coming up from the sea a little to the east of Copt Point, are continued in the cliff thence to the west of Sandgate ; between which place and Folkstone distinct sections are disclosed. The greater part of the country from Folkstone, through Cheriton, to Newington is occupied by this bed, and the heights of Dibgate and Sine Farm, where it finally disappears, are capped with it. (18.) Where the sand emerges from beneath the Gault, it is often loose, and of a white or buff colour; but at the immediate junction there occurs, in many places, a course, from six inches to a foot in thickness, of concretions of pyrites, often investing fragments of silicified coniferous wood, of a dark brown colour. 'The composition of this bed resembles, in several respects, that of the Blackdown sands in Devonshire, the stone which it includes con- sisting principally of siliceous spongy concretions, like the whetstone of that place. ‘The most instructive specimens are to be found in the loose decom- posed masses on the shore. In the vertical faces of the cliffs, the surface exposed by fracture and falling away is at first clean and uniform, no traces of the stratification appearing ; but after a time the sand crumbles from the surface, while the stony portions remaining fixed, become prominent. The whole of these cliffs consists, in fact, of sand and conglomerates more or less firm, produced by the agglutination of the loose materials which formed the original submarine deposit. The strata vary in texture and composition, from the state of sand to that of very hard limestone or chert, of various shades of grey and brown; the latter passing into chalcedony, with which the cavities are sometimes coated*. The transition from the sand into compact stone is sometimes very rapid ; in other specimens the gradations are almost insensible. (19.) The principal components of these conglomerates are the following: 1. Quartz, in rounded fragments, from the bulk of a large pea to the minutest visible size, of several shades of grey and white, varying from trans- parent to nearly opake, and in some instances passing into chalcedony. 2. Small, worn fragments of quartzose jasper, red, or greenish; with flat surfaces, in some cases, indicating stratification. * It is remarkable, that notw:thstanding the abundance of siliceous matter in the concretions near Folkstone, few or none of the petrifactions are formed of it; while at Blackdown in Devon- shire most of the shells in this formation are casts in chalcedony. Dr. Frrron on the Strata below the Chalk. 117 3. Fragments, frequently much larger than those above mentioned, of very compact, dark brown, black, or grey flinty slate. Sometimes the appearance of these fragments is internally that of hornstone, approaching to jasper. 4, Fragments, often angular, or slightly rounded, of schistose granular quartz, or sandstone, interspersed with very minute particles of mica; not effervescent; its colours varying from smoke grey to greenish. 5. Near Ashford, in the ferruginous sand at the top of the formation, frag- ments are found of brown hematitic iron ore; but much less abundantly than in the corresponding part of the section at Redcliff, near Sandown, in the Isle of Wight, and at other places. 6. Near the top of the sands, in the blocks of fenotnpésed stone, upon the shore, lumps are found, from the size of a walnut downwards, of a dark brown substance, externally spongy, and of irregular surface, and within having the fracture and appearance of the phosphate of lime described in Section (13)*. In these brown masses are also some grains of quartz, and small portions of shell. This occurrence of phosphate of lime, both in the gault and at the upper part of the lower green-sand, is an additional proof of the continuity of their deposition. (20.) The stone of the more uniform beds (‘ Kentish-rag,”’) has great variety of characters, from those of a granular or sparry compound to com- pact limestone, some specimens of which might be taken for that of older formations. In many cases, the calcareous cement is so crystalline, that light is reflected continuously from extensive surfaces, although the face of the fracture is thickly set with small pebbles of quartz; in other cases the stone is a dense conglomerate, composed of quartz grains with a small proportion only of the cement. All the varieties contain disseminated grains of the green matter above described in section (10); which is frequently so abundant as to give its colour to the stone. In many of the rolled fragments on the shore near Folkstone, this constitutes more than half the compound, the remainder being decomposed carbonate of lime, inclosing grains of quartz and flinty slate. In the more advanced state of decomposition, the mass has the ap- pearance of mortar ; and, in most cases, the stone effervesces copiously with acids, the green particles remaining undissolved. The chert of this upper stratum is frequently of a dark grey colour, and * The specimens here referred to were sent me from the shore immediately on the west of Folk- stone, by my friend the Rev. J. D. Glennie ; but there can be no doubt of their having fallen from the adjacent cliffs. Among the darker masses mentioned in the text were portions of the claws of an Astacus. On the shore hereabouts plicated Terebratulze were found in nodules of arsenical pyrites, 118 Dr. Fitton on the Strata below the Chalk. very like chalk flint. In some specimens, this dark variety adjoins, with scarcely any gradation, a light grey, or white siliceous agglomerate, in which the original sandy structure is still discernible ; while in the adjacent darker chert the fracture is flat-conchoidal and splintery, with the glimmering lustre of hornstone, all trace of the grains having disappeared ;—as if a sand of wax had been consolidated by gentle softening, in a heat not sufficient for its liquefaction. In its passage to chalcedony, the siliceous matter often assumes a white colour, the aspect being nearly that of porcelain, and it becomes translucent when moistened. (21.) A section of the upper part of this member (a) of the lower green- sand, in the cliff about midway between Folkstone and Copt Point, was as follows : Top of the Lower Green-sand. Feet. Inches. Bluish grey clay (Gault), a few feet in thickness, at the top of the cliff: then— 1. At the junction of the clay and sand is a bed consisting of pyrites in lumps, more or less decomposed; about ..... srevatoteretsietere Ssscolazevoere, efetlevehers 10 veg DLO 2. Grey quartzose sand, with numerous green particles .....+.2seeeeeeeees « 4/90 3. Sand, in which lines of false stratification are conspicuous ...... Bogoopmone sb Ae SiMilarpDUticOArserssand earyererereieteeieieiieiiiere Richer stetcrererereverels Rioteleletehete srevsie’ OR 5. Sand, yellowish, slightly concreted, irregular in thickness; much more solid in the eastern partiofithe icliff; "about... 1c s:. bie « = sieve sio'ejieierars een ccceee - 8&8 @ Gem Sandiesretetetetelelaicielelsjolersioreiencicvere GOOD DO AUTOR GAOCO COO Od0 06 MeooooDGddD | 7. Irregular siliceous concretions .....00+++seeeee- «i.e, 6 s1']s 8 ayo'e oe myais-siejeieie oon) Ol am 8. Sand, nearly as above, with a few dispersed concretions ........ occ ecece .) oo 9. Irregular concretions, like No.7 .........6. sole eisteie) o(etsvelchele etstsleiaiateneatete 1's 10. Sand, with a few scattered concretions ........cssecccsccccccvesece ccoee ORE 11. Irregular concretions, in sand; more dispersed ........+-+.0+ Somd0a0000N 2 © 12. Sand, as above..... atau lorageherieveroveyoie re sxe lols) ¢+s) «lope teraveueseie enero lover detehonomeneeetete 4 6 SH eConcretions) 1-16 //e1sle\el abies sicisieperskere /oletelsiets oretave: stelelieve:cheredeetenenerenerenern tere . Ov Sito {ASI Sandeaspaboves DUtINer + AD OUL,. «cle /cle) alors ciclete oie lcle ol cialersicietetercielerneroneteiete by (0) 15. About four courses of concretions, with sand between ......--.2eseee0e Pe 16. Sand ;—to the foot of the cliff.......... araralelecatclereig i cise alee eieteterercketene oct A eo Total; about =... coum0e The concretions of Numbers 5, 7, 9, 11, 13, 15, consist of siliceous spongy stone, like the whetstone of Devonshire, varying from a loose friable mass, to the consistency of chert. In many instances the surface has the form of cylin- drical stems. * The height of the cliff at this place is really not more than thirty feet; but the proportions are nearly as above given. Dr. Fitton on the Strata below the Chalk. 119 (22.) In another section of this part of the stratum, at one of the quarries about midway between Risborough and the east of Sandgate*, the detail was thus: Surface of the hill. Feet. Inch, Feet. Inch. 1. A group, consisting of alternate courses of sand and irregular siliceous 7 concretions :— a. Sand, with a few interspersed concretions .....eeseeeeeeeeee O 8 b. Stone, in irregular spongiform concretions, including fragments of Oysters or Gryphites, and passing into grey, compact chert, which in some instances graduates into chalcedony ;—retaining, however, traces of the original sandy structure. The concre- tions include also minute fragments of calcareous matter, so that the surface effervesces in detached points; about ...... 0 2 c. Sand; loose, somewhat coarse, consisting principally of grains of about QUATEZ «cc ccccccescecreserccveccrccccccsesscecsesees 0.6 3.0 d, Stone; in loose spongy concretions, white, opake, and in some places more compact within, like chalcedony; not effervescent. 0 4 e. Sand; coarse, dark brown, not effervescent; a great part con- sisting of grains of translucent quartZ .....eeesscecsecceee O 6 f. Stone; in roundish, flattened concretions. A conglomerate of gra- nules of quartz, with some portions of flinty slate, and dark green specks, cemented by sparry carbonate of lime: from 2 inches to 0 8 g. Sand; dark greenish grey, not effervescent, including casts of PTAC AY THES 9 os + o!05 ala.o's sels «sie pio winieialoicicwis alvclae <0 i, SUBWE 660 boat b0 6066 SAREE OER nee Donn BORE aneae o m Oo B t. Sand; dark greenish grey, gritty, not effervescent .........++6 0 the whetstone of Blackdown; not effervescent .....-eceesececcecs 3. Beds of sand, partially concreted, somewhat coarse, soft, effervescing copiously, and including concretions of cherty stone. The false stratifi- cation of this part of the cliff is very conspicuous ......20.ese0eee: 4. Stone, alternating with sand: thus :— a. Stone, in somewhat compact concretions, oblique to the general stratification, including cylindrical portions, like the stems of Siphonaria; the greater part siliceous, white and opake, but effervescing in detached spots; about ......sesesccecseeee b. Sand, greenish grey, effervescing copiously........seeeeee0e. c. Stone, in loose, spongy, irregular concretions ........2+e+200 oo 0 6 oon 6 d. Sand, loose, greenish grey, effervescent ......ssseseeeeeeees e. Stone, in spongiform concretions, like 1. 6, above, passing into eh Sacchi ia loleti =: mpicipicip in p)a'vid-s\nydyesa.nieswiessie mya ei civieli chic gislniaensilaspinsisincenceesensae 0. 9 g. Stone, in spongy concretions; as at Blackdown ......0++.ee00% J 2. A bed of siliceous and porous concretions, nearly continuous; very like | o aS * See the Map, PI. VII. fig. 1. 120 Dr. Firron on the Strata below the Chalk. 5. Sand, with concretions; greenish grey, uniform, not effervescent, At the 2 bottom of this bed is a course of concreted sand passing into stone, with seams oblique to the general stratification. The stone is in some places opake and white, like chalcedony, including however minute dark green | particles: the looser pieces are spongy, like the Blackdown whetstone. . 6. Sand and stone: thus :— 7 a. Sand, resembling that of No. 5, but of darker colour ........- b. Stone. A dark grey, compact, fine-grained, conglomerate of cal- | careous spar and grains of quartz, in some places traversed by about EMI VEINS OL SPAT -teloledeteiede ate ole Kelateroh stole cl orelaeenetetele sia ete tetas 3. 0 c. Sand, resembling a, uniform, not effervescing..........2+. ts d. Stone ; a compact conglomerate, including small portions of dark SS flintyiislateitenstyeteleteeteltedelercts¥- wieteitsteletsi ee el ois) visdelrcelvere retake es Total .... about 16 0 In another quarry, immediately beneath this one, the composition was ap- parently the same ; but the beds of chert were more numerous. (22.) The false stratification above alluded to, or the subdivision of the beds by lines oblique to the general course of the stratification, is a promi- nent circumstance in the upper part of the lower green-sand in this neigh- bourhood. It is observable in several places on the road from Hythe to London ; and was very well exhibited in the sides of the road through the hill between Sandgate and Folkstone, where the sketch subjoimed was taken. 4 SS rk a (oa 5 Sear ee A Ch ae In the beds, of which a portion is here represented, not only the lines of division, but the concretions within the strata exhibit the oblique arrange- ment; and in some instances, the larger cherty masses, the general direction of which is that of the prevailing stratification, send out offsets in the direction of the false strata, as expressed in the sketch. ‘There is no appearance of Dr. Firton on the Strata below the Chalk. 12] variation in the circumstances under which the different strata were deposited, although some of those traversed by the lines above described alternate with others, in which no traces of them, or scarcely any, are to be seen. (23.) The concretional masses described in the preceding sections give rise to. some questions of great interest in geology. ‘There can be no doubt that all these strata were originally deposited in the state of sand and gravel ; but in the quarries of East Kent all stages of gradation can be perceived, from distinctly separated concretions of stone*, to others so nearly uninter- rupted, that the next step into perfect continuity can be easily conceived. The sands below the Portland-stone the coral-rag and the inferior oolite, afford examples of the same character: and in all these cases the concretions must have been formed after the deposition of the sand which includes them, and probably beneath a great depth of compacted materials. In such a mass, shut off from the free access of air and change of temperature, there is no obvious reason for disturbance of the affinities which maintained the original form of the components, except the decomposition of the animal and vege- table remains diffused among the stony substances; yet here we have not only solid limestone, where nothing but loose sand and gravel were before, but firm siliceous concretions, pervading, and so identified with, the separated particles of the quartzose sand, that the whole is nearly homogeneous. If the decomposition of the organized substances, continually acting throughout very long periods of time, be not sufficient to produce the whole of these effects, perhaps it may be supposed that electricity is the cause which sets free the elements, and disposes them to combine anew f. (24.) The second, or middle subdivision (b.) of the lower green-sand, first * Concretions nearly globular occur, in the uppermost yellowish sands, at Parkhouse, near Folkstone. + In preparing nitric acid in a chemical laboratory where I was attending some years ago, the glass retort broke towards the close of the operation, and a quantity of the concentrated solution of bisulphate of potash oozed out through a very fine crack into the surrounding sand. On re- moving the retort some time afterwards, a large part of the sand was found to be agglomerated into beautiful concretional masses, like bunches of grapes, the greater portion of which, of course, was sand, and the cementing substance the crystallized salt. ‘The masses of gravel frequently found cemented by carbonate of lime, or of iron, in consequence of the escape of the carbonic acid which had held those substances in solution, is an example of another mode of concretion. In the first of these two cases the loss of heat, in the latter the escape of a chemical solvent, has obviously been the cause of the consolidation. But the case mentioned in the text is distinct from both. Dr. Turner justly remarks, respecting substances usually considered as insoluble, that “ although “the weight of such bodies is not perceptibly diminished by trials conducted in the laboratory, “ during a short interval of time, and with small quantities of water, the effect of the same opera- VOL. 1V.— SECOND SERIES. R 122 Dr. Firron on the Strata below the Chalk. appears upon the shore on the west of Folkstone, at a point immediately be- neath the church*, which is well marked by the breaking out of a spring. It is there conformable to the strata described in the preceding sections, and the whole of it has risen to some feet above the sea, on the east of Sandgate, where rocks of the subjacent group (c.) make their appearance on the shore. This second stratum forms the middle of the cliff above and behind the village of Sandgate, but thins off and disappears in the heights on the west of Nail-Down, where some outlying portions of the superior sand (a.) cap the summit of the hills. Its thickness appears to be from 70 to 100 feet: it abounds in green matter, and in some places in pyrites; from the presence of which substances (though in what manner is not obvious), or perhaps of some portions of clay, it acquires a retentive property ; so that the soil over it is marshy, and ponds are frequent upon its surface. The tracts, therefore, which it occupies, have in some cases in the interior been erroneously sup- posed to belong to one of the beds of clay subjacent to the green-sand. (25.) The boundaries of this middle bed, where it is disclosed by the streams having cut through the incumbent sands, are sufficiently indicated on the map. In following up the streams towards Inbrook and Frogwell, the contrast of the two strata is very conspicuous, the junction of this retentive middle group with the sands above being indicated by the breaking out of springs}; and a line drawn through the heads of the streamlets thus arising would be throughout at distances from the outcrop of the chalk nearly pro- portioned to the inclination of the strata. (26.) The presence of this stratum occasions frequent falls of the incum- bent sand beds, and has given origin to an under-cliff covered with vege- tation, which extends from Folkstone to Sandgate. The sections therefore are obscured; but enough is visible to prove that it contains no prominent beds of stone, and that concretions are comparatively rare in it. Near its junction with the stony strata beneath, the consolidated sand affords several characteristic fossils; and about the middle of the heights over Sandgate f, a line of ferruginous nodules has been found, inclosing fossils, like those of ‘tion, as performed on the great scale in the mineral kingdom, during hundreds and thousands of ‘years, and with unlimited quantities of the menstruum, might be, and doubtless was, very dif- “ferent.” —‘ Report of a Lecture on the Chemistry of Geology’; Lond. and Ed. Philosophical Magazine, 1833, vol. iil. p. 24. * See the View, Plate VIII. + It is not impossible that the site here mentioned may correspond to that of the Sandrock spring, in the Isle of Wight. A ferruginous spring, I was informed, does exist in the vicinity of Sandgate. + In the grounds of Encombe, the seat of Mr. Dawkins. The place is indicated in Plate VIII. Dr. Firton on the Strata below the Chalk. 123 Shanklin Chine in the Isle of Wight, and of Parham Park in Western Sussex. (27.) The following sections, at a prominent point of the cliff, between Sandgate. and Folkstone, include a portion of the first or upper member of the lower green-sand (a.), with the upper part of the middle stratum (0.). Section of the Cliff between Folkstone and Sandgate. ( (a.) Feet. In. Feet. In. 1. Sand, with numerous courses of concretional stone, and traces of false about BELHEMCAPION. | ‘ejais of eerste claieietals 8:6 60 CAOIOG ROH AES eC AO renee as TO 0 2. A prominent group of sand and concretional stone ; qa, Stone. Firm, uniform, fine-grained, sparry, conglomerate, with 3) minute, dark green particles. | Some of the blocks on the shore, apparently fallen from this | about bed, consist of close-grained splintery limestone, somewhat + 2 0 sparry, including minute dark grains, disseminated in small one proportion. They afford excellent specimens of the ‘Kentish 8 ? 0 “5 feo op GbE GSO BebOr CNBr ae Stevesatelers.« Heidaden- “5 b. Sand, including concretions of chert; about ........ sieretelege ek ia c. Stone. Loosely concreted conglomerate, including shells, effer- about vescing copiously ; when decomposed looks like mortar .... i a 3. Several courses of sand and concretional stone ; @. Sand.........+: BEM Iels aia elelS nis, © 5.0356, 01 0'6.0 is ¢ sealers cp oe 4 49 b. Thin course of concretional cherty stone, nearly continuous.) 9g 4, | The chert passes into chalcedony, and the spongy portions to I A CINGEe SHEIIS' ‘srcctelelayeles cles o sicic.c siavole sloletetebeletercvateterernrcicie 0 6 altogether ec. Sand, with spongy concretional stone, approaching to that of } 4 aaa Blackdown, but IGoser wee cose eveccnsse eyopdate sie ore oe 5 EU EME )< acis sc crs ow sieges os rehe o/s: ai-n/e\ eit ele clots «00S st mci e Abiko ? e. A bed of siliceous masses, like the stems of Siphoniz ; about . 0 .6 Batu. cas. be hee ene 4 As ele ED - r | g. Greenish grey concretional stone, in irregular masses........ 2 J about 25 feet. (5.) 4, Greenish grey and yellow sand, including various concretions ; MIENSAMhs vias oieleen cartes Siete ora colaio aiata c's ele ce u's s about 5 or 6 0 7 b. Very large concretional nodules, consisting of greenish sand, : | woe Sada COMER EL (oh: 515 ove /alci «sje sim/e.0's:6's «,< 6.0.6 0.0 506-0, and ce. Sand, without prominent beds of stone; about....... ap ein shee 40 0 50 0 Total ...... from 70 to 80 feet. Beneath is the plateau of the under-cliff, supporting ponds, and producing R 2 124 Dr. Firron on the Strata below the Chalk. rushes ; probably thirty-five to forty feet in thickness, down to the sea :—of. part of which the section is as follows :— ( b.) By rs 1. Yellow sand; face nearly vertical, from a recent fall.........seeeeee eiereherotorete { ; to 7 2. Dark smoke-grey, crumbling, sandy clay, or cohesive sand, greenish at the about NXE oo oodosdongp0adoDbdGDDR00DONDD ED DOUDANDAGH solleloleraiateiolelelslelotst= } 8 0 3. A band of firmer green-sand, splitting horizontally into very thin layers, from the interposition of lighter-coloured sand, which seems to occupy the place of ain | cylindrical stems or twigs. In this bed the hammer leaves a mark of a vivid green colour, but the general above hue is dark greenish grey. It consists of very minute particles of quartz, in- 0. a3 timately mixed with a large proportion of the silicate of iron, soft, and of a full green colour ; not effervescent, except in minute spots. The gradations from this compound through all shades of colour and consistence, to brown, and even yellow, sand, axeumaperceptibler <-jjclelstetekettetefetareisteteletelel= telet=(ole: ~ At the more northern of these quarries, A, the beds are distinctly, but slightly, curved; and the strike is not parallel to the general course of the ridge, but runs from about 16° east of north to 16° west of south ; forming, with the direction of the ridge, an angle of about 64°. At the second quarry, B*, (of which a sketch on a larger scale is given below,) both sides of the saddle are visible within the distance of a few paces, the beds on the north rising at an angle of about 60°, while on the south they decline at an angle of about 45°. North. 3 South. In the southern portion of this section, which is about twenty-two paces in length, and twenty-five feet high, I counted twenty-two beds of concre- tional stone alternating with sand, and varying in thickness from eighteen inches to nine. * This place is immediately on the east of a barn on the road-side, north of Dry Hill Farm, and about 270 paces distant from A, on a line bearing about 36° west of south. Dr. Frrron on the Strata below the Chalk. 135 A second break or open space, like those above mentioned, (p. 133.), occurs immediately on the west of Sundridge Church, which stands on the northern slope, very near the summit of the ridge ; and a third break, with a flat of about 100 paces, separates the continuation of that height from another, occupied by a small wood belonging to Brasted Place, and called by the inhabitants the “New World”: and here the top of the curve is visible in several places, from one of which this sketch was taken. The cracks in the principal bed here represented, (which is about nine- inches thick,) are wide and irre- gular; but the stone has every ; appearance of having been once continuous. The bending of the strata is also very well disclosed in the grounds of Brasted Place itself, at the opposite side of the lane by which they are separated from the little wood of the “New World.” The curve is there less rapid than in the wood ; and the thickest bed of stone, marked A, is traversed by cracks from a quarter to half an inch in width, the separated portions being somewhat displaced, as if they had been forced out of continuity. | North. : 2 nai, 58 te South. (43.) A continuation of the ridge above described may be traced westward from Brasted Place, for about four miles; and on the roadside ascending to the Chart near Moorhouse, about midway between Westerham and Lympsfield, beds are exposed, which dip rapidly to the north ; obviously forming a por- tion of a saddle, like that of Dry Hill, and, to all appearance, a prolongation of it.* From what I have seen in other parts of this country, I have little doubt that many of the ridges within the tract occupied by the lower green-sand may be ascribed to similar disturbances of the strata. A slight indication of something of this kind near Folkstone has been already referred to (32.). On the Ordnance map a prominent range is represented as running nearly north-west and south-east, from the village of Seal, through Seal Chart, to the * Marks of disturbance along a line of direction different from that described in the text, are observable also about half a mile south of Dry Hill, near the Manor Farm House; where the beds on one side of the ravine dip towards a point about 20° south of east, while on the opposite side they are inclined to the west of north. 136 Dr. Firton on the Strata below the Chalk. heights above Stone Street on the south of Ightham Common. This, if not very much exaggerated, is probably a derangement like those just mentioned. The greater ridge of the Hog’s-back itself, on the west of Guildford in Surrey, of which the direction is nearly continuous with that of the ridge at Brasted, may be also connected with it; since the line of the Hog’s-back, if prolonged eastward, would pass through the high range of sand _ hills between Shalford and Martha’s Chapel, and thence almost directly through Park Hill, Cockham Hill, and Tilburstow Hill, which last-mentioned place is the seat of a similar disturbance. The distance from Tilburstow to the inclined strata at Moorhouse, is not much more than four miles, and the whole course of this elevated line is almost uniformly from east to west; the line from Moorhouse to Montreal, through Sundridge, deviating from that direction only:a few degrees te the north. Mr. Martin has described similar cases of much greater prominence and interest in Western Sussex *. (44.) The abrupt rise of the beds in many of these ridges, and the speedy return of the ground to its general inclination, imply the action of a force which, if direct, must have been very near the surface, and too much circum- scribed to be reconcilable either with the effect of gaseous expansion or the impulse of mineral matter in a state of fluidity. The space between the north and south chalk downs seems, in fact, to have been elevated, not by the mere protrusion of one central ridge, but to have been broken up in several different places, so that large portions were thrust outwards, or bent into ridges, by a lateral push, as when a cloth is wrinkled on a table; a mode of accounting for the formation of such inequalities of the surface, which seems more probable than the action of any direct violence from beneath F. * Memoir ec. Ps) 01 et seq. + There is indeed another hypothesis, which would account for the ‘formation of promi- nences of small extent, by forces originating at very great depths. If we suppose a series of strata, comparatively soft and flexible, to be deposited over a tract composed of older rocks, with hills and ridges on its surface, and the whole to be then thrust outwards by a force beneath, the protuberances of the lower mass would compress and bend the strata above them into forms corresponding with their own;—just as in bound books the little inequalities of the cover, or any of the leaves, are impressed on the adjacent pages, and sometimes propagated through a large part of the volume. Nor is this case wholly imaginary. The masses of granite which are found, in many instances, to project above the disturbed strata adjacent to them, must have been elevated after they had cooled,—when their comparative solidity must have been very great :—and among the newer formations, the interval of time between the deposition of many of the groups, now in im- mediate contact, (as of the red mar! and the oolites, near Bath,—the mountain limestone and green- sands in the Lower Boulonnois,) must have been more than sufficient both for the condensation of the lower strata, and their subsequent erosion into prominences and valleys, even if the original surface had been uniform. Dr. Firron on the Strata below the Chalk. 137 SURREY. (45.) Godstone.—The upper green-sand assumes a new character near Godstone ; and a step-like projection at the foot of the chalk appears there more distinctly than in the country to the east. As the productions of the little district between Godstone and Reigate are valuable in commerce, and its structure has been a subject of some doubt, I have given a separate map of it, in Plate VII. fig. 2.* The section, Plate X.a., No. 2., on the line from the chalk through Godstone, shows the position of the firestone beds in the upper green-sand; with the site of a remarkable elevation of the strata at Tilburstow Hill, an account of which has been already published by Mr. Mantell+: and No. 3., the section through Merstham, includes the site of the Fuller’s-earth pits of Nutfield. (46.) The firestone subordinate to the upper green-sand, in this part of the country, was, in 1827, extracted only between Godstone and the west of Reigate. The principal pits were situated on the west of the London road to the former place. ‘The stone was obtained by an adit between five and six feet in height, and the succession of the beds affording it was thus: Section of one of the Firestone Pits near Godstone. Feet. In. - “Hard roof.” This, like the firestone beneath, is a uniform fine-grained con- glomerate or sandstone, effervescing strongly with acids, and easily cut into any desired form, Throughout the stone are dispersed numerous minute scales of mica, and dark particles, scarcely perceptible without a lens. forms a roof to the mines, of such firmness as to support itself to a width 2 17 feet, extending indefinitely inwards. 23 but harder and somewhat finer in grain, easily broken down into sand, effer- ‘fa vescing. The beds 2. 3. and 4. though separated by seams of stratifica- 4, tion, are of nearly uniform character. 0 10 “Green bed” of the workmen. (Firestone.) Stone of the same nature as the last, i 8 5. A bed of bluish grey siliceous concretions, called ‘‘flints” by the workmen, pass- } ing into stone like that above mentioned. Fracture flat-conchoidal. Yielding with great difficulty to the knife; but effervescing slightly. The greyer stone near these concretions is much harder than elsewhere. The siliceous matter as it becomes more pure acquires greater hardness, with a splintery fracture and a glimmering lustre; and the micaceous particles, which are numerous in the softer varieties, are then scarcely apparent. J] 6. “Green bed ;”—like 2. 3. and 4.¢ .......00ceeace Bahr clalaat enenesssareseretetfevose 0 10 * In the small maps of this Plate the inequalities of the surface are not expressed: but the oon can easily be transferred to the Ordnance map. Tt “Fossils of Tilgate,” &c., p. 22. { The more uniform and softer rock of these pits is used, principally, for ieaip fire-places VOL. IV.—SECOND SERIES. x South. 138 Dr. Firton on the Strata below the Chalk. 7. Bottom of the quarry. Stone unfit for working, from its containing much flinty matter. All these strata dip at a very small angle to about 20° west of south. The rock is traversed by fissures, which divide it into somewhat rhomboidal masses; and smaller cracks are sometimes found within the blocks of stone. (47.) The gault hereabouts occupies a tract which bears the name of “ Black- land,” and forms a slight depression below the band which affords the firestone. (48.) The lower green-sand has distinct indications of a subdivision into three, like that of the vicinity of Folkstone (16.)._ On the line of section, No. 2. Plates VII. and X. ponds are frequent, in a situation corresponding to that of the greener middle group (24.); the surface being comparatively low, with vegetation of a somewhat different character. The stony beds of the lowest group then rise to form the escarpment of Tilburstow Hill*, which is nearly on a level with the chalk downs; and at the highest point, there is decisive evidence either of a sinking towards the chalk, or of elevation in an opposite direction ; for at the top of the hill, the beds, which on the north of that place rise uniformly at an angle of not more than 10°, are suddenly thrown up to about 45°. The appearance of the section here is represented in the sketch subjoined : WU \ KK ‘. > Neer oe and furnaces, but is employed also for buildings under water. Great care is necessary, in build- ing, to place the blocks so that the planes of stratification shall be horizontal. The equivalent of these beds in the upper green-sand of the continent, (the Pliner kalkstein of the Germans,) is employed for exactly the same purposes, at Aix-la-Chapelle and other places. * This is the spelling of the Ordnance map: the word in the country is pronounced ‘* Tilbuster.” Dr. Fitton on the Strata below the Chalk. 139 Inclined Strata, near the bottom of the Lower Green-sand, Tilburstow Hill. Soil and loam (marked a a in the cut). 1, Soft nearly uniform sand; when dry of a bright buff colour .........-++.+++ rae) This has the appearance of having slid or subsided upon the next bed below. Immediately above 2. the sand is green. Fuller’s-earth; very like that in the upper part of the pits at Nutfield, hereafter ] mentioned, and also like that which occurs in the lower green-sand at Brill in Buckinghamshire. This clay becomes soft and is diffused in water, but does not break down with the rapidity of common Fuller’s-earth. The bed varies in thickness from 6 inches to 12: the masses of which it is composed have smooth surfaces and a saponaceous feel, with the aspect and lustre of bee’s wax, probably produced by compression and motion on each other ........ A bed consisting of chert and soft sandrock (“ Hassock”), intimately mixed, Feet. In, about Gand 3 and passing into each other; about Oe AC This and the beds 4. 5. and 6. end abruptly above, as represented in the sketch. 4, A course composed of almost continuous bands of brownish grey chert, from 3 or on 10. is like that on the northern surface of the hill, where it is much used for re- pairing the roads. By exposure it becomes divisible into slaty portions, ap- proaching to.a rhomboidal figure... .......ccccecccccssccccsevesvvctes to 6 inches thick, alternating with, and passing into, soft sandrock. This ef . Soft sandrock (“ Hassock”), including green particles: the hue is various where ie exposed. In some places tinged with oxide of iron .......cceeseeceeees . Sand; green while it is moist, but when dry and exposed nearly white, containing } layers which consist of stem-like or vermicular portions of white, translucent, quartzose sand, surrounded by sand of a green colour. This contrast of | colour becomes indistinct in dry specimens, but is very conspicuous when they are moistened. The white vermicular portions have a border of darker green than the rest: they are generally about 3th of an inch in diameter, somewhat curved, and in some cases have short lateral branches with round extremities. This remarkable structure is very characteristic of several parts of the lower green-sand, and is probably connected with the former presence mere AHI Ze DOGIEG, 2 Facial’ 6's ele'sa o'e\s'e! o's a - Seehullers-carthwon an uniorm) bluish! colour ™. 02.1.1. 0 .elee sees os ccees oe oe 7 In this stratum, about 3 or 4 feet from the top, detached nodules are found, | (from six inches to nine in diameter,) of sulphate of barytes, crystallized in > 16 0 oblique four-sided prisms, truncated at the edges and bevelled at the extre- mities, semi-transparent, and of a wine-yellow colour...........+++ee00 9. White sand. The thickness of sand beneath,—between this stratum and the Weald clay, I did not ascertain. The dip of the strata above detailed is about one in fifteen: (the angle, therefore, between 5° and 4°,) towards a point about 40° west of north. * This was sold at the pits (September 1828) at 5s. per ton. The yellowish earth of another 142 Dr. Firton on the Strata below the Chalk. (52.) Reigate-—The map and sections, Plate VII. fig. 2. and X a., Nos. 2. and 3., sufficiently indicate the general relations of the beds here, which have been already the subject of a paper in the Geological Transactions by Mr. Webster* ; where a sketch is given of the history of the remarkable ancient quarries at this place. The firestone forms a terrace beyond the chalk, nearly level with the top of the remotest sand-ridge ; and the gault runs out from the base of the terrace, at first horizontally, and then rises towards the tunnel, by which the road is conducted through the first ridge of the Lower green-sand{+, here composed of cream-coloured and yellowish sandrock. From the town of Reigate the strata rise again towards Cockham Hill: so that there are here two ridges ; first, that through which the tunnel is cut, and secondly, the southern ridge, formed of the lowest sand beds,—with what ap- pears to be the middle, greener sand between. At Earlswood Common, about a mile to the east of the outcrop, the clay of the Wealds is found. The sud- den fall from the chalk to the valley of Reigate and the abrupt rise thence to the outermost ridge of Red Hill, &c., is exceedingly striking. At Reigate Heath, on the west of the town, the vale which seems to be occupied by the middle sands is rushy and moist, bearing pools upon its surface: but the fall of the ground still farther west, where the continuation of the outer ridge of sands might be expected, is also a remarkable feature. (53.) In proceeding westward, the rise of the sands at Buckland is like- wise very rapid. ‘Thence to Holmwood Common, on the south-west, no ob- servations have been made, but the boundary between the green-sands and the Weald is less obviously marked ; and there is a strong contrast between this space and the prominent ridges of Leith Hill; the lower tract, it will be observed, being that in which the streams converge to join the Mole before its passage through the gorge at Dorking. . (54.) It will be seen, even from the map (Plate IX.), that the outcrop of the Lower green-sand, from Reigate to the head of the valley of the Wealds, is not continuous ; two, if not three, distinct tracts of this formation, bounded pit was more in request; the price, however, the same. It is necessary for the purposes of the woollen manufacturer, that the Fuller’s-earth should be free from any admixture of ochre or sand, which are found to cut the cloth. * First Series, vol. v. p. 353, &c. + The relations of a stratum of dark greenish sandy clay, about seven feet thick, immediately above the tunnel at Reigate, are at first sight doubtful. It might be taken for an advanced portion of the gault; but is, more probably, a subordinate bed within the first division of the Lower green-sand ;—a detached portion, as it were, of the middle greener beds, which it resembles in mineral character. A similar bed occurs, in a corresponding situation at Pulborough, which Mr. Martin, with whom I examined it, has since ascertained to belong to the place here mentioned. Dr. Fitton on the Strata below the Chalk. 143 on the south by almost rectilinear escarpments, projecting successively be- yond the narrow and comparatively regular line of the previous outcrop, on the east*. The breaks between these steps coincide with the gorges of the Mole and the Wey; a fact in favour of the hypothesis which ascribes the formation of these gorges to transverse fissures. 1.—The first of these tracts of sand lies between Leith Hill and the opening cut across the sands towards Guildford, by the south-eastern branch of the Weyt, in which the Surrey and Sussex canal has been dug. Its southern verge extends from Leith Hill, through Holdenbury Hill, to Bearland and Stroud-Green, with a mean breadth from the chalk of about 31 miles. 2.—The next step projects about 3 miles further south, with an average breadth of about 6 miles; and its escarpment is nearly parallel to the Hog’s-back throughout the greater part of its length, from the Telegraph Hill, south of Hascombe, to Emily Farm, a little east of the centre ofa line from Hindhead to Thursley. The anticlinal line, hereafter mentioned, along the top of Grayshot Down, may perhaps be the continuation of a ridge, or saddle, of which the beds rising towards Hascombe are the remaining northern portion, the southern slope having been carried away by denudation}. 3.—The sands on the north of the valley between Ludgershall and Harting-combe, may possibly be considered as a third step in these parallel outcrops, though much less regular than the two just mentioned: the lofty summit of Blackdown, at its eastern extremity, is standing out like a promontory, about two miles beyond the other parts of the escarpment on the south of Hindhead. It is impossible not to connect these appearances with the general action of the force by which the whole of this country has been upheaved; all the features coinciding with the hypo- thesis of its elevation on a line or lines parallel to the axis of the forest ridge. (55.) Dorking to Leith Hill, &c.—The tract between Leith Hill and Guildford affords nothing particularly deserving of notice, except the great height (993 feet) to which the outcrop of the lower green-sand rises, at the point on which the tower is placed. The space included between the escarp- * To understand the structure of this country, the reader ought to have before him a map on a much larger scale than that in Plate IX., as Mr. Greenough’s Map of England ;—or the eighth sheet of the Ordnance Survey,—which, however, is by no means equal, in correct representation of the surface, to the more recent portions of that work. ‘} This stream has no name in the Ordnance map. { Another anticlinal line, but in a direction oblique to that here mentioned, is indicated by the line of heights which runs from Milford, through Godalming, and thence by Unsted and Sum- mersbury to Western Street, near Albury; the strata on the south-east of this line, near Godal- ming, dipping at a’small angle to the south-east, obliquely from the range of the Chalk Downs. 144 Dr. Firton on the Strata below the Chalk. ment and the downs from Dorking to Guildford is of nearly uniform character : but in approaching the latter place, the Lower green-sand rises with such rapidity, that Martha’s Chapel equals or out-tops the chalk, though less than a mile distant from it horizontally. Slighter indications, also, of dis- turbance are evident throughout this tract. ‘The lower marly chalk at Deerleap above Wotton is divided by smooth surfaces, produced by the sliding of large masses upon each other: and where the road rises from the mill towards Abinger Church, at a point which corresponds with a con- tinuation of the ridge above mentioned, near Brastead and Sundridge, the beds are curved, so as clearly to indicate derangement. (56.) The road west of Dorking, between Westgate Heath and the Rookery, is cut through the first beds of the Lower green-sand, the top of which is eroded into irregular cavities, resembling those which are found, through_ out the south-east of England, on the surface of the chalk; and, like them, filled with reddish loam and fragments of chalk flints. This being one of many indications, on the margin of the great Wealden valley, that the agents, whatever they were, by which the chalk was excavated, acted in tlie same manner on the beds beneath it, and filled up the cavities with similar mate- rials, at least as far down as the Lower green-sand. Wave c eres Surface. a ...-dteddish Loam and Gravel. 4 oe 00 Or°7ge IC g ° +32 9%QS ie © Vo %200 Bye avalareatave Loner Green-sand. The lower strata of the quarries near Cold Harbour, immediately under the tower at Leith Hill, are almost identical with those of Tilburstow, (p. 139); consisting of very green sand and soft sandrock, which alternate with chert, and include green matter, with white, vermicular or stem-like bodies, as at that place. (57.) Guildford, Godalming, Farnham, Hindhead.—The tract on the south and west of Guildford, and thence to Hindhead, forms one of the most ex- tensive surfaces of the Lower green-sand to be found in England; and the section from the heights on the north-west of Farnham to the Weald, (Plate X a., No. 4.) includes a succession of strata, from the Bagshot sands, one of the highest members of the English series, down to the Weald clay. Dr. Fitton on the Strata below the Chalk. 145 The quarries on the roadside between Guildford and Shalford, disclose a good section of the chalk, with numerous flints, dipping at an angle of about 5° or 6°, a little to the west of north; and on the opposite side of the Wey, beneath St. Catherine’s Hill, the relative position of the lower strata is very well displayed. (58.) The Hog’s-back.—The remarkable ridge called the “ Hog’s-back,” which runs from Guildford to a point about two miles from Farnham, has been produced evidently by an upthrow of the chalk, and the breaking off of the southern portion of the curve. The inclined position of the remaining side of the flexure is very well seen at the western extremity of a large chalk-pit between Guildford and Puttenham, where the strata dip towards the north, at an angle of about 30°. The upper beds are very white, with courses of the usual dark flint nodules; and a remarkable feature in this quarry, is the distinctness with which the chalk is divided into masses approaching to a rhomboidal figure, by seams oblique to the stratification ; the angles of the portions thus bounded, standing out in the face of the cliff, like splinters in the shattered fracture of a crystal. The Upper green-sand forms a slight projection along the foot of the Hog’s-back ; the Gault, a corresponding narrow depression along its whole length; and the Lower green-sand rises so rapidly beneath, that one or many inflections are necessary to account for its wide extent to the south. In approaching Farnham, the gault, near its contact with the sands, abounds in nodules containing a large proportion of phosphate of lime; resembling those of the vicinity of Folk- stone (13.). The upper beds of the Lower green-sand rise, like the chalk, at a very high angle, and must have been bent suddenly in an opposite direction, since they are now continued, with a moderate inclination, several miles to the south, Along the north of Puttenham Common, the sand is reddish, and very like that of Red-cliff at Sandown Bay, in the Isle of Wight. A nearly continuous surface of the sands extends towards the south from Compton to Hurtmore, and North Brook Place, and is resumed on the south of the river, through Westbrook and Upper Eashing. It is again cut through by the stream, which the London road accompanies, on the south-west of Godalming ; but recurs, in the heights south-east of the town, from Holloway-hill and Crown Pit to Munstead Heath, which seems to be nearly on a level with the top of the Hog’s-back. On the west, the upper beds of sand form several prominences, among which Crooksbury-hill is the most conspicuous ; their elevation having probably been the effect of pro- trusion. On the south-west of Crooksbury, the upper sands seem to expand, and to occupy a still wider horizontal space in that part of the denudation which corresponds to the less inclined beds about Farnham. (59.) The general thickness of Lower green-sand here seems to be nearly the same with that of the coast, and may be taken as between 350 and 400: feet; though, from its superficial extent, a much greater thickness might be ascribed to it, if the disturbance and inflexion which it has undergone were not kept in view. ‘There can be no doubt, both from the features of the VOL. IV.—SECOND SERIES. U 146 Dr. Firron on the Strata below the Chalk. surface, and the hue and texture of the strata, that the subdivision into three, which is conspicuous near Folkstone, and not much less distinct in Western Sussex, exists also in this tract. But the precise boundaries of these groups are by no means obvious, for there are not hereabouts those characteristic beds of stone, which are found near the coast; their place being supplied, in the uppermost group, by concretions of a coarse conglomerate, which in the country bears the name of “ Bargate Sione*;” and, in the lowest group, by chert and indurated sandrock, like those of Leith and Tilburstow hills. This comparative scarcity of calcareous matter is one of the principal differences between the eastern and western tracts of this formation. The more ferruginous concretions, (the “ carstone” of Norfolk,) which are very abundant in the upper part of the Lower green-sand of this neighbourhood, are often so compact as to ring under the hammer, and are thence called “ clinkers” by the quarrymen; sometimes forming plates or flakes, a quarter of an inch and upwards in thickness, and curved so as to resemble portions of concentric layers of petrified trees. This stone furnishes an excellent material for the roads, and gives a remarkable reddish hue to some of those which are macadamised in this country. Frag- ments of brown hematite also, like those of the Red-cliff near Culver in the Isle of Wight, are found at many places in this vicinity; as at Thursley, &c. (60.) Godalmng.— The heights about Godalming afford excellent sections, which may with some probability be assigned to the lowest part of the Green-sand formation. The order in general was thus :— Holloway-Hill, Godalming. Feet. In. 1. Green and variegated sand, abounding in large concretions of chert, and of cal- careous conglomerate, (‘“‘ Bargate-stone ;”) which is hard and sparry, and in some places passes into chert. It contains traces of shells and of alcyonic a stems. False stratification is here remarkable; the concretions also following theiobliqueronmalseslinests: 283 .kietok ochre ote stat oy. oe tie eee eee eres gj Some of thelarger masses of this rock are precisely like the concretions on the shore near Folkstone (20.);—a very compact sparry variety of ‘** Kentish-rag.” In the upper sands of Polstead, near Puttenham, irregular concretions of this compound occur, imbedded in soft sandrock, and contain- ing carbonate of lime in rhombs. 2. Sand, of the same kind, without concretions; but including thin beds of a tough] about clay, like pBallleris-earthnte tric eet Licks vie oslo ciel eve ole sieeve elt ee } 25 0 The dip here is towards the south of east, and all the summits are flat and uniform. * The origin of this term is somewhat doubtful. A place called “‘ Burgh-gate,” from whence it may have been derived, occurs in the Ordnance Map, on the south of the escarpment be- tween Hambleton and Hascombe. + The Fuller’s-earth would refer these strata to the lowest division of the sands. Thin beds of that mineral, however, are found throughout this formation. Dr. Frrron on the Strata below the Chalk. 147 Among the looser sandy materials of Holloway-hill are spongy concretions, which show, when moist, the same vermicular structure as at Tilburstow-hill. ‘ Blackheath, south-east of Guildford, seems to have been once a continuation of the sands near Godalming. Its top is nearly level with the chalk range, but lower than Martha’s Chapel hill. On the south, the ground descends to Farley Heath, with a sort of escarpment like that of Crooks- bury and Farnham commons, hereafter mentioned; and the road thence by Farley-green to Hound-house is in a richer sand, supporting pools in several places, and probably belonging to the middle group. Crooksbury Common seems to consist of the upper members of the formation, impending, like an outcrop 150 to 200 feet thick, over the valley of the Wey, between Elstead and Tilford; and on the south of the stream the heights of sand are renewed. Farnham Common is analogous to that of Crooksbury, and apparently a continuation of the same plateau, deeply cut through by one of the principal streams of the Wey. On the south of these, is the lower tract of Frensham and Thursley commons, and thence the ground rises rapidly towards Hindhead, the ascent consisting of sand deeply trenched into channels. A conspicuous group of barren, somewhat conical hills, on the south of Frensham Common, called the “ Devil’s Jumps,” is apparently the remaining por- tion of a stratum of sand reduced by abrasion to the present irregular form; and the pebbles and rolled masses on Thursley Common, immediately on the north of Hindhead, are sandrock, passing into chert, which seems to be unmixed with other matter, and to be the debris of the beds now removed. (61.) Hindhead.—The crest of Hindhead is on the north-east of a de- pression called the “Devil’s Punchbowl,” round which the road is conducted. The highest part of the curve, or anticlinal bending, of the Lower green- sand, seems to be just at a point where the new road, on a lower level than the old, has exposed a face of 10 to 25 feet in height. The flexure is very slight, but sufficiently perceptible, occurring in such a place, to be de- serving of notice. The strata consist of soft sandrock, containing con- cretions, and nearly continuous beds of chert, passing into chalcedony, of various shades of yellow and brown ; with occasional layers of bright yellowish sand, in which the lines of false stratification are conspicuous. All over Gray- shot Down the subsoil is a soft, loose sand of the same description. (62.) The whole of the tract here occupied by the sands, though not unpicturesque, is wild and barren in its aspect, destitute of wood, producing only ferns, heath, and furze. The surface is in fact, to this hour, nearly such as it may be conceived to have been when first uncovered by the departure of the sea; and its structure is just what may be imagined to result from the levelling effect of water under the influence of motion of no great violence. In crossing this desolate region by the main road from London to Portsmouth, it is difficult to believe that we are only forty miles distant from the capital, and midway to one of the chief naval establishments of the empire: but the nature of the soil effectually prevents improvement, and it is not improbable that this tract may remain for centuries U2 148 Dr. Firron on the Strata below the Chalk. unchanged, and still exemplify the power of geological causes in modifying the civil condition of countries, as well as their external features. In the bottom of the “ Punch Bowl,” perhaps 200 feet beneath the road, a small stream arises, and the north flank of the highest ridge of Hindhead, which runs nearly west from the summit, is furrowed by nine or ten similar and nearly parallel trenches: the deepest of these is called Hack- ham Bottom, the stream from which is continued along the verge of Thursley Common to the Wey at Elstead. The ridge represented in the section No. 4. is that of Grayshot Down, as it appears from the lower ground on the north. It declines westward to Harem, and also to the south; so that there is here distinctly an anticlinal line, more than three miles north of the central valley of the Weald between Ludgershall and Harting-combe. (63.) Although Hindhead is the most prominent point in this part of the country, it is not, strictly speaking, the escarpment of the Lower green-sand ; for the strata, which rise very gradually on the west of the denudation, run out to the east beyond the highest summit, and caps of sand are preserved on some of the advanced ridges and in several detached points. For the same reason, Blackdown Hill, about four miles south of Hindhead, is no more than a massive cap of sand, resting with a very slight inclination upon the Weald clay : and all the deep ravines which separate the heights and ridges on the west and north-west of Blackdown, towards Lynchmere and Haslemere, have sand only at top; the clay rising here to not much less than six hun- dred feet above the sea. Blackdown forms the north-eastern promontory of what may be called the central valley of the denudation; the opposite and converging side of which is a similar escarpment of the Lower green-sand, extending from Harting-combe to Bexley-hill. The floor of the narrow intermediate space consists of the Weald clay, which, close to the junction, abounds in Cypris Faba; and where the valley opens into the wider expanse of the Wealds, the first range of the Wealden sand and sandrock, described by Mr. Martin, about 25 feet thick, and at a vertical distance of about 200 feet from the top of the clay, forms a sort of bar, or elevated ridge, across the entrance ; occupying an extensive surface between Ludgershall upon the Lod, and Northhurst, and being thence continued, at a corresponding distance from the top of the clay, all round the denudation. The course of the Lower green-sands on the south and south-west of this valley having been pointed out by Mr. Murchison, it is unnecessary to pursue this description farther. (64.) Weald Clay.—The lowest beds of the tract near Guildford have recently been exposed in a pit for the extraction of gravel at Pease-marsh, an extensive flat on both sides of the London road, between Arlington, south of Guildford, and Godalming. On examining the place, to which my attention was called by Mr. Murchison, I found beneath a thick- ness of four or five feet of flint gravel and sand, distinct strata of blue clay, Dr. Frrron on the Strata below the Chalk. 149 nearly horizontal, though with an irregular surface, including flat nodular con- cretions of iron pyrites, also horizontally disposed. No fossils were visible; but from the situation and characters of the clay, it seemed most probably to be that of the Weald, brought up into this close proximity to the chalk, by the general elevation of all the strata. It is indeed probable that the Weald clay is very near the surface in many other places ; but as the middle group of the sands is also retentive of water, and capable of sustaining ponds, the distinction can be ascertained only by attention to local circumstances. The difference of level is so small in the different portions of the Wey, from Pease-marsh, by Godalming, Pepperharrow, Elstead, and Tilford, that this clay may be the base of the stream throughout ; but many of the ponds which occur at higher levels, in the tract between Dorking and West Sussex, may safely be referred to the middle group of the sands *. (65.) Tucksbury-hillt, &c——The summit of this hill, which forms the northern extremity of the section, Plate X. a. No. 4. is an outlier composed of siliceous and ferruginous sand, upon the surface of which are numerous angular fragments of pale yellowish flint. The ground descends from it on all sides, but with the greatest rapidity towards the valley of the Wey ; and it affords an excellent view, both of the successive outcrop of the strata in the lower country, on the south-east, and (especially) of the tract on the north, occupied by the Bagshot sands}, to which the cap of the hill seems to belong; the flat-topped ranges and the lower barren tracts of that formation being seen from hence very distinctly. The summits of Romping-down and Chobham-ridge project above the surrounding country, with escarpments towards the east, nearly at right angles to the range of the Chalk Downs; but the general rise of the sands is towards the south, conformably to that of the chalk§. The succession of strata observable in * Such are probably the ponds of Berry-hill, Lonesome, Wotton, and Abinger, near Dorking ; of Thorncombe-street, Wormley-heath, Witley, and Lea-house, near Godalming; Frensham Great Pond; and many of the pieces of water in Woolmer Forest. Several of the ponds near Pulborough can with certainty be referred to the geological place mentioned in the text. + This name of the hill is taken from the Memoir connected with Mr. Greenough’s map. Ir the Ordnance map, one point on the summit is called Farnham Beacon. { Warburton: in Geol. Trans., 2nd Series, vol. i. page 48. § I had proof of this rise, in passing along the main road from Guildford. At an early hour of the morning, in October, all the flat country on the north was occupied by a dense uniform fog, which filled the inequalities at the foot of the sand-heights on every side. Above this sea or lake of mist, which afforded a sort of fluid level, the tops only of the ridges were visible, like long dark islands, the southern extremities of which were uniformly higher than the northern; the intermediate line declining at a very small but perceptible angle. 150 Dr. Firron on the Strata below the Chalk. descending from the elevation to the valley of the Wealds, is very in- structive. At the west end of the hill, beneath Warren’s-corner, on the road to Basingstoke, Septaria are found in a stratum of the London clay, which occupies a considerable thickness on the slope of the hill, below the cap of sand. I was informed that “ Pot-earth,” of a different quality, occurs lower down, in Clarehouse-Park, in the situation of the Plastic clay ; and I have seen the Chalk in the decline of the hill, between Lower Old Park and Halfway-house. The Upper green-sand forms a slight prominence beneath this chalk, on the south of Dip- penhall-house, between the words ‘ Dean’s-farm’ and ‘ Ridgway’ on the Ordnance map, the strata dipping not much more than 5° to the north. The rock, which is there called ‘ Marl-stone,’ does not precisely agree with any I have seen between this place and the coast, but is very like some of the strata in the corresponding place at East Knoyle, on the north of the Vale of Wardour. It is a subcalcareous sandstone, or variety of “ fire-stone,” very soft, uniform, of a yellowish-grey or cream-colour, scarcely effervescent, and remarkable for its lightness ; and it includes concretions of a hard splintery limestone, approaching to chert, and of much greater density than the stone which surrounds them. The Gault, on the line of the section, first comes up on the road descending from Ridg- way to the river Wey, but is more distinctly seen at the extremity of Wracklesham; and, in consequence of the more gradual rise of the strata, on the south-west of that village, it occupies a more expanded surface in Alice-Holt Wood, as described in Mr. Murchison’s paper above referred to. On the south of the main London road, where it is crossed by the road to Wracklesham, is a bank with the Lower green-sand at the bottom, rising towards the village. The surface is waved remarkably; and the inequalities are filled up with gravel, consisting of broken flint pebbles, in large proportion, mixed with red loam, and in immediate contact with the yellowish sands below. The top of the gravel, is nearly level; but its depth to the sand varies from 1} to 4 feet. This fact is analogous to the erosion of the sands near Dorking, mentioned above (56). (66.) The mode in which the drainage of the north-western portion of the great valley of the Wealden is effected, and the different manner in which the streams escape, in this part of the country, from that of their egress through the North and South Downs, support the hypothesis of Mr. Scrope and Mr. Martin, that the gorges themselves were not produced by simple de- nudation, but at least prepared, by antecedent fissures cutting entirely across the Weald: while the appearances of the surface, above described, are so unlike those which would have been produced by rapid diluvial action, as to indicate either a long period of submersion, at no great depth, or very gradual drainage and long-continued decay. The principal branch of the Wey, from its rise near Alton, to Farnham, is nearly straight, in a direction from south-west to north-east; but immediately below Farnham, instead of cutting across the chalk downs, it turns abruptly to the south-east, to join another branch; which likewise runs in a straight line nearly parallel to the former, from its source in the chalk near Selborne, through Kingsley, by Frensham, to Tilford Bridge, where the streams unite: and then taking a: tortuous course, but in a general direction parallel to the Hog’s-back, the river cuts deep Dr. Frrron on the Strata below the Chalk. 151 through the platform of the sands, on the north and west of Godalming, receiving several stream- lets by the way. But there, instead of continuing its direction, it turns suddenly to the north ; and receiving another branch from beyond Cranley, far within the valley of the Wealds, cuts almost directly across both the green-sand and the chalk, and makes its way to the Thames at Weybridge. The mere closing-up of the defile at the mills on the north of Godalming, would convert the whole of Pease-marsh, Frensham, and Thursley commons into a lake :—and, on the other hand, a slight excavation towards the north, through Frensham to the river, would drain the great pond there. The sudden change in the direction of the Wey, near Farnham, is the more remarkable, as the Blackwater, which rises on the northern slope of the chalk downs between Farnham and Alder- shot, about two miles from the angle of the Wey near the west end of the Hog’s-back, runs on the Bagshot sands, towards the north and west, by Frimley, Blackwater, &c., to join the Lodden, not far north of Strathfieldsay, in its course to the Thames near Shiplake. The line of the Wey, therefore, from Alton to Farnham, is nearly a continuation of that of the Blackwater* ; the two streams being separated only by the prominence of the chalk between the Hog’s-back and the foot of Tucksbury Hill. The gorge of the Wey is nearly opposite to that of the Arun, on the south of the Wealden, one branch of which runs almost directly north and south, from a point between Loxwood and Slin- fold, to the sea at Little Hampton; and the structure of the two rivers is very much alike. The Arun rises in the centre of the Wealden tract, whence it runs directly to the sea; as does the Wey from Cranley: but it receives, near Pulborough, at right angles to the main stream, the copious branch (if it be not rather itself the principal stream,) called the Rother; which, having risen near the ponds of Wolmer Forest, very near the sources of the Wey, and followed the curves of the denudation for more than twenty miles, in the trough between the chalk escarpment and the Lower green-sand, is then carried suddenly out of that direction, and withdrawn from the valley of the Weald. (67.) From whatever cause the transverse course of the streams may have originated, the relative composition of the strata was favourable to their retain- ing that direction, when once they had made their way across the chalk and Upper green-sand. For, as the lower beds of the chalk itself, and still more the Gault, are remarkably retentive, while the upper chalk is permeable by water,—the slope of all the strata being outwards, or from the central ridge of the valley, the whole of the waters imbibed by the chalk would be deter- mined outwards, if any pervious channel were opened at its bottom. And if a fissure were cut through the whole series, without great vertical displace- ment, the retentive beds of the chalk-marl and clay, would immediately re- unite, and close it below; while, the chasm in the chalk above remaining open, a permanent drainage outwards would be produced, and the break would be continually enlarged. * The main stream of the Wey is that which runs direct from Wolmer to Shalford. See the map. + It should, however, be kept in view, that the bed of the Blackwater hereabouts is several feet above that of the Wey. 152 Dr. Fitton on the Strata below the Chalk. (68.) The following is a list of some of the fossils obtained from the strata above the Weald clay, within the portions of Kent and Surrey mentioned in the preceding sections (37. to 67.) :— List of Fossils of the Gault and Green-sands, in the 1nrerior or Kenr, and part of Surrey. Ammonites dentatus. Gault. Brick-field near Westerham. F. A lautus. Gault. Same place. F. A splendens. Gault. Bletchingley, Surrey. Mantell. A tuberculatus. Gault. Brick-field near Westerham. F. A ? A fragment of a very large Ammonite (or Hamite?), was found by one of my sons (W. I. F.), among the lowest beds of the green-sand on the south of Brasted in Kent; which, when complete, must have formed a spiral between two and three feet in diameter. The separate convolutions are about nine inches in breadth; and the flutings of the surface, which are simple, are about two inches across the broadest part, and in depth about an inch. The specimen be- longs, not improbably, to one of the large species which occur in the Gault of Yorkshire, (see Phillips). A Four species occur at Boughton quarries.* Ampullaria canaliculata. Gault. Bletchingley, Surrey. Mantel]. Belemnites minimus. Gault. Bletchingley. Mantell. B —. A large species. Boughton quarries. Also at Cold Harbour, near Mont- real Park, Sevenoaks, Kent. F., Cucullea. (Species doubtful.) Lower green-sand. Boughton quarries. F. Dentalium decussatum. Gault. Brick-field near Westerham. F. Exogyra conica. Boughton. F. 18; levigata. Boughton quarries. F. Fistulana. (Species doubtful.) Ditto. F. Gervillia. (Species doubtful.) Boughton. F. Gryphaa sinuata. Boughton. Also near Brasted; West Kent. F. Inoceramus concentricus. Gault. Brick-field near Westerham. F. _— latus. Ina fragment of yellow quartzose chert, loose on the surface, near Brasted, Kent. F. Modiola parallela. Lower green-sand; Near Maidstone. M.C. Mya. (Species doubtful.) Boughton quarries. F. Nautilus elegans. Boughton. F. Nucula pectinata. Gault. Brick-field near Westerham. F. Pecten quinquecostatus. Lowest green-sand. Riverhill. G. Pholadomya. (Species doubtful.) Boughton. F. * All the specimens from Boughton were found in the Lower green-sand: the greater part in the soft grey calcareous rock, full of green particles, called “ Hassock.” Dr. Firron on the Strata below the Chalk. 153 Plagiostoma. A small species. Lowest beds of the green-sand: Riverhill, near Sevenoaks. Mr. Goodhall. Pleurotomaria striata*. Pl. XIV. f.16. Boughton. F. Plicatula pectinoides. Boughton. F. Rostellaria carinata. Gault. Bletchingley. Mantell. Serpula. Boughton. F. Sphera corrugata. Lowest green-sand. ‘Trevereux, near Lympsfield, Surrey. F. Terebratula Gibbsiana. Boughton. F. T———— oblonga. Lower green-sand. Riverhill. G. Thetis major? Boughton. F. Trigonia aleformis. With two or more other species. Boughton. F. Turbinolia Kenigii. Gault. Bletchingley. Mantell. Venus angulata? (Cyprina.) Large, flat. Boughton. F. Wood, Dicotyledonous. Boughton; and near Brasted, West Kent. F. Hyena. Portions of the bones of the extremities of this animal, and fragments of the skull and teeth, both molar and canine, with pieces of Album Gracum, have been found imbedded in brownish sandy loam, at the top of the quarries of Boughton Mount. F. Jguanodon. Distinct remains of this reptile, found by Mr. Binstead in the Lower green-sand at Rockhill, near Maidstone, have been examined and described by Mr. Mantell. See note on (38). HampsHire AND WesTERN Sussex. The south-western portion of the Wealden denudation has been so fully described by Mr. Murchison and Mr. Martin, that I shall refer to their publi- cations already quoted, for an account of it; giving here only some additional facts with which I have been favoured by those two gentlemen: and for a similar reason I shall leave untouched the territory of Mr. Mantell in Western Sussex. (69.) Hampshire —Accumulations of broken chalk flints have been found very extensively, over the surface of the Lower green-sand, on the newroad from Petersfield to Midhurst in West Sussex; at Sheet Hill; and several other places in this part of Hampshire. In the former situation, which is about three miles from the nearest chalk, the detritus covers an uneven surface of the sand, which appears to have been acted upon precisely in the same manner as that * In the list of the fossils of the vicinity of Folkstone (p.131.), this shell has been called a Trochus: but a very fine specimen obtained from Kent, and kindly mentioned to me by Mr. Charles Manning, has since convinced Mr. Sowerby that the true genus is Pleurotomaria. See the de- scriptions of the new species, in the Appendix. VOL. IV.—SECOND SERIES. x 154 Dr. Firron on the Strata below the Chalk. of the chalk itself; the sand being eroded into irregular cavities, sometimes almost tubular, which are now occupied by chalk flints, a great part of them in small fragments, and all of a rusty yellow colour. Equally abundant accu- mulations of these are seen also on the hills of white sand (one of the upper members of the Lower green), at Stedham and Trotton commons, between six and seven miles east of Petersfield ; but in this case the flints are not dis- coloured. This latter place is distant nearly three miles from the nearest point of the chalk, and between nine and ten miles east of that where the chalk escarpments are confluent. In the angle of the chalk west and north- west of Petersfield, particularly in the ascent to Alton by Stoner Hill, such heaps are yet more common. These facts coincide with the observations already mentioned, near Boughton, Dorking, and Wracklesham (38, 56, and 65); so that it would seem as if chalk flint gravel above the Lower green- sand was of general and frequent occurrence all around the denudation. Mr. Murchison, however, adds, that he has still no knowledge of any such debris beyond the limits of that formation, or within the Wealden properly so called. (70.) The stiff and retentive marly beds, at the base of the Downs, sus- taining the water which descends through the chalk, have produced a line of ponds along the bottom of the escarpment of the South Downs ;—a result pre- cisely analogous to the breaking-out of the springs above the mar], at Lydden Spout, upon the coast (8.), and all along the base of the Downs on the north. (71.) One of the chief characteristics of the tract near Petersfield, consists in the great relative extent and prominence of the Upper green-sand; which runs out beyond the foot of the chalk escarpment, like a step or terrace, throughout the tract from Farnham, by Selborne and Petersfield, to the south of Petworth, and affords some of the best sections anywhere to be found, except perhaps in the Isle of Wight. Though in the parishes of Buriton, Harting, &c., there is an insensible passage from the grey chalk and chalk marl, into the Upper green-sand, still the whole of the terraces (there at least two miles broad) are exclusively composed of what is called in the country Malm-rock*. 'The grey or lower chalk of this portion of the South Downs is charged with the Inoceramus mytilordes, I. Cuviert, I. Brongniarti, and two species of small plicated Terebratula, and does not contain any of the cha- racteristic malm-rock fossils enumerated in Mr. Murchison’s memoir; nor does the malm-rock contain, so far as his observation goes, a single specimen of the genera Inoceramus and Terebratula, so abundant in the overlying * The Malm-land, which is remarkable for the fine crops of corn produced upon it, is, pro- perly, the soil over the lowest beds of marly chalk, which are carried out upon the tops of the projecting terraces; the term, ‘‘ Malm-rock,” being confined to the stony beds beneath. Dr. Frrron on the Strata below the Chalk. 155 chalk : a fact which is the more deserving of attention, as several other genera and species are found both in the Upper green-sand and the Lower chalk*. (72.) Vicinity of Pulborough.—I am indebted to Mr. Martin for the section (Plate X a. No. 5.) across the Wealden district, from Duncton Beacon on the South Downs, through Petworth, to Cranley; and I have, from my own ob- servations, continued it in the same direction to the North Downs. This section shows, what Mr. Martin’s recent observations have fully confirmed, that the subdivisions of the sands below the chalk, in the north-west of Sussex, correspond with those above described, in the neighbourhood of Folkstone ; and that a similar valley distinctly marks, in both cases, the place of the middle greener and retentive sands, (24.). I have had myself also an opportunity of seeing, with Mr. Martin, a section parallel to that of Plate X a., in which this structure is very clearly displayed, on a line about half a mile west of Pul- borough, passing through the heights of Park-hill farm and Pethenden (with the valley of the middle sands between), to a detached summit within the Weald-clay, called Pickhurst Hill; (See Plate X b. fig. 2.). Fuller’s-earth like that of Nutfield, appears at Fittleworth Church, near Pulborough. Besides the mass of this intermediate group, a detached stratum, about 40 feet in thickness, of dark-coloured, greenish grey, retentive sand, including much pyritous matter, occurs above it, with some feet of ferruginous and yellowish sand between ;—-a subordinate bed, in fact, within the upper ferruginous mass of the sand: and this ought to be held in view, as in some cases it might be mistaken for the Gault. It is very conspicuous on the ascent of the London road, from the flats on the south, to the church at Pulborough; and can be traced thence, almost continuously, for some miles both to the east and west. No fossils have been found in this stratum, except some impressions of what may be the branches of fuci. A bed of dark hue, with the same characters, seems to occupy a corresponding place in the series near Reigate: See note f on (52.). (73.) This country has been the scene of several upheavings and derange- ments of the strata, analogous to those above mentioned in West Kent (41. to 43.), but much more complex and extensive. Some of these have been described in Mr. Martin’s work already referred to; and of others, more re- cently observed by that gentleman, I hope he will himself soon publish a description}. * See Mantell’s “ Tabular Arrangement of the Organic Remains of Sussex”—Geol. Trans. 2nd Series, vol. ill. p. 210. Terebratule are there mentioned among the genera common to both deposits. t The forces by which such derangements may have been effected, appear to be still in action in this part of England. In the spring of the present year, 1834, distinct shocks of an earthquake were felt throughout a tract, of which Chichester seems to have been the principal point. At Pulborough, they were of such force as to ring the bells at the parsonage. An account of the phenomena, is, I believe, in preparation, by some members of the Philosophical Institution at Chichester. x 2 156 Dr. Firron on the Strata below the Chalk. (74.) The junction of the sands and clay,at Stopham brick-yard, on the west of Harwood’s Green, near Pulborough, affords the only indications that have come to my knowledge, of any interruption or disturbance between the de- position of the upper part of the Weald clay, and of the incumbent Lower green-sand. Thesurface of the clay at the place in question is hollowed into irregular roundish cavities, at the bottom of which portions of green-sand were found, including several of the characteristic fossils of that formation ; while the clay, immediately below, is equally characterized by the presence of Cypris. At the junction, the clay was mixed with sand; and specimens of Panopea plicata were found even two or three feet within nearly pure clay, along with ferru- ginous concretions, containing fossils of the Wealden, impressions of Cyclas, Cypris, and remains of fishes: and this mixture was observable to the depth of several feet ;—so that both the sand and clay must have been at the time of mixture in a state of sottness ; or the sand must have been introduced over a surface of argillaceous mud, before it had consolidated. When | had the pleasure of examining the place, with Mr. Martin, the circumstances were unfavourable to observation: and, as the junction of the two formations here, is on the slope of a hill, it might have been doubted whether the appearances could not be explained by the effects of subsidence producing intermixture, during very rainy weather, or under water, before any of the strata had emerged. Mr. Martin, however, who had seen the place when the phenomena were better exhibited, is of opinion that this explanation of them would not have sufficed. In this brick-yard, the loamy sand found near the junction is used alone for making the bricks; sand being required in the manufacture, only for sprinkling the moulds. (75.) List of Fossils from the Beds below the Chalk, in part of Hampsnire and Western Sussex. [ Upper Green-sand. | The following List of Fossils from the Upper green-sand in the vicinity of Petersfield, in addition to those mentioned in Mr. Murchison’s paper on that district, (Geol. Trans. 2nd Series, vol. ii. p. 99.) I owe to the kindness of Mrs. Murchison, in whose collection the specimens are placed. Ammonites catillus. Fishes. Scales and vertebre. A—— splendens. Gryphea columba. Arca carinata. G vesiculosa. Avicula grypheoides. (See Pl. XI. f. 3.) G sinuata. Cucullea. Much compressed. Nautilus elegans ?? Much compressed. Echino-spatangus. (Three new species.) Pecten asper. ~ Dr. Firron on the Strata below the Chalk. | 15 Pecten Beaver. Solarium granulatum. Mantell. P nitidus. S or Trochus. Another species. P orbicularis. Thetis major. P quinquecostatus. Besides one or Vegetable impressions. Like those of the two other species, indistinct. upper chalk near Lewes. Mantell, Plicatula inflata. | CE Pe RO Ce [Lower Green-sand. | Ammonites dentatus. Stopham brick-yard, West of Pulborough, Sussex ; in a mass of phosphate of lime. his, with the other fossils from the same place, was found by Mr. Martin covered by green-sand, in an excavation at the top of the Weald clay. Martin MSS. A————.. (Near to Nuifieldiensis, but a distinct species.) Lowest member of the sands near Pulborough: Martin. A——_——. (Impressions of one or two other species.) Stopham brick-yard: Martin MSS. One of these is in a roundish mass of phosphate of lime, precisely like spe- cimens found near Copt Point, Kent: the outer surface is whitish, and is eroded in small tortuous grooves, as if eaten by worms: the interior brown. Auricula (new species). Martin, cbid. Avicula? Martin, zbid. Cardium? (New species; delicately striated.) Stopham brick-yard : Martin MSS, Coprolite. Stopham brick-yard : Martin MSS. Corbula gigantea. Bowyer’s Common: Mrs. Murchison. C. striatula. Bowyer’s Common, near Petersfield: Mrs. Murchison. Parham : Mantell, and Martin. Cc (new). Near Pulborough: Martin, p. 32. Crustacea. “‘ At Bognor Common, in Fittleworth parish, there is a vein of friable “‘ oreen-stone, rich in Pectens, Trigonia, and the remains of a crustaceous fossil “like a shrimp.”” Martin, p. 34, note. Cucullea decussata. Parham: Mantell, and Martin. C glabra? Bowyer’s Common: Mrs. Murchison. C (Another species—or two?) Stopham brick-yard: Martin MSS. Cyprina angulata. (Venus, Min. Con.) Stopham: Martin MSS. Cytherea parva. (Venus, Min. Con.) Parham: Mantell. Bowyer’s Common, and Lyss near Petersfield: Mrs. Murchison. Upper ferruginous member of the Lower green-sand, Pulborough Mount: Martin MSS, Gervillia acuta. Parham: Mantell. G aviculoides. Parham Park: In concreted masses of fine-grained ferruginous sand, with several other species mentioned below; all casts: Martin. Also Bowyer’s Common: Mrs. Murchison. G solenoides. Parham: Mantell. G (Another species, probably new.) Upper ferruginous member of the sands: Martin. Inoceramus gryphaoides. Lowest group of lower green-sand: Martin, p. 33. 158 Dr. Firron on the Strata below the Chalk. Lima semisulcata. Plate XI. fig. 10. Pulborough: Martin. Lucina? Bowyer’s Common: Mrs. Murchison. L (Perhaps two species.) Lowest member of the sands; near Pulborough: Martin. Modiol. lis. Ae eqalts Parham: Mantell. M. bipartita. M— imbricata. Upper ferruginous sands: Mantell, and Martin. M— bella. Plate XI. fig. 9. M.- (A new species.) Near Pulborough: Martin, p. 32. Mya mandibula, Wowest member of the sands. Pulborough: Martin. M-— plicata. (See Panopeea plicata). M—. (Two species not figured.) Martin, p. 33. Lowest group of lower green- sand. Mytilus edentulus? Martin, p. 32. M— lanceolatus. Parham: Mantell. Natica. Parham: Parkinson; Organic Remains, vol. 3. Pl. 6. fig.2. Lyss near Petersfield: Mrs. Murchison. Nautilus. Near Pulborough: Martin, p. 31. Nucula impressa. Parham: Mantell. Lowest member of the sands; Pulborough : Martin. N— antiquata. Upper ferruginous member of the Lower green-sand; Pulborough Mount: Martin. Orbicula. (Not figured.) In sand rock: lowest member of the sands; Pulborough and Stopham: Martin. Panopea plicata. Lower member of the sands; Parham Park, and Stopham brick_ yard: Martin MSS. Patella. Parham: Mantell. Pecten obliquus. Parham: Mantell, and Martin. Ji orbicularis. Pulborough: Martin. Parham: Mantell. yd quadricostatus. Parham: Mantell. Je (A new species.) Martin. Pholadomya. Wowest member of the sand near Pulborough : Martin, p. 32. and MSS. Pinna tetragona. In sand-rock ; lowest member of the sands: Martin. P (A cast.) Stopham brick-yard: Martin. Rostellaria calcarata. Parham: Mantell. R— Parkinsonii. Parham: Mantell. Upper member of the sands ; Pulborough Mount: Martin. R———. (Very like Pes Pelicani.) Parham: Mantell. helene emialis: j Parham : Mantell, and Martin. T: inequalis. ‘ p. ? (A species not figured.) Lowest member of the sands, near Pulborough : Martin. Terebratula lata. 1 oT, Parham : Mantell. | , Dr. Firron on the Strata below the Chalk. 159 Terebratula nuciformis. Upper member of the sands; Pulborough Mount : Martin. ye depressa. Upper ferruginous member of the Lower green-sand ; Pulbo- rough Mount: Martin MSS. [T—__—.. (Another species—uncertain.) Same place : Martin. Thetis major. Lowest member of the sands; Pulborough: Martin. T: minor. Bowyer’s Common, and Lyss, near Petersfield: Mrs. Murchison. Parham: Mantell. Upper member of the sands; Pulborough Mount: Martin. T—— (new). -Stopham brick-yard. Martin MSS. Trigonia alaformis. eee Common: Mrs. Murchison. Parham: Mantell. Stop- T—— clavellata? | ham: Martin. T—— dedalea. Parham: Mantell. ft spinosa. Pulborough: Martin, p. 33. Turbo rotundatus. Parham: Martin MSS. T—. (Another species.) Near Pulborough: Martin, p. 31. Turritella granulata. Parham, and Pulborough: Martin MSS. T (Another species.) Near Pulborough: Martin MSS. Venus angulata. See Cyprina. : — } Patham Mantell. V—- ovalis. V— parva. See Cytherea parva. V—. (Casts of two other species.) Stopham: Martin MSS. Vermicularia concava. Parham-park, Parkmount-lane near Pulborough, Chiltington- common. Martin, pp. 33 and 34. Tor WeEaLven. (76.) In adopting this general denomination, proposed by Mr. Martin, for the formations below the green-sand, in the Wealds of Kent, Surrey, and Sussex, I have extended its acceptation to the Purbeck strata also, which do not occur within those counties ; because the whole group abounds in fossils of the same character. And though the Purbeck strata consist principally of limestone, which has many indications of lacustrine origin, they include, like the upper members of the Wealden, distinct alternations of marine fossils with those of freshwater :—one very thick bed especially, which consists al- most entirely of oysters,* showing that the sea must have had access to the waters from which they were deposited. Mr. Martin has ascertained that the Wealden strata above the Purbeck, consist, throughout, of alternations of sand, sand-rock, and grit, with clay and marl; so that the separation of the Weald-clay from the Hastings sands, is in a great measure arbitrary. But as in the only tracts where this group has yet been observed, the sands rise above the valley of the clay, into a very prominent ridge, which forms a striking fea- * Webster: Geol. Trans., 2nd Series, Vol. IL., p. 40. 160 Dr. Firron on the Strata below the Chalk. ture of the surface, this subdivision is to a certain extent natural, and may be retained with advantage. (77.) Valley of the Wealds.—The‘beds of sand, sand-rock, and limestone subordinate to the Weald clay, have been traced by Mr. Martin throughout the tract represented in his map of Western Sussex, and I refer to his memoir for an account of them: their place is indicated in the Section, Pl. X. a. fig. 5. L have myself observed beds of the same description,—no doubt con- tinuous with those described by Mr. Martin, though I have not traced their continuity, on the opposite side of the Wealden and of the forest ridge, about Ewhurst, and on the east of that village*. And in the course of the valley eastward, through Surrey and Kent, distinct and almost continuous ridges, apparently produced by the greater durability and prominence of similar strata, are observable from the escarpment of the sands, and are in part ex- pressed in the Ordnance Maps. Two, if not three lines of these subordinate strata cross the road which descends from the escarpment of the sands through Ewhurst. 1. The first is at the foot of a height, which runs from the south of Coneyhurst Farm, through Woodland; the beds consisting of limestone, (Sussex marble) full of large Paludinz and Cypris. A group, possibly a continuation of this, occurs in Mr. Turner’s grounds, north of Forest Green, at Atherley, about two miles east of Woodland, below Leith-hill Place; but there the stone is greenish micaceous grit, in three contiguous courses, each about 12 inches thick, containing very large Paludinz, Uniones, and stemlike concre- tions, where the stone adjoins the whitish sand, on which it rests. Above Henhouse Farm also, about a mile and a half east of Atherley, a range of high ground indicates the presence of firm bands of stone; and grit is found there, which includes similar Uniones, and a few Paludinz. 2. A second band, composed of ironshot sand, over variegated reddish brown clay, crosses the road, at the church of Ewhurst, passing thence eastward through Lyefield Farm. The stone-pits of Forest Green seem to be on this line, but they consist of beds of grit including Uniones and Cypris, above yellowish sand, reddish clay, and concretional sandstone, with casts of Uniones. 3. At Bowles’s Farm, on the east of Cranley, is a bed of very compact sand-stone, apparently lower in the series than those above mentioned: and the roads hereabouts are repaired with grit from Newhouse, between Cranley and Ewhurst. Stone is also found nearly on the same line east- ward, at Redford and Standling; and again on the south of Capel (on the road from Dorking, about a furlong north of the 30th mile-stone), is a prominent ridge, with a course of sand, in beds from 2 to 6 inches thick, in light-coloured clay. The height last mentioned, near Capel, may probably be the continuation of a ridge which, on the Ordnance Map, begins about 34 miles to the east of that place, passing from Stand-hill, through Norwood and Horse-hill; and which (being resumed on the east of the Mole), forms a range nearly parallel to the escarpment of the Lower green-sand,—by Lady-farm, about two miles south of Earlswood-common on the road from Reigate to Brighton, Outwood-common, Lostland, south of Gayhouse-farm, and thence, through Hook-stile, to the stream south of Comfort’s-Place farm, and Moat farm. On the east of the place last mentioned, the ridges between the Lower green- * See the eastern part of the Section, fig. 5. Dr. Fitton on the Strata below the Chalk. 161 sand and the Hastings sand, are not so well defined; but on the south of Boughton, a series of heights extends from Marden to the east of Staplehurst. (78.) Coast of Kent. There is, strictly speaking, no section of the Weald clay and the upper part of the Hasting sands on the coast of Kent; the line of heights which, at some very remote period, may have been sea-cliffs washed by the English Channel, being now covered with vegetation, and separated from the sea by the wide tract of Romney Marshes. Having, myself, some years ago, observed indications of sand and stone, in the Weald valley near the coast where it is difficult to find good sections exposed, my friend the Rey. G. E. Smith was good enough, at my request, to examine that part of the coun- try; and from his notes I learn that the greater part of the series there must consist of sand and sandy clay,—the blue fissile clay, which occurs in the upper part of it, not recurring, or not having been detected, farther down. The first rise of the clay from beneath the green-sands, is represented in the view Plate VIII.; and the general section of the coast between Folkstone and Beachy Head, (Plate X. a. No. 6.) includes the strata on the west of Hythe. The shore beneath that town, which is sometimes laid bare, when the sea carries away the shingles, during the prevalence of easterly winds, consists of soft bluish clay, which has the characters of river mud, and differs much from the uniform slaty clay of the Wealds. But the latter has been cut through in sinking wells above the main street of Hythe, which, in some instances, have gone to the depth of 75 feet entirely in clay. In one of these wells, the succession of beds was thus ;—beginning at a point about 60 feet beneath the bottom of the Lower green-sand. Upper Part of the Weald-Clay at Hythe. Ft In. oe ot ROR OAR Ge rn atest stainleieto vara 2 6 RR RCOMNT CLAY Sates sas oe ew oe vee osnensetnes scenes ne 6 to 7 0 3. Greenish sandy clay, in thin bands, alternately of dark and lighter hues.. 5 to 6 0 4. Blue, uniform, slaty clay, containing Cypris about a foot from the top.. about 5 0 5. A band, composed of argillaceous iron ore, abounding in Paludina elon- . 20 PU eS ie so ee een ne 2 18 0 6. Blue clay continued. Here a boring was made to a depth of about 20 feet : aUBtantaisUncinverie ci Magee shs Pe PLT Mifesal 20 0 hotahs 0 ote ts. 38 0 Blue clay with Cypris occurs also, according to the Rev. G. E. Smith, immediately below the green-sand, at Aldington Corner ; but nothing like it, he informs me, in the succeeding parts of the section towards the south. A bed of limestone, with Paludinz (‘ Sussex marble”) occurs at Hurst}, beneath Court-at-Street, and seems to be continued in the clay which passes from that place round the base of Aldington Knoll; and a similar stone is found, in a corresponding situation in the cypriferous clay, at Daniell’s Water on the south-west, Stanford Bridge, on the *In descending from the sands at Linton, south of Boughton, and in many other places, the top of the Wealden is seen to consist of very red clay. ‘| The term Hurst is of such frequent occurrence in the names of places in Kent, Surrey, and Sussex, that the Ordnance Maps alone afford a List of about 120 such names. Having sent this List to the Rev. Joseph Hunter, late of Bath, that gentleman has favoured me with some obser- VOk. IV.—SECOND SERIES. Y 162 Dr. Firron on the Strata below the Chalk. west of Ashford, and near Bethersden, about 22 miles south of Stanford Bridge. A continuous range of slightly elevated ground, extending from Lovelace near Bethersden towards Shadoxhurst (in a direction parallel to that of the other ridges of this country, and to the range of the chalk escarpment), may also indicate the existence of some stratum of greater firmness than the clay. Mr. Smith mentions two subordinate courses of sand, with sand-rock, sandy clay and loam, as occurring in the lower tract, or valley of the Weald, between Aldington Corner and the cliffs of sand and grit on the north of Rye. (1.) The first of these runs from near Bilsington, through Orleston ; with which line a range in the interior seems, from the map, to be continuous, for about four miles more towards the north-west,—through Woodchurch Beacon and Redbrook Street. It seems to be parallel to the ridge above mentioned between Bethersden and Shadoxhurst; and sections of the strata are disclosed at Bilsington Priory; on the roads from Bilsington Cross to High-house; from Ruckinge to Ham Street, and from Ham Street to Orleston; and perhaps near Warehorn Leaton. (%.) The second course, which consists of red clay with sand and sand-rock, begins at Brookarm, on the verge of the marshes, and passes through Bench-hill. On the south of this last-mentioned range, sand and sandy clay appear to abound: concretional beds of hard vations of so much interest, that, but for the immediate object of these pages, I should willingly have inserted them in full. ‘“¢ The word,” Mr. Hunter states, “does not occur in Lye’s Saxon Dictionary; but I observe “ that the modern Lexicographers speak of a Saxon word, hypyz, as synonymous with sy sys and as TE) it seems, occurs in low Latin, for ‘wood’. Wachter explains Horst, Germ, ‘locus * “nemorosus et pascuus’; and refers it to dpos, mons. Kilian has Horscht, Teut. ‘ virgultum; ** «sylva humiles tantiim frutices proferens.’ “In England, Hurst appears to signify a small wood; but, in’ Scotland, a barren height or ‘““ eminence, and sometimes a shallow in a river. I do not find the word,” Mr. Hunter continues, “in any of the provincial glossaries ; and yet I think it is not quite out of use, in its uncompounded ‘« state, to denote a Wood, generally; but I much doubt whether any specific difference can be dis- ‘* covered between the sense of this word and that of many other words, in a language which is ‘particularly rich in terms which designate woods, or woody places: grove, thicket, copse, “* brake, &c. “Tf Drayton’s authority (Polyolbion, viii. 2.) were not thought sufficient to prove that in ** England the word was formerly used to signify a Wood, the combinations in which it occurs in the ** names of innumerable places, dispersed all over the southern part of the island (1. e. south of the ‘‘ Tweed), would be sufficient to prove it. There is Oak-hurst, Ake-hurst (a varied form of Oke- *‘ hurst); Elm-hurst, everywhere ; En-hurst, Hasel-hurst, Ash-hurst, Ashen-hurst, Maple-hurst, “ Nut-hurst, Beam-hurst (Staffordshire), Brere-hurst, Box-hurst; besides many Hursts without * any prefix,—of which Hurst-Monceawx is one ; Monceaux being an addition made after the Con- * quest, from the name of some Norman Lord. ‘“* So many instances in which the names of trees are united with this word, would, I think, of ‘* themselves be sufficient to prove that it was really in use in England, in the sense of ‘wood’; and “it may be added, that it lies deep in the language,—the woods so designated being older than ** the towns’ which have risen near them, and those towns of Saxon foundation. “‘ Again, there are other instances in which the adjunct is congruous with this idea of Hurst; such “as Hawk-hurst, Crow-hurst, Broad-hurst, Buck-hurst, Brocklehurst (Brock-hole-hurst),—the wood ‘‘ where the badger (brock) made his holes. So also Brock-hurst, Park-hurst, Coney-hurst, &c. &c. “Tt must, however, be admitted, that there are many names of places, into the composition of ‘which the word Hurst enters, of which it is extremely difficult to trace the origin; and when “ those for which we can account are taken out of the list, it is hard to form even a conjecture con- ** cerning those which remain. In this respect, however, the compounds of Hurst are but in the “‘ same predicament with the prefixes to -ton, -ham, -field, -by, and many of the local terminals; ‘““and probably they are, in many instances, the names of early Saxon proprietors, detorted “ from their original forms. Some, however, more skilful etymologist, or one better acquainted ‘‘ with the language of our ancestors of the 6th and 7th centuries, when probably these names first “ became fixed, might explain :—Shadocks-hurst, Cog-hurst, Bub-hurst, Tile-hurst, Sissing-hurst, “ Capen-hurst, Desron hurst, &c. &c.” Dr. Firron on the Strata below the Chalk. 163 grit, with Paludinee and Cypris, occurring in the sands about Stone and Knock-house; and still more conspicuously in the range of heights further south, which extends from Boons-hill to the cliffs below Playden, not far from Rye. (79.) Hastings Sands.—Mr. Webster has described and given a drawing of the cliffs on the east of Hastings, in a preceding volume of these 'Trans- actions* ; and a general section of the coast between the chalk downs of Kent and Sussex will be found in the annexed Plate, X.a, No.6. I shall not, therefore, here detail the stratification of this portion of the Wealden, espe- cially as lists of the strata will be given hereafter, in describing the coast of the Isle of Wight and of Dorsetshire ; but shall confine myself to an account of the cliffs, on the west of those represented in Mr. Webster’s Sectional View,—which were uncovered to a great extent during the progress of the buildings and improvements recently carried on between Hastings and St. Leonard’s f. (80.) Shore on the West of Hastings.—The anticlinal line of the ridge consisting of the Hastings-sands runs inland, from the shore towards a point about 60° west of north; beginning on the east of Hastings, about Lee Ness Point, and passing through Battle, and thence along a series of ridges, to its greatest height at Crowborough Beacon, on the south-west of Tonbridge Wells. The strike, on the west of Hastings, is not parallel to the anticlinal ridge, but oblique to it at an angle of about 44°, the strata running nearly from east to west, and dipping generally towards the south. The direction of the coast line for a short distance, at St. Leonard’s, co- incides with the strike, but from Hastings to the entrance of that place, makes an angle with it of about 10°,—the line of the shore running from about 14° north of east, towards the south of west; and on the west of St. Leonard’s, the coast turns a little towards the north of west, and again makes a small angle with the strike. In going along the shore, therefore, from Hastings towards Bulverhithe, the strata first appear to be inclined * Geological Transactions, 2nd Series, Vol. II. p. 31, &c. For additional information on the Wealden tracts in general, the reader is referred to Mr. Mantell’s publications; Mr. Lyell’s “ Prin- “ciples of Geology,” (3rd edition), Vol. IV. chap. 21 and 23, pp.165—191, 219, &c.; and to “ A Sketch of the Geology of Hastings,” 12mo, 1832, by the author of the present paper. + This general section is on the same scale of relative height and horizontal distance, as all the others in Plate X. a.; but asa correct estimate of the elevation is, in this case, important to theory, the heights are given in true proportion, on the line immediately below, as has been done by Mr. Lyell, in one of his chapters on the structure of the Wealden. t The Sections following in the text, from (80.) to (90.), formed the substance of a Notice read before the Geological Society, in November, 1833 (Proceedings, vol. ii. p. 1.); and are here introduced by the permission of the President and Council. y 2 164 Dr. Firton on the Strata below the Chalk. to the south of west; then to become horizontal; and beyond St. Leo- nard’s, to rise a little from the sea,—the same beds recurring there in a re- versed order. The Section, Plate X. b, fig. 2, which is on a much larger scale than Plate X. a, No. 5, represents the cliffs here referred to, and will illustrate the structure above described. (81.) The top of the great stratum of white and nearly pure sand, which forms the cliff under the castle at Hastings, comes down to the shore at the White Rock, and disappears under the sea on the west of it. A stratum which has many of the same characters, and seems to be a continuation of that of Hastings, rises at the bottom of the cliff, about 350 paces west of the church at St. Leonard’s ; all the beds in the intermediate space being con- sequently higher in the series. There is still some obscurity as to their rela- tions, from the effects of disturbance ; and some points are concealed : but the following list gives an approach to the order of their succession, descending,— with an estimate of the relative thickness of the groups, and the places in which they are found. Supposed Groups of Strata on the Shore between Hastings and Galley Hill. Estimated Thickness. No. Feet. Feet. I, Sand, and sand-rock, in large proportion ; with clay, in alternate courses .... 15@ a. Heights above and within the entrance of St. Leonard’s, from Hastings ... 50 | b. From the archway at entrance of St. Leonard’s to Warriors’ Gate...... 50 c. Space corresponding to the vacancy at Warriors’ Gate (thickness it Eo mated fromthe noxizontal distance): .c\ctsc sees vos + osis'e e eeieae ett Dl Sand-rock, clay, ane Pmller’s-eartlis/c\cte's clots hots ete clea « ate! ciel ete etenels about 75 a. Heights between Warriors’ Gate and the White Rock ; nearly thus, in detail ; Me aOLAb YP ClAY petewlelc.-f-rere 8 feet. 7. Dark sand-rock, with lignite.. 2 2, Sand and sand-rock. .20 8. Alternations of sand-rock, g. Fuller’s-earth ...... 2 sand, and sandy clay, about } Aim and=rockspryese ier 4 W752 o-Pullers-earthe yf. 2 9. Light blue clay, ae > Gynsand-Tock reer ae 12 downwards into (III.).... III. Sand-rock, alternating with grit, slaty clay, and clay iron-ore, and including one or more layers of Endogenites erosa, with numerous other fossils... . between 50 and 60 a. Ledge under the White Rock. b. Strata in the cliff behind the new Brewery on the east of the White Rock. Endogenites erosa in great numbers. The connexion of a. and b. with the light blue clay, (II 9.) was not dis- closed: but the whole group seems to be the same with III. e. c. Ledge of rocks under the “* Marina” at St. Leonard’s. d. Beds around St. Leonard’s church, and in the cliff on the west of it. At these places the grit and conglomerate include remains like those of Til- gate Forest. Dr. Firron on the Strata below the Chalk. 165 IV. White sand, and soft sand-rock, including thin flakes of light grey clay, and some PGnenansiO! MMe S) oi cast wa et- Seca alerd ets ani oietls shai als Din wlee ws\\s upwards of 80 a. Cliff under the castle, Hastings. b. Shore below, and on the east of the White Rock. c. Bottom of the cliff, near the Sussex Hotel, west of St. Leonard’s. cs Or V. Brownish sandy clay, with much lignite, immediately beneath IV............. a. Under the Castle-cliff, behind Pelham-place, Hastings. VI. Yellowish and ferruginous sand, and sand-rock, including nodules of pyrites, and grains of reddish (pisolitic) oxide of iron............-.0.00004- } a. Shore, about low-water mark, beneath the town of Hastings. b. Shore between St. Leonard’s and the Martello Tower, No. 39. VII. Variegated clay and sand, of various shades of red inclining to purple, and Vipht Greenish reverent cso: - scien cee ee ee aden ee ne i a. Heights west of Bopeep. b. Shore from Bulverhithe to Galley Hill. ec. Similar beds, with granular oxide of iron, are found on the east of Hastings, in the bay of the Lover’s Seat, &c. (82.) The following details respecting the strata just enumerated may be worth preserving, as the surface of the cliffs will probably soon be concealed. I. a.—The highest members of this series are partially exposed on the north of the back street, near the eastern buildings of the Marina and the archway at the entrance of St. Leonard’s ; from whence down to the shore is a series of strata, which are horizontal on the line of the strike, but rise in reality towards the north, at an angle between 12° and 15°. The uppermost beds con- sist of soft grey sand-rock, with some intermixture of clay, and form a total thickness_of about 66 feet above the road. The lower members are visible in the back street, and on the west of the houses are seen to rise towards the west. The horizontal portion occupies about 150 paces from west to east, and after that space, in consequence of a change in the direction of the shore towards Hastings, a rise towards the east begins to be apparent. The strata which connect this group with the beds of clay around the church hereafter mentioned (III. d.), have been carried away or are concealed. I. b.—The group next below is partially seen on the shore between St. Leonard’s and the White Rock. Between the archway and the vacancy in the range of heights, which is called Warriors’ Gate, is a low cliff about 250 paces in length, and about 30 feet high, which has been cut away to admit of the erection of houses. It consists of sand-rock, alternating with clay or marl ; the beds of which rise and disappear in succession, corresponding altogether to a total thickness of about 50 feet. I. c.—The opening at Warriors’ Gate occupies a horizontal space of about 300 paces, and within it, on the north, is a bank of sand-rock like the strata last described. On the east of this opening, a low range of grass-covered cliffs, from 40 to about 60 feet in height, extends without interruption to the beginning of the road over the projecting masses at the White Rock*; and two * The storms during the high tides of 1833 and 1834, had so shattered the mass which bore the name of the White Rock, that very few of the interesting appearances represented and described by Mr. Webster now remain, the face of the rocks which aftorded them having been either con- cealed or carried away. The destruction had been such in April 1834, that the town of Hastings, goatee concealed by the prominence of the shore, was then visible from the entrance of St. eonard’s. 166 Dr. Fitton on the Strata below the Chalk. remarkable beds of greenish Fuller’s-earth, in general about two feet thick, but in some places much thicker, separated by about four feet of sand-rock, rise upon the road-side, and are continued steadily in the face of the cliff, nearly to the White Rock, being, near that place, more than 30 feet above the bluish clay (II. 9.) at the bottom. The base of the cliffs here is about 20 feet above a floor of rocks which is bare at low water, and consists of yellowish, firmly concreted sand, or sand-rock, abounding in granular (pisolitic) reddish oxide of iron*. This granulated rock forms, hereabouts, a ledge beneath high-water mark, dipping to the west of south, at an angle of about 11°, with a strike towards a point about 6° or 7° south of east. II.—About 120 paces west of White Rock, where the road formerly began to rise over that prominence, the cliff behind the new houses, about 40 feet high, consists of a large proportion of sand and sand-rock, with alternations of clay; and in some places contains so much lignite, in the form of indistinct fragments of stems and portions of branches, as to have a dark brown or blackish hue. A bed of light bluish clay (II. 9.) forms the lowest part of this cliff, and seems to be continued downwards ; it probably corresponds to the beginning of the series of beds of clay &c., (III. c.) near the church of St. Leonard’s. On the shore at low water, about 150 paces west of the place last mentioned, is a group of beds which are curved, so that their dip is divergent, those on the east dipping towards the south, at an angle of about 10°; they consist of sand-rock, and may possibly be continuous with the sloping bed at the White Rock, shown in the section, and inferior to the bluish clay of II. 9. Other ap- pearances indicate that this has been the scene of some derangement, so that the relations of the beds, above described, to those under the White Rock and on the west of it, are still doubtful: the whole series, however, is nearly conformable, and almost continuous with the rest of the strata _ towards St. Leonard’s. On the east and south of the nook, in which is the light bluish clay, II. 9. a bed of brownish sand-rock about 10 feet thick, immediately adjoins the road, dipping to the south of west, at a much more rapid inclination (about 18°) than that of the adjacent strata. This bed, neverthe- less, may be a continuation of those which form the curve represented above; and its present position may have been the result either of subsidence, which has caused it to fall away from the apparently continuous mass of strata within it on the north, or of some more extensive derange- ment of the coast at this place. III. a— White Rock Ledge. —The great ledge visible upon the shore at low water, to the solidity of which the prominence of the White Rock (so long as it remained) was to be ascribed, rises beneath the sea, about 200 paces to the east of the rock, and seems to be continued for a consider- able distance in that direction. A series of conformable strata of sand-rock, concretional grit, and slaty clay, here occupies the whole space between high- and low-water mark, for more than 100 * This stratum I did not see in these cliffs: but granular oxide of iron abounds in those on the east of Hastings, and seems to be very generally diffused in a lower part of the series. The grains which I have here called Pisolitic, seem to have existed originally in the form of iron pyrites ;—of which substance globules of various sizes from that of pistol bullets downwards, are still found on the sand-rock at St. Leonard’s. The origin of the ore of iron to which the name of Pisolitic has been applied, is ascribed by Haidinger to the decomposition of pyrites.—Trans- lation of Mohs’ Mineralogy, vol. il. p. 412. Dr. Firron on the Strata below the Chalk. 167 paces; with a strike to about 20° east of south, and dip to the west of south: and this remarkable _ group contains in some places pisolitic grains of reddish oxide of iron, disseminated in yellow sand-rock, like that which is found in the strata beneath. III. b.—The beds in the upper part of the cliff behind the Brewery are a continuation of part of the group upon the shore (III. a.), and, like it, contain great numbers of the singular fossil which has been called Endogenites erosa. They are probably the same with those of III. c. which rise on the shore under the Marina at St. Leonard’s, of which an extensive section was exposed in excavating the site of the church; and both groups are interesting, for their apparent identity with the Tilgate strata, which have furnished to Mr. Mantell an almost inexhaustible store of extraordinary fossil remains. Beds of the Group (III. b.) in the Cliff on the North-east of the White Rock. Ft. In, Ft. In. 1. Earthy brown sand-rock, about... .......- 2.6. see eee eee eee eee eee ee 2. A group, about 10 feet in average thickness, composed as below. a. Sand in thin courses, alternating with clay, which includes Cyclades. ] The sand passes into grit, and in some instances also abounds in Cyclas media in the state of pulverulent carbonate of lime. From the different hue of the sand and clay, the cross fracture is perceptibly | striped in very thin layers; and in the darker beds the surfaces of the f clay are often dotted with white specks, the sections of very small cylin- drical cavities, now filled with very fine sand or clay, which seem to have passed through several of the adjacent folia, vertically or obliquely 6. Thin courses of subcalcareous grit, alternating with bands of clay. The grit is in small concretional masses, often not more than half an inch in thickness, which thin off to an edge. On the surfaces adjoining the lay are very mumerous Cyclades 0.220002. SP J y. Flat, nodular masses of argillaceous iron ore, containing Cypris. In the fallen debris are fragments, apparently from this place, which contain |: ) also clusters of Paludina elongata in great numbers .............. 5. Soft argillaceous sand-rock, alternating with thin layers of darker clay, é and including some portions of iron ore...........-......4.. ae 2) 6 e. Alternate layers of grey sandy clay, and yellowish ferruginous sand-rock, passing into grit, and including the remains of Endogenites erosa. } This and the succeeding stratum very much resemble (b.) above .... as in (6.). This bed contains Paludina fluviorum, and Cyclas media, in g. Light greenish grey sand, passing into grit, and alternating with clay, | 0 PUCALNMMOETS Re Pes eae. Ee Ai OS, OAL DAD tt 3. Yellowish sand-rock, with ferruginous stains, passing in some places into grit.. 3 0 4. Slaty clay, alternating with yellowish and brown sand, and including remains of leaves and stems, in the state of lignite, generally about th of an inch in thickness. The lignite is divided into rhomboidal portions, separated by thin partitions of clay, which, when the coaly matter is removed by decomposition, have a deceptive resemblance to organic struc- ture. This group passes insensibly into (5.)........... HEISE tare \- ? 4 168 Dr. Frrton on the Strata below the Chalk. Ft. In. Ft. In. 5. Uniform sand, with alternations like those described above, (2. 6. and 2. e.). Continued nearly to the bottom of the cliff, where the rock is a fine uniform white sand-rock, like that of the great cliff at Hastings. The distance from the bottom of 5. to the base of the cliff, is about ....... 45 0 The total height of the cliff being........ about 65 0 The foregoing divisions are evidently arbitrary. In a general view, this section may be said to consist of rather more than 50 feet of thinly stratified sand and clay, with grit in concretions; including, at the upper part, a stratum of darker colour, about 12 feet thick, near the middle of which the remains of Endogenites are found. (83.) The rock composed of alternating layers of sand, and darker sandy clay, No. 2. a. of the preceding list, constitutes a large proportion both of the Weald clay and the Hastings sands; anda similar alternation of sand and clay of different hues and consistency, extends upwards beyond the limits of the Wealden, into the Lower green-sand. When the masses of the rock are dry, the structure is less conspicuous, but it becomes beautifully appa- rent when they are moistened. The delicacy and distinctness of the folia which are then seen in the cross fracture of the beds, are very remarkable ; the separate leaves being frequently as thin as paper, yet perfectly di- stinguishable, from their different alternating shades of greenish grey ; and commonly continued with great regularity for considerable spaces ; a structure clearly indicating very tranquil deposition, such as might be expected in a fluid suspending solid matter divided to extreme minute- ness, yet subject to frequent changes at nearly equal intervals; which may well be conceived to have taken place in the waters of a lake or estuary, at different seasons, or during different conditions of the waters,—if it be going too far in theory to suppose the minuter laminz to have been the pro- duce of successive tides. (84.) The continuity of the ledges of rock under the Marina at St. Leo- nard’s, with those of the shore under the White Rock, is rendered more pro- bable by the occurrence of the Endogenites erosa in both*. The principal ledge at the former place is very conspicuous on the shore at low water, and is one of the most remarkable geological features on the west of Hastingst. The following are the beds of which it is composed: * I did not myself see this fossil at St. Leonard’s; but Mr. Woodbine Parish, jun., informed me that the specimen represented in fig. 8, Plate X1X., was obtained at the foot of the cliff around the church. + These prominent ledges are precisely analogous to those which occur in the Hastings sands on the south coast of the Isle of Wight, where several reefs of rocks run out almost directly into the sea, and have obtained separate names from the inhabitants. On the Sussex coast they are less conspicuous, from the more rapid dip towards the sea, and the obliquity of the strike to the line of the coast; but many more such ledges do exist, between the flat near Pevensey and Cliff-end, about midway between Hastings and Winchelsea :—see hereafter, (95.) Dr. Fitton on the Strata below the Chalk. 169 Beds of the Group (III. c.) composing the Ledge on the Shore beneath St. Leonard’s. 1. Hard, subcalcareous, greenish grit, full of fossils; chiefly Cyclades, with Paludine, } 1 6 and some large Uniones ..+..++++eeeeeeeeeeeecseeeenee iveievorsushé 5 ois bie A thick and nearly continuous stratum, very like the stone of Hollington about 24 miles north-west from Hastings; its structure, however, like that of the White rock, is distinctly concretional. The top of the concretions, when ex- posed and washed by the sea, exhibits beautifully the minute stratification of the original sand; and the globular masses on the underside project into the sand (2.) below. The stone is traversed nearly at right angles by veins of cal- careous spar, and includes portions of trees, converted into lignite. It is asso- ciated also with patches of a looser conglomerate, consisting chiefly of rounded grains of whitish, nearly opake, quartz, including the teeth, scales, and bones of fishes, and of a species of Trionyx?. The strike of this)stratum is about 10° south of east, and the dip towards the west of south, at an angle of about 11°. 2, Yellowish sand-rock, abounding in impressions of Cyclades, and also resembling } Mtg part of Hollington group ...+++-.+- Spsisitalefels) ois t.0,.cia en « cic ete sjaielsielel evel olive ects) eerie 20 «90 5. Greenish Fuller’s-earth.......... eferavelorsienste ete ieieel keveles« oncosnace ye oO Gh WE esihle oohanbcodiocorsouosmonG adcucoDSDGonwbosooO6aoseou) 3 7. Band of iron-stone ..... Sietete oa erwin rie cele cere) etansveversiaterere ster ete sietersveneore a Onmmmes 17 G 8. A band of ‘clay iron-stone and slaty clay ©.0..:02.-.scscecsecene san lOme to 9. Slaty clay approaching to clay iron-stone............-- aoouooucco §=©6 G 20 ~O 10, Firmer slaty clay including small flat nodules of iron-stone with numerous Maree Gycladesy 66 eM eee eae colt ete ten cee ee ener 10) Oy jSetlard!grit; about’. ..%0 1... sogass00056 Hrabooeissuaaedouss SovEeD Lis ee Softesand rock Imi 3 (Or AnCOUNSES meleletel oteleletehetecolelenstelel oleleletcielenerclatsrate 2. 6 13. Firm sandy clay, with Cyclades ; firmer and more sandy at bottom.... $ 6 14, Yellow and reddish sand (or very soft sand-rock), in very thin alter- nating courses..... e's, clo) 0) elallel ee vias’ s\n ieleVolieiotel(elela/s (olavelo/e\ allele! s/s ieie tes pL iG) 15. Soft sand-rock, resembling the last but of lighter colour. This seems to go down to the base of the church. Visible, about............-. 9 0 16. A bed of firm sand-rock (immediately on the east of the church), about 2 0O 17. Thin beds of slaty clay; with interposed layers, or thin masses, nearly con- tinuous, of clay iron-stone, including layers of Cyclades. Visible about 6 0 Total thickness (visible)..... nie eieyonela BARON ae The strata in the roadside on the east of the church dip towards the east of south, at an angle of about 10° to the horizon ; but behind the church the dip is 3 in 40 (or about 4°), towards the north. The following is an approximate list of the strata in the cliff on the west of the Sussex Hotel, between the bottom of the group last mentioned (III. d.), and the White sand-rock IV. ; cor- responding therefore to the strata on the east of the White Rock, beneath the group III. a., which contains the Endogenites. The measures exceed the truth, but the proportions are probably correct. ies LO WM SAC KOCK Wretelercuelsioteta clei s\eletsia sisterate shee leted ote fa/e)iofe aj el ojo loreietete let aeletenet el aE 40 2. Sand-rock with clay, including Cyclades, about ........... sb0sn654 oes ss oneal 3. Beds of darker hue, apparently consisting of clay and sand .........-. + one siete 4. Dark yellowish brown sand-rock .......eseeeeeeeee ov 0/6, « elu o)ejcle)s ola)ieiaiel aie 70 5 tom of the cliff, and is continued downwards. The femur of an Iguanodon was . Very white sand-rock, or slightly coherent sand, occupies about 30 feet at the bot- | 30 found in this stratum ...... asererier sey siieleiieiel eta rereheerewererete eis) a oreteliereretonelenete wane Totalvabout.-eeree oa | 00 I n. 0 0 0 0 0 0 I1V.—In the space between the base of the cliff at the Brewery and the Castle-hill, all the beds have been carried away. But the great white sand bed IV. a. & b. is itself visible at high-water mark immediately below the middle point of the White Rock; and thence to the place where the road to Hollington is cut through this stratum. thick, it is continued with perfect uniformity of character to the top of Fairlight Down*. From the Castle-hill, where it is at least 80 feet * The massive beds of scarcely concreted sand around Tonbridge Wells,—on the Race-ground, at Rusthall-common, and in the heights of Frant and Eridge-park, appear to be a continuation of Dr. Frirron on the Strata below the Chalk. 171 IV. c.—The white sand-rock above supposed to be a continuation of that on the Castle cliff, pro- bably rises on the shore under St. Leonard’s church, but is not visible in the cliff, till it reaches a spot on the east of the Sussex Hotel, where caves have been cut in the mass of almost uniform sand, not to be distinguished from that of Hastings. It would be very desirable to ascertain by experiment whether marine salt exists in this deposit. V.—Immediately below the sand-rock (IV.), at the western extremity of the Castle rock, is a thickness of about 35 feet, of dark brownish, tough, sandy clay, including lignite in considerable quantity, some of the continuous pieces being several feetin length. This group goes down to the level of the road or street ; and thence to low water mark, a space about 20 feet in thickness is concealed. But under the Parade on the east of Pelham-place, a floor of grey sand-rock, is exposed at low water, the strike of which seems to be nearly from east to west. It includes crusts and patches of brown oxide of iron ; and is traversed by two sets of cracks, one running nearly north and south, the other from the north of east to south of west, which divide the surface into nearly rhomboidal portions, with angles of 72° and 108°. VIL.— Cliffs on the West of St. Leonard’s.—The line of the coast at St. Leonard’s coincides with the strike for about 200 paces west of the arch at the entrance to that place; and the strata at the water level appear to be horizontal; but about 400 paces west of the Sussex Hotel, the heights turn inland towards the north of west; so that the strata in the retiring portion of the cliff are lower in the series than those upon the shore. They agree with those which are visible at low water be- neath the town of Hastings, and with the lower strata in the cliffs around the shallow bay, or cove, at the Lover’s Seat. VII. a.—The cliff west of the Church is continued for some distance at an uniform height of about 100 feet. It becomes lower in approaching Bopeep; and at a point where it turns inland, between 200 and 300 paces east of the Martello Tower No. 39, is a floor of sand-rock, at low- water mark, full of grains of oxide of iron, like that of the coast to the eastward; the strike being towards the east about 25° south; and the dip east of north, at an angle of about 11°. The upper part of the cliff at this place, which is about 40 feet high, is composed of brown sand-rock, in beds from 2 inches to 6 in thickness. A grass-covered height, of less elevation, occurs immediately on the west of Bopeep, and the rock exposed there to a thickness of about 10 feet, consists of reddish sandy marl (VII. a.), not distinguishable from the Red marl of Devonshire. A low flat hill about 300 paces west of the Tower No. 40, consists for about 20 feet at the top, of sand alternating with clay, in beds dipping very gently to east of north. VII. 6.—At the east end of the cliff at Bulverhithe, on which stands the Tower No. 43, the beds dip regularly about east 30° north, at an angle of about 1°. Thence, along the shore, to the Tower upon Galley-hill (No. 44.), strata of reddish sandy clay or marl, variegated with light tea-green, are very well disclosed, declining, towards the east, at an angle between 2° and 3°: and above these coloured marls, is brownish sand-rock, about 50 feet thick. this stratum of Hastings. On the north of those great beds, and above them, is a group com- posed of thin, alternate beds of sand-rock and slaty clay, in many respects resembling that of the Brewery near the White Rock. These upper beds are quarried at Huntley’s Farm, about a mile west of the northern entrance of Tonbridge Wells; where they abound in Cyclades, Paludine, and Cypris Valdensis (C. Faba of Min. Conchology), and include the remains of several plants, among which are Sphenopteris Mantellii, and a new species of fern, represented in the wood-cut at p. 181. The relations of the strata at this place, and in the tract on the north of it, towards the valley of the Weald, are well deserving of attentive examination: I am indebted to the Rev. Mr. Pope of Tonbridge Wells, for having pointed them out to me, and for a collection of specimens obtained there by himself. z2 172 Dr. Fitton on the Strata below the Chalk. On the west of Galley-hill, the strata in the banks, which scarcely can be called cliffs, are in- clined slightly to the west of south; and the flat shore, near Cowden Point, consists of beds of clay and sandy clay, varying in colour from dark to bright blue, declining very gently towards the south-west, and extending outwards to some distance under the sea, with a strike towards a point about 16° south of east. Under the Martello Tower, No. 51, about four miles west from Galley- hill, is sand-rock, with ferruginous seams, and thin alternating beds of clay, slightly inclined to the west; from their situation not improbably one of the groups subordinate to the Weald-clay men- tioned by Mr, Martin. (85.) Endogenites erosa.—In cutting down the cliff on the east of the White Rock, immediately within the site of the new Brewery, large sur- faces of the several strata were successively laid bare ; and I was so fortunate as to visit the place when one of them was exposed, which contained a great number of the singular fossil bodies to which the name Kndogenites erosa has been given, and to see some of them in their original position before they were disturbed. ‘The workmen assured me that the fossils had been still more numerous in a portion of the same strata cut away not long before. The place in the series, of the strata which include these fossils, has been already mentioned (p. 164—8.). I observed but one line in the face of the cliff which seemed to afford them, about 6 feet from the top of the group ITI. 6. (81.) and (82.), which was about 10 feet in total thickness. The workmen told me, however, that some were afterwards found at a short distance below, where the strata were still nearly the same. I did not find any specimens of the fossil upon the shore ; but fragments are frequently washed up by the sea in the neighbourhood of this place ; and I saw a very © large specimen in the face of the bank, on the side of the road over Cuckoo Hill, which joins that from Hollington to Hastings. Mr. Woodbine Parish obtained one, (Plate XIX. fig. 8.), which was dug out in his presence near the Church at St. Leonard’s. Their occurrence at Tilgate Forest, where they were discovered by Mr. Mantell, has been mentioned in the Geological Transactions and in his own publications*; and Mr. Martin mentions the Endogenites, as having been found near Mulsey, in Western Sussex, in the first course of sand with reddish clay, subordinate to the Weald-clay, and above the Sussex marbleft. There can be little doubt that when the corresponding beds in other parts of the Wealden district have been examined, they will be more extensively discovered. The rapid change of character in the beds of this formation appears from the fact, that the great concretions of grit, several feet in length, and 2 or 3 feet in thickness, which are found upon the shore to the westward, do not occur in this cliff, though not more than 200 paces distant ; their place being apparently supplied, in the strata above those which include the Endogenites, by nodular masses of hardened sand-rock. ‘The bed III. b. 2. e. (p. 167.) which includes these fossils, passes both above and below into the adjacent strata, but has in general a darker hue. ‘The fossils were closely enveloped in a mass of slightly coherent sandy clay ; and I was enabled, with care, to preserve some specimens, (one of which is represented in Plate XIX. fig. 4. a. and b.) with part of the surrounding rock still adhering, as a proof that the coating of coal by which the nucleus was invested had never been of greater thickness, and that the whole of it was retained. (85.) All the specimens of this singular fossil which I saw, lay with their * Geol. Trans., 2nd Series, vol. i., p. 423;—and Mantell’s Fossils of Tilgate, p. 54. + “ Memoir” &c. p. 41, note f{. Dr. Firron on the Strata below the Chalk. 173 longer diameter and their flatter surfaces in the horizontal position. Their appearance when first uncovered by the removal of the rock above, was that of elongated and flattened elliptical bodies, tapering at both extremities ; as represented in fig. 1. of the subjoined wood-cut, ‘They consist of two distinct portions ; a stony nucleus, of a dark brownish grey colour, with a very slight tinge of purple; and a crust or case, in the state of lignite, which has externally a nearly uniform surface, and varies in thickness, in different specimens, and in different parts of the same specimen, from about =}; to+aninch. This crust becomes thicker near the extremities of the nucleus, and, in many instances, extends considerably beyond it, in a sort of appendage at both ends; but in other specimens of smaller size these appendages do not appear to have existed. ‘The annexed wood-cut explains the structure of one of the largest specimens, and shows the relative propor- tion of the parts ; and the figures in Plate XIX. show some of the principal varieties of form which the fossil has hitherto presented. Fig. 1 of the wood-cut on this page represents the external appearance of the entire fossil, as seen from above ; the situation of the nucleus being indicated by an obscure dotted line. Fig. 2 is a longitudinal and vertical section, on the axis or line a, b; and fig. 3, a transverse vertical section, on the line c, d; showing the proportion of the coating to the nucleus, The figures in Plate XIX., which are on a scale of one sixth, in diameter, of the natural dimen- sions, are intended to represent some of the forms of the complete fossil, and of the nucleus when divested of its coating of coal. They are, however, from necessity so much reduced, as to con- vey but a very imperfect impression of the bulky objects which they represent. Fig. 1 represents the greater part of a very large nucleus, of which only one of the extremities seems to be wanting. The remaining extremity is of irregular shape, as if it had been broken; and the specimen is much compressed in the middle. Fig. 2 is a nucleus apparently complete, tapering towards one extremity, nearly as may be supposed to have been the case in the part which is wanting in Fig. 1. Fig. 3, a and b, are horizontal and side views of a much smaller specimen, still retaining its coaly covering, with part of the smooth surface, hereafter mentioned. Fig. 4 is a larger specimen, with some of the sandy clay in which it was imbedded still adhering, the laminze of which are curved as if they had adapted themselves to its form. The specimen 174 Dr. Firton on the Strata below the Chalk. retains the greater part of its covering of coal, which has a smooth outer surface, of a light brown or drab colour: and at the lower part, a portion of the coal has been drawn away from the nucleus, apparently by the contraction of the investing matter to which it strongly ad- heres. One end of the specimen, where a portion has been accidentally broken off at b, shows P P y the proportionate thickness of the coating to the nucleus within. Fig. 5 is a smaller nucleus, nearly complete, very short in proportion to its width. Figs. 6 and 7 are sections of speci- mens broken across, and exhibiting the flat surface of the fracture in the nucleus, with the proportion of the coaly covering, and the porous structure of the nucleus. Fig. 8 is the nucleus of a large specimen found by Mr. Woodbine Parish, in the strata near St. Leonard’s Church. It is remarkable for the compressed appearance of one extremity, and seems to have been originally longer in that direction. It still retains a portion of the investing coal, and of the smooth outer surface of that coating, but the greater part has been removed or disturbed. Fig. 9 is taken from a specimen from Tilgate Forest, presented to the British Museum by Mr. Mantell, which is remarkable for its length, its nearly cylindrical figure, and the acute tapering of the extremity. The superficial furrows also, in this specimen, are deeper and much larger than in the greater number of the nuclei found near Hastings *; but inthis respect it is approached by Figs. 1 and 2. Fig. 10 represents rather more than one half of a complete nucleus, of the natural size: the upper surface of a, of which fig. b is a separate representation, showing the appearance of a fracture on the line of the longer axis. (86.) The size of the different specimens varies considerably. The largest that I saw in its place, and from which the foregoing wood-cut was taken, must have been in the whole full nine feet long; but there were portions of other nuclei of greater size, among the fallen specimens previously dug out. The lignite at one extremity was three feet in length; the nucleus 43 feet; and the workmen assured me that the coal at the other end extended to about 18 inches. ‘The width in the middle was 12 inches, and the greatest thickness 4 inches. Another specimen, which had been for some time exposed to de- composition, was about 73 feet long ; the nucleus about 52 feet, with about 12 inches of lignite remaining at each extremity ; and from these dimensions there seem to have been gradations down to a few inches in length. The nucleus of the smallest specimen that I obtained, which is represented, of its natural size,in Plate XILX., fig. 10, is not more than 3 inches long, and about 2 inches wide; yet the external figure is complete, and the internal tubes are not smaller than most of those in the largest masses. (87.) The original form of this vegetable was probably cylindrical ; and that shape is still retamed in a large specimen of a nucleus from Tilgate Forest, now in the British Museum ; Plate XIX., fig. 9: but in the majority of the specimens the figure has evidently been compressed, and the section is now an oval variously modified; figs. 6,7, 10. In those represented in * Since this sheet has been at the press, I find, on examining several other specimens in Mr. Mantell’s museum, that the uncompressed figure and greater size of the external tube-like furrows, are general characters of this fossil at Tilgate Forest. Dr. Firron on the Strata below the Chalk. 175 figs. 2 and 9, the extremity is more acute than in the greater number of the specimens. In a few instances (as in fig. 8, and less obviously in figs. 2, and 1,) the nucleus seems to have been suddenly reduced in thickness near the broader end; but no specimen of this form was observed zn situ. None of the specimens exhibited the tapering figure, somewhat like that of a ninepin, represented in the engraving in the Geological Transactions* ; but many of the broken and worn fragments washed up on the shore near the White Rock had acquired some approach to that form. There was not, in any of the spe- cimens, the slightest indication of lateral branches from the main body ; but they all lay as if they had been distributed without connexion in the stratum in which they were found. (88.) The coaly covering did not, in any instance, show traces of or- ganic structure; it burned with a slight flame when thrown upon hot coals, and in the flame of a candle became white, and was reduced in bulk without losing its form. In some of the fresh specimens it was coated with a thin crust, of a light brownish or drab colour, with a very slight glistening lustre ; apparently consisting of compressed clay. This is represented especially in figs. 4, a and b, and partially shown in figs. 3 and 8. (89.) The internal structure of this fossil has been partially described and represented in the Geological Transactions+, by the Secretaries and a Com- mittee of the Members. I am enabled to add some further particulars to what is there stated, through the kindness of my friends Mr. Brown and Mr. Stokes: the former having lent me the specimen represented in Plate XX., fig. 3., and given directions for making the slices, figs. 1. and 2.; to which Mr. Stokes was so good as to add a very thin slice, represented in figs. 4.and4.a. The vermicular cavities or tubes, of which a longitudinal section is represented in fig. 1., and a transverse section in fig. 2. and 4., are all coated within with transparent quartz crystals, the summits of which are discernible with a lens; and in some cases the cavity of these tubes was partially oc- cupied by exceedingly minute crystals of quartz, either detached in the state of sand, or intermixed witha flocculent coaly matter. The transverse sections of these tubular cavities exhibit a similar change of form, from circular to elliptic, to that shown by the entire plant. In the greater number of cases no trace of truly organic conformation could be detected with the microscope in these sections ; but in two specimens a distinct indication of the original vegetable structure was to be seen. These are represented in Plate XX., fig's. 3.and4. The former figure, drawn from the extremity of a solid and opake * Second Series, vol. i. Plate 48. t Second Series, vol. i. Plates 46 and 47: and Mantell, Tilgate Fossils, Plates 2 and 3. 176 Dr. Firron on the Strata below the Chalk. mass, a little decomposed, shows, within a cavity, a somewhat circular band, exhibiting organic structure, which is probably tubular* ; and the same kind of structure is indicated in the other figures, 4. and 4. a, which are taken from a transparent slice belonging to Mr. Stokes; the latter being a more highly magnified portion of fig. 4. (90.) Fossils of the Wealden—The catalogue of the organic remains of Sussex, published by Mr. Mantell in the last volume of these Transactions, and which he has stated to have been intended to accompany these pages 7, renders it unnecessary to insert here the fossils of that portion of the Wealden. The following list, therefore, will contain such species only as have been found in the tracts described in the preceding pages of this paper, or as do not occur in Mr. Mantell’s catalogue: and I have been enabled to add se- veral species to those of my own collection, through the kindness of Lord Greenock, Mr. Hills, Mr. Martin, and especially of Mr. Mantell. List of Fossils of the Wealden, in Kent, Surrey, Hants, and Western Sussex tf. Bulla Mantelliana. Pl. XXII. f. 3. With Unio antiquus, within a cavity in the grit of Tilgate Forest: M. Corbula alata. Pl. XXI.f. 5. Pounceford near Burwash, Sussex: M. Cyclas angulata. Pl. XXI.f.12. Weald clay: M. C. maor. Pl. XXI. f.13. Weald clay, in nodules of clay iron ore, with Cypris Valdensis and Paludina elongata, Hythe (Kent): F. With Cypris, fish-bones, and pyrites, in iron ore; upper part of the Weald clay, near Pulborough: Martin. Henhurst, near Ockley, Surrey; in Weald clay. With Paludina fluviorum in thin bands of very hard ferruginous calcareous grit, passing into ferruginous sand ; near the top of the Weald clay on the west of Leith-hill, Surrey: F. Cyclas media. (Cyrena media, Ann. of Phil. Vol. VIII. p. 376. Cyclas media, Min.. Con. Tab. 525. f.2.) Pl. XXI.f. 10. So generally diffused throughout the Wealden strata that the specification of localities is hardly required. The fol- lowing are some of the circumstances under which this shell has been found. In coarse grit near the top of the Weald clay, at Atherley, south of Tanhurst, Surrey. In very compact uniform grit, with thin carbonaceous vegetable im- pressions,—shell calcareous : also in very fine-grained micaceous sand-rock, with * In this figure, from the greater difficulty of representing the opake object, the partitions between the dark spots which denote the cavities of the tubes, are much too wide: the real proportion of the cavity to the partition is more correctly expressed in fig. 4. a. ’ t “ A Tabular Arrangement of the Organic Remains of the County of Sussex.” Geological Transactions, 2d Series, vol. iii. p. 215. + In this list the letter M. denotes that the specimen is in Mr. Mantell’s collection; F. in that of the author. Dr. Firron on the Strata below the Chalk. 177 Cypris; impressions only, without traces of the shell: Hollington, near Has- tings. In nodules of clay iron ore: Cliffs west of St. Leonard’s. In shale, called “Shab,” alternating with beds of limestone called ‘‘ Greys,” (a stone al- most entirely composed of thin shells): Limestone pits north-west of Battle: F. With Paludina fluviorum, in bluish compact and sparry limestone, (“ Sussex mar- ble”); Daniel’s Water, Kent. In sand-rock near Tunbridge Wells: M. At the top of the Weald clay, mixed with bivalves of the Lower green-sand; Stopham brick-yard near Pulborough: Martin, Cyclas media. (Young.) Plate XXI. f.9. Hastings sand, Hollington, in hard grit ; shell converted into carbonate of lime: F. Etchingham near Robertsbridge, Sussex: M. ——. (A gibbose variety.) Plate X XI. f.11. Penhurst pits, in a bed of lime- stone, about 3 inches thick called ‘“‘ Top-greys’’: F. C——. A wider species than media. Hastings sand, Hollington: F. C—— membranacea. (Cyrena membranacea, Ann. of Phil. 1824. viit. p. 376.) Cliff west of St. Leonard’s, in sandy shale, with Cypris: F. Weald clay, Shipley, near East Grinstead, Sussex, with a spiral univalve (Potamides?): M. Limestone pits near Battle: F. Penhurst, Ashburnham, and Pounceford: M. C—— subquadrata. Plate XXI.f.8. Hastings sand, East Cliff, Hastings, in soft, fine, sandy clay, not effervescent: also cliff west of St. Leonard’s: F. C——. One or two other species, probably new, occur in the Weald clay, at Ather- ley, Surrey: F. Cypris granulosa. Pl. XXI. f. 4. In ferruginous sand, Tilgate Forest: M. C. C tuberculata. Pl. XXI.f.2. Frequently black. With Cypris Valdensis and Paludina elongata, in nodules of clay iron ore, near the top of the Weald clay : found by Lord Greenock, at Hythe C. Valdensis. Pl. XXI.f. 1. (C. Faba, Ann. of Phil. 1824, vir. p. 376.; Min. Con. Tab. 485.) This fossil occurs in such numbers in every part of the Wealden group, that it may be considered as characteristic of the formation; and being found in all the places where these strata have been hitherto observed, the speci- fication of localities would be superfluous. Its profuse abundance may perhaps be accounted for by the fact, that the animal which inhabits the valves or crusts, sheds them periodically*. The Cypris to which the specific name of “‘ Faba,” was given by M. Desmarestt, occurs in strata probably superior to the chalk; and though the characters of the valves nearly approach to those of the Wealden Cypris, M. Deshayes is of opinion that it probably constitutes another species{. On these grounds, I have thought it expedient to adopt a new specific name for the fossil represented in Pl. XXI. f.1.; and that of Valdensis (of, or belonging to the Wealden) is intended to indicate both its geological or stratigraphical position, and the local situation of the tract in which it has hitherto been found in the * Lyell “ Principles,” &c., 3rd edition, vol. iv. p. 98. + Brongniart and Desmarest, ‘‘ Crustacées Fossiles,” p. 141, Pl. XL, fig. 8. t “ Coquilles Characteristiques,” p. 255, Pl. 10. figs. 4. aud 5. VOL. IV.—SECOND SERIES. 2A 178 Dr. Firron on the Strata below the Chalk. greatest abundance. A description of the several species of this genus repre- sented in the annexed plates will be found hereafter, in the Appendix. Melanopsis ? attenuata. P\. XXII. f.5. (Melania attenuata, Ann. of Phil. 1824, v111. p. 376.) Inthe Hastings sands, Hollington: F. Pounceford: M. —? tricarinata. Pl. XXII. f. 4. (Melania tricarinata, Ann. of Phil. ibid.) Pounceford near Burwash, Sussex: M. Mytilus Lyellii. Pl. X XI. f.18. Beds below, or at the bottom of the Hastings sands, near Battle: F. In slaty clay, near Pounceford: Messrs. Lyell and Mantell. ; Neritina Fittonii. (Mantell ; South-East of England, p.248.) Pl. XXII. f.7. Casts in the grit of Tilgate Forest: M. Ostrea ? (a thin-shelled species). Sand-rock of the Hastings sands, west of St. Leo- nard’s: F. Paludina carinifera. (Min. Con.) Hastings-sands, west of St. Leonard’s; below the White Rock, Hastings; and at Hollington: F. In Septaria, at Resting-oak Hill, near Lewes: M. M. P elongata. (Min. Con.) This fossil is very generally diffused in the Weal- den strata. It occurs in nodules of clay iron ore, near the top of the Weald clay, at Hythe: F. In hard blue grit, with Cypris Valdensis and C. granulosa? In the grit of Tilgate Forest: M. Near Ockley, in Surrey: F. P fluciorum. (P. vivipara, Min. Con.) One of the most abundant univalves of the Wealden. On compact calcareous beds in the Weald clay; Bethersden and Daniel’s Water, Kent. At Henhurst, Surrey; in ferruginous sandstone. In concretions of grit in the Weald clay, very large. At Forest-green, and near Ewhurst, Surrey; near Ockley, Surrey, with Cypris Valdensis, in beds of “Forest marble.”” South of Den-park, Sussex: F. yb Sussexiensis. Pl. XXII. f.6. Resting-oak Hill, near Lewes, Sussex: M. P. two or more other species, probably new, occur at Tilgate: Mantell. Potamides ? With Cyclas media, in shale, alternating with limestone; pits north-west of Battle: F. In Weald-clay, East Grinstead: M. Psammobia? Tellinoides. Pl. X XI. f. 6. With Cyclas in limestone; Pounceford near Burwash, Sussex: M. Tornatella Popii. P}. XXII. f.8. Lenthington (pronounced Langton) Green, near Tonbridge Wells, in dark brown ferruginous sand-rock, with Unio, Cypris, and Cyclas: Rev. Mr. Pope; and M. Unio aduncus. Min. Con. Bolney, near Pulborough: Martin. Near Cuckfield, Sussex: M. U— antiquus. Min. Con. Weald clay, near Pulborough: Martin. Tilgate Forest, very frequent: M. U— compressus. Min.Con. Weald clay, near Pulborough: Martin. Tilgate Forest : M. U— cordiformis. Min.Con. Tilgate: M. U— subtruncatus. Pl. XXI. f.15. With Cypris Valdensis, Cyclas media, and Tor- Dr. Fitton on the Strata below the Chalk. 179 natella Popii? in dark brown ferruginous stone, Lenthington-green, near Ton- bridge Wells. Also at Tilgate Forest: M. Unio Gualterii. Pl. X XI. f.16. Discovered by Mr. Walter Mantell in the dark brown ferruginous sandstone of Lenthington-green, near Tonbridge Wells: M. U— Mantellii. Pl. XXI. f. 14. In calcareous grit, passing into ferruginous sand, near the top of the Weald clay ; Atherley and Henhurst, Surrey: F. Tilgate : M. U— Martinii. Pl. X XI. f.17. Upper part of the Weald clay, near Henhurst, Surrey: Martin, and F. U— porrectus*. Min. Con. Weald clay, near Henhurst and Atherley, Surrey: F. Large specimens, with Paludina fluviorum and Cyclas media, eccur in the cliffs west of St. Leonard’s, in firm bluish grit: F. In sandstone, Tilgate Forest: M. Reprives. The reptiles of the Weald clay and Hastings sands in Sussex, nearly all of which have been discovered by Mr. Mantell, have been so fully treated of in his various publications, that I shall refer to those works for an account of them, and here only enumerate their names, with some of the chief places of their oc- currence. The remains, however, of oviparous quadrupeds seem to be dispersed throughout the whole of this formation, though hitherto found principally in the Weald clay and the upper part of the sands beneath it: it is from this latter situation, in the grit and sand-rock of Tilgate Forest, that the greater number of Mr. Mantell’s specimens were obtained. Trionyx Bakewelli. (Mantell, S.E. of England, p.255.) Tilgate Forest. Emys, (species unknown.) Same place. Chelonia. Ditto. Saurians,—of at least six genera. Crocodile. Remains of two, if not of four, species. (Ibid. p. 265.) The teeth, scales, and some of the bones, are mentioned by Mr. Mantell, as oc- curring at Tilgate. A vertebra, which was considered by the Baron Cuvier, as belonging to this genus, was found in the strata of shale and limestone at the bottom ofthe Hastings sands, near Briglitling, Sussex: F. Phytosaurus cylindricodon. The teeth: Tilgate Forest. (Mantell, S.E. of En- gland, p. 292.) Plesiosaurus. Vertebra, teeth, and other remains: Tilgate. (Ibid. p. 281.) Megalosaurus Bucklandii. The teeth, (supposed) ribs, and vertebra. Tilgate Forest. (Ibid. p. 260.) Hyleosaurus. (First described by Mr. Mantell, in a paper read before the Geo- logical Society (Proceedings, &c. Vol. 1. p. 410.), and since published in his Geology of the S. E. of England; p.289, &c. Plate V.) The remains were found in Tilgate Forest. Iguanodon. (Mantell, Philos. Trans. 1825, p. 179.) The remains of this mon- Several indistinct specimens of this genus, including probably some new species besides those above mentioned, have been found at Henfield and Atherley, in Surrey, by the Author; and near Pulborough, by Mr. Martin. 2a2 180 Dr. Firton on the Strata below the Chalk. strous reptile have hitherto been found chiefly in the upper part of the Has- tings sands at Tilgate Forest: but very large bones, belonging, as it now appears, to the same animal, have been obtained much higher up in the Weal- den series, at Loxwood, and Headfold wood, in Western Sussex*: and very recently, even beyond the limits of the Wealden group, among the lower strata of the Green-sand, near Maidstone, (as already intimated, p. 132; note +): they occur also as far down as in the Great Sand-bed of the cliffs on the coast near Hastings, where that stratum reappears on the shore west of St. Leonard’s. Iam requested by Mr. Mantell to state, that the mass of remains from Maidstone confirms the appropriation to this reptile, which he had pre- viously made, of other bones of great size found detached, and in different places; and that, among other new points in the osteology of this extraordinary creature, the Maidstone specimen has enabled him to ascertain that certain phalangeal bones which approach to the mammalian character,—with flattened claw-like extremities, resembling those of land-tortoises,—belong to the hind feet of the Iguanodon; while the fore feet of the creature appear to have been long and slender, like those of the recent Iguana. In addition to the Saurian remains which can be referred to distinct genera, there are also in Mr. Mantell’s collection, detached bones, probabiy belonging to new or nondescript reptiles. Birps. Fragments of some long bones found at Tilgate, and at first supposed to have belonged to Pterodactyles, appear to be really those of a bird, probably a species of Ardea. (Mantell, S. E. of England, p. 283.) Fisues. The fishes of the Wealden, especially of the two upper members, have hitherto been imperfectly collected; and it still remains to be determined to what species of this tribe many of the remains which frequently occur in the Weald clay are to be referred. All the specimens from this formation in the col- Jections of the Geological Society, of Mr. Mantell, and Mr. Martin, have been recently examined by Mr. Agassiz, with a view to his work on Fossil Ichthyology, now in progress ; and the following are some of the genera to which he has re- ferred them. Pycnodus microdon. Teeth. (Represented in Mantell’s Tilgate: Pl. XVIII. f. 26, and 27.) Hybodus grossicomis. Teeth. (Ibid. Pl. V. f. 14, and XV. f. 2.) ————-. Two other species, not yet figured. The dorsal defences referred by Mantell to a Silurus, (Ibid. Pl. X. f. 4, and f.6.), Mr. Agassiz considers as belonging to an Hybodus. Lepisosteus. (Lepidotus, Agassiz.) The remains of one or more species of this genus have long been known, as diffused throughout the Wealden ; in every part of which detached scales and fragments of the scale-covered surface are very commonly found. The Teeth are represented in Mantell’s Tilgate fossils, P]. X. f. 2.; the scales, in Pl. X. figs. 3,4, 15, and 16; and from an examination * Murchison: Geol. Trans. 2nd Series, vol. ii. pp. 104, 105. Dr. Frrron on the Strata below the Chalk. 18] of these, and of some very fine specimens of the head and fore part of the fish, belonging to Mr, Martin, Mr. Agassiz has been led to divide the genus into two species, distinguished by the forms of the teeth. Coprolite,—(or, more correctly, masses of phosphate of lime approaching to the form, and possessing many of the chemical characters of Coprolite,) has been found by Mr. Martin in cavities on the surface of the Weald-clay, at Stopham brick-yard, near Pulborough, but so mixed with fossils of the Lower green- sand that the whole may probably have belonged to that formation. The re- cent discovery of the Iguanodon, near Maidstone, forms an additional link of connexion between those two formations; and coincides with other evidence which indicates the probable continuity of their deposition. REMAINS OF PLANTS. A Cone ofan unknown species, (Pl. X XII. f.10.), remarkable forthe double prominence, or ridge, in most of the scales; (see Appendix No. 1.) : ina mass of hard, greenish grit. From a quarry on the estate of Henry Shirley, Esq., at Pippingford in Ashdown Forest, very near the highest point of the ridge of the Hastings sands. Endogenites erosa. (Plates X1X.and XX.) Described in the preceding sections (85.) to(89.). Tilgate Forest: M. Coast west of Hastings: F. In the first course of sand in the Weald-clay, near Mulsey’s Farm, about 24 miles north-east of Pul- borough, on the main road to London: Martin. Sphenopteris gracilis : represented in the subjoined wood-cut. See the descriptive note in the Appendix A, p.349. From beds of sandrock and slaty clay, in the quar- ries at Huntley’s Farm near Tunbridge Wells, above the great bed of White sandroek: Rev. W. L. Pope. 1 BA iy Y7) = SN vi i pn | i B, 2 < Va USS. bio, 182 Dr. Firron on the Strata below the Chalk. Tae Istz or Wigur. (91.) The general relations of the strata on the southern coast of the Isle of Wight, have been described by Mr. Webster* with so much ability, that little was left to succeeding observers but the task of filling up details, and of supplying some facts respecting the lower members of the series, which did not fall within the immediate scope of his inquiries. Having already pub- lished a general account of these lower strata in another placef, I shall here give some farther observations on what is commonly called ‘‘the back,” or south side, of the island. (92.) As the chalk passes entirely across the Isle of Wight, nearly from west to east, in a narrow ridge composed of vertical strata, and again invests a pordon of the southern promontory of the island, with a cap of almost horizontal beds, at present detached from the central ridge and ex- tending nearly to the sea,—the result is, that two very distinct sections of the vertical chalk and inclined strata beneath it are disclosed upon the shore, at the extremities of the central range; and again, two other sections, in which the same strata are prolonged from beneath the horizontal chalk, on each side of the promontory that projects towards the south, so as to meet the continuation of those which rise from the middle of the island, and with them form very flat curves. The coast thus exhibits a series of sections of almost unequalled richness and variety : and though the general characters of the strata are well known, there is still quite enough to be learned in this most interesting geological region, to repay such detailed researches as have been of late years devoted to some other portions of England, but whieh those only who reside near the place can carry on with complete success. (93.) The Section, Pl. X.a. No.7. (which is on the scale of the Ord- nance Survey), shows the general order of the strata on the southern coast of the island, and, with the aid of a good map, will enable the reader to follow the ensuing detail. In the lower of the two lines, the heights are on the same scale as the horizontal distances. Chalk.—The relations of the lowest beds of the chalk are best seen, on the west, at Compton Bay ; and on the east, in the cliffs under Bembridge Down; both sections exhibiting admirably the passage from the white chalk to the Upper green-sand. Large portions of the chalk are pre- * «Tetters to Sir Harry Englefield,” &c. 4to. 1816. + “ Annals of Philosophy,” Nov. 1824, p. 367, et seq. { The map annexed to Mr. Webster’s Jetters, in Sir H. Englefield’s volume, (Plate 48.) though less accurate geometrically, gives many names, and much information useful to the Geologist, which are not to be found in the Ordnance Survey. i | Dr. Firron on the Strata below the Chalk. 183 served also at the top of the higher Downs, on the south of the island, resting on a plateau of the Upper green-sand ; and the lower beds of the chalk are in many places visible in descending from these heights, as from Niton to the undercliff, and above Old Park, on the south-west of Wol- verton. The gradation of hue and texture, from the whitest chalk,—through various shades of grey, and various degrees of softness, to the state of bluish marl, resembles precisely what is observable in the same part of the series at Beachy-head, on the shore near Folkstone, and on the opposite coast of France, under the cliffs of Blanc Nez. The central ridge, or anticlinal line of the chalk, it will be remarked, is neither continuous nor rectilinear ; but is divided, about the middle of the island, between Carisbrook and Shorwell, by a tract of irregular ground, intervening between two nearly parallel branches of the chalk range about three miles apart. The first, or southernmost, of these branches runs directly from the Needles to Brixton-down; the more northern from Arreton-down to Bembridge-down and Culver-cliff. The course of the principal streams of the island is transverse to that of the central chalk range: the ‘river Medina, which nearly bisects the island from north to south, rising high upon the sands, about Stroud Green on the south of Kingston, and running almost directly northward to the estuary at Cowes. The other principal stream, the Eastern Yar, springs beneath the southern chalk, about Whitwell, not far from Niton; and after a tortuous course, instead of joining the sea in Sandown Bay, it cuts through the ridges of the green-sands and the chalk, between Yaverland and Brading. The egress of the streams, therefore, is here analogous to that already described in Kent and Sussex: and this effect may not improbably be ascribed, in both cases, to fissures, by which the lines of drainage were in the first instance determined. Upper Green-sand.—This formation is but partially disclosed along the base of the central ridge of chalk; but is distinctly seen in the sections at Compton-bay, and on the south of Bembridge- down, and in several places along the escarpment of the underclitf*; the course of which, it is to be observed, is not exactly parallel to the anticlinal ridge, but oblique to it, running towards a point about 17° south of west. The total thickness here, in some places approaches to 100 feet, and on an average is not much less than 70 feet: its step-like projection beyond the ehalk, as in Western Sussex, is conspicuous in several places, especially beneath St. Catherine’s Down. One of the most accessible sections is in the ground rising above the ravine at Luc- combe, where the road from Shanklin to Bonchurch crosses the strata obliquely. About the middle of Old Park is a continuous section of beds, apparently undisturbed and more than 3 of a mile in length, rising very gradually towards the south, or west of south, and consisting above, for between 30 and 40 feet, of subcalcareous sand and stone, alternating with chert in concretions,— and below of similar sand, with spongiform masses, like those of the upper part of the sections near Folkstone ; (21.) and (22.). But one of the best sections, perhaps, of the Upper green-sand, is visible above the road from Niton, towards Blackgang-Chine, over the Sand-rock spring. The brow of the cliff at that place is about 591 feet above the sea}; and the beds composing the ver- tical face at top, which is itself more than 100 feet high, may be thus divided : Alternations of soft subcalcareous stone, with concretional chert. ..30 to 40 feet. Yellowish grey sand and stone, with some chert......++e+++++++60— 80 Alternations of yellowish grey and bluish stone, and sand........15 — 20 * As above Western Lines; above St. Lawrence, where the road comes down from the interior, and thence westward; between Rans and Marables. At the place last mentioned the precipice is about 60 feet high, with gault beneath, and is traversed obliquely by a footpath up the whole face. + Englefield and Webster, p. 238. VOL. IV.—SECOND SERIES. 2B 184 Dr. Frrron on the Strata below the Chalk. Gault.—This stratum consists, in the Isle of Wight, of dark, bluish grey, harsh, sandy clay, in- terspersed with minute particles of mica: but I did not discover, anywhere, the beds of light bluish, plastic clay, like that of Folkstone, which abounds in the characteristic fossils, and which, I believe, forms the lower part of the formation. The clay here, which seems not to exceed 70 feet in thickness, contains very few fossils, and these, from their imperfect preservation, are difficult to obtain. The tract, however, which this stratum occupies has been very little explored. One of the best sections of the gault which I saw, was at East-End, between Luccombe and Bonchurch, where the clay contains nodules, and branching crystalline rods of pyrites, some thin shells in frag- ments, and minute crystals of sulphate of lime, perhaps produced by decomposition. The top of the sands beneath this stratum, here slopes both towards the west, and outward, towards the sea ; so that on the melting away of the gault, everything favours the subsidence and ruin of the upper part of the cliffs. Loner Green-sand.—This stratum, which forms the principal portion of Mr. Webster’s ‘ Ferrugi- nous Sands,’ occupies a great part of the surface on the south of the Isle of Wight, and is everywhere conformable to the chalk; a ridge of highly inclined strata of sand parallel to that of the central chalk, crossing the island, from the shore on the south of Bembridge Down to the foot of Afton Down. The sands are then reflected southwards, and form the lower ground in the interior, from Mottestone, through Brixton, Shorwell, Kingston, Godshill, and Newchurch, to the coast. ‘Throughout the greater part of the shore at the ‘ back of the island,’ this stratum is either below the level of the sea, or concealed by the debris of the undercliff; but where it rises,— westward from Rocken-End, and eastward from Bonchurch Cove, it exhibits the most distinct and fully developed sections. When I examined the Isle of Wight, I was not aware of the subdivision of the Lower green-sand into the groups, which I afterwards found to be so well displayed in Kent (16, &c.), and Western Sussex (72.); but from the map of the island, and the characters of the strata on the coast, I have no doubt that it exists also here. A range of heights from Kingston to Walpen, which in the Ord- nance Map is a very prominent feature, and seems to be continued to the shore between Walpen and Whale Chines, appears to be the outcrop of the upper member of the formation; and the heights on the south of Chale seem also to belong to this uppermost or ferruginous subdivision ; while the darker beds of Shanklin and Blackgang Chines must represent the middle, or more retentive group: and even among the highly inclined strata of the Red-cliff, in Sandown Bay, green, mud-like, beds are distinguishable in the corresponding part of that escarpment. A bed at the bottom of the cliffs, both at Atherfield, and on the east of Shanklin, which abounds in fossils, espe- cially the Gryphea sinuata, is probably the equivalent of the lowest group of stone at Hythe. The total thickness of the Lower green-sand in the Isle of Wight may be considered as about 300 feet. (94.) The Wealden.—The Purbeck strata do not make their appearance in the Isle of Wight; and the two remaining members of the Wealden pass into each other by insensibie gradation, the Weald clay constituting but a small proportion of the whole. A valley or depression, however, corresponding to the site of the clay, is still a well-marked natural feature : the escarpment of the green-sands projecting over it on the one hand; while on the other, the Hastings sands rise into a small prominence, even in the compressed section of Sandown Bay ; and form, on the west, an undulating, dome-shaped ridge, between Barne’s Chine and Compton-Grange Chine, the section of which corresponds to that of these sands on the Sussex coast. Dr. Firron on the Strata below the Chalk. 185 The affinity in mineralogical composition,—indeed in most of the cha- racters except the species of the fossils which they contain, between the strata in this portion of the series in the Isle of Wight, and those above the chalk on the north of the island, is exceedingly striking ; though the groups are separated by the entire mass of the green-sands and the chalk. In both we find reddish and variegated sandy marls, of various and similar shades of tea-green, purplish, and grey; in both, also, beds of sand and of erit*; and in both series, too, is an alternation of beds containing marine fossils, especially Oysters, with strata which abound in Paludina, Cypris, and: other productions of fresh water. The inferences from these facts are now so obvious, that nothing, it would seem, but the strongest prepossessions in geological theory could so long have kept them out of sight f; and the proof they furnish of the repeated submersion and re-elevation of the land, is irresistible. (95.) On the other hand, there is a very obvious resemblance, in mineralo- gical character, between a great proportion of the deposits, both above and below the chalk in the Isleof Wight, and the reddish and variegated marly sands of the new red sandstone (red marl), of England. Nothing can better prove the insufficiency of mineralogical characters, as a ground of identi- fication in geology, than this close resemblance in the productions of periods so distant ; while it demonstrates also the permanence and uniformity, both of the substances out of which the strata have been composed, and of the operations which produced their aggregation {. Weald Clay.—This stratum is visible on the coast, in one of the sections at Sandown Bay, and in both of those on the west of Rocken-End, forming a narrow band of comparatively low and flat ground,—encircling, and, as it were, insulating the Hastings sands, which rise from beneath it into heights of small elevation. In Sandown Bay, the most eastern portion of the clay, which * Grit, not in itself distinguishable from that of Hastings, and containing Paludine, occurs on the north-east coast of the Isle of Wight, near Cowes. See Mr. Webster's “ Letters,” &c. p. 321; —and “ Annals of Philosophy,” 1824, vol. viii. p. 379. + Soon after my examination of this part of the Isle of Wight, I had the pleasure of a visit there from M. Constant Prevost; and the following passage in one of his letters, written on his return from an excursion to the west of the island, coincides precisely with what is mentioned in the text :—‘ La succession des couches rappelle tout-a-fait celle de méme nature, que sur une échelle “‘ moins grande recouvre la craie, ou mieux est posterieure a Ja craie, 4 Alum Bay: c’est la méme “ disposition générale, le méme assemblage de couleurs, les alternatives de sable et d’argile avec “lignite, les mémes septaires, &c.; tout est analogue dans les deux series, a l’exception des “fossiles. On peut retrouver une analogie aussi forte entre les argilo-sables (Hastings sands) “ inferieurs a la craie, et la grande formation du nouveau gres rouge; les argiles verte, jaune, et “youge, les gres blancs et bigarrés, les conglomerats,” &c. } The abundance of the variegated reddish and greenish sandy clays in the upper members of the Wealden group, both here and in Sussex, is such,—and their proportion to the whole so great, that the name of the deposit might very well have been taken from them; and if the term Red-marl be retained as a general denomination, these and the new red sandstone might with some advantage be called the Upper and Lomer (or first and second) red marl; which would in- dicate both their mineralogical resemblance, and their relative position in the series. : 282 186 Dr. Firtron on the Strata below the Chalk. succeeds the sands of Red-cliff, is much obscured by intermixture with the ruins of several different strata fallen from above ; but it abounds in the characteristic fossils. The corresponding portion of the Weald clay, on the west of the Hastings sands, between the fort at Sandown and Shanklin Chine, forms a flat shore, which is visible only at low tides. Beyond Atherfield- point, in like manner, the clay rises from beneath the Lower green-sand, and exhibits beautiful sections in the Chines immediately on the north-west of that prominence: thence it passes inland, through the lower grounds of Sutton, Thorncross, Yafford, Marsh-Green, Mottestone, Brook- House, and Compton-Grange, and meets the coast on the south of the Lower green-sand ridge, at Compton-Grange Chine ; where a similar section to that of the west of Atherfield (or rather to that on the east of Sandown Bay), is exposed: but thereabouts the strata seem to have been disturbed,—whether by mere subsidence or the presence of a fault, I did not ascertain. Hastings sand.—The general position and relations of that portion of these sands which is visible on the coast of the island (for the sections do not go down to the lowest strata), will be obvious from what has been already stated, with the aid of the section, Plate X.a. No.7. In Sandown Bay the sands form but a small insulated spot, of an irregular figure, surrounded by the Weald clay: but on the south-west coast the superior strata of the formation are much better developed ; occupying an oblong tract, approaching to the shape of half an oval, from the west of Cowleaze Chine to Compton-Grange Chine. It will be seen from the Ordnance Map, that two small but remarkable prominences called Atherfield Rocks, and Brook Point, project beyond the general line of the shore, between Rocken- End and Freshwater Bay: so that the coast is divided into three shallow recesses, called Chale Bay, Brixton Bay, and Compton Bay; the last being, in fact, only the eastern portion of Fresh- water Bay. Atherfield Rocks, and the heights on the south-east of them, belong to the Lower green-sand, of which they are the outcrop. Brook Point (or perhaps the more obtuse prominence of the shore between that place and Southmore,) is apparently the central and lowermost portion of the Hastings sands; the culminating point being much nearer to the chalk in the centre of the island, than to that on the south, in consequence of the more rapid rise of the strata in the central range. ste sete’ ojcletsteme ? nous or carboniferous, which includes at the bottom concretions of quartzose Here the ground rises into the promi- grit, and contains Cyclades.......... 9 nence called Worbarrow Knob; and the A group including beds of stone com- back on top of a very extensive mass of posed of small Paludinz, in a cement stone is waved, like the ripple-mark on containing much green matter :—the the sea-shore. In the little cove between “marble” and “marble-rag” of the the “knob” and Gad Cliff, a thickness Swanage quarry-men .........-...- 16 of about 50 feet consists of clay, alter- Brownand grey clay,alternating with bluish nating with beds of limestone very much grit, and thin beds of stone .... About 25 contorted. (104.) Purbeck strata—The ridge of the Purbeck and Portland strata runs nearly from east to west, entirely across the peninsula; but the dip is not uniform, and the strata form a curve, or a portion of a dome-like promi- nence, of which the highest part is between Acton, St. Alban’s Head, and the heights above Kimmeridge, and thence to Tineham Hat; the culminating point being about Swyre Head, which seems to be about 700 feet above the sea,—nearly on a level with the chalk down at the western extremity of Pur- beck Hill, and perhaps 100 feet higher than the summit of Ballard Downy. The whole of the Purbeck series is exposed in the ruinous cliffs of Durl- stone Bay, where the strata have been enumerated in detail by Mr. Webster. At the upper part they consist of compact limestone, alternating with clay, and abounding in freshwater shells, especially of the genus Cyclas: but in- cluding also a thick bed called “ cinder” by the quarry-men, which is almost entirely composed of oyster-sheils. At the lower part, the formation consists principally of fissile limestone, the junction of which with the Portland strata exhibits some very remarkable appearances. All the stone which is quarried at present, occurs in the upper part of the series; and from Mr. Webster’s list it appears that in a thickness of about 125 feet, 55 consist of beds of useful stone ; 12 feet of the “cinder’”’ composed of oyster-shells ; and the remaining 58 of slaty clay, and thin beds of unpro- fitable stone. I was informed that about 150 feet more, of what the work- * This is the spelling of the Ordnance Map, and the word is so pronounced in the country. It is sometimes printed War-borrow, and by Mr. Webster, Worth-barrow. + The top of the Down between Acton and Bottom, (about the place of the final s in “ Down- shay’s Farm”, in the Ordnance Map), is much higher than St. Alban’s Head, and not much below Swyre Head. It seems to be nearly level with Encombe Head (Hound’s-Tout), and the east end of Ballard Down. t Geol. Trans. 2nd Series, vol. ii. pp. 38, 39. “ Dr. Frrron on the Strata below the Chalk. 209 men call “rubbish ” and “slate ’’, intervene between the lowest of the courses (or “ veins’’) of good stone, and the top of the Portland formation ; so that the total thickness of the Purbeck formation here is about 275 feet. Ft. In. Ft. In. Workable stone, and “rubbish”..........+..00. 99 O EOIN Chik Vorers fo al's7a (slots. oi bie aie ete) steuthe@iaerabiesches op LZ of 124 8 Workable stone, and “rubbish”........c00ces+e- Lo 8 RIOR IRD AISA” GLACE 5 cterare cles vines Kio] a x/ofala: ayalatate’e! epeterare;e 6° 150770 HOO dence ace Gas sonore db coucoe nde 274 8 The high ground between Peverell Point and Durlstone Head is divided by a depression or ravine, on the north of which, in addition to the flexures and contortions seen in all the sections, and well represented in Mr. Webster's plates, the strata are traversed by fissures, produced by upheaving, or subsidence, or both. The effect of these disturbances can be traced by means of the “cinder” bed; disjointed portions of which are still visible, inclined at different angles, in three or four successive falls, the first throwing down that bed more than 100 feet, and others 40, 15, and 3 feet. The fissures which separate the disjointed masses are widest at the top, and are filled with fragments of the dislocated strata. The place where these derangements occur is called “the Gulley”: on the south of it the strata are much less disturbed, and the “ cinder ” can be traced almost continuously in its proper situation, till it disappears near the face of the hill, not far from Durlstone Head. The groups at the top of the formation called the ‘‘ Marble” and the “‘ Marble rag”, consist for the greater part of small Paludinz, cemented by carbonate of lime with a very large proportion of green matter. ‘These beds are exposed on the shore at Peverell Point*, and were quarried many years ago at Langton, from which place it is said the pillars in the interior of Salisbury Cathedral were obtained. Another stratum, also containing a large quantity of green matter, but of a conglomerated or coarse sandy texture, is found at the top of the formation in some of the sections westward,—as near Worbarrow Knob, and on the east of Lulworth Cove. It includes a large and thick species of Unio; the shell, as Mr. Webster has remarked, being so abundant as to constitute a very large proportion of the whole mass. A characteristic of the upper part of the Purbeck series, both on the coast and in the interior, is the occurrence of seams of fibrous carbonate of lime, frequently more than two inches thick, and either detached within the beds of clay, or adhering to the limestone beds, like the thinner crusts attached to the limestone of the Weald clay. The bivalves, principally Cyclades, of which a great part of the Purbeck stone is composed, are not less numerous, and commonly much more distinct, in the slaty clay of the “‘ rubbish” between them ; which cannot be distinguished from the clay with Cyclades (‘‘ Shab”) of the limestone pits on the north-west of Battle in Sussex. The “Slate”, a coarsely fissile limestone at the lowest * A very remarkable appearance, which I am at a loss to explain, was observed by Mr. Bab- bage and myself in 1824, on the back, or top of the Purbeck strata, at that time exposed on the shore between the town of Swanage and Peverell Point. The surface there, which dipped at an angle of 7° or 8° towards the north, was depressed in some places into nearly circular pits or cavities, from 4 to 7 feet in diameter, and about a foot deep in the middle,—as if the beds had been forced in by a violent blow; the depressed surface being divided by irregular but nearly concentric cracks, which were filled with white sparry carbonate of lime. Three of these depressions were visible ; two of them about 6 feet apart, one of which was 74 feet, the other about 43 in diameter at the outeredge. A third, about 10 paces to the west of these, was of smaller dimensions. 2E2 210 Dr. Firron on the Strata below the Chalk. part of the Purbeck series, was formerly much quarried for roofing, in the hill above Tillywhim, and near the south coast of the peninsula: and there, as well as in the corresponding beds of Portland and the north of Weymouth, I have found in it casts in calcareous spar of one or more species of Cypris. (105.) Portland Stone.—This formation first appears upon the coast be- neath the Purbeck strata at Durlstone Head, and rises slowly in the rocky cliffs on the west of Tillywhim to a point about midway between Winspit and St. Alban’s Head, where it is succeeded by the Portland sand. The stony strata there retire as they rise from the shore, and occupy the margin of an irregular space thence to Gad Cliff, where they return to the coast and sink under the sea: so that between the extreme points of Durlstone Head and Gad Cliff (or rather Worbarrow Knob, a rocky hummock on the west of that place), a real curvature combined with the general inclination of the strata towards the north, which is in some places very rapid, has caused an extensive disclosure of the lower beds, excellent sections of which are visible on the west of St. Alban’s Head. ‘Phe component strata of the Portland stone in Purbeck, agree with those of the Isle of Portland, which have been described by Mr. Webster. (106.) Portland Sand.—I propose to give this name to a group of strata which holds the place of that mentioned by Mr. Conybeare as occurring beneath the equivalent of the Portland stone at Shotover Hill in Oxfordshire, and in Bucks; and which in the interior contains a large proportion of sand, including green particles, ascertained by Dr. Turner to be of the same composition with those of the green sands beneath the chalk*. I have found a similar group abounding in green matter, and containing, as at Shotover, very large concretions of grit, in a corresponding place in the lower Bou- lonnoist, where a great part of the formation consists of sand. But on the Dorsetshire coast, and I believe, in the Vale of Wardour also, the beds are generally of a dark grey colour, more coherent, less sandy, and the calcareous matter which they contain, is more uniformly diffusedt. The group is certainly of sufficient importance to require a separate name, and that of Portland sand, while it expresses the more usual character, indi- cates also its intimate connexion with the Portland stone. On the other hand, it graduates into the Kimmeridge clay beneath; and its position seems to be * See above, (10.) note §. t Geol. Soc. Proceedings, vol. i. pp. 9 and 27. t{ On the west of Upway, however, near the coast of Dorsetshire, nearly half the substance of this stratum is made up of grains of green earth; and along the whole line of the formation in that quarter, the prevailing character is that of siliceous sand and green earth.—See Dr.Buckland’s and Mr. De la Beche’s Memoir, in the preceding part of this volume: p. 20, and note. Dr. Pyios on the Strata below the Chalk. 211 analogous to that of the sand and subcalcareous grit which occur between the Oxford oolite and Oxford clay,—the inferior oolite and the lias clay : ?? The whole mass of strata deposited in the first instance, having been in all these cases, sand and mud; the upper part of which abounding more in calca- reous matter, was subsequently converted into stone, and the lower more or: less concreted into nodular masses of calciferous grit, in proportion to the quantity of carbonate of lime diffused through it. In the Isle of Purbeck, the Portland sand first rises above the sea about midway between Winspit and the point of St. Alban’s Head, and is disclosed by denudation on the north of that remarkable promontory, in a ravine called Pier Bottom, near which place the Kimmeridge clay appears to rise on the shore. A good section of the sand is visible at Emmet’s Hill, a ridge capped with Portland stone, between Pier Bottom and Chapman’s Pool; and the group may be traced thence, beneath a capping of stone, all round the inflections of the high ground from Bottom Farm, by the prominences called Encombe Point (or Hound’s Tout), and Swyre Head, through Kimmeridge, to Gad Cliff, where it declines along with the stone and sinks again under the sea. Its relative place and its effect in modifying the surface, are well seen in the amphi- theatre of high ground which nearly encircles Kimmeridge Bay ; of part of which Pl. X. a. No. 9, and X. b. fig. 6, are illustrations: the summits all around consisting of Portland stone, and the rapid grass-covered slope beneath of this sand, resting upon a tract comparatively flat and uniform, which is occupied by the clay of Kimmeridge. The sand again makes its appear- ance on the coast west of Purbeck, in a small portion distinguishable by its bluish grey colour, beneath the rocky cliffs called Horsewalls, which form the most prominent part of the shore between Lulworth and Durdle Cove. In the complex and disturbed tract on the north and west of Whitenore, the Portland sand is found wherever the superior strata rise high enough to dis- close it; and in the Isle of Portland it everywhere accompanies the stone, and has the same characters as on the coast of Purbeck. The following is a List of the strata at Emmet's Hill, immediately on the north of St. Alban’s Head :—PI. X. b. figs. 5 and 6. Feet. 1. Portland stone, with layers of flint near the bottom, forming a shattered and inac- cessible precipice at the top of the cliff .............-. ‘ geacdsare 50 to 40 feet 2. Portland sand. Soft stone, or marly coherent sand, with a rugged external surface ] of a yellowish grey or brownish colour; but in the recent fracture, of a dark bluish or greenish grey. It includes concretions of firmer consistence. In a bed of stone 25 to 80 uv of the same description at the cross-roads above Kimmeridge Farm, which seems to belong to the same place in the series, Trigonia clavellata, Ammonites giganteus, RNR AE ERIE SATE MNO iol ««) Scie: a) + dhe shite ls Ate yee» . -80—90 (110.) Isle of Portland *.—The coast of Dorsetshire, from the promontory of Whitenore to Lyme Regis, forms the subject of a memoir by Dr. Buckland and Mr. De la Beche, which is printed at the commencement of the present volume: I shall not, therefore, give any general description of it ; but having been favoured with a perusal of that valuable paper, I find it necessary to mention some details respecting the appearances observable near the junction of the Purbeck and the Portland formations, with a view to a comparison of this part of the series in the interior, with that of the coast in England, and in the Boulonnois. Mr. Webster, in his account of the strata above the Portland stone, has described a remarkable bed, called by the quarry-men the “ Dirt” or “ Black dirt’, which he found to contain portions of the trunks of silicified trees; one of which he himself saw standing upright, and divided at the lower part, “so as to give the idea of roots”. He states that these trunks were not found in any other part of the series ; but not having seen any fossils in the beds above the Portland stone, he expresses liimself with caution as to the place of the boundary between the Purbeck strata and the oolitic group beneath * The substance of this and the following sections, to (116.) inclusive, was read before the Geological Society on the 13th of May, 1835; and is inserted here by permission of the Pre- sident and Council. T Geol. Trans., 2nd Series, vol. ii. p. 39, &c.; read Nov. 1824. I 218 Dr. Firron on the Strata below the Chalk. it ; intimating, however, that it will probably be found at the top of the chert or flint in the upper part of the oolite. Some years afterwards Dr. Buckland described specimens of a new family of fossil plants from the “‘Dirt-bed” above mentioned; to which, at the suggestion of Mr. Brown, he gave the name of Cycadeoidee *, but which M. Adolphe Brongniart, adopting a different system of nomenclature, soon after formed into a genus which he called Mantellia Ff. Dr. Buckland was subsequently led to infer that the “ Dirt-bed”’ was actually the soil in which both the silicified trees and the Cycadeoidee had grown: and in a paper read before the Society in 1830 {, now published in this volume, he and Mr. De la Beche have stated several facts respecting that remarkable bed ; adding in a note§ that Professor Henslow had ascertained the existence of two other beds of dirt (or of clay with carbonaceous matter) below it; one of them about seven feet beneath, the other about two feet still lower down. On visiting the Isle of Portland last summer, with a knowledge of these facts, I found that the clay, or “dirt”, below the Cap, (the upper appa- rently of the two additional clays described by Professor Henslow,) itself contains Cycadee, in an upright position, and to all appearance in the places where they had grown; and I obtained also some new evidence respecting the character of the beds immediately above. (111.) The following are a sketch and enumeration of the strata exposed at the time of my examination, in the quarries about the middle of the island, and westward of that point ; which I was enabled to revise during a second visit to Portland, when I had the satisfaction of being accompanied by Mr. Brown. The whole mass of the strata which now form the Isle of Portland must have been subjected to great disturbance long before the surface acquired its present configuration; by which the vertical rifts, from a few inches to some feet wide, were formed, which are now observ- able in the face of the quarries, passing indiscriminately through both the Purbeck and Portland strata, and having in many instances produced displacement in the separated portions: and this at such distances from the present coast of the island, as to prove that no recent disturbance or subsidence of the sea-cliffs has had any share in producing them. Yet it is remarkable that the surface over these disjointed beds is now perfectly uniform; the inequalities occasioned by the sinking and fracture of the slaty Purbeck strata near the top having been com- pletely filled up to a level by rubble and vegetable soil. In one place a fissure between two and three feet wide cuts down, almost vertically, through about thirty feet of stony strata, * Geol. Trans., 2nd Series, vol. ii. p. 395; read June, 1828. + Prodrome d'une Histoire des Végétaux Fossiles, 1828, pp. 92 and 96. + Proceedings of the Geol. Soc., vol. i. p. 217. et seq. § Page 16. of the present volume. Dr. Frrron on the Strata below the Chalk. 219 and still retains its width at the bottom. The thin slaty beds of the Purbeck are in this instance disturbed and bent, downwards and towards the fissures, to some feet on both sides ; but the soil above is perfectly level; and in some other cases, where two or more cracks are near each other, the intermediate masses are still more contorted and displaced. It will be shown hereafter that appearances of the same kind are observable in the Portland-stone quarries in Wiltshire, Oxford- shire, and Bucks. Section of one of the PorTLAND Quarrizs. 1834. 1. Vegetable Soil ...ccsccsscseenereceeeeeees BRU DMCUSIGLE.: \icsddededes's Ue. lade birds dds seis . Clay, or “ Dirt” ...... ceereecss soou0banS — . © Bacon-tier’’...cccecccveccceresess ae. tee Soft Burr” ..csccoceoeeee Peussecenas cote © Black Dirt”? scsccsecessseseveseeceesers = SM Ao S > Purbeck Strata (Freshwater). © 2 aS} oe eeeeees 10. “ Dirt”, with Cycade@ .......sseeree. 11. “Shull-Cap” .....+.. Seecseecs scnes nome NORMAN GU seal loses te omestens sens shecsiiecereas. 14. “ White-Bed”’........ Bae eaicsislvieves nas Bottom of the Quarry. Portland (Marine). 2. The “‘ Slate” of the preceding section is nothing more than the coarsely fissile limestone which pervades the whole of the Purbeck formation, but at the lower part less frequently alter- nates with clay. Its thickness varies in different parts of the Isle of Portland, from about fifteen to less than six feet. In some places it includes small veins of rhombic carbonate of lime in minute crystals; but has commonly the general aspect and flat conchoidal fracture of freshwater limestone. On a close examination these beds are found to contain the remains of one or more species of Cypris*; and I saw a few traces of small Modiolz, like those which abound in the corresponding strata in the Vale of Wardour and Buckinghamshire. The Cypris, in fact, is found in all the beds above the oolite (13. of the Sketch above); so that no doubt remains respecting the boundary between the Purbeck and the Portland formation below. Nothing can i with few exceptions, casts only of the interior of the crusts are obtained here, it is difficult to determine the species of these fossils. Mr. Sowerby is disposed to refer most of them to a ri Bperics, C. tuberculata, Pl. XXI. fig. 4.; and a few perhaps to the C. Valdensis, Pl. XXI. g.1.; both of which abound in the corresponding part of the Purbeck formation in the interior. 220 Dr. Firron on the Strata below the Chalk. be more remarkable than the immediate contact of these two groups; the upper consisting of freshwater limestone with few fossils; the lower distinctly oolitic, with fossils in great number and variety, and all of them marine*. 3. Besides the “* Black Dirt” (No. 8.), or, as it is usually called by the quarry-men, “ the Dirt”, two or more thin courses of clay occur above the Cap: one (No. 3.), about two inches thick, between the Bacon-ledge and the Slate; another (No. 5.), about an inch in thickness, dividing the former from the 4sh. The number, however, of these thin beds of clay varies in the different quarries ; and, in general, it may be said that such alternations with the limestone are not unfre- quent. They all bear the name of “ Dirt”, and are more or less mixed with fragments of stone and with carbonaceous matter; but contain commonly much more clay than either of the two beds hereafter mentioned, which include the remains of plants. 4. The Bacon-tier consists of calcareous slate alternating in some places with thin beds of sand. It is from 2 feet to 25 feet in thickness. 6. The Ash is a soft fissile limestone, like the last-mentioned bed, from which it is easily sepa- rated in working. In general it is from eighteen inches to two feet thick, and is closely connected with the Soft Burr, 7. When the incumbent beds are removed, it generally exhibits an uneven surface, with numerous bosses or prominences, enveloping the broken tops of the trunks, which stand upright in the dirt-bed below, as described by Dr. Buckland and Mr. De la Beche. Oblong depressions also are frequently observed on the surface of the Ash, called by the quarry- men “graves”, the origin of which it is not easy to explain. 7. The Burr of the Ash, or Soft Burr, is between two and three feet thick. It has obviously been deposited around the lower part of the petrified trunks, and is always separated from them by a small space, at present occupied by the carbonaceous matter produced by the decomposition of part of the tree: and this is the case also where the Ash envelopes the top of the broken stumps. The junction of these two beds, around the trunks, is often attended with some very interesting appearances, for an account of which I refer to a note by Professor Henslow in the preceding part of this volume t. 8. The “ Dirt”, or “‘ Black Dirt”, in Portland is separated from the stone, both above and below, by well-defined surfaces; while some of the other beds of clay, or dirt, pass by gradation into, or adhere closely to, the stone which adjoins them. It is from twelve to eighteen inches thick, and differs from all the other beds alternating with the slaty limestone, in containing large worn fragments of stone {, from three to nine inches im diameter, in such numbers that the whole deserves the name of coarse gravel. With these are mixed coarse carbonaceous matter and minuter fragments of stone ; but seldom, in the Isle of Portland, any continuous or cohesive clay :—the carbonaceous matter arising, no doubt, from the remains of vegetables, and being most abundant immediately around the trunks and Cycadez, which this bed includes, or supports. At Upway, on the north of Weymouth, the representative of the “‘ Black Dirt” likewise con- tains petrified trees: but the pieces of stone which it includes are few and much smaller, and it approaches more nearly to the usual form of vegetable mould, or of clay. On the north-east of Weymouth its place can be distinctly recognised in the cliffs between Lulworth Cove and Wor- * Compare what is here stated, with the account of the junction of the marine beds with the top of the Wealden, at Atherfield in the Isle of Wight (supra, p. 196, last lines). + Pages 16. and 17. { In these fragments I could find no fossils ; Mr. Webster considers them as belonging to the lower beds of the Portland stone. Dr. Firron on the Strata below the Chalk. barrow Bay; and in the Isle of Purbeck, beneath Wor- barrow Knob. In the loftier cliffs at Gad Cliff it is not accessible; but among the fallen ruins on the shore were some portions of silicified trunks. Between Tillywhim and Durlstone Head a cavity can be perceived in some places, in the part of the cliff where this bed might be expected. Petrified Trees.—The portion of the trees left standing above the dirt-bed in Portland, is frequently more than three feet in height: and one instance was mentioned to me in which six feet of a trunk stood thus in the up- right position. I did not see any case in which the roots penetrated into the Cap below; but observed several fis- sures in the top of that bed, some of them coated with a crust of stalactitic carbonate of lime. In one instance a prolonged branch of the root had evidently been bent out of its course by meeting the Cap, and was continued ho- rizontally along its surface for several inches: the quarry- men said that such cases were not uncommon, and that the roots sometimes ran along the top to a much greater distance, but never penetrated the Cap itself. Some very fine specimens of the silicified trunks had been found not long before I saw them ; one of which had been judiciously restored, by joining the fragments and placing the whole erect against the wall of a house. The total height from one extremity to the other was above 205 feet; the diameter of the stem where the roots went off, about113 inches. The trunk was nearly straight and undivided for about 17 feet, and the branches slight in comparison with the main stem. A still finer specimen, found, I believe, near the same place, in Dungeness Quarry, and at the same time with that just described, has been brought to London for sale; and I am enabled, through the favour of Mr. Freeman, in one of whose warehouses the specimen was deposited, to insert a representation of it, from a drawing made by Mr. Sowerby, after careful admeasurement, as it lay horizon- tally, the fragments which had been separated appearing to fit exactly. The total length, from the extremity of the roots to that of the branches, was about 234 feet, and to the bifurcation nearly 20 feet. The roots and undivided portion of the stem to the first crack, occupied about 2 feet. The situation of the other cracks, of which there are fourteen or fifteen, is expressed in the figure. The trunk is compressed throughout ; the branch on the right, * especially, having been much flattened near its extremity. SSS=s —S ~ —s" —<——= ———S—-= = = 222 Dr. Firton on the Strata below the Chalk. At 2 feet from the extremity of the root, the greatest diameter is 183 inches, the transverse diameter only 125; at 4 feet, the diameters are 165 and 114 inches; at 11 feet, 143 and 112; and at 18 feet, 15 and 93 inches. The right branch at its extremity, 11 and 43 inches. The specimen here represented is much like that which is preserved in the Isle of Portland, in general aspect and proportion; but many of the stumps which I saw standing in the quarries were much larger. One that I measured,—of which 5 feet stood upright from the lowest point of the roots to the top of the broken trunk,—was 2 feet in one of its diameters, and 6 feet 9 inches in circumference. Another, 5 feet 10 inches in total height, was about 2 feet 10 inches in diameter, and 9 feet 4 inches round; and I was assured that others had been found of much greater thick- ness. All the larger trees that I saw were in the quarries on the north-west of the church; one of which afforded also the specimen represented in the wood-cut, with several large Cycadez. In many places I saw large branches lying prostrate, and partially immersed in the Dirt;—one of them, above 3 feet long, within 2 feet of another portion, about 10 feet in length, and in the same direction with it*. From the evidence afforded by thin transparent slices, both of the transverse and longitudinal sections, which have been examined under the microscope+ by Mr. Brown, the fossil trunks of Portland are found to possess the characters uniformly belonging to coniferous wood: but it must be observed that these characters are not absolutely confined to Conifere. The Cycadee found in the “ Black Dirt” are generally from 9 inches to a foot in diameter, and about 9 or 10 inches high. I myself saw but one specimen, which had been recently taken from its place, in this bed; and it was stated by the quarry-men that on the west of the main road from Chiselton to the church, they have been found, or noticed, only in the Dirt above the Cap; while on the east of the road, as I shall presently mention, they are certainly found below that bed. In the eastern quarries, indeed, the workmen, who had not seen them elsewhere, asserted that the Cycadez were never found above the Cap ; but this I found afterwards to be incorrect. In both situations, they are much less common than the coniferous trunks. 9. The “ Cap” is the thickest of all the strata above the Portland stone ; the average thickness being about 8 feet, the extremes 6 and 9 feet; of which, in some cases, about 18 inches at the top are easily separable from the rest. When recently exposed, the whole of the remaining mass is continuous, and consists chiefly of uniform limestone of a light brownish or drab colour, with a flat conchoidal and splintery fracture ; but it cannot be used for building, as, in the workman’s phrase, “ it will not square.” About the middle and towards the lower part it is spongy, or cavernous, including tortuous cavities surrounded with botryoidal carbonate of lime; and it has * It would be desirable to ascertain the direction in which the prostrate stems lie, with respect to the meridian, and to the roots and portions of the trunk remaining upright, in order to deter- mine whether they were overthrown by an uniform current of wind or water. + One of the longitudinal slices examined by Mr. Brown was broken from the extremity of the left branch of the tree represented in the annexed wood-cut. The process by which these slices are prepared for the microscope has recently been carried to great perfection by Mr. Nicol of Edinburgh. It consists in attaching a thin polished slice of the fossil, separated by the ordinary method, to a piece of plate glass, by means of a uniform cement; and then grinding it down as far as possible on the lapidary’s wheel. In this way tran- sparent slices have been obtained, which exhibit the internal structure of fossil wood with beau- tiful distinctness, and show the extreme delicacy with which the original vegetable structure has been preserved during the petrifactive process. ‘Two papers by Mr. Nicol on the structure of the recent and fossil Coniferze are published in the Edinburgh Philosophical Journal, vol. xvi. 1834, pp. 137 and 310; and a third in the Report of the Fourth Meeting of the British Asso- ciation for the Advancement of Science, 1834, p. 160. Dr. Firron on the Strata below the Chalk. 223 altogether a very strong resemblance to the Z’ravertine of Italy. The top is sometimes penetrated by conical and nearly vertical cavities, encrusted with a yellowish stalagmitic coating. In the Isle of Portland it is compact and continuous at the bottom ; but in other places the lower part, and in some cases the whole, is resolved by decomposition into slaty strata. At Upway, on the north of Weymouth, the lower portion of the Cap consists of a series of thin beds of limestone alternating with very thin courses of clay. In Portland, even where most compact, it contains a few casts of a small species of Cypris; and these seem to be more frequent (perhaps because more easily detected) in the more fissile representatives of the bed at Upway and Bacon-hall. In one or two instances I found in it obscure traces of small univalves like those of Garsington and Combe Wood near Wheatley in Oxfordshire. In a nook or recess, called by the boatmen Bacon-hall*, upon the coast about a mile east of Lulworth Cove, the section of this part of the series was as follows: a. “Black Dirt” of Portland. b. Cap, consisting of: i. Slaty limestone, divided by dark lines of stratification; which at the lower part become more distinct, and at last take the form of ii. ii. Dark grey indurated slaty clay ; one bed of which is nearly 2 inches thick.—Beneath it is iii. A thin flake of soft whitish limestone. e. Dirt. An indurated bed, of a light brown colour, 4 to 5 inches thick; composed of argil- laceous (and carbonaceous) matter, and including small fragments of stone. d, (Skull-cap?) Limestone, somewhat botryoidal ; the more compact portions having a flat con- choidal fracture ; 2 to 6 inches thick. e. Portland stone, abounding in the characteristic fossils, and including, about 6 feet from the top, a band of flint, in detached masses, about 4 inches thick. 10. “ Dirt” below the Cap. Immediately below the Cap in the Portland quarries, and conse- quently separated from the “Black Dirt” by a thickness of about 8 feet, is another bed, also called “ Dirt” by the quarry-men, from 2 to 6 inches thick, but more uniform in its texture than the former, resembling coarse silt or indurated loam, and containing in some places small frag- ments of stone, but never such large masses as the ‘“ Black Dirt”. This lower bed deserves especial notice, from its affording specimens of Cycadez, in an upright position, and partially immersed in it, as if they had grown there. Of these I myself saw two in their original place at a quarry called “‘ the Wheat-croft ”, on the east of the ‘‘ Traveller’s-rest” ; one of them about six inches high, surrounded with the Cap, into the lower part of which it projected above the Dirt for about half its thickness, so that it was necessary to cut away the stone to take it out; and from the existence of many other specimens in the debris of the same quarry, which the workmen assured me had all come out of this bed, I believe them to be of frequent occurrence. Among the latter was one of unusual size, larger indeed in its horizontal dimensions than any other specimen I have seen, either from this bed or the Dirt above the Cap{. This, from its flatter form, may possibly * Notwithstanding the apparent firmness of this rocky coast, great changes are constantly in progress there. An old boatman who conducted me, without having been asked a question, expressed in very strong terms his surprise at the alterations produced, to his own knowledge, within the last thirty years. + The specimen is now in the museum of the Geological Society. It is of an irregular figure approaching to an oval, and measures 20 inches by 19 in its horizontal diameters, the vertical thickness varying from 63 to 9 inches. Another less perfect specimen which I saw in the same quarry, was about 9 inches thick, and its diameters not less than 34 and 30 inches. Of the Cy- cadez from the Upper Dirt-bed very few exceed 10 inches, in height and horizontal diameter. The largest I have seen is nearly 10 inches high, and about 12 in diameter near the bottom. VOL. IV.—SECOND SERIES. 26 224 Dr. Firron on the Strata below the Chalk. belong to the species nidiformis of Adolphe Brongniart (Cycadeoidea megalophylla of Dr. Buck- land): but it deserves inquiry whether the specimens in the lower bed agree in all respects with either of those found in the upper one. In the Isle of Portland, no trees have hitherto been found in this lower dirt; which, from its smaller thickness, might seem to have been less adapted to their production than the upper one. But if I can rely upon a single observation, part of a prostrated trunk exists in the Dirt below the Cap, in a section exposed on the west of the road leading from Upton (on the main land of Dor- setshire) to Poxwell. T came to this conclusion from observing that the inclined stratum of lime- stone over the bed including this specimen was distinctly botryoidal, and of great thickness,—two characters which accord with those of the Cap; while the stone below it contained Portland fossils. But I saw no Cycadez in the bed at this place. 11. “ Skull-Cap.” The thickness of this bed in Portland varies from one to three feet, and it frequently swells out suddenly from 15 or 18 inches to double that thickness, and returns as rapidly to its previous dimensions. It is less uniform than the Cap, and sometimes has an obscurely conglomerated appearance, but, like that bed, consists of freshwater limestone, and is in some places botryoidal. It includes also, as Mr. Webster has stated, small cavities coated with minute rhomboidal crystals of carbonate of lime, like those found in the slaty beds above. 12. At the lower part, the “‘ Skull-Cap” is closely attached to, or passes into, a seam of argil- laceous matter, sometimes not more than half an inch, and seldom more than 24 inches thick, by which it is separated from the Portland stone. ‘This seam appears never to be wanting in these quarries, and is much more uniform than the Dirt immediately above the Skull-Cap, which is very unequal in thickness : in some instances it is incorporated with, or adheres very closely to, the top of the Portland stone *. 13.and 14. The top of the Portland series consists of very fine-grained oolite, resembling the roe of fishes, and of a very light brownish hue. With the oolitic particles, other rounded frag- ments, less regularly shaped, are mixed and united by a calcareous cement, so that the whole compound is very like the recent conglomerates which abound on the shores of New Holland, of many of the Indian Islands, and of Bermuda; especially resembling the newly-formed masses of the last-mentioned islands, described by Lieut. Nelson in a paper lately read before this Society +. This oolitic portion is seldom more than four inches thick, and passes at the lower part into dark grey flint, in irregular concretions, which form an interrupted range near the top of the bed, and include the same petrifactions (but silicified), with those which abound in the limestone imme- diately around and below them. The stone below the flints, to a distance of from two to four feet from the top, is called ‘* Roche” by the quarry-men, and is essentially continuous with the lower part of the bed; but it contains so many casts of shells (of which, indeed, it is almost entirely composed), as to be useless for the purposes of building, and is therefore always sepa- rated in the quarry. The remainder of this stratum, about 8 feet thick, is known in the island as the ‘‘ White-bed”, and is that which is now, almost exclusively, quarried for the market under the name of Portland stone. This and the lower strata of the formation, which are not worked at present, have been already described by Mr. Webster. Among the fossils of the White-bed in Portland, are a Corbis ?, Cytherea parva, Lithodomus, Pecten lamellosus, Perna quadrata, Plicatula, Terebra Portlandica, Trigonia gibbosa, T. incurva. * The existence of Cycadez within three feet of the Portland beds being certain, it deserves inquiry whether they may not occur also in this lower and thinner Dirt-bed immediately above the stone. ¢ Proceedings, vol. ii. p. 81. Dr. Frrron on the Strata below the Chalk. 225 At Upway, this bed, or one of those immediately below it, is beautifully white, like chalk, and contains nodules of dark grey flint, frequently hollow and lined with quartz crystals, which it would be impossible, without attending to their fossils, and their geological position, to distin- guish from those of the chalk. One of the characteristics of the best Portland stone, both of this and other beds, is that the blocks ring very distinctly under the hammer, giving out a clear and agreeable note. (112.) It appears, therefore, that on the Dorsetshire coast the Portland strata are everywhere succeeded by a series of beds of freshwater limestone, alternating with beds of clay, or of a compound called “dirt”, which con- tains carbonaceous matter and fragments of stone; and that two at least of these “dirt’’ beds, the first about three feet, the second about twelve feet above the top of the Portland series, include the remains of plants, which grew in the places where they are found ; nor is it wholly improbable that similar remains may hereafter be discovered in some of the other and thinner beds of “dirt”’. A point which Mr. Brown considers as well deserving of remark is, that the only remains of vegetables hitherto found in these strata, under the circum- stances above described, belong to two nearly related families, Coniferee and Cycadex, which have lately been regarded as forming a distinct class, cha- racterized not only by the greater simplicity of the parts of fructification, but also by some peculiarities of internal structure, and thence have been con- sidered as intermediate between Phanogamous, and Cryptogamous or Aco- tyledonous plants. Another striking fact connected with the remains included in the “ dirt beds” is, that they are composed almost entirely of silex, though surrounded either by limestone or by the mixed components of the dirt itself. The cavities in the petrified trunks are lined with minute crystals of quartz; and Dr. Prout, who has been so kind as to examine specimens of the coniferous wood taken from the confines of the Purbeck and Portland formations, in Port- land, and other places to which I shall refer hereafter,—finds them all to consist almost wholly of siliceous matter, with very slight traces only of carbonate of lime and of iron; some of the darker parts of a specimen, from the Vale of Wardour containing also bituminous matter. The Cycadeew likewise are described by Dr. Buckland as being almost entirely siliceous, “‘varying from “coarse granular chert to imperfect chalcedony” *. (113.) The great abundance of small, worn, fragments of shells and stone at the top of the Portland formation, is what might have been expected on the surface of an island of small height, just protruded from‘ the sea, * Geol. Trans., 2nd Series, vol. ii. p. 398. 262 226 Dr. Firron on the Strata below the Chalk. perhaps so gradually as to have been near the surface for some time before its emersion. The next step, in the series of revolutions which produced these strata, must have been the diffusion of fresh water over the new land, from which the “Skull-cap” was deposited; and this was followed by a drying up or retirement of the water, so as to disclose and convert into dry land the lower of the two beds of clay, or dirt, which now contain the Cy- cadee. Iam not sufficiently acquainted with the habits of the recent plants of this family, to form any opinion as to the length of time necessary for their acquiring the size of the specimens now found petrified, nor to judge how far the rapidity of their growth would be modified by climate: but all the known species are said to be of slow growth; and being found at Japan, as far north of the equator as 40°, and at the Cape of Good Hope and Port Jackson, in the southern hemisphere, about latitude 34°, they cannot be considered as strictly tropical productions. A second submersion of the surface in fresh water must have followed the production of the Cycadez in this lower bed, from which the “‘Cap”’ was accu- mulated, to a thickness of between seven and ten feet, and the ‘* Black Dirt” deposited above it; anda third, and apparently more durable submersion, still in fresh water, must afterwards have taken place, by which the “slate” and a great part of the Purbeck strata were produced. In this last case the water seems to have been at first unmixed, but to have become after a time ac- cessible to the sea; since not only does the Purbeck formation contain a thick bed of oyster-shells, but thence upwards, throughout the Wealden, oysters are found, in strata which in several instances alternate with others abounding in freshwater shells. (114.) Mr. Lyell has pointed out the resemblance between the geological events which produced the strata of Portland Island, and those which are known to have occurred at the mouth of the Indus, from the effect of suc- cessive earthquakes connected with volcanic eruption*; and it is clear that all the changes above supposed to have taken place,—depression and elevation of the land, through comparatively small depths and at different periods, with alternate though irregular submersions both in salt and fresh water,—have been produced in that region, not only within the period of tradition, but many of them so recently as in 1819. Among other facts, it is stated, that for some years after the earthquake of Cutch, which happened in that year, “the withered T'amarisks and other shrubs protruded their tops above the “‘ waves, in parts of the lagoons formed by subsidence, on the site of the * Principles of Geology, 4th edition, vol. ii. p. 237-242. Dr. Firron on the Strata below the Chalk. 227 “village of Sindree and its environs. Every geologist,” Mr. Lyell justly remarks, “will at once perceive, that forests sunk by such subterranean “movements may become imbedded in subaqueous deposits both fluviatile “and marine, and the trees may still remain erect ; or sometimes the roots “and part of the trunks may continue in their original position, while the “currents may have broken off or levelled with the ground their upper “ stems and branches*.” (115.) It is very desirable that the examination of the Portland quarries should be repeated from time to time: for as the valuable stone lies deep in the series, and it is necessary, for the purpose of obtaining it, to remove the whole of the incumbent matter, the features described in this paper are con- stantly undergoing a process of destruction ; while, on the other hand, new facts are continually brought into view, which are lost if not observed at the moment. ‘The greater part of the phenomena described by my predecessors had thus disappeared when I visited the island, and a few hours might have removed the fossils which I observed in the bed below the Cap. Geologists may assure themselves that the trouble of a journey to Portland will be most amply rewarded ; since few places, it is probable, in the world, exhibit with such distinctness and in so small a space, phenomena of more extraordinary interest, or of greater importance to theory. _ (116.) The strata, abruptly cut off by the sea on the west coast of Port- land, are found no more in that direction in England f ; nor do they occur on the opposite coast of France immediately on the south, which consists of the primary masses of Guernsey, Auvigny, and the main land about Cherbourg. On the east of the last-mentioned promontory, where they might be expected to appear among the beds beneath the chalk between the mouth of the Seine and Bayeux, their presence, I[ believe, has not been distinctly ascertained. And on the north of the Seine they must be far below the level of the English Channel, at least as far as Etaples, where the rocks upon the shore consist of chalk with flints i sitw. The Portland beds, with a thin covering of the lowest Purbeck strata, rise from beneath the chalk and green-sand on the south of Equihen in the Lewer Boulonnois, and are found all along the cliffs thence to the north of Cape Gris-nez, where they again give place to the superior strata. They have not yet been discovered, so far as I am in- formed, further to the north in Europe. * Principles of Geology, 4th edition, vol. iv. p. 274. + The most western point where the Portland strata have been found in England, is on the main land near Portisham, twenty miles west of Lulworth Cove. See p. 15. of this volume. 228 Dr. Fitton on the Strata below the Chalk. (117.) List of Fossils from the Beds below the Chalk, on part of the Coast of DorseTsHiRe. [Upper Green-sand. | Cirrus depressus. Worbarrow Bay. Exogyra conica. Face of the Hill top, W. of Osmington Mill. E: levigata. Worbarrow Bay. Gryphea vesiculosa. Swanage Bay, under Ballard Hill. Hill top, W. of Osming- ton Mill, with stems of Siphonia. Ostrea, new. Between Ham Cliff and Osmington Mill. Pecten asper. Swanage Bay. Hill top, W. of Osmington Mill. Je orbicularis. Swanage Bay. W. of Osmington Mill. P— quadricostatus. Swanage Bay. Worbarrow Bay. P quinquecostatus. Swanage Bay. P A very convex variety (young ?). Worbarrow Bay. Serpula antiquata. Swanage Bay Siphonia. Stems. Worbarrow Bay. Hill top, W. of Osmington Mill. Terebratula pectita. Swanage Bay. Vermetus concavus. Swanage Bay. Osmington Mill. [ Gault. ] Mya mandibula. Punfield*, Swanage Bay. [ Weald Clay. | Cyclas media. Punfield. In thin beds of bluish limestone, encrusted with fibrous carbonate of lime (‘ cone in cone’’). C. membranacea. Punfield. Cypris tuberculata. Pl. X XI. f.2. Punfield. C Valdensis. (C. Faba, Min. Con.) Pl. XXI.f. 1. Punfield. Exogyra? Punfield. In brown clay. Melanopsis? attenuata. Pl. XXII. f. 5. Punfield. In blue clay. M- ? tricarinata. Pl. XXII. f.4. Punfield. In blue clay. Ostrea. A plicated species. Punfield. Ina bed of stone subordinate to the Weald clay, the greater part composed of shells; with a striated bivalve (a Cardium ?). O——. Asmooth species. Punfield. In greenish sandy stone, coated with fibrous carbonate of lime. Paludina acuminata. Punfield. Pp. elongata. Punfield. With Cyclas media, in greenish grey sandy clay. Unio. Punfield. In thin, slaty, dark bluish clay. Saurian Rertites. Fragments of bone of a Saurian; and the teeth apparently of a Crocodile. Punfield. Woop. Coniferous, silicified, in fragments. Punfield. * Punfield is a small nook or recess on the north of Swanage Bay, between the ridge of Bal- lard Down and the sand-cliffs. Dr. Firron on the Strata below the Chalk. 229 [Hastings Sand. } Cyclas media. Sand-cliff between Swanage and Punfield. In nodules of clay-iron- ore, with Paludine; also in hard subcalcareous grit. Paludina elongata. Same place and situation. Unio. One or more species occur in the concretions of grit within the sand-beds, be- tween Punfield and the town of Swanage. Saurian Rerrives. Large bones of the Iguanodon have been found loose on the shore at the foot of the sand-cliffs near Swanage, by the Rev. T. O. Bartlett; (see Dr. Buckland’s Notice, already referred to*;) but their precise place in the cliffs is still to be ascertained. Woop. Large portions of the stems of silicified coniferous trees have been found on the shore under the sand-cliffs in Swanage Bay, by the Rev. T. O. Bartlett. The stone into which they are converted is of a very dark brown colour, re- ceives a fine polish, and does not effervesce with acids. [Purbeck Strata. ] Corbula alata. Pl. XXI.f.5. Numerous in slaty limestone, at Upway, on the north of Weymouth, with Cyclas media. Durlstone Bay: Isle of Purbeck. Cyclas media. Pl. XXI. f.10. This fossil occurs throughout the series of Pur- beck strata, and is one of the most abundant fossils of the formation, some of the beds being almost entirely composed of it. Upper beds of the series, at Peverell Point, and Durlstone Bay, At Upway, west of the road, 50 feet above the “ Cap”. angulata. Pl. XXI1.f. 12. In “ Quarry vein”, one of the strata worked for stone, near Swanage. In hard stone resembling the lower chalk, when indurated ; Durlstone Bay. Of large size, in slaty stone, at Upway, N. of Weymouth. Cypris.. Casts, in transparent carbonate of lime, of the interior of one or more small species of this genus, occur in great abundance in the beds of slaty limestone, which frequently includes rhombic crystals of carbonate of lime, at the bottom of the strata above the “‘ Dirt bed”’, as well as in the “ Cap” over the Portland stone : but it is difficult to determine the species, as the external surface is commonly wanting. Ina few instances an exterior spine or prominence, like that of Cypris « spinigera, P|. XXI. f. 3., is perceptible ; and in others the protuberance at the end of the valves, represented in the figures of C. Valdensis, Pl. X XI. f. 1., was observed. It is not, however, improbable that some of the casts may belong to species different from both of these. Isle of Purbeck, and coast thence to the west of Lulworth Cove. Quarries at Upway, north of Weymouth. Isle of Portland : in the “slate”’. Exogyra bulla. Pl. XXII. f. 1. Durlstone Bay. Ostrea distorta. Pl. XXII. f. 2. Durlstone Bay. The bed called “ Cinder ’’, about the middle of the strata which are worked for stone, consists almost entirely of this and other species of oyster. C. * Proceedings of Geol. Soc., vol.i. p.159.; and Geol. Trans. Second Series, vol. iii. p.421. et seq. 230 Dr. Firtron on the Strata below the Chalk. Ostrea. A new species? Durlstone Bay. West side of Lulworth Cove, in bluish . sandy stone. Durdle Cove, in a bed like the ‘ Cinder”’. Paludina carinifera. W. of Lulworth Cove, with Unio compressus, and a pearly oyster, in the uppermost of the Purbeck beds, some of which are almost entirely composed of shells of Paludine. Also, with bones of fishes, in very blue com- pact and sparry limestone. P. elongata. Peverell Point. Abundant in the uppermost beds of the Pur- beck stone, with much green matter. Durlstone Bay, with Cyclas media. P- Sussexiensis. Pl. XX. f.6. Peverell Point; in splintery limestone, with disseminated calcareous spar. Durlstone Bay. Unio compressus. Durlstone Bay ; in oolitic stone, with Cypris. U— new species? At the upper part of the series; in beds composed of carbonate of lime, apparently derived from the presence of these shells, with a large pro- portion of green matter (silicate of iron). East side of Lulworth Cove. Wor- barrow Bay. [The occurrence of bivalves in this place is mentioned by Mr. Webster, Geol. Trans., 2nd Series, vol. ii. pp. 39, 40.] Reprtites.—Turtles. Fragments of the shell and bones of Turtles are not unfre- quent, and even entire skeletons are sometimes found in the Purbeck strata. Saurians. Fragments of bone, and teeth. Fisnes. Palatal bones: Durlstone Bay. The scaly remains, also, of different spe- cies, are frequent in the slaty strata of the Purbeck stone. Puants. Near the junction of the lower slaty beds of the Purbeck with the Portland stone, large trunks and branches of coniferous wood are found in great abundance in the “ Black Dirt” above the “ Cap’’, in the Isle of Portland, and on the coast east of Lulworth Cove ; and in the dirt below the “‘ Cap”? between Upton and Poxwell. A Cone, represented in Plate XXII. f. 9., and stated to be “ from Purbeck”’, is in the Museum of the Geological Society. It has some slight resemblance to the cone of a Dammara of the Moluccas. Cycadeoidea (Mantellia of Adolphe Brongniart, ‘“ Prodrome”’, &c.). Remains of at least two species of Cycadee occur in the Isle of Portland, along with the trunks of coniferous trees, in the “ Black Dirt” above the “Cap”; and those of at least one species, also in the dirt or clay, between that bed and the “ Skull- Cap”. [Portland Stone. | Ammonites biplex. Isle of Portland. A new. Isle of Portland. Cerithium? excavaltum (Turritella excavata, Min. Con.). West of the Isle of Port- land. Cytherea parca (Venus, Min. Con.). West of Portland, in the flint of the “ Roche”. Lithodomus. New. Upper part of the “ White Bed’’, Portland. L —. Another species? Same situation. Dr. Frrron on the Strata below the Chalk. 23] Monodonta. New. Lowest beds of the Portland stone. Near Blacknore, Isle of Portland. Pecten lamellosus. Lowest beds of the stone. Same situation. Plicatula? Casts of the interior, numerous in the “‘ Roche” immediately over the “ White bed’’. Portland. Terebra Portlandica. Pl. XXIII. f.6. Very numerous in the “ Roche” the ““ White bed”. Portland. Trigonia incurva. PI. XXII, f.14. (Miss Benett*: Pl. XVIII. fig.2.) In the “White bed”. Portland. T——— gibbosa. Frequent in the “ Roche’’. Portland, and elsewhere on the coast. T: A variety, approaching to incurva, but less oblique. Portland. Venus parva. (See Cytherea.) : also in {Portland Sand. | Ammonites giganteus. Cross-roads above Kimmeridge Farm, on the north-east. Isle of Purbeck. New species. In concretions of splintery indurated marl, or soft lime- stone. Lowest beds of the Portland sand. Emmet’s Hill: Isle of Purbeck. Cucullea. (A small species.) Portland. Exogyra nana. West side of Portland Island, on an Ostrea. Ostrea levigata. Kast side of Portland. Panopea depressa. (Mya depressa, Min. Con.) In concretions of dark bluish grey indurated marl. Lower part of the sand. Emmet’s Hill: Isle of Purbeck. Pecten. A new species? Upper part of the sands. Blacknore, Portland. Serpula tricristata. Pl. XXIII.f.3. East side of Portland. Qua. in Kimmeridge clay? variabilis. P]. XXIII. f.7. East side of Portland. Qua. in Kimmeridge clay? A Ss Trigonia clavellatat. Cross-roads above Kimmeridge Farm on the north-east. Isle of Purbeck. Fisnes. Scales of fishes are found in strata apparently belonging to this formation, under Gad Cliff, in the Isle of Purbeck. Rays of dorsal fins (see the abstract of a paper by M. Agassiz, Pro- ceedings of the Geological Society, vol. ii. p. 101.) occur in nodules either of this formation or of the Kimmeridge clay, on the east coast of Portland. [Kimmeridge Clay. | Ammonites biplex. Numerous in the bituminous shale of Kimmeridge Bay, with transparent sulphate of baryta: sometimes along with an Ostrea. * “A Catalogue of the Organic Remains of the County of Wilts;” 4to, with 18 plates. Warminster, 1831. t Besides the shells mentioned above, two or three other bivalves, of which the genera are indistinct, have been found in the Portland sand, at Emmet’s Hill and other places, in the Isle of Purbeck. VOL. IV.—SECOND SERIES. 2H 232 Dr. Firron on the Strata below the Chalk. Ammonites mutabilis. Young. Astarte cuneata? In firm brown shale. Kimmeridge Bay. Panopea depressa. Kimmeridge Bay ? Ostrea deltoidea. East of Portland. Que. in Portland sand ? Fisues. Teeth. Rays of dorsal fins. [ Weymouth Strata and Oxford Oolite*.} Ammonites circularis. Pl. XI. f.20. In reddish sandy beds above the pisolite. Ab- botsford. Astarte cuneata. In ferruginous sandy stone. Near Weymoutht. Belemnites fusiformis. North of Weymouth. Clypeus clunicularis. (Smith, “ Strata Identified’”—Coral Rag, fig. 6.) Weymouth; in oolitic sand. Exogyra nana. In whitish oolitic stone, between Ham Cliff and Osmington. North of Weymouth. Gervillia aviculoides. In the coarse grit between Ham Cliff and Osmington Mill. Melania Hedingtonensis. In oolitic sand, near Weymouth. In reddish sand-rock, above the pisolitic clay, near Abbotsford. Modiola bipartita. In hard reddish clay. Osmington. Ostrea. A thick-shelled species, near Abbotsford, in oolitic sand, at the top of the oolite. O Species? Between Ham Cliff and Osmington Mill. Nerinea Goodhallii. Pl. XXIII. f. 12. Cliffeast of Osmington Mill ; in coarse rag. Mr. Goodhall. 4 Pecten annulatus. n sandy beds, near Osmington ? Pullastra? Yn marly pisolite at the top of the Oxford oolite, near Backwater, going from Wycke Church; Weymouth. Terebratula inconstans. Near to Osmington, in blue clay. Boat Cove. T————. New? Oval: reddish beds above the pisolite. Abbotsford. Trigonia clavellata. Abundant on the shore between Ham Cliff and Boat Cove. In ferruginous sandstone near Weymouth, with Astarte cuneata. T. costata. Osmington. Trochus Sedgwickii (olim T. reticulatus). From the reddish beds above the pisolite. Near Abbotsford. Upper part of the Coral rag, and lower of the Kimmeridge clay. Near Weymouth. * As the sands and clays of the Weymouth group pass insensibly into the Oxford oolite, it is difficult, and perhaps unnecessary, to distinguish them by a definite boundary. The fossils appear to be the same. + Most of the specimens here referred to, from the neighbourhood of Weymouth, are in Mr. Goodkall's collection. Dr. Firron on the Strata below the Chalk. 233 DeEvonsHIRE. (118.) The coast on the west of Portland as far as Sidmouth has been described by Dr. Buckland and Mr. De la Beche* in these Transactions ; where also the former has published a map of the coast between Teignmouth and Portland, with views from Sidmouth to Bere Head, and from Lyme Regis to the vicinity of Weymouth and Portland +. The coast of Devonshire, therefore, requires no additional illustration ; and for the local extent and distribution of the strata in the interior of that county, it is now in my power to refer to the beautiful Geological Map recently completed by Mr. De la Bechet, and to be followed by an explanatory memoir and sections. As the beds between the chalk and the bottom of the lower green-sand on the west of Purbeck appear to have coalesced, and are no longer marked by the previous subdivisions, the green-sand of Devonshire may be regarded as the equivalent of the whole series. The lower green-sand seems especially to have been reduced in bulk, in its progress westward. The gault has wholly disappeared ; but some of its characteristic fossils are found in the sand and grit of the cliffs on the west of Lyme. At the bottom of the sands the boundary is everywhere distinct: and the plateau which shoots out to the west of Dorsetshire is found successively in apposition with the lower oolite, the lias, and new red sandstone ; while its remotest portion rests on grauwacke slate. Throughout the greatest part of the tracts thus occu- pied, the green-sand forms a flat-topped, uniform cap, investing the hills, as far west as Sidmouth on the coast, and the Blackdown range on the north of that place, nearly to Wellington ; and finally, it constitutes an exten- sive outlier, from the north-west of Teignmouth to Penhill, about six miles south-west of Exeter, which caps the heights of Great and Little Haldon, and is detached from the more continuous tract above mentioned by an interval of more than twelve miles, occupied by the new red sandstone. Several insulated portions of chalk, however, still remain above the eastern portion of the green-sand platform, especially upon the coast between Sidmouth and Lyme, and along the line from Beaminster through Chard and White Stanton. The transition from the chalk to the sands is well seen at some of the junctions, especially on the south-west of Axmouth, where the strata * See their joint memoir at the commencement of the present volume; Geol. Trans., 2nd Series, vol. i. p. 40, &c.: and a separate paper by Mr. Dela Beche, vol. ii. p. 109, &c. T Ibid:, vol.i. p. 95, &c. t “Ordnance Geological Map of Devon, and of portions of Cornwall and Somerset, by H. T. “De la Beche, Esq.,” in eight coloured sheets. 2H 234 Dr. Firron on the Strata below the Chalk. rise a little towards the north from the point of Bere Head, so that sections of the subjacent beds are exposed in the cliffs on both sides of that promontory. The beds immediately below the chalk are best seen on the shore towards Branscombe, and have been described by Mr. De la Beche, who has also mentioned the quarries near that place, from which stone corresponding in situation to the firestone of Surrey is extracted *. The section at Whitecliff, on the east of Bere Head and of the village of Bere, is thus : Feet. 1. Chalk: white at top, yellowish below; very sandy, containing throughout numerous } small nodules of flints, both in bands and irregularly disseminated,—more numerous at top.) Vermetus is a frequent fossil here... 200.6000 c0sdesnicevecscenscevccvnsesus 0 [At the bottom is a course of very sandy chalk, including concretions or lumps of { — greater firmness, produced apparently by the unequal diffusion of the siliceous matter. | | Total, 60 or 70 feet. 2. Yellowish grit, with green stripeS ». nese cene secs ceen cn eers re ceccsscnss selene 3. A conglomerate of lumpy concretions, and apparently of fragments also, of hard matter ; with green particles between the lumps. Petrifactions numerous ..............About 4, Beds of chert; both continuous and in irregular concretions, alternating with bands of xc 2 : : 2 50 siliceous grit ; from 3 or 4 feet down to a few inches in thickness .... Total, about 40 or 5. Bluish green and grey sand, with bands of more solid texture, increasing gradually in 40 number towards theibottom .). 03 J. cls ve sie ole © wiecle’ ibimcitia ts eicls ele ble clic tN DOME ONE 6. Bluish moist sand, in some places almost black, abounding in petrifactions, and becoming } darker in colour downwards, the hue apparently depending on the degree of moisture. This bed contains Gryphites, traces of large Ammonites, Vermetus, and numerous stems of Siphonia «i100. tie ele cles e so sieciee ec cee vee sisie vais of si 2/5 +96» About 50) or 60tect ama [This darkly coloured sand contains at the lower part large nodules, consisting of greenish grit, in courses from 3 to 6 feet apart. The stratum is in immediate contact with the red marl. Springs come out at the junction. | 7. Red marl. At the top containing gypsum in nests; throughout including spots and patches of a light greenish grey, and alternating with beds, of irregular thickness, of the same hue. (‘ Bunter sandstein ”?) I have inserted the preceding list from notes taken during the summer of 1825, as its coinci- dence with that since published by De la Beche, shows the correctness of both. It will be evident, upon comparing these lists with each other, and with that of the sands near Lyme, that the group which here succeeds the chalk is the equivalent of the Upper green-sand ; the local variations in this formation on the Devonshire coast not being greater than those of the range which extends from Folkstone into Surrey; in the course of which the Upper green-sand is in some places almost wholly wanting, while in others it acquires great thickness, and often contains beds almost suddenly developed, no trace of which is to be found in the intermediate spaces. The grizzle of Sutton quarry, and the Beer-stone, are varieties of the siliciferous stone on the confines of the chalk and Upper green-sand, which under various denominations, “ Fire-stone”, ‘‘ Totternhoe-stone”, &c,., occurs very generally in that part of the series, and is everywhere in request for building. The total absence of blue clay is remarkable in the section at Bere. The place where it might have been expected is immediately beneath the cherty groups of Mr. De la Beche’s figures 1 and 2+; and if the gault were added to those sections, estimating * Ina large pit or quarry at the bottom of the chalk, near Sutton and Widworthy, a stone, called Grizzle by the quarry-men, is dug in the situation of the firestone. The beds are altogether about 5 feet in thickness. It contains green particles, and does not burn to lime. Among its fossils is Catillus Cuviert. t+ Geol. Trans., 2nd Series, vol. ii. pl. 16. Dr. Firron on the Strata below the Chalk. 235 its thickness only at 100 feet, the total thickness of the whole of the green-sand group would not be more than 300 feet: the actual thickness of the sands being nearly 200 feet at Lyme Regis ; and at Whitecliff, according to my own measurement (it is not stated by Mr, De la Beche), about 160. The beds below this cherty group represent Mr. De la Beche’s “ Fox mould” (No.6. of the above list); and are apparently the equivalent of the upper and more ferruginous group of the lower green-sand: the lower, moist, and dark-coloured sands, with the ‘‘ cowstones” at the bottom, being probably the equivalent of the middle, dark, cohesive sand of Sandgate (24.), Shanklin (192.), and Black-gang Chine (195.);—the ‘ cowstones” representing the calcareous group of Hythe, &c. This occurrence of nodules dispersed in sand is frequent wherever calcareous strata are near their termination ; as in the cases of the Portland stone, the lower oolite, &c. I have stated these resemblances that the whole case may be before the reader: butin the vale of Wardour,—where the distinct occurrence of a bed of blue clay with the characteristic fossils of the gault, leaves no doubt as to the place where the sands are divided,—the inferior beds of the Upper green-sand acquire a character very like that of the Lower in other places; and the latter is either wholly wanting, or very imperfectly represented. (119.) Blackdown Hills.—In approaching the hills of green-sand, their aspect on every side is the same, precisely resembling that of the long’ flat- topped ranges of this formation, and of the Bagshot sands, in Kent, Surrey, and Hampshire. The surface is barren, and the chief products, at present, seem to be furze and heath ; though in former times, it is reported, extensive woods were here. 1 ascended first from Wellington on the north of the Blackdown Hills, and found red mar! for more than two thirds of the height, so nearly resembling some of the sandy and variegated clays of the Wealden, especially of the Hastings sands, that but for the presence of sulphate of lime in crystalline nests, it would be difficult to distinguish them; while the greenish varieties of the marl also very much resemble some of the beds above the chalk in the Isle of Wight. From Beacon Hill, on the south-west of Wellington, the uniform level of the summits is very striking, the eye being carried over the whole range without interruption, and the ravines quite lost sight of. The absence of the remains of chalk from the debris on the top of these hills is remarkable : I searched long, but did not see a single fragment of flint, all those which I could find being chert, easily distinguishable from chalk flints. In the yellowish sand near the surface, at the Barnscombe side of the hill, brown iron ore is found, in polished fragments of very high lustre, resembling those of the lower green-sand at Sandown Bay in the Isle of Wight (1200; p. 188.), of Surrey (59.), and Western Sussex. Although the strata forming these hills are in a general view continuous, the whole country is divided by fissures, attended in some cases with considerable dislocation; for an account of which I refer to Mr, De la Beche’s Map of Devonshire, and his essays on Theoretical Geology *. * « Researches in Theoretical Geology,” 1834, p. 185, &c. 236 Dr. Fitton on the Strata below the Chalk. Three nearly parallel lines of fault, running about north and south, are especially remarkable in Mr. De la Beche’s Map; one on the east of the county, passes from about a mile north of Combe Beacon, through the hill which bears that name, along the valley of Wambrook, and the streamlet west of Chardstock, across the Axe, to a point about two miles east of Axminster ; the total extent to which it has been traced being about ten miles. A second fault extends from Balay Down on the north of Challenge, through Membury, to the bed of the Yart south of Yetlands; the lias being thrown up into immediate apposition with the green-sand through a great part of its course, as is also the case in the preceding fault near Wambrook. A third and shorter fissure, about three miles in extent, reaches from the north of Wilmington to Stockers, about two miles south of Widworthy, crossing the main London and Exeter road, and skirting the eastern slope of an outlying hill of chalk on the south of that village. (120.) The hills which have furnished the greater number of the Black- down fossils form the western range of the group between Honiton and Wellington, about six miles to the south of Beacon Hill above mentioned. Their escarpment, between Punchey Down on the north, and Upcot Pen on the south, is distinguishable at a great distance by the white line produced by the refuse thrown down from the openings of the sithe-stone pits; the heaps thus formed constituting an almost continuous horizontal stripe in the face of the hill. The whole thickness of the sandy strata above the red marl in this part of the country, seems to be about 100 feet. ‘The contrast between the barren- ness of the upper sands, and the comparative fertility of the marl beneath, is everywhere very conspicuous ; and it would seem from the unequal ascent of the hedge-rows and cultivated ground that the surface of the marl is very uneven. The strata which afford the whetstones are about 80 feet below the top of the hill, to which they are parallel. The mines (or “pits” as they are called) are driven in direct lines into the hill, almost horizontally, and in some cases to considerable distances. The stony masses from which the sithe-stones are cut, are concretions of very irregular figure, imbedded in looser sand, nearly resembling those which occur in the upper division of the Lower green-sand near Sandgate (21.): and though very irregular in shape, marks of the stratification of the sand can be traced on their outside. The masses of which the sithe-stones are made, vary from 6 to about 18 inches in diameter, and the beds which afford them would form a total thickness of about 7 feet, of which about 4 are fit for that purpose; the looser stone at the top and bottom being employed for building. The following is a sectional list of the beds in one of the principal sithe-stone pits at Punchey Down, which, I was informed, was a fair representative of the whole: Ft. In. Ft. In. 1. Reddish sand rock, extending upwards to the top of the hill. 2, “ Fine vein”. Concretions of firmer consistence; the best for sithe-stones. [Shells are found in all the strata here, but abound remarkably in this one, jo 2 .to Vee and inthe ‘frock beneath iti) <0)... ee cea. SOA 05 Sa ASRS nics oe 3. “ Top sand rock”; sand with irregular concretions; of no use.......... 5 0 to 4 0 Dr. Frirron on the Strata below the Chalk. 237 Ft. In. Ft. In. 4. * Gutters”; concretions of stone in 4 or 5 courses, in the sand, This bed is S268 tos that most commonly used for sithe-stones ........+eeeeeeecerreeeeeees 5. * Burrows”; stone and sand of the same kind, but used only for building... 2 0 to 3 0 6. “ Bottom stone”; a range of concretions, affording excellent sithe-stones.... 0 2 to 0 6 [These concretions sometimes extend downwards, even to 5 feet, in the sand. | 7. “Rock sand”; chiefly sand, with fewer concretions; of no use ........-- 4 0 8. “ Soft vein”; concretions which afford excellent sithe-stones ............ O 2 to O 6 0 The strata below are not known to the workmen. ‘The total thickness, therefore, of the strata which furnish the material for sithe-stones, including the rejected sand and rubbish, is from 12 to 18 feet; the whole of which is removed in cutting the drifts or galleries. Sithe-stones.—As the manufacture of these stones occupies a great number of the inhabitants of the country, and is of some commercial importance, a large proportion of the whole quan- tity used in England being supplied from the Blackdown pits*, I shall here describe the method of preparing them. The sithe-stone men take from the owners of the soil the privilege of digging for stones, leaving 40 yards on each side between the drifts (or “ pits” as they are called). There is no limitation as to depth, and the drifts are commonly pushed to about 500 yards inwards, greater distances not repaying the labour of bringing out the sand. When first taken out, the stone is greenish and moist, and can be cut or chopped with ease. The tools employed are a sort of axe or adze with a short handle (fig. 2.), called a “basing-hammer”, which is ground to a sharp edge. These are made at the adjacent village of Kentisbere. The other tools are “ picks”, without any peculiarity of struc- ture, and “ hollowing-shovels” (fig. 1.), for digging the masses of stone out of the sand. For the purpose of cutting the stones, a vertical post of wood, or “anvil”, is so fixed in the ground as to stand between the knees of the workman, who sits upon a sort of bench built of stone, with some strong pieces of old leather attached as a de- fence to his left knee. He first, with the edge of his “ basing- hammer”, splits from the blocks, upon his knee, long portions approaching to the shape of the sithe-stones f ; and then cuts or 12 inches chops them down, nearly to the required size, upon the anvil and his knee,—just as a carpenter cuts timber with an adze. After being thus rudely shaped, the stones are “ hewn” to the proper dimensions with a larger “hammer”, and then rubbed down with water by women, on a large stone of the same kind; and when dried they are fit for sale. The stones when finished vary from about ten to twelve inches in length; some have the shape of a portion of an almond, with the ends and sides cut square, and about 2 inches by 14 in thickness; others are almost cylindrical, but smaller at each end, with the sides a little curved ; the diameter in the middle about 2 inches. * Sithe-stones are also manufactured in great numbers in Derbyshire from the sandstone of the coal formation. (Farey’s Derbyshire : 8vo, 1815; p. 437-8.) ue The masses of stone, I believe, split best in the direction of the lines of stratification of the sand, 238 Dr. Firton on the Strata below the Chalk. A good workman can cut out of the blocks about seven dozen of the stones per day *. They are sold by the makers chiefly to one merchant at Honiton, who supplies the retail dealers. The prices (in 1825) varied from 2s. per dozen, for the finest stones, 11 to 12 inches long, down to 8d. a dozen for the coarsest, 10 inches in length. (121.) Between the sand and the red marl beneath it, I did not observe any perceptible valley, nor any indications of an intermediate bed of clay. In a lane at Standhill, between Wellington and Bryants, about half a mile from the latter place, the strata were thus; belonging to what is, here, the upper part of the new red sandstone. Ft. In. . Dusky red clay, or marl, adhering to the tongue ........ sfeloke okshexeagte lip orpiets vie oloipin . Light greenish clay, with glittering particles (mica) .......++22eeeeeeee ++ -about o.o ©&.o 2 1 . A band of greenish sandy clay, in part concreted and sparry, irregular in thickness .. 0 sutoreenish clay, like NOj2.. o/s: ajeltetensestare teat leialcretetaccle /ovele ican. teteteletatetatareieta +« ADOUt NS cor B® GO tO = . Reddish clay, like No. 1., in part concealed at the bottom........... bi sieee @elele atone These beds are scarcely distinguishable from those at the top of the Hastings strata, at the back of the Isle of Wight. At Kentisbere, about 15 mile west of the escarpment of the hills which contain the stone pits, the strata of red marl appeared to dip to the south-east. They consist of coarse gravel and con- glomerate of a dull red hue, under firm, red, marly sand: and here there is a distinct alternation of yellow sand with the red marl, the former appearing below the marl in thick stony beds at Jeast 50 feet thick. A rough section at this place is given in Plate X. a. No. 12, (122.) Fossils —The great numbers and variety of the Blackdown fossils may be ascribed in part to the extent of the quarries, which have been dug for sithe-stones during a long series of years ; but the beds themselves must be more than commonly fertile in these productions, since the entire thickness of those from which almost all the specimens have been obtained, does not exceed twenty feet. Their beautiful preservation arises, in some measure, from the loose sandy character of the matrix in which they are imbedded, and from which they are easily detached: but the compo- sition of the fossils themselves has also contributed to this effect ; for, with very few exceptions, the shells are converted into chalcedony, and the * Mr. Meade, of Chatley near Bath, has favoured me with the perusal of a letter from the Rev. Mr. Steinhauer, dated in 1813, in which, after an account of the whetstone pits at Black- down, it is stated that the preparation of the sithe-stones is so injurious to the health of the work- men, that in the little village of Punchey Down, which is inhabited exclusively by the stone-cutters, the writer saw but one elderly person, and was informed that few reached the age of forty. The complexion and figure of the greater number he describes as striking and interesting in a high degree; but it was the hectic aspect, and itself a proof of disease. When I visited the place about twelve years afterwards, I did not meet with anything that called my attention to the health of the quarry-men: but the facts described by Mr. Steinhauer are analogous to those which prove the frequency of consumption among the grinders of needles, and the workmen at some other trades, where minute particles of solid matter are diffused in the air, and taken into the lungs. Dr, Frrron on the Strata below the Chalk. 239 whole of their calcareous matter has disappeared*. This is the more remarkable, as in many other places, indeed generally, the fossils of the green-sands consist of carbonate of lime; the absence of which, however, is prevalent throughout the sand of the Blackdown Hills, which seldom effervesces with acids ; and to this circumstance, probably, the excellence of the concretions which they contain, as a material for whetstones, is to be attributed. A very extensive collection of fossils from the Blackdown pits was formed by the late Mr. Miller, of the Bristol Institution ; and is now in the museum of that establishment. The Managers were so good, at my request, as to allow the whole of this valuable collection to be sent to London, where it was examined by Mr.Sowerby, by whom the subjoined list, and the annexed plates, have been prepared: and I have great pleasure in expressing my obligation for this mark of their confidence and favour. (123.) List of Fossils from the Sands of Bracxpown, and of some other places in DevonsHiRet. Ammonites auritus. M. A— denarius. A thin crust of hydro- phanous chalcedony, over spongy sili- ceous stone. M., Min.Con., F. A— dentatus. M. A— falcatus. M. A— Goodhallii. Blackdown. M., F., Min. Con. Near Lyme. D. A— Hippocastanum. Dowlands cliff, near Lyme. Min. Con. A— lautus. M. A— splendens. Pinhay, in hard green sparry stone. F. A—triserialis. Pl). XVIII. f.27. Mr. Sowerby’s museum. A— tuberculatus. M. * See Conybeare ; “Outlines,” &c., p. 128. Ammonites varians. A gibbose variety. M. Pinhay. F. A— varicosus. M., F. A— Another species, probably new. M. Amphidesmatenuistriatum. M. P1.XVI. f. 7. 4rca rotundata. M. Pl. XVII. f. 8. Astacus, Portions of. Pinhay. Miss An- ning. Near Lyme. D. Astarte concinna. Pl. XVI. f.15. M. Mr. Sowerby’s museum: D. A— cuneata. F. A— formosa. M. Pl. XVI. f. 16. A—impolita. M. Pl. XVI. f. 18. A— lineata. ¥F. + All the Fossils in this list are from the Whetstone Pits at Blackdown, except those to which a different locality is assigned: and all the specimens from the Blackdown pits, where a different composition is not mentioned, are casts in chalcedony. The letter M. denotes that the specimen is from the collection of the late Mr. Miller, now in the museum of the Institution at Bristol: Min. Con. refers to Mineral Conchology : D. to a paper of De la Beche, on the chalk and sands in the vicinity of Lyme Regis and Bere; Geol. Trans. 2nd Series, vol. ii. p. 109 et seq.: F. to the Author’s Collection. VOL, IV.—SECOND SERIES. 240 Dr. Frrron on the Strata below the Chalk. Astarte striata. M. Min. Con. A— multistriata. M. Pl. XVI. f. 17. Auricula? incrassata. M.,F. Min. Con. A—? Two species, not figured. F. Aviculaanomala. M. Pl. XVII. f. 18. Cardium Hillanum. ¥F., M., and Min. Con. C— proboscideum. M. Min. Con. Corbula truncata. M. Pl. XVI. f. 8. C— elegans. ¥., M., Min. Con. C— gigantea. M., Min. Con. C— levigata. Min. Con. C—. Two other species, probably new. M. Cucullea carinata. M. like stone. Min. Con. C— costellata. M., F. Min. Con. Col lumpton, Devon: near Lyme. D. C— decussata. Pinhay or Bere? F., Min. Con. C— fibrosa. M., F. The sand-rock of this specimen is very like that of Ris- borough, near Hythe. In red jasper- like stone or chalcedony. Min. Con. C— glabra. Pinhay. In firm sparry grit. M., Min. Con. Near Lyme. D. C— formosa. M. Pl. XVII. f 7. Cyprina angulata. (Venus angulata. Min. Con.) The shell about one third filled with chalcedony, as witha liquid. In some specimens the shell, the place of which is now occupied by chal- cedony, had been bored through, as represented in the Plate: in others the shell is covered by a thin outer crust of chalcedony, opake and hydro- phanous ; and the cavity is nearly full In red jasper- of very fine siliceous sand, over which in some places is a thin crust of flat botryoidal translucent chalcedony. M. Teignmouth. Min. Con. C—cuneata. M. PI. XVI.f.19. Drawn from a specimen in Mr. Goodhall’s collection. Cyprina rostrata. M. Pl. XVII. f. 1. Cytherea caperata. (Venus. Min. Con.) M., F. Variation in the depth of striz. Min.Con. Blackdown, and near Lyme. C— lineolata. (Venus. Min. Con.) M Min. Con. Berehead. F. C— parva. (Venus. Min. Con.) M., Min. Con. Pinhay? F. C— plana. (Venus. Min. Con.) M., Min. Con. Pinhay? F. C— subrotunda. M. Pl]. XVII. f. 2. Dentalium cylindricum. Near Exmouth. Min. Con. D— ellipticum. F. D— medium P\.XVIII. f. 4. M., Min, Con. Echinus, portion of an. Bere: In white calcareous sandstone. F. Exogyra conica. (Chama, Min.Con.) M., F. Ware, west of Lyme Regis. Pin- hay. Bere. F. E— conica: var. Ridge high and sharp. Berehead. F. E— halyotoidea? Blackdown. F. E— levigata. (Chama, Min. Con.) Low- est part of the green-sand at Bere- head: In soft agglutinated sand, abounding in green particles. F, E— undata. (Chama, Min. Con.) M. and Min. Con. Fusus clathratus. M. Pl]. XVIII. f. 19. F'— quadratus. (Murex, Min. Con.) M. Pl. XVIII. f. 17. F—rusticus. M. Pl. XVIII. f. 18. F— rigidus. M. PI. XVIII. f. 16. #— another species? M, Gervillia aviculoides. M. Lyme. Min. Con., F. G— solenoides. Min. Con. Gryphea canaliculata. (Chama, Min. Con.) M. Outer surface calcareous and effervescent, chalcedony within. F. Me} (Chama, Min. Con.) Dr. Firron on the Strata below the Chalk. Al Gryphea canaliculata: a broad variety. In yellowish effervescent sand, with green particles. F’, G— vesiculosa. Berehead? M. Hamites spinulosus. M. Inoceramus concentricus. M. Iniridescent chalcedony: Pinhay. In green hard stone. Min.Con., F. Near Lyme. D. I— gryphaoides. M. Near Lyme Regis: In concretional masses of hard green- ish grit, including very small scales of mica, and some minute black specks, under Dowland’s Cliff. Miss Anning; and F, J— sulcatus. Berehead. M. Tsocardia? ¥. Lima semisulcata. (Plagiostoma semi- sulcatum. Nelson.) M. PI. XI. f. 10. L—? subovalis, M. Pl. XVII. f. 21. Littorina pungens. M. Pl. XVIII. f. 5, I— gracilis. M. Pl. XVIII. f. 12. Lucina? orbicularis. M. Pl. XVI. f.13. T— Pisum. M. Pl. XVI. f. 14. Lutraria striata. Pinhay near Lyme. Min. Con. Mactra angulata. M. PI. XVI. f. 9. Modiola reversa. M. PI. XVII. f. 13. Murex Calcar. M., F. In iridescent chal- cedony. Min. Con. M— quadratus. (See Fusus.) Mya leviuscula. M. Pl. XVI. f. 6. M— mandibula. Pinhay Cliff. In firm green micaceous sparry grit. F. M— plicata. (See Panopea.) Mytilus inequivalvis. M. PI.XVII. f. 16. M— lanceolatus. Min. Con. M—prelongus. P]. XVII. f. 15. M—tridens. M. Pl. XVII. f. 14. Nassa costellata. M.? Pl. XVIII. f. 26. N— lineata. M. PI. XVIII. f. 25. Natica (Parkinson, Geol. Trans.). F. N—? carinata. M. Pl. XVIII. f. 8. Natica granosa. M. PI. XVIII. f. 7. N— canaliculata. (Ampullaria, Geol. Suss.) M. Pl. XVIII. f. 6. Nautilus elegans. M. Also in the sand near Lyme Regis. D. Nucula angulata, M., F., Min. Con. N— antiquata. M., F., Min. Con. N—apiculata. F. Pl. XVII. f.10. N— impressa. M., F., Min. Con. N—lineata. M. Pl. XVII. f. 9. N— obtusa. M. Pl. XVII. f. 11. N— pectinata. Pinhay. In hard greenish stone. F. Ostrea carinata. M. Near Lyme Regis. D. O— macroptera. Berehead. F. Panopea ovalis. M. Pl. XVI. f. 5. P— plicata. (Mya, Min. Con.) M. Pin- hay. F. Pecten Stutchburiensis. M. Pl. XVIII. f. 1. P— asper. M. P—compositus. M. Pl. XVII. f. 20. P— Millerii. M. Pl. XVII. f. 19. P— orbicularis. M. Pinhay. F. P— quadricostatus. M. A cast in grey chalcedonous chert. F. Haldon Hill, Devon. Min. Con. P— quinquecostatus. Pinhay. F. P—,(new.) Bere. F. Pectunculus umbonatus. Blackdown. F. Haldon, Devon. Min. Con. P— sublevis. Min. Con. Perna rostrata. M. Pl. XVII. f. 17. Petricola canaliculata. M. Pl. XVI. f.11. P— nuciformis. M. Pl. XVI. f. 10. Phasianella pusilla, M. Pl. XVIII. f. 13. P— formosa. M. Pl. XVIII. f.14. P— striata. M. Pl. XVIII. f. 15. Pholas prisca. M. In silicified wood. The shell is chalcedony. Pinna tetragona. M., Min. Con. Podopsis striatus. M., F. Effervesces. Pollicipes levis. M. Pl. XVI, f.1. (See also Pl. XI. f. 5.) 212 242 Dr. Fitton on the Strata below the Chalk. Psammobia? gracilis. M. P). XVI. fig.12. Thetis minor. Large. A castin firm sparry Pyrula Brightii. F. Pj. XVIII f. 21. grit. Pinhay, or Bere. F. Black- P— depressa. M. PI. XVIII. f. 20. down, and near Lyme. Min. Con. Rostellaria calcarata. M., Min. Con. T—(new.) Pinhay. A cast. F. R— macrostoma. M. PI. XVIII. f. 23. Tornatella? affinis. M. Pl. XVIII. f. 9. R— Parkinsonii. M., Min. Con., F., Pl. Trigonia affinis. M., Min. Con. Blue XVIII. f. 24. mammillated chalcedony. R— retusa. M. Pl. XVIII. f. 22. T— aleformis. Blackdown. M.:—Ridges R— Another new species. F. very sharp. F. Near Lyme. D. Scalaria pulchra. M. Pl. XVIII. f. 11. T— dedalea. M., Min. Con. Serpula ampullacea? M. T— eccentrica. M. Hembury Fort, S— antiquata. M. Pinhay. Calcareous. Devon. Min. Con. S—carinella. M. Min. Con. T— pennata. Teignmouth. Min. Con, S— filiformis. M. Pl. XVI. f. 2. T— quadrata. M. Pl. XVII. f. 12. S— plexus? M. Effervescent. T— spectabilis. M., Min. Con. S— tuba. (M.. Pl. XVilies. T— spinosa. M., Min. Con. Near Lyme. S—vermes. Pl. XVI. F. f. 4. D. Siphonia pyriformis (Goldfuss). PI. Turbo conicus. M., Min.Con. KGa: T— moniliferus. M., Min. Con. Solarium conoideum. (Cirrus plicatus, T— rotundatus. M., Min. Con. M.C.) M. Turrilites costatus. M. Not chalcedony. Spatangus Bufo. (Goldfuss, Pl. XLVIT. Turritella costata. M., Min. Con. £73) Mi. T— granulata. M., Min. Con., F. S— Portion of another species, proba- Venus angulata (see Cyprina.) bly new. M. V— caperata (see Cytherea.) Tellina inequalis. Pinhay; M. Black- V— Faba. F., Min. Con. down; Min. Con. V—?immersa. M. PI. XVII. f. 6. T— striatula. M. Pinhay; F. Black- V—?sublevis. M. Pl. XVII. f. 5. down; Min. Con. V— lineolata (see Cytherea.) Terebratula biplicata. M., F. Calcareous. V—? ovalis. M., Min. Con., F. T— dilatata. M. Pl. XVIII. f. 2. V— parva T— dimidiata, Haldon, Devon.; Min. V— plana (see nC ythenca® Con. V—? truncata. M. Pl. XVII. f. 3. T— latissima. (T. lata, Min. Con.) M. V—?submersa. Pinhay. F. Pl. XVII. f.4. Z— megastrema. M. PI. XVIII. f. 3. V—. (‘Twoother species ; probably new.) T— Pisum. M., Min. Con. Vermetus concavus. Pl. XVIII. f. 10. T— striatula. M. Pinhay. Berehead. M. T— Lyra. M. V— polygonalis. Calcareous. Bere. F. Thetis major. Blackdown. M. Berehead; | V— radiatus. (Planorbis radiatus. Min. Min. Con., F. Con.) M. In addition to the species mentioned in this list, there are several others in Mr. Miller's collection, apparently new ; but being too indistinct for figuring, they have been omitted. Dr. Firron on the Strata below the Chalk. 243 (124.) Blackdown to Shaftesbury.—The great range of the chalk escarp- ment in the interior of England, which stretches, like the shore of a sea or lake, from Crewkerne in Dorsetshire to the north-east of Dunstable in Bed- fordshire, is perfectly analogous in structure and appearance to the downs of Surrey and Sussex. It is interrupted by three or four indentations or gulfs ;—one of great width, opening towards the west, between Crewkerne and the heights about Stour-head in South Wiltshire; another expanding to the north-west and terminating in the defile where the Thames cuts through the chalk, in its course to the south-east from Buckinghamshire and Oxfordshire. The vales of Pewsy and of Warminster are intermediate bays of the same general structure but of smaller dimensions ; and all these valleys are apparently the result of denudation, aided by previous disturbance of the strata,—which has carried away the chalk, and laid bare to various depths the strata beneath it*. The Green-sand hills range nearly from west to east for about ten miles on the south of Wellington and Taunton, and are then broken through irre- gularly, retiring towards the south to join the north-western extremity of the Dorsetshire chalk, of which some large outliers exist in the vicinity of Chard and Crewkerne. The chalk escarpment is thence continued in a direction parallel to the northern range of the Blackdown hills, to an opening on the north of Blandford, through which the Stour makes its way to the sea at Christchurch ;—the tributary branches of that river, before it cuts through the chalk, winding extensively over the country around Sturminster, from whence the waters of the whole bay are conducted to the south-eastern coast. From the opening of the valley of the Stour the escarpment turns nearly north towards Shaftesbury, between which place, or rather between the promi- nence of the Upper green-sand on the north of it, and Mere, is the opening of the vale of Wardour. The beds immediately below the chalk from Crew- kerne to Shaftesbury, have not yet been examined in detail, but the general distribution of the strata is represented in Mr. Greenough’s Map. Sourw WiTsHiRre. (125.) Vale of Wardour.—This tract may be considered as an eastern prolongation of the first of the great gulfs above mentioned, which being suddenly reduced in width between Shaftesbury and Mere, is continued east- * The principles of structure in these tracts, are ably discussed in Dr. Buckland’s well-known paper “On the Formation of Valleys, by Elevation of the Strata that inclose them,” (Geol. Trans., 2nd Series, vol. ii. p. 119, &c.,)—where the vales of Wardour, Warminster, and Pewsy are expressly mentioned in illustration of the author’s views. 244 Dr. Firron on the Strata below the Chalk. ward as a valley surmounted on both sides by hills. It will be seen from the Map, Plate IX., that the anticlinal line by which this lower tract is tra- versed coincides in direction with that of the great Wealden denudation of Hants, Surrey, and Sussex; and is parallel also to the line of upthrow on the coast of Dorsetshire and the Isle of Wight, and to other shorter lines of elevation, the connexion of which is not at present visible, on the north of the Weald,—through Burgh-Clerc, Ham, Shalbourne, and Burbage, to the Vale of Pewsy. One of the anticlinal lines of the lower strata, beneath the new red sandstone, from Frome to the Steep Holm in the Bristol Channel also runs nearly from east to west; whilst, on the contrary, another line of fault by which the lower beds are intersected, beginning near Portishead- point on the west of Bristol, runs northward, across the Severn, through Newnham, and thence to the north-west of Gloucester *. (126.) The Vale of Wardour has the general form of a triangle, the base of which extends from the chalk hills on the south of Shaftesbury to those of Mere, the apex being a little to the west of Harnham Hill on the south-east of Salisbury : for it is deserving of observation, that the stream of the Nadder escapes from this valley, not directly through the angle at its geological sum- mit, but through the north side; ma manner perfectly analogous to that of the egress of the streams from the Wealden denudation in Kent and Sussex. The heights which bound the vale consist at top of chalk, the inclination of which, like that of the strata beneath it, on the north of the anticlinal line, is in many cases more than 20°; while on the south, it is seldom more than 3° or 4°, apparently deviating but little from the general disposition of the strata in the South-east of England ; and this anticlinal line itself is throughout much nearer to the north than to the south side of the vale. The strata from the chalk down to the gault inclusive seem to be continued all through, and to be nearly uniform in thickness ; but the surface between the chalk hills is very irregular, and is divided by a ridge or bar formed by the escarpment of the Portland strata, on the east of which the ground is hilly, but on the west comparatively flat and low :—the appearances being altogether such as would arise from the deposition of the green-sands and chalk, over a tract partially occupied by the Purbeck and Portland forma- * The anticlinal lines near Bristol, on the Map, Plate IX., are taken from Messrs. Buckland and Conybeare’s paper on that district. For a full account of their reiations to those in the South- east of England, the reader is referred to a paper since published by the Rev. W. Conybeare (London and Edinburgh Phil. Mag. for 1832, vol. i. p. 122, &c.), who states that one of the great lines of fault, by which the transition strata of the Quantock Hills in Somersetshire (beyond the range of the Map, Plate IX.,) are traversed, runs also nearly east and west. Dr. Frrron on the Strata below the Chalk. 245 tions, so as to overlie the latter, and beyond them come into immediate contact with the subjacent clays. The small map, Plate VII. fig. 3, gives a plan of this valley on a larger scale than that of Plate 1X., and the Sections as to Gu, Pl. X.a., No. 13., further illustrate its structure:—the strata being the Chalk,—Upper green- sand,—traces of the Lower green-sand, and of the upper members of the Wealden; beneath which the Purbeck and Portland formations are more fully disclosed. (127.) Chalk.—The beds at Harnham Hill, immediately on the south of Salisbury, are inclined to the north ; and about a mile to the west of that hill a curved ridge, or horseshoe, formed of the upper chalk, seems to be the first divarication of the strata which bound the Vale of Wardour*. It therefore deserves inquiry whether the continuation of the fissure produced by an upheaving on the east of this point, may not be discoverable in the space between Salisbury and the head of the Wealden denudation. The southern limb of the chalk forms a continuous and lofty ridge from Harnham, through Compton Hill and Chiselbury, to White Sheet Hill, around the base of which the Upper green-sand occupies the whole space from Berwick St. John’s to Shaftesbury, the escarpment of the latter formation, which is the immediate boundary of the vale, being continued all along the foot of the chalk range, and rising from beneath it towards the north. On the summit of the ridge at Chiselbury, the chalk includes black flints in spongiform nodules: the Down slopes northward at an angle of upwards of 26°; and at its foot there is a depression or trough. The lower and marly chalk form a ridge at Hoopside, about 200 feet above the stream at its base, and perhaps 100 below the summit of the highest range, which as the name in- dicates is curved, and nearly parallel to the curve of the upper chalk at the Race-course. The hill in Wilton Park belongs to the upper chalk, which there crosses the stream of the Nadder, passing through North Burcombe and thence towards the north of west, to form the higher downs, on the north of the valley, at some distance from the ridge of the sands. The lower chalk and chalk marl constitute an intermediate tract, in several places outtopped by the sand ridge. In the height above South Burcombe, is chalk with veins and nodules of flint; and nearly on a level with the river, north-west of Hoopside, the Upper green-sand comes in. The succession from the flinty chalk to the Upper green-sand, on the north of the valley, is well seen in the road from Hindon to Fonthill Gifford. The ridge on which the archway stands, at the entrance to Fonthill Park, being chalk with large flint nodules, exposed in a pit imme- diately without the plantations, dipping north about 12°, and separated by a depression from the ridge of the Upper green-sand, which is here very low. * The Map, Plate VII. fig. 3, unfortunately, was engraved before I had observed the structure described in the text, so that the points here referred to are not included in it: but the features are well represented in the Ordnance Map; the aid of which, indeed, is almost necessary through- out these pages, to understand what is stated respecting the structure of the country. 246 Dr. Firron on the Strata below the Chalk. (128.) Upper Green-sand.—The effect of the unequal inclination of the two sides of the valley is remarkably shown by the great difference in the extent of the spaces occupied by this formation. On the south, the upper beds are concealed at the foot of the chalk hills; but the lower strata shoot out into plateaus, which form the tops of the hills all the way to Shaftes- bury ; but on the north the whole series of the Upper green-sand rises ab- ruptly and forms a very narrow ridge of unequal height. The Map and Sec- tions, Plates VII. fig. 3.and X.a., No. 13., sufficiently explain this structure. Some of the best sections of the transition from the chalk into the Upper green-sand are visible near Barford St. Martin and thence to Baverstock. In the lane over Baverstock Hill (called in the country Cloudles) the series consists of alternate beds of chalk and sand with green particles, succeeded by a thick bed of green-sand abounding remarkably in Gryphea vesi- culosa, which can be traced almost entirely round the valley. The ridge of these sands over Dinton House is full 200 feet above the bottom of the depression between it and the lowest chalk. The greatest superficial extent of this formation occurs in the vicinity of Shaftesbury, where the upper part seems to have been better preserved than in the continuation of it eastward. The sections vary from 50 to 60 feet in thickness; of which about a third at top contains beds of chert like those of the Isle of Wight: but the lower beds only are found in the plateaus which project beyond the chalk. Several good sections of the upper strata are visible in the lanes about Shaftesbury ;—at Lud- well, Hernsham Street, in the ascent from Brookwater, and thence to the foot of White Sheet Hill, where some of the quarries include chert and veins of chalcedony. From Castleditches,—-an ancient fort or encampment on the summit of a remarkable promi- nence, the sand which composes the top declines uniformly towards the foot of the chalk range, but extends with an even surface, westward to Shaftesbury, and eastward to Barford Heath. The beds have many points of general resemblance to the sands of Blackdown;—with this important dif- ference, that a very distinct stratum of bluish clay (Gault), which is wanting at Blackdown, is here found, everywhere, below the sand. The relations of these strata are well shown in a large quarry at the top of the hill east of the valley of Fovant and of the Pembroke Arms, where the following was the order :— Fovant Quarry. ron . in. Soil and Grass. 1. Greenish sand, alternating with gray, including stone which passes into chert, in irre- 16 0 gular concretional bands and masses :—very like the sands of Blackdown .... 14 to 2, Sand of a much darker hue, below passing into ston€.......sseeseeeceecees about 5 6 3. Stone called “Greenstone”, in firm beds, whichare quarried for building; upper surface 9 0 irregular; contains Gryphea vesiculosa, Pectens, and shark’s teeth ........ about This stone is valuable from its not being affected by frost. It can therefore be dug at any season, and stands well in water, as the foundations of bridges, and in exposed situations, as in copings, &c. 4. Stone; but not good ......-cccsceesscne Sinlaisle.c/atetoc/elsials) stolo/eiateleuaerar: cocccens) tn 5. Sand; depth unknown. On the north of the valley, the Upper green-sand appears likewise to consist of two portions; Dr. Firron on the Strata below the Chalk. 247 that which immediately succeeds the chalk, the equivalent of the fire-stone of Surrey, and the Malm-rock of Western Sussex, abounding in chert. To the lower portion the term Green-sand is strictly applicable, as it is composed of sand, and abounds in green particles. About two miles west of Ridge the sands suddenly expand and occupy a large space from the north of Fonthill Abbey to Stop Beacon, where the surface is strewed with fragments of chert, the remains, probably, of the higher beds which have disappeared. But further west, between the Abbey and East Knoyle through Middlemore, the ridge again is narrow and highly inclined ; but so much reduced in height, that the chalk of Hindon can be seen over it from the flat country at the mouth of the vale. The sands again expand a little on the west of East Knoyle; but at Upton their dip is not much less than 40°; so that the horizontal section occupies but a few paces, and on the north the chalk is seen at a lower level, connected by insensible gradation with the sands, (129.) Gault.—The clay beneath the Upper green-sand seems to be co- extensive with that formation. It forms on the south of the Vale of War- dour a rapid slope; on the north, a depression, immediately below the sand; and is identified in several places with the gault of the eastern coun- ties by the characteristic fossils. At Lower Donhead, under Lidhurst, it contains Ammonites with coproid masses of phosphate of lime; and at Ridge, where one of the most distinct sections is exposed, many other fossils have been found, the clay having been long used for tile-making. The beds all dip to the north, between 6° and 7°; anda well has been sunk through the clay, and a thin bed of sand beneath it, down to the Purbeck strata ; the order being thus :-— Section at the Tile-pits, Ridge. South. Purbeck Upper Green-sand. North. Stone-pit. Sand. Gault. Tile-pits. Well. QE | =) Feet. coe j ——— 100 715 =e 15 = SS = Ft, In 1. Upper Green-sand, at the upper part of the hill, consisting of— a. Green-sand. b. Green sand-stone, full of Gryphea vesiculosa at the upper part......8to 10 ft. PPCRPEEMASIU SANG: 6 ole\e seine sencle selec nes clsisteeecisiene cs cces --more than 30 d. A bed called by the workmen “ malm-rock ”; sand with stems of Siphonia and impressions of Ammonites ....0-eseeceesscrecceccessees -about 100 0 2. Gault, including near the top a bed of pyrites, shot through with veins of calcareous spar, of which some large crystals are found here. The rest is clay* containing 75 0 Ammonites, and other characteristic fossils, with Septaria and ovoid concretional magaces Of phosphate OF ME ....-secneccesscesrecvesscnsecscesvascesscccs * About 3 feet of clay, which occurs on the north-west of Ladydown, may belong either to this stratum, or to one of the beds subordinate to the Purbeck formation. VOL. IV.—SECOND SERIES. IK 248 Dr. Firron on the Strata below the Chalk. 3. Sand; (perhaps the representative of the Lower green-sand) said to be like that of 15 the hill top. Masses of a calcareous conglomerate in the upper part ..+..+-seee- 0 4, Fissile stone ; some of the upper beds of the Purbeck series :— a. Slaty limestone, abounding in Cypris and Cyclas, with smooth Paludinz, and another acute spiral univalve. b. Fine-grained oolite in uniform globular particles, like the roe of fishes. (130.) Lower Green-sand.—This formation is nowhere prominent in the Vale of Wardour, and scarcely observable throughout the greater part of it. The ferruginous sands below the gault in the eastern portion of the valley may not improbably be referable to some of the Wealden sands; but on the road descending from the Pembroke Arms to Catherine Ford, a bed of greenish sand occurs below the gault, which seems to be superior to the Wealden strata; and if this be continuous with a bed of sand which appears at Penthurst and Fovant, it must belong to the marine beds; as I found at the former place a Pecten and the stem of a Siphonia. Ochreous sand, with some blue clay, to a total thickness of five or six feet, occurs likewise above the Purbeck strata at Totterdale (Totteridge of the Ordnance Map),—a height on the south of Tisbury, to which I shall hereafter have occasion to refer. On the north side of the valley, sand of the same doubtful character occurs immediately below the gault ; but a bright ochreous clay, in a corresponding place between Apsell and Chicksgrove, is in my notes referred distinctly to the Lower green-sand ; and a part of the sands from Fonthill Abbey to Stop Beacon, may also belong to the same formation. On the whole, however, the difference between the bulk of the Lower green-sand here, from that which it exhibits in Kent, Sussex, and the Isle of Wight, is very remarkable, and accords with the rapid thinning out of the formation westwards, on the coast of Dorsetshire and Devon. (131.) Wealden.—The indications of the upper members of this group in the Vale of Wardour are likewise indistinct, nor did 1 find here any of their fossils ; but where the strata rise slowly from beneath the gault on the east, under Fovant Wood, and thence by Catherine Ford and the sloping ground towards Dinton and Teffont Magna, (PI. VII. fig. 3; and Pl. X.a., No. 13.) are traces, probably, of the Weald clay and Hastings sands; the pond at | Dinton Parsonage, especially, resting on a bed which answers well to the site of the Weald clay. ‘These indications deserve notice, as they furnish the only instance with which I am yet acquainted, of the occurrence of the upper members of the Wealden in the interior of England. The place where these strata may be looked for with the greatest chance of success, is on the descent from the plateau of the Upper green-sand to Catherine Dr. Firron on the Strata below the Chalk. 249 Ford; and their existence is rendered more probable, by the distinctness with which the connected strata of the Purbeck group are developed ; the whole series apparently thinning out towards the west. (132.) Purbeck Formation.—The Purbeck beds rise from beneath the sand and clay at Dallard’s Farm, near the eastern angle of the Vale of Wardour ; and from that point they can be traced,—on the south of the Nadder, at least as far as Totterdale, south of Tisbury ; and on the north, to Ashley Wood, west of Ladydown, or perhaps to Stop Street, a hamlet above the village of Fonthill Giffard ; occupying also the greatest part of the inter- mediate heights between these extreme points. The strata throughout agree with those of the coast ; their fossils, with the exception principally of oysters, belonging to freshwater genera ; and at the lower part near their junction with the Portland stone, they likewise include beds of clay alternating with limestone ; one of which at least contains the trunks of silicified trees. The abundance of marine shells in the Portland beds immediately below, is here as remarkable as in the Isle of Portland. The Map and Sections, PI. VII. fig.3., and PI. X.a., fig. 13. aB &c., show the general relations of the Purbeck series. The principal quarries open, in the upper part of this formation, when I examined the country, were at Dailard’s Farm above mentioned ; at Dashlet on the south of the Nadder, about mid- way between Catherine Ford and Chicksgrove; and on the opposite bank of the river, at Teffont Evias and near Legh-barn. ‘The junction of the Purbeck and Portland strata was best seen in a quarry at Wockley, on the south-east of Tisbury, the counterpart of a much larger one, worked some years ago at Chicksgrove (or Chilmark) Mill, but now obscured by decom- position from long exposure. At Dallard’s Farm, the beds first seen, on the west of the upper green-sand and gault, were thus :— Ft. In. Ft. In. 1. Soil and Grass. 2. Yellowish brown ferruginous loam, or clay......-cceccccercceccvccrers bo56 3. Slaty stone and clay, including seams of fibrous carbonate of lime : a. Slaty limestone, containing Ostrea distorta, Pl. XXII. fig. 2. ......000. 0 6 b. Fissile whitish calciferous clay, called “ Spangle” by the quarrymen, in- onic cluding great numbers of a small Modiola ........eeeeeeeseeeesecs ce. Whitish uniform limestone, including Corbula alata, Pl. XXI. fig. 5., like aLt9 Benmmenr thecoash at Upwayie tie ists ciels O25. £101 safe ois whisicle elsiew werele ois d. Fissile clay..... Rateithls will hes jota vie atktal s Slaieiiara\uiatele)a cis »'owletdialdiditidie 6a ly 0 e. Clay ; somewhat like d, but more approaching to stone ......s.+..04- 0 6 J. Fissile clay, like ‘‘ Spangle ”, with Modiolz, like those of b. ........0+ e510 4 6 Ke? 250 Dr. Firtron on the Strata below the Chalk. Ft. In, Ft. In. 4. Slaty limestone in firm beds, alternating with blue fissile clay : a. Rough and irregular above ..... eoe vane a)ieisle)6 6101 s)is\¢ 0010 6 coeee-6in.toO 9 b. Stone; firm and durable, abounding in Cyclades;—within the valves of which are deposited beautiful casts of a small species of Cypris. See } 3 LAGOON ly Ha, 7/5, ei area Bobo BUH OUD OOCT OO Oma OO Nd GUC" Soc amaoae z 8 5. Alternations of very blue fissile clay, with thick slaty stone, containing Ostrea Le ABSLORLG tra) atten Hele) ste s foliniole sl vie o: = slelstetekclolercheieinicysley = miei ict heii Os Stones contac! Gowen GAdoaoc5 60 4g05064cs0000000050005 visible 2 0 These lower beds are of different tints of blue and gray ; the gray by exposure becoming white, and the blue portions graduating into a hard, somewhat splintery stone, which in some spe- — cimens might be taken for limestone of the carboniferous series ; some of the slaty strata alter- nating with clay (3 above), consist of worn, rounded, fragments of shell and of stone, and are very like some of the upper beds of Bermuda. The outer surface of the more uniform lime- stones is here much eroded by the weather; and when the masses are split, the natural partings are frequently found to be furrowed or eroded with tortuous irregular channels, from half an inch downward in diameter. The pits along the south bank of the river, where the Purbeck series emerges from beneath the heights of sand, afford several good sections ;—very much alike, and fairly represented by the following detail of one at Dashlet. (See the Map, Pl. VII. fig. 3.) Section of the Stone-pits at Dashlet. 1. Brown, loam-like clay, including, or passing into 2. ........ee seve eeeeee ie 2. Concretional, but nearly continuous masses of soft stone, with layers of Cy- 0 6 clades and Cypris, and oolitic particles .......sessseesseeeescvons about The oolitic particles, when decomposed, leave empty cavities in the firmer cement, which might be mistaken for casts of Cypris. 3. Fissile stone, in irregular beds, almost entirely composed of Cyclades and 1 3 OniretMreigu gue sooeaddcuoddn cdcd Udad 860s 55 SoC eR MOBMenED SSou goo 4. A group of clay and limestone : a. Thin slaty, calciferous clay, including b. ........+e+seeeceeees cstce) Ob Re b. Delicately fibrous carbonate of lime, with impressions of Cyclas media 0 2 on the surfaces adjoining the clay ; the beaks unusually sharp ........ Cc. Clay Pee eer weer cree reese reser sess rereesessesesesesssssses Op 1. 3 d. Flattened roundish masses of uniform white and gray stone, imbedded 0 4t- ue in the clay of c. and d.; vertical cracks within, as in Septaria ........ 1 6 FAI OWINS WEAF oa d045 qopoouc cod OnODBOIIBA saoUoGdoOOKI ODDS lin. to. 05 2 J. Fibrous carbonate ’ordumerrerysc): +/<'<). + 87 sie iohep sis « pista yt Geta ele 0,1 ie. Fissilevclay, caleticroussbelowsmoenel-\>micfacsis,c%)-feise cists = eyelet ete lin, to J0556 5. Compact limestone, in some places bluish, containing very large Cyclades 1 4 (C. major); a large flat bivalve (Unio?); small bones and palates of fishes ; } to and fragments of Ostrea distorta, Pl. X XUN. fig. 2.0... cane « occ clecie scissile 1 6 The slaty limestone in the pits hereabouts affords the same beautiful casts of Cypris as are found at Dallard’s, frequently inclosed within the valves of Cyclades, of which, in fact, the beds are almost entirely composed. In other cases the surfaces of the strata are covered with im- pressions of a small Modiola. The clay is often divisible into fragments, which are polished, as if by friction under strong pressure. Dr. Firron on the Strata below the Chalk. 251 Some of the beds of uniform whitish limestone, to which the workmen give the name of “ Lias”, very much resemble the stone of Monte Bolca; and where most compact, are so like the stone used in lithography, that their application to that purpose seems to be well deserving of trial. The exposed edges of the thicker folia are eroded deeply into spongiform cavities. In some of the pits, the limestone, alternating with clay, has the appearance of united concretions or lumps; but within the stone is uniform, the aspect that of freshwater limestone, and the fracture splintery or very flat conchoidal, resembling a rock found in a corresponding place at Gar- sington near Oxford, which is there called “‘ Malm”. The masses split into irregular flakes at right angles to the surfaces, not more than a twentieth to an eighth of an inch thick. Both the clays and limestones in this part of the Purbeck series have sometimes a bluish colour; and both inclose large specimens of Ostrea distorta. On the north side of the valley, as the Purbeck strata rise more rapidly, the sections are not so much expanded; but about Teffont Evias slaty limestone, alternating with clay and fibrous carbonate of lime, is seen not far from the gault, dipping about north 15° west, at an inclination between 2° and 4°. A thick coating of these strata invests the heights thence to Ladydown, (see the section, Pl. X.a., fig. 13. aB.); but about midway to that place, it is cut through by a natural ravine, which runs from Chilmark to the Nadder at Penthurst Bridge, and not impro- bably may have originated in a dislocation. The Portland beds which form the lower part of the ravine have been extensively quarried on both sides. At Ladydown, near the highest ground occupied by the Purbeck formation, quarries have long been worked to great extent, chiefly for the sake of the fissile cycladiferous stone, like that of the Isle of Purbeck, which here bears the name of “Tilestone”. Among these beds is a group which abounds in the remains of fishes. On the south of the Nadder, near Benston, a prominence, like a step at a lower level, extends beyond the sands and clay which form the upper part of the hills, and is continued to Wockiey and the west of Anstey Water, capping the height occupied by Totterdale Farm, where the Pur- beck beds run out. In the lower part of this projection, a large quarry was for many years worked at Chicksgrove Mill, and another more recently at Wockley ; the bottom of the former is nearly level with the river; the top about 50 feet above it, and about 30 feet lower than the top of the prominence above mentioned. The total thickness of the Purbeck strata indicated by these data does not exceed 60 feet. A few beds occur in the upper part of the section at Chicksgrove, which do not remain at Wock- ley ; but the rest are so nearly the same at the two places as not to require a separate detail. List of the Beds at Chicksgrove Mill, and Wockley Quarries. BE ine) Eitsain, Chicksgrove.— Fn a yl all «gol gama he Deeg dh: Sa Ree Meh IE about 0 9 1, Loam; including fragments of stone, like the “lias” of the pits above men- Ris Ge Peale da ioteys vial helenae SE SOONOOL POETS ASSN about =» bluish clay, passing into 3..........-...- capotovee he sesey OU to Om. (OO 3. Yellowish brown, tough clay, very uneven at the bottom; filling up the ir- 6 Lop RE CT a ie on hair ale I a i a a B56 ges ot Oita 2 0 nearly continuous ; in many places having the aspect of magnesian limestone, 4. A bed of coarse, somewhat gritty limestone, very irregular in thickness, but and containing nests of carbonate of lime in rhombic crystals.....1 ft. to 3 ft. or Sc 252 Dr. Fitton on the Strata below the Chalk. Ft. In, 5. A bed, likewise very irregular, consisting of— a. Brownish clay, at the upper part. b. Cavernous concretions or crusts of carbonate of lime, in the form of irre- gular flakes ; which in some places have a deceptive appearance of or- ganic structure. This bed accommodates itself to the inequalities in the surface, both of 4 above and of 5 below it; and seems to be a mass of loose loamy clay, shot through by stalagmitic carbonate of lime....... . 6. A bed much decomposed, and very unequal in thickness: apparently consist- ing of soft, calciferous clay, with some portions of firmer limestone ........ All the preceding beds seem to be above those of the Wockley Quarry. 7. (Apparently the same with 2. and 3. of Wockley.) Irregular portions of limestone, very indistinct from decomposition ; sometimes wholly wanting; sometimes in the form of thin slaty beds waving over the inequalities of the Clay (8:) below 222 ss silat eflelelsleieleles lelele clsivivie o'eisie 1 ft. to 1 ft. 6 in. The whole thickness from 4ft. to 7ft. inclusiveis........ about 8. Tough clay, (seems to be the same with 4. of Wockley). Wockley.— Grassy surface. 1. Ferruginous loam and sand, filling the irregularities in the top of 2.....6 in. to 2, Compact limestone, much decomposed, but in the fresher pieces mottled, grey and bluish. At the bottom this bed is divisible into flakes or thin strata, curved, or waving; very like the lower part of the “slate” of Portland, and the fissile beds above the Portland stone at Bacon Hall, (p. 223.) (Que. | thet Soft Burr,: or “Bacon-ledge |’)s.c' sie 1 « -\<1-'+ <6 ws+» 1 ft. Gin. to 2 ft. J is) . Decomposed whitish, fissile limestone ; passing at the lowest part into 4., and very nearly resembling the “ Cap” at Bacon Hall .............. about 4, (8. of Chicksgrove Quarry.) Tough dark clay, in some places very like Fuller’s-earth : seems to represent one of the “ dirt beds” of Portland and the coast near Lulworth, but is more uniform, and does not contain fragments of SEOME Wafetets lolol elect tele oiskeye fav oleh re feteteictetehofer «6 BbddocgoadHosdn d. Irregular concretional masses of black flint, rugged without anew de- tached ; not in themselves distinguishable from chalk flints ......... — c. Fissile calcareous matter, in beds of unequal thickness, curved at | 0 10 o>) . (10. of the Chicksgrove section.) Fissile, somewhat gritty limestone; at top } enveloping the flinty masses 5.d.; below adheringto7. This bed at the upper | part contains casts of Cypris in great numbers. ‘The proprietor of Chicks- grove Quarry told me that fishes, like those of Ladydown, were found in this r part of the series, both there and at Wockley; but the specimens which I | could obtain were much smaller than those of that place...........00..00+ J Ft. In. 6 0 1 0 heag 2 6 2 Dr. Firron on the Strata below the Chalk. 253 Bein, «Et. Its 7. (11. of Chicksgrove.) Uniform, soft, very white limestone, here called “chalk”; but abounding at the upper part in Portland fossils: Pecten la- mellosus, Cardium dissimile, Trigonia gibbosa, Ostrea expansa. This bed is not fit for building, and is burnt into lime: it seems, nevertheless, to represent | the “ white-bed ” of Portland, though without oolitic structure ..... 8. (12., &c., of Chicksgrove.) From 7. to the bottom of the quarry, a depth of about 25 feet, in 8 or 9 beds, is called ‘* Freestone ”: the detail as follows :— a. Whitish stone, called ‘‘ chalk”, of uneven, subconchoidal fracture ; con- taining great numbers of Pecten lamellosus and Cytherea ..... a eevee Z b. Cream-coloured, somewhat sandy stone, also with Pecten lamellosus.... 2 6 o ce. Similar stone; T'rigonia gibbosa, Cytherea, Pecten lamellosus. Sometimes 3 6 this bed includes 5 to 8 inches of sand ..... setolelhetetetiol oreheveharahets 2 ft. to d. Concretional stone and sand. MIEIICIDN 72°52 cidoierstel(ete sta clalass Avia sidlisi ais aierleaingan,d 0 0 tol 8 iil. Sand, separating and surrounding the concretions of i. 4.0 .t0.2.96 about — 4 0 e. Stone and sand :— MAC ONCKEHONALSEONE: «4, < 6,sj0 0/2, 6 « oe. es SA ss WE Z = OG Chert. \\ o> CX ee aa 1. Represents the Upper Chaik. Feet. 2. Chalk Marl, here called ‘“‘ Malm”. In this a well had been sunk, which afforded the following strata, by report of the well-sinker :— a. “Malm”; like the chalk-marl of Lewes in Sussex, full of the characteristic : 5 ‘ 100 fossils: ‘sharks’*teeth in great abundances)... <2). « sin vfelvieeeinsisinin cd stsnce O 4 See sami PUDBIy WaTl SL ee ee tielele a ncelscacsscpeieisccvgissiceslessseseces & O [ Portland. | 4, Very hard brown sandstone, with a few Trigoniz, anda bone of a crocodile ........ 1 0 “5, Rubbly stone, with numerous casts of Trigonia, the shells having decayed into a 1 0 SECT HOWL: « 5 055 10+4,'nrp ie} 4501 0p \010! oe 00:0) 450 5a apeloieie ia, 0 Djayaye ways werbie weicile 3.0 2 b,9.0m,0.0\0 SOI Totals Ai Ree he hes kislatetarel steve steers umvate 10 0 The first three beds exactly resemble the sandy strata which extend from this point to the top “ of the hill, a height of about 50 feet, and which I am disposed to regard as belonging to the “ Wealden group. The nodules of ironstone containing the supposed freshwater shells, occur at a “height of about 30 feet above No. 4.” Purbeck Strata.—What remains of the Purbeck strata in this part of the country is best seen in the pits in the southern part of the Shotover range, at Combe Wood and Garsington. The junction of the incumbent strata with the Portland beds, is first disclosed in the quarries at Great Hazeley. The section at Comzz Woop consists of,— 1. Reddish loamy soil, passing into 2. 2. Ferruginous sand (Lower green). 8. A thin bed of very tough clay (Fuller’s earth?); which, with 2, enters into, and follows the deep erosions and irregularities at the top of 4. 4. Purbeck.—Stone, and soft rubbly matter ;—(the ‘“‘Malm” of the pits at Garsington); containing freshwater shells, like those of that place:—Cypris; Mytilus, two species; Modiola; Paludina elongata, and perhaps another species?; Planorbis/?. Some portions of the stone are compact and uniform, with the usual characters of freshwater limestone ; others, though containing the same fossils, are composed of grey and brownish, fine-grained, oolite, in which a very small 276 Dr. Frrron on the Strata below the Chalk. univalve—perhaps a Paludina—occurs in such numbers, as in some places to form nearly the whole mass. 5. Portland stone; with numerous Trigoniz and Perne. Great Hazeley.—In the principal quarry at this place the strata dip to about 20° east of south, at an angle of about 4°; and are traversed by joints nearly in the same direction. The order is as follows : Stone-pit at Great HazeELey. WUHTE di er we all Ge WME ws , ny Mp veal 5. STEN ial 15. 20. 1.. Soil, forming a level and uniform surface 2... +000 e0cncsescesccevscs se ce cle iE 2. Loam, brown and red ; containing fragments of ferruginous conglomerate, (carstone) 6 on and ofa brown substance, like umber; passing below into ferruginous sand. . 3 ft. to 8. Thinly stratified firm clay or marl, of a light grey colour, approaching to stone, not effervescent, containing between the folia impressions of plants, and including portions of reddish sand, in horizontal masses of very unequal thickness. It breaks down 6 6 rapidly in water, like Fuller’s earth, and its place corresponds best (so far as my observations went) to that stratum) feist «nla sic loinie «> = +\0\lc «01s ois! 010) ofe) oleo)=teln leita 4, Dark brown clay; like the Fuller’s earth of Tilburstow (p.139.), and of the pits near Aylesbury. Some of the masses into which it is easily divided, are polished, by sliding on each other under pressure. At the bottom ferruginous sand alternates With) the Clay. are isi< tals oletelolaler= iain wleielarele aiwiclolalefolole\'e aus oiels e/einjeicleiteheielr oj at or op av ov ever sy even, ove; 0 Shsiatlohetedaye’ ala “of otanetelfateyc) steteso.b “ale ters inte Oe ate MipmGroodestone, called “ Buzlders”’ often bIWISh), ...<,0.0,5.0,0.0,9,0.0,010.0,000,0 0,9.0,0,0.0,0,9,0,0,0,0 66 24.6 Bottom of the Pit. Total about 10 ft. to 12 0 Pits at the top of Quarntow Hix1, About a furlong east of the Ordnance Station, which is 754 feet above the sea _ Beds inclined towards the south at about 3° 30'.—See the Transverse Section, Pl. X. b. fig. 10. [Lower greensand, and Wealden? ). 1. Red sand, with concretions of hard ferruginous conglomerate ; ochre at the bottors :— visible about 2 0 2: a. Clay and sand; brownish and grey, in thin alternating flakes ....about 1 6 b, Fuller’s earth ; wax-like, as at Brill, (4. p.280.) .......- Vile serose) YO Or. 298 2p2 290 Dr. Firron on the Strata below the Chalk. Ft. In, 3. White, and brown, sand and clay .............- 6BTb Sige lae.lg > ‘oie 'ote bib pleflone halls 1a en 4, Alternate beds of white, reddish, and yellowish sand, and thin courses of grey clay A to 6 0 5, a, Dark brown clay, called here “ Black Dirt”. .......00++00++.--about : 1 0 b, Alternate beds of tough grey clay and sand........ ata cca apeverstenets atecats 6. Greenish sand, said to be 6 feet thick ,..........- ai sinteeveteeofetentneiens socccajeketctateteetene Totalicicc.cavetac .+...-about a 0 The beds next below are obscure, from subsidence: the order was stated to be as follows :— i. selaemairt «tough dark (clay \. ssipalatetepn'e/oiohs mieievatera tates about 2 0 [| Purbeck. | 1. a. Light yellowish grey clay, passing into stone ...... mielsiatelatalefelshetecsierets 1 Ol, b. Rubbly limestone... 2... .cesccceccepesecesccvences Manca bee a5 O29 [Portland Stone. | 2. Soft, uniform, marly limestone, abounding in fossils ;—Ostrea expansa ; Pecten lamello- | 6 sus, Buccinum naticoide, Pl, XXIII. fig. 4, Perna alia Pleurotomaria, ee Venericardia, and large Ammonites ........ john ospabonrounosnc0060- 4 ft. to * Moor Hill, a height about a mile and a half north-west of the village of Quainton, has a nearly horizontal top; and, not improbably, is capped with Portland stone or sand. + Smith’s map of Buckinghamshire represents the Gault as extending to the north-west from between Hulcot and Wing, as far as Cublington and thence to Cottesloe. If this be correct, the Portland beds may exist ‘within that space, at a depth below the surface at least equal to the thickness of the Lower green-sand in this part of the country: but the map near Aylesbury re- quires much correction. 292 Dr. Firron on the Strata below the Chalk. Ft Im 3. Uniform, yellowish-grey sand; precisely resembling that which includes the la o- called “ Les Grises” in the quarries near Boulogne....... Sasso cies . -visible about {Portland Sand. | 4. Hard, dark brownish-grey stone, of irregular thickness, containing Perne. Appr 2 e ing to the nodules of Shotover........+-sseeeeeees sie io ajo ieue byateteks piekelatey eel . Bottom of the Quarry. a 5. Below is green matter, used to form the floors of barns ; not visible here at present, but —__ well seen near Dunton. In a pit at Dunton, the equivalent of the bed 3. is only three feet thick ; and that of 4. consists” of rubbly calcareous stone, alternating with sand, the whole full of green particles, with small pebbles of black flint,—at the bottom of which is a continuous bed of greenish stone, about 2 feet thick, with dark particles, containing large Ammonites, Perna quadrata, and many other fossils. The equivalent of 5. is tough green matter, apparently the same with that which gives the greenish hue to the stone. This has been dug to the depth of about 3 feet. ‘oo Kimmeridge Clay.—This clay is sufficiently characterized, at several points near Aylesbulga by its occurring immediately beneath the Portland sand, and by its fossils. On the north- west of the town, towards Bierton, it appears beneath about five feet of brownish sandy clay, E (Portland sand?,) which includes numerous fragments of flint; and it contains Septaria, with Ammonites. The tiles made of it are of a full red colour. Thence to the entrance of W! hitchurch on the south, the road appears to be cut wholly in the clay: but there are variations in the hue c of the beds exposed along the road, and perhaps some alternating layers of sand. In descending to the streamlet south of Hardwick, were iridescent fragments of shells, with Gryphea (Exogyra) virgula, (Pl. XXIII. fig. 10), and Aptychus, (Pl. XXIII. fig. 11), in the ditches at the road-side. At Quainton, clay forms the slope of the hill beneath the stone-pits ; and a well had been dug, at Pi cet the village, in clay, to the depth of 60 yards; among the fossils brought up from which, were Pinan beautiful specimens of Ammonites Gulielmi, like those obtained, along with 4. biplex, from East Claydon, about three miles north of Quainton, where they were found about 20 feet deep in clay. , The clay-pits beneath the hill at Stewkley, about midway between that village and the Warren above mentioned, also afford Aptychus, and Exogyra virgula; with compressed Ammonites of the Kimmeridge clay, and a species supposed to be new. (153.) Section No. 21,—from Dunstable through Hockliffe to Woburn;— and No. 2\', Hockhffe to Fenny Stratford—The tract occupied by the strata below the chalk, from Aylesbury to the coast of Norfolk, is even less know mn geologically, than that between Buckinghamshire and the south-eastern coast; the maps of Mr. Smith and Mr. Greenough, and the general descripti yn of Messrs. Conybeare and Phillips being the only publications relating to it. The want of correct maps would alone have prevented the complete examina- tion of this district ; but this impediment will soon be removed by the com- pletion of the Gpdbance Survey from Bedfordshire to Cambridge. The fol- lowing observations indicate only some of the more prominent facts connected with the beds below the chalk. Dr. Firron on the Strata below the Chaik. 993 The series of strata in Sections 21 and 21’, differs from that of the preceding sections, principally in the absence of all the beds between the lower green- sand and the Kimmeridge clay, which are found in immediate contact, at the _ village of Little Brickhill, on the brow of the descent to Fenny Stratford : —this junction, which was to have been expected hereabouts, from the evident thinning out of the Purbeck and Portland formations in the north-east of Buckinghamshire, is continued thence, through Bedfordshire, into Cambridge- shire, and even to the coast of Norfolk. The great accumulation of gravel and transported matter, rising in several places into hills and extensively concealing the strata, is another circumstance which distinguishes the vicinity of Leighton Buzzard from the country towards the south-west, and renders the examination of the strata difficult or impracti- cable. A similar coating of gravel is found not only throughout Bedfordshire, and a great part of the counties on the north-east of it, but far to the east of the chalk escarpment itself*. The fossils, and stony substances, which com- pose this deposit, have been derived from many different formations, some of them very remote, and are deserving of attentive examination. My collec- tion includes only a few specimens from one of the ravines which descend from Little Brickhill, and from the Platform between Stewkley and Soulbury, about 510 feet above the sea, where the multifarious gravel includes frag- ments of granite, and a large proportion of chalk. This deposit does not there form an escarpment, like the sands at Brickhill, but declines gradually towards the north, in a series of lower inequalities: on the ’south and east, it occupies a great part of the surface towards Leighton, Wing, and Cub- lington. On the line of the Section, No. 21, the ridge of the chalk attains nearly the greatest height which it anywhere exhibits,—Kensworth Hill, south of the road near Dunstable being 904 feet above the sea; but the general elevation and that of the principal summits both rapidly diminish towards the north- east. Near Tring, the difference in height of the upper and lower chalk escarpments is strongly marked ; and the retreat of the former is still more conspicuous near Dunstable; but the boundary of the lower chalk is less distinct. The Upper chalk forms the elevated range from the Five Knolls, and Kensworth Hill, 904 feet, by the heights above Zouche’s Farm, 850 feet, towards Luton, and thence to Whitehill Farm, on * At Muswell Hill, on the north of Highgate in Middlesex, an accumulation above the Lon- don clay, includes worn fragments of granite, porphyry, micaceous sandstone, mountain-lime- stone, coal, lias, and chalk, with many of the characteristic fossils of those formations: the chalk especially being so abundant, as to give the whole a chalky character.—Mr. Spencer, in Proceed- ings of the Geol, Society, 1835—6; vol. ii. p. 181. 294 Dr. Firron on the Strata below the Chalk. the north of that village, and Lillihoe in Hertfordshire, an Ordnance Station 604 feet above the sea. The Lower chalk, on which the village of Dunstable is placed, runs from Totternhoe on the south-west of the main-road, through Houghton Regis, Upper Sundon, and Streatley, on the north-east of it. On the north-east of Totternhoe mines are driven into the hill at the bottom of the chalk, for the purpose of extracting a bed of uniform light greenish-grey, marly and sandy, firestone, from seven to ten feet thick. The strata are traversed by numerous cracks, which seem to pervade the hill, and indicate disturbance,—or perhaps the effect of subsidence. The Gault, in Smith’s map of Buckinghamshire, occupies a large part even of the higher ground between Whitchurch and Wing. The Lower green-sand runs out without interruption from Whit- church to Winslow, and is continued thence by Drayton, Parslow, and Soulbury, to the south of Leighton. On the north of that line, a denudation on the course of the Little Ouzel river having cut down to the subjacent clay, breaks in upon the outcrop of the sands, which would otherwise have been continuous from Winslow to Brickhill, and the mass of the Woburn sand-hills. Be- yond the two tracts at present continuous, several] outlying patches of sand, some miles distant from each other and from the general escarpment*, are ascribed to this formation in the map; all of which, as well as the wider tract between Winslow and Leighton, deserve examination, for the purpose of ascertaining whether any of the Wealden beds are to be found there. The greatest expanse of the Lower green-sand in the midland counties, occurs between Leighton and Ampthill in Bedfordshire ; rising, at the Ordnance station on Bow-Brickhill, to the height of 685 feet above the sea,—or about 430 feet above the lowest point in the valley on the west of the escarpment near Fenny Stratford. One of the most remarkable subordinate beds of the forma- tion in this neighbourhood, is Fuller’s earth, which, when I was there (in 1824) was brought out by mining from the north-west escarpment of the sand-hills, near Hogstye-end, between the main road from Woburn to Northampton, and that from Hockliff to Stony Stratford. Fuller’s earth Pit, near Woxsurn. Ft. In. 1. Sand; nearly uniform, greenish-grey, and yellowish, including consolidated masses 130 0 of sand-rock, and dipping to the east and south. ........++eeeee0+++++ about 2. Fuller's earth. a. “ Top” of inferior quality ; not diffusing itself in water till after it has ] been dried: unfit for the purposes of the clothier .............-05 3.0 | 10 b. Ferruginous? clay ......... Beto cesib is eet (ors, soecseceeseveevabout 0 c. Fuller’s earth, of the best quality, very light olive green; (sold at the | pit-mouth to cloth-manufacturers, for one shilling per cwt.) ..7ft.to 9 04 4. “ Bottom”; hard quartz or sand-rock ; the equivalent, probably, of the chert of the 5 0 Kentiand ‘Surrey sand-hillles ce pisitatia’ «le vlesfoitles bletn we btets bieyatave exe 2 ft. to . Sand, like 1; thickness not ascertained. or The Geological place of the Fuller’s earth is here, therefore, nearly the same with that of * ‘These outliers are represented on the Buckinghamshire map by patches of colour, each about half a mile in diameter, at Roundhill, Whaddon, Totternhoe, Wroughton, Milton-Keynes, Broughton, Moulsoe, and Astwood. In Mr. Greenough’s map, (1st edition,) both Winslow and the heights of Whadden Chase on the north of that town form a portion of the tract coloured as Oxford clay; but this, no doubt, requires correction. Dr. Firron on the Strata below the Chalk. 295 Nutfield described above (141.); which, however, is thicker than this of Bedfordshire, and is continued through a much larger space. I did not find here any of those nodules of sulphate of barytes, which are frequent in the earth of Nutfield; and in neither of these two situa- tions, does this bed contain the great number and variety of fossils by which the Fuller’s earth at the bottom of the Lower green-sand is distinguished, at Atherfield in the Isle of Wight. In the sands of this part of Bedfordshire silicified coniferous wood is frequently found in large detached pieces. These pits have continued to supply Fuller’s earth for more than a hundred years. They were described, in 1723, by Dr. Holloway, in a letter to the celebrated Woodward, which is remarkable in the earlier history of stratigraphical geology in England*: the author pointing out the paral- lelism of the range of sands, to that of the chalk in the Chiltern hills, and suggesting distinctly, upon geological grounds, the probability that other portions of the sand range would afford the same valuable material; which, we have seen, coincides with the result of modern investigation. The junction of the Lower green-sand and the Kimmeridge clay at Little Brickhill, (Section 21’ ) occurs at the north-west end of the village, in the garden of a small public-house called the King and Queen, on the south of the road. Copious springs break out on the road about 50 paces above this house. The clay, which is here of a dark blue colour, includes very fine spe- cimens of an Ostrea deltoidea, with Belemnites; and I was told that sand alternates with the clay for a short distance below this point. (154.) North-east of Bedfordshire.—The Lower green-sand, according to Smith’s map, passes through the whole of this county, in a band which is in general parallel to the chalk escarpment, and about five miles in width; but its apparent dimensions vary much, in consequence of the irregular en- croachments of the gault over the surface ; that stratum, immediately on the north of Section 21, extending northward from the little village of Heath, through Potsgrove and Froxfield, to Steppingley and Flitwick. Again, on the east of Ampthill, an insulated portion of clay, (the colour of which, in Smith’s map, is intended either for Gault or Kimmeridge clay,) stretches in a north-eastern direction from around Maulden to South Hill, crossing the great London road to Bedford, about the 43rd milestone. Since, however, the full development of the Lower green-sand in Bedfordshire renders it probable that the subdivisions of the Kentish coast may be found also in this country, it may deserve inquiry whether some of these detached por- tions, which have been considered as clay,—(especially between Maulden and South Hill) may not belong to the middle, dark-coloured, and retentive member of the sands; and the same question may be applied to a part, at least, of the remoter tract assigned by Smith to the Gault, on the north of Hockliff. ® This document has been inserted in Conybeare and Phillips’s “ Outlines”, p.138-9. Dr. Woodward himself speaks almost poetically of the value of the English Fuller’s earth ; which, he says, is beyond that of the Diamond mines of Golconda, &c. :—Edinb. Rev. 1819, vol. xxix. ; and London and Edinb. Phil, Mag. 18382, vol. i. p. 155. VOL. IV.—SECOND SERIES. 2e 296 Dr. Firron on the Sirata below the Chalk. The course of the upper chalk is prominent on the north of east, from Dunstable through Hitchin and Baldock, to Royston Down in Cambridge- shire, which is 464 feet above the sea: but the boundary between the lower chalk and the strata next below is not distinctly indicated by the external features of the country. The change occurs on the main road from London to Bedford, between Hitchin and Shefford, about the 37th milestone: and there the difference in the elevation and general appearance of the ground is very slight; in part from the very gradual rise of the strata, but chiefly from the general diffusion of a coating of transported materials, which con- ceals them. (155.) List of Fossils from the Beds between the Chalk and the Oxford Oolite, in part of Oxrorpsuire, Buckinenamsuire, and Beprorp-— SHIRE- [ Superficial Gravel. | Ammonites (fragments). Chelsey, near Leighton, Bedf. (From the Gault ?.) Belemnites minimus? (fragments). Stone Lane, north of Heath, Bedf. B——. Gravel-pit north-east of Stewkley, Bucks: with fragments of chalk; top of the high grounds, Brigginton, &c., near Leighton, Bedf. Gryphea dilatata (much worn.) Gravel-pit north-east of Stewkley, Bucks. G (fragments). Stone Lane, north of Heath, near Leighton, Bedfordshire. G obliqua (much worn.) Gravel-pit north-east of Stewkley. Ostrea deltoidea (fragments). Stone Lane, north of Heath, Bedf. Serpula. Gravel-pit, north-east of Stewkley. Terebratula. In rolled piece of sandy limestone. Gravel-pit north-east of Stewkley. Spongia? Flint, enveloping Sponges?: worn. (No doubt from the upper chalk.) Gravel-pit north-east of Stewkley. [Lower Chalk and Chalk Marl.] Ammonites lautus. In pale marly clay (chalk marl). Tetsworth, Oxf. Terebratula semiglobosa. 'Tetsworth, Oxfordshire : in flint. [Upper Green-sand. | Inoceramus. Between Tetsworth and Thame, Oxf.; with Vermetus, in bluish grey firestone. Mytilus (new species?). Between 'Tetsworth and Thame: in soft gritty firestone. Siphonia. Impressions of stems. Totternhoe, Bedf. Vermetus. Between Tetsworth and Thame: with Inoceramus; in bluish grey stone. [ Gault. | Ammonites decipiens. Compton, Bedf. Mr. Goodhall. Avicula. Compton, Bedf. Mr. Goodhall. Crenatula. Compton, Bedf. Mr. Goodhall. Dr. Firron on the Strata below the Chalk. 297 Exogyra conica. Compton, Bedf. Mr. Goodhall. Inoceramus sulcatus. Compton, Bedf. Mr. Goodhall. Nucula. Compton, Bedf. Mr. Goodhall. [Lower Green-sand. ] Siphonia, Casts of stem. Quainton pit, east of Ordnance Station: in the “ Bottom rock.” Wood, Coniferous, silicified. Woburn Sands, Bedf. [Hastings Sand?. | Cyclas, impressions of. Quainton, Bucks: pit at the highest part of the hill in grey calciferous grit, “‘ Hardstone.” Paludina elongata? Impressions. Same place and situation. Serpula?. Coney Hill, Bucks. In grey uniform grit,—“ Sandstone”’. [Purbeck Strata. | Astacus?. Whitchurch, Bucks. In freshwater limestone, “‘ Pendle”, with worn par- ticles like oolite. Astarte. Same place and situation. Cyclas media, Hartwell, Bucks; with Modiola. Whitchurch; with Cypris Val- densis. Weedon; in stone like the “ tilestone ’’ of Ladydown, and the “ slate” of the Isle of Purbeck. C. elongata. Whitchurch, Bucks. C—— parva. Horton’s Pit, near Bishopstone, Bucks; in slaty soft limestone. Bishopstone (Dr. Lee’s pits) in soft bluish stone. In great numbers at Weedon, in the “ Pendle”. Whitchurch ; impressions in freshwater limestone, with worn rounded particles. Quainton; Western Pit, in the “ Pendle”’. C— (a large species). Quainton, West Pit. Whitchurch, Bucks, Haddenham, Bucks: in slaty limestone. Garsington, Oxf.: in the “ Malm”. Cypris Valdensis?. Whitchurch, Bucks. Bishopstone, in soft bluish shale, Quainton. C—— (species uncertain). Combe Wood, and Garsington, Oxf.: in the “‘ Malm”’; with Paludina elongata. Denton, Bucks: in slaty soft clay. Weedon; in stone like the ‘‘ Tilestone ”’ of Ladydown, and the “ slate”’ of Purbeck. Ford, numer- ous. Horton’s Pits, Bishopstone in sub-oolitic ; stone: and in soft bluish slaty stone, at Dr. Lee’s pit. Southwarpe. Quainton. Whitchurch. Limnea?. Garsington: in the “Malm”’,—the representative of the “Cap” of Port- land. Melanopsis?. In dark-brown clay above the Portland strata. Road from Whitchurch to Winslow. Modiola. Remains of two or more species, one deeply striated. Garsington and Combe Wood, Oxfordshire: in the “Malm.” Hartwell and Bishopstone, Bucks. Southwarpe: in soft fissile limestone. Whitchurch. Quainton: a small species in tough sandy clay: in the bottom of the “‘ Heath’’, over the “‘ Pendle ”’. 292 298 Dr. Firron on the Strata below the Chalk. Mytilus Lyellii? Pl. XXI.f.18. Bishopstone: Dr. Lee’s pit. Near Whitchurch, on the road to Winslow: numerous; in light greenish grey, alternating with dark, tough clay, over the top of the Portland strata. Another species, smaller and narrower than M. Lyellii. Combe Wood, “Malm”. Dinton, Bucks. Bishopstone. Horton’s Pit; in slaty soft limestone. Dr. Lee’s pits. Weedon. Whitchurch. Quainton. Ostrea expansa. Horton’s Pit, Bucks. (Qua. in Portland-stone ?) O—— (thin-shelled). Combe Wood: ‘ Malm”’. O— (fragments of another species). Whitchurch, Bucks; in the “ Pendle.” Garsington, Oxfordshire: “ Malm”’. Paludina elongata. Combe Wood, and Garsington: in the ‘‘ Malm”; casts, with Cypris. Southwarpe, Bucks. Bishopstone, pit near Morton’s. Impressions of another species? Southwarpe, Bucks. Horton’s Pit: in freshwater limestone. Quainton: in the grey uniform grit; Que. Hastings M- Je sand. (a ribbed species). Garsington and Combe Wood, Oxfordshire: in the ‘“¢Malm’”’. Planorbis. Garsington and Combe Wood, Oxfordshire: casts in the “Malm”; Horton’s Pit, near Bishopstone, Bucks. Potamides carinatum. (Melanopsis, Min.Con.) Horton’s Pit, Bishopstone, Bucks. Psammobia?. Garsington: “ Malm”’. Unio. Bishopstone, Dr. Lee’s Pits: in soft bluish slaty stone. Quainton.* P. Fisues. Bones; impressions only. Southwarpe, Bucks: in soft earthy fissile lime- — stone. Vertebre. Whitchurch, in freshwater limestone, “‘ Pendle ’’. Coney Hill: in calciferous grit. Scales. Bucks: Bishopstone, Ford, Horton’s Pit, in oolitic stone: Dr. Lee’s pits; in soft bluish slaty stone. Whitchurch in the “Pendle”, with worn roundish particles. Quainton: pit top of the hill; in the “ Hardstone”. Reptives. Portions of a spongy bone, probably Saurian. Garsington, Oxf.: in the ‘¢ Malm’. Priants. A specimen, represented in P]. XXII. f.11., the nature of which is still doubtful. It was bought at Quainton, Bucks, and said to be from the stone-pits at the hill-top; but the precise place was unknown. Nort siliceous: effervescing with acids ; and in this respect different from the Cycadee of Portland. * Besides the shells above enumerated, the following were found in the strata representing the fo) Purbeck series, within the tract now under consideration; viz. Bivalves—of two or three species probably new, but too indistinct to be determined,—at Combe Wood, Oxfordshire; Bishopstone, Weedon, Whitchurch and Quainton, Bucks. Spiral univalves—at Garsington and Combe Wood, Oxfordshire, (specimens exhibiting beautifully the internal column of the shell); at Great Hazeley, Oxfordshire, with oolitic particles; and on the road from Whitchurch to Winslow, Bucks,—(a new Paludina ?) Dr. Firron on the Strata below the Chalk. 299 Impressions of very narrow leaves. Great Hazeley, Oxf. ; in fissile clay, re- presenting, probably, the Fuller’s earth of the Lower green-sand. Trees. At Brill, the trunk of a large tree converted into lignite, was found in bluish grey clay. A most remarkable specimen, 40 feet long ; at first entire, with numerous branches; but when I saw it, split into small fragments from de- composition of the pyrites. Wood. Coniferous, silicified wood, precisely like that of Portland, is found in fragments, in the “ Malm’’, at Garsington, above the Portland stone, and along with portions of freshwater limestone. [Portland Stone. ] Ammonites biplex. Road near Walton turnpike, Bucks. A—— giganteus. Oving and Dinton, Bucks: with Exogyra nana, in sandy stone. A Langcombe, Oxfordsh. Great Hazeley, Oxf.: in grey concreted sand. The Warren, near Stewkley, Bucks: in limestone. Arca (new). Stone-pits west of Great Milton: a cast in oolitic stone. Astarte cuneata. Beneath Garsington, Oxf.: in concretional stone. Brill, Bucks: in hard compact limestone. Buccinum naticoide. PI. XXIII. f. 4. Whitchurch, Bucks. The Warren near Stewkley ?. B——. Quainton. Cardium dissimile. Quainton, Bucks. Brill. Long Crendon: a cast, in grey, very sandy stone. Bishopstone, Moreton’s pit: a cast. Tring, road near Walton Turnpike. The Warren near Stewkley. Cytherea? rugosa. Pl. XXII. fig.13. Southwarpe, Bucks. Exogyranana. Dinton; Bucks: with Ammonites giganteus: in sandy stone. E——. Whitchurch: adhering to Pecten lamellosus. Gastrochena?. Denton, Oxf. : perforating Perna quadrata. Garsington: with Pecten lamellosus ?. Gervillia aviculoides. Langcombe, near Oxford: in calcareous spar. Gryphea dilatata. Langcombe. A young shell; in Portland stone ?. Lucina Portlandica. PI. XXII. fig.12. Southwarpe, Bucks. Modiola (large). Denton, Oxf. Whitchurch, Bucks: in white stone. Mytilus. Whitchurch. Natica elegans. Pl. XXIII. f.3. Great Hazeley; a cast. Ostrea expansa. Bucks: Village of Stone; Whitchurch, with Pecten lamellosus ; Quainton; Brill; Horton’s pit, near Ford; the Warren near Stewkley, Bedf. O—.. Remains ofa thick-shelled species are found at Great Hazeley, Oxf.: in con- cretions of gritty stone, in yellowish sand. Haddenham, Bucks. Dinton, with Plicatula. Panopea depressa. Brill. i gibbosa. Brill: a cast. 300 Dr. Frrron on the Strata below the Chalk. Pecten lamellosus. Oxfordshire: Denton, with Trigonia gibbosa; Garsington, with Gastrochena. Bucks: near Towersey Windmill; Brill, with Exogyra, adher- ing; Quainton, pit east of Ordnance Station,—in soft limestone ; Whitchurch, with Serpula, &c., in white stone; The Warren near Stewkley. orbicularis. Oxf.: Beneath Garsington; in concretional Portland stone, with Astarte cuneata; Langcombe, with Trigonia clavellata, in sandy stone. Brill, Bucks. Perna quadrata. Oxf.: Garsington?; Denton, with Modiola, &c.; Great Hazeley, in gritty stone. Bucks: Towersey, in bluish limestone, with pyrites; Long Crendon, in very sandy stone; Brill; Quainton, ‘‘ West pit.” Plagiostoma rusticum. Great Hazeley, Oxf.; in calciferous gritty stone. Pleurotomaria: with large whorls, roundish and flattened. Casts occur at Brill, and at Garsington. P P———. A more acute and larger species, Great Hazeley, Oxf., in calciferous sandstone. Brill; and at the Warren, near Stewkley, Bucks. Plicatula. Dinton, Bucks: a cast, same as in the “ Roche”’ of Portland. Pullastra. Remains of shells, perhaps referable to this genus, have been found at Cuddesden, Oxf., in sandy Portland stone; and at the Warren, near Stewkley, Bucks. Serpula. Remains of. Oxf.: Langcombe; Great Hazeley, in very sandy stone. Bucks: Whitchurch; in white stone ; Haddenham, in calciferous sand; 'Tower- sey, some specimens of great beauty; Coney Hill. Siphonia?, casts of Stems: Quainton; Bucks: in soft calcareous sandstone, “‘ Bottom Rock’’. Terebra Portlandica. Pl. XXIII. fig. 6. Abundant everywhere in the Portland stone of Oxfordshire and Bucks: at Combe Wood, Oxf.; Southwarpe, Whit- church, Towersey, &c., Bucks. Trigonia clavellata. angcombe, Oxf.: in sandy stone; with a Pecten. T: gibbosa. Universal and abundant in the Portland stone. Oxfordshire: Denton, Great Milton, and Combe Wood, immediately in apposition with the “Malm.” Bucks: Brill; Long Crendon ; Whitchurch ; Quainton; Bishopstone. imcurva. Quainton, Bucks. Venus?. Beneath Garsington: in concretional Portland stone; with Pecten orbi- cularis, and Astarle cuneata?. Quainton, pit east of Ordnance Station : in soft limestone *. ry. Fisnes, Vertebre of. Coney Hill: in “‘ sandstone”’ calciferous grit. Chimera Townsendii : (Buckland, Proceedings of Geol. Soc. vol. ii. p. 286.; and Lond. and Edinb. Phil. Mag. 1836. (vol. viii.) p.4—7.) The beak has been found in the Portland stone at Great Milton, Oxfordshire, bythe Rev. C. Townsend. * Besides the foregoing, fragments of bivalves, too indistinct to be determined, were found in the Portland stone, at Great Hazeley in Oxfordshire; and at Haddenham, Southwarpe, Stone, and Quainton, Bucks. Dr. Firron on the Strata below the Chalk. 30) Rertites. Bone of a Saurian. Great Hazeley: in ferruginous stone. [Portland Sand. | Ammonites bipler. Oxf.: Dropshot, near Thame, in grey sandy limestone, with numerous green particles, and small pebbles of quartz. Bucks: Dunton, in greenish stone, with dark particles ; Quainton, with a Trigonia. A-———_ giganteus. Oxf.: Dropshot, (very large specimens): in dark grey lime- stone, with green particles and pebbles of black chert*; Shotover; in grit. Bucks: Brill; Whitchurch; Dunton; in greenish grey stone, with dark par- ticles. Quainton. i ? Dunton, Bucks: in greenish grey stone, with dark particles. Avicula. Oxf.: Shotover, with Serpula and a Pullastra? in sparry grit. Bucks: Whitchurch ; large, a cast. Buccinum naticoide. Pl). XXIII. f.4. Brill: a cast. Cardium dissimile. Oxf.: Langcombe ; Dropshot, casts, in matter almost wholly green. Bucks: Hartwell Lodge, with Trigonia gibbosa, in bluish grey stone ; Dunton ; Brill, with Serpula ; Whitchurch; Muswell Hill; Quainton. Cytherea? rugosa. Pl. XXII. f.13. Hartwell, Bucks. Gastrochena. The Warren, near Stewkley, Bucks: and Shotover Hill, Oxf.: in Perna quadrata. Lucina. Village of Stone, Bucks. Mytilus (probably a new species). Denton Village, Oxf.: with Trigonia clavellata. Brill, Bucks. Ostrea solitaria. Dunton, Bucks. O——. Species indistinct. Shotover, Oxf.,with Serpula, &c. adhering to Ammonites giganteus, and bent into its inequalities. Brill, Bucks. Panopea?. Whitchurch, Bucks. Pecten lamellosus. Dunton, Bucks: in greenish grey stone, with dark particles: and in a mass almost entirely composed of green matter (silicate of iron), with Perna quadrata. Muswell Hill; Brill ?. i, Another species ?. Shotover: with Serpula, &c. Perna quadrata. Oxf.: Dropshot, near Thame, in dark grey limestone, with nu- merous green particles and pebbles of black chert; Shotover, in sparry grit, perforated by Gastrochena; witha Venus. Bucks: Muswell Hill, in stone ; containing green particles; the Warren; with Gastrochena, in grey stone; Dunton; in a green friable mass, and in greenish stone, including fragments of black flint, with Pecten lamellosus. Plagiostoma obliquatum. Near Thame, Oxfordshire. P—— rusticum. The Warren near Stewkley: in bluish grey stone, with minute dark particles. * At the quarries in the Portland-sand at Barley Hill near Thame, imperfect worn casts of several bivalves, in black flint or chert, are found in the sandy stone, along with pebbles of the same substance. 302 Dr. Firron on the Strata below the Chalk. Serpula. Shotover, with Ostrea ; Brill; Coney Hill; Dunton, in green matter. Trigonia clavellata. Wong Crendon; Casts in conglomerate, with siliceous pebbles ; and in sandy limestone, with numerous green particles. Dunton, Bucks; with Mytilus. ih gibbosa. Denton, Oxf. Hartwell, Bucks; with Cardium, in bluish grey stone. Dunton, and Whitchurch, Bucks. T. gibbosa: a variety, less oblique. Brill. T. incurva. Brill, Bucks. Venus. Shotover Hill, Oxf.; with Perna quadrata. Hartwell, Bucks; with Tri- gonia, in soft stone. [Kimmeridge Clay. | Ammonites bipler. Clay-pits near Aylesbury. Road from Aylesbury to Whitchurch. A= biplex (small). East Claydon, Bucks; 20 feet from surface, in clay: A——— giganteus?. Clay pits south-west of Stewkley, Bucks: in blue clay. A—— Gulielmi. East Claydon, Bucks: in clay ; beautifully iridescent. A———— like Gulielmi. Quainton, Bucks. A———— Selliguinus. Clophill, Bedf. Mr. Goodhall. A——— (probably new). Clay-pits, south-west of Stewkley, Bucks, in blue clay. Aptychus (Von Meyer). Pl. XXIII. fig.11. Roadside between Aylesbury and Whitchurch, about a furlong from Hardwick. Clay pits south-west of Stewk- ley ; fragments of very large specimen. A—— (a smaller species ?). Roadside between Aylesbury and Whitchurch. Exogyra nana. Between Aylesbury and Whitchurch: with Ostrea levigata. E virgula. Pl. XXIIL f.10. (Gryphea virgula of Deshayes.) Roadside be- tween Aylesbury and Whitchurch. Clay-pits south-west of Stewkley: good specimens in bluish grey clay. Gryphaa bullata. Clophill, Bedf., Mr. Goodhall. G dilatata. Wolvercot, Bucks?. Clophill, Bedf. G— virgula. See Exogyra. Mytilus. Quainton. Ostrea deltoidea. Aylesbury Clay-pits: a distorted form of the shell. Little Brick- hill, clay immediately below surface: fine specimens. O—— levigata. Between Aylesbury and Whitchurch. O———\—— (young). Thornborough, Oxf. O—— leviuscula (young). Road from Aylesbury to Whitchurch: in blueclay. Little Brick Hill, Bedf. O—— near to deltoidea, but wider at the hinge; still very thick. “Ina bed of stiff “ clay, about two miles north-north-west of Leighton, under the red sand of the “heath, and about 20 feet above the river.” Mr. W. Mathews of Leighton: Roadside between Aylesbury and Whitchurch ; Bucks. Panopea depressa, Headington Quarry, Oxf. Pecten arcuatus. Vicinity of Aylesbury. P Lens. Little Brickhill. Brow of the hill, in clay immediately below sand, Dr. Firron on the Strata below the Chalk. 303 Pleurotomaria reticulata (Trochus, M.C.) Headington; Oxf. Serpula tetragona. Clophill, Bedf., Mr. Goodhall. S tricarinata?. Roadside between Aylesbury and Whitchurch. “In stiff clay, “about two miles N.N. west of Leighton.” Mr. W. Mathews. Fisues. Chimera Egertoni: (Buckland, Proc. of Geol. Soc. vol. ii. p.206.; and Lond. and Edinb. Phil. Mag. (1836), vol. vill. p.4—7.) Shotover-hill, Oxf. Psammodus reticulatus: (Agassiz; in Egerton’s Catalogue of Fossils); Shot- over-hill, Oxfordshire. Reptives. Bone of a Saurian. Clay-pits south-west of Stewkley : part of a flat bone. Plesiosaurus; Vertebre. Headington Quarry, Oxf. Coprolite ; or coproid masses of phosphate of lime. Beneath Whitchurch. Clay- pits south-west of Stewkley: one specimen occupying the cavity of an Am- monite. [Oxford Oolite. | Melania Heddingtonensis. Wheatley, Oxf.: cast of part of interior. Ostrea? Thornborough, Oxf. Wheatley; in compact, blue, sparry oolite. Pholadomya deltoidea. Headington (Coral rag). Spongia?. Wheatley, Oxf.: in sandy stone. Terebratula tetrahedra? Thornborough, Oxf.; and Wheatley. C4M BRIDGESHIRE™*, (156.) In this county, as in Bedfordshire, the Wealden and Portland groups are wanting; and the strata, rising with a very slight inclination from the south of east, and thinning off near their outcrop, are frequently cut through by denudation, so that distant outliers, especially of the lower green-sand, are frequent. Mr. M’Lauchlan, who was engaged in the Ordnance Survey of this part of England, remarks, that the summits of the chalk decline rapidly in * T am indebted to my friend Professor Sedgwick for the greater part of the following infor- mation respecting Cambridgeshire. The only publications connected with the geology of the county, are a paper by Professor Hailstone, Geolcgical Transactions, 1st Series, vol. iii. p. 243, &c. ; a short paper on the Northern division of Cambridgeshire, by Mr. Lunn, (1818),—Geol. Trans., Ist Series, vol. v. p. 114, &c. ; an account of some verbal communications made to the Cambridge Philosophical Society, London Philosophical Magazine, (1835,) vol. vi. p. 74; and the report of a field Lecture by Professor Sedgwick, which appeared in the Cambridge Chronicle of the 10th of April 1835. Hunrinapowsuike I have passed over, not having myself examined that county ; and I am not acquainted with any publication specifically relating to it, except Mr. Smith’s county map. A small space at the south-eastern verge of the county, on the confines of Bedfordshire, is occupied by the Lower green-sand ; but all the tract adjoining Cambridgeshire is assigned by Smith to the Oak-tree clay, a term which I believe denotes, in this case, the Kimmeridge clay. thereabouts are much obscured by transported matter. VOL. 1V.—SECOND SERIES. 2R The strata 304 Dr. Firron on the Strata below the Chalk. height on the north-east of Bedfordshire: Kensworth Hill, south of Dunstable, being 904 feet above the sea at low water ; the hills east of that town 850 feet; Lilleyhoe, 664; Barkway, Windmill-hill, 513; the station near Royston, A84 feet; Balsham, on the east of Cambridge, 380; Newmarket station, 267; Brandon in Suffolk, 190 feet. The summits of the lower chalk suc- cessively decline in the same direction ; Orwell station being 250 feet, Chapel- Bush, near Haslingfield, 220 ; Swaffham-Prior (near Reach), 140. And the lower green-sand also falls rapidly : the hills near the outcrop at Bow Brick- hill being 683 feet high; that of Haddenham on the north of Cambridge, 133 feet; and the general surface of the lower green-sand, which tops the hills near that place, ranging from about 60 to 120 feet; at Ely 75 feet. The level of the Cam, upon the gault, at Cambridge, is only 243 feet above the sea at low water on Lynn Deeps; that of the Kimmeridge clay at Ely Bridge, 14 feet; and of the Cam, at Upware, probably not more than 12 feet. So that if the sea were not dammed out by artificial means, a great part of the marshy tract on the confines of this county, Huntingdonshire, and Nor- folk, would be inundated at high water, as appears to have been the case at no very distant period. ‘The hydrography and drainage of this low tract, which are intimately connected with geological principles, have been the subject of some valuable publications, but do not fall within the immediate scope of these pages. (157.) Another general circumstance which characterizes the north-west of Cambridgeshire, is the great extent and varied composition of the transported masses with which the strata are in many instances thickly invested. This superficial deposit includes worn masses of greenstone, with fragments of many of the lower members of the English series,—and rounded pebbles of chalk, in such abundance as to form a very large proportion of the entire mass. With these stony substances are fragments of the fossils of most of the strata, Belemnites, large Gryphites, the Ostrea (or Gryphite) of the Ox- ford clay, and portions of the skeletons of Elephants, Rhinoceros, Hippo- potamus, Deer of several species, gigantic Oxen, and of the Horse. The mass thus composed forms many of the hills on the borders of Cam- bridgeshire and Essex, and occupies a great part of the platform which runs along the confines of the former county and Huntingdonshire; a brown variety of it obscures the junction of the gault and lower green-sand on the west of Cambridge, forming an upland which extends trom Bourne by Toft and Hardwick to Dry Drayton, where it declines into the plain*. * Mr. Hailstone mentions particularly, that the deposits just described are perfectly distinet from that which occurs above the Gault in Cambridgeshire. ‘The former are very well known Dr. Firron on the Strata below the Chalk. 305 These accumulations, it will be perceived, closely resemble those already mentioned in the account of Buckinghamshire and Bedfordshire, especially near Leighton, and at Stewkley. They occupy, in fact, a great extent of the surface, and form one of the most interesting geological deposits throughout the East of England ; but there are circumstances respecting their relations to each other, and to the crag of Norfolk and Suffolk, which still remain to be investigated and explained. (158.) The strata therefore which are found below the chalk in Cambridge- shire, consist of Chalk, Upper green-sand, Gault, Lower green-sand, Kim- meridge clay, Oxford oolite, and Oxford clay ; the last occurring only in a few places, and in the remote part of the county, in which it is the lowest member of the series. The sections, Plate X. a, Nos. 22, 23, and 24, explain the general relations of these strata, but have no pretensions to accuracy of local detail. ‘The following notes describe some of the principal appearances con- nected with the object of this paper; and the publication of the Ordnance maps of the county will no doubt soon lead to the complete examination of it by the geologists of Cambridge. Chalk.—The upper chalk range passes from the heights near Dunstable, through the north-west of Hertfordshire, by Hitchin and Baldock, to Barkway and Royston Downs, and thence by Balsham and Newmarket into Suffolk. Mr. M’Lauchlan informs me that the chalk ridge at Thorfield (about 570 feet high) is an anticlinal line, and that the overflow of water in Wardington Bottom, near Newsell’s-bury Park, while the rest of the country is dry, renders it probable that some of the lower beds are there brought up to the surface. On the Ordnance maps two ridges are distinctly marked, which meet thereabouts at an angle; one passing from Berry Barn through Norfield to Barkway Mill (313 feet high), the other, striking off from Thorfield for about a mile towards the north, turns suddenly to the east, to the group of hills above Royston and Burley, and is continued thence to the north-east through Chishill, 470, and Heydon, 480 feet. ‘The lower tract, in the angle between these ridges, from Newsell’s to Known’s Folly, may possibly be a valley of elevation like those of Kingclere described by Dr. Buckland. The outcrop of the lower chalk and chalk marl, is nearly parallel to the range of the upper strata, and to that of the heights above mentioned ; its general course being from the neighbour- hood of Orwell, through Haslingfield, Cherry Hinton, and Bottisham, to Reach on the margin of the Fens. Thence, from about Milden-hall in Suffolk, near the confines of Cambridgeshire, to Hunstanton, on the north-west coast of Norfolk, a distance of about forty miles, the direction of the chalk escarpment is nearly from south to north. The chalk which forms the principal part of the lower hills in Cambridgeshire, bears the local name of “Clunch.” It is described by Mr. Hailstone as being harder than common chalk, and usually of a grey colour. It affords, as the lower and marly chalk is found to do in many other places, remarkably good lime: and it would seem that some of the lowest beds, which bear the name of Clunch, agree in their properties, as in geological position, with the firestone of Surrey, throughout the Isle of Ely under the name of White Gravel, (the latter is Red); and, Mr. Sedgwick states, are older than the beds of flint gravel in Cambridgeshire. ZR 306 Dr. Firron on the Strata below the Chalk. being applied to the same purposes in the construction of fire-places, &c. Very large pits of clunch have been opened at Reach, on the immediate confines of the Fens, and on the line of Section No. 23. Upper greensand. This formation here differs from that of some of the more southern counties, in its much smaller thickness, in the absence of chert, and the comparative rarity of green particles, which are here confined to a stratum not more than eighteen inches thick, by which the lowest beds of the chalk are separated from the gault, as is well seen in the section exposed at the Castle Hill, Cambridge. The presence of this green bed, however, is remarkably constant; and it contains many fossils, some of which are common to this formation, and to the chalk,— but others, at least in this country, are confined to the sand; among which, Mr. Sedgwick informs me, Hippurites are found near Bottisham. Gault.—The term Gault, or “Galt,” adopted by Mr. Smith as the denomination of this re- markable stratum, is in Cambridgeshire the popular name for the blue clay, which comes in between the green bed last mentioned, and the ferruginous (Lower green) sand. Its thickness and relations have been well ascertained in this county, from the numerous borings to obtain water, which pierce through the clay to the sand below, especially on the line from Basingbourne north-west of Royston, through Meldrith, and thence towards Cambridge. Its average thickness is about 150 feet*, which is nearly the same as on the south-eastern coast: but the surface of this stratum is much obscured by superficial gravel and a thin coating of the lowest chalk; and good specimens of its fossils are rare, as the upper beds contain but few. Among those, how- ever, which I found between Cambridge and Ely, are the characteristic Anmonites of different species, 4. inflatus, A. lautus, A. varicosus ; Exogyra conica; and spines of an Echinus. In the museum of the Geological Society is a specimen from the Gault near Cambridge, which M. Agassiz has found to belong to a new species of Chimera +. Lower green-sand.—This stratum occurs throughout this county between the Gault and Kim- meridge clay, in the form of sand of different shades of grey and brown, but chiefly as a coarse ferruginous compound of quartzose sand, cemented by hydrate and oxide of iron, and more or less indurated. At the top, however, is some green-sand, as appears from the first discharge from the borings through the Gault, after the rod has passed the clay ; the water subsequently obtained depositing an ochreous matter, of the colour of the Woburn sands. I have no fossils from this stratum in Cambridgeshire. Its thickness is obviously much less than in Bedfordshire ; and its internal composition was not discernible in any of the sections which I saw; but at Ely I found numerous concretional blocks, precisely resembling Kentish rag ; which had been obtained, I was informed, from a place near the gallows on the south-west of the town, in a deposit which there forms an extensive outlier over the Kimmeridge clay, and consists of coarse, ferruginous, and sili- ceous sand and conglomerate, containing a large proportion of brown iron-ore (hydrous oxide of iron), like that of Shanklin in the Isle of Wight. At Ingoldsthorpe in Norfolk, where the thick- ness of the stratum is probably not greater than at Ely, it is said to contain Fuller’s earth t. Quitting Potton, in Bedfordshire, Mr. Lunn states §, ferruginous sand is observed within the * Mr. Lunn supposes the thickness to be 200 to 220 feet.—Geol. Trans. vol. v. p. 115. aE Proceedings of Geological Society, 1835, vol. ii. p- 205, note. { In Mr. Greenough’s geological map, sulphate of barytes is mentioned as occurring on the main road from Royston to Huntingdon, at Longstow near Caxton. This mineral, it will be recol- lected, occurs in the Fuller’s earth at Nutfield in Surrey, ((51.) p. 141.); a situation which answers to that of the Lower green-sand on the line of section No. 22. § Geol. Trans. Ist Series, vol. v. p. 114, &c. 7 Dr. Fitton on the Strata below the Chalk. 307 borders of Cambridgeshire, at Gamlingay, with Gault resting upon it; ‘ and in some of the pits, “the line of junction is as well defined as that of two immiscible fluids”; but the sand contiguous to the clay is more highly impregnated with iron than the lower part, and is cemented by the oxide, so as to form a hard rock. Leaving to the south-west the two villages of Hatley, both on the Gault, the boundary passes between Little and Great Gransdon, and west of Caxton, (which is on the clay), through the north-west sides of the parish of Eltsley, by Passworth St. Everard’s, and Passworth St. Agnes, to Hilton and Fenny Drayton. In the parish of Fenny Stanton and that of Croxton, a bed of clay (Gault?) rests on the sand. The sand can be traced across the lower country, in a direction nearly parallel to the chalk, from Caxton (Section No. 22.) by Co- nington, and Long Stanton, through Cottenham and Denny Abbey, where the surface is occupied by low hillocks of gravel; and on the north of those places it forms the summit of many of the heights of small elevation on the south-eastern verge of the Fens. Thus at Haddenham, the hill, 133 feet high, is capped with sand; and the prolonged height, or ridge thence to Aldreth, called “the Sandy-way,” about 122 feet, is likewise composed of it. The junction of the sand and subjacent clay is well seen, Mr. Sedgwick states, at the clay-pit on the east of Ely; and sand is visible in the drains from about the fifth to the ninth milestone, along the road from Littleport towards Downham, cutting across the Fens on the north-east of Ely, in a direction corresponding to the previous course of this formation near Cambridge. Kimmeridge clay.—This occupies all the lower tract on the north and west of the line of sands above mentioned, as on the course of the Ouse, or Old West river, from Fenny Stanton and Ho- lywell on the west, to its junction with the Cam at Thetford, and thence towards Ely. Sec- tions are of necessity rare; but a very good one, exhibiting the junction of the clay and Lower green-sand, is exposed in the pits east of Ely. On the west and south-west of Ely the clay is capped in many places by sand, in the form of outliers, on the summits of the heights, which here range from about 120 feet to 50 (see the list in the Appendix C.): and the clay is continued uniformly through their bases, to a point north-west of Haddenham, on the road to Chatteris, where it is succeeded by the Oxford oolite. Oxford oolite.—A remarkable exception to this uniformity of structure occurs at Upware, on the Cam, about three miles north-west of Reach (see the Section, Plate X.a. No. 24.); where the upper strata of the Oxford oolite make their appearance, in a low ridge extending for about three miles north of Upware, in a direction nearly parallel to that of the Cam, which is here not much more than 12 feet above the sea at low water. The stone beds have been opened here in two or three quarries; a very large one being near the river, and on the line of the section 24. The strata are slightly inclined to the west of north, in a direction opposite to that of the beds below the chalk. The stone here laid bare to a depth of about 10 or 12 feet, consists of a loose rubbly limestone, of a cream colour, in some places coarsely oolitic, and containing many of the charac- teristic fossils, for a collection of which I am obliged to Professor Sedgwick and Mr.M’Lauchlan :— Spines of Cidaris; Corals; an Arca; Fusus, a new species; Gervillia aviculoides; Isocardia, an acute species; Modiola; Ostrea gregarea; Pecten viminalis; Plagiostoma; Plicatula; Turbo muricatus, &c. The coralline beds (the proper “ Coral rag” of Smith) do not come up to the surface at this place; but they break out, Mr. Sedgwick informs me, beyond Haddenham, going towards Chat- teris; and he suspects that the shelly beds of this formation occur in some other places in the county, between the Kimmeridge and the Oxford clays, from the occurrence of numerous bits of the coral rag and of its fossils in the brown clay, which masks so much of the surface of Hunting- donshire and Cambridgeshire, and in a condition which makes it probable that they had not been drifted far. 308 Dr. Firtron on the Strata below the Chalk. Oxford clay—The Oxford clay succeeds to the coral rag on the north-west of Haddenham, as has been mentioned, and of Ely. It is the lowest stratum in Cambridgeshire, and forms the base of the Great Bedford Level. (159.) Chalk in Rutlandshire —The rise of the strata last mentioned, com- bined with the general features and structure of Cambridgeshire, would seem to indicate the final outcrop and disappearance of the upper members of the Series ; but from a passage in a paper by Mr. Barker, published in the Philo- sophical Transactions for 1791*, and quoted by Dr. Buckland {, it appears that chalk has been discovered at Ridlington in Rutlandshire, about forty miles from the general range of the chalk hills in Cambridgeshire and Norfolkf. So that if this statement be correct, we might expect to find some of the beds below the chalk, in the wide tract of intervening country. The only cir- cumstance mentioned by Mr. Barker which throws doubt upon the suppo- sition that this chalk is in its original position, is, that the flints, which he states to occur “in rows, lying in it as is usual in the South of England,” are “ broken, and not whole ones.” So that it is possible that the entire mass may consist of transported fragments of chalk, and be analogous, but ona much larger scale, to the loose pieces of that substance found by Mr. Cony- beare in my presence during an excursion in Northamptonshire, near Sywell; a place about thirty miles distant from the nearest point of the chalk escarpment. Ridlington, where this patch of chalk is stated to have been observed, is placed in Smith’s map of the county, on the verge of a platform of the Lower oolite, resting immediately on the blue marl at the upper part of the lias; and the map bears no indication whatsoever of any other stratum. * Vol. lxxxi.p. 281. + Geological Transactions, 1st Series, vol. v. p. 539. t I shall here insert the whole passage, as the best mode of presenting the facts to the reader. My. Barker, writing at Lynden, near Uppingham in Rutlandshire, says: “I did not know till lately “* that we had any chalk nearer us than Moddingley”—(see Pl. X.a. No. 22.); “but several years “‘ ago the people of Riddlington in Rutland, digging for stone to mend the roads, met with a bed of “ chalk, at which they were much surprised, and did not know what it was, never having seen a “ chalk-pit before. After I had heard of it, I went to examine the place, and found a regular chalk ** pit, with rows of flints lying in it as they are wont to do in England. The chalk is not soft, like “* that they write with, but very much like that they dig about Baldock: nor are the flints so black ‘‘ as those in the South of England, but veined, of a light-coloured flint, and white; some parts “much mixed with chalk, and are broken, not whole ones. ‘They may have dug the pit six yards “long and two deep, but how far the chalk reaches I do not know.” Mr. Barker adds, that he had seen a little patch of chalk a few yards long, in a bank by the road side, along the turnpike road near Stukely, about three miles north-west of Huntingdon, which place is about twenty miles from the nearest chalk-hills. Dr. Frrron on the Strata below the Chalk. 309 Traces of the Wealden in Northamptonshire.—The preceding statement is rendered more in- teresting by the discovery at Wansford in Northamptonshire, a place about ten miles east of Ridlington, and thirty from the chalk-hills in Cambridgeshire, of a mass of calcareous grit, containing an impression of Lonchopteris Mantellii*, a fossil species found by Mr. Mantell in the grit of Tilgate Forest, Sussex, and hitherto peculiar to the Wealden strata; indicating therefore the presence of that group at the distance of more than forty miles from the nearest point on the south, at which its existence has yet been ascertained in England. For an opportunity of examining the specimen in question, I am indebted to the kindness of Mr. Woodward of Norwich, to whom it belongs ; and I find it to consist of crystalline calciferous grit, of a yellowish grey or drab colour, containing a very large proportion of carbonate of lime,—which may very well have formed a part of one of the concretions of grit subordinate to the Hastings sands. The form of leaf of the plant is beautifully impressed upon the stone, and very well represented in the plate of the Fossil Flora: and the only question is, whether the locality has been correctly stated, which Mr. Woodward has no reason to doubt. It may be added, that the existence of the Wealden in this new situation is rendered more probable by the occurrence of chalk in Rut- landshire, at a point not less remote from the great body of that formation in the South-east of England. : Norrotx t. (160.) The strata below the chalk appear only on the west of this county, and the series is generally the same with that of Cambridge ; but the Upper green-sand soon ceases to be conspicuous, or disappears altogether ; and the Gault is so much reduced in thickness, and changes its character so remark- ably, that it is only by means of its fossils and by tracing its continuity with the more usual form of the stratum, that its identity can be ascertained. The ferruginous beds of the Lower green-sand are sufficiently distinct, but the formation is much thinner than in the south-eastern counties. No traces of the Wealden or Portland groups have yet been found, nor are there any * Lindley and Hutton’s Fossil Flora, (1835) vol. iii. p. 372. Plate 171. + The publications on the geology of Norfolk, besides the general maps of Smith and Green- ough, and the County map of the former, relate principally to the eastern portion of the county. But since these pages have been at the press, an excellent account of West Norfolk, by Mr. R. C, Rose, of Swaffham, has appeared in the London and Edinburgh Philosophical Magazine’, to which I beg to refer the reader who wishes for detail. The preceding papers relating to this part of the county, are Mr. R. C. Taylor’s plate and description of Hunstanton Cliff, 1823°; a paper by the same author, on the alluvial strata and the chalk of Norfolk and Suffolk’ ; and a list of the fossils of Hunstanton, in Mr. Woodward’s Geology of Norfolk*. Some occasional notes connected with the west side of the county, may also be found in the tracts more immediately relating to the beds above the chalk. 1 Vol. vi. and vii. 1835—1836. ® Phil. Magazine, 1822, vol. lxi. p. 81—83,; republished in a tract on the Geology of East Norfolk, 8vo, 1827. 5 Geol. Trans. 2nd Series, vol. i. p. 374—378. * “ An Outline of the Geology of Norfolk,” 8vo, 1833. 310 Dr. Fitton on the Strata below the Chalk. distinct indications of the Oxford oolite, between the Kimmeridge and Ox- ford clays. The line of hills, nowhere probably exceeding 600 feet in height, which stretches for about forty miles from the chalk range of Cambridgeshire to the north-west coast of Norfolk, bounds the fen-country like the low shore of a sea ; and a very slight change of level would again convert the fens into a shallow estuary, by the waters of which these hills would be washed at their base. At present, the face of the heights is covered with vegetation, so that it is only in detached spots casually exposed, that the strata can be seen. Not having, myself, any good section of this part of the district, Mr. Rose has been so good, at my request, as to prepare an enlarged copy of the sketch annexed to his paper on West Norfolk, on the line from Swaffham to Lynn, (see Pl. X.a, No. 25.); and I have inserted also a section and a sketch of Hunstanton Cliff, (Plate X. a, No. 26; and X. b, fig. 12, a, b, andc,) the only natural section that is visible upon the coast. Deposits above the Chaik.—The portion of the fens immediately adjacent to the chalk-hills in West Norfolk, bears the name of Marshland. It is composed of alternating beds of lacustrine silt and peat, covering, in the vicinity of Lynn, a deposit of marine silt; the whole resting upon a stiff clay, which incloses small nodules of chalk, and is obviously the same with the superficial deposit, already described as including chalk fragments and being generally of similar com- position, in Cambridgeshire and near Leighton; beneath which are the strata of Kimmeridge in Oxford clay. In a well, sunk and bored at Lynn, to the great depth of 630 feet, the detail of which will be mentioned hereafter, a bed of the clay containing portions of chalk, was found beneath about 23 feet of sand, loam, and peat, and marine silt ; and the clay was, at the bottom, in immediate con- tact with what Mr. Rose considers as the Oxford-clay, but with some doubt whether it may not be that of Kimmeridge. For an account of the newer subaqueous deposits, and of the more recent changes which the surface here is proved, by historical documents, to have undergone, I refer to the publications of Mr. R. Taylor, Mr. Woodward, and Mr. Rose, in which references will be found to preceding authors, some of whom are of very ancient date. Chalk.—An account is given in the publications of this Society, of two borings in the south of Norfolk, which illustrate the relations of the chalk to the beds immediately beneath it. One of these, described by Sir H. Bunbury, was made at Mildenhall in Suffolk*, a spot about twenty miles north-east of Cambridge, and thirteen from Ely, near the point where the chalk range changes its direction from about south-west and north-east, and runs northward, to join the sea at Hun- stantont. Another sectional list has been published by Mr. John Taylor, derived from a boring at * Geol. Trans. 2nd Series, vol. i. p. 379. + The general course of the chalk escarpment in the Wolds of Lincolnshire (see a paper by Mr. Bogg, Geol. Trans. Ist Series, vol. iii. p. 392.) and of Yorkshire, is from south-east to north- west ; so that the line of its course in Norfolk may be considered as forming the bottom or most eastern shore of a deep bay, (and the lowest part also of the range, with reference to the level of the sea); from the extremities of which the escarpment diverges in both directions ;—north- westward, for about ninety miles, to its final termination on the parallel of Flamborough Head ; and towards the south-west, for more than two hundred miles, to the coast of Devonshire. Dr. Firron on the Strata below the Chalk. 311 Diss, on the confines of Norfolk and Suffolk*, about five-and-twenty miles east of Mildenhall ; through which place if a line were drawn on the line of dip, it would pass nearly through Down- ham on the margin of the Fens. In this section, the entire thickness of the chalk was cut through, and combining it with that at Mildenhall, the result stands thus ;—subject, however, to some un- certainty, from the imperfect condition of the specimens brought up in boring. Diss. Feet. MiILDENHALL. Reet. mma, Clay ...... ain RAS 50 TY Sandy 10am». wesc eee Lines 1 MEDIC se ccc csc ssc eces 50 100 2. Chalk. II, Chalk. a. Without flints, soft, marly. 100 a, White, without flints .. 35 b. With flints, in layers ope ee b. Yellowish, gritty...... 5 a yard from each other . e c. Grey, hard .......... 136 476 c. Grey,with occasional layers 60 of white: no flints...... d. Light bright blue chalk, TIL. a. Blue clay... + sei cee os 54 eng oy, with i 20 510 6. Ditto, darker and harder 10 white cha erator [On penetrating the light blue clay, the boring-rods sank rapidly, and wa- ter rose to within 47 feet of the sur- face. | 3. Sand;—characters not stated ...... 4 615 ce. Ditto, mixed with oy 10 sand 7h 250 IV. Green sand, with many fossils .... 11 V. Blue clay,abounding in fragments of large shells, having a high polish. . [Water coming in here, the work was discontinued. | 9 270 The section at Diss is valuable, as it cuts through the entire thickness of the chalk, which is here 510 feet; of which, it will be remarked, the uppermost 100 feet are marly and without flints. The light blue stratum, 2. d, referred by Mr. Rose to the Gault, may, perhaps, rather eorrespond to the lower portion of the chalk-marl, and to part of III. in the Mildenhall section ; in which case 3. at Diss would represent the Upper green-sand. V.at Mildenhall is distinctly referred by Sir H. Bunbury to the Gault, which he supposes to occupy the flat surface of the ad- jacent fen. Mr. Rose states that the chalk range in West Norfolk dips to the south-east, about five yards in a mile; or about 1 in 350. He has requested me to mention that he considers the estimate of the heights given in his paper as probably exceeding the truth; and at my suggestion, derived from the levels in Cambridgeshire, he has reduced the altitudes in the section, Pl. X.a. No. 25. The upper chalk of Norfolk includes the usual flint nodules; and among the larger flinty masses are some like those described by Dr. Buckland, under the name of Paramoudra. Many of the fossils of the uppermost strata, according to Mr. Woodward, are different from those of what he has called the medial chalk, which also contains flints. Near Swaffham, the chalk without flints, which seems to belong to some intermediate beds between the upper and lower * Proceedings of the Geol. Soc. (1833-4), vol. ii. p. 93. VOL. IV.—SECOND SERIES. 2s 312 Dr. Frrron on the Strata below the Chalk. groups, forms a range of somewhat lower hills, on the west of that constituted by the superior strata. It is hard enough to be used as a building stone, divides naturally into rhomboids, and contains horizontal seams of argillaceous matter ; but Mr. Rose remarks, that although the hard- ness increases progressively downwards, the increase is not regular nor uniform, some portions as hard as any of the lower occurring in the upper part of it. His list of fossils from the chalk with flints contains about 78 species; of which, according to Mr. Mantell, only 40 occur in the corresponding part of the formation in Sussex. The relations of the lower strata of the chalk are best exhibited in the section at Hunstanton Cliff, which will be presently described. Mr. Rose’s list of fossils from the chalk without flints, includes altogether 54 species; of which 30 are found in the upper part of Hunstanton Cliff:— of the whole number only 15 species are wanting in Mr. Mantell’s catalogue of the Sussex chalk fossils*. Upper green-sand.—It is probable that attentive examination would discover the usual green matter on the confines of the chalk and the representative of the gault in this county: but gene- rally the Upper green-sand is scarcely perceptible. In the section at Mildenhall, inserted above, 10 feet of clay mixed with green particles, precede 11 feet of (upper) green-sand with many fossils, which rests on blue clay, no doubt the Gault: and the five feet of sand which occur at the bottom of the boring at Diss may also (possibly) belong to the former. Mr. Murchison considers one of the beds at Hunstanton, as the representative of the malm rock of Western Sussex; and Mr. Rose also mentions a rock like firestone, on the confines of the chalk, a re- semblance which I find is indicated in my own notes. Gault.—This stratum is very distinct at Mildenhall, below green-sand ; and is represented in Smith’s map, as occurring all along the line of escarpment, between the lower chalk and the lower ferruginous sand. I have myself seen it with the characteristic fossils at East Winch and several other places. Thus at Mosshill Farm (“ Muzzle” of the Ordnance Map), west of the house, towards Denver, are several pits, in a patch, or cap of bluish clay, over the Lower green- sand: the former including Belemnites in great numbers, phosphate of lime in kidney-shaped (coproid) concretions, a few specimens of Ammonites, and fragments of Inocerami in great num- bers. On the heights between Middleton Tower and Devil’s Bottom, north of the section, Pl. X. a. No. 25, are patches of white and yellowish grey clay, containing many of the Gault fossils; —Belemnites, Inocerami in fragments, Echinus-spines, and portions of Encrinites. In fact, most of the heights in this part of the country, are thinly covered with gault; while the sand beneath it rises slowly towards the west. The average thickness of the Gault in West Norfolk is not more than 15 feet, according to », Mr. Rose, who has traced the connexion between the detached portions, indicated in Smith’s map, as far as West Newton, about three miles south of Ingoldsthorpe. The valley between the chalk and Lower green-sand is there interrupted by an advance of the chalk, and beyond that point the blue Gault is no longer observable ; its place being occupied by the red marly stratum of Hunstanton Cliff. The position of this red matter falls in with the strike of the blue Gault in the southern part of the range, at Newton; and it has been detected, between that place and Hun- stanton, at Dersingham Mill, and at Ingoldsthorpe, where I myself have seen that the red stratum is immediately succeeded by sand, the blue beds being wanting. * Geol. Trans. 2nd Series, vol. iii. p. 201, &c.; and Geology of the South-east of England, (1833.) p. 370, &c. Dr. Firron on the Strata below the Chalk. 313 Lower green-sand.— This formation here consists, at the upper part, of highly ferruginous coarse sand, one of the most remarkable components of which is Titaniferous oxidulated iron*. The sand abounds in hard concretions of siliceous grains cemented by ferruginous matter, in the form of thin flakes or bands, irregularly ramified, which, in Norfolk, are called “ Carstone ”;—beneath which is finer sand of different shades of grey, yellowish, and white. The course of the out- crop is generally parallel to that of the chalk: the chief localities and the local varieties are indi- eated in Mr. Rose’s memoir. In descending a hill on the road from Lynn to Snettisham, about a mile from the village of Dersingham, is white sand, under yellow slightly consolidated sand; and near the line of the section No. 25, between 38 miles and 39 from Norwich, about half a mile from Middleton, are pits of yellowish and white sand, with ferruginous concretional bands, apparently belonging to the upper member of the Lower green-sand; and very like the Woburn sands. Organic remains must be very rare in this formation, as Mr. Rose states that he had not obtained any specimens. At Ingoldsthorpe, however, in a brick-field near Mount Amelia, 1 found casts of the following shells, in masses of agglutinated ferruginous sand, like those of Parham-park in Western Sussex, and of the cliff on the west of Shanklin Chine in the Isle of Wight; Auricula incrassata; Avicula, a new species; Corbula striatula; Mya plicata; Rostellaria calcarata ; Turritella granulata; Venus Faba; and some other indistinct bivalves and univalves. No indications occur in the sections of this formation which I saw, nor in those mentioned by Mr. Rose, of the threefold subdivision of the Kentish coast; but in the lower part are thin courses of Fuller’s earth, not more than an inch in thickness. The lower beds are stated by Mr. Rose generally to contain thin strata of Fuller’s earth; as in Surrey and at Woburn. (161.) Hunstanton.—The cliff at this place exhibits an epitome of all the lower strata above described: the section is very distinct, and the dif- ference in the characters and proportion of the beds from those of the south- ern counties is so remarkable, that I think it necessary to give an account of them, although the place has been already described by Mr. R.C.'Taylort and Mr. Rose. Pl. X.a. No. 26, represents the cliff, on the same scale with the other sections in that plate, and with Plate X. b. fig. 12. a, which is copied from a portion of the Ordnance Map of Norfolk. Fig. 12. b. is a sec- tional elevation, for which I am indebted to Mr. Murchison; and fig. 12. c, a sketch of part of the cliff, by Mr. Whewell, with whom and Professor Sedgwick, I had the pleasure of examining the place in 1827. The following is Mr. Murchison’s description of his section, (Pl. X. b. fig. 12. b.), with some additions from my own notes. The dip is, generally, to the north-east ; but it will be observed that there is an angle in the coast; so that the section is strictly divisible into two portions, in different planes, neither of them coincident in direction with the line of dip. * London and Edinburgh Phil. Mag., 3rd Ser., vol. vii. p. 179-; Phillips’s Mineralogy, 3rd edit. p. 223. Tt Geology of East Norfolk; and Phil. Mag. 1823, vol. Ixi. p. 81. 2s2 314 Dr. Fitton on the Strata below the Chalk. Section at HunsTantTon CiirFr. Ft. In. 1. Dunes * of loose blown sand. 2, Reddish clay, passing downwards into fine laminated sand; with bands of small ) 10 0 pebbles ...-.. see eeereececeeeeecs sie tiehe SHINO DO Oe soeceseess 9 Oto . Chalk, increasing as it rises, and attaining its greatest thickness in the cliff under the lighthouse. It is there about 30 feet Nee ‘and divisible into three :— a. Grey chalk, in thin beds..... Bre DOO OOS THOS OF Oe Ibid. 4 Tabular View, 2nd edit. 5 Section, No. 6. Plate X. a. 6 Phillips, Geol. Trans., 1st Ser. vol. v. p. 18. 7 Supra (149.), p. 284; and Sect. 20, Pl. X. a. 5 (160.), p. 311. 9 (9.), p. 107. 10 (49.), p- 140. ‘Murchison, Geol. Trans., 2nd Series, vol. ii. p. 99. Dr. Firron on the Strata below the Chalk. 319 is between 70 and 80 feet!; in the Isle of Wight, about 70 feet®. At Blackdown the thickness of the sand is about 100 feet? ; in the Vale of Wardour, probably from 60 to 80+; near Swindon, 30 to 50 feet®: but at the Castle Hill, Cambridge, it is not more than ,18 inches®. Thence through West Norfolk, the stratum is not anywhere distinctly seen; and at Hunstanton, the only beds which can be supposed to represent it, are not more than 2 feet thick7. Gault.—The thickness of this stratum near Copt Point, derived from barometric measurement, is about 130 feet®. In the interior it is difficult to obtain good estimates, and accurate measures can be expected only in wells. At Merstham it is about 150 feet thick®; in the Isle of Wight probably about 70 feet'®: at Ridge, in the Vale of Wardour, it is about 75 feet!!; at Cotmore Wells near Thame, 90 feet'*.. In Cambridgeshire, the entire stratum has been cut through re- peatedly in wells and borings, which give an average thickness of 150 feet !°; but at Mildenhall in Suffolk, the blue clay, which seems to represent it, is only 9 feet'*. In West Norfolk Mr. Rose considers that the utmost thickness cannot be more than 15 feet'!®; and at Hunstanton the red marly beds which are supposed to contain Gault fossils, are only 4 feet thick!®. Lower green-sand.—The measured thickness of this formation can be most easily obtained on the shore between Copt Point and Hythe, where the uppermost subdivision is about 70 feet thick '7; the middle group, 70 to 100 feet '*; and the lowest, 60 to 80 feet'!’; the total thickness consequently about 250 feet. In Western Sussex, Mr. Murchison states that nearly 400 feet of sand were passed through in a boring, at Petworth Summerhouse2°; and Mr. Martin conceives that the two lower members may be together about 150 feet thick®!. In the Isle of Wight the thickness, between Bonchurch Cove and Sandown, Rocken End and Atherfield Rocks, cannot be less than that of the formation near Folkstone, and seems to be much greater. At Brill, in Buck- inghamshire, about 26 feet remain”; in West Norfolk, Mr. Rose considers the thickness of the whole formation to be about 80 feet *. Wealden.—No measures, on good estimates, of the thickness of the strata in this group have yet been obtained. Mr. Martin assigns 281 feet to the Weald-clay cut through in boring, at Petworth in Western Sussex2*; but in the section at Tiepit and Cowleaze Chine in the Isle of Wight, the clay seems to be no more than 140 feet thick®. The section of that part of the Hastings-sands which is visible between St. Leonard’s Church and the top of the great sand rock bed, may be about 200 to 250 feet; the-sand rock bed itself, under the castle, about 80 to 120 feet; and thence to the lowest point upon the coast, east of Hastings, about 200 or 250.—Total thickness, between 400 and 500 feet 26, It is difficult, from their contortions, to estimate the thickness of the Purbeck strata on the coast. Mr. Webster has given in detail the stratification of a portion of them, which amounts to 124 feet, 8 inches?” ; to which may be added about 150 feet,—making a total of about 275°. In the Vale of Wardour, the total remaining thickness of the group appears to be from 40 to 60 i EEE ann ina ! Martin, p. 20,—who states, however that 100 feet would probably be no exaggeration of the thickness, where the stratum first emerges from beneath the chalk. 2 Webster, Letters, &c., p- 140.: and supra (93.), p. 183. 3 Supra (120.), p. 236.; and (93.) p. 183. = (t28.), p 216.; (129.), p. 247. * (1441.), p. 265. © (158.), p- 305. 7 (161.), p. 314. 8 (11.), p. 109. 9 (49.), p. 140. 10 (93.), p. 184. 11 (129.), p. 247. 12 (148.), p.279. 13 (158.), p. 306. 14 (160.), p. 311. 15 Rose, p. 181. 16 Supra (161.), p. 314. a (17.), p. 116. 18 (25.) p. 122. 19 (32.) p. 126. 20 Geol. Trans., 2nd Ser. vol. ii. p- 102. 21 Martin, p. 36—40. 22 (148.), A. p. 280. °3 Rose, p. 176. 2 Martin, p- 36.and40. °% Supra(100.), p. 198. 26 (80.) to (84.), p. 163—172. °7 Geol. Trans., 2nd Ser. vol. ii. p. 39. 28 Supra (104.), p. 209. VOL. IV.—SECOND SERIES. a 320 Dr. Firron on the Strata below the Chalk. feet', and in Buckinghamshire still less. Mr. De la Beche estimates the whole formation at 250 feet’. The aggregate thickness, therefore, of the three groups which compose the Wealden, cannot, probably, be less than 800 feet. Portland stone.—This formation being well defined and fully exposed, its thickness is well as- certained ; and in Portland Island it seems to range between 60 feet* and about 70,°; at Swindon it is about 60 to 65°: at Great Hazeley in Oxfordshire 27 feet7; at Brill, about 23 feet®; near Quainton and Whitchurch in Buckinghamshire, from 4 to 20 feet’. Portland sand.—Near St. Alban’s Head, Isle of Purbeck, 120 to 140? feet!°; in the Isle of Portland, 80 feet!!; near Thame in Oxfordshire, about 50 feet '*. Kimmeridge clay.—The thickness of this group is uncertain, and seems to vary much in dif- ferent places. On the coast Messrs. Buckland and De la Beche assign to it 600 feet, at Kim- meridge Bay'’; but they state the thickness at Ringstead Bay to be only 300 feet'*. At the Headington quarries in Oxfordshire, I found, in one of the pits, only 20 feet of clay'*. The general thickness is stated by Mr. De la Beche to be 500 feet'®. Oxford oolite.x—On the coast near Weymouth, 150 feet!’.. The whole, in Wiltshire, according to Mr. Lonsdale, about 200 feet !*; Mr. De la Beche, 150 feet 9. Oxford clay.—On the Dorsetshire coast, near Weymouth, 300 feet®: at Lynn in West Nor- folk Mr. Rose assigns to this formation the whole depth of a well, which would make the thickness about 630 feet®'; but part of this depth may possibly be Kimmeridge clay. Mr. De la Beche’s estimate for the whole formation is 600 feet 2%. (164.) Order of Geological Events.—The succession of events which the preceding pages demonstrate, has been already detailed in some other pub- lications* ; but they are too important not to be recited here. The evidence bearing on the following propositions, derived from the South Eastern Coast, the Vale of Wardour, and Buckinghamshire, is all in perfect harmony; and the inferences are so directly connected with the facts, as to be rather corol- laries than deductions from them. 1. Deposition, beneath the sea, of the following groups of strata, beginning with the lowest :— a. Oxford oolite. b, Weymouth and Kimmeridge strata. c. The Portland sand and stone. . Elevation of the Portland strata above the sea. . Submersion, by fresh water, of the newly disclosed land. tm CoO to . Deposition beneath fresh water, above the Portland strata,—first, of a thin bed of clay ; and then of a crust of freshwater limestone, the “ skull-cap.” (111.) p. 224, and (118.) p. 226. | Supra (132.), p. 251. 2 (150.), p. 285-6. 3 Tabular View. * Webster, Geol. Trans. vol. il. p. 42,43; and Pi. VI. fig. 3. | ° Buckland and De la Beche, PI. III. fig. 1. of this volume. ® Supra(141.),p.267. 7 (144.),p. 276-277. ° (148.), C.p. 280-1. 9 (152.), p, 288, 290. 10 (106.), p. 212.—Section, fig. 5. Plate X.b. ‘' Buckland and De la Beche, p.19. of this volume. 12 Supra (148.) p. 282-3. 1S Page 19. of this volume.—This estimate, however, appears to be too great : see above, (107.) p. 212-13. __'* Pl, ILL. of this volume, fig. 1.; and p.22, 1.6. 15 Supra (146.), p. 278-9. 16 ‘Tabular View. '7 Buckland and De la Beche, p- 23. of this volume, |. 2. from bottom. 's Geol. Trans. 2nd Series, vol iii. p. 261. '9 Tabular View. °° Buckland and De la Beche, p. 28. of this volume. "1 Rose, p. 174.5 supra (161.) p. 316. 2 Tabular View. * See the works of Mr. Mantell; Dr. Buckland’s and Mr. De la Beche’s paper in the present volume ; and the ‘‘ Geology of Hastings”, p. 79, &c. Dr. Firron on the Strata below the Chalk 321 5. Deposition upon the “ skull-cap” of a bed of “dirt”, (110.) p.223.; and exposure of it as dry land. 6, Growth upon this land, of the Cycadezx now found in the Dirt-bed, i situ, and in the upright position. 10: p. 223-4. 7. Second submersion (at least), of the Jand, in fresh water; proved by the deposition and exist- ence of the “cap”. (111.) 9, p.222, 3; and (113.) p. 226. 8. Exposure of the surface of this “‘cap” as land; and growth upon it of coniferous trees, and of Cycadez. (111.) 8, p. 220-22. 9. Ravages (from the effects of currents of wind, or water,—or from earthquakes), by which the trees were overthrown, or broken off at short distances above the roots. 10. Third submersion, in fresh water ; and deposition of slaty limestone, containing freshwater fossils only, but near the bottom alternating with clay*. (111.) p. 219, 220.; and (113.) p- 226. 11. Alternation of Oysters with freshwater fossils in the slaty Purbeck limestone; proving access of the seat, apparently in an estuary (104.) p. 208; and (113.) p. 226. 12. Continuance of the estuarine condition during the whole remaining epoch of the Wealden ; proved by the occasional presence of oyster-shells, throughout the Hastings-sands and Weald-clay. (98.) p.190.; and List of Fossils, p. 178. 13. Sudden, or rapid, depression of the entire Wealden, to such a depth as to be covered with salt water; proved by the sudden and exclusive appearance of marine productions and fossils, above and in immediate apposition with strata containing only freshwater fossils, though mineralogically of the same composition, (100.) p. 196-7. (165.) Local Distribution of the Strata.—If a line drawn from the coast at Folkstone, touching London on the north, and thence towards Newport Pagnell; and another line from about Atherfield in the Isle of Wight towards Faringdon in Berkshire, the tract intervening wiil comprise the space throughout which the beds immediately below the chaik are most fully developed : and if the standard be taken from the condition of the strata when possessed of their greatest bulk, that of the Green-sands and Wealden may be said to occur in Kent, Sussex, and the Isle of Wight; from which central tract these groups appear to thin out in every direction. The whole series immediately below the chalk is finely developed between * The alternations, in this case, are distinguished from those of the coal formation, (in which also the remains of terrestrial and freshwater productions alternate—in some instances repeatedly— with those of marine origin), by the growth of plants upon the surface of some of the alternating strata ; a proof of their exposure, as dry land, between successive immersions. Mr. Prestwich, in a valuable paper on the coal-field of Coalbrook Dale, has justly remarked, that the repeated alternations in that district are no proof that the tract itself was raised above the sea and again depressed, as many times as the freshwater remains alternate with the marine ;—since the facts may be accounted for by supposing that the strata were accumulated in an estuary liable to freshes from a river of considerable size.—Proceedings of Geol. Society, 1836, vol. ii. + Lamarck (Animaux sans Vertébres, vol. vi.) mentions altogether 81 species of the genus Ostrea; 48 of which are of existing species, 33 known only in the fossil state. Of the 48 recent species, 40 are marine, and 8 uncertain, but also probably marine. In the present state of our knowledge therefore, the occurrence of Oysters may fairly be considered as proof of the former access of the sea. Pin © Be) Dr. Firron on the Strata below the Chalk. Farnham and Petersfield and around the west end of the Wealden denu- dation; the Lower green-sand, especially, is nowhere better disclosed, except in the Isle of Wight. It is not improbable, that the part of these groups which once intervened between the Isle of Wight and the Sussex coast, and is now concealed by the sea, was likewise fully expanded; but at Folkstone the Upper green-sand has already become much thinner. It remains yet to be ascertained whether in their prolongation northward in England, and towards the east on the continent of Europe, these groups again assume their more bulky and varied form, as our Upper green-sand is observed to do after reduction, even within very short distances; and whether, if they do so expand, the relative proportions of the component members be the same in remote countries ; an inquiry which is the more in- teresting in the case of the green-sand formation, from its very wide diffu- sion, and the great space which it occupies in different parts of Kurope. Deraits.—The following are some of the local variations in the strata composing the groups above referred to :— Chalk.—It may be remarked that the chalk rises much more rapidly towards its outcrop, between Wiltshire and Hertfordshire, than in the more northern counties of the South East of England. In departing from that central tract, both towards Devonshire on the south, and northwards, the rise is comparatively small; the beds shooting out very gradually, and occupying very wide spaces of uniform, flat country. The disturbance, by which the ridge of the Wealds and the parallel range of elevations through the Isle of Wight and Dorsetshire were produced, wasprobably the principal cause of this variation: and the mean course of the Thames itself, from the point where it cuts through the chalk, may possibly be connected with that derange- ment. But in the chalk itself, on the south-west of London, much local variation is found in the angle and direction of the dip; and from the facts mentioned by Mr. De la Beche, respect- ing the faults in Devonshire, and what I have seen of the minor irregularities on the shore near Hastings, it is probable that if the whole surface in this part of England were examined with equal attention, it would prove to be pervaded by cracks and slight dislocations. The Upper green-sand is especially remarkable for great variation in its thickness and compo- sition; and it is everywhere so intimately connected with the lowest beds of the chalk, that if we had more accurate measurements of our strata, the total thickness of that formation, in- cluding the Upper green-sand—might, perhaps, be found to be nearly uniform. The latter passes most commonly by insensible gradation into the soft dark-coloured marly chalk. In many cases, it forms a very thin and scarcely distinguishable group,—as near Folkstone, where it is not more than 20 feet thick ; in others, the chert which it contains becomes conspicuous, and it affords also beds of firestone, which together giving it firmness and durability, cause it to project as a step or prominence beyond the foot of the chalk range. On the west of Portland, the green-sands thin out so rapidly, that at Blackdown a series about 200 feet thick is their only representative ; and it is difficult to decide whether this be a con- densed equivalent, of the whole group between the chalk and the lowest green-sand,—or, (which seems to be more probable,) only a continuation of the lower part of the Upper green-sand, from the Vale of Wardour. In following the range of these formations towards the north-east, Dr. Firron on the Strata below the Chalk. 323 a similar reduction of the green-sands is observable, as the section at Hunstanton remarkably proves; but the diminution is by no means uniform throughout the intermediate space. Along the coast of Devonshire, the beds at the bottom of the upper sand seem to adopt the characters which the Lower green-sand exhibits in other places ; and the latter, as well as the usually inter- vening gault seems to be wanting. In the Vale of Wardour also, where the Lower sand is scarcely apparent, the Upper green-sand exhibits many of its characters; but the Gault is very distinct between them. The Gault is seen in the greatest perfection on the coast at Folkstone, where its fossils are especially beautiful and numerous. It seems to be thinner and to contain few fossils in the Isle of Wight, and is almost wholly wanting on the west of Purbeck. But in the interior—in the Vale of Wardour, and thence northward to the sea at Hunstanton,—this stratum everywhere appears, and contains throughout many of the same fossils, though it changes its character and is much reduced in bulk in Norfolk. The almost constant presence of this distinct band of clay between the chalk and Lower green- sand, considering its small relative thickness, is a remarkable fact: and its retention, both in En- gland and on the Continent, of the same mineralogical characters and fossils, renders the Gault a very important member of the series. I have seen it in its proper place, and in the form of bluish clay, all around the Lower Boulonnois; in the vicinity of Aix-la-Chapelle ; and in the country between that place and Liege. The Lower green-sand thins out remarkably towards the west, from the central tract just men- tioned, (p. 321-2.). The traces of it in the Vale of Wardour are obscure, but they become gra- dually more distinct towards the north. The subdivisions of the Kentish coast, detailed in (16.) to (35.) and in Sussex (72.), deserve comparison with the more expanded equivalents of this formation in other countries. Their existence in the Isle of Wight is almost certain; and they will probably be found in Bedfordshire: but thence, north-eastward, the sands again become thinner, though they still preserve their relative place. The Wealden.—This group, also, is best developed near the central tract already pointed out. The Weald-clay is seen in the greatest perfection in the Isle of Wight; and the Hastings-sand in the Forest ridge of Kent and Sussex, &c. But the Purbeck strata are fully expanded only in the Isle of Purbeck, and on the adjacent coast of Dorsetshire. No traces of any member of this group have been found west of the Isle of Portland; nor eastward of that island, near the coast, except in the vicinity of Battle in Sussex. In the Vale of Wardour, the Weald-clay and Hastings-sands are reduced almost to nothing ; and they have not yet been found along the line of the green-sands between that place and the neighbourhood of Oxford*. Thence, to Quainton and Whitchurch in Buckinghamshire, the representatives of the Purbeck strata, though perfectly distinct, are but a few feet in thickness, and belong to the lowest beds of the formation. Other indications of the Wealden may be looked for, north of Whitchurch, in the detached portions of sand represented in Mr. Smith’s maps of Buckinghamshire and Bedfordshire: and the speci- mens of Lonchopteris said to occur at Wansford on the north-east of Northamptonshire, (if they be really found in situ), would prove that the Hastings-sands exist at that place. * The subdivisions of the Wealden, especially at the upper part, being in some measure arbitrary, it is often difficult to determine which of the three groups any given portion of unconnected strata ought to be referred to. The same fossils pervade the whole; and beds of sand, clay, and stone, almost identical may be produced from all parts of the series; so that collective evidence alone can be resorted to for the purpose of distinction. 324 Dr. Firron on the Strata below the Chalk. The places beyond the limits of the tract described in the preceding pages, in which the existence of the Wealden has been ascertained, or rendered probable, are mentioned hereafter, (168.) p. 526. The sudden change from the marine fossils of the Lower green-sand to the freshwater pro- ductions of the Wealden is remarkably exhibited at Atherfield in the Isle of Wight (100.) p.196; where the former stratum contains nearly thirty species, of about twenty genera; while the Weald- clay, not more than ten feet vertically beneath, contains scarcely any other shells than Cypris, Cyclas, and Paludina*. The contrast, in descending from the Wealden group, is equally striking and abrupt ;—the Purbeck strata near their junction with the Portland affording scarcely any fossil but Cypris, while the “‘ Roche” at the top of the Portland group, within a few inches of the freshwater limestone, is full of marine remains. (111.) p. 224. The Wealden strata, though differing so widely as to their fossils, appear to be conformable to those of the adjoining formations, both below them and above. On the Dorsetshire coast, in the Vale of Wardour, and in Buckinghamshire, the Purbeck beds correspond exactly in dip and direction to the Portland stone beneath; and at Hythe in Kent, and in the Isle of Wight, the lowest beds of the green-sand are perfectly continuous with the upper beds of the Weald-clay, (98-) p. 189. The only place with which I am yet acquainted, where a want of conformity is in- dicated between these formations, is at Stopham in West Sussex, adverted to in (74.) p. 156. But the eroded cavities, filled with what seem to be green-sand and Fuller’s earth, in the upper part of many of the quarries in Oxfordshire and Buckinghamshire, (of which those at Great Hazeley and Dinton are good examples,) indicate an interval and some intervening disturbance, between the periods of their production. (114.) p. 276; and (151.) p. 286. (166.) Theory of the Wealden.—The mode in which the Wealden is disposed, in the South-east of England, accords with the hypothesis of its having originated in a lake of fresh water, or in the estuary of a large river. it remains to be determined whether similar deposits are found to occupy a corresponding situation in other parts of the great European basin, of which England is but a small portion. The chalk and green-sands in England are so frequently prolonged be- yond the limits of the beds below, concealing their outcrop, that no certain * Wocdward, so long ago as in 1702, pointed out the resemblance of the Wealden Paludine, to some recent freshwater species': and Mr. Sowerby, about 1812, after mentioning their oc- currence at Bethersden in Kent, remarks that ‘from these different localities of shells, appa- “rently of the same genus, we must conclude, either that analogy is not sufficient to prove that ** these fossils are of freshwater origin; or else that there are more freshwater formations than ‘are generally supposed?”. Mr. Webster, about the same period, distinctly mentioned the existence of freshwater shells in the Purbeck strata, and the probability that a part of that formation had been deposited from fresh water’. In 1822, Mr. Mantell reasoned with great sagacity upon the inferences derivable from the fossils, discovered by himself at Tilgate Forest*: but the geology of the strata connected with that group was then undetermined ; and the diffi- culties, I believe, were not removed till 1824. ' “History of Fossils”; quoted by Webster,—Letters, &c., pp. 142, 192. | % Min. Con. vol. i. p- 76. tab. 31. > Letters, &c. to Sir Harry Englefield, pp. 192. and 237. + Illustrations of the Geology of Sussex, 4to, 1832. Dr. Firron on the Strata below the Chalk. 325 inference can be drawn with respect to the continuity beneath them of the Wealden and Portland strata. It is not improbable that what now appear to be detached portions, may in many cases be united ; but it seems to be con- sistent with the mode in which freshwater deposits have been formed, whe- ther in lakes or estuaries, that they should, in more extensive regions, occur in detached, rather than continuous portions; and that the outlines of the spaces which they occupy should be irregular. The former existence of the upper Wealden strata in the interior of England, is rendered probable by the ero- sion of the Purbeck beds in many places where the Lower green-sand comes into contact with them, (151.) p. 286,—which has clearly been effected by the action of water, and proves that something was carried away, before the sand was deposited: the argument from these appearances being the same as that derived from the erosions on the surface of the Oxford oolite and of the chalk, (143.) p. 274. The great extent of the surface occupied by water in North America is a striking feature in every ordinary map. Dr. Richardson, in his observations on the geology of that region, has remarked that a large tract near the confines of the primitive and secondary regions is occupied by lakes of the most varied outlines and dimensions ;—in which the deposition of shells and other exuvie of organized beings has been going on ever since the surface of the globe assumed its present aspect. If that part of the northern hemisphere were now to be sunk beneath the sea, we should probably have, after a short time, one universal sheet of marine strata, lodged upon the surface of the present land, so as to conceal not only the deposits of the several lakes, but the intervals between them: and if we could, then, examine the interna! structure of the tract, we should find it to be occupied by a numerous series of Wealdens, detached from each other, and bordered, it is more than pro- bable, by deposits analogous to those of the dirt-beds of Portland, wherever the fluctuations of the lacustrine waters left time and space for the growth of plants upon their margin. The external boundaries of these deposits would be as various and irregular as that of the lakes which now diversify the map of North America: and we should expect, in such cases, that the mineral! components in the deposits of the lakes, would vary according to the nature of the surrounding land. Their fossil contents would, probably, have a great general resemblance throughout large districts ; but, in the remoter tracts would differ as much as the productions of modern lakes are found to vary ;—as those of the lakes in the North of England differ from those of Switzerland, and both from those of the South of France, &c.; or, as in America, those of Slave-Lake differ from the productions of Lake-Superior 326 Dr. Fitton on the Strata below the Chalk. or Lake-Erie. 'The lacustrine deposits, again, would be occasionally diver- sified by the presence of the products of estuaries, such as those of the St. Lawrence and of other rivers around Hudson’s Bay and the north-east coast of America; and in these we should probably find, along with the species of shells which usually inhabit the mouths of large rivers and the borders of the sea, some scattered remains of the products of the adjacent shores,—the plants and animals of the land, with some admixture of freshwater shells. (167.) Wealden in other Districts.—The following are the places beyond the limits of the tract described in the preceding pages, in which the presence of the Wealden strata has hitherto been ascertained, or rendered probable. Scottanp.—In the Isle of Skye Professor Sedgwick and Mr. Murchison discovered, in cliffs of blue shale associated with trap, on the eastern shore of Loch Staffen, flattened masses of limestone, containing several species of shells; some of which are identical with fossils which I had found in the upper beds of the Weald-clay at Swanage Bay on the Dorsetshire coast; and all the rest are freshwater species belonging to genera found in the Wealden of the south*. The coincident species are the following; some of which are figured in the plates subjoined to these pages :—Cyclas media (Plate XXI. fig. 10.); Cyclas, a larger species (C. major, Pl. XXI. fig. 13., Isle of Wight); Cyclas cbovata?; Neritina Fittoni, Mantell (Pl. XXI. fig. 7.); Ostrea distorta, found with Cyclades in the Isle of Wight, (Pl. XXII. fig. 2.); Paludina elongata; Isle of Wight and Swanage Bay; a transversely elongated Bivalve, (Isle of Wight); an Unio, or Anodon. There can be little doubt, therefore, as Mr. Murchison has inferred, that this deposit was con- temporaneous with the English Wealden. Continent oF Evrore.—The places out of England, where the equivalents of the Wealden beds have hitherto been found, are the two following. 1. In the Lower Boulonnois the presence of the lower member of the group, at least, is certain; the strata bemg almost identical with some of those upon the confines of the Purbeck and Port- land formations in Dorsetshire and the Vale of Wardour. Having given an account of that part of the French coast on another occasion f, it will be sufficient to mention here, that the line of the cliffs from Equihen on the south of Boulogne to Cape Gris-nez on the north of that place, is capped at intervals with a thin crust of the Purbeck strata, resting upon those of Portland, and consisting of slaty beds of limestone, which contain freshwater shells, and include a bed of tough dark-co- Joured clay, in which are numerous fragments of silicified coniferous trunks not distinguishable from those of the Isle of Portland. It is highly probable that a more exact examination of this part of the series, in the cliffs near Boulogne, may lead to the detection of these trunks in the upright position; and of the Cycadez by which they are accompanied on the Dorsetshire coast. 2. The Pays de Bray, near Beauvais, is a narrow tract on the line from Dieppe to Beauvais, extending in length, from the north-west of Neufchatel to the south of the latter city, a distance of about thirtyEnglish miles, and in breadth, at the widest part near the middle, about eight English miles. (See the annexed Map, Plate IX.) It is an opening, or valley of elevation, in the chalk, * « Supplementary Remarks”, &c., (1827,) Geol. Trans., 2nd Series, vol. ii. pp. 352 and 366. t In a paper including some account of the Lower Boulonnis: See the abstract; Geol. Soc. Proceedings, Dec. 1826, vol. i. p. 9. Dr. Firton on the Strata below the Chalk. 327 within whick a very slight elevation of the central tract has brought into view the subjacent strata, as far down as those which immediately precede the representative of our Oxford oolite, with perhaps the mountain limestone beneath. I have not myself examined this interesting district ; and the only publications relating to it that I have seen, are the report of the proceedings of the Geological Society of Paris during their excursion to Beauvais in 1831 *, and the splendid work of M. Passy on the Geology of the Department of the Lower Seine} :—but from the notes and sectional sketch of M. Cordier in the former of these works, and the full descriptions of M. Passy, there can be no doubt that the strata in the Pays de Bray are the same with the upper part of the series in the Lower Boulonnois. The following is the order of the strata in the Pays de Bray, with what appear to me to be their equivalents in England; my list of equivalents, 1 am glad to find, coinciding very nearly with that of M. Passy himself. 1. La Craie.—(CHaAxx). 2. Glauconie sableuse de la craie.—( Upper GREEN-SAND), Fossils said to be the same as of the Lower Chalk. 3. Marne micacée et Marne blewe.—(Gavtt). Divisible, (at Ferte en Bray) into two portions :—1. Brown and micaceous. 2. Blue. At Meulin the blue marl is about 50 feet thick; it abounds in iridescent fossils, among which are, Ammonites splendens; Hamites intermedius; Inoceramus sulcatus; Nucula pectinata. 4, Gres, et sable, Glauco-ferrugineux.—(LowER GREEN-SAND). At Cap la Héve are two beds of sand and ferruginous conglomerate, separated by a micaceous and glauconious marl. Que. the three subdivisions of Folkstone??. At Forges and Neufchatel the ferruginous sand is 70 feet thick: it occurs above the Argile bigarée, mentioned hereafter, and contains, among other fossils, Gryphea sinuata. At Les Friches de St. Germain is iron ore in grains, including small portions of ochreous hydrate of iron, with marine shells. 5. Argile bigarée (Glaise Marbré.)—Variegated marl clay, and, sand,—(of tHE WEALDEN ; —or Beds subordinate to the Lower GREEN-SAND.) This deposit, which, according to M. Passy, is found everywhere in the Valley of the Pays de Bray, seems from the description to be very like the variegated sandy clay of the Wealden; but at St. Paul, near Beauvais, it is said to contain marine shells, the species of which, however, are not mentioned. Its place is commonly below the first stage of ferruginous sand and grit, and above the Argile a fougéres ; a situation corresponding to the place of some of the Wealden marls. 6. Argile a creusets; Argile de Forges; Argile a fougéres—(WEALD-CLAY). This clay in one place, at Neufchatel, is extracted by means of a shaft 70 French feet in depth, and occurs beneath sand of different shades, belonging to the Glauco-ferruginous beds,No. 4. above. At St. Germaine la Poterie, a bed of slaty clay (lignite) is found, containing impressions of Lonchopteris Mantellii, and from one to two metres thick§: and among the beds found by M. Graves near Songeons, is one, described as ‘‘ Marbre d’eau douce a Paludines,” and referred by him to the Purbeck strata||. There can be little doubt, therefore, that some equivalent of the Wealden heds exists in this tract; but M. Passy appears to me to be in error when he is led, (no doubt by the indistinctness with which the strata are developed and exposed in the Pays de Bray), to regard the Wealden * Bulletin de la Société Géologique de France, 1831, p. 1.to 23. t Description Géologique du Departement de la Seine Inférieure, 4to, Rouen, 1832. t Passy, p. 237 to 272 ;—and Plates I. II. II. IX. and XVII. fig. 1. § Passy, p. 255. || Ibid., p. 257. VOL. IV.—SECOND SERIES. Oh 328 Dr. Frrron on the Strata below the Chalk. generally, in England, as no more than in a particular and subordinate bed of the Glauco-ferru- ginous sands*. 7. Grés glauconnieux; Grés vert.—(PoRTLAND-sTONE AND SAND.) These terms are applied to green-sand passing into grit, which again passes into a calcaire glauconnieux. Both the grit and limestone are full of green particles: they alternate with beds of sand, and are generally quarried throughout the Pays de Bray: and the grés calcaire is stated to he identical with that observed by M. Rozet, at Mont Lambert in the Boulonnois. Among the fossils are Ammonites ; Crassatella ; Cuculleea; Ostrea; Serpula ; Trigonia; and teeth of the Diodon. M. Passy justly expresses doubt whether this grit has hitherto been recognised in England, — I believe it to belong to what I have proposed to call the Portland-sand; the characters and relations of which, though long since generally intimated by Mr. Conybeare, have not hitherto been fully understood in England: and, from my own observation, I have no doubt that some of the concretional masses of the Boulonnois belong to this part of our series. It will be observed, on comparing M. Passy’s sections with those in the interior of England, that the lower greenish grit (Portland-sand) of M. Passy ‘+, is not conformable to the beds above ;—a fact analogous to the existence of chasms and “ gullies”, in the Lower Purbeck, and upper part of the Portland strata, in Oxfordshire and Bucks:—supra(111.), p. 218; (141.), p. 265; (144.), p. 276, (151.). 8. Calcaire glauconnieux ;—a limestone composed of fragments of shells, united by sparry carbonate of lime, containing green particles, rolled grains of quartz, and flints of different hues. The fossils include Ostrea gregarea, and other indistinct species; T’rigonia; and Crassatella. The limestone in this group alternates with grit, and includes a bed of green or bluish marl. The whole belongs to the group between the Portiand-sand and the Oxford-oolite in the Lower Bou- lonnois and is represented in England by part of the series on the coast near Weymouth. 9. Marne et calcaire marneux ;—a Gryphea Virgula; Calcaire lumachelle. The strata of this group are described as occurring unconformably—(‘ étendues en couches dis- cordantes”), beneath the ferruginous sands: a statement which accords with the relations of the group to the Upper green-sand,—but not to the sands of Portland. The formation is characterized by Gryphea Virgula, and some of the beds contain Ostrea deltordea. On the coast, from Havre towards Henqueville, it occupies a thickness of 30 metres (about 100 English feet), between the chalk and the oolite{; and it seems to be the equivalent of the series of shale, limestone, and cal- ciferous grit abounding in petrifactions, which connects the Kimmeridge-clay with the Oxford oolite, on the coast of the Boulonnois, and of Dorsetshire. 10. The lowest strata of the Pays de Bray “consist of blackish compact limestone, like that of ‘“« Marquise in the Lower Boulonnois ;—the carboniferous limestone of England:” and these suc- ceed immediately to the group last mentioned. If this be so, the oolitic series, from the Oxford oolite to the bottom of the lias, is wanting; together with new red sandstone and the coal forma- tion :—another point of resemblance to the Lower Boulonnois. (168.) Marine deposits coeval with the Wealden.—It is obvious that, during a period of time sufficient for the accumulation of the Wealden, the deposition of matter in the adjacent seas could not have been inconsiderable ; so that we might expect to find, interposed between the strata which then formed the * « .,..que l’argile Veldienne qui contient les coquilles d’eau douce, n’est qu’une couche “ particuliére de terrains glauco-ferrugineux d’Angleterre.”—p. 256. + Passy, p. 272; and Plates I. and II. t Ibid., p. 262, 265. Dr. Fitton on the Strata below the Chalk. 329 ‘bottom of the sea, and the Lower green-sand, a series of beds coeval with the Wealden in point of date, but differing from it in possessing the charac- ters of a marine deposit, and including marine shells and other productions of salt water ;—with which, near the shore, the productions of the land, or even the freshwater shells of the rivers, might be occasionaly intermixed. And if the Portland strata constituted at that epoch, both the dry land, and the bottom of the sea, and were afterwards submerged, we ought now to find the Lower greensand, in some places immediately in contact with the Portland,— in others with the Wealden,—and in others again with the marine equivalent of this latter group. Two results would probably attend the state of things here supposed, which are deserving of notice: Ist, That the Wealden and its marine equivalent could not both be found in the same place ; and consequently, (since we have the former in England), that the marine beds of that date are not to be expected generally in this country: 2ndly, That the marine fossils of the beds cotemporaneous with the Wealden would probably be distinct, both from those of the Portland group beneath, and of the Green-sands above them ; a consideration which gives peculiar interest to the fossils of this in- termediate group. The strata between the chalk and the oolitic system on the continent of Europe have not yet been sufficiently examined, to furnish all the evidence that may be expected upon this subject ; but indications of such an equivalent to our Wealden as has been mentioned, have been already found in so many detached points, that its occurrence in other places, or even the existence of a continuous marine deposit of that age, is by no means improbable. Mr. De la Beche* has brought together evidence which shows that such a group exists in the department of the Haute Sadne, in France ; at Candern, in the Brisgau ; near Aarau ; in Poland ; and on the confines of Silesia. To these may be added the Isle of Bornholm in the Baltic, and the vicinity of Helsing- burg, in Scania, which have afforded specimens of fossil plants resembling those of our Wealden, along with marine shells ; but at Bornholm, although the shells are also marine, they are generally such as may be supposed to have inhabited, either the estuary of a large river, or the seas immediately ad- jacent to the coast. In most of the cases mentioned by Mr. De la Beche, a group of strata between the chalk and the dolitic system is found to contain pisiform iron ore; but the fossils which accompany that mineral are marine. A very extensive deposit of this kind in Poland and Silesia is described by Professor Pusch, which includes also argillaceous iron ore; and among its-fossils are the genera Ammonites, * Geological Manual, (1833.), p. 309. 2u 2 330 Dr. Firron on the Strata below the Chalk. Cardium, Venus, Trigonia, Sanguinolaria. The pisiform ore of the Haute Saéne appears from the statements of M. Thirria to be above the Portland strata; butits relations to the superior forma- tions are less distinct. It contains Ammonites, Hamites, Nerinea, Cirrus, Terebratula, and Pentacrinites, with teeth of fishes and of Saurians : and it is observable that the uppermost stratum in the group supposed by M. Thirria to represent the Portland stone, is “‘a compact conchoidal ** limestone, a little tubercular, which contains a species of Paludina? near to Vivipara fluviorum “of Sowerby ;”—a description which might very well be applied to some of our Purbeck strata. M. Walchner has ascertained that the pisiform and reniform iron ores of Candern, belong te two distinct formations, of very different date. The lower rests upon beds of “ Jura limestone ”, which he refers to the Coral-rag or Portland-stone, and which are decidedly below the molasse of Switzerland. The second and more recent pisolitic deposit occupies eroded cavities on the sur- face of several different formations; it consists of transported matter containing fossil bones, and is not covered by any solid strata. M. Merian is cited by M. Walchner in support of this view of the relations of these deposits; but in the description given by the former, of the strata which im- mediately cover the pisiform ore of Aarau, there are features very like those of our Wealden itself: for they are mentioned as consisting of ‘“ grit and bituminous schist passing into lignite, and “containing a great number of petrifactions, among which, though commonly indistinct, are a ‘Planorbis, and other freshwater shells.” The doubt which obviously presents itself with respect to the evidence above mentioned, is, whether a formation thus contiguous to the green-sands, and so very nearly coeval with them, may not really be a part of that formation itself; the presence of some fossils distinct from ours, not being sufficient to prohibit this identification. But the peculiar character and abundance of the iron ore, are important circumstances of difference. The evidence respecting Bornholm occurs in a paper read before the Geological Society by Dr. Beck of Copenhagen*, who states that the beds below the cretaceous group in that island, exhibit many of the characters of a coal formation, containing coal and numerous impressions of ferns, among which are several of the genus Pecopteris; and with these was found the seed vessel of a Restiacea, considered by Dr. Beck as identical with one from the Hastings-sand at Heathfield in Sussex, which he himself had seen in Mr. Mantell’s collection. The existence in the vicinity of Hoer, of fossil plants analogous to those of the Wealden, but probably be- longing to the oolitic series, had been previously pointed out by Mr. Adolphe Brongniart+: but from what has been very recently mentioned to me by Professor Nilsson of Lund, after he had examined some of our best collections of the Wealden fossils, it is probable that a deposit contemporaneous with that formation may be found at Helsingburg in Scania, between the chalk and green-sands which occur near the coast of the Baltic, and the Lias, known to exist on the north-west of that place The observations of M. Boblaye in the northt, of M. Desnoyers § in the north-west, and of M.Dufresnoy|}; in the south-west of France ; with those of M. Elie de Beaumont, on the boundary of the Paris and London Basins] ; of Mr. De la Beche **, M. de Caumont++, M. Desnoyers{f, * « Proceedings ” (1835-6) vol. ii. p. 217. + Annales des Sciences Naturelles, 1825. + Ibid., 1820, t. xvii. p. 35. § Ibid., 1825, t. iv. p. 353. || Ibid., 1829, t. xvil. p. 192 @ Ibid., 1829, t. xvii. p. 354. ** Geol. Trans. 2nd Series, vol. i. p. 13. ++ Mém. de la Soc. Linn. du Calvados, t. i. 1824, p. 49 et 67; t. ii, 1825. p. 447, &e. cs Mém. de la Soc. d’Hist. Nat, de Paris, t. ii. 1825. at Dr. Firron on the Strata below the Chalk. 331 M. Constant Prevost*, and M. Passy t, on the coast of Normandy and the adjacent district ; and more recently of M. Thirria, in the department of the Haute Sadnef, have shown that many of the beds between the chalk and the oolitic system in the different provinces of France, agree with each other, and with those of England, perhaps as nearly as the more distant portions of the same formations are found to do in our country: the Portland strata, which form the lower boundary of the Wealden, occurring at several detached points along their course ; while above them, the chalk affords a limit which cannot be mistaken. It may deserve the inquiry, there- fore, of resident geologists, whether traces at least, of all the intermediate groups between the Portland and the chalk may not be detected generally along the line of connexion; and I am not without hope that the task of comparative examination may be assisted by the preceding pages. Among the points deserving of notice by those who examine the beds below the chalk in dis- tricts imperfectly known, I would mention especially the characters of the Portland Sand ;—from the facility with which that formation may be confounded with other sands, likewise charged with green particles. I have reason to believe that a neglect of the distinctions between these dif- ferent sands, and a consequent ignorance of the distance by which they are separated in the series of strata, has produced difficulty, and led to much confusion in the arrangement of the groups be- tween the chalk and the oolitic system. (169.) Beds below the Wealden.—The groups next below the Wealden, in the tracts described in the preceding pages, are connected by several cha- racters; the Portland sand forms a transition to the Kimmeridge clay; and the latter, at its lower part becomes charged with sand and calcareous matter, and passes insensibly into the Oxford oolite. The fossils, also, of these associated groups are very much allied, and there is no reason to suppose that the deposition of this part of the series was interrupted by any important change of circumstances. Portland strata.—The space occupied by the Portland strata, so far as they have yet been dis- covered in England, is bounded on the west by a line passing from Portland to the outcrop of the Portland stone in the Vale of Wardour, and thence towards Swindon. On the east of that line the Purbeck and Portland formations are visible only in the remaining portions of the once- continuous sheet, which seems originally to have invested a great part of Oxfordshire and Buck- inghamshire. Whether the Portland beds exist, or ever have existed, under the sands of the Isle of Wight, Sussex, and Kent, it is now impossible to say; though it is probable that they did so, from their occurrence on the opposite coast of France, and their thickness in that quarter. The peculiar circumstance relating to the junction of this formation with the Purbeck beds, is the distinct character of superficial soil, which the bed in which the trees and Cycadee are found, exhibits in the Isle of Portland. Trees and plants have occurred in the upright position in many other places, and in other parts of the series of strata; but the soil in those cases had lost its recent character, and been in a great measure assimilated to the surrounding matter. Some other thin beds alternating with the lowest strata of the Purbeck limestone, have likewise more * Mém. de la Soc. d’Hist. Nat. de Paris, t. ii. 1825. p. 389. + Sur le Département, §c. 4to, Paris, 1833. t Mém. de la Soc. d’Hist. Nat. de Strasbourg, 1830, t.i. 332 Dr. Firron on the Strata below the Chalk. or less of the character of a mechanical agglomerate ; but none of them approach to the grayel- like texture and composition of the “ Black-dirt” of Portland and the adjacent coast. The small extent which the Portland strata occupy with reference to the Kimmeridge clay, is a remarkable fact ; showing either that the former, like the Coral-rag, was originally deposited in detached portions ;—or that the portions of the Portland group that we now see, are only the re- maining and eroded borders of one continuous coating originally lodged upon the clay. It is remarkable, also, that the Wealden has not yet been found beyond the limits of the Port- iand group; never reposing, as the green-sands are frequently seen to do, on any of the formations beneath the Portland stone: but before this exclusion be adopted, it will be necessary to examine more completely the counties on the north of Buckinghamshire. Reciprocally, in all the places where the Portland beds have hitherto been found, one or more members of the Wealden group are connected with it. It is possible, therefore, that the Portland strata formed the only land, at the period when the freshwater beds of the Wealden group began to be deposited. The Kimmeridge clay thus more widely diffused than the Portland and the Wealden, forms the continuation upwards, of a long series of alternate strata of oolitic limestones, sand, and clay. The extent, thickness, and development, of this formation, vary much in different places, the upper beds alone being visible at the point from whence the name has been derived. The relations of the groups are fully seen on the coast near Weymouth, and still more completely on the shore of the Boulonnois, and near Scarborough: but, although the clay extends, without interruption, from Dorsetshire to Norfolk, it is seldom seen to advantage in the interior of En- gland. Near Oxford, the lower members, which form the transition from the bituminous clays of Kimmeridge to the Oxford oolite, are evidently wanting; and the surface of the calcareous reestone beneath the clay, is deeply worn and eroded. (170.) Composition of Strata.—Among the circumstances relating to the composition of the strata above mentioned, below the chalk in the South-East of England, the following are deserving of attention. 1. Proofs of the formation of stone, in the midst of strata of gravel, sand, and clay, distinctly of mechanical origin. This fact, which is of universal occurrence throughout the series of secondary strata, is especially remarkable in the Lower green and the Hastings sands of Kent and Sussex : sex: the former containing masses of siliceous grit, chert, and chalcedony, and concretions of chert, evidently formed subsequently to the division of the beds which inclose them, yet traversed by the same lines of false stratification which pervade the looser matter :—(22.) and (23.) 2. The change, in the fossil trees of Portland, of the original woody substance into silex ; and the contrast of their composition with that of the surrounding matter in the “ Dirt-bed”, in which fragments of soft limestone are abundant; the strata, both above and below, likewise, consisting principally of carbonate of lime. In the Lower green-sand also, at Woburn, the petrifying petrifying matter of the coniferous wood is silex*. 3. The shells preserved in the green-sands of Kent, consist of carbonate of lime; but in the sands of Blackdown, though shells occur in still greater numbers, the calcareous matter has almost entirely disappeared, and with very few exceptions has been replaced by chalcedony; and the surrounding sand, instead of effervescing with acids, imbibes them tranquilly. * The fact remarked by Mr. Brown, that all the fossil wood hitherto discovered in the strata mentioned in these pages, is either monocotyledonous, coniferous, or cycadeous, has been already adverted to: (112.) p. 225. Dr. Firron on the Strata below the Chalk. 333 4, The occurrence of oolite containing freshwater shells, near the bottom of the Purbeck strata at Combe Wood (144.), p. 275-6, is another fact deserving of notice, and may perhaps explain some doubtful appearances in the uppermost bed of the Portland Series (the Roche); which, although full of marine petrifactions, and commonly oolitic, has very much the aspect of fresh- water limestone. It can easily be imagined that the bank, or land, consisting of the Portland strata, when first raised above the sea, was covered with marine remains, which might subse- quently have been cemented together, at the bottom of a freshwater lake. 5. The existence of pisolitic (or granular) oxide of iron, in the Wealden, is probably not con- fined to the coast near Hastings, where I found it to be generally diffused; p.166. The fact of its occurrence in this formation is the more deserving of notice, from the great abundance of that ore in the marme deposits supposed to be contemporaneous with our Wealden, in other parts of Eu- rope: supra, (168.) p. 330. (171.) Stmilarity of Deposits of different Epochs.—The mineralogical resemblance between some of the strata above and beneath the Wealden, is very remarkable.—T he upper part of the Portland formation in the Vale of Wardour is so like chalk, that it bears that name in some of the quarries; and both there and upon the coast of Dorsetshire it contains flint nodules, not distinguishable from those of the chalk.—The Portland sand abounding in green particles, cannot, in itself, be distinguished from the green-sands above the chalk, nor from those below; the green matter in all is of the same nature; the calcareous concretions are like those of the ‘ Kentish- rag”: yet the deposition of these groups was separated by intervals of time sufficient, in the first two cases, for the accumulation of all the Wealden strata, and in the two latter, for that of the chalk.—The strong re- semblance of the variegated sands and marl of the Wealden to those of the new red sandstone, and of both to the tea-coloured and variegated marls of the beds above the chalk in the Isle of Wight, has been already mentioned. —The Wealden, again, has many striking points of resemblance to the coal measures. ‘The shale, sandstones, and clay iron-stone of the latter are not distinguishable from those of the Hastings-sands, which are, in fact, a coal formation : and in addition to the Unios and other freshwater shells long known in the coal formations, the recent discovery of Cypris, in freshwater limestone, among the coal measures in Scotland*, is another point of agree- ment. These resemblances, of which other examples might easily be given, in de- posits separated by great intervals of time, demonstrate the identity of the processes which are still going on with those of the more ancient epochs, * See, however, upon this subject, the remark of Mr. Sowerby, as to the possible resemblance of the fossil crusts of the marine genus Cytherina, to those of Cypris: Appendix, p. 345, under the head Cypris Valdensis. 334 Dr. Firron on the Strata below the Chalk. and prepare the mind for the reception of other proofs of that continuity of action, which has of late been so ably discussed. (173.) Fossils.—A systematic list of all the fossils mentioned in the pre- ceding pages* is given in the Appendix B: andI have connected with ita series of columns, exhibiting at one view the stratigraphic distribution of the several species. My collection is so incomplete, that many of the columns are un- occupied ; and most of them afford very inadequate representations of the facts: but it will be advantageous to keep in view the completion of such a list, whenever sufficient materials shall be obtained to fill it up. The number of specimens collected from any given district or series of strata, depends on so many circumstances purely accidental,—the texture of the matrix, the num- ber of open quarries, the relative skill and activity of collectors,—that the richest collections can very seldom be regarded as fairly representing the fossil contents of the groups from which they are obtained ; and there still are large tracts, in every part of the English series, the fossils of which are un- known. The proportion, therefore, which the species we are acquainted with, bear to the whole number contained in the strata, is so far from being de- termined, that any general reasoning upon this subject at present would be of little value. From the imperfect lists of fossils given above, it would seem that even short distances are attended with greater variation in the contents of the strata, than might have been expected ; and that although some species pervade the whole range of the formations in which they are found, others occur in several of the tracts described which have not yet been obtained elsewhere. I cannot conclude these pages without expressing my great obligation to Mr. Lonsdale, for his kind and unremitting assistance during their passage through the press ; which has been doubly acceptable, from its having been conferred on me by one of my most valued personal friends. W. H. EF London, August 16, 1836. * It may be proper to mention here, that the whole of the author’s collection re- ferred to in the preceding lists, has been presented to the Geological Society, and will be found in their Museum. App. A. | Dr. Fitton on the Strata below the Chalk. 335 APPENDIX. APP. A. Descriptive Notes respecting the Shells figured in Plates XI. to XXIII. By James pe Carte Sowersy, F.L.S. &c. PLATE XI. Fig. 1. Tornatella elongata. Elliptical, elongated; surface furrowed; furrows crossed by short lines ; whorls about four ; lip slightly thickened. This resembles Acteon ( Tornatella) simu- latus (Min. Con. t. 163. f.2.) of the London clay, even in the dotted furrows upon the surface of the shell, but it is much longer in proportion, and is only half the size. Fig.2. Lucina? globosa. A nearly globose smooth shell, with the lines of growth peculiarly waved near the posterior margin. TI have not seen the interior. Fig. 3. Avicula Grypheoides. ‘The convex valve nearly orbicular, with a projecting incurved beak, and two small unequal ears: when alone, it may easily be mistaken for Znoceramus con- centricus, but the parts about the beak, especially the ears, show the difference. The other valve is nearly flat, orbicular, and has one small and one large ear. The convex valve a. is represented from specimens found at Nursted in Hampshire ; the other valve, b. is from Cambridgeshire. Fig. 4. Pentacrinus. The stem only has yet been found; it is various in size, the sides are concave, the angles rounded. Joints equal, the margins of their surfaces ornamented with short strie. Some specimens show the bases of lateral arms. It strongly resembles a species found in the chalk ;—(Mantell ; Fossils of the South Downs, p.183; Geol. of the S.E. of England, p.112.); which is, however, much larger. Fig. 5. Pollicipes levis. The lateral valves are rhomboidal, smooth, thin, and nearly flat: in the partially decomposed state in which they are found, they appear to be composed of layers, of different degrees of transparency and depths of colour. This species also occurs in the green- sand at Blackdown: see Plate XVI. fig. 1. Fig. 5*. Pollictpes unguis. Smooth, the valves are all remarkably curved, and broad in pro- portion to their length. Fig. 6. Pollicipes radiatus. Valves wedge-shaped, flat, marked with sharp, elevated rays, di- verging from their apices. Fig. 6*. Pollicipes rigidus is distinguished by thin transverse elevations, which are very promi- nent upon the posterior valves: the lateral valves are elongated. Fig. 7. Venus? tenera. Shell lenticular, rather transverse, neatly marked with concentric strie ; lunette lanceolate. Fig. 7*. Venericardia tenuicosta. Transversely oblong, approaching to square. It varies much in convexity: and when old or interrupted in its growth, is nearly globose, rather heart~ shaped. Specimens have been found twice the length of that represented in the figure, both of the oblong and globose form. The surface of the rays is rough, with slightly elevated obtuse scales. The interior of the margin is crenated. Lunette rather deep, heart-shaped. Fig. 8. Nucula bivirgata. Very convex; the surface ornamented with two sets of linear furrows, which meet towards the posterior slope, at acute angles directed towards the beak of each valve; the junction producing a regular line, without forming a ridge. Lunette broad. VOL. 1V.— SECOND SERIES. 2x 336 Dr. Firron on the Strata below the Chalk. App. A.J} Fig. 9. Modiola bella. Neatly striated, convex, with parallel edges, nearly equal sides, and obtuse beaks. Fig. 10. Lima semisulcata. (Plagiostoma semisulcatum, Nilsson, Petrif. Suec. 25, t. ix. f. 3.) Ovate elongated, very convex, the beaks incurved, short ; ears nearly equal, sinall. Where the lines of growth cross the ridges, which vary in number from 11 to 16, they form obtuse, short scales or grains. Fig.11. Auricula inflata. (Benett’s Catalogue of Wiltshire Fossils, 4to, p. 2.) Shell ovate; spire small, pointed ; the last whorl large; aperture at the lower part approaching to square, but with one of the upper angles elongated and acute; the lips united, thick, obtuse; the colu- mella has two plaits, the lower sometimes divided by a groove along its middle. The surface of the shell is marked with numerous spiral lines of elongated punctures. The thick lip separates this from several species of Tornatella, to which in other respects it bears a strong resemblance. Auricula incrassata of Min. Conch. t. 163. is shorter and smaller, and has the lip more enlarged. A. incrassata of Mantell (Geol. Sussex, t. xix. figs. 2, 3, and 34.) also resembles it, but has a much shorter spire. Fig.12. Natica canaliculata. (Ampullaria canaliculata, Mantell, Geol. Suss. tab. xix. fig. 18.) Globose, depressed, smooth. Umbilicus large, circular, gradually expanded into the base. Around the upper edges of the whorls is a concave, transversely striated groove, best defined in the young shell,—as in c. The inferior specimen, a. b. is filled with brownish phosphate of lime. See the figure of a much larger specimen, Plate XVIII. fig. 6. Fig. 13. Solarium ornatum. Discoid, with a small portion of the spire elevated and acute ; aperture rhomboidal. Surface, above ornamented with obtuse, radiating ribs,—and near the margin, both above and below, with granules in quincunx order. Fig. 14. Solarium conoideum. (Min. Conch. t. 11.) A conical shell as high as it is wide; the umbilicus large and smooth. The outer coat of the shell is represented in this figure; and shows the upper part of each whorl to be concave, and elegantly marked with decussating strize forming rows of granules; aperture rhomboidal, nearly square. Fig. 15. Pyrula Smith. Ovato-fusiform; two obscure keels and numerous strie wind round its surface; spire rather elongated, acute. ‘These two figures, perhaps, represent different species: fig. a. is more distinctly keeled than fig. b., which, however, being considerably worn, — has lost much of its external sculpture; but shows also longitudinal undulations, which can hardly be traced upon fig. a. Both the specimens are from Copt Point, near Folkstone. Murex — Smithii (Min. Con. 578), lately removed to the genus Pyrula, is a different shell. ie Fig. 16. Rostellaria elongata. Presumed to be a Rostellaria, from its resemblance to R. mar- ginata, fig. 18. ; from which it differs principally in its great length and the smaller number of” ribs. Turrited, much elongated, ribbed, transversely striated; upper edge of the whorls smooth. Fig. 17. Rostellaria buceinoides. A neat, subulate, costated shell, approaching to A. rimosa ; it has but one varix upon each whorl: the lip is not lobed. Fig. 18. Rostellaria marginata, ‘Turrited, conical, transversely striated ; ribs eight or ten upon each whorl, short and obtuse ; last whorl keeled, without ribs. Named from a ridge or narrow band upon the upper edge of each whorl; which is more or less conspicuous in every specimen, and assists in distinguishing the species from Rostellaria Parkinsoni. See Pl. XVIII. fig. 24. Fig. 19. Rostellaria carinata. (Mantell; Fossils of the South Downs, p- 86, Pl. XIX. figs. 10, 11,12, and 14.) This figure, from a drawing by the Rev. G. E. Smith, exhibits the lip in an ad- vanced stage of growth. The spire is nearly subulate, composed of eight or nine convex whorls; a row of small tubercles, or short ribs, winds round the middle of each whorl except the last, - v3 a App: A] Dr. Firron on the Strata below the Chalk: 337 which has two acute keels; the lip has a long forked projection arising from the upper keel ; the beak is long and subulate; the whole surface striated. Fig. 20. Ammonites? circularis. Aperture circular; whorls just touching each other: nearly close, acute, cif¢ilar; sometimes forked ridges cover the surface. This specimen may, perhaps, be a portion of an Hamites or Scaphites ? Fig..21.. Ammonites symmetricus. Aperture nearly square; ribs blunt, slightly tumid as they approach ‘the hollow in which the rounded keel is immersed, and though not equal in length, elegantly uniform in their elevation; the sides of the whorls flattened. The specimen here fi- gured, though a fragment only, differs from every Ammonite known to me. Fig. 22. Ammonites crenatus. Sides flattened; the inner whorls much exposed, their margins nearly smooth and rounded, those of the outer whorls crenated on each side of a narrow concave space over the siphuncle. Distinguished from 4, splendens by the more exposed inner whorls. Fig. 23. Ammonites cristatus. (De Luc, in Brongniart, Env. de Paris, pl. vii. 10.) Some of the ribs being acute and much more elevated than others, form the distinguishing character of this species. I believe 4. cristatus and A. subcristatus of De Luc to be varieties of the same species : I have seen both from Folkstone : the specimen before us belongs rather to the latter variety. PLATE XII. Figs. 1, 2. Hamites rotundus. (Min. Conch. tab. Ixi. fig. 2, 3.) The peculiar structure of the inner extremity in this species, is indicated, rather than distinctly seen, in these figures ; which have been engraved from drawings by the Rev. G. E. Smith, taken from specimens collected by Lord Greenock, near Copt Point in Kent. Mr. Smith observes, in a note sent with the drawings, that the termination in a minute whorl, (imperfectly seen in the figures,) had been traced distinctly in more than one specimen; which proved that the coils of the spiral were nearly parallel to the straight part of the stem, and the axis at right angles to it. The spiral appears to have been open, as in many recent Serpule; so that its perfect preservation in the fossil could scarcely have been expected : and this would 4 account for the defective state in which the Hamite is commonly found. Mr. Smith adds that the spiral portion appeared invariably to have been decayed, as if it had been filled up with soft Matter, as in the case of Magilus. The figures show the remains of the spiral, in two different specimens; but in both much broken and displaced. The spiral part is round, with contiguous annular ribs, also round and regular. Fig. 3. Hamites attenuatus. (Min. Conch. t. lxi. fig. 4. and 5.) Both ends of this species, when complete, are similarly bent or folded in, not spirally, but so that the segments become parallel toeach other. The larger parts are rather compressed, the smaller cylindrical; the ribs are annular and rounded. Fig.4. Hamites spiniger. The general form of this species is like that of Scaphites Yvanii, (Bull. de la Soe. Géol. de France, vol. ii. p. 355, pl. ii.) ; one portion being a flat volute, like an Ammonite, but with unconnected whorls; the other bent into the characteristic form of a Hamites: the sides are flattened. The spines form one of the chief specific characters: there are three rows of them on each side, placed upon the larger ribs on the involute part of the shell ; they are gradually lost upon the other parts. PLATE XIII. Fig. 1. Echinus? arenosus. 'The underside is imperfect, and the genus therefore doubtful. Fig. 2. Panopea rotundata. Only a cast, which is nearly smooth. The ridge separating the posterior area, which is small, is strongly marked, and projects on the margin. 2x2 338 Dr. Firron on the Strata below the Chalk. [ App. A. Fig. 3. Trigonia spinosa, var. Distinguished from Trigonia spinosa (Min. Conch, t. lxxxvi.), of which it is a variety, by the presence of longitudinal ridges continued from the bases of the spines, and by its more oblique form. It is often longer than the specimen here figured. Fig. 4. Diceras Lonsdalii. The small portion hitherto examined of the external impression of this curious fossil, shows the shell to have been squamose, like an Oyster, and of considerable thickness. The two valves are less equal in size than is usual in the genus Diceras. The larger valve is an elongated cone, rather flattened and curved twice round; and it appears to have been attached to some foreign body, as in Diceras arietinum. The other valve has only an oblique conical umbo. PLATE XIV. Fig. 1. Pholas giganteus. In general aspect much resembles a Pholadomya; but the appa- rently squamose structure of the surface shows it to belong to the same section of the Pholades as P.candidus. Its valves are so convex as to form nearly a cylinder when closed. The reflected margin near the beak, so large in some Pholades, is probably broken away in this specimen. Fig. 2. Modiola lineata. ‘The depth of each valve is equal to its width; the beaks are ob- tuse ; the margins are arched and nearly parallel; the surface Jongitudinally and finely striated. Fig. 3. Avicula pectinata. A slightly convex shell, with large, square, depressed ears, and short acute linear ridges, alternately longer. Fig. 4. Ostrea retusa. This, like most Oysters, is very variable in form, but generally much curved and nearly orbicular; the shell is moderately thick, plain in the middle, but strongly plicated at the margin with angular plaits. It occurs in massy groups. It is not so flat as O. semiplana, a fossil of the chalk ; nor are its valves so equal, nor so thin, as in that species, which it otherwise much resembles. Fig.5. Anomia radiata. Irregularly orbicular, flat, finely radiated. The radii are coarser, and more distant, than the fine striae which occur in the London clay species, Anomia lineata, (Min. Conch. t. 425.) Fig. 6. Anomia levigata. Much smoother, and more even, than any other known species : very thin, orbicular, and flat. The figures a. and b. are taken from different specimens; a. in Mr. Smith’s collections; b.in Mr. Sowerby’s. fig. 7. Anomia convera. A remarkably convex species, with a large and prominent beak, and smooth surface. The furrows are produced by a Terebratula to which this specimen was attached, and to which it consequently bears a great resemblance. [The name of this new species has been omitted, by mistake, in the list of Lower green-sand fossils of the Isle of Wight, p.204. It was found there in the debris fallen from the cliff, on the shore east of Shanklin Chine. | Fig. 8. Yerebratula Tamarindus. Nearly orbicular, smooth; margin very obtuse. Disk rather flattened ; beaks but little curved, with an angular, slightly prominent ridge on each side, passing down the sides of the valves. Fig. 9. Terebratula quadrata. Ovate, gibbose; beak large; front broad, straight, with a few large plaits. Fig. 10. Terebratula Faba. Elliptical, narrow, gibbose; front concave, but not elevated, very narrow ; the perforated beak short, but prominent. Fig.11. Terebratula elegans. Transversely obovate; beak prominent, pointed, nearly straight; plaits numerous, sharp ; front slightly elevated, straight. Fig.12. Terebratula convera. Angles rounded; valves very regularly convex; beak large; plaits numerous, rounded ; front slightly elevated. App. A. | Dr. Frrron on the Strata below the Chalk. 339 Fig. 13. Terebratula parvirostris. Imperfectly tetrahedral, rounded; beak small, sharp; sides slightly produced and angular; plaits numerous, angular ; eight or nine of them much ele- vated in the front. Fig. 14. TYerebratula prelonga. Ovate, much elongated, gibbose; front slightly elevated, with a depression in its middle ; beak prominent, large ; surface smooth. The figure a. is from a drawing by the Rev. G. E. Smith; b. from another specimen, also found near Sandgate. Fig. 15. Lingula? truncata. Ovate, depressed, flattened most along the middle; front straight. Fig. 16. Pleurotomaria gigantea. (Trochus; British Mineralogy, t. 403.) Conical, height and breadth equal; whorls slightly overlapping each other; sides straight; surface concentrically striated. The transversely striated band proceeding from the deep sinus in the lip, which marks the genus, is well preserved on a specimen seven inches in diameter, in the collection of Charles Manning, Esq., who obtained it from near Hythe, after this plate was engraved. Some speci- mens of this shell are so much changed by pressure as not to be above one inch high, while they are three or four inches in diameter, with a sharp margin. Fig.17. Ammonites furcatus. Discoid, sides and front flat; inner whorls partly exposed ; aperture with a square front, oblong, deeply impressed with the preceding whorl, lateral angles truncated ; ribs not very numerous, thick, curved, many of them forked, passing at right angles across the front. PLATE XV. Scaphites Hillsii*. General form obovate, compressed ; the inner whorls exposed, not touching each other, but still curved into a regular volute, compressed, bearing numerous small, close» rounded ribs: the outer whorl strikes off from the others, in nearly a straight line, to a con- siderable distance, and then bends back so that the aperture nearly touches the preceding whorl, furnished with ten or more distant, very prominent, sharp-edged ribs, which are most raised upon the sides. Aperture nearly square, thin-edged, preceded by a short rib over the front; Siphuncle small, close along the front, or outer margin of the whorls ; septa much sinuated, not very close. ‘The system of inner whorls occupies rather more than half the longest diameter of the entire shell, which is about fourteen inches. Fig. 1. represents a specimen of the inner whorls, reduced to half the real diameter. A small Exogyra was found attached to the inner margin of one of the whorls of this individual, showing that there was always a space between it and the next whorl. Fig. 2. is drawn from a portion of an outer whorl, also half the natural size. The specimen is irregularly flattened. The above description has been made from several nearly entire specimens, obtained from the vicinity of Maidstone after this plate was engraved, and now in the possession of Sir Philip Grey Egerton, Mr. Bowerbank, and Mr. Sowerby. An outline, taken principally from Sir P. G. Eger- ton’s specimen, on a scale of one fifth of the original dimensions, is inserted in the plate at fig. 3. Mr. Sowerby has also a specimen, from the same place, of a species nearly agreeing with this one, but probably distinct: it is much larger; and its system of inner whorls is free from radii and undulations. * In the list at p. 128, this fossil is erroneously called Hamites; perfect specimens not having been found, when that page was printed. 340 Dr. Fitton on the Strata below the Chalk. [ App. A. PLATE XV. a. Siphonia pyriformis. (Goldfuss, Petrefactenkunde, tab. vi. fig. 7.) This plate represents several varieties in the form of this Siphonia, with some details of its structure ; from which it may be inferred that the upper, enlarged part becomes broader in proportion, and more pear-shaped, as it increases in size. But although this may be stated as a general rule, the exceptions are numerous, and there seems to be as much variety in the form of the full-grown specimens of the fossil, as in that of the fruit from which this species has been named. Figure 4, a specimen nearly entire, shows the root-shaped, lower, part of the stem, by which it was fixed to the rock on which it grew. The condition of the fossil does not enable us to speak decidedly as to the original state of the external surface in the living animal: we can perceive, however, that beneath the surface was a system of large tubular canals, placed in a circle, with some degree of regularity as to their distance from each other, and succeeded at intervals by other concentric circles of similar tubes. These are shown in the vertical and horizontal sections fig. 6. and 7., which had been very carefully ground down by the late Mr. Miller, for the pur- pose of showing the structure, and in the broken and abraded specimens, fig. 4. and 5. Fig. 8. is a specimen of a lower portion of the stem which belonged to the late Mr. Goodhall, F.G.S: Its external surface having been removed, the tubes which form the lower part of the stem are well displayed: and a similar observation may be applied to the head, fig. 5. In fig. 9. a head is represented, the greater part of which is embraced by a Serpula. From this tube being at present nearly half immersed in the substance of the head, and from the groove-like impression visible in some places, it would appear that after the Serpula had attached itself, the head must have increased considerably in diameter; still, however, preserving its general form and proportions, where not covered by that tube. PLATE XVI. Fig. 1. Pollicipes levis: from Blackdown, Devonshire. Supposed to be of the same species as Plate XJ. fig. 5, found in the Gault near Folkstone. Fig. 2. Serpula filiformis. The mode of grouping in this Serpula is remarkable. It consists of smooth, round tubes, slightly curved, and aggregated into elongated, often branching masses. The tubes are rather thick, nearly equal throughout their substance. This fossil may be the same with that which Goldfuss calls S. soczalis, (Petrefactenkunde, tab. lxix. fig. 12.) ; but as he iden- tifies the species from the oolite with that of the green-sand, I would retain his name for the former only. The substance of this shell in our green-sand fossil is thinner, and the tube gene- rally more curved, than in the S. soczalis of the oolite. » Fig: 3. Serpula Tuba. Simple, almost solitary tubes, of nearly uniform diameter throughout; shell ‘thin. ; - Fig. 4. Serpula Vermes. The tube gradually increases in size, and has a carina along its upper surface. It is a larger, coarser species than Serpula carinella, (Min. Conch. t. 598. fig. 2.).) S. conformis of Goldfuss (Petrefact. tab. Ixvii. fig. 13.) is like it, but has subangular sides. Fig. 5. Panopea ovalis. The regularly oval form shown by the lines of growth, distinguish this from the species found either in the crag or recent: neither does the anterior side gape so much as in any of them. It is moderately convex and smooth; the beaks are nearest the anterior side, which is closed; the posterior extremity is rounded and gaping. Fig. 6. Mya leviuscula. So perfect is this cast in calcedony, that even the asperities of the epidermis, such as occur in recent species, are preserved. The shell, which is nearly twice as | App. A. | Dr. Firron on the Strata below the Chalk. SAl wide as it is long, is moderately gibbose, and has a characteristic depression along its middle. The sides gape slightly. ; Fig. 7. Amphidesma? tenuistriatum. A transversely elongated, oblong, very flat shell, with numerous impressed stria, the posterior extremity slightly truncated ; the beaks nearly central, not produced. The genus is rather doubtful. ’ Fig. 8. Corbula truncata. Very similar to one, or two, species in the London clay. Its form is oblong-ovate; the posterior side is produced, obliquely truncated, and pointed towards the front. ‘The surface is transversely striated. - Fig. 9. Mactra? angulata. Smooth, subtriangular; the posterior side defined by a ridge ; beaks small, nearly close ; hinge unknown. Fig. 10. Petricola nuciformis. Suborbicular ; striated longitudinally ; the edge serrated ; the beaks small, sunk into the shell. Fig.11. Petricola canaliculata. Orbicular, very convex, longitudinally furrowed; furrows nearly covered over edge graiiulated. The concealed furrows are represented in the magnified section; the edges of the costae between them are sometimes connected across the furrows. Fig. 12. Psammobia? gracilis. Much elongated transversely, nearly cylindrical; surface marked with many raised lines, which are most elevated at their extremities; posterior side de- fined, produced, and pointed. Fig. 13. Lucina? orbicularis. Orbicular; convex; longitudinally striated; striae numerous, often forked; beaks small, distant; edge entire. Fig. 14. Lucina Pisum. Nearly globose ; fifteen, or more, reflected ridges cross the surface. Fig. 15. Astarte concinna. Oblong, convex, concentrically furrowed, thick; lunette elon- gated, deeply sunk; beaks oblique. In everything, except the elongated form, this resembles Astarte striata, (Min. Conch. t. 520. f. 1.), which is orbicular. Fig. 16. Astarte formosa. Orbicular, approaching to triangular, rather flat, with thick edges ; about ten prominent reflected ridges on the surface ; lunette elongated, concave. Found in great numbers at Blackdown. Fig. 17. Astarte multistriata. Very convex; rather wedge-shaped; with many concentric ridges, and numerous fine longitudinal striae between them ; lunette large and broad. A small, rare species. Fig. 18. Astarte impolita. Obovate, convex, rather angular at the beaks: surface anti- quated ; ligament imbedded in a lanceolate groove. Fig.19. Cyprina cuneata. Cordato-cuneiform ; surface even; posterior side straight, a little produced at its extremity ; beaks prominent; valves deep; shell rather thin. The specimens found at Blackdown are seldom larger than the small figure: the large one was in the collection of the late Mr. Goodhall. PLATE XVII. Fig. 1. Cyprina rostrata. Distinguished by its general form from Cyprina (Venus) angulata (Min. Conch. t. 65.), which it nearly resembles. It is less convex, the posterior extremity is more produced, and the line thence to the beak straighter. Fig. 2. Cytherea subrotunda. Fiat, lenticular, nearly orbicular, smooth; lunette elongated ; fulcrum arched. One specimen has an Exogyra adhering to an eroded part of the surface. Fig.3. Venus? truncata. Rather less convex than V. lineolata (Min. Conch. t. 20.); strongly marked with lines of growth; the posterior side expanded and truncated; lunette obscure, lanceolate. 342 Dr. Firron on the Strata below the Chalk. [App. A. Fig. 4. Venus? submersa. Nearly orbicular; valves tumid; the posterior extremity truncated ; lunette obscure; hinge-slope rather straight. Fig. 5. Venus? sublevis. Very fiat, elliptical, smooth ; lunette undefined, not sunk. Fig. 6. Venus? immersa. Very flat, ovate, smooth ; lunette deeply sunk ; its edge not defined. Fig. 7. Cucullea formosa.’ More deeply striated than C. fibrosa; and in form resembling C. carmata (Min. Conch. t. 207.). Very convex, transversely elongated; posterior extremity pointed. Fig.8. Arca rotundata. Surface longitudinally striated; the sides unequal; both rounded. There is no space between the beaks. Fig. 9. Nucula lineata. Elliptical; posterior extremity slightly truncated, with a short point af its upper angle; surface transversely striated, with lines straighter than the lines of growth, which they consequently cross twice. Fig. 10. Nucula apiculata. Convex, smooth, transversely obovate; posterior extremity pointed. Fig.11. Nucula obtusa. Convex, smooth, elliptical ; lunette prominent, elongated. Fig.12. Trigonia quadrata. Nearly square, flat; anterior extremity rounded ; concentrically ribbed ; each rib bent at a right angle in the middle, where there is an obtuse knob. Fig.13. Modiola reversa. Transversely elongated, rather flattened; the posterior portion expanded ; surface ornamented with thin concentric ridges, which are bent back or reversed upon the shell. In some individuals they are worn away. Fig. 14. Mytilus tridens. The hinge is furnished with three unequal teeth; elongated, convex, carinated ; beaks pointed; the surface very smooth. The teeth distinguish this species from M. edentulus (Min. Conch. t. 439. fig. 1.). Fig. 15. Mytilus prelongus. Hinge without teeth; shell very thick, much elongated, keel- shaped. It approaches to M. lanceolatus (Min. Conch. t.439. fig. 2.); but, independently of its remarkable thickness, the sides are nearly parallel, as far as the termination of the hinge-line, which is marked by an angle. Fig. 16. Mytilus inequivalvis. Shell broad; one valve much flatter than the other; both smooth. Fig. 17. Perna rostrata. Ovate, nearly flat; the surface very smooth; the lesser wing pro- duced; the shell thin, contracted at its base. Fragments of this species are very common at Blackdown, but perfect specimens rare. Fig. 18. Avicula anomala. Obliquely elongated, imperfectly five-angled, flat along the middle; many longitudinal, narrow, elevated ridges extend over the surface, and are crossed by fine lines of growth. The valves are very deep, together measuring about 14 inch, with a square section; length three inches. This shell I believe to be an Avicula, although the hinge is not visible. Fig.19. Pecten Millerii. Oblong, rather convex ; radii smooth, sharp, numerous, especially towards the edge; close together. The two smaller figures represent an unusually convex specimen. Fig. 20. Pecten compositus. Oblong; with about 20 smooth, sharp, radii, and two rows of scales between each of them. Fig. 21. Lima? subovalis. Rather quadrangular, elongated; radii very numerous, equal to the furrows between them, and ornamented with one row of rather obtuse distant scales. PLATE XVIII. Fig. 1. Pecten Stutchburiensis. Suborbicular, compressed; radii more than 60, alternately smaller, scaly ; those towards one side large and distant, with oblique striz between them. + App. A. ] Dr. Firron on the Strata below the Chalk. 343 Fig. 2. Terebratula dilatata. Wider than long, depressed, imperfectly three-lobed; plaited, plaits about 50, sharp; central lobe elevated; beak of the larger valve short and large. This resembles Terebratula Vespertilio of Brocchi, but is not so wide nor so distinctly three-lobed. Fig. 3. T'erebratula megatrema?. Moderately convex, transversely obovate; with a few distinct ribs. The beak is large and produced, with a very large perforation: whence the name. Fig. 4. Dentaliwm medium. (An inferior figure is in Min. Conch. t. 79.) Subulate, very slightly curved, striated ; stric sharp, elevated, alternately smaller, gradually disappearing towards the aperture. Fig. 5. Litorina pungens. Conical, acute, smooth; whorls five or six, the last inflated ; aperture orbicular, with a projecting angle above; columella slightly compressed. This species, probably, belongs to a group of shells which Lamarck has called Ampullaria; and which in the Mineral Conchology is referred to Natica, but in the Index to that work is named Globulus. The columella is, however, rather different. Fig. 6. Natica canaliculata. Species the same as Pl. XI. fig. 12, but a much larger specimen. Fig. 7. Natica granosa. Subglobose ; spire prominent, pointed, small; covered with spiral ridges which are divided by the lines of growth into rounded granules; whorls very convex ; aperture oblong, expanded ; umbilicus open. Fig. 8. Natica? carinata. Oblong, with a small distinct spire ; surface marked with five pro- minent rugged keels ; aperture large. This shell appears to be umbilicated, but is not perfect ; hence the genus is doubtful. Fig. 9. Tornatella affinis. Ovate, pointed; base truncated; surface grooved, grooves crossed by lines; columella with one simple and one double fold. Very like Acteon ( Tornatella) simulatus of the London clay, (Min. Conch. tab. 163. fig. 5. to 8.) but more elongated, more acute, and smaller ; yet shorter than Tornatella elongata, (tab. 11. fig. 1.), Fig. 10. Vermetus concavus. (Min. Conch. t. 57. fig. 1.to 5.) Tube rounded, curved into a depressed spiral, which is concave beneath; the whorls united by an expansion of the shell from the sides. These figures show the prolongation of the tube beyond the spiral part, which is not shown in the Mineral Conchology. Fig. 11. Scalaria pulchra. An acute shell, with blunt costz ; whorls ten, close: a band con- necting the costz passes along the bases of the whorls. Fig. 12. Littorina gracilis. A pretty, elongated, acute shell, with round whorls, bearing de- cussated furrows on their upper parts; aperture round, with an angle at the base. Fig. 13. Phasianella pusilla. Elliptical, elongated, pointed, perfectly smooth ; aperture ellip- tical, more than half as long as the shell. Fig. 14. Phasianella formosa. Elliptical, elongated, rather blunt; smooth, except a few striz at the base; aperture more than half the length of the shell. Fig.15. Phasianella striata. Elliptical, pointed, strongly striated ; aperture oval, above half the length of the shell. This is like Phasianella princeps (Defrance), but more regularly oval. Fig. 16. Fusus rigidus. Fusiform, costated, transversely striated ; costze rounded, roughened by the lines of growth; transverse striae prominent, about 10 upon each whorl; whorls five or six, swelled in the middle, compressed at the upper part; aperture more than half as long as the shell, elliptical, pointed at both ends; beak variously elongated. The individuals of this species differ much in length and asperity ; the edge of the aperture is frequently reflected. Fig.17. Fusus quadratus. (Murex quadratus, Min. Conch. t. 410, young.) Fusiform, rhom- boidal, with a short conical spire, transversely striated and obscurely bicarinated ; base produced, conical ; whorls about five ; aperture sub-rhomboidal. The form of the shell is fully developed in the specimen here represented. VOL IV.—SECOND SERIES. 2Y 344 Dr. Firron on the Strata below the Chalk. [App. A. Fig. 18. Fusus rusticus. A short, rugged, ovato-rhomboidal shell; with 10 or 12 ribs, each of which is formed into two knobs, so arranged as to give a squareness to the whorls; transversely striated ; aperture ovate. Fig. 19. Fusus clathratus. Sub-pyriform, costated and transversely striated; four carine crossing the costz divide the surface of each whorl into three rows of cells; spire very short. The form is nearly that of a Pyrula. Fig. 20. Pyrula depressa. Pyriform, with the spire sunk beneath the surface of the last whorl. Ornamented with many transverse, thread-shaped ridges. Fig. 21. Pyrula Brightu. Ovate, sub-rhomboidal, ventricose, transversely bicarinated, and coarsely striated: aperture sub-rhomboidal; whorls four or five. Some specimens resemble Fusus quadratus, (fig. 17.); but they are shorter, have fewer and more thread-like strize, and crenated carine.—Named after Richard Bright, Esq. of Ham Green, near Bristol. Fig. 22. Rostellaria retusa. A short, ovate, striated shell; whorls rounded, with one distinct and one obscure carina on each. It has only one elongated, narrqw branch to the lip. The surface between the strize is particularly smooth. Fig.23. Rostellaria macrostoma. Turrited, with convex, carinated whorls; carine five, the middle one most prominent ; aperture small, round, with a very much expanded and flattened lip, furnished with at least two branches besides the curved beak. Fig. 24. Rostellaria Parkinsoni. (Mantell; Geol. of Sussex, t. 18. figs. 1, 2,4, 5, 6, and 10. Min. Con. t. 558, upper fig. 3.) Turrited, transversely striated, costated; costee numerous, oblique, long; aperture narrow ; its broad lip furnished with one large subulate process directed upwards, and a broad angular expansion below it; beak long and subulate. The specimen, of which two views are here represented, is not perfect, but yet shows the form of the shell better than any before published, and proves that Mr. Parkinson’s specimen from Faversham is a dif- ferent species, although figured as the same in the Min. Conchology. Fig. 25. Nassa lineata. Ovate, acute, wide at the base, transversely striated ; whorls flattish, the upper edges sharp, distinct; aperture longer than the spire. Several species from the crag of Suffolk somewhat resemble this; but in them the body whorl is much smaller. Fig. 26. Nassa costellata. Subulate, costated, and transversely striated ; whorls about eight, ventricose, each bearing one varix; aperture nearly orbicular ; lip thick. Fig.27. Ammonites triserialis. Discoid, with a flat margin, umbilicate, radiated. Three rows of protuberances, upon the marginal portions of the radii, and about ten tubercles around the umbilicus, distinguish this species. The aperture is nearly square. All its parts are elegantly rounded. PLATE XXI.* Fig. 1. Cypris Valdensis. (C. Faba?, Min. Conch. t. 485.—See the observations on the specific names; supra, p.177.) Oblong-ovate, convex, punctated; front slightly concave; at one ex- tremity of each valve is a small oval lobe; back hollow between the valves. It is very doubtful whether this be the Cypris Faba of Desmarest+, which is the inhabitant of a much newer fresh- water formation than the Wealden, and appears from the figure to be of a somewhat different form. When the figure in the Min. Conch. above referred to, was published, the author was not aware of there being more than one fossil species of Cypris, and supposed that the minute differences * Plates XIX. and XX, containing representations of Endogenites erosa, are described above, p. 172—176.: see also hereafter, p. 349. + Bull. de la Soc. Philom. 1818, p.259. P1.1V. No. 8.; Hist. Nat. des Crustacés Foss, p. 141. Pl. XI. fig. 8. App. A.] Dr. Fitton on the Strata below the Chalk. 345 which he himself had observed, might have escaped the notice of Desmarest’s draughtsman ; nor has he yet seen specimens from either of the localities given by that author. Besides the fossil species of Cypris engraved in this plate, we are now acquainted with five others; one in the freshwater formation at Hordwell, (see Lyell in Geol. Trans. vol. iii. p. 288.); one in the coal of Newcastle, (Cypris arcuata, Bean MSS.); and three found among tertiary marine shells of a modern period, in the island of Java;—though the last possibly may belong to the Cytherina of Miller, a genus so near to Cypris, that it may not be distinguishable in the fossil state, and the living species of which inhabit the sea. Fig. 2. Cypris tuberculata, Discovered by the Rev. G. E. Smith at Seabrook near Hythe. Oblong-ovate, convex ; with a narrow border to the margin, and from three to twelve tubercles upon the surface. The defined tubercles, and a distinct margin distinguish this species from C. Faba; it is also rather broader and flatter; but the general form and the number of the tuber- cles are variable, as well as the division across the middle of each valve, which in some speci- mens, as at letter a., is so remarkable, as to indicate a distinct species, or even genus. More perfect specimens, however, shown at 6. and c. are quite free from this division; and interme- diate forms have been observed. The specimen represented in the upper figure at a.is from Swanage Bay; all the others are from the vicinity of Hythe. Fig. 3. Cypris spimigera. Discovered by Mr. Lonsdale in the Weald-clay of the Isle of Wight. Oblong-ovate, broadest at one end, punctated ; furnished with a single, short, conical spine on each valve; by which, and a shorter form, it is distinguished from the other species. It has a narrow lobe at one end of each valve of the same kind asin C.Faba. The specimens a, are from Sandown Bay; 0b. from Atherfield. Fig. 4. Cypris granulosa. Oblong-ovate, punctated ; with prominent granules upon its sur- face ; the lobe at one end observable in C. Faba is wanting in this species. Fig. 5. Corbula alata. A rather gibbose, smooth shell, with the posterior side produced and truncated. Fig.6. Psammobia? Tellinoides. (Psammobia, Mantell, Geol. S.E. of England, 251.) Shell ’ transversely oblong-ovate ; nearly flat, with conspicuous lines of growth. There are a few longi- tudinal furrows upon the posterior side. Fig. 7. Cyclas parva. Rather thick, smooth, obovate, approaching lenticular ; longer than Cyclas media. The larger figure, under letter a., is magnified. The shell is found in great pro- fusion in the Vale of Wardour. In the specimen represented at b., from Dallard’s Farm, (supra, p- 259, and also from pits at Dashlet,) the shells are filled with the crusts of a small smooth Cypris. Fig. 8. Cyclas subquadrata. Transversely oblong, with straight sides; strongly marked with lines of growth ; flat (perhaps from pressure). Found,at St. Leonard’s, Sussex. Fig. 9. Cyclas elongata. Transversely elongated, convex, nearly smooth; posterior ex- tremity more or less obliquely truncated : the casts of the outside show that the surface is finely striated concentrically. There are two species of Cyclas in the specimen of slaty clay repre- sented in the upper figure, a., which was found at Etchingham near Robertsbridge in Sussex. The same forms occur also in the ferruginous sandstone of Langton Green, near Tunbridge Wells, with Unio, (see below Pl. XXI. fig. 16.); and ina bed of clay at the top of the cliffs on the west of St. Leonard’s. It is probable that the rounder species is Cyclas parva. Fig. 9. 6. is a variety of C. elongata, from Hollington near Hastings. Fig.10. Cyclas media. (Min. Conch. t. 527. fig. 2.) Alarge specimen; with another showing the hinge and its single tooth under the beak. Transversely obovate, depressed, thick, smooth ; anterior side small; posterior rather pointed. 2y 2 346 Dr. Fitton on the Strata below the Chalk. [ App. A. Fig.11. Cyclas media: var. Gibbose; posterior side rather cuneiform and truncated. It has the appearance of being a little distorted by age. Fig.12. Cyclas angulata. 'Transversely ovate, convex ; posterior side truncated, and sepa- rated by anangle and a point. A wider, thinner, more transverse, and larger shell than C. media. Fig. 13. Cyclas major. (Cyrena, “larger species,” Ann. of Phil. N.S. vol. vili. p. 376, et passim.) A convex, smooth shell :—the specimens are generally so imperfect, that their size is almost the only character to be observed. Fig. 14. Unio Mantellii. Dorsal and ventral margins nearly parallel, straight; valves flat- tened, twice as wide as they are long; anterior side small, rounded. Fig. 15. Unio subtruncatus. Ovate; valves flattish, thick, with obtuse edges: the posterior extremity obliquely wedge-shaped. Fig. 16. Unio Gualterii. Nearly square, with the anterior side rounded ; depressed; marked with twice bent parallel rugz ; posterior side somewhat eared. The only fossil species known that shows to any extent the waved ruge so frequent in the recent species of this genus. The depression in the middle is not constant. Fig. 17. Unio Martini. Ovate, rather convex, nearly smooth, posterior side pointed ; um- bones not far from the middle, not prominent. Fig. 18. Mytilus Lyellu. Oblong-ovate, somewhat flattened, especially towards the front; convex towards the pointed beaks. PLATE XXII. Fig.1. Exogyra bulla. Oblong, convex, nearly smooth; beaks short, curved. The laterally curved beak distinguishes this shell from the Ostreze of the same beds. Its shape, however, is _ very variable. Fig. 2. Ostrea distorta. (‘‘Ostrea; an undescribed species”, Ann. of Phil. N.S. vol. viii. p. 376.) Elongated, narrow towards the hinge; one valve flat, both nearly smooth. This and the Exogyra, fig. 1. occur in masses, so closely grouped, that the form of the shells can seldom be traced. Fig. 3. Bulla Mantelliana. (Bulla, Mantell, Geol. S.E. of England, 249.) A smooth cylin- drical shell, nearly twice as long as wide, truncated at both ends: here accompanied by a small Pa- ludina, supposed to be P. elongata, but which has a smaller spire than that shell generally has. Fig. 4. Melanopsis? tricarinata. (Melania tricarinata, Amn. of Phil. N.S. vol. viii. p. 376.) Subulate, conical; whorls seven, carinated. Three carinze occupy the exposed portions of the whorls, and are crossed by distinct lines of growth; the central one is the most prominent. More perfect specimens have induced me to remove this from the genus Melania to Melanopsis. Fig. 5. Melanopsis? attenuata. Subulate, elongated ; whorls about nine; with several carine crossed by undulations, strongest at the upper part of each whorl. The length is in proportion greater, and the whorls more numerous than in the last species, fig. 4. Fig.6. Paludina Sussexiensis. Spire an elongated cone, with nearly straight sides; whorls five, smooth, more numerous than in either P. fluviorum, lenta, or carinifera of Min. Conch. There are, probably, several other species of Paludina in the Wealden strata. Fig.7. Neritina Fitton. (Mantell, Geol. S.E. of England, p. 248.) Convex ; tricarinated; aperture large; spire very small. The specimens do not show the aperture, and are hardly suf- ficient to prove this shell to be a Neritina rather than a Nerita. The lowest figure is magnified. Fig. 8. Tornatella Popii. Elliptical, pointed, smooth; spire small, of about three whorls. The cast shows two plaits upon the columella. Named from the Rev. W. L. Pope, of Tonbridge Wells. ~- App. A. | Dr. Frrron on the Strata below the Chalk. 347 Fig. 12. Lucina Portlandica. Orbicular, compressed ; surface finely striated concentrically. Very like ZLucina concentrica, (Annales du Mus, tome vii. p. 238, and tome xii. Pl. XLII, fig. 4. a. b.), but much more neatly striated ; as shown by the cast of the outer surface, represented in the lower figure, which is from the Isle of Portland. The upper figure is from Swindon. Fig. 13. Cytherea rugosa. Subtriangular; posterior extremity and beaks pointed ; valves very convex near the beaks; outer surface concentrically furrowed, furrows most numerous on one side. Fig. 14. T'rigonia incurva. (T. incurva, Benett, Wiltsh. Fossils, tab. xviii. fig. 2.) Convex, flat- tened posteriorly, transversely much elongated; surface tuberculated ; width more than twice the length. Since this Plate was finished, I have seen specimens from Brill, retaining the shell, which is tuberculated, as in 7’. clavellata, but the tubercles are smaller. PLATE XXIII. Fig. 1. Ostrea falcata. Elongated, curved towards the posterior side; one valve flat, thick ; the other unknown. Fig. 2. Nerita angulata. (Nerita, 2nd species ; Benett’s Catalogue, p. 4.) Subglobose? ; with a single carina; spire rather small, obtuse; aperture oblong. This cast shows the muscular im- pression very distinctly. Fig. 3. Natica elegans. Ovato-rhomboidal, smooth; spire small, pointed; whorls four or five, rather angular, their uppermost edges rounded ; aperture more than two thirds of the length. The shell in this specimen, whose form is well preserved in silex, is very thin and smooth. Fig. 4. Buccinum naticoide. (Ampullaria elongata, Benett’s Catalogue, p. 2.) Ovate, smooth, thick; spire produced ; whorls four or five, their upper edges rounded, the last whorl ventricose ; aperture ovate, two thirds the length of the shell; spire longer than in the last species; shell very thick. Fig. 5. Buccinum? angulatum. Fusiform, short; sides of the spire straight; the last whorl has one keel in the middle; aperture rhomboidal, with a short rounded beak. In the produced beak, this specimen approaches to the genus Fusus, but the canal appears to be too broad. The external form has not been seen. ; Fig. 6. Terebra Portlandica. (Turritella, Smith, Strat. Ident. Portland-plate, fig. 2.) Tur- rited, longitudinally striated ; whorls rather concave near the upper edge, where they have also longitudinal furrows; aperture acutely elliptical; beak very short, curved. A very common species in the Portland stone; where, however, the form of the aperture is rarely seen. Here, it is preserved in chalcedony. Fig. 7. Serpula variabilis. A cylindrical, rugose shell; with a considerable portion of the tube unattached, and an irregular suture on one or more sides. When young, the attached por- tion is triangular. . ‘Fig. 8. Serpula triserrata*. A thick, externally triangular, attached tube; with three thin, serrated keels upon the upper angle. Attached to a portion of Ostrea deltoidea. Fig. 9. Mya depressa, var. Oval, compressed, smooth, twice as wide as itis long. A much wider specimen than that figured in Min. Conch. t.418. Intermediate forms are also met with. Fig. 10. Exogyra Virgula; Goldfuss, tab. lxxxvi. fig. 3. (Gryphea Virgula, Defrance.) Much elongated, arched; one valve convex, the other concave or flat; convex valve marked with ele- vated lines; by which the species is well distinguished. * This specific name is substituted for “ tricristata,” given to fig. 8, at p. 231; the latter having been appropriated by Goldfuss to a different species, from the lias near Bantz.—(See Goldfuss, p. 226. tab. Ixvii. fig. 6.) 348 Dr. Firron on the Strata below the Chalk. [App. A. Fig. 11. Trigonellites latus Parkinson*. (—Ichthyosiagones problematicus, Dr. Riippell+; A ptychus levis, Von Meyer}.) Oblong, triangular, compressed; one edge and one angle rounded ; the longest edge flattened; one surface concave, striated; the other nearly flat, smooth, but marked with numerous minute circular pits ; tissue cellular. I have just learnt from a specimen lent by Mr. Bean, that fig. 18. in Pl. V. of Phillips’s Geology of Yorkshire, is a species like this. It is referred by Mr. Phillips to the Oxford clay; but Mr. Bean observes that he has had the same fossil from the Kimmeridge clay of Shotover Hill. A larger species is found at Scarborough, perhaps the same as that before us. (supra, pp. 273, 292, and 316.) Dr. Fitton, by whom the specimens here represented were found, in clay, near Whitchurch in Buckinghamshire, and at Southrey between Cambridge and Ely, (supra, pp. 273, 292, and 316,) remarks: “ When I found this fossil in 1827, I was unacquainted with the publications then “ relating to it, and those of Dr. Rippell and Mr. Von Meyer had not appeared ;—but so far as “TI can recollect, there was nothing in the circumstances attending these remains that could illus- “ trate their origin and connexions. Along with them I found in Buckinghamshire Gryphea Vir- “* gula, but no Ammonites: in Cambridgeshire, Ammonites Lamberti is mentioned as occurring “at the same place (p.316.). The valves of the fossil, like those of the Gryphza, at both places “Jay in the clay which contained them, as detached shells might be expected to do, if they had “ been lodged confusedly in soft mud. Smaller and thinner valves, perhaps of a different species, “‘ accompanied the larger specimens at Whitchurch, Bucks.” “Of the many names given to this fossil, I have, after some hesitation, retained that of T’ri- “* gonellites, which indicates no more than form; the relations of these singular bodies being still “obscure. As the valves are very often found detached, the term may be used provisionally, or “‘ even ultimately remain, as a convenient denomination; in the same manner as Belemnites con- ** tinues to be employed, although the bodies to which that appellation is given, are no more than ‘* subordinate portions of some complex structure.” “If the fossils represented in Plate XXIII. be truly of the same species with those of Solen- ‘‘hofen, their identity is deserving of notice, geologically.” Fig. 12. Nerinea Goodhallu. Turrited, smooth; whorls numerous, half as long as they are wide, concave. There are three plaits in the interior, one upon the columella, one opposite to it, and one above it within the whorl; aperture rhomboidal. The section represented in the left hand figure shows the generic character. The same species but much larger, is found in the Bou- * “ Organic Remains &c.,” vol. iii. Plate XIII. fig. 9. and 12. + Abbildung und beschreibung einiger neuen oder menig gekannten Verstemnerung, aus den Kalkschiefer Formation von Solenhofon: von Dr. Ed. Rippell,—4to, Frankfurt, 1829. Since this sheet has been at the press, (July 1836,) a short paper by Dr. Riippell has appeared in the Lon- don and Edinburgh Philosophical Magazine, (July 1836, vol. ix. p. 32, &c.), to which I wish to refer the reader. Dr. Riippell regards the two species of Parkinson’s Trigonellites, as belonging to distinct genera: in one of which (7. lamellosus, P.) he supposes the valves to have formed the opercula of an animal somewhat resembling an Ammonite, but destitute of septa: this he proposes to denominate Pseudammonites. For the second genus, (to which the specimens represented in Plate XXIII. appear to belong,) Dr. Riippell retains the name of Jchthyosiagones, originally used by Bourdet ; and in this case the valves appear to have been internal shells, in large elliptic mus- cular masses, the structure of which has not yet been brought to light. Subsequently to the pub- lication of Dr. Riippell’s first memoir, Mr. Von Meyer, in a paper referred to below', proposed a different view of the relations of these bodies; and gave the name of Aptychus to a genus compre- hending all the different forms. ' Acta Acad. Leop. Carol. Nat. Cur. vol. xv. Part Il. Read October, 1829; pp. 68—125. tab. Iviii. fig. 1, 2, 4. App. A*.] Dr. Firron on the Strata below the Chalk. 349 lonnois ; where also other smaller species of this genus occur. This species is named after the late Mr. Goodhall, F.G.S., an indefatigable collector of fossils, and remarkably liberal in affording the use of them to inquirers. The Wood-cut at p. 129. represents a portion of Nautilus plicatus, one third of the original size. The parallel linear furrows which pass over the whorls, are bent three times at acute angles, once on each side and once in the middle, the central angle being directed backwards. There is often some irregularity in the junction of the lines at the angles. APP. A. FIGURES OF VEGETABLE REMAINS. Sphenopteris gracilis—The wood-cut at p.181 represents the impression of a species of fern, discovered in the Hastings-sands, near Tonbridge Wells, by the Rev. W. L. Pope of that place. It has been referred to the genus Sphenopteris of Adolphe Brongniart*, notwithstanding its acu- minate pinnule, and a certain degree of resemblance to Odontopteris minor, (Brongn. Veg. Foss. Pl. Ixxvii.), on the ground of its apparent affinity to Sphenopteris Mantelli (1bid., p. 170. Pl. xlv. fig. 3—7); its pinnule having a midrib, but no lateral veins. This specimen was accompanied by the impression of a species very nearly allied to, and perhaps no more than a variety of, Sphenopteris Mantelli. PLATES XIX. anp XX. Endogenites erosa.—The description of the plates representing the external form and internal structure of this singular fossil will be found above; (85.) to (89.), p- 172,176. After those pages had been printed, two remarkable varieties of the form were discovered, in cutting down the cliffs near the White Rock at Hastings; in which the stony nucleus was not only very irregular in figure, but apparently divided into flat lobes, disjoined, or scarcely connected by very thin flakes of stony matter; the whole being externally coated with lignite, which occupied the en- tire thickness of the fossil in the intervals between the lobes. The form and mode of connexion, or apposition, of these stony nuclei, when divested of their covering, were such as to suggest a com- parison with some varieties of Cactus. PLATE XXII. All that is known of the Cones and cone-shaped body, Figures 9, 10, and 11, of this plate, is mentioned in the list of fossils, at pages 181, 230, and 290. A section of that represented in fig. 11. on its longer diameter, did not exhibit any indication of vegetable structure: but the ge- neral resemblance in the outline and aspect of this specimen to part of the reduced figure of Zamia horrida given in Dr. Buckland’s plate, (Geol. Trans. 2nd Series, vol. ii. Pl. xlviii. fig. 4.) is, perhaps, deserving of notice. A Cone has recently been found on the shore of the Isle of Portland, not improbably derived from one of the beds of clay, or “ Dirt”, subordinate to the lower part of the Portland strata, the structure of which, according to Mr. Brown, approaches in some respects to that of Arau- caria. Iam indebted to the kindness of the Rey. David Williams, of Cross, near Bleadon in So- mersetshire, to whom it belongs, for an opportunity of submitting this beautiful specimen to the examination of Mr. Brown, who will, I hope, describe its structure in the Transactions of the Linnzan Society. * Prodrome, &c., p. 50.—Hist. des Vég. 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LIST OF HEIGHTS.* Tue following list may be useful to those who examine the country described in the preceding paper, by furnishing some points of known elevation, from which it will be more easy to estimate the surrounding altitudes, than if the entire heights above the sea were to be conjectured. The height of the tides upon the English coast is influenced by so many variable circum- stances, that in selecting a zero for a list of heights, some permanent natural or artificial mark, of easy access, is very much to be preferred to the level of the sea, either at high or at low water; the latter, especially, being objectionable, from the greater difficulty of ascertaining it, and from its being frequently concealed. On this point, I am supported by the opinion of Mr. Lubbock, whose publications on Tides give great weight to his authority. In the subjoined lists, therefore, I should have adopted, as the common point of reference, one of the standard marks hereafter mentioned, had not the heights obtained during the Ordnance Survey, and some others mentioned below, been all referred to the level of the sea at low water; while, as the mode in which that point was determined is unknown to me, I have thought it best not to make any change in the original measures, by conjectural reduction. The Tide-marks on the Thames, in London and its vicinity, which are referred to in legal pro- ceedings, and which form the base line, or “ datum”, of many of the railroad sections, have been derived from a long series of observations on the depth of water, first made, I believe, at the East India Docks, by Capt. Huddart, and subsequently at the London Docks; from which latter place, marks, corresponding to the average spring tide high-water mark, have been transferred by levelling, to most of the bridges, and to the lock on the Thames, at Teddington above Richmond, which is, at present, the farthest range of the tide. The time of high water varies a little, at different points along this interval, but the ultimate heights are supposed to be the same throughout. In the year 1830, Mr. Lloyd having fixed a standard mark at the Sheerness dockyards, found the mean rise and fall of the spring tides at that place to be 17°6150 feet; and of neap tides * The exact determination of heights is, by geologists, regarded as of small importance ; but the judgment upon this subject is, perhaps, unconsciously influenced by the difficulty which attends it; since if we could measure heights as easily as horizontal distances, it cannot be doubted that the former would be recorded and reasoned upon more frequently. As geology advances, it becomes more and more necessary that none of the elements which enter into the physical history of the globe should be neglected; and it is probable that many important inferences, not at present foreseen, might result from a correct acquaintance with the levels throughout large portions of the earth’s surface. Already it has been ascertained in Sweden, that the land has been gradually raised within a few years, by a small but very perceptible quantity ; and in all countries, especially those subject to earthquakes, it is a point of great interest to determine whether the relative levels of the sea and land, are truly as permanent as they are supposed to be. In the Survey now in progress in Ireland, and in the operations for a new map of France, the heights are carefully ascertained and inserted on the maps: perhaps it may still be hoped, that some general system will be adopted for connecting the measurement of heights in England with the Ordnance Survey. In the mean time it is satisfactory to find that at the late meeting of the British Association for the Advancement of Science, (August, 1836), a committee was appointed, and a portion of the funds placed at their disposal, (small, it is true, with reference to the object), for the purpose of devising and conducting observations on the relative level of the land and sea upon our coasts» 3 Ba 370 Dr. Firron on the Strata below the Chalk. (App. C. 11:320 feet ; his mark (called the “ North Standard”), being 4°0661 feet above the mean level of high water, and 21-6811 feet above that of low water at spring tides, He then ascertained by very careful levelling, the heights above the standard, of several points in the vicinity of the Thames, between Sheerness and London*: whence it appears that what is called the “ Trinity TRINITY H.W. 1800. A ‘* high-water mark,” at the London Docks, ( answering to XXIII. of the indices ‘“‘ marked on the south-west side of the entrance”,) is 2°0112 feet below his “ North standard,” and consequently 19°6699 feet above low-water mark at Sheerness. The last-mentioned quan- tity, therefore, must be added to the height of any station above the Trinity mark, at the London Docks, in order to obtain the height of the same station above the sea at low-water at Sheerness. The places in the South-East of England mentioned in the subjoined lists, are grouped in the order of the counties referred to in the preceding pages, beginning on the north. The names are disposed alphabetically. The heights are expressed in feet and decimals of a foot. The au- thorities and references to them are the following : 1. “ O.”—An alphabetical list of all the heights ascertained during the progress of the Ord- nance Survey, given in the official account of that operation, published in 18111, calculated from the level of the sea at low water. The places of the stations are mentioned in the Phil. Trans. for 1800, pp. 576 to 583; and in the “ Account,” above mentioned, pp. 70 to 81. 2. “C.”—Bradshaw’s maps of the canals and navigable rivers in the midland counties of En- gland, in three parts. The heights are taken from low water at Liverpool, (at a point 6 feet 10 inches below the sill of the Old Dock); which point is stated to be 21 feet below the Trinity House high-water mark at the London Docks, and consequently 1°331 feet beneath low-water mark, mean spring tides, at Sheerness, according to Mr. Lloyd. 8. “ M.”—A manuscript list of heights, principally in Cambridgeshire, ascertained by Mr. M‘Lauchlan, of the Ordnance Survey, and Mr. Glaisher of Cambridge, and for which I am indebted to the former gentleman. In this list (which is not an official document,) the heights are counted from the level of the sea at low water, in Lynn Deeps. 4. “ B.”—A MS. list of heights above the sea at low water, ascertained by the late Mr. Bevan of Leighton, for which I am indebted to his son, Mr. Bevan of Wellingborough, and to Mr. Mat- thews of Leighton. 5. “ W.”—A short list of heights in the Isle of Wight, subjoined to Mr. Webster’s letter to Sir H. Englefield. These are chiefly barometrical, and from their being connected with some of the mea- surements of the Ordnance survey, it is probable that the zero was low-water mark. * Phil. Trans. 1831; p. 167 et seg. Mr. Lloyd (p. 190,) “ concluded his levellings at a “standard mark at the landing-place on the north-east side of the New London Bridge;” which “ mark was 2°3967 feet below the North Standard mark at Sheerness;” and conse- quently 0°3855 foot, (= 4°626 inches), below the Trinity mark at the London Docks. The mark here referred to is a flat piece of brass, let into a cavity in one of the two large flags or slabs of granite, which form the landing-place at the bottom of the second flight of steps, de- scending from the footway on the north-east side of the bridge. The upper flight consists of 29 steps ; the second, at the foot of which is the mark, of 26 ; the lowest flight is commonly more or less concealed by the water. The cavity in which the mark is lodged, is about 3 inches square, with rounded angles; and is two feet from the eastern wall or side of the bridge, and 2 feet 8 inches from the southern edge of the stone. The surface of the brass is about half an inch beneath that of the stone, which is itself a few inches below the level of the water at high spring tides. + “An account of the Trigonometrical Survey, &c. 1800, to 1809; by Lieut.-Col. Mudge, and ‘Capt. (now Lieut.-Col.) Thomas Colby, R.E.”; 4to, 1811, vol. i. p. 299—311. This work refers to the previous publications in the Phil. Trans. for 1795, 1797, 1800, and 1803, and carries on the account of the operations to the end of 1811. App. C. | Dr. Firron on the Strata below the Chalk. 371 6. “ F,”—A small number of heights upon the coast of Kent and Sussex ascertained by myself, from observations with excellent barometers and thermometers by the late Mr. Carey. The lower station in these observations was‘either the shore itself, (the height of the barometer, below or above the spring-tide high or low water marks, being estimated),—or the drawing-room floors of the houses at Sandgate and Hastings, in which I resided, the height of which above the sea was ascertained by a mean of several observations, sometimes checked by comparison with more elevated stations measured directly from the shore, and again from the houses. The variation of the tides at Sandgate was assumed to be the same as at Dover, = 18°30 feet, and at Hastings, = 21°50 feet; which Capt. Beaufort, by whom I have been favoured with these numbers, states to be respectively the mean derived from a series of observations at those places, in 1834 and 1835. Above the sea Stations. at Low Water. Norrouk. Yee Denver Sluice, near Downham Market, above the Deeps at Lymn ,...scssseceeseee CAMBRIDGESHIRE. Aldreth station, between Haddenham Mills and Aldreth..........0000. Revccscesccarssers O.| 122 Ps GIShAMOVA.| StAUOM 12 0 8 5 Breadth of each ramus of the sternum at the narrowest part 1 7 ty) Length from the central union of the bones of the sternum to the posterior margin of the dorsal shell............ 10 5 6 Length of the tail beyond the margin of the shell ........ 12 0 6 5 From a comparison of these details, we find that, taking the dimensions of the dorsal shell as the standard, the following proportional differences exist between the fossil and recent species. The expansion of the upper shell in the fossil is greatest at some distance posterior to its union with the branches of the sternum ; that of the recent is widest at the union. The breadth of the lateral branches or rami of the sternum, in the former, is not less than one eighth of the whole breadth of the sternum ; in the latter it is not more than one seventeenth. These differences, with the much greater comparative length of the tail in the fossil species, warrant me in considering it as a distinct species, to which I propose to give the name Chelydra Murchisonit, after the distinguished president of this Society, to whose kind interference I owe my possession of it. To his pen I leave the detail of every particular relative to the geological situation of the specimen *, but I think it may not be uninter- esting to state a few facts illustrative of the habitat and manners of the recent species, especially as the organization of the two species is so similar as to preclude the possibility of any considerable difference in their habits. The Chelydra serpentina is strictly and exclusively an American form. There is no approach to it in any species inhabiting the Old World. It is found in the southern states of North America, where it is known by the name of the snapping turtle. It has also been termed the alligator tortoise, * Geological Transactions, Second Series, vol. iil. p. 281. “Mr. Bett on a fossil Species of Chelydra. 381 an appellation which it has derived from its general form, especially the deeply carinated tail, as well as from its predatory habits. It is strictly a freshwater form, and is highly carnivorous, seizing its living prey with great avidity, and with a sudden snapping movement; to which circumstance it owes its common name. Its food consists of young water-fowl, fish, and aquatic reptiles ; and the length of the neck, the strength of the jaws, and the robust and sharp claws with which the feet are armed, are admirably adapted for seizing and tearing its prey. I have observed in several speci- mens which I have kept living, that when teazed they will remain for a time motionless, the head withdrawn underneath the shell, until, at a convenient moment, the head is thrown forwards by an instantaneous extension of the neck, and the object of its attack seized by a sharp sudden snap of the jaws. I have seen a stick nearly as large as the little finger snapped in two by this sudden movement. It frequently wanders to a considerable distance from the lakes in which it habitually resides, and is said to hybernate either in mud or in the ground near the water. A specimen which I possessed last year repeatedly endea- voured to dig a retreat for itself in soft earth, which it removed by its fore feet with great rapidity, entirely concealing itself in the space of a few minutes. The whole of the freshwater forms are strikingly contrasted with those of the terrestrial group, in the ease and rapidity of their movements, and in their carnivorous habits, for the enjoyment of which these qualities are essentially required; and the group to which the present genus belongs may be con- sidered as possessing those powers and habits in the greatest degree, with the exception, perhaps, of the family of the Trionychide, which, however, if they exceed the former in the quickness of their motions, must yield to them in strength. 3D2 EMER hoy res. olidtbit sagt ny ile and, 40: sisiher Aen ee og py! Marya My Tela OVE ae eet a tha i diya a(s wii Ce ee ovlibons Veta a; fee on ir> bietal Ns ayinariaend rr wie all | | (‘hee weit, ag vile y a, nt | eS mitre Ped oat nial POH) bey, ove | CAE ceo eyed Te t ’ Skt Gael’ aed iy ase PANE, bhi eee PN Sg Sa byt. hie ul in Ml nih vet repay wy EME va Heo eo A a ELE TT " | | :. det a nein etre al /ivaae Chiag yee f heal i Li.) ih tee, 4. 4 A fa , HO pk A Teg wuld ¥og, vith al be! nt dial) a tip). « 9 a did a Vie ints ‘onan dual Tins etme Fl ’ Pig} MiPMee Ae ae Level ’ | gig 0h Moa. adele pt natal Tala 2a Wy Reais, UL ited gupta vt . Pet! ok elem aly haasne 1 sy i= tt) Lone Bena va ed, Fy, mat wey it (ah bhai Saati HN lone Mees eA Ty Ue a ee i ow ia iat ohh i eee ol ie a Say ns fi ’ hi aie ha f L et Aa aaa my ay Toa . Cs, ” willy : bs i. / Ree ” ax’ 7 + iy i : ‘ k % il VI.—On the new Red Sandstone Series in the Basin of the Eden, and north-western Coasts of Cumberland and Lancashire. By tue Rev. ADAM SEDGWICK, F.R.S. V.P.G:S. &c. (WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. ) [Read February 1, 1832.] Introduction. IN two papers read before the Geological Society during the Sessions of the past year*, 1 endeavoured to describe the phenomena exhibited along the line where the carboniferous chain of Yorkshire and Westmoreland strikes against the old slate rocks of the Cumbrian mountains. ‘Taking up the sub- ject where it had been left by Mr. Phillips}, a series of enormous faults and dislocations were traced, nearly along this line of junction, to the foot of Stainmoor; and it was shown that mountain masses of rock, torn off from the carboniferous series, were thrown down with a reversed dip into the higher part of the valley of the Eden, near Kirkby Stephen; and that after many breaks and contortions, they gradually gained a more regular strike and dip, and were prolonged into a chain, forming the northern outskirt of the primary Cumbrian system, and terminating at Egremont. It was at the same time shown that another fault, ranging under the escarpment of the Cross Fell chain, produced a corresponding effect on that part of the carboniferous series ; and that both these great disruptions took place at a period anterior to a portion of the conglomerates of the new red sandstone}. In this paper I purpose to give a sketch of the new red sandstone series, which spreads from both banks of the Eden to the base of the neighbouring mountains, and afterwards skirts the coasts of Cumberland and Low Furness. In performing this task I shall endeavour to describe in order, Ist, The geographical distribution of the red sandstone series, and the features of the country through which it ranges ; 2ndly, Two or three masses of older rock, which appear within the limits of the red sandstone ; * Geological Transactions, Second Series, vol. iv. pp. 47, 69. + Geological Transactions, Second Series, vol. iii. p. 1. + See Plate XXV. fig. 2. 384 Prof. Sepawick on the New Red Sandstone Series in the 3rdly, The successive deposits entering into the red sandstone series, with a view to their comparison with the corresponding groups in Yorkshire and Durham ; : Athly, By way of conclusion, I shall endeavour to give a general compa- rison of the red sandstone series of Scotland and England, in the hopes of thereby establishing some general subdivisions, by help of which the several groups may be brought into at least an approximate comparison with each other. The details of this, and of the two other papers, will nearly define the geo- graphical limits of the primary Cumbrian mountains, a general description of which I hope in a short time to lay before the Society. § 1. Geographical distribution of the Red Sandstone Series, &c. Between the chain of Cross Fell and the primary Cumbrian mountains the red sandstone series fills a triangular area, the vertex of which may be placed in one of the tributaries of the river Iden, not far from Brough, and its base on the frontier of Dumfriesshire and the Solway Firth. Respecting the range of the north-eastern side of this triangular area, I have few details to offer which are worth recording ; but I may state in general terms, that if the vertex be placed on the banks of the Belah (above the bridge on the road from Brough to Kirkby Stephen), the bowndary line may thence be drawn, by Brough Castle and the north-eastern side of Brough Hill, to the foot of the carboni- ferous chain a little above Helton ; and that in the remaining part of its course to the frontier of Scotland, it continues to skirt the chain very nearly, as is represented in Mr. Greenough’s map*. * During the summer of 1834 I examined a part of the Cross Fell chain with Mr. Bowstead, of Corpus Christi College, Cambridge ; and from our joint observations, as well as from information he has had the kindness to communicate, I may add the following account of the north-eastern demar- cation of the new red sandstone. After skirting the north-eastern side of Brough Hill, it ranges nearly in the direction of Burton; and the rock is seen, in the form of a highly calcareous conglo- merate, in Walk Mill Beck. Thence the line ranges above Burton; and skirting the hills at a con- siderable elevation, passes under the base of Roman Fell (which is composed of disturbed beds of old red sandstone), and is prolonged a little above Helton, and just above Murton. Beyond the last- named village the line has, for a few miles, a more westerly range, so as to pass considerably below Keisley ; after which it is, by amore northerly course, brought a little above the village of Dufton, from which it may be traced across Swindale Beck, near the village of Knock. From this place the line (still skirting the hills at a considerable elevation, though the beds of red sandstone are nearly horizontal) may be traced above Milburne, Ouseby, and Melmerby; through Raven Beck, a little above Renwick; and just above Croglin, from which place it is prolonged near the base of the great carboniferous escarpment, as may be seen in numerous sections where the rocks are laid bare Basin of the Eden ana north-western Coasts of Cumberland, &e. 885 The direction of the south-western boundary has been ascertained much more correctly, by observations carried on from one end of it to the other. Its minute description is, however, thrown into an appendix, being necessarily made up of details, which, though tiresome and uninstructive if read before the Society, may assist in the completion of our geological maps, and be of some value as matters of reference. Such facts only will be mentioned here, as throw light on the structure of the red sandstone, and help to establish its subdivisions. Where the red sandstone series first appears in the ramifications of the Eden, near Brough and Kirkby Stephen, it is chiefly seen as a conglomerate, abounding in fragments of mountain limestone, and cannot, when it has that form, be mineralogically distinguished from the overlying conglomerates on the skirts of the Mendip Hills. It is generally in a state of complete indu- ration where the calcareous fragments abound ; and it sometimes passes into mere brecciated beds of liméstone: but other parts, especially where the peb- bles are rounded, and the sand and cement abundant, are soft and crumbling. In the arrangement of the several varieties of the formations, though the beds are nearly horizontal, there is very little approach to symmetry or order. Hence the conglomerates offer a very unequal resistance to the action of the elements ; and above Kirkby Stephen, where the Eden makes its way through them, they have been worn into channels of extraordinary complexity. Chasms and deep basins are naturally scooped out where the rock offers the least re- sistance ; and by these inequalities great eddies are formed in the river during every mountain flood, which by whirling round the hard pebbles at the bottom of each basin, gradually grind away the solid rock, and carry on the work of excavation far below the surface. Caverns are thus formed; and masses of conglomerate become so far undermined, as sometimes to allow a new passage to the river far below the level where it once flowed. A fine example of this kind occurs at Stenkreth Bridge near Kirkby Stephen, where the waters, after washing the inclined strata of mountain limestone be- low Pendragon Castle, plunge among the horizontal masses of conglomerate ; after which, for a short space, they are heard roaring in a subterranean chan- nel, communicating by a narrow cleft (called the span of the Eden) with what by mountain torrents. Further towards the north the calcareous chain declines in elevation, and the demarcation of the new red sandstone is often ill defined. The best approximation to its course that has yet heen published, may be seen in Mr. Greenough’s map. It passes (as there represented) to the east of Brampton, after which it ranges, in a sinuous line, very much concealed by alluvial detritus, but on the whole bearing nearly due north till it crosses the Liddel and enters Scotland ; then it is deflected nearly to the west, and crosses the Esk just above Canobie Bridge. 386 Prof. Sepewick on the New Red Sandstone Series in the appears to have been the ancient bed of the river. Within the memory of man this cleft might be spanned by the human hand; but it is now, by an act of wanton mutilation, despoiled of a portion of its honours, so that the projecting ledges of rock, at their nearest point of approach, are about two feet asunder. A little way below Kirkby Stephen the conglomerates are in a state of ex- treme induration, and rise in large flat beds, sometimes used for coarse flag- stones and coping-stones, a purpose to which the conglomerates of the new red sandstone are also applied in the neighbourhood of the Mendip Hills. The relations of the overlying series are extremely obscure for several miles below Brough and Kirkby Stephen, being much concealed by enormous masses of transported materials. ‘The new red sandstone is however seen, in several places, in the channel of the Eden, and the line of demarcation passes, on the whole, considerably to the south of its left bank*. In the rivulet which descends to Little Ormside, and at Burrels, to the south of Appleby, the conglo- merates are again exposed; and (though the sections are obscure) appear, from their position, to be at the base of the red sandstone seriest. Near Burrels they form a fine escarpment, parts of which contain large fragments of mountain limestone (sometimes rounded but generally angular) and are extensively burnt in the neighbouring kilns: other parts of the escarpment are of a finer structure, rise in thick flaggy beds, and are used for building. The imbedded pebbles and fragments of gritstone and limestone seem to be derived exclusively from the neighbouring carboniferous formations ; and are held together by a red, calcareo-ferruginous cement, more or less mixed with siliceous sand, and in a very variable state of induration. Subordinate to the cement (which does not, as in some parts of England, contain an excess of magnesia) are a few concretionary nodules of red oxide of iron. The range of the demarcation through the remaining part of Westmore- land, till it crosses the Eamont below Eamont bridge, presents no phenomena of much interest. It, however, deserves remark, that in this district, especially near Cliburn, the red sandstone is sufficiently hard and thin-bedded to be used * In this portion of the range, by far the greatest area of the red sandstone is expanded beyond the right bank of the Eden. Partly in consequence of the great fault above noticed, all the older formations, near the base of the Cross Fell chain, have a high angle of inclination, and must have once formed a deep trough for the reception of the newer deposits. As a natural result of this position, the red sandstone is often found abutting against the inclined strata close to the base of the chain; which throughout presents a steep escarpment towards the neighbouring plain. The south-western boundary of the red sandstone rests (on the contrary) on slightly inclined beds of the carboniferous series; and is, consequently, thrown off to a great distance from the primary central groups, and in one or two places approaches very near to the left bank of the Eden. t+ See Plate XXV. fig. 3. Basin of the Eden and north-western Coasts of Cumberland, &c. 387 for roofing-slate. In England sucha structure must be considered rare ; but in Dumfriesshire the new red sandstone not unusually rises in flagey beds which are, I believe, sometimes applied to a similar purpose. The further range, to the coast of Cumberland, is detailed in the Appendix (p. 405); and it is sufficient in this place to state, that the line of demarcation incloses Penrith Beacon, Thiefside Fell, and the great quarries of Highhead Castle ; and that, after skirting the Bolton coal field, it stretches in a direction nearly east and west, and runs into the sea on the south side of Maryport. Along this line there are no traces of conglomerates (like those above described) ; nor, in general, is there anything in the position of the red sandstone beds to prove that they are unconformable to the carboniferous beds on which they rest*. They make no regular escarpment, and there is moreover a difficulty in determining their exact limits, of which those who have only studied the types of our south-western coal fields can hardly form a just estimate. The gritstone beds of the carboniferous series are, here and there, of a deep red co- Jour, and cannot always be distinguished from the new red sandstone. More- over there seem to be, along some portions of this line, traces of a lower red sandstone, forming a connecting link between the true carboniferous rocks and the formation I am now describing f. Between the south-western boundary of the new red sandstone and the banks of the Eden, there’are many tracts of wild sterile land. For the rich gypseous marls, which give so much fertility to the great plain of central England, are there almost entirely wanting ; and the subsoil is composed of a barren sandstone, on the parallel, if I mistake not, of the forest sand of Not- tinghamshire. This sandstone has been exposed to great degradations since the time of its first deposit ; but by taking the height of Penrith Beacon, and adding to it the depth of the borings in search of coal, near its base, we have a proof that the portions of red sandstone, still remaining, are in some places of a very great aggregate thickness t. The great degradation of the red sandstone is proved, not only by the * The neighbourhood of Rosley seems an exception to this remark, for the coal strata are there much shattered, and in some places highly inclined, while the overlying formation of red sand- stone is nearly horizontal. + Among the dislocated and highly-inclined beds near Brough, the grits of the carboniferous series are generally iron-shot, and not unusually of a deep red colour. Rocks of a similar colour, but of more doubtful relations, occur near the line of the road between Penrith and Newton Raney; also in the same neighbourhood near Catterlem and Hutton. Again, a few miles west of Mary- _port, there are examples of a red grit (probably portions of the “lower red sandstone”) near the demarcation above noticed. t Ata place called Honey Pot, close to the banks of the Eamont, a little below Penrith, they VOL. V.—SECOND SERIES. 3) 101 388 Prof. Sepewick on the New Red Sandstone Series in the outline of the country, but also by the enormous masses of drifted materials by which it is accompanied. It is no part of my object to describe these materials in detail; but I may here remark, that mingled with them, and overlying them, are great bowlders of Shap granite, which have been drifted over the hills and plains skirting the Eden from Appleby to the foot of Stain- moor* ; that enormous masses of Carrock Fell syenite and other crystalline Cumbrian rocks have been drifted as far as the shores of the Solway Firth, where they are found mixed with other great bowlders, brought by opposite currents from the mountains of Dumfriesshire ; and lastly, that the red sand- stone is often buried, for miles together, under great heaps of the old alluvial detritus, which has modified all the external features of the region, and some- times produced a fertility little known where the undisturbed rock is near the surface. From the red cliffs of Maryport to St. Bees Head (a distance of thirteen or fourteen miles, estimated in a straight line), the whole coast is occupied by the coal measures, excepting one place a little north of Workington, and two or three places near Whitehaven, where we find an intermediate sandstone, form- ing, apparently, a connecting link between the true carboniferous and new red sandstone groups. The red sandstone of St. Bees Head appears to dip con- formably to the coal measures, from which it is separated, not only by the in- termediate sandstone before noticed, but also by thé magnesian limestone and conglomerate which strike across the headland to Ben How quarry +, where they are cut off by the valley of St. Bees, to the south of which the yellow limestone is no more seen in Cumberland. Notwithstanding the position of the beds at St. Bees Head, it is obvious that, when considered on a great scale, the formation is unconformable to the coal series; for the same beds, in their prolongation to Egremont, cross ob- liquely over the range of the mountain limestone, and the new red sandstone is expanded in irregular outliers far within the limits of the coal fieldf. Between Egremont and Gossforth, the formation appears to have undergone a movement of elevation ; for its beds dip at a considerable angle to the west, bored seventy-four fathoms in search of coal. It is said that they passed through only fifteen fathoms of red sandstone before they reached the coal measures. * It is well known that the bowlders of Shap granite have drifted over Stainmoor to the plains of Yorkshire, and even as far as the eastern coast. They have also been drifted to the western coast below Milnthorp in Westmoreland ; and they abound in the masses of gravel which are found near the tops of the high hills between Sedberg and Kendal. + See Plate XXV. fig. 4. { These outliers will be laid down on a map to accompany a subsequent memoir on the White- haven coal field. Basin of the Eden and north-western Coasts of Cumberland, &c. 389 and the demarcation ranges at a high elevation along the flanks of the neigh- bouring mountains*. To the south of Gossforth, all the low region border- ing on the coast is so much concealed by transported matter, that the red sand- stone is visible only in a very few places: it, however, comes to the surface, or has been reached by artificial excavations, in several places north of Bootle, where it appears to rest immediately on the granite+. Indeed, all the cliffs for eight or ten miles south of Ravenglass are composed of a coarse red gra- vel, looking like materials formed by the breaking up of the red sandstone, and probably resting on it,—a conclusion confirmed by the appearance, during low spring tides, of two reefs of red sandstone (Brandreth Scar and Codlin Rock) not far from the coast. Between Bootle and Duddon Mouth no red sandstone has been found zm situ, though the coarse red gravel extends several miles to the south of the former place. All the southern part of the promon- tory (with the exception of Hodbarrow Point, where there isa patch of moun- tain limestone), is, however, composed of marsh land or of drift sandt. To the south of the Duddon estuary, the red sandstone again appears in great force, overlying the carboniferous series ; and though buried in many places under enormous mounds of diluvial gravel, there can be no doubt that it forms the subsoil of the whole south-western extremity of Low Furness. It deserves remark in this place, that at Hole Beck, near Stank, in a very deep denudation, yellow, cellular beds of magnesian limestone are exposed at the base of the red sandstone §. The red sandstone is probably also expanded under the low region at the south-western extremity of Cartmel Fells ; as it is said to have been reached in two places by excavations, and it appears, as a very characteristic conglo- merate, unconformable to the mountain limestone near Flookborough Spaw. No traces of it have, I believe, been discovered on the neighbouring coasts of Westmoreland and Lancashire; but it reappears (far beyond the limits of the country Iam attempting to describe) in a small patch, at Westhouse, near Ingleton ; as has been already noticed by Professor Phillips |]. These detached masses of the new red sandstone prove, at least, that the formation was at one time expanded over a much larger surface than it is at present : indeed, there can be little doubt that it once extended, in a conti- nuous mass, from the shores of Cumberland to South Lancashire and Cheshire. That much of it has been swept away, is shown by the whole aspect of the * See Plate XXV. fig. 5. + See Plate XXV. fig. 6. + By comparing this description with Mr. Greenough’s geological map, it will be seen that he has extended the red sandstone of the Cumberland coast considerably too far south. § See Plate XXV. fig. 7. || Geological Transactions, Second Series, vol. iii. pl. 2. SE2 390 Prof. Sepewick on the New Red Sandstone Series in the neighbouring country. I have already noticed the accumulations of old allu- vial detritus south of Eden ; but they bear no comparison to the vast heaps of similar materials which cover, to an unknown depth, nearly all the tracts of low land bordering on the coast of Cumberland : and all the islands off the coast of Low Furness are exclusively composed of rounded masses of rock (sometimes many tons in weight,) brought down from the old Cumbrian and Lancashire chains, and imbedded in a kind of red alluvial loam derived from the degra- dation of the red sandstone *. In some parts of the coast the alluvial con- glomerates are solidified, and only to be distinguished from the true conglo- merates of the new red sandstone by the greater freshness of the imbedded pebbles : for the pebbles of the old conglomerates (however distinguishable in mineral structure,) have, in the regions | am describing, almost universally undergone a progress towards decay, and are sometimes hollow and entirely incoherent f. Before I go on to the next section of this paper, it may be well briefly to recapitulate. (1.) The red sandstone series above described appears among the last ra- mifications of the Eden, in a position decidedly unconformable to the carbo- niferous limestone f. (2.) In its prolongation it rests upon the upper portion of the carboniferous * The erratic blocks of the Cumbrian mountains are not confined to the places above indicated, but have been carried, in incredible abundance, over the plains of South Lancashire and Cheshire. They are also found, at a great elevation (for example, near the top of the pass from Macclesfield to Buxton), on the chain of hills which separates Cheshire and Derbyshire. I also found them last summer, though generally much diminished in size, on the flanks of the Denbighshire hills, above Oswestry. To what cause are we to attribute this drift of the Cumbrian rocks? Whatever it may have been, it must have acted at a comparatively recent period ; for many of the travelled bowlders, though lying bare on the surface, are very little decomposed, and still ring under the hammer. The present condition of the Cumbrian valleys confirms the previous statement ; for an examination of them leads us inevitably to two conclusions: Ist, that they were not formed by the erosion of the waters now flowing through them; 2ndly, that the causes by which they were brought into their present form must have ceased their action at a comparatively recent period. Every Cum- brian valley which contains a lake gives an independent proof of what is here asserted. + Considered as mere mineral specimens, the conglomerates of the old red sandstone, in the North of England, have often a much newer appearance than those of the new red sandstone. This fact may be partly due to the cementing principle, and partly to the more indestructible nature of the imbedded pebbles of the old red conglomerates. Both in the South-west and North of England, the fragments of mountain limestone, which enter so largely into the new red conglomerates, are generally well preserved where the cementing principle is highly calcareous; but where the cement is siliceous, the limestone pebbles are, I believe, universally decomposing, and in some instances have almost disappeared. t Plate XXV, fig. 2. Basin of the Eden and north-western Coasts of Cumberland, &c. 391 series ; and, in the long range from Appleby to Maryport, there are few places where the two formations can be shown, by their dip or inclination, to be in an unconformable position. (3.) At St. Bees Head it has apparently the same dip as the coal measures *. But in the same neighbourhood it is proved to pass obliquely over their out- crop; and, after overlapping the mountain limestone, to range along the flanks of the primary mountains f. (4.) It overlies the carboniferous system of Low Furness, and reappears in the next promontory, as a conglomerate unconformable to the mountain lime- stone. It offers, therefore, most obvious analogies to the new red sandstone series of many other parts of England. In one respect, however, it greatly differs from the overlying red sandstone of the great Bristol and Welsh coal fields ; as its beds are, in a part of its range, not only parallel to the beds of the car- boniferous series, but appear, through an intermediate sandstone, so nearly to pass into them, that it becomes extremely difficult to define the precise limits of the two formations. § 2. On some detached Masses of the Carboniferous Series within the area of the New Red Sandstone. There may be three causes to account for the appearance of such masses : Ist, When the chain of Cross Fell was severed (by the great dislocation above noticed), from the carboniferous chain now forming the outskirts of the primary Cumbrian system, it seems probable (independently of direct evidence), that some large dislocated masses of rock would be left in the intervening area which is now generally covered with the new red sandstone. 2ndly, The red sandstone may, when first deposited, have been of a very irregular thickness, and in some places may have left the inferior rocks partially uncovered. 3rdly, The protruding masses of the older rocks may have been laid bare by the great denudations already mentioned. ‘To one or more of these causes we may attribute the appearance of the detached portions of the carboniferous series I am about to notice. The first example occurs near the middle of Broadfield (once a wild heathy tract of land, but now inclosed), about six miles due south of Carlisle, and about a mile and a half east-south-east of the village of Gatesgill. Close to the meeting of four roads, fine contorted masses of mountain limestone are exposed in three quarries, two on the east side of the Penrith road, and one * Plate XXV. fig. 1. + Plate XXV. fig. 5 & 6. 392 Prof. Sepewick on the New Red Sandstone Series in the on the west*. In the two eastern quarries we have fine thick beds of moun- tain limestone, some dipping south-south-east, and others nearly perpendicu- lar, surmounted by several impure beds, which will not burn to lime, and by about fifteen feet of gravel, tinged red with fragments of the new red sand- stone. In the western quarry the dip is about north-north-east. At one end of it the limestone is more than twenty feet thick ; but it thins off, at the other end, to about half that thickness. This mass is associated with a white free- stone, and with an impure, ferruginous, encrinite limestone unfit for use. Some purple-coloured shale and siliceous gritstone, laid bare in a small excavation about half a mile south-west of these quarries, appear also to belong to the car- boniferous series ; but how far they are expanded over the plateau of Broad- field, it would be no easy matter to determine, in the present concealed state of the country. In the valleys of Ivegill and Raw Beck, to the south and east of Broadfield, there are, however, very fine escarpments of new red sandstone. The next example is seen in Chalk Beck, about a mile north-east of Rosley, and three quarters of a mile above Chalk Foot. On the right bank of the rivulet there is an escarpment of limestone between 20 and 30 feet thick, sur- mounted by 30 or 40 feet of red diluvial gravel. Close to this escarpment are beds of new red sandstone, partly resting upon the limestone, and partly sepa- rated from it by thin beds of conglomerate containing angular fragments of limestone. In such a position it might easily be mistaken for a portion of the formation of magnesian limestone, especially as some of the beds are earthy and cellular; and all of them are yellow, and contain magnesia. It, however, on the whole, more resembles the dolomitic varieties of mountain limestone ; and it dips slightly to east by south, while the nearest beds of red sandstone dip north-north-west. Moreover, it contains Orthoceratites, beautiful corals of the genus Caryophyllia, resembling species well known in the mountain limestone, and large Producte, among which, if I mistake not, is the Pro- ducta Scotica ; but it does not contain any characteristic fossil of the magne- sian limestone formation. On these accounts I do not hesitate to class it with the outlying rocks of Broadfield, which are undoubtedly of the carboniferous order +. The last instance which fell under my notice, of any outlying portion of * The locality is defined on the county maps by the meeting of four roads,—from Gatesgill, from High Burnthwaite, from Burghthwaite, and from Itonfield. + There may be some doubt whether the Chalk limestone be mithin the area of the new red sandstone, of which it is impossible to lay down the demarcation in a continuous line. There is, however, an outbreak of the red sandstone at Green quarry, about half a mile further up Chalk Beck. Basin of the Eden and north-western Coasts of Cumberland, &c. 393 the carboniferous rocks within the area of the new red sandstone, occurs near the village of Aketon, about four miles north of Wigton. Some of the neigh- bouring country is much covered by ancient turf bog and a peculiar sandy al- luvion ; but to the north of the village some beds of limestone and shale are laid bare on both sides of the road; and if I have not been misinformed, a bed of coal 16 inches thick was proved, by boring, to be associated with them, at a place called Moor Dyke, on the west side of the road. I mention these facts in the hopes of calling to them the attention of future observers; for I know of no place within the limits of the red sandstone, where a search for coal could be commenced with the same prospect of success. My knowledge of the central portions of that great area, within the basin of the Eden, which is chiefly covered by the new red sandstone, is, however, extremely limited. My examination of Cumberland was chiefly confined to the carboniferous rocks and the central cluster of mountains ; and whenever, in making a tra- verse, I was led to the edge of the new red sandstone, I generally considered my immediate labours at an end. § 3. On the successwe Deposits which compose the New Red Sandstone Series, &c. The preceding details give a general notion of the distribution of the new red sandstone series within the basin of the Eden, and on a part of the coasts of Cumberland and Lancashire ; but they give only a very inadequate indica- tion of the structure and order of those great mineral masses of which it is composed. This information is, however, conveyed in a much more perfect manner by the coast section, from Parton to St. Bees Head, which I now pro- ceed to describe*. The rich coal field of Whitehaven, constituting that part of the carboniferous series which is superior to the millstone grit and mountain limestone, may be separated into two divisions, the upper containing the great maz and bannock bands, the lower containing four or five workable beds, but of inferior quality. The united thickness of these two divisions is, perhaps, not less than two thousand feet; and from this estimate the carboniferous limestone and its asso- ciated beds are of course excluded. The upper beds are worked in a small field on the coast, immediately south of Workington ; but in consequence of an enormous upcast fault they are thrown out, and the lower division is brought into the cliff, and occupies an extensive plateau stretching from Har- rington to the hills north of Morresby, about two miles and a half from the har- bour of Whitehaven. Near the crown of these hills (and about a mile from * See Plate XXV. fig. 1. 394 Prof. Sepewick on the New Red Sandstone Series in the the point where the accompanying section commences) another great fault, producing a downcast to the south-west, probably of not less than a thousand feet, once more brings in the upper rich division of the coal field. Unfortu- nately, however, between this fault and the village of Parton, the beds dip to the east; so that all those which are below the high-water mark necessarily crop out under the sea. The result is, that no one has been able to extract the coal, in consequence of the great quantity of sea water which finds its way through the beds along their planes of dip. At Parton there are other considerable dislocations, not merely altering the relative level of the beds, but again producing a reversed dip, by which the whole series of coal measures, as well as all the overlying groups extending to St. Bees Head, are made to plunge to the south-west at a small angle of inclination. The successive strata, therefore, after this last inversion of dip, have their outcrop in the interior of the country; and the coal seams are perfectly protected from the sea water by the impervious overlying beds of shale. Such is the position of the submarine portion of the coal field of White- haven ; and it does not seem possible to assign any limit to the works that may there be conducted under the sea in the direction of the dip. But it is foreign to my purpose to give any description of these works, as the pre- ceding remarks are introduced for the sole purpose of explaining the nature of the base line on which the accompanying section is constructed™. The north-eastern extremity of this section commences at Parton, among some broken and contorted beds. The confused ground extends about 150 yards, after which the beds acquire their regular south-western dip above de- scribed. Following the coast towards Whitehaven, we find the cliff composed of shale and sandstone, which, after being continued several hundred yards, is sud- denly cut off by a downcast fault, of 24 fathoms, to the south-westt. From this point to the north end of Whitehaven, we find an uninterrupted rock of coarse sandstone (resembling many well-known varieties of millstone grit), generally of a gray or brownish gray colour, but here and there with stains and streaks of red. Parts of the rock are of a very strong texture, and have been extensively quarried for the new piers at Whitehaven. It has also been cut through by the old tunnel between Whitehaven and Parton, as well as by a * I owe the knowledge of most of these facts to my friends Messrs. Peile, of the Colliery Office, Whitehaven; and in a subsequent memoir on the carboniferous series of Cumberland (in which a description of the Whitehaven coal field will of course form an important part), Mr. W. Peile has promised to be my fellow-labourer. + This is the second fault marked on the section. Basin of the Eden and north-western Coasts of Cumberland, &c. 395 new tunnel, now excavating for the purpose of a ready communication with the hills west of Dissington, where the main coal seam is about to be worked. Its structure is therefore very well exposed. Close to the north end of Whitehaven comes in another fault, producing a downcast to the north-east, of eleven fathoms ; but if we follow this fault into the interior, the quantity of dislocation produced by it is enormously increased. By this and two other faults, elevating the strata in the same direction, we may explain the high position of the quarry sandstone in the hills immediately south of the town. At Saltom, as is seen in the section, are two faults, pro- ducing downcasts in opposite directions: their joint effect is to bring the great sandstone once more to the level of the sea, after which it is continued nearly a mile in a lofty cliff; and its component beds are carried by their dip (with the interruption of one fault) in regular succession towards the base of St. Bees Head. The general character of this sandstone is the same as in the tunnel cliff, north of Whitehaven ; but it is of a much redder colour, contains many small ferruginous nodules, andin mineral character is perfectly identical with many portions of that peculiar red sandstone which separates the Yorkshire coal measures from the magnesian limestone. It is generally without any trace of fossils: the very extensive excavations carried on in it on both sides of White- haven, have; however, brought to light a few obscure impressions of Equiseta and Calamites. It makes, therefore, a very near approach to a true coal grit ; and in the surveys hitherto published, as well as in the estimation of the coal viewers of the neighbourhood, it has, I believe, always been regarded as a true member of the coal measures. Under Barrowmouth this sandstone is surmounted by a conglomerate, exactly like the magnesian conglomerates of our south-western coal fields, but only two or three feet in thickness. Its lower part is of a reddish colour, and contains, among other fragments, rolled masses of mountain limestone mixed with hydrate of iron. The upper parts of it have a calcareo-magnesian ce- ment; and it is surmounted by, or rather graduates into, a yellow, foliated, cellular, magnesian limestone. This limestone is not well exposed at the sea-side, being almost buried under the overlying red marls; but some of its upper beds are mixed and striated with red ferruginous matter, and seem to pass into a singular, red, siliceous sandstone containing jasper and chalcedony. It is, however, extensively worked at Barrow and Preston How quarries, and shows in great perfection most of those peculiarities of structure which so well mark the formation. I do not know of any section where all its beds are exposed ; but it probably never exceeds 60 feet in thickness. Of its relations to the coal VOL. IV.—SECOND SERIES. 3 F 396 Prof. Sepewick on the New Red Sandstone Series in the measures, there could not be a shadow of doubt, though there were no other section besides that on the coast ; and in Croft Pit it has been sunk through into the lower sandstone and down to the mazn and bannock seams. Along with the other upper strata, it strikes across the peninsula of St. Bees Head, and is seen in Ben How quarry (near Green Bank farm), on the low road from St. Bees to Whitehaven, where it is made, by a remarkable fault, to abut against the lower red sandstone*. Beyond this point the yellow, cellular limestone beds do not appear ; but the magnesian conglomerates are found to the south of the valley of St. Bees (at Parkhouse, and in the rivulet which runs down thence towards Linethwaite), forming the base of the new red sandstone group. Over the preceding deposit of the coast section, come several feet of gray, thin-bedded, sandy marls, to which the red jaspideous bed, above noticed, ap- pears to be subordinate. This sandy deposit is surmounted by alternating beds of unctuous, red marl and gypsum, amounting in thickness to eight or ten fathoms. ‘The two substances are so mixed together, in some places, as not to be separable ; but in other parts of the section (and especially in the higher and lower portions of it) the gypsum is found in strong beds, which have been much worked; and in one of the excavations was found a bed, about half an inch thick, composed of a nearly pure, earthy, semi-indurated carbonate of zinc. This fact deserves remarking, as carbonate of zinc occurs in con- siderable abundance in deposits on the Mendip Hills, nearly of the same age with those here described. Lastly, the gypseous marls are surmounted by sandy marls and micaceous, slaty sandstone, rising to a considerable height in the red precipice of St. Bees Head ; and these are overlaid by a great, thick-bedded freestone, which in some places loses the lines of stratification, and decomposes into rude, grotesque, castellated forms. These upper rocks are identical with the finest specimens of the new red sandstone of Cheshire and Lancashire, of Low Furness, Ap- pleby and Carlisle, and may be regarded as one of the most characteristic exhibitions of the formation to be seen in our island. The several beds entering into the structure of St. Bees Head, are carried by their south-western dip, and by a downcast fault, one after the other under the sea; and no superior formation is visible on any part of the neighbouring coast. The “upper red marl and gypsum,” completing our red sandstone series up to the lower lias marls, are therefore wanting, either having been washed away by those causes which have produced the present deep indentations of the coast, or being, perhaps, buried under the waters of the western sea. * See Plate XXYV. fig. 4. Basin of the Eden and north-western Coasts of Cumberland, &c. 397 So far the account of the accompanying section, and of the successive groups of rocks overlying the Whitehaven cecal field, has been purely descriptive, and unmixed with any hypothesis. The facts themselves contain, however, their own interpretation. I have already stated that the lower sandstone, overlying the Whitehaven coal field, resembled in structure the lower sandstone imme- diately overlying the great Yorkshire and Durham coal fields. The former contains, though very sparingly, impressions of Equiseta and Calamites; and so does the latter, as I have now ascertained, though I was unacquainted with the fact at the time the detailed account of the structure of the magnesian limestone series was published in a former part of our Transactions *. Again, though the “lower red sandstone” of Yorkshire and Durham ap- pears, in some cases, to graduate into the coal measures (on which account it was classified with them by Mr. Smith in his geological map of Yorkshire) ; yet, when considered on a great scale, it is unconformable to them, and on that account was separated from them and arranged, in the paper just quoted, as the lowest member of the new red sandstone group. In the same manner, in the coast section above described, the lower overlying sandstone appears to be conformable to, and to graduate into, the coal measures of Whitehaven. But, during many excursions in that neighbourhood, I have traced it from the sea-side to the interior of the country, to the top of the hills above Dissington, over the summit of Whillimoor, and to the crest of the hills overhanging Ar- lecdon ; and thus ascertained that it spreads over the edges of the coal mea- sures, and that, when considered in its whole extent, it is, as far as regards the position of its lower surface, perfectly analogous to the “lower red sand- stone” of Yorkshire and Durham. But the analogies do not end here. It is proved by several of the sections published in a former part of our Transactions}, that the “lower red sand- stone” in certain parts of Yorkshire had undergone considerable movements, and been exposed to considerable degradations, before the deposition of the magnesian conglomerate and magnesian limestone: for they are here and there seen resting on its inclined edges, while in other places (for ex- ample at Pontefract, in many parts of the County of Durham, and on the coast of Northumberland), the “lower red sandstone’ and magnesian limestone graduate insensibly into each other, without any break of continuity what- soevert. Now we meet with precisely the same accidents of position in the * Vol. iii. p. 37. et seg. Very fine impressions of Equiseta or Calamites have been found in the “lower red sandstone” of Hooton-Lovett in Yorkshire. + Geological Transactions, Second Series, vol. iii. Plate VI. figg. 3. 4. 5. 6. $ Ibid., vol. iii. p. 67. 3F2 398 - Prof. Sepewick on the New Red Sandstone Series in the neighbourhood of Whitehaven: for in following the overlying deposits into the interior of the coal field, we find many traces of magnesian conglomerates, with rolled masses of mountain limestone, in every respect identical with those of the coast section (for example, at Gilgaron, near Arlecdon, at Sand Closes, &c.) ; and we have the clearest proof that the lower red sandstone had been exposed to considerable degradations, and scooped out into great hollows before the conglomerates, which form the base of the magnesian lime- stone, were first accumulated. It follows, therefore, that the “lower red sand- stone’? overlying the Yorkshire and Durham coal fields, and the lower red sandstone of Cumberland, are identical in their structure, their relations, their fossils, and in all the accidents to which they were exposed during their de- position. We may therefore conclude that they are true geological equiva- lents ; that they are probably on the parallel of, at least, the lower portion of the eres des Vosges ; and that they are unquestionably the equivalents of the rothe todte liegende overlying the coal series at the southern extremity of the Hartz mountain. The magnesian conglomerates, described in the previous details of this paper, cannot be classed with the lower red sandstone, to which they are sometimes unconformable ; but they graduate into, and form an integral part of, the magnesian limestone, sometimes appearing entirely to replace it. The magnesian limestone of the coast section is evidently on the exact parallel of the magnesian limestone of Nottinghamshire, Yorkshire, and Dur- ham, though not developed on so large a scale, or separable into the same number of minute subdivisions. It is not coextensive with the upper division of the overlying sandstone series ; but it may exist in many places, under the great heaps of transported matter; and it breaks out, as above stated, ma very characteristic form, from beneath the new red sandstone of Low Furness, in a deep valley near the village of Stank*. With this exception, I have never seen it beyond the promontory of St. Bees Head, in any place within the limits of the range of country above described. The red marl and gypsum under St. Bees Head are very nearly on the parallel of the “dower red marl and gypsum” of the Yorkshire series} ; and the red sandstone of St. Bees Head is unquestionably the exact equivalent of the upper red sandstone of that series. ‘The ‘upper red marl and gypsum” * See Plate XXV. fig. 7. + There are in Yorkshire two deposits of red gypseous marls under the great mass of the upper new red sandstone ; one under, the other over the thin-bedded limestone of Ferrybridge. With either of these the gypseous marls of St. Bees Head may be brought into comparison, as the Ferrybridge limestone is not seen in Cumberland. Basin of the Eden and north-western Coasts of Cumberland, Se. 399 (probably on the parallel of the marnes irrisées and the keuper of France and Germany) do not appear in the coast section, for reasons already stated. From all these facts, I conclude that the series of deposits overlying the Cumberland coal fields is, as far as it goes, perfectly analogous to the corre- sponding series of Yorkshire and Durham, as described in a former paper. Nor need we he surprised at this analogy, when we consider the almost perfect agreement of the great groups of the new red sandstone series in En- gland and central Germany. I need not repeat the evidence on which this conclusion rests ; but I may add, that it is even more complete than I supposed at the time the former memoir was published. Three obscure corals, found in our magnesian limestone, had already been figured by Mr. Goldfuss under the generic name of Gorgonia*; and on referring to his account of the lo- calities from which his specimens were derived, it will be seen that they come from the magnesian limestone formation of Mansfeld. Nor has this conclusion been drawn from the mere resemblance of the figures; for both the British and German specimens have been examined by that accomplished naturalist, and the fossils found to be specifically identical, as he has himself informed me. This fact alone, to which, however, a thousand others might be added, is a sufficient reply to the assertions of some modern writers, who have ventured to affirm that organic remains are of no value in determining the contempo- raneity of distant formations. In our south-western coal fields the deposits immediately overlying the car- boniferous rocks are subdivided into three principal groups: the lowest com- posed chiefly of conglomerate, with a calcareo-magnesian cement; the middle group of red and variegated sandstone ; and the highest of red and variegated gypseous marls. I think it at least probable that the conglomerates of the Bristol coal fields are on the exact parallel of the magnesian conglomerates described in this paper; from which it follows that the Bristol conglomerates, as well as those in the valleys of Devonshire (if they be all of the same age), are the true representatives of the magnesian limestone, and not of the rothe todte lLegende. I ventured to express this opinion in a former paper}; and it is greatly con- firmed by the facts here stated, as well as by some other facts which fell under my observation last summer (1831), while crossing over one of the coal for- mations of Shropshire. About six or eight miles south-west of Shrewsbury there is a small coal field, stretching at the base of a greywacké chain from * See Goldfuss, tab. vii. fig. 1; tab. xxxvi. fig. 1; and tab. x. fig.1; Gorgonia dubia, G. anceps, G. infundibuliformis; and compare them with Geological Transactions, Second Series, vol. ili. p. 120; and Plate XI). figg. 5. 6.7. 8. + Geological Transactions, Second Series, vol. iii. p. 122. 400 Prof. Sepewick on the New Red Sandstone Series in the Pontesford towards Westbury, and surmounted by a series of deposits con- nected with the group of the new red sandstone. The order of succession, as laid bare by a deep cut for the road near Aldbury, is as follows: 1st, Coal measures. 2ndly, Coarse reddish sandstone, in character intermediate between a coarse coal grit and a true red or variegated sandstone. 3rdly, A very fine magnesian conglomerate, forming a distinct range of hills by Cardeston, Rownton, and Adenbury, and in mineral structure like the Bristol and De- vonshire conglomerates*. 4thly, Red and variegated sandstone descending into the great plain of Shropshire, and of unknown thickness. Here, there- fore, the section is more complete than at Bristol, and is perfectly analogous to the Cumberland coast section, with this exception, that the conglomerate is developed at the entire expense of the magnesian limestone. The con- clusion naturally deduced from this section is the same as that at which I before arrived —viz. that the magnesian conglomerates do not represent the rothe todte liegende, but a part of the next superior division—the magnesian limestone, or zechstein. In comparing the Bristol and Exeter conglomerates with the rothe todte hegende, our geologists made use of the best evidence with which they were acquainted. But the new red sandstone group is now better understood ; and in future comparisons with Continental deposits of the same age, we should use, as our types, those sections which are most complete, instead of the Bristol or Exeter overlying groups, in which more than one half the series is abso- lutely wanting. Nor is any assistance to be derived from the accidental pre- sence of porphyry pebbles ; in as much as they occur in the Shropshire con- glomerates, as well as in those of Exeter, and are in truth of no value in de- termining the relative age of any secondary rock. it must, however, be allowed that a considerable part of our difficulties have arisen from the ill-defined language of some of the German geologists. ‘The term rothe todte liegende has probably been often applied to conglomerates of the same age with our magnesian conglomerates. It originally designated certain, coarse, red sandstones overlying the coal measures of the Hartz, which, after a personal examination of them, I believe to be the exact equivalents of the “lower red sandstone” above described. In the late works of Mr. Hoff- mann the same term is applied to a red sandstone under the coal measures of Wettin, and therefore on the parallel either of some of our lowest red coal grits, or perhaps of our old red sandstone. * The condition of the pebbles imbedded in this conglomerate is very remarkable. Some of the mountain limestone pebbles retain their mineral structure and characteristic fossils; others are so altered as hardly to be distinguishable ; some having become granular, and some perfectly pul- verulent. See a previous note, p. 390. Basin of the Eden and north-western Coasts of Cumberland, &c. 401 It only remains for me to notice the importance of the lower red sandstone in another point of view, entirely distinct from the former. All who have written on our south-western coal fields, have noticed the total break of con- tinuity between their component strata and the overlying series: and in the beautiful illustrations accompanying the paper of Dr. Buckland and Mr. Cony- beare*, it is impossible to point out the highest members of the inclined coal measures, in as much as an indefinite number of them may possibly be buried under the superior horizontal deposits. In Shropshire there is, I think, no such break of continuity, the gap being filled up by the lower red sandstone. Again, though the lower red sandstone of Yorkshire is, on a great scale, unconformable to the coal measures, and ought, on that account, to be consi- dered as the base of the new red sandstone series ; yet there are places in that county, where, for twenty miles together, there is no trace of any want of conformity ; and the lower red sandstone (containing, as already stated, a few coal plants) forms a true connecting link between the highest coal grits and the group of the new red sandstone f. Considering, then, that the red sandstone group sometimes forms a passage into the coal series, —that the fossils of the magnesian limestone are very nearly the same generically, and sometimes specifically, with the fossils of the carbo- niferous limestone {,—that the grits of the coal measures in the North of En- gland are not unusually of a red colour,—that on the confines of Scotland the lowest division of these coal grits alternates with red gypseous marls, and passes downwards into beds of red sandstone and red shale, nearly, if not exactly, on the parallel of the old red sandstone §,—considering all this, I think that the phenomena exhibited by our lower secondary deposits lend some support to a classification now generally adopted in Germany, which regards the whole carboniferous group but as an integral part of a great formation of red sandstone, commencing with the old, and ending with the new red sandstone series. The zoological argument certainly gives some consistency to this arrangement. I do not, however, mean to deny the full propriety of the classification of the same great groups, now adopted by English geologists. It is good, because founded in nature ; and each country ought to be described without any accommodating hypothesis, according to the type after which it has been * Geological Transactions, Second Series, vol. i. p. 2i1. ¢ Ibid. vol. iii. p. 57. No. 5. { Ibid. p. 119: § The description in the text was derived from phzenomena, observed in 1830, in the valley of the Tweed. The gradual passage of the coal measures into the old red sandstone is still more strikingly exhibited on the coast of Scotland, north-west of St. Abb’s Head. 402 Prof. Sepewick on the New Red Sandstone Series in the moulded. But in comparing the unconnected deposits of remote countries, we must act on an opposite principle ; learning to suppress all local pheno- mena, and to seize on those only which are coextensive with the objects we at- tempt to classify. In this general view the arrangement of the red sandstone and carboniferous series in one great group, is perhaps the best fitted to the present state of our knowledge. §4. General Comparison of the Red Sandstone Series of Scotland and England. It has been shown by Mr. Murchison and myself, that in the Isle of Arran a carboniferous series is interpolated between two enormous masses of red sandstone and conglomerate ; and that the whole group passes, in the ascend- ing order, into a formation of red sandstone, which may represent either one of the red, sterile parts of the Scotch carboniferous series, or the lowest di- vision of the new red sandstone*. It is almost impossible to ascertain the precise limit of this upper red sandstone of the Isle of Arran: but the best way of approximating to it would be to trace the old red sandstone group from the south flank of the Grampians to the west coast of Scotland; and from thence to follow the red sandstone series to the coasts of Ayrshire. By the help of such an examination (a desideratum in Scottish geology), we might perhaps establish such analogies as would enable us to determine the exact upper limit of the Arran section. I consider it now established beyond doubt, that the great masses of red sandstone and conglomerate which fringe the Highland coasts, and range, on the south flank of the Grampians, from one side of Scotland to the other, belong almost exclusively to the old red sandstone. The large development of the bituminous schist of Caithness has thrown some unnecessary difficulties in the way of this conclusion. Jt alternates, however, with the old red con- glomerates to their base, and cannot be separated from themT ; it is overlaid by a red sandstone decidedly of older character than any variety of the new red and variegated group ever seen in other parts of Great Britain ; it con- tains a suite of fossils peculiar to itself; not, as far as is known, interchanging a single species with the magnesian limestone ; it is represented (and by no means in an unusual form) on the south flank of the Grampians by a series of thin-bedded strata, placed by Mr. Lyell even lower than the old red sand- stone}: and, lastly, the remains of fish have been found by Dr. Fleming in groups of slaty sandstone, which, though superior (like most of the Caithness schists), to the lowest old red conglomerates, are inferior to the true carboni- * Geological Transactions, Second Series, vol. ii. p. 21; and Plate III. ¢ Ibid. pp. 140. 157, 158. ¢ Ibid. vol. ii. Plate X. Basin of the Eden and north-western Coasts of Cumberland, &c. 403 ferous formations of Fifeshire. I conclude, therefore, that the true position of the ichthyolites of Caithness is out of ali doubt, and adhere, with very slight modi- fications, to the classification published by Mr. Murchison and myself*. By way of conclusion, I may add, that the anomalies at which I have pointed, in different parts-of this paper, and the difficulties they throw in the way of any universal classification, can be no matter of surprise. The great cause for wonder is, that among such vast and rude, mechanical operations of nature, we should be able to trace even the approximate ele- ments of order. Whatever may be hereafter decided about the general group- ing of the coal measures, the near coincidence of even the minute minera- logical subdivisions of the new red sandstone series in the North of England and central Germany, and the general correspondence of their fossils, must be regarded as one of the most satisfactory conclusions of secondary geology. POSTSCRIPT. Cambridge, August 7, 1835. In consequence of the long delay in printing our Transactions, memoirs must sometimes appear which, at the time of their publication, do not express correctly the opinions of the respective authors. The preceding paper is published (with the exception of verbal corrections and the addition of the short notes) as it was read to the Society. Had the concluding remarks been written now, they would have been considerably modified. I have taken for granted that the Exeter conglomerates, and those over- lying our south-western coal fields, are of the same age. Mr. De la Beche has, I believe, ascertained, since this paper was read, that the former are older than the latter. Hence, the remarks intended to show that the magnesian conglomerates (e. g. those of the Bristol coal fields, the flanks of the Mendip Hills, &c.) were not the equivalents of the rothe todte liegende, cannot be applied to the conglomerates of Exeter, at least without some modification. The Exeter conglomerates may, then, be equivalents of the upper part of that sandstone which, in the North of England, fills up the chasm between the coal measures and the group of the new red sandstone. There is, however, in all the sections of Somersetshire, Devonshire, and South Wales, a want of continuity in these formations. Their position is perfectly discordant, so that it is physically impossible the successive deposits should be complete: something is wanting, which is supplied by the uninterrupted sections in the North of Englandf. * Geological Transactions, Second Series, vol. iii. p. 157. + Precisely in the same way, the sections in the North of England, connecting the old red sand- stone and the slate rocks, are not continuous; and there is just the same break in Denbighshire VOL. IV.—SECOND SERIES. oO) (e! A404 Prof. Sepawick on the New Red Sandstone Series in the The discussion on the age of the Caithness schists might now be con- sidered unnecessary ; but when the paper was read, there were many mem- bers of the Society who were disposed to identify them with the ichthyolites of Mansfeld. The question is now set at rest by the generic and specific characters of the Caithness fossils, and by the discovery of fossil fish in the old red sandstone of Herefordshire, identical with specimens found in the old red sandstone of Scotland. Were I to make any change in the Caithness section, published by Mr. Murchison and myself *, I should alter the colour of the sandstone of Dunnet Head, and make it of one tint with the lower conglomerates ; thus including the highest beds of the series in the old red sandstone. The formation would then have three divisions, which might be respectively compared with the three divisions of the Herefordshire sandstone, first given by Dr. Buckland and Mr. Conybeare; and the echthyolites of Caithness would then come on the same parallel with the cornstones of Herefordshire. If such a comparison be considered as too refined for the evidence on which it rests, I may at least assert, that the words ‘“‘ newer red sandstone,” placed under the colour representing the group of Dunnet Head, tend only to mis- lead the reader, and do not correctly represent our opinions at the time the section was published+. By these words, English geologists have generally designated deposits of the age of the upper sandstone of St. Bees Head, with which it was never our intention to bring the rocks of Dunnet Head into com- parison}. It is true, that the upper limit of these rocks must remain in some measure ambiguous ; but I have now little doubt that the whole of them ought to be classed with the old red sandstone. The relations of the red sandstone group of Shropshire to the carboniferous series have been described during the past year in great detail by Mr. Mur- chison ; and I believe his views agree perfectly with what is stated above (pp. 399, 400.). I had few details to offer, and only alluded to the Shropshire formations for the purpose of confirming conclusions drawn from certain phenomena in the North of England. and Flintshire. How many terms of the series are wanting it is impossible to tell without more evidence; but this evidence is given in the Shropshire and Herefordshire sections described by Mr. Murchison. * Geological Transactions, Second Series, vol. ni. Plate XIV. fig. 2. + I am the more anxious to make this correction, because Mr. Conybeare has adopted and ex- tended this error in his Memoir on the Progress of Geological Science, published in the first volume of the Reports of the British Association for the Advancement of Science. t Geological Transactions, Second Series, vol. it, pp. 157, 158. Basin of the Hden and north-western Coasts of Cumberland, &c. 405 APPENDIX. On the Demarcation of the New Red Sandstone Group, described in the preceding Memoir. The northern line of demarcation, commencing near Brough and ending on the Scotch border, has been already noticed (supra, p. 384, note). The remaining line may be traced as follows. Com- mencing, as before, at the top of the flat lands near the bifurcation of the Belah, the line may be drawn a little south of the left bank of the river, so as to leave out Caber. It then turns, about south by west, till it just touches Winton, from which it ranges a little to the west of Hartley, just under the road from Hartley to Naitby, which place it incloses within the area of the red sandstone; thence, crossing the river, it enters the north end of Wharton Park, and ranging nearly due north, passes along the brow of the hilljust above Kirkby Stephen. The range then appears to be about north-west for more than a mile, when the line makes a bend, passing the rivulet about half a mile south of Soulby; thence to the rivulet a little north of Crosby, from which a curve line may be drawn skirting the high lands, so as to pass a little east of Musgrave; afterwards nearly parallel to the Eden, so as to pass about a quarter of a mile south of Warcop Bridge, north of Birks Chapel; half a mile south of Little Ormshead ; and from the last-mentioned point to the rivulet just above Hoff. The line is then nearly defined by the left bank of the rivulet, and passes to the north-west just above Colby, which it incloses. Part of the preceding line is imaginary, the country being covered by enormous masses of red diluvial gravel. But the conglomerates are seen at Belah Bridge, in the river under Winton, at Naitby and Kirkby Stephen, and in the river above Soulby. Again, the red sandstone is seen on both sides of the river near Warcop; and the conglomerates break out in the rivulet south of Little Ormshead, and at Hoff and Burrels. From Colby the line runs down close to the left bank of the Eden, under Beuley Castle ; thence, through Bolton to the rivulet a little south of Walk Mill; afterwards nearly parallel to the rivulet, and a little to the west of its left bank; thence, skirting the low lands, to a point about half mile south of Cliburne. The remaining demarcation to the Eamont, is very obscure ; but it passes by Clifton Dykes, and under Brougham Hall, into the alluvial flat of the river, and then enters Cum- berland*. For many miles, after it enters Cumberland, the line of demarcation is very ill defined. To the east of the Petteril is a lofty ridge of new red sandstone hills, commencing with Penrith Beacon. But on the road from Penrith to Hutton and Hesket Newmarket, we pass a very doubt- ful country, which has always been coloured as new red sandstone. Some of the red sandstones in that district (for example, at Catterlen, Hutton Park, &c.,) appeared to me, however, (when I ex- SE ee: PP yy ST yet i tae SEE * The area inclosed by the line above described is extremely covered with red gravel, formed, in part, by the breaking up of the new red sandstone. Within the same area are also some places where the new red sandstone has been washed off. Thus, near Warcop, there is in the bed of the river an inclined micaceous red grit, probably belonging to the carboniferous series. Some very remarkable red gritstones, associated with a magnesian limestone, are found on the hills west of Soulby, and are clearly a part of the carboniferous system. I do not think the lower division of the new red sandstone is found in this district; though I ought not to make the assertion with much confidence, having never examined it since the year 1823. 362 A06 Prof. Sepewick on the New Red Sandstone Series in the amined the district in 1823,) more to resemble the ferruginous coal grits, or the lower red sand- stone; and I think it probable (after what has been stated above respecting Broadfield, supra, pp- 391, 392,) that a spur of the older rocks, between the Petteril and the Caldew, encroaches con- siderably on the line I am describing. I throw this out as a mere conjecture, confirmed, however, by the fact, that inclined beds of a hard red gritstone are also found along the Petteril, at least as far north as the Broadfield limestone. Passing, then, this doubtful tract, we find characteristic beds of new red sandstone between Macey Bank and Ivegill; and thence, south of Highhead Castle to the banks of Raw Beck, and down both sides of that rivulet for more than a mile. Here, again, the demarcation is not only obscure in many places from the want of good sections; but difficult also from the appearance of lower grits, of a red colour (“lower red sandstone” ?), which break out in both the above-mentioned rivulets. No rock is visible for some way west of Raw Beck; but an imaginary boundary may be drawn to the Caldew, a little south of Rose Bridge, and thence to Green Quarry, a little south of the Chalk limestone above described (supra, p. 392). From that quarry the line sweeps round nearly by toler) able dislocated coal field of Rosley, now nearly deserted). From Tracing Tree it passes through a wood, a little above the confluence of Silver Gill with the rivulet, and thence under Church Hill, and on the north side of Islekirk to Parson Bridge ; from whence it may be traced near Cross Hill, a little above Bridge Mill, and close to Low Blaithwaite ; from which place the line sweeps to the south-west a quarter of a mile south of Elfield, and more than half a mile above Crook Dyke Mill; Howrigg, Height, Brackenthwaite, Cragg Houses, and Tracing Tree (almost inclosing a remark- and so after crossing the river in a direction about south-south-west, it turns west, ranging a little north of the Leesrigg road, through the hill above King Gate, along the south side of Brayton Hall Park, under the village of Aspatria, under Hayton, a little south of the road from Hayton to Al- lerby, just under Crosby ; thence deflecting to the north-west, it passes north of Birkby, and down by the right bank of the Ellen to the sea at Maryport. We may pass over the coast from Maryport to St. Bees Head, as it is either occupied by the > coal measures, or by the “lower red sandstone,” in places already described. Across St. Bees Head the range is defined by quarries, ending (as above stated) at Ben How*. On crossing the valley, it reappears in Walton Wood, just above Linethwaite, and thence passes just under Bank End, and at the base of an escarpment, from which it descends between Gill Foot and How Bank ; and, inclosing Orgill, it disappears in the alluvial plain of Egremont. Beyond this plain the line appears to range nearly east and west from New House to Grange ; and from a quarry near the latter place it strikes about south-south-east into the valley of Kirk Beck. It crosses above the mill, and then ranges above Head of Hail and Hall Garth to the north end of Cold Fell near Side; from whence it descends into the valley of the Calder, in a di- rection about south-south-east. It crosses below Thornholm, and then ranges east-south-east on the way to Farmary, and is exposed in quarries at the hill-top. It then strikes across the Gill, and is laid bare about a quarter of a mile above Hurrel Barrow; thence it ranges through Blaing Fell, leaving Lockray and Whinray to the east, just touching Bank House, and forming the whole escarpment of the hill above Gosforth. We have no regular escarpment of the formation on the Cumberland coast south of Gosforth ; but the rock is seen at the following places: Drig Cross, west of Gosforth; Brandreth Scar and * The range of “ the lower red sandstone” over the coal field, as well as certain outliers of the new red sandstone, will be given in a subsequent paper. Basin of the Eden and north-western coasts of Cumberland, &c. AQT Codlin Rock, two reefs to the south of Ravenglass, only seen at low water; on the Cross House estate, half a mile north of Bootle; and, lastly, in wells and other excavations at Mopus, Hise Moor, Well Bank, and Old Highton, all in the same neighbourhood, and on the north side of the Bootle rivulet. Crossing the estuary of the Duddon to the limestone of Roan Head, we find the superior rocks concealed under blown sand ; but the new red sandstone breaks out south of Wet Flats, and may be traced by Little Mill, Billing Coat, and Newton; and thence by Bousfield, Stank, and Hole Beck. Beyond the last-mentioned place everything is buried under alluvial accumulations to the sea-side ; but at low water the red sandstone is seen just to the north of Rampside. It appears also at the north point of Old Barrow Island. In the Cartmel promontory the new red conglomerates appear at Rougham Point, west of Humphrey Head; and the red sandstone is said to have been reached by boring between Cannon Winder and Ravend’s Winder, and close to Lower Hosker. By help of the preceding notice, the demarcation of the new red sandstone may be laid down on the large county maps with a near approach to accuracy. Had the Ordnance maps of the northern counties been published, such details would have been perfectly useless, as the information would have been more correctly conveyed by a superficial colour, than by any verbal description. i 4 7 : il \ i eh Mee pattciay, wy. adh. o' se i «ak firs % A? J ‘ CI y w ! wrcidoab Beis din 1% ia , ee ; ote a i - . vik ie I oiWw endl be ' hit red 2 ae . a4 ihe i By, ma ! ' tip loop holy ut : es é ald bite Wi F n " 7 E ‘ pil sa i £ ¢ 2 S ' it? J P vr j ; ih 7 i 7 + * \ ‘ . i * . ‘ ) ‘ ° ’ ' i ‘ ’ ‘i ‘. 4 oo ns ie ? } ‘ e VII.—On a portion of Dukhun, East Indies. By Lizutenant-Cotoner W. H. SYKES, F.R.S. F.G.S. F.LS. [Read January 23, 1833. ] My personal observation of Dukhun (Deccan) and Konkun (Conean) * is not confined to the boundaries laid down in the following geological memoir ; but as the rock and mineral specimens remaining at present in my possession are from Dukhun only, I have not thought it proper to extend my details beyond the limits I here prescribe to myself, although I might venture to do so from notes taken at different periods, without exposing my accuracy to question. I will, however, in closing this paper, offer a few ob- servations on the trap and other formations of India; the amazing extent of the former not appearing to have been appreciated hitherto in European geo- logical works. : Boundaries. My tract + is bounded on the west by the range of mountains usually deno- minated by Europeans the “Ghats”, from a misinterpretation of the term ghat, which simply means a pass, the proper name of this range being the ““Syhadree’”’; on the north by the Mool river, as far as Rahooreh; on the east by a direct line from Rahooreh to the city of Ahmednuggur, and sub- sequently on the north-east by the Seena river until its Junction with the Beema river below Mundroop; on the south-east by a line from Mundroop to the celebrated city of Beejapoor; on the south by a line from Beejapoor to the town of Meeruj; and from this place the boundary in the south-west is the Kristna and Quina rivers, to the hill fort of Wassota, situated in the Ghats. The western boundary line extends, as the crow flies, about 144 miles; the northern 72 miles; eastern and north-eastern 159 miles; south- eastern 41 miles; southern 80 miles ; and south-western 88 miles. Agree- ably to observations made by myself and the officers of the revenue survey in * With respect to the pronunciation of native words, the “u” is the w in “hut,” and the “a” the a in “all.” t+ See Map, Plate XXVI. 410 , Lieut.-Colonel Sykes on a Portion of Dukhun. Dukhun, the tract lies between the parallels of north latitude 16° 45' and 19° 27', and east longitude 73° 30! and 75° 53’, and, roughly calculated, may be said to comprise an area of about 26,000 square miles. Stratification. Previously to entering into descriptive details, I will state, in a few words, that the whole of the country comprised within my boundaries is composed of distinctly stratified trap rocks, without the intervention of the rocks of any other formation. Whether at the level of the sea, or at the elevation of 4500 feet, in all and every part, beds of basalt and amygdaloid are found alternating, whose superior and inferior planes preserve a striking parallelism to each other, and, as far as the eye can judge, to the horizon. Barometrical measurements and the course of rivers indicate a declination of the country to the east-south- east and south-east. From the town of Goreh, latitude 19°03 and longitude 74°-05, on the Goreh river, following a mean course for the river until it falls into the Beema, and subsequently, continuing a mean course for the Beema until its junction with the Seena river, the distance is about 200 miles, and the declination 671 feet : there may therefore be a trifling dip of the strata ; but as a succession of low terraces occur in that distance, the apparent horizontal position of the strata may be unaffected by the above difference of level. Dr. MacCulloch, describing the overlying or trap rocks, says, “these masses are generally irregular, but sometimes bear indistinct marks of strati- fication *.””. As Dr. MacCulloch’s language implies the rare occurrence of stratification, instead of its being a distinctive feature, at least of the Indian branch of the trap family, I deem it necessary to quote the few authors who have written on Indian geology, in confirmation of the fact I have stated +. * Classification of Rocks, p. 466. + “These mountains (the Vindhya range), like every other in Malwa, appear to be distinctly stratified, consisting of alternate, horizontal beds of basalt or trap and amygdaloid. Fourteen of these beds may in general be reckoned, the thinnest at the top, and rapidly increasing in thickness as they lower in position, the basalt stratum at the bottom being about 200 feet thick.” Again, at page 327, he says: “In the upper plains of Malwa every point of view presents the same uni-— form and distinctly streaked appearance noticed in the Vindhya range.”—Captain Dangerfield, in Geological Notices of Malwa, in Appendix No. 2. to Sir John Malcolm’s Central India, pp. 322, 327. Dr. Voysey, in a paper on the Geological and Mineralogical Structure of the vicinity of Nag- poor, says: “ From the summit of the hill of Sitabaldi the difference in the outline of the rocks eastward is very perceptible. The flattened summits and long flat outline, with the numerous gaps of the trap hills, are exchanged for the ridgy, peaked, sharp outline of the primary rocks.”— Physical Class of the Asiatic Researches, p. 127. In asecond paper in the same work, on some petrified shells in the Gawelghur range of trap Lieut.-Colonel Sykes on a portion of Dukhun, All Ghats. The Dukhun rises, by a succession of terraces or steps, very abruptly from the Konkun*. Its valleys and table-lands have a mean elevation above the sea of about 1800 feet. The Konkun is a long strip of land from thirty to fifty miles in breadth, lying between the Ghats and the sea; the mean elevation of this strip is less than 100 feet ; but it is bristled with isolated hills, or short ranges, some of which attain an elevation equalling that of the Ghats. Numerous shoulders or salient angles are thrown out from the Ghats from the western or Konkun side, and by means of these the ascent to Dukhun is effected ; with what difficulty, will be understood when I state that the military road of commu- nication between Bombay and Poona, up the Bore Ghat, rises nearly 600 feet ina mile. The western portion of my tract along the crest of the Ghats is ex- ceedingly strong : spurs of different lengths extend from the main range to the eastward and south-east, leaving many narrow tortuous valleys between them, some of which have the character of gigantic cracks or fissures ; other valleys, although occurring less frequently, when looked at from the neighbouring ranges, appear as flat and smooth as a billiard-table, even to the crest of the Ghats, but when traversed are found to be cut up by numerous narrow and deep ravinest. Stupendous scarps, fearful chasms, numerous waterfalls, dense forests, and perennial verdure, complete the majesty and romantic interest of the vicinity of the Ghats. As the spurs extend to the east and south-east they diminish in height, until they disappear on approaching the open plains in my eastern limits, between the Beema and Seena rivers. The area of the table-land on their summit often exceeds that of the valley between them; such is the case with the spur bordering the left bank of the Beema river for forty miles from its source, occupying, in fact, the whole country between the sources of the Beema and Goreh rivers. The spurs are rarely tabular for their whole length, but narrow occasionally into ridges capped with compact basalt, and subsequently expand into extensive table-lands. ‘The spur ori- ginating in the hill fort of Hurreechundurghur affords a good example. The fort is about eighteen miles in circumference: on the east it presents a salient mountains, extending for 165 miles along the left bank of the Tapty river, from its source to the city of Boorhanpoor, he describes the principal part of the range as formed of “ compact basalt “ very much resembling that of the Giant’s Causeway. It is found columnar in many places, and “ at Gawelghur it appears stratified ; the summits of several ravines presenting a continued stratum ** of many thousand yards in length.” —Physical Class of the Asiatic Researches, p. 189. * See Plate XXVIII. + The valley of the Malsej Ghat, for instance. VOL. 1V.—SECOND SERIES. 3H A12 Lieut.-Colonel Sykes on a portion of Dukhun. angle to the neighbouring mountain ; absolute contact, however, only com- mences at about 400 feet from the top of the scarp, leaving a gap and an ex- tremely narrow ridge, over which lies a difficult footpath of communication between the valley of the Malsej Ghat and that of the Mool river. The spur then widens ; some lateral ramifications shoot out, on one of which is situated the fort of Koonjurghur ; at the Brahmun Wareh pass it narrows considera- bly, but not into a ridge; it subsequently expands into the extensive and well-peopled table-land of Kanoor and Parneir, twenty-four miles long by twenty broad, having diminished in height, by a succession of steps, from 3894 feet in Hurreechundurghur to 2866 at Brahmun Wareh, 2474 at Par- neir, and 2133 on the terrace of Ahmednuggur. From Ahmednuggur the spur bends southward until it is finally lost in the neighbourhood of Sholapoor. It is, in fact, the margin of a great plateau, which has a mean elevation of about 300 feet above the valley of the Godavery river, and over which the rivers Goreh, Beema, Seena, &c., take their course. The basaltic caps of the ridges appear more or less columnar, from numerous vertical fissures ; the weathering of these exposed rocks produces pillars, spires, towers, houses, and other forms of works of art*. Another feature of these spurs is the occa- sional occurrence on their table-lands of small hummocks or conical hills with a truncated apex. Dr. Voysey{ mentions ‘‘ groups of flattened summits and “ isolated conoidal frustra” in the Gawelghur trap mountains. One of the longest of the spurs originates in the Ghats north-west of Sata- rah, and runs nearly east-south-east, about 110 miles, towards Punderpoor. The spur immediately south of Poona, on the ramifications of which are situated the formidable fortresses of Singhur (4162 feet), Poorundhur (4472 feet), and Wuzeerghur, adjoining Poorhundhur (at nearly the same ele- vation), has an extent of ninety-five miles. The accompanying section, Plate XXVIII. fig. 2. represents this spur. Valleys. Much having been said respecting valleys of excavation, I think it may be acceptable to offer a few observations on the valleys between the spurs. I shall describe only those that present the greatest contrasts to each other. Valley of the Mota River.—The valley of the Mota river, south of Poona, originating in a mass of hills on the edge of the Ghats, is so exceedingly narrow, that for some miles the bases of the opposite hills frequently touch each other, leaving, at intervals, little horizontal plots, of a pistol- shot in width, ‘These plots occur in terraces, on lower levels as they extend eastward. * See Plate XXVIII. fig. 1. and 2. on the Konkun; and Plate XXVII. fig. 1. + Physical Class, Asiatic Researches, p. 189. Lieut.-Colonel Syxes on a portion of Dukhun. 413 Vale of the Sa le valley of the Under river, north-west of Poona, presents a perfect contrast to the last. It is level for twenty miles, running east and west to the very edge of the Ghats ; and a person can stand at the head of the valley upon the brink of a searp le almost from the Konkun. Here, at the source of the river, it is nearly six miles wide. The river Under runs down the valley 150 feet below the level of the cultivated lands. Vale of the Baum.—The neighbouring valley of the Baum river, unlike that of the Under, originates about seven miles from the crest of the Ghats, at a spot where the mountain masses separate into two spurs. Hence it continues level for fourteen miles, gradually widening east- ward. The Baum river, like the Under, runs at a level of 150 feet below the cultivated lands ; these lands, in fact, being upon one terrace, the river upon a second and lower terrace. Vale of the Beema.—The next valley on the north is that of the Beemariver. The river rises on the elevated table-land above the Ghats, at 3090 feet, and within the first few miles it tumbles over several terraces. The valley, for eighteen miles, is occasionally as narrow as that of the Mota river. Vale of the Goreh.—Next on the north occurs the valley of the Goreh river, which, from the source of the river to Munchur, (twenty-nine miles,) is exceedingly narrow and tortuous. Here it expands into the broad horizontal plain of Kowta, ten miles wide. Vale of the Malsej Ghat.—In conclusion, as a contrast to the first part of the Goreh valley, I must mention the valley of the Malsej Ghat, on the south of the Dukhun-base of the fort of Hur- reechundurghur. It is several miles wide, and literally as level, even to the brink of the Ghats, as if smoothed by art. Many of the valleys of the Ghats, particularly that of the Mool river, from the continued scarped character of the marginal mountains, and the flatness of the bottom for miles in extent, look like fosses to a Titan’s fortress. If all these valleys be valleys of excavation, the present rivers could scarcely produce such, were we to suppose their powers of attrition in operation from the origin of things even to the end of time! Those of a fissure-like character might have resulted from the upheaving of the beds of trap from below the sea, and the consequent probable fracture of the surface ; but the same explanation will not apply to those valleys associated with the preceding, broad, flat, and margined by scarped mountains, which valleys are as wide at their origin at the crest of the Ghats, and at the sources of the rivers which run through them, as in any part of their length. Terraces. As the rise from the Konkun to the Dukhun is by terraces, so the declination of the country eastward from the Ghats is by terraces; but these occur at much longer intervals, are much lower, particularly in the eastern parts, and escape the eye of the casual observer. In the neighbourhood of Munchur, on the Goreh river, there are five terraces rising above each other from the east to the west, so distinctly marked, that the parallelism of their planes, to each other and to the horizon, gives them the appearance of being artificial. An artificial character also pervades the form of many insulated hills: some of which viewed laterally, appear to have an extensive tabie-land on the summit, 3H 2 414 Lieut.-Colonel Sykes on a portion of Dukhun. but seen endways look like truncated cones. Conoidal frustra in the Gawel- gurh range have been already noticed. Other insulated hills are triangular in their superficial planes, as the forts of Teekoneh (three-cornered) and Loghur. Escarpments. Stupendous escarpments are occasionally met with in the Ghats. In these instances the numerous strata, instead of being arranged in steps, form a con- tinuous wall. At the Ahopeh pass, at the source of the Goreh river, the wall or scarp is fully 1500 feet high* ; indeed, on the north-west face of the hill fort of Hurreechundurghur, the escarpment can scarcely be less than double that height. On the other hand, the steps are sometimes effaced, and a hill has a rapid slope. This criginates in a succession of beds of the softer amyg- daloids, without any basaltic interstratification ; their superior angles disinte- grate, and a slope results. But most usually three or four beds of amygdaloid are found between two strata of compact basalt; the former disintegrates, leaving a slope, which is not unfrequently covered with forest trees, forming a picturesque belt: the basaltic scarp remains entire, or it may be partially buried by the debris from the amygdaloids above; but its great thickness usually preserves it from obliteration, and it rises from the wood below with majestic effect, its black front being finely contrasted with the rich and lively green of its sylvan associate. It is these strata, arranged in slopes and scarps repeated three or four times, and so commonly met with in insulated and other mountains in Dukhun, that constitute the amazing strength of the hill forts of the country, leaving a succession of natural walls encircling a mountain. This feature did not escape the observation of Captain Dangerfield in Malwa, who says, “From the great difference in the resistance made to decomposition by “these trap and amygdaloid beds, their exposed ends acquire a very distinct “ degree of inclination and character ; the amygdaloid forming a great slope, “and affording a loose mould covered with vegetation, the trap retaining its “ original perpendicularity and dark bareness f.”’ In the alternation of the strata there does not appear to be any uniformity ; but the general level, thickness, and extent of a stratum are preserved, as in sedimentary rocks, on both sides of a valley ; the basalt and hardest amyg- daloids being traceable for miles in the parallel spurs or ranges; but the im- bedded minerals, and even the texture, vary in very short distances. Columnar Basalt. A great geological feature of Dukhun is the occurrence of columnar basalt. * Plate XXVIII. fig. 1. ¢ Malcolm’s Central India, Appendix, p. 322. Lieut.-Colonel Sykes on a portion of Dukhun. Ald The basalts and hardest amygdaloids run so much into each other that the line of separation is not always readily distinguishable, excepting of course the lines of horizontal stratification. I observed the prismatic disposition more marked and perfect in the basalt strata than in the amygdaloids, and the more or less perfect development of determinate forms was dependent on the com- pactness and limited constituents of the rocks. Basalts and amygdaloids, how- ever compact, with many imbedded matters, rarely formed columns. Perfect columns were generally small, of four, five, or six sides; but the prismatic structure sometimes manifested itself in basaltic and amygdaloidal columns many feet in diameter. A bare mention of the places where they occur will testify to their extended localities. On the low table-land of Kurdah, near Serroor, between sixty and seventy miles east from the Ghats, columnar basalt occupies an area of many square miles. Small columns are seen in most of the slopes of the very narrow sinuous valleys of the flanks of the platform, and frequently the tops or terminal planes of columns are observed on the table-land forming a pavement. The perfect columns in the flanks are generally small, four, five, or six-sided, and rest on a stratum of basalt or amygdaloid. In some spots the columns are articulated, in others not. In amass of columns in the face of the table-land towards Serroor the columns are of different lengths, but spring from the same level. More articulations having been washed from the outer columns than from the inner by monsoon torrents dashing over them, a pretty flight of steps remains. The columns of this table- land are for the most part erect, but sometimes stand at various angles to the horizon, usually at 45°, In one instance, near the village of Kurdah, they lean from the east and west, towards a central upright mass: these are about fourteen feet in length, and are not articulated. In a mass of columns facing the west, and two miles south of the cavalry lines at Serroor, some are bent and not articulated ; they are nevertheless associated with straight columns, which are articulated. At Karkullah, thirty miles north-west of Poona, between Tellegaon and Loghur, a hill has been scarped for the great military road. Very numerous small columns occur in the escarpment, and they lie piled upon each other in a horizontal position ; the only instance of the kind within my knowledge in Dukhun. Two or three hundred yards west of the village of Yewtee Purgunnah Kurdeh, in the rocky banks ofa rivulet, imperfect columns are seen. On the right bank they are so marked, as to have excited the attention of the natives (an unusual event) ; and they are daubed with red lead, in the manner of Hindoo deities, and venerated. At Kothool, twenty-two miles south of Ahmednuggur, there is a thick stratum of close-grained gray homogeneous basalt in the face of the hill on which is seated the temple of Kundobah. Ver- tical and horizontal fissures are seen in the lateral plane or exposed edge of this stratum, but they are so far from each other as to leave huge blocks between them, giving the appearance of the superstratum of the hill being supported by massive articulated pilasters. Parts of the exposed edge are detached from its mass, leaving rude columns four or five feet in diameter, eight or ten high, and composed of three or four weighty stones disposed to assume geometrical forms. In the water courses near Kurroos Turruf Ranjungaon, columns are observable. The basalt is bluish gray, compact, has a vitreous hue, and sharp fracture. The columns occur very abundantly in the slope of the hills, on either side of a very narrow valley running westward from the village of Ankoolner, Ahmednuggur Collectorate. They are five- or six-sided, articulated, and from a foot to two feet and a half in diameter, and of various lengths; the lateral planes perfect, but in 416 Lieut.-Colonel Sykes on a portion of Dukhun. some instances the sharpness of the angles has been affected by weathering. The texture is close-grained, colour almost black, and they affect the needle. At Jehoor, near the source of the Seena river, in an insulated hill, an obscure columnar disposi- tion is met with in a rock, in which in other places I had not seen the slightest trace of it. A stratum of red, cellular, amygdaloid fifteen feet thick has subcolumns in its exposed edges eight or ten feet indiameter. In the banks of a water-course running into the Hunga river, half a mile east of Parneir, on the elevated table-land between the cities of Ahmednuggur and Joonur, basaltic co- lumns are very numerous ; they are five or six feet high, not articulated, and are not quite perpen- dicular. This formation is evidently extensive, as the ends of columns, chiefly pentangular, appear in the bed of the water-course for some distance, forming a pavement of geometrical slabs. The ends of columns of different lengths also appear in the southern bank at intervals, forming flights of steps. The basalt of which these columns are composed is very close-grained, almost black, with shining specks of a metallic lustre. The rocky banks of the Kokree river at Jambut, in the plain of Joonur, exhibit a strong inclination to a large columnar structure. In the hill fort of Singhur, at an elevation of 4162 feet, at the western end of the fort, there is a sheet of rock which has the appearance of a pavement of pentangular slabs. The slabs are no doubt the terminal planes of basaltic columns. The same is observed in the hill fort of Hurreechundurghur, about seventy miles north of Singhur; also in the bed of a water-course one mile north-east of Bar- lonee, near the fortress of Purrunda, 112 miles east-south-east of Singhur ; and, lastly, in the bed of the Mool river at Gorgaon, Poona Collectorate. These pavements extend to Malwa, as Captain Dangerfield mentions their occurrence in the beds 2 lia dudigdieg ta of the Chumbul and Nerbuddah (Nermada) ri- i TT if vers*. The other localities of basaltic columns, or are a marked disposition to this structure, were in a well at Kumlepoor, between the fortress of Pur- rundaand Barlonee, near the left bank of the Seena river ; at Kheir Turruf Rasseen, in the face of a headland, abutting on the Beema river, on which the town stands; in the ascent to the temple of Boleshwur Turruf Sandus, Poona Collectorate ; and, finally, in the scarps of a mountain running down into the Konkun, and seen from the Naneh Ghat, about three miles distant. Here the Giant’s Causeway in Ireland is brought to mind; but the scale of the mountain is infinitely more magnifi- cent, being fully 4000 feet high. There is a dou- ble row of columns ; but from their inaccessible situation, I could only examine them through my telescope, and cannot testify, therefore, to their perfect development; but the accompanyingsketch will give a just idea of their appearance to me, Captain Dangerfield only once speaks of columns. They lie about a mile from the Ner- buddah (Nermada), between Mundleysir and Mhysir, at 696 feet above the sea: they are either * Malcolm’s Central India, Appendix, pp. 329, 330. Lieut.-Colonel Syxts on a portion of Dukhun. Al7 vertical or highly inclined. General Hardwick has published a lithographic sketch of them*. I have already stated that Dr. Voysey found columnar basalt in many places in the Gawelghur range. Schistose Structure. Following the preceding formation, I may mention, that in some few places a schistose structure was met with ; but its extent was limited to a few yards, the lamelle were vertical, from an inch to three inches in thickness, being perfect tables, with parallel bounding planes. The rock in which this struc- ture occurs, is a simple, indurated, gray clay, which flies into fragments under slight blows from the hammer. At Dytneh near Serroor some very perfect specimens have led the inhabitants to connect mystic influences with so arti- ficial a development of inorganic matter. The spot is daubed with oil and red lead, and venerated. Basalt en boules. Another characteristic feature is the general diffusion of those rounded or oval masses of compact basalt, with concentric layers like the coats of an onion, which the French geologists denominate ‘ Basalt en boules’”’, and ourselves, nodular basalt. : These concretions are usually found at the base of hills, buried in the debris from the decom- posing strata; but in the Konkun, between Choke and Campolee, (the latter at the foot of the Bore Ghat,) two villages on the high road between Bombay and Poona, I met with them lying on the surface over a considerable area. They occur in a similar manner on the table-land of the ball-practice hill at Poona. At Koothool (already mentioned), in the slope of the hill, and in the debris at its base, and along the edge of the table-land near Paubul, they are abundant ; but the finest specimens are seen near the village of Karkullah, thirty miles north-west of Poona, associated with horizontal basaltic columns. The hill has been cut away, to form the great military road. In making the escarpment the balls were met with, and it being impossible to cut through the nuclei in vertical sections, it was either necessary to leave them projecting or to remove them altogether: in the latter case cavities remained equal to the hemispheres of the nuclei; and the vertical sections display from ten to fifteen concentric layers of friable gray stone, which in some instances I have found to affect the needle. I compared specimens of the nuclei; with a mass brought by me from the Solfatara at Naples, and found them quite similar in aspect, colour. hardness, and great weight. This formation excited the attention of those gentlemen who have visited the northern and eastern parts of the great trap regiont; but Dr. Voysey was quite mis- * Malcolm’s Central India, Appendix, p. 323. + Dr. Voysey says, ‘The nodular wacken or basalt is one of the most common forms of trap ** in the extensive districts composed of the rocks of the family south of the Nermada (Nerbuddah) “river. It occurs perpetually in the extensive and lofty range of mountains, (the Gawalghur) “ situated between the Purna and Tapti rivers, and appears to form their principal mass. It is “ found equally abundant throughout the whole of Berar, part of the provinces of Hyderabad, Beder “ and Sholapoor, and appears to form the basis of the great western range of trap hills which separate “ the Konkun from the interior of the Dukhun.”—Physical Class, Asiatic Researches, pp. 126, 189. 418 Lieut.-Colonel Sykes on a portion of Dukhun. taken in supposing it formed the basis of the Western Ghats. Captain Coulthard speaks of it in Sagar*, Major Franklin also noticed it in the trap of Sagar, in lat. 23° 51’, and long. 78° 44’, at 1933 feet above the sea, as “ frequently globular ; the nuclei of the decaying masses, varying in “ size from an egg toa large bombshell, and their decomposing concentric lamellze being generally “ very thin, and often very numerous” f. Dykes. I now pass to the basaltic dykes, several of which came under my notice in different parts of the country. They are all vertical, and I did not observe that they occasioned any disturbance or dislocation in the strata of basalt and amygdaloid, through which they passed. Two dykes run obliquely across the valley of Karleh, (35 miles north-west of Poona), and intersect each other: they are about four feet thick and cut amygdaloidal strata. A prismatic disposition is generally observable in the fracture, and from one of them I obtained a square prism, which lay at right angles to the walls of the dyke. The texture is compact, The military road running through this valley and down the Bore Ghat to Panwell, is frequently crossed by ridges which I presume to be the outcrops of dykes. A dyke is seen on the southern slope of an insulated hill, near the villages of Bosree and Digghee, 74 miles north of Poona}. It is about four feet thick, has a transverse prismatic fracture, is compact, and runs from the bottom to the top of the hill; but it is not discoverable in the northern slope. It is visible from the can- tonments at Poona. A similar dyke occurs in the hill at Ombreh, twenty miles north-north- west of Poona. But the most remarkable dyke runs vertically, from east to west, through the hill fort of Hurreechundurghur. It is first seen, of a thickness of six or seven feet, in the ascent of the mountain on the south-east from Keereshwur, about 400 feet below the crest of the scarp. The path of ascent into the fort is intersected by it, and its prismatic fracture, at right angles to its planes, offers a few available steps in the ascent. It is traceable for about 300 feet in perpen- dicular height. On the top of the mountain, within the fort, about a mile to the westward, it is discoverable at intervals, cutting through basaltic and amygdaloidal strata. J could not ascertain whether or not it appears in the western scarp of the mountain, the point to which it directs its course being wholly inaccessible. The gentlemen whose geological memoirs I have quoted, rarely advert to the subject of trap dykes, and their notices are very brief. Capt. Dangerfield says, «'The trap of the southern boundary of Malwa is much intersected by verti- “ cal veins of quartz, or narrow seams of a more compact heavy basalt, which ‘ appears to radiate from centres§.”’ Beyond the continuous trap region of the peninsula, Dr. Voysey notices a basaltic vein in sienite, near the Cavary river * « The base of the hills is invariably broader than the summit; and if the sides of a hill are ‘“‘ smooth and even, balled trap, often a concentric lamellar variety will be the principal component “‘ matter, decomposing and decomposed into a predominating workable clay, still showing the ‘« narallel converging layers.” —Physical Class, Asiatic Researches, p. 78. + Physical Class, Asiatic Researches, p. 30. } See Plate XXVIII. fig. 1. § Malcolm’s Central India, Appendix, p. 330, Lieut.-Colonel Sykes on a portion of Dukhun. AI9 at Seringapatam, which must have been propelled upwards, as it broke through an oblique seam of hornblende in the sienite, and carried the pieces up above the level of the hornblende vein*. “On the eastern coast,” Mr, Calder says, “from Condapilli northward, the granite is often penetrated “and apparently heaved up by injected veins or masses of trap, and dykes of “ greenstone ft.” Ferruginous Clay. The next distinctive feature is the occurrence of strata of red ochreous rock, in fact, Mac Culloch’s ferruginous clay underlying thick strata of basalt or amygdaloid, precisely as is seen to be the case in the Giant’s Causeway in Ireland. It passes through every variety of texture, from pulverulent, friable, and indurated, to compact earthy jasper. The stratum is from an inch in thickness to many feet. The rock makes a red streak on paper, with the exception of the very indurated kinds, and does not affect the needle. It is pulverulent near the basaltic columns at Serroor, friable under sub-columnar red amygdaloid, near the source of the Seena river, indurated under basalt at Kothool. Although hard, it is here so cellular as to have the appearance of sponge, and reduced to powder, looks like brickdust. In the scarps of the hill fort of Hurreechundurghur and a mountain near Joonur in which are excavated numerous Boodh cave temples, it is found compact and homogeneous, and is, in fact, an earthy jasper. In these localities it lies under from 300 to 600 feet of basalt. In the former locality it is about three feet thick, in the latter one foot. At Nandoor, north-north-west of Ahmednuggur, in the valley of the Godavery river, it is found as a porphyritic stratum many feet in thickness, and is used as a building stone. The imbedded matter consists of very minute crystals of lime. At Wangee, lying nearly in the latitude of Barlonee, but differing 18 miles in longitude, and at Barlonee it occurs as an earth: as both places lie on the same level, I have no doubt the stratum is continuous between them. It occurs abundantly in the Ghats, frequently discolouring the rivulets, and giving a ferruginous character to the soil over a considerable area. When thin, and under heavy beds of basalt or amygdaloid, the exposed edge of the stratum projects, is rounded, and double the thickness of the stratum itself; as if it had once been in a tenacious fluid state, and squeezed out by the superincumbent basalt. Such is the case at Jehoor, and an illustrative specimen accompanies this paper. Pulverulent Limestone. Limestone is met with, in the Dukhun, only in three states: pulverulent, nodular, and crystalline. The first occurs in thin seams on the banks of rivers and water-courses and at the base of hills in debris. The seams are from an * Physical Class, Asiatic Researches, part i. p. 22, ¢ Ibid., part i. p. 10. VOL. IV.— SECOND SERIES, 31 420 Lieut.-Colonel Sykes on a portion of Dukhun. inch to three feet in thickness, covered by a few feet of black earth. Some- times in whiteness it resembles pounded chalk, and is then used by children to smear their writing boards. In this state it ocecurs at Jehoor and Islampoor near Ahmednuggur. At Kurkumb and at Salseh, ten miles south of the fortress of Kurmaleh, it is met with under black earth in unusually thick strata, and of a peculiar whiteness. Major Franklin notices “ a stratum of earthy limestone, white as chalk, at Sagar, occurring under a stratum of amorphous trap *.” Nodular Limestone. The nodular limestone, which is the well-known kunkur f of India, (kunkur being a native word for nodule,) occurs, like the preceding, disseminated or diffused in the soil, and also on the surface. I have never seen the nodules of a regular crystalline form. They vary in size from a marble to a twelve- pound shot, and many of them are exceedingly irregular in shape, particularly those dug from the banks of rivers. ‘They are sometimes obscurely lenticular. They are so abundant in certain localities that they appear as if showered upon the earth, and disguise its colour. Dr. Buchanan mentions the same in Rajmahl. When upon black soil, they are usually minute and tolerably uniform in size: on other soils their form is variable. In the Ghats neither pulverulent nor nodular lime is met with. It is unnecessary to particularize the localities of the nodular kind, as it is of common occurrence eastward from the hilly tracts of the Ghats, and is the only source of lime for mortar, a class of persons making a livelihood by collecting the larger nodules. When carefully burnt, they make an excellent cement. Captain Dangerfield de- scribes ‘ the occurrence (in Malwa) in some parts, particularly near the bottom of the small hills and banks of the rivulets, of a thin bed of loose marl or coarse earthy limestonet”’. Captain Coulthard says, ‘“‘ In Sagar a white patch of this limestone moulder- “‘ ing by the weather is the source from whence comes the particles of kunkur, «mixed with the black basaltic earth of the neighbouring valley, in such pro- “ portion as to add increased fertility to it; and if a rivulet meanders through “ that valley (and such is generally the fact), patches made up of aggregated “ particles of the same, will here and there be found ; and this it is which the “« native families pick out and work into lime §”. Captain Coulthard refers the origin of the nodules to limestone rock underlying basaltic strata, but I * Physical Class, Asiatic Researches, parti. p. 30. + The Mahratta word is not spelt with an “a.” + Malcolm’s Central India, p. 328. § “Trap of the Sagar District,” Physical Class, Asiatic Researches, p. 60, Lieut.-Colonel Sykes on a portion of Dukhun. AQ] cannot trace them to such a source, not having seen strata of compact lime- stone, properly so called, in the Dukhun. The only specimen of compact limestone met with by me was in the bed of the Beema river near Pundur- poor. It was an insulated, amorphous, gray mass, four or five feet in dia- meter. I looked upon it as an aggregation of the pulverulent particles of the lime disseminated in the neighbouring banks. A specimen of it ac- companies this paper. Crystalline Limestone. Lime in a crystalline state occurs only as an imbedded mineral in the amygdaloidal strata, in quartz geodes, and in the nucleus or compact part of masses of mesotype or stilbite. It is rare compared with the preceding varieties. Loose Stones. Another feature of Dukhun is the occurrence of immense quantities of loose basalt stones, as if showered upon the land; also masses of rock heaped and piled into mounds as if by the labour of man. Their partial distribution is not less remarkable than their abundance. For the most part, the stones have a disposition to a geometrical form, and it is by no means rare to meet with prisms of three or four sides and cubes almost perfect: stones with one or two perfect planes are very common. Their texture is close-grained and the colour verging to black. At Dehwuree, Hungawaree, Behloondee, Kothool, and Dytneh in the Ahmednuggur Collectorate, they are very abundant. At the last place they cover fields several acres in extent, so thickly that the black fertile soil on which they rest is not discoverable: they vary from an ounce to several pounds in weight. Amongst these I picked up a perfect square prism. In neighbouring fields, most unaccountably, there is not a stone to be seen: patches of sheet rock occur in their vicinity. Other localities are the top of the Neem Durra Ghat near Ahmednuggur; the junction of the Beema and Seena rivers below Mundroop; right bank of the Seena at Kurmaleh; between Kurjut and Meerujgaon; and generally it may be stated that the precipitous slopes of the low table-lands of the Desh (open or flat country) are very strong and rocky. For ten miles between Jeetee and Soagaon, Ahmednuggur Collectorate, the fields, and even the road, are so thickly strewn with large basalt stones as to render cultivation difficult and travelling penible. Rocky Heaps. The singular heaps of rocks and stones above noticed occur at Kanoor, Patus, Kheir, between Kurjut and Meerujgaon, and at other places in the Desh, but not in the Mawals, or hilly tracts of the Ghats. The heaps are from twenty to seventy feet in diameter, and the same in height: when com- posed of rocky masses without small stones, blocks of three or four feet in dia- 312 422 Lieut.-Colonel Sykes on a portion of Dukhun. meter and with a disposition to determinate forms, are piled upon each other, constituting rude pillars. In certain parts of the country from fifty to sixty of these heaps are seen within the area of a couple of square miles, and it ex- cites surprise that the intermediate ground is destitute of stones. Sheets of Rock. Mention must not be omitted of the constant recurrence of sheets of rock of considerable extent at the surface, and totally destitute of soil: this is par- ticularly the case in the Mawals, or hilly tracts along the Ghats, They abound with narrow vertical veins of quartz and chalcedony. When of suffi- cient thickness, the vein splits in the centre parallel to the surface of its walls, the interior being drusy with quartz crystals: the walls consist of layers of chalcedony, cachalong, hornstone, and semi-opal. These veins supply the majority of the siliceous minerals so abundantly strewed over Dukhun. The localities where the sheets of rocks particularly struck me were Lakungaon, on the plain of Joonur, and generally in the valley of the Goreh river; at Kothool, Pergunneh Kurdeh; at Kheir and Raseen; in the hill fort of Hurreechundurghur ; most markedly between Kooldurrun and Pairgaon on the Beema river. At Aklapoor, on the Mool river, they were very extensive ; and at Angur, Mohol, Kurjut, and Patkool. Generally in the eastern and south-eastern parts of my tract, much decomposing amygdaloid is found at the surface of the low table-lands or terraces, which, in favourable monsoons, is equal to the support of Jowaree*; but a small deficiency in the rains occasions the destruction of the crop. Structure and Mineral Composition of the Trap Rocks. The structure and mineral composition of the trap rocks in Dukhun vary exceedingly in short distances, even in the same stratum ; nevertheless, the predominant character does not disappear, although the basalt in a con- tinuous bed may pass several times from close-grained, compact, and almost black, to gray, amygdaloidal, and externally decomposing. The same ob- servation applies to the amygdaloids. A variety of compact basalt, of an intense green colour, is susceptible of a brilliant polish, and rivals the cele- brated Egyptian kind. It is of great weight and remarkable hardness: the natives use it to work into idols for their temples, pedestals to the wooden columns in their mansions, and slabs for inscriptions. The bulls of the size of life, always placed before the temples of Mahadeo, are cut out of this variety at Raseen, Wurwund, and the renowned Boleshwur. Some of the pedestals in the gateway of the Mankeswur palace at Teimboornee look like * Andropogon Sorghum. — Lieut.-Colonel Syxes on a portion of Dukhun. 423 mirrors. In the temple at Pooluj south of Punderpoor, there is a slab six or seven feet long and 23 broad, covered with an inscription in the Kanree language ; and in Punderpoor the streets are paved apparently with the same basalt. At Jehoor and near Ahmednuggur is found a compact kind like the last, but not so heavy. It has a crystalline character and sharp frac- ture, and has angular siliceous pebbles imbedded : an occasional pebble is loose in its cell. In the Happy Valley near Ahmednuggur the basalt is com- pact and smooth, with reddish flat transparent crystals imbedded. It opposes a feeble resistance to the hammer, and flies into fragments, some of which have right angles. The basalt, even of the true columns, is not of a uniform texture in different localities : at times it is blackish or gray, and very small, granular or compact ; at others, earthy and ferruginous, particularly exter- nally. The basis of the amygdaloids is clay, with more or less hornblende disseminated : they embrace the cellular, porphyritic, hard, friable, and de- composing. I endeavoured to class them“agreeably to the prevalence of quartz, chalcedony, lime, mesotype, or stilbite, as imbedded minerals, but found the method of very limited application. Sometimes one mineral only is imbedded, occasionally two, and often the whole. In Hurreechundurghur quartz amygdaloid prevails: at Aklapoor on the Mool river it is characterized by mesotype, that mineral being imbedded in large masses, and the radii (six or seven inches) are the longest I have seen. At Nandoor it is porphyritic with minute crystalline specks of lime: near Ahmednuggur is seen a cellular, indeed spongiform kind, which is hard, and the cells are empty. A small cellular and pisiform variety is found in the wonderful cave temples of Ellora, and some of the sculptured figures appear as if marked by the smallpox. This observation is partially applicable to the Boodh and Hindoo cave temples of Elephanta, Salsette, Karleh, Joonur, the Naneh Ghat, and the Adjunteh Ghat; all of which are excavated in basaltic or amygdaloidal strata. The stilbite or Heulandite amygdaloid is of very common occurrence ; but the most prevalent kind is that in which all the minerals noticed above are associated. The stone usually selected for building is of various shades of gray or bluish gray ; has hornblende dis- seminated in very small crystals; works much easier than some of the com- pacter basalts, but takes a good polish. The entire temples of Koorul and Boleshwur, with their innumerable alto-relievo figures and laboured orna- ments, are built of this variety of trap, which is, in fact, a greenstone, although less crystalline than the European rock. There is a variety selected carelessly, also used in building, which has the structure and nearly the external characters of the last, but which, in weathering, exfoliates, and the 424 Lieut.-Colonel SyxEs on a portion of Dukhun. buildings fall to ruin; such is the case with the great temple in Hurree- chundurghur. I must not omit mention of two remarkable rocks which, as far as my reading extends, have not been noticed by authors on European geology. The first is an amygdaloid in which compact stilbite is imbedded in a ver- micular form. One of its localities is the insulated hill on which stands the temple of Parwuttee in the city of Poona* ; and it is met with in many other places. Captain Dangerfield observed the same peculiar stratum near Sagar. He says, “There occurs an amygdaloidal or porphyritic rock con- * sisting of a compact basis of wacké, in which are imbedded in great abun- “dance small globular or uniform masses, but more usually long curved cy- “ lindrical or vermiform crystals of zeolite +.” The other rock occurs as a thick stratum of amygdaloid at the elevation of A000 feet, in the hill forts of Hurreechundurghur and Poorundhur; and in the bed of the Goreh river at #800 feet, near Serroor. The matrix resem- bles that of the other amygdaloids, but the mineral imbedded is a glassy felspar in tables resembling Cleavelandite, crossing each other at various angles, and so abundant as to occupy a moiety of the mass. I have only remarked it in the above localities, and it does not appear to have come under the notice of the gentlemen I have so often quoted in other parts of the peninsula. Minerals. Minerals are not uniformly dispersed in Dukhun. In one part quartz pre- dominates, in another chalcedony ; and these are more or less associated with jaspers, agates, hornstones, heliotrope, and semi-opal or cachalong. In other places particular members of the zeolite family prevail, nearly to the exclusion of the siliceous class ; and elsewhere there is a diminution of minerals amount- ing almost to privation. Amethyst quariz is rare in Dukhun ; when met with it constitutes the crystal, lining the interior of geodes of agate. I have not seen it in veins. Pseudomorphous quartz is common; the most frequent impression is that of rhomb spar. Lime occurs only in three crystalline forms : rhomb, dog-tooth, and the dodecahedron. ‘The first is found on the surface, and imbedded in masses of quartz and compact mesotype; the two latter forms are associated with ichthyophthalmite in cavities in the amygdaloid strata tf. * See Plate XXVIII. fig. 2., near to the city of Poona. + Central India, p. 328. { That comparatively rare European mineral, ichthyophthalmite, is most abundant and of great beauty in the neighbourhood of Poona. Lieut.-Colonel Syxrs on a portion of Dukhun. A25 The following are a few of the mineral localities : At Kothool, south of Ahmednuggur, the numerous quartz and chalcedony veins cover the country with agates, colourless quartz-crystals, and chalcedony; some of the specimens are fully a foot thick, including both walls of the vein. Here are met with some few crystals of calca- reous spar inclosed in quartz. At Ahmednuggur, to the above siliceous minerals, some members of the zeolite family are to be added, principally stilbite. At Nandoor, on the plain of the Goda- very river, the zeolites disappear, and the siliceous minerals are limited in number. On the con- trary, at Jamgaon, eighteen miles west of Ahmednuggur, on the upper terrace or plateau, in ad- dition to all the minerals enumerated, bits of yellow and red jasper and heliotrope occur. As- cending the Mool river from Nandoor, at Aklapoor, great masses of mesotype, with radii several inches long, are found imbedded in friable amygdaloid. North of Aklapoor, at Gorgaon, a new mineral occurs in a mass two feet in diameter. Its depth I do not know, as it lay partly buried in the amygdaloid bed of the river: its colour green, and breaking into rhombs. Gorgaon is the only locality known to me of this mineral. Its measurements are those of calcareous spar, but the specific gravity is less. It is stated to be coloured by green earth. It is interesting from being unknown in the cabinets in England. A few miles further up the Mool river, at the village of Chas, in the shoulder of a hill formed of numerous thin horizontal beds of decomposing amygdaloid, many specimens of cloudy calca- reous spar, imbedded in stilbite, are found, and the siliceous minerals are rare. Ascending to the source of the river the same scarcity prevails. Three miles south-south-west of Chas, at Brah- munwareh, great masses of stilbite, of the radiating foliate kind, are imbedded in hard amygdaloid. In the hill fort of Hurreechundurghur, although siliceous minerals are not abundant, crystallized quartz of various colours is seen, a feature not characterizing the Desh or open country. South of Ahmednuggur, as far as Soagaon on the Beema river, and Meerujgaon on the Seena river, the Ahmednuggur minerals prevail; hence descending the Beema to its junction with the Seena, a gradual diminution takes place, and at the junction they almost disappear; returning north, at Ashtee, between Kurkumb and Mohol, a few are met with. At Oondurgaon, and up both banks of the Seena river to Purrunda, numerous and very fine specimens of milk opal, with a flame- coloured tinge in transmitted light, are found on the surface; and this is the only locality where I met with opal as a distinct mineral; and here the members of the zeolite family are very rare. At Tudwull, between Oondurgaon and Barlonee occur the only specimens of black calcareous spar seen by me in Dukhun; it is associated with transparent calcareous spar. In excavating wells in the cantonments at Poona, splendid specimens of ichthyophthalmite were brought to light; and generally in the bed of the river Mota-Mola and the neighbourhood, fine specimens of heliotrope and coloured quartz occur. The other minerals are nadelstein, analcime, chabasite, and laumo- nite. Captain Dangerfield’s details prove that the minerals of Malwa are identical with those of Dukhun. Natural Salts. Only two kinds of natural salt came under my notice, namely, muriate and carbonate of soda. With respect to the former, many of the wells at Ahmednuggur are brackish; and there is a rivulet running into the Seena river about two miles north-west of the city, which has its source a few miles distant, called the Salt Brook. It passes over a saliferous soil; and in its dry bed, or 426 Lieut.-Colonel Syxes on a portion of Dukhun. on insulated stones standing in its stream, are incrustations of common salt intimately mixed with carbonate of lime. No use is made of this salt. The saline impregnation of the soil extends to some distance west and north-west of Ahmednuggur, as I found a handsome well at Kurjooneh, eight miles distant, filled with water so brackish as not to be available for domestic use. At Wur- gaon, between Kurjut and Pairgaon, a peculiar hoary appearance of a patch of ground in the midst of withered grass, led me to examine it. The whiteness was occasioned by lime in minute particles, mixed with a little muriate of soda. The third locality of common salt was in the bed of a rivulet at Koond Mawlee, near the falls on the Kookree river, between Serroor and Kowta. A little common salt, with a trace of carbo- nate of soda, appeared, incrusting the rocky bed for a few feet near the water line. I did not observe common salt elsewhere. My attention was first directed to carbonate of soda at Serroor, by observing washermen digging for earth in the banks of a rivulet ; learning that they used it to wash their clothes, I obtained a quantity; lixiviated the earth, boiled down the lixivium, and on cooling obtained a large crop of crystals, which the usual tests indicated to be carbonate of soda. I only met with one other bed, although I have no doubt they are numerous. At Kalbar Lonee, twelve miles east of Poona and two miles south of the Mota-Mola river, within an area of 200 yards, a constant moisture and partial absence of vegetation is observed. An efflorescent matter appears on the surface every morning, which is carefully swept up and sold to washermen; it is carbonate of soda. The occurrence of salts in the trap formation did not escape Captain Dangerfield’s notice. He states that ‘“ the banks of the Nerbuddeh (Nermada) near Mundleysir, consist of an upper thin bed of vegetable mould; a central bed, chiefly of indurated marle, strongly impregnated with mu- riate of soda; and a lower bed, of a reddish hue, with much carbonate of soda, In the dry season these salts form a thick efflorescence on the surface of the bank*.” Saltpetre is manufactured in Dukhun, not from nitrated soils, but from the scrapings of old walls. I have also seen specimens of muriate of ammonia obtained by the brick and tile makers in burning dung, stable and other refuse matters in their kilns, Ores. No other ore than that of iron is found in Dukhun. It is only worked, to my knowledge, at Mahabuleshwur, at the source of the Krishna river. It occurs as a nodular hematite, associated, I understand (for I have not been at the spot myself), with laterite. This ore produces the celebrated Wootz steel. Organic Remains. I did not meet with organic remains of any kind whatever. Captain Coult- hardf in Sagar, Major Franklin in Bundelkand, and Captain Dangerfield in Malwa, were equally unsuccessful. Dr. Voysey, indeed, mentions a bed of freshwater shells in a stratum of indurated clay near the Tapty river in the Gawelghur hills ; also at Medconta, 2000 feet above the sea, on trap; but these may have been recent, as he does not say to the contrary+. Mr. Calder, in his general observations on the Geology of India§, says, “ But hitherto the * Malcolm’s Central India, p. 324. t Physical Class, Asiatic Researches, p. 81. } Physical Class, Asiatic Researches, p. 194, § Ibid., p. 16. Lieut.-Colonel Sykrs on a portion of Dukhun. A27 most striking phenomenon in Indian geology is the almost total absence of organic remains in the stratified rocks and in the diluvial soil.” As this must have been written with a knowledge of Dr. Voysey’s paper, it being in the same volume with his own, it is probable he considers the shells recent. Thermal Springs. Thermal springs do not exist in Dukhun within my limits; but there are three distant localities in the Konkun below the Ghats, where hot water gushes up from numerous crevices in trap rocks over an extensive surface. The first is at Vizrabhaee, forty-eight miles north of Bombay, where the principal springs are in the bed of a river, and in the monsoon are consequently lost in the swollen stream; but in tra- versing the jungle in the vicinity I have met with detached pools of hot water, which are unaffected by the rains; their temperature is very high. The second locality is that mentioned by the late Dr. White, of the Bombay army. The hot wells are called Devakl Unei, and are fifty miles south- east from Surat*, at the foot of some hills; the temperature in the different springs ranges from 111° to 120° Fahr. They are spoken of as being in the vicinity of Anaval and Veval, but as these places, agreeably to the map of India, are only thirty miles from Surat, there is evidently some mistake with regard to the distance. The third locality is at Mahr, on the Bancoot or Fort Vic- toria river, about seventy-five miles south of Bombay. I know of these springs only from report. The whole of the above springs, extending through 3° of latitude, lie nearly in the same parallel of longitude (73°), and are within twenty-five miles of the sea, In a manuscript report to the Government of Bombay, on the province of Khandeish, Colonel Briggs has the following passage testifying to the occurrence of thermal springs above the Ghats $ ‘Among the natural curiosities of Khandeish are the hot springs of the Satpoora hills, particu- larly those of Soonup Deo and Oonup Deo, the former in the district of Arrawud, and the latter in the deserted Pergunneh of Amba. The former is so hot that the hand cannot be borne in it; the latter is less ardent, and is used as a hot bath; they are both said to possess medicinal quali- ties, and are considered useful in the cure of cutaneous disorders,—amongst others leprosy.” Dr. Buchanan speaks of hot springs at Rishikunda and Bhimband in the trap mountains of Raj- mahl+; and the Rev. Mr. Everest mentions a thermal spring associated with a trap bed at Kat- camsan, between the 23rd and 24th parallels of latitude, and longitude 86° and 87°¢. Dr. Adam mentions that of Sitakhund near Monghyr on the Ganges§. Dr. Davy speaks of one at Cannina, Ceylon ||; and I am informed they are to be met with in Canara. Mr. Crow, formerly commercial agent of the Bombay Government in Sinde, in his manuscript reports, mentions a thermal spring near Corachee on the Indus, of which the water is almost boiling hot. In Major Cruickshank’s manuscript revenue map of part of Goojrat a hot spring is placed at Tooee, near Ruttenpoor on the Mhye river, in latitude north 22°49', and longitude east 73° 30’; and there is another at Lawsoondra, eighteen miles west-north-west of Tooee. These instances, which I am satisfied could be multi- plied by diligent inquiry, afford ample proof of the wide occurrence in the peninsula of India of those singular phzenomena, the satisfactory explanation of the causes of which is still a desideratum in geology. a * Transactions of the Royal Asiatic Society, 1833. + Gleanings of Science, vol. i. p. 36. + Gleanings of Science, May 1831, p. 135. § Geol. Trans., 1st Series, vol. v. p. 349. || Geol. Trans., 1st Series, vol. v. p. 313. VOL. IV.—SECOND SERIES. 3K 428 Licut.-Colonel Sykes on a portion of Dukhun. Craters. Volcanic products were not seen by me, nor any conformation of the hills that might be deemed an extinct crater; although the porcelain and ferruginous clays, and the exterior coat of the various quartz and jasper minerals indicate their having been exposed to igneous action. Captain Danger- field did not meet with volcanic matters or craters in Malwa or the Vindhya range, but states a tradition exists of the celebrated city of Oogein, and eighty other places having been destroyed at a remote period by a shower of earth; and the people say that in the Vindhya range and Rajpeeply hills there are hollows near their summits ‘sometimes filled with water, which may be craters*.” As the old city of Oogein stood upon a river constantly overflowing its banks, it was probably buried in alluvium. Mr. W. Hunter attributed its destruction to one of three causes,—earthquake, overflowing of the Seeprah, or drift earth by high winds; and, although the least probable of the three, inclines to drift earth. He states there are not any traces of volcanic agency in the buried city, nor in the neighbourhood f. The remains of the city of Mhysir, on the banks of the Nerbuddeh (Nermada), are found in alluvium. We may safely say, therefore, there are not any indications of volcanic action of a comparatively recent date. Extent of Trap Region, &c. I will now offer a few observations on the amazing extent of the trap, la- terite, nodular limestone, granite, and gneiss formations in the Peninsula, limiting their application to 25° of north latitude. My personal knowledge of the country extends from the sea on the western side, to Arungabad, in 75° 33', and Sholapoor, 75° 53! east longitude ; north, nearly to Kandeish, and south, to Beejapoor and the Kristna river. Captain Dangerfield takes up the country on the north, nearly where my knowledge of it terminates, and says, «Tt (Malwa, including the Vindhya range) appears to constitute the northern termination of a very extensive secondary trap formation, which extends from the extremity of the Dukhun, and probably even Mysore, forming all the country above the Ghats, and part of the plains below, on the western side of the Peninsula, including the islands of Bombay, Salsette, Elephanta, &c.}”’ He carries the continuous trap north to Neemutch, in latitude 24° 27', at 1476 feet above the sea. Its western limit is at Dohud, longitude74°. Major Franklin and Captain Coulthard take it up in the eastern limits of Malwa, and trace it through Sagar; and it continues to an unknown extent towards Sohagpoor and the source of the Nerbuddeh river, on the table-land of Amarakantah, in longitude 82° east. Dr. Voysey describes its eastern limits at Nagpoor, lati- tude 21°10' N., and longitude 79° 14’ E. at 1000 feet above the sea. Mr. Cal- der states it passes from Nagpoor southward by the confines of Hyderabad, as low as the 15th degree of latitude, and taking a north-west direction termi- nates on the sea-coast at Bancoot or Fort Victoria, in latitude 18°. But speci- mens of rock shown to me from the Kolapoor country above the Ghats, between * Malcolm’s Central India, Appendix, p. 325. + Asiatic Researches, vol. vi. p. 39. t Malcolm’s Central India, Appendix, p. 320. Lieut.-Colonel Sykes on a portion of Dukhun, 499 the parallels of latitude 16° and 17° N., bear testimony to the trap extending nearly a degree and a half further south along the Ghats than Mr. Calder supposed. Indeed its southern limit in the Konkun, Mr. Fraser states to be at Malwan, fifty miles north of Goa*. From the above evidence we have proofs of a continuous trap formation covering an area of from 200,000 to 250,000 square miles, a phenomenon unexampled in any other country whose geolo- gical structure has been examined. It appears to me, however, that the above are not the absolute limits of the trap. Dr. Buchanant and Mr. Jonest+ describe the Rajmahl hills in latitude 25° and longitude 88° to 89° E. as trap; the latter says the basalt is of amazing thickness. The Rev. Mr. Everest §, in a journey from Calcutta to Ghazipoor, passed four distinct broad beds of trap between the parallels of north latitude 23° and 24°, and longitude 84° and 87°. He states these beds to have an inclination to a common axis, and he thinks it probable they are connected beneath the granite and gneiss. Mr. Royle travelling the same route, observed the same beds. Mr. Everest’s diagram shows their longitudinal axis ona line between the Rajmahl hills and the sources of the Nerbuddeh and Soan rivers ; and as the trap of the Vindhya range and Sagar extends towards these sources, it is very probable the rami- fications are connected with the beds (seen by Mr. Everest) and the Rajmahl hills, forming a belt across India from the 73° to the 89° of longitude, ex- tending, in fact, from near the mouth of the Nerbuddeh river to the Ganges at Rajmahl. The southern limit of trap is much lower than is assigned to it by Mr. Calder, as Dr. Voysey describes a basaltic dyke at Seringapatam, in latitude 12° 26’; and Mr. Calder himself mentions partial deposits of over- lying rocks as far south as Cotallum, at the extremity of the great western range, between the parallels of latitude 8° and 9°. Mr. Babington, passing through Mysore, describes all the black rocks he met with as hornblende pass- ing into basalt. He evidently adverts also to nodular basalt]. Age of Trap. With respect to the age of the great trap formation of India, it would ap- pear from Major Franklin’s Memoir on Bundelkund, that its northern ex- tremities rest on sandstone, which he considers identical with the new red sandstone of England; the trap would therefore be posterior to the carboni- ferous series and belong to the supermedial order. But the Rev. Mr. Everest 1 adduces valid reasons for questioning the correctness of Major Franklin’s opinion ; and it may be inferred, that he is doubtful with respect to the exact * Geol. Trans., 2nd Series, part 1. p. 153. + Gleanings of Science, vol. iii. Jan., 1831, p. 1. + Phys. Class, As. Researches, p. 165. § Gleanings of Science, vol. iil. p. 135. || Geol. Trans., 1st Series, vol. v. p. 325. q Gleanings of Science, vol. ili. p. 211. 3x 2 430 Lieut.-Colonel Sykes on a portion of Dukhun. equivalent in Europe of the Indian sandstone, as it is much associated with the primitive rocks *. In fact, where are the oolitic rocks above, and the mag- nesian below the red sand, where the rock salt and gypsum, and where, above all, the characteristic organic remains of the lias and magnesian limestone ? It would be idle, therefore, to speculate on the era of a formation without a standard of comparison to direct the judgement. The question of the manner of the formation of the horizontal beds of trap with their vertical edges is very interesting. It will be said they were ejected under the pressure of an incum- bent ocean. If such had been the case, where are the marine remains, and would not there have been sedimentary deposits upon them? Moveover, if viewed as coulées from craters, would not the beds have thinned out, instead of preserving the parallelism of their superior and inferior planes and their vertical edges ? Laterite. Laterite is a ferruginous clay mottled red and yellowish. When first dug from its bed, it is soft and is easily fashioned into the form of bricks or large square masses for building ; and if my recollection serves me right, it consti- tutes the material of the walls of the fort at Tellicherry and the jail at Calicut. It rapidly indurates on exposure to the atmosphere. It is destitute of fossils, as far as is yet known. That curious and very extensive rock, aptly denominated laterite, (I learn from the information of a friend,) occurs at the source of the Kristna river in latitude 17° 59', at an elevation of 4500 feet above the sea. It covers the low land between the sea and the great western range from the southern Konkun to Cape Comorin, and, agreeably to Dr. Davy, passes into Ceylon. I casually observed it at Tellicherry and Calicut, respectively 744 and 756 miles south of Bombay ; and at Calicut granite rises through it. On the low land at the base of the great eastern range, Mr. Calder says it reappears between the 11° and 12° parallels of latitude, and recurs in increasing patches passing northwards, covering granite. The Rev. Mr. Everest speaks of laterite forming a fringe to great part of the bay of Bengal and covering the edge of the granite of either peninsula f. Nodular Limestone. In addition to the evidence already adduced of the extensive occurrence of nodular limestone, Dr. Buchanan mentions having met with it in Rajmahl trap hills, in Bengal, and in Mysore. A writer in the ‘Gleanings of Science’ t states that it occurred in repeated borings for water in Calcutta, at from 50 to 112 feet below the surface. Another writer§ says, it is “very extensively distri- “ buted throughout Hindoostan,”’ and further asserts that it is a “most distin- ‘ guished feature of Indian geology.’’ The Rev. Mr. Everest and Mr. Royle remarked it in their journey before adverted to. The few organic remains * Gleanings of Science, vol. iii. p. 213. + Ibid., vol. ii. p. 135. $ Ibid., vol. i. p. 169. § Ibid., vol. i. p. 365. Lieut.-Colonel Sykes on a portion of Dukhun. 431 hitherto found imbedded, belong to living species. The following is the ana- lysis of “‘ Kankar ’’* (nodular limestone) by Mr. Prinsep f. Wister Of AbsOrptlonye. < ees 0 6 9. Gray plastic clay «6.000 sccsdecct ns cescveccersccssecesces 5 0 10. Earthy lignite and bituminized wood........seesereesveces 8 0 11. Highly bituminous and pyritous clay .......--+++.- esevcces 5 0 12. Leafy mass; chiefly bituminized stems, branches and leaves .. TG 13. Bituminized Wood... 0.0 ccc cccccccrcccccsccenscevscvsces 1 6 14°’ Same'as INO. 10.) crderstae te eielasistete ste sl e' c's o 1c wie ove etaitle mieianaie 3 0 15, /Same.as No, 12:0 sees ee ee sie Lsla lel» cioleie\ers ale Waieletdere cletenshe 2 6 UGS Same as No. 1Ojand aie cote sacisisle <'el> inj om «14 iyi ete a eis Li U7. Same as No. 12 sane monies treritelelalerelels's sles «)'s 01 6idiele feel iateteiete 2 6 18. Same as No. 9., bored into to the depth of ..........-eceeee- 24 0 79 6 Of which the lignite beds constitute ........ sis ole choleistte ote sheks 24 6 In most places the lignite rests upon clay, and below that come the sand- stone and loose sand, the latter being generally the lowest. At Roisdorf, near Bonn, the sandstone is covered by bituminous clay ; and at Frechem, near Brihl, thick beds of clay and lignite lie upon loose sand. In many places the sandstone occupies the surface, so that the clay and lignite have either never been deposited upon it, or have been carried away by sub- Mr. Horner on the Geology of the Environs of Bonn. A457 sequent denudation. At Friesdorf the clay and lignite beds rest imme- diately upon the ends of highly inclined strata of grauwacke. I have already noticed, p. 442. the alternation of trachyte tuff with the beds of the brown-coal formation ; and at p. 441. I have described the occurrence at Quegstein of trachyte tuff lying upon sandstone. I have also said, p. 443. that basalt occurs in connexion with the brown-coal formation: the place where this has been most distinctly seen is at Utweiler, on the north-eastern border of the district, about four miles from the centre of the trachytic and basaltic eruptions of the Siebengebirge, but situated in a valley between two knolls of basalt, the Rother Hardt, nearest to it, and the Hinzberg, not very far off. I visited this place in 1832 with Professors Néggerath and Mit- scherlich, to see the workings in a new shaft which had been sunk to obtain the coal. The former has lately published in Karsten’s Archiv fiir Bergbau, &c., an account of his observations, together with some subsequently made by M. Augustus von Strombeck, on this occurrence of basalt in the lower ground. M. von Strombeck drew up the following account of the different beds sunk through in the new shafts : Ft. In. Soil, «2... aie n pip wives bisie aise pleeo aie STORE >> 9e ipa laieep emai 4-0.pi 9.0) ¥,0)0 sp 2 6 2S LDCS 05 vc nce sw cnnerccwsereces pxspohe ioneje b =yphnbenia pinion eis seeees sis ps>.o 0 vhs ops 9 5 B. Prasat sre ncn tees ¢ owes 0.0 0 00 sete aps e]sj ols ip aie MiEate’slele aie ohe’salerote ohn ike cots] se ~ |, 30.6 The upper part consists of globular masses in some degree decomposed ; then comes a dark gray compact basalt, containing olivine, augite, and magnetic iron ore, but not regularly columnar. The lower part of the mass is formed of 4, A compact bluish gray argillaceous stone, a decomposed basalt or tuff, similar to what usually accompanies volcanic masseS......-essceeccescccscvcecsces . Les 5. Here begin the brown-coal beds properly so called; an indurated clay of a black colour from a mixture of coal, which splits into prisms about three inches long, and from eight to ten lines in diameter, the interstices filled with crystallized dolo- mite; a structure probably occasioned by the heated mass of basalt covering it al 6. Dark-coloured clay, containing much coaly matter ‘and pyrites, but neither slaty HOF COWMMMUAL . 206s. 6 oe ceeeeeseceee eveioi sie’ oe maida teidietel eaves etal covesesne 0 6 It is remarkable that this bed should show no indication of that columnar structure which is so marked in the beds which lie immediately above and below it. A similar fact has been observed in the Meisner. Then come the lignite beds, consisting of 7. Black pitch coal, separating into prisms of from an inch to an inch and a half in diameter, standing perpendicular to the face of the basalt bed, with the inter- stices lined with crystallized dolomite .. ....ccseeceesrseesecesecesseece This passes gradually into 8. AP mala: 0's. on Ds cls iala ole Do vec sev oesesvacece eereereee eee eeeee vee 458 Mr. Horner on the Geology of the Environs of Bonn. x Ft. In 9, Unaltered brown coal or bituminized wood, preserving the woody texture ....., 8 6 Total thickness of coal 13 feet 8 inches. In the lower part of this last bed occur kidney-shaped masses of compact clay iron stone. 58 10 Then comes a trachyte tuff, with portions of hard trachyte, into which they had sunk to the depth of two feet. It is here the usual underlier of the brown-coal beds, but it is also found lying between them, so that it is very possible if the shaft were sunk deeper, that this tuff would be gone through, and other brown-coal beds be found below it. M. Von Dechen states* that in the district of Briihl the beds lie con- siderably above the Rhine valley, and this seems to be equally the case on the right bank. It is worked at several places on the right bank, but by far the most considerable mines are on the other side of the river, and in the district immediately around Briihl. The united thickness of the lignite beds in dif- ferent situations in the plateau is very various, often too inconsiderable to be worth working. It has not been ascertained by actual trial whether they stretch quite across the plateau, the mines being situated on the east and west sides, but this is very probably the case. The following table will show the thickness of the brown-coal beds at different points on each side, lying east and west of each other. The thickness includes the clay beds that may be interposed between one layer of brown-coal and another, West Side. East Side. Feet. Feet. Walberberg near Bruhl ....From 12 to 30 Wine lane reistetatetelelelalelele icles From 6 to 66 Metzmacher....-+.-scegsrscee 26 to 49 An der ‘Gabgay fyi tecciaetel. 43 Bingsdortete se cretelelete ite tetele . 364 ZISSCISTMAAL veleils 1 ste). siecle Tee 16 to 63 Hennersgrube ......ss+cereres 40 to 52 Aurich einen erevelors ieielt epee 10 to 60 Altstadter Berg” =). <1s pis cieihommt 6 to 60 Gleneler Beng elie citer teeter 18 to 70 _ Schlenderhany-6..1. ses eo 14 to 40 Frechemer Berg... 25.0005. 19 to 55 The various mines of brown-coal in the district give occupation to about 1200 persons. The coal is consumed almost entirely by the poorer classes, as its strong peculiar odour, and sometimes sulphurous vapours, render its use disagreeable. Some of the harder kinds are used as they are taken from the pit; but these form a small proportion, and are, moreover, not so valuable for fuel: the greatest part is used after it has been artificially prepared. It is * Karsten’s Archiv, uti supra, p. 417. Mr. Horner on the Geology of the Environs of Bonn. A59 beat and trodden after being well mixed with water, and is formed in shapes like the crown of a small hat, which are laid out to dry like bricks, and these when dry are preserved for use by being piled up under cover. In this state they are called Alitten, and are sold on the ground for about nine groschen per hundred ; and as each of the kliitten weigh about five pounds when dry, the price is equal to about four shillings per ton *. The beds of the brown-coal formation are generally either horizontal or deviate only a few degrees from it. In the immediate neighbourhood of Ut- weiler, however, under a bed of loess about fourteen feet thick, there is a se- ries of about twenty distinct strata of clay, distinguished by various colours, and containing four layers of lignite, each about six inches thick, which have an inclination about 60°S. This elevation was probably occasioned by the eruption of basalt which is in the immediate neighbourhood. On the left bank of the Rhine, and near Brithl, near which no unstratified rocks appear, there have been also considerable disturbances subsequent to the deposition of the beds. At Hennersgrube, near the old monastery of Beuten, the lignite beds are suddenly cut off by a fault to the depth of forty-nine feet}. By referring to the Map, it will be seen that the brown-coal formation exists to a considerable extent within the volcanic region of the Siebengebirge, especially in the valley of Haisterbach. It is found in two small patches in Kénigswinter valley, one at a place called Kuckstein, pretty high up in the ascent to the Drachenfels, where clay beds are found; the other in the bottom of the valley at Quegstein and Tanzchen, as already mentioned. Here the sandstone members of the series only occur, the quartzose conglomerate occurring in great detached masses, seemingly piled together. These probably formed indurated portions in a deposit of sand, which has been since washed away, as has been often noticed in sandy beds of the plastic clay and other tertiary de- posits. In the southern parts of this district the brown-coal formation occupies much higher situations. The Papierkohle of Orsberg, near Erpel, which contains the impressions of reptiles and insects, is 372 feet above the Rhine ; and continuing the ascent towards Bruckhausen, there is a plateau of about a mile square, which seems to be entirely composed of the brown cval formation. At the very foot of the Mendenberg, at Ehl and at Stésschen, there is a very extensive deposit of lignite on the slope of the mountain, very high above the adjoining valleys, which has long been worked for the purpose of making alum, the clay and lignite being highly pyritous. The latter splits into thin plates, and contains numerous impressions of leaves, and occasionally those of insects, and is about sixteen feet thick. The beds occur close to the basalt ; and the workmen told me that they rise towards it, but that the actual contact is not seen. It appears that formerly four different beds eee ee ee eee eee * The pigment called Cologne earth is prepared from an earthy lignite. It is said that a great quantity of the light pulverulent varieties is sent to France and Holland, to be used in the adul- teration of snuff. t+ Von Dechen, in Karsten, uti supra. VOL. IV.— SECOND SERIES. 30 460 Mr. Horner on the Geology of the Environs of Bonn. of lignite were worked, separated from each other by clay and friable sandstone *. The Menden- berg is 1198 feet above the Rhine, and the lignite beds occur within 300 feet of the summit. Loess. The substance to which this name is applied is a sandy calcareous loam of a yellowish brown colour, slightly coherent, and absorbing water with great avidity. It is a deposit which has been generally considered to be peculiar to the Rhine valley +, and it is found, to a great extent, at detached points on both sides of the river, from Basle to Bonn. It has not been noticed by pre- vious writers on the district described in this paper with that attention to which its geological importance entitles it. Loess is specially noticed by Leonhard in his Charakteristik der Felsarten, published in 1824, who has adopted this trivial name, given to it in the neighbourhood of Basle {; but a fuller account of it has more recently been given by Professor Bronn§, in his description of the environs of Heidelberg, and from which I have put together the fol- lowing particulars. It is found on the sides of the hills next the Rhine valley, and penetrating into the side valleys, such as that of the Neckar, Mayn and Lahn, and occurs chiefly in those situations where the form of the land presented a barrier against its being washed away by a descending stream. It is, for example, more abundant near Worms and Oppenheim than near Heidelberg, because the force of the Rhine is chiefly directed there against its right bank. It is found at various distances from the plain of the Rhine, as much as nine miles, and it is in some places 600 feet above the level of the sea. One hundred parts of that near Heidelberg yielded 50 per cent. of siliceous sand, 164 of * Von Oeynhausen and Von Dechen in Hertha, vol. xii. 1828. + In the synopsis of the successive deposits in the basin of Vienna, given by Mr. Murchison, the uppermost is described to be “ Alluvial loam, called Zéss, with terrestrial shells of existing ‘‘ species, (of the genera Pupa, Helix, and Succinea,) mixed with bones of elephants of extinct spe- “cies. The average thickness of this deposit is about 60 feet, but at some places the thickness is “much greater.” Further, “It is greatly expanded near Krems and St. Polten, reaching occasion- “ally the thickness of 140 feet, and having, near these places, the exact appearance of the old allu- ‘vial hillocks in the valley of the Rhine, which have been described by M. Voltz.”—Geological Transactions, vol. iii. pp. 402, 405. Loess is said to occur also in the valleys of the Garonne and the Allier.—Rozet, Journal de Géologie, i. 57. t It is mentioned by the name of Britz by Steininger in his Neue Beitrége zur Geschichte der Rheimschen Vulkane. 1821. 8vo. \ § Gea Heidelbergensis, oder Mineralogische Beschreibung der Gegend von Heidelberg. 1830. See also Voltz, Uebersicht der Mineralogie der beiden Rhein-Departemente; and Rozet, Sur le Diluvium de la Vallée du Rhin, in Journal de Geologie, vol. i. Mr. Horner on the Geology of the Environs of Bonn. 461 argillaceous earth, nearly 32 of carbonate of lime, a trace of magnesia, and it was coloured by iron and manganese. In the immediate vicinity of the primary mountains it has a somewhat different character, being more sandy, and containing mica. The loess does not contain what can properly be called petrifactions, but a vast number of cal- cined land-shells of living species, more usually in the upper than in the lower parts of the deposit, and they seem to belong to particular horizontal beds. There have been found near Heidelberg the following species: Helix pomatia, H. nemoralis, H. hortensis, H. hispida, H. ericetorum, Bu- limus radiatus, B. lubricus, Lymneus ovatus. Some years ago, the lower part of an elephant’s tusk was found near Weinheim, at an elevation of 100 feet above the Rhine, and some fragments of elephants’ grinders had been previously found at a little distance from the same spot. It is found lying on granite, porphyry, red sandstone, muschelkalk, keuper, and lias, and near Oppenheim on grobkalk (calcaire grossier). The greatest elevation at which I have seen loess in the district described in this paper is near Erpel, above Orsberg, where it lies upon the brown-coal formation, a height which is fully 400 feet above the Rhine*; and it occurs, at about 200 feet high, near Steinsbusch, above Honnef. A very extensive deposit of it may be seen at the Bruckersberg, near Rhondorf, immediately south of the Drachenfels, where it forms an irregular mass from three to twenty-five feet thick, and covers trachyte and grauwacke, as represented in the wood-cut, p. 440. It is found at Quegstein in the valley of Konigswinter, covering trachyte tuff, and near Paffroth and Ober Dollendorf, on the slope of the Petersberg, covering grauwacke. Between Ober Dollendorf and Haisterbach it lies upon grauwacke, covering the summit of a ridge over which the road passes, in the side of the valley leading to the Stenzelberg, and at Roth Kreuz, covering trachyte tuff. It is found in the narrow valley which opens at Ober Cassel, and covering basalt at a considerable elevation on the Raben- lei. It occurs also, to the depth of fourteen feet, near Utweiler, covering basalt. These are the places where I have seen it on the right bank of the Rhine; but it is met with, no doubt, in many others. On the left bank a narrow ridge of it runs in a south-east direction from Bonn for about three miles ; and it is seen in the high bank of the river, covering the gravel of the Rhine plain, the surface of which is deeply channelled, the loess filling up the furrows. It is seen on the north- western slope of the Kreuzberg, in the valley between the Kreuzberg and Venusberg; in a valley behind Godesberg, near Marienforst ; to 4 considerable extent near Lannesdorf, where very deep clefts are cut in it; and it skirts the northern and eastern sides of the volcano of the Roderberg. Above Rolandseck there is a quarry of grauwacke, and upon the ends of the elevated strata of that rock lies gravel covered by loess. The basaltic columns in the quarry opposite to Unkel are covered by it at a very great height above the river, and where it is nearest to the basalt it con- tains rounded fragments of that rock. It is here, as elsewhere, an unstratified mass, which seems to have filled up deep furrows and irregularities of the preexisting surface. The absence of all signs of stratification is universal in this district. At Unkel it contains a considerable quantity of calcareous concretions. * Dr. Hibbert says that at Monrepos, in the neighbourhood of Neuwied, about ten miles seuth of this spot, and on the same side of the river, loess occurs at a height of 600 feet above the Rhine ; —History of Extinct Volcanos, &c., p. 205. 302 462 Mr. Horner on the Geology of the Environs of Bonn. The following are the shells which I have found in it in this district: they were named by Professor Goldfuss. Helix pomatia, H. nemoralis Linn., H. arbustorum Linn., H. hispida Linn., H. pulchella Drap., H. incarnata Drap., H. glabella Pfeiff., Lymneus mimutus Drap., Pupa muscorum Linn., P. unidentata Pfeiff., Bulimus radiatus Drap., Clausitia obtusa Pfeiff. Bones of Elephas primigenius and Rhinoceros tichorhinus have been found in the loess which covers the basalt in the Unkel quarry. In that near Lannesdorf I found a fragment of a rib belonging to an animal of the size of a horse or ox, and I obtained from the neighbourhood of Ober Dollendorf a few bones, which upon showing to my friend Dr. Miiller, Professor of Ana- tomy at Berlin, he considered to belong to the lower jaw of a young individual of a species of deer. It is remarkable that such a deposit should be almost devoid of all vegetable remains. ‘They are not noticed by Professor Bronn and other writers, and I have never found any*. Valley of the Rhine. The Rhine, from Linz downwards, flows through a deep deposit of gravel, with the exception of about three miles on the left bank, between Remagen and Rolandseck, where the hills come nearly to the water’s edge, and the grauwacke strata appear in the side and channel of the river. The gravel is composed for the most part of grauwacke and quartz, but the former predo- minates. It is very distinct in its character from that which covers the brown- coal beds on both sides of the river, in which quartz is the prevailing material, and which is usually of a bright yellow colour, from an admixture of oxide of iron, which I have never found to be the case in the gravel of the plain, deep sections of which are shown in pits in several places distant from the river. It is of an unknown depth; wells which have been sunk sixty feet have not passed through itf. The plain which spreads out on both sides from the gorge near Rolandseck, has by no means an uniform flat surface: there are long low ridges in the direction of the stream, but not parallel to its present bed, which seem to indi- cate that the Rhine, previous to the historical epoch, had occupied a different channel from that in which it now flows: that at one time its course was very near the foot of the ridge from Ober Cassel to Kiidinghoven, and at another time close under the brown-coal plateau on the left bank, westward of Bonn. The situation of Cologne, founded in the early part of the first century, proves that it has flowed in its present course for at least eighteen hundred years. * See Appendix VIII. p. 474. + See Appendix IX. p. 478. Mr. Horner on the Geology of the Environs of Bonn. 463 Mineral Waters. There are three springs of some celebrity ; at Roisdorf and Godesberg near Bonn, and at Heppingen near Landskron, in the valley of the Ahr. They are cold, and contain a considerable quantity of carbonic acid gas. Their con- tents, according to analyses which have been published, are as follow : Roisdorf*, 1°37 volume of carbonic acid gas : Carbonate! ofisoda eajjients ato: iccctiera cliniors oierd storie’ 7°86 Sulphate Of Sodaracerpeitemssits << ep<'as ameuile « evipis 4°78 Muriate'of soda) ey .e+.5. Mictaterecst ahaa s of a) cletens 19°01 Phosphate Of SOda icicces cuscccccss cece eseees 0°06 Carbonate Of lime ntact nce cleseisie.e.s:0 «ccs oiSere ore 2°81 Carbonate of magnesia........... oh Coane we 3°98 Iron, alumina, and silica, about ............-e. 27 58°77 in 10,000 parts. Godesberg +, about 16 cubic inches of carbonic acid gas in a pound of the water, and Carbonate: Of sodas eparsreycvels eis: arevsyenavele oistovaletstone’s 7°00 grains. Carbonate of magnesia .........0+0% hoon hee 3°32 Carbonate ofelime cin lelacin ofareter corsteleteterste tele sis 2°70 Miuriate, Of SOGAY si. sh<'> se els ple ls civic! hate sisi sisi otclers.g 1°33 Garbonaterof irom. pe siecle nels © seve cit CISL CRO 75 15°10 in 1 |b. Heppingen f, 80 cubic inches of carbonic acid gas in 100 cubic inches of water, and one pound of water yielded Carbonate of soda ........e+++-: aetebtsies sisere sit) OF20 Carbonate of magnesia ....... s aaetsarist cher eRe isteretate 2°40 Muriate of soda ....... Mee tiie BU leiete s: 3 Soper. 3°00 Sulphate of soda....... SCO GIE O CODER eereoe 2°10 Carbonate, of lime ngeretesctels c)siefs)r1s, 01+ ofare © si slievencie ele 1°30 15°00 No mineral waters appear to have been found within the region of the Sie- bengebirge § ; and no water from which any calcareous deposit has been pro- duced exists in any part of the district: there seems, indeed, to be an entire absence of limestone in any form, * Bischof, Die Mineralquellen zu Roisdorf. Bonn, 1826. + Wurzer, in Harless, Gesundbrunnen in Grosherzogthum Nieder Rhein. 1826. ¢ Funke, in Harless, uti supra. § Harless, uti supra. 464 Mr. Horner on the Geology of the Environs of Bonn. Of the relative Ages of the Sedimentary Rocks. The oldest of these is the grauwacke, and, as If have already said, it has every appearance, in the more northern part of the district at least, of belong- ing to the latest periods of that formation. The whole series of the secondary rocks, from the grauwacke to the chalk, inclusive, is wanting ; not a trace of them is to be found én situ in any part of the district *. This brown-coal formation has been hitherto held by those who believe in the universality of tertiary formations, according to the types in the Paris ba- sin, as belonging to the plastic clay ; but on what grounds I have not seen stated. 'The clays, sands, sandstones, clay ironstone, pyrites +, gypsum, and . the lignite itself, when without a recognisable organic structure, prove nothing as to age, for all these are found in formations much earlier and much later than the plastic clay. We can found no safe reasoning upon any other ground than upon a comparison of the organic remains with those in other deposits. The Flora of the several brown-coal or lignite deposits has not yet been explored by a botanist of authority, with the exception of the short notices we have received from M. Adolphe Brongniart. It is to be hoped that in the future progress of his valuable general work he will direct his special attention to this branch of his subject. In his Prodrome d’une Histoire des Végétaux Fossiles, published in 1828, he says, “‘ From all I have yet seen I do not be- «lieve that a single distinctly dicotyledonous leaf has ever been found in any “formation older than the chalk. Future researches may prove the existence “ of such vegetable productions in the secondary periods, but it is at least cer- “tain that they are extremely rare, and that they did not begin to be very nu- “¢ merous until the period which succeeded the deposition of the chalk.” (p. 148.) In speaking of the lignite formation, including those of the molasse and plastic clay, he says, “This formation is one of the richest in vegetable remains, but “it is however very rare to find them in such a state of preservation that they “can be determined with any degree of precision ; or they belong to classes of * M. Alex. Brongniart has been much misinformed when he says, ‘ Les masses immenses de “lignite terreux de Bruhl et de Liblar, ne peuvent étre placées que sur la craie tufau, qui est la roche “« fondamentale de ce pays.” —Descr. Min. des Environs de Paris, 345; and Dict. des Sciences Natu- * relles, art. LicnirE, p. 386. + M. Alex. Brongniart says, “ Les terrains thalassiques ne contiennent méme au dessus des ar- “ giles plastiques aucun sulfure métallique en quantité notable.” — Tableau des Terrains, p. 129. Were there no exceptions to this rule, the existence of pyrites would become a valuable document for the determination of the ages of deposits ; but the London clay abounds in pyrites. Mr. Horner on the Geology of the Environs of Bonn. A65 ** plants in which the power of determination becomes much more difficult.’ (p. 205.) He only alludes to the brown-coal of this district, by naming among the Palms “ Cocos Fauasi,”’ and under Monocotyledons of uncertain families “ Endogenites ”; both from Liblar. M. Alex. Brongniart, who has entered more fully into the subject of lignite than any other systematic writer I have met with, both in a special article on lignite in the Dictionnaire des Sciences Naturelles, and in his Tableau des Terrains, assigns this deposit to the plastic clay ; but it is obvious that he has not visited the spot himself, and that what he says about it, as well as the above notice of it by his son, is taken in great part from the memoir of Faujas St. Fond, above quoted, who thirty years ago visited the Liblar mine only, and in whose memoir everything that relates to organic remains is far from satisfactory, in so far as regards observations on the spot by the author himself. Now although the leaves of dicotyledonous trees may settle the question of this lignite deposit being superior to the chalk, they do not fix it to any parti- cular epoch of the tertiary period, unless it can be shown that they have an equally limited range ; and it has not yet been ascertained what species of di- cotyledonous leaves are peculiar to the earlier, what to the later beds of the tertiary series, and whether there be any common to all. So far, therefore, the present state of our knowledge of the fossil botany of the deposits above the chalk does not afford any sure criterion for determining the age of a bed. The usual and most exact medium of identification, by the remains of mol- luscous animals, entirely fails in this case; for, with the exception of the sili- ceous mass or blocks at Marienforst, not a single shell of any description has been found in any part of this brown-coal formation*. Now these are abun- dant in the lignite deposits of the Paris basin, of Soissons, of those in the mo- lasse of Switzerland, and in the great deposit in the valley of the Inn at Hi- ring, which may be taken as types for comparison ; and, moreover, in all of these, marine shells are more or less mixed with those of fresh water. So far, therefore, all proofs of similarity fail; nor do we derive any aid from superior beds, as these are entirely wanting in this district. We are thus limited to the evidence which can be derived from the remains of fish, insects, reptiles, and the Marienforst shells. Although found in considerable abundance, one species of fish only has been met with in this brown-coal formation, the Leucescus papyraceus of Agassiz, and that belongs to fresh water. Now in none of the-great lignite deposits above mentioned have the remains of fish of any kind been yet * See Appendix V. p. 473. 466 Mr. Horner on the Geology of the Environs of Bonn. stated to have occurred ; but Mr. Agassiz mentions that several species of the genus Leuciscus are found in the beds of Giningen. With regard to the remains of Frogs, they do not appear to have been known to exist in a fossil state previous to the memoir of Professor Goldfuss on those found in the papierkohle of this district; for Cuvier says, under the head Des Ossemens de Batraciens, ‘‘ Je crois qu’il n’y a de certain que ceux “des carriéres si problématique d’C&ningen* ;”’ and here he does not allude to Rane. Mr. Murchison, however, in his late memoir on Giningen, when speaking of the collection of fossils from that place in the museum at Carlsruhe, says, “I observed specimens of Rana and Testudo.” I have had no means of ascertaining whether the same species of Salamander exists at Giningen with that found in our papierkohle; but Professor Goldfuss informs me that the Salamander Ogygia is scarcely to be distinguished from the living species, The insects in the papierkohle are another distinctive character of this brown-coal formation, for no such occurrence has been mentioned in any of the other great lignite deposits above alluded to, and two of those found in the papierkohle also occur at Giningen, viz. Anthrax and Cerambyx. It is impossible to decide whether the siliceous mass of Marienforst belongs to the lower or the upper part of the brown-coal formation, but the quartzose sandstones are always found in the lower part. As far as casts enable one to decide, and these only are met with, the species Planorbis rotundatus and Lymneus longiscatus have been made out by M. Deshayes. Mr. Lyell enumerates them in his Tables of shells, constructed on the authority of M. Deshayes, as occurring in his Eocene and Miocene periods, and not in the Pliocene. It thus appears that there is no evidence to prove that this brown-coal for- mation belongs to the period of the plastic clay, and all the phenomena seem to assign it to a more recent period, and they prove it to be of purely lacustrine origin. It seems to have been deposited in a vast inland lake of fresh water, fed by some great river or rivers, which brought the sand and clay and wood, that subsided gradually to the bottom ; and the perfect state of preservation of some delicate leaves shows also that the lake was surrounded by trees or shrubs. I have been thus particular in endeavouring to fix the age of the brown-coal formation, not only on account of the great extent and importance of the deposit in itself, but because it affords, as I shall presently show, a criterion for judging of the period when the unstratified rocks of the Siebengebirge were ejected. * Cuvier, Ossemens Fossiles, tom. v. p. 385. Mr. Horner on the Geology of the Environs of Bonn. 467 Of the relative Ages of the Volcanic Rocks to each other and to the Sedimen- tary Rocks. The trachyte tuff appears to me to be the oldest of the volcanic eruptions, for it has nothing of the character of having been derived from preexisting trachytes, and it is traversed by a dike of trachyte, as I have described at p. 439. This is quite in accordance with what takes place in active volcanos, where nothing is more common than for an eruption of ashes to precede that of a stream of lava; and it is also in accordance with what has taken place in another part of this district, at Siegburg, where dikes of basalt traverse basaltic tuff. The masses of solid trachyte contained in the tuff are not fragments, but, as was observed to me by Professor Mitscherlich while we were ex- amining together the trachyte tuff of the Konigswinter Holle, are similar to the bombs we had found in such abundance in the ashes of the volcanos of the Eifel, and which are of frequent occurrence in the ashes of active volcanos *. They often, it is true, resemble, nay, are almost identical with, the trachyte of the adjoining hills, but they are very frequently of a kind unlike any found en masse. That there may be some secondary trachyte conglomerates is very probable ; indeed I am inclined to consider that variety at Ober Cassel, con- taining portions of basalt and balls of clay ironstone, as having been derived from preexisting trachyte and trachyte tuff. Previous writers on this district have said that they were unable to point out any difference of age between the trachyte and the basalt. I presume, therefore, that the dike of amygdaloidal basalt which traverses the trachyte in the Keilsbrunnen quarry must have been only lately exposed, for that is de- cisive of the question. Another proof of the basalt being more modern than the trachyte is, that the trachyte tuff, except in the case of that at Ober Cassel above alluded to, never, as far as my observations and information go, con- tains any detached masses of basalt. There is, besides, no instance of a tra- chyte dike traversing basalt, but many of the latter traversing trachyte tuff. That the trachyte and basalt are later than the grauwacke requires scarcely * Mr. Poulett Scrope in describing the trachyte tuff of the Ponza Isles (which he calls conglo- merate,) mentions the occurrence of numerous “ fragmentary blocks” in it, and says, “ None of the fragments are water-worn, and they all have evidently been enveloped in the base immediately upon their ejection by the volcanic impetus.” He also shows that eruptions of solid trachyte have taken place subsequently to the ejection of the tuff: “this rock [prismatic trachyte] bears on most points the appearance of having forced its way upwards by cutting through the incumbent conglomerate in various directions, and occasionally of having spread laterally over it.”—Geological Transac- tions, Second Series, ii. 203 and 206. VOL. IV.— SECOND SERIES. 3 P 468 Mr. Horner on the Geology of the Environs of Bonn. to be mentioned ; the numerous fragments of it included in the volcanic rocks, and the basalt rocks traversing it, remove all doubt. The great disturbance of the grauwacke strata in the neighbourhood of the trachyte and basalt may have been produced by their eruption. It is clear that volcanic eruptions took place during the deposition of the beds of the brown-coal formation. Trachyte tuff covers the sandstone at Quegstein, alternates with clay and clay ironstone in the neighbourhood of Rott and Utweiler, contains fragments of wood at the Langenberg, and leaves of trees, identical with those found in the papierkohle and sandstones, at Scheuern and Ofenkulenberg*. The basalt tuff of Siegburg contains fragments of wood, bituminized and penetrated by iron, not to be distinguished from that found in the lignite deposits. In con- formity with what has been said of the more modern age of the basalt, we find it at Utweiler lying over the brown-coal beds to the depth of thirty feet; and no fragments of basalt occur in any of the beds of the brown-coal forma- tion, as far as I have been able to ascertain. Besides the instance of alternate beds mentioned above, the trachyte tuff in many places shows an arrangement that could only have been produced by the materials being moved under the surface of water. All these facts seem to me to prove that volcanic eruptions were going on in a freshwater lake, in the same manner as we have submarine eruptions at the present day, during the time that the brown-coal beds were in the course of being deposited. It is probable, however, that all the volcanic rocks we now see were not ejected at that period, but that subsequent eruptions took place which heaved up the Siebengebirge and the cones to the south, carrying up the brown-coal beds along with them, in some instances, as at Stdsschen, to the height of nine hundred feet above the present surface of the Rhine ; the same action, probably, heaving up the plateau on the left bank of the river, although with a less degree of force, as the basaltic outbursts on that side are comparatively on a limited scale. The great fault in the brown-coal beds, described p. 459, indicates a powerful and sudden disturbing force. It would appear, also, that the great mass of gravel which covers the brown-coal beds had been strewed over them previous to this elevation, for it is found on both sides of the Rhine at a great height, and never in the intermediate plain, the gravel of which, as far as my observations go, has quite a distinct character. I have endeavoured to obtain some distinct evidence as to the relative age vf the volcanic eruption of the Roderberg, described p. 447, the whole cha- racters of which are very different from anything in the Siebengebirge. I * See Appendix X. p. 478. Mr. Horner on the Geology of the Environs of Bonn. 469 have not been able to find anything more precise than that the loess at its base contains portions of scoriaceous basalt, and that a mass of the same gravel which covers the brown-coal formation, occurring at the edge of the crater, lies under a dark volcanic tuff, or indurated mud. Dr. Hibbert states that in the road from Andernach to Frauenkirchen he saw a section where a bed of pumice, twenty-one feet thick, lies over a fine loess from forty-five to forty- eight feet thick, and a coarser loess eighteen feet thick: he mentions other places, which show that the volcanos in the Lower Eifel were in activity subsequently to the deposit of the loess, and it is probable that this was also the case of the Roderberg*. Of the relative Age of the Loess. This remarkable deposit, abounding in terrestrial and fluviatile shells of ex- isting species, and containing in many places, some of which are more than two hundred feet above the Rhine, bones of extinct species of the elephant and rhinoceros, rests at Bonn, as it does at Strasburg, upon a deep mass of that same gravel through which the Rhine flows in the greater part of its course from Basle. It is the latest deposit found in this district prior to the commencement of the recent period. It is difficult to conceive how it should have been produced, except by some vast flood, which, if no elevations or subsidences of the land have since taken place, must have been of the depth of at least six hundred feet, and several miles in breadth, and so densely charged with mud as to leave behind, at an elevation of two hundred feet, masses covering hundreds of acres, two hundred and fifty miles distant from the spot where its first traces are to be seen, simi- lar masses occurring at intervals not far asunder during the whole of that course. That it was a sudden inundation, and that the loess was not gradually and tranquilly deposited from stagnant water is probable, from there being no signs of stratification, by its containing the remains of land and fluviatile shells, and of land animals only, and by the great rarity of vegetable remains in it. That plants and trees were not swept along by such a flood is extremely im- probable; but they would obviously not sink in so dense a fluid, hurried along with such a velocity as that with which it must have moved. Had there been a gradual subsidence, not only would there have been stratification, but beds of lacustrine and fluviatile shells, and abundance of leaves and other vegetable remains. We must ascribe such a flood to the sudden bursting of the barrier of a vast lake, the volume of water rushing over a great extent of land, and * See Appendix XI, p. 478. 3P2 470 Mr. Horner on the Geology of the Environs of Bonn. becoming charged as it rolled along with the earthy contents it afterwards de- posited in the lower part of its course. We know that in the upper part of the Rhine valley, between the lake of Constance and Basle, there must have existed at one time a vast freshwater lake, where the great deposits of lime- stone and marl at GEningen took place, forming a mass of horizontal beds, six hundred feet thick, counting from the present bed of the Rhine. That the discharge of the waters when these (iningen beds were laid bare was that which brought down the loess is, perhaps, even a conjecture too hazardous from one who has never been near the spot. To give a history of the loess in the valley of the Rhine, by a careful examination of its composition, organic remains, its form of deposition and levels, and to trace it, if possible, to its source, would be a most interesting subject of inquiry, and could not fail to prove a valuable contribution to geological science. It was my intention to have compared this district with the great trachytic eruptions of Hungary and Central France, but I found that to do so to any useful purpose, I must have entered into details which would have extended this paper beyond all reasonable bounds*. Table of Heights. The following heights are extracted from a Table of barometrical mea- surements, by M. Moliere of Saarbruch, Civil Engineer, a manuscript belong- ing to the Council of Mines at Bonn. The measurements are in Paris feet+, above the mean height of the surface of the Rhine at Bonn, which, according to Van der Wyck, is 193 English feet above the level of the sea. I have classed them according to the nature of the rock at each place. * See Appendix XII. p. 479. + 1 Paris foot = 1:0658 English; so that adding th part of the height in Paris feet gives very nearly the exact height in English feet. Mr. Horner on the Geology of the Environs of Bonn. Grauwacke. Feet. Greatest height to which it rises on south slope of Mendenberg .......+++++ 908 Ditto between the Hummerich and Mit- telberg wescccsescsececvees coooe 841 Ditto on west slope of Petersberg .... 658 Trachyte. Drenkelberg .....ceecceeseeeesees 1188 Briingelsberg .....ececeecesessees 1131 WGHE Pre ae oo 0:0 + wiv nn oon vs sie ese pe asl Scheerkopf ....... a ciaiaidin sieiaisieb\ denen eC Bruderkunzberg ....+.-eeeseeeeeees 1022 Hlummierich ...,cecccsesssccvesscs 996 Gross Mittelberg ....+seccceseesses 936 Buckeroth ....2csceccscsssesescoes 927 Wasserfall ....ccccccccosccccsvess 919 Perlen Hardt <2 .c--cnesccedcaceess 917 Gross Rosenau .cccesscoecescesees 883 Gross Geisberg ....-.ccccoeccseee 871 Jungfer Hardt....+seeeeceeeseesee 865 Wolkenburg .....ccccccescccesess 865 Gross Breiberg ...ccccescccescceee | 846 Schallenberg ....scccccesceescecces 818 Klein Mittelberg.....ceccccseccess 199 Drachenifels...012 J scccicciceccaccicaci, 100 Stenzelberg ...sceccccssccccseceee 760 Hirschberg ..cccccscscccsesescces O19 Trachyte Tuff. Rises to height of : On west slope of Oehlberg ........+. 933 At Margaretha Kreuz.....seeeseees 834 On south-east slope of Geisberg...... 776 On north slope of Nonnen Stromberg.. 638 Basalt Dikes. Keilsbrunnen, through trachyte...... 785 Lowenburg Tranke, through trachyte 949 AT) Feet. Between Drachenfels and Hirschberg, through trachyte ..ssecescsceeees 443 Steinsbusch, through grauwacke...... 216 Siegburg, through trap tuff.......... 211 Wolsberg, through trap tuff.......... 230 Grimprich, through trap tuff......... 189 Konigswinter Holle, through trachyte HEE. wiaseieternie Sietst stata/siols] sles sion) efere!« 184 Basalt. Diisberg, neat EiMzZjecsicece sce css s we lioge Gross Ochi bergy). sss cise claus s:> «0,0 1289 Lowenburg .cccsccccccsseesersees 1272 Mendenbergicn aie « cles aieisinicie ce nraais = 1198 Klein OchIbere “032. seis cera. s © « 974 Ley berg paar. Sat ws seine em toue een o7 Petersbers: 22.) io aie sete cists sr er 904 Nomen Stromberg)... 00.05.0000 - 818 Ober Dollendorf Hardt ............ 619 Limberg “7.12... <% Bid a ateinlntedni sts eans ooo Grose WirlBer. Peele Sloe ewewenes O97 Steinringsberg ...s.cccccccscvess «+ 565 Hartenberg ....cscccccscccesessee 050 Gross Scharfenberg .....00000++008 560 Whomasberg .'ss0 0 ccc ceccsecccccens 541 aICMDENS /cfoiec ccntasia vee sce ets 538 Rabenlelscicct sccvccccenncssccess A420 Hinzberg ocescccciecccccens succes 429 Finkenberg, -o.0 00,016.00 010 90 selec clnle ee 210 Brown-Coal Formation. Stoschen, at foot of Mendenberg...... 913 At village of Vinxel .....cesesee. - 400 At Orsberg, near Erpel .......++0-- 372 Between Drachenfels and Wolkenburg. 445 Auf dem Stein, near Ober Cassel, where a bed of silicified wood was found .. 402 At Rott, where fish arefound........ 298 At Tanzchen, sandstone beds........ 226 472 Mr. Horner on the Geology of the Environs of Bonn. APPENDIX.—Marcu, 1836. See Page 433. I. Page 433. M. van per Wycx makes the mean height of the surface of the Rhine at Bonn 188 Rheinland feet (193°6 English feet), and at Konigswinter 192 Rheinland feet (197°72 English feet) above the level of the sea. Barometer- Hohen—Messungen des Rheinstroms, in Leonhard and Bronn’s Neues Jahr- buch fiir Mineralogie, &c. 1835, p.260. One Rheinland foot = 1:0298 En- glish. II. Page 434. From the smallness of the scale to which my map has been reduced for publication, it is scarcely possible to define the boundaries of the several mi- neral formations with precision. ‘Those who wish to examine the Sieben- gebirge will do well to provide themselves with a copy of a geological map published at Bonn in 1835 by Henry and Cohen. III. Page 442. M. Tuomas, in the memoir cited in the next note, mentions the occurrence of trachyte tuff in the lane leading from Nieder Bachem to Liessem, p. 48. IV. Page 447. A very detailed account of the Roderberg has been recently published, entitled Der Vulkanische Roderberg bei Bonn. Geognostische Beschreibung semes Kraters und seiner Umgebungen, von Cart Tuomas. Bonn, 1835. Those who wish to examine and understand the structure of this interesting geological feature of the district should take this memoir as a guide. I ex- tract the following particulars in this place, and I have refered to it in other parts of this Appendix. The highest point of the crater is 330 Rheinland feet (339°8 English feet) above the surface of the Rhine. He estimates the longest diameter of it at a thousand paces, and the shortest at seven hundred paces. The lava at the north-east side of the crater was at one time quarried, in Mr. Horner on the Geology of the Environs of Bonn. A73 the hope of obtaining millstones, like those of Nieder Mendig; but it decom- poses readily when exposed to the air, and masses of sufficient size without rents could not be had. Fragments of grauwacke and of quartz are common in the lava; they are fast imbedded in it, and their surfaces are frequently vitrified. These vitrified pebbles are met with abundantly among the scoriz on the sides of the hill, varying in size from a foot to the tenth of an inch in diameter. “ Any one,’ says M. Thomae, “who had not picked them up himself on the spot from “among the brown cinders, might swear they came out of a porcelain furnace.” p- 17. Volcanic bombs are sometimes found, and some which M. Thomae “ broke presented the following remarkable appearance. “ Three almost per- “ fectly round balls, the largest of which might be about the size of a man’s ‘ head, contained in the interior rapilli, small rounded portions of porous lava, “ vitrified and non-vitrified quartz pebbles, and small fragments of grauwacke, “some friable, others vitrified, and some unchanged. The bodies, which were “ of the size of nuts, filled the whole interior space of the bomb ; they lay chiefly “loose, often five or six were adhering together, or single ones were fixed to “the sides of the bomb, so that in breaking the porous lava shell, which was “ about a finger’s breadth in thickness, great caution was necessary to prevent “the contents falling out. In the interior of one of the bombs there was a “‘ small detached crystal of augite.” p. 21. V. Pages 450 and 465. In Leonhard and Bronn’s Neues Jahrbuch fiir Mineralogie, &c., for 1835, p. 678, there is the following communication from Professor Noggerath to the Editors. , “ Bonn, 30 October, 1835. “Hitherto no shells have been found in our Rhenish brown-coal. Recently “‘ some freshwater shells were brought to me from a bed which seems to be in- “termediate between earthy brown-coal and bituminous (brown-coal) clay. “'This bed, which is of inconsiderable thickness, covers the alternations of “‘ compact clay ironstone, which occur near Rott, eastward of the Siebenge- birge, an account of whichis given in my Rheinland Westphalen, iv. p. 388. “« You will see by the specimens sent herewith that the shells are changed into “a kind of brown-coal, and are almost quite flat. If M. Bronn will venture to “‘ pronounce an opinion upon these, I should wish you to insert it along with “this notice in your journal.” M. Bronn adds, “ All these shells belong to the genus Planorbis, but they “are so crushed as to be almost wholly unrecognisable. The largest and best- ATA Mr. Horner on the Geology of the Environs of Bonn. « preserved specimen nevertheless appear to be Planorbis carinatus ; the rest ‘seem to belong to the same species.” VI. Page 452. I visited the lignite deposit at Friesdorf in September 1835, in company with Mr. Robert Brown, when he collected several specimens of the vegetable remains. He informs me that all the wood he found is coniferous, which, taken along with the evidence derived from the leaves already noticed, might point rather to a temperate than an equinoctial climate. VII. Page 453. M. Agassiz examined the specimens accompanying this paper, in a late visit to England. Besides the Leuciscus Papyraceus, he found another spe- cies, which he named Leuciscus Macrurus. VIII. Page 462. Since this paper was read, J have seen the loess in three situations, which are remarkable as connected with the geological events which, in compara- tively recent times, have occurred in this district. I learned in the summer of 1833, that, in the preceding spring, the pro- prietor of the farm in the bottom of the crater of the Roderberg, in sinking a well near his house, had passed through a bed of loess. I went there, accom- panied by Mr. Lyell, and we ascertained that, after a few feet of scoriz, they had found loess, and had penetrated it to the depth of 62 Rheinland feet (632 English feet), but without passing through it. Part of that which had been dug out was on the ground near the well, the rest had been scattered over the adjoining field. It had the usual characters, and several of the cal- careous stony concretions were lying about. In the left bank of the Rhine, a short distance below Neuwied, and near Andernach, I observed the loess lying under a bed of volcanic scorie, and that covered by a considerable thickness of alluvial soil. On a visit to the Laacher See in September 1835, I observed a section close by the edge of the lake, and within a quarter of a mile of the monastery, where loess, containing its characteristic shells, is covered by a succession of beds of volcanic sand, scoriz, and pumice, and altered fragments of grau- wacke. In a paper on the solid contents of the Water of the Rhine, which was read before the Geological Society in March 1834, and published in the London and Edinburgh Philosophical Journal for January 1835, p. 102, I showed that the Mr. Horner on the Geology of the Environs of Bonn. 475 sediment obtained from a large quantity of the water has the same appearance, and is of the same composition as loess. In the Edinburgh Philosophical Journal for July 1834, there is a paper by Mr. Lyell on this peculiar deposit: he has treated of it very fully in his “Principles of Geology,” vol.iv. p. 44, 4th edition; he read some addi- tional observations upon it at the Geological Society in December 1835, an account of which is given in the Society’s “ Proceedings,” vol. ii. p. 221, and he again refers to it in his Address at the Anniversary of the Geological Society, in February, 1836. M.Thomae, in the work above cited, has recorded several interesting facts respecting the loess which lies around the Roderberg. We learn, from the observations of these gentlemen, the following particulars in addition to those mentioned in my paper. Of the shells found in the loess near Bonn the terrestrial predominate greatly over the aquatic; the same rule holds good, though not to the same extent, with respect to the shells now drifted down by the Rhine, and con- tained in the mud and sand of its shores; and the greater proportion of these last agree specifically with those buried in the loess.—Lyell, Memoir of 1834, p. 3. The loess absorbs water with great avidity, and where exposed to the action of water is often carried away in great masses. It affords a very fertile soil ; but the husbandman is sometimes doomed to see his hopes blasted by a violent storm of rain washing away the whole soil from his field, laying the roots of his vines bare to the sun.— Thomae, 26. On the east side of the Roderberg there are five round-back ridges, co- vered with vegetation, which seem to radiate from the lower part of the hill towards its base. ‘These are composed of loess; and, at their inferior ex- tremity, are in some places laid open, exhibiting a vertical section from twenty to thirty-five feet in height, resting upon a mass of gravel, identical in com- position with that forming the present bed of the Rhine, and from four to eight feet in thickness. —Thomae, 29—31. “On the north-north-west side of the Roderberg a valley separates the volcano from the Zilliger Haidchen, heathy hilly ground composed of loess, which is furrowed in several places to a great depth. ‘These excavations are called in German schluchten, meaning hollow ways. In some of these the loess is seen to be intermixed with volcanic products, and containing detached ac- cumulations of scoriz in amorphous masses. In several places there are con- tinuous beds of scoria lying upon and covered by loess. In one of the schluchten a section is exposed, exhibiting alternate layers of scorie and tuff, resting on the fundamental grauwacke, and covered by loess; in another a VOL. IV.— SECOND SERIES. 3 Q A76 Mr. Horner on the Geology of the Environs of Bonn. volcanic breccia, composed of fine blackish grey sand, including small frag- ments of clay slate and grauwacke five feet thick, rests upon loess, and is covered by another deposit of loess fifteen feet thick, identical in composition with the lower deposit. The flat surfaces of the slate and grauwacke frag- ments, and numerous scales of mica, lie horizontal, producing a slaty structure, and indicating their having assumed that position under the surface of water. The schlucht, which opens towards the village of Lannesdorf, exhibits a similar intermixture of scoriz in the loess, and it is about two miles and a half distant from the crater of the Roderberg.—Thomae, 36—A43. I shall now point out some of the more important observations of Mr. Lyell on the loess in the higher parts of the Rhine valley and the adjacent country, contained in the memoirs above mentioned, which throw light on the history of this remarkable deposit. He observed it near Andernach, alternating with volcanic scorie, &c., and in one place ‘‘ covered with beds of pumice, trassy pumiceous sand, and small dark volcanic cinders, forming upon the whole a mass from ten to fifteen feet in thickness,”—ejections from the neighbouring volcanos of the Lower Eifel. In an excursion through part of the duchy of Darmstadt by Mayence, Oppenheim, Alzey, Flonheim, Eppelsheim, and Worms, he found the loess spread almost everywhere over the country. On the oppo- site side of the Rhine, in the elevated table land above the Bergstrasse be- tween Wiesloch and Bruchsal he observed the loess attaining a thickness of 200 feet. Near Strasburg large masses of it are seen at the foot of the Vosges mountains on the left of the great plain of the Rhine, and at the base of the mountains of the Black Forest on the other side. It occurs in con- siderable force at Basle, and still higher up the Rhine at Waldshut, and it is said to terminate between that place and Schaffhausen. In the hills called Bruder Holz, about two miles south of Basle, it rests upon nearly horizontal beds of molasse, and it has here an elevation of more than 1100 feet above the sea, which is more than 900 feet above that ridge of loess that stretches between Bonn and Riungsdorf. In a section exposed at Bruder Holz, he found the usual terrestrial and aquatic recent shells, and along with them two vertebra, which M. Agassiz says belong decidedly to a small species of the Squalide, or Shark family, perhaps to the genus Lamna. Mr. Lyell has been so good as to allow me to have figures taken of these organic remains, the first ichthyolites hitherto found in the loess and so remarkable in a freshwater deposit*. | * See Plate XXIX. Mr. Horner on the Geology of the Environs of Bonn. ATG Ascending the valley of the Neckar, he found a section near the Manheim gate of Heidelberg, exhibiting alternating layers of loess and gravel, to the thickness of 12 feet. He saw it near Heilbronn at an elevation of 500 feet above the level of the sea, and was informed that it lies on the hills in that neighbourhood, 300 feet higher. Further up the Neckar, at Canstadt, near Stutgardt, it overlies a freshwater formation of tuff travertine and marl, and south-east of Stutgardt, between Géppingen and the little watering-place of Boll, he found it in a valley watered by a small tributary of the Neckar. From Géppingen his route lay eastward hy Weisenstein and Heidenheim to Nordlingen, and between Weisenstein and Heidenheim he crossed elevated land, on the west side of which the waters flow to the Rhine, on the east to the Danube, and eastward of this ridge no more loess was to be seen. Returning again to the tributaries of the Rhine, in proceeding westward from Bamberg in Bavaria, he found the loess at Dettelbach, a small town on the Mayn, eastward of Wiirtzburg ; and not only in the valley, but on the neighbouring hills of muschelkalk, at a height of five or six hundred feet above the valley. It was here of a somewhat redder tint than in Wiirtem- berg, and Mr. Lyell conjectures that the colouring-matter may have been derived from the neighbouring red bunter-sandstein. Lower down the Mayn, he again saw the loess at Hochst below Frankfurt, and at Soden, where it abuts against the elevated grauwacke ridge of the Taunus. Crossing the Taunus to the valley of the Lahn, he again found the loess at the village of Elz near Limburg. ‘On the north of this village,” he says, “is a hill, which forms one boundary of the valley of the Lahn, and here loess is seen with all its usual characters, with many land and freshwater shells, and alternating, as at Heidelberg, with gravel. I observed, in par- ticular, a horizontal layer of white quartz pebbles, a foot and a half in thick- ness, resting on a mass of loess fifteen feet thick, and covered by loess five feet in thickness, the loess, in both situations, including in it entire shells. Follow- ing the road, I found the slope of the hill above to consist of horizontal beds of quartz pebbles, which have a base of loess. Hence it appears that the valley of the Lahn, which is excavated through highly inclined greywacke, has, at some period since its excavation, been partially filled up with beds of gravel al- ternating with loess, a great part of which has since been removed by de- nudation.”’ It is material to observe that all the above-mentioned places, where Mr. Lyell observed the loess, have a direct communication with the main valley of the Rhine ; that is, form part of one hydrographical basin. The quantity left bears but a small proportion to the mass which we must suppose to 3Q2 478 Mr. Horner on the Geology of the Environs of Bonn. have been originally deposited. It has been shown that the great avidity with which it absorbs water, renders it liable to be easily washed away ; and accordingly, wherever it is not protected by the form of the land, or by a dense covering of vegetation, it is carried off by every shower; and this is in a great degree the cause of the yellow colour and the muddy state of the Rhine after heavy rains. IX. Page 462. In a gravel-pit near Bonn, I found a tooth of the Ahinoceros tichorinus. The gravel is not that yellow alluvium which lies over the brown-coal forma- tion, but resembles that of the present bed of the Rhine, and which I have shown to be older than the loess. X. Page 468. Trachyte tuff is intermixed with the upper beds of the brown-coal forma- tion in the lane between Nieder Bachem and Liessem, on the left bank of the Rhine.—Thomae, p. 49. XI. Page 469. We have seen that from the volcanic focus of this district, limited though it be in extent, products have been erupted which differ very much in their nature, and that these different products must have been ejected at distinct periods. The trachyte tuff appears to have been the first eruption, then trachyte, then basalt, and lastly, the lava and scoriz of the Roderberg, which resemble the ejections of the neighbouring Eifel, and partake very much of the characters of those of active volcanos whose productions have more of an augitic than a felspathic nature. That there was an eruption from the Roderberg subsequently to the com- mencement of the deposit of the loesss, is proved by the thick beds of scorize which are incumbent upon loess near Lannesdorf; and that it had become extinct prior to the termination of that particular deposit is shown by beds of loess covering the volcanic ejections, and still more conclusively by its accu- mulation to so great a depth in the very bottom of the crater; for had the volcano been subsequently in activity, the loess must have been blown into the air. That the edge of the crater must, in part at least, have been under the surface of the water which transported the loess, is manifest, and that collected at the bottom is probably the amount of the solid contents of the fluid which filled the cavity. All the phenomena seem to lead to the con- clusion, that the Roderberg was a subaqueous eruption during the period of Mr. Horner on the Geology of the Environs of Bonn. A79 the loess, and that it was subsequently raised up gradually, en masse, into its present position. XII, Page 470. The additional facts which have come to my knowledge since this paper was read, the most important of which are narrated in the preceding notes, have led me to modify in some degree the opinions I had formed relative to the history of the loess. Its origin remains as uncertain as before; but it is very evident that it came from above Schaffhausen ; and as it is so uniform in its nature through- out, with the exception of the somewhat redder tint of that at Dettelbach on the Mayn, which may have been produced by some local intermixture, it is fair to presume that it was derived from one source. Do its characters indicate that it was brought down by the water of the Rhine, and was deposited gradually during a long period ; or, that it sub- sided in a vast lake, into which the Rhine then entered, as the Rhone now does into the lake of Geneva, and whose waters ran up into all those sinu- osities of the land where remains of the deposit are still to be found? or, do they point to the sudden rush of a muddy torrent, occasioned by the bursting of a barrier which drained a vast lake, as I have already suggested ? The generally homogeneous unstratified nature of the loess, even though in masses between 200 and 300 feet in thickness, always appeared to me to be strongly presumptive evidence that it was deposited from a flood of water densely loaded with mud, and moving with a velocity sufficient to transport its solid contents to a distance so great as that from Basle to Bonn, before they had time to fall to the bottom ; but the alternations of loess with gravel in the valleys of the Neckar and the Lahn, and with volcanic ejections around An- dernach, the Laacher See, and the Roderberg, show that, if it was a flood, there must have been more than one. Were the idea of a lake at all admissible, there would be nothing extra- vagant in supposing that the loess near Basle, which is more than 1100 feet above the level of the sea, and that of Bonn, which is less than 200 feet, might have been deposited in one and the same lake ; for it is only sup- posing the water at the latter place to be 900 feet deep; and the lake of Geneva, according to Mr. De la Beche, is in some places 984*. But if the loess were a gradual deposit from the waters of a lake, there would surely have been indications of successive layers in the structure of the loess itself; the shells would have been found more frequently in something like a similar * Manual, 3rd edit. p. 22. 480 Mr. Horner on the Geology of the Environs of Bonn. mode of arrangement, in place of being scattered, as they generally are, without order through the mass; and vegetable remains would not have been entirely wanting ; or so rare, if they do exist. ‘Then there must have been a barrier to contain the waters of the lake, at the head of the delta of the Rhine near Bonn, and that barrier must have been wholly swept away ; but a country with forms more unlike those which we might expect, had such a barrier ever existed, can hardly be imagined. All the appearances of the Rhine valley favour the supposition that, at the time of the deposit of the loess, there was a free river communication be- tween Basle and the sea, and the vertebra of the Lamna certainly render that supposition more probable. ‘It may seem very extraordinary that the first remains of fossil fish obtained from this freshwater silt should belong to a marine genus, but M. Agassiz has informed Mr. Lyell that both in the Se- negal and the Amazon certain species-of the Shark and Skate families (Squa- lus and Raia, Linn.) have been known to ascend to the distance of several hundred miles from the ocean, and analogous facts are referred to in Mar- grave and Pisa’s Natural History of India *.”’ In a work descriptive of Bonn and its neighbourhood +, there is the fol- lowing statement. ‘The chronicle of Bonn further informs us of a visit to “our river from an animal of the remote north; a sea monster, whose appear- “ance may be brought forcibly before our imagination by the steam-boat of ** modern days, as it works its way through the waters of the Rhine. In the be- *‘ ginning of the year 1680, a Sea Cow, or Walrus, more than fourteen feet in “length, was seen swimming up the Rhine past Bonn. A violent and unheard- “ of agitation of the water was observed, accompanied bya loud noise, and by “ two lofty jets of water spouting from the forehead of the monster. The whole **town rushed to the river to see the great beast, the very name of which was “then unheard of bythem. The centinel on the Alten Zoll fired at it several ‘times but missed it, and the animal proceeded on its way upwards undis- “turbed, and is said to have got above Strasburg. ‘Two months afterwards, it “‘was cast ashore dead, near the village of Niel, about three miles below Co- *‘logne, with four wounds from bullets below the head ; but it was not known “by whom or where it had been killed.”’ In the present imperfect state of our knowledge, there seems to be no explanation, upon the whole, so rational as that suggested by Mr. Lyell in the Address above alluded to, who says, “ Instead of supposing one continuous * Geological Society’s “ Proceedings, ” vol. ii. p. 222. + Hundeshagen, Die Stadt und Universitit Bonn am Rhein, mit ihren Umgebungen. Habicht, Bonn, 1882, p. 15. Mr. Horner on the Geology of the Environs of Bonn. 481 “lake of sufficient extent and depth to allow of the simultaneous accumulation “ of loess at all heights and throughout the whole area where it now occurs, I “ conceive that subsequently to the period when the countries now drained by “the Rhine and its tributaries, acquired nearly their actual form and geogra- “ phical features, they were again depressed gradually by a movement like that “now in progress on the west coast of Greenland. In proportion as the whole «« district was lowered, the general fall of the waters between the Alps and the “ ocean was lessened, and both the main and lateral valleys, becoming more “ subject to river inundations, were partially filled up with fluviatile silt con- “ taining land and freshwater shells. After this operation, when a thickness of “many hundred feet of loess had been thrown down slowly,and in the course of “many centuries, the whole region was once more upheaved gradually, but “ nerhaps not equally, throughout the whole region. During this upward move- <«‘ ment most of the fine loam was carried off by denudation to such an extent that _ the original valleys were nearly re-excavated. The country was thus restored * toits pristine state, with the exception of those patches of loess still remaining, “and which, from their frequency and their remarkable homogeneousness of “composition and fossils, attest the original continuity and common origin of “the whole. By introducing such general fluctuations of relative level, we may “dispense with the necessity of erecting and afterwards removing a great “barrier more than 1200 feet high, sufficient to exclude the ocean from the “valley of the Rhine during the accumulation of the loess.” Sweden has afforded the most unequivocal proofs that upward and down- ward movements of the land may take place in countries where no ordinary volcanic action is to be seen ; and that so gradually, as to be imperceptible to all who are not watching the phznomenon : and, as there are so many in- dications of volcanic action in early times, on both sides of the Rhine valley, it does not seem to me to be stretching theory beyond the limits of just phi- losophical reasoning, to suppose that such oscillations may have taken place in this district, during the gradual accumulation of the loess, and subsequently to its deposition. END OF VOL. IV. pl, vl aiieoht rit! Hip vided et — i re is if iy A veh i oh 7 f sini) oe nk bile Py My BLY ‘i Paty diode } mL isi: RET RITRS 1 ‘bowie alll whey 48 al r ies, ew | ae oS ge, ie AARAU, pisolitic iron ore of, 350. Afton Down, Isle of Wight, section at, 200. Agassiz, M., on the fishes of the Wealden, 180. , examination of Mr. Horner’s speci- mens of fishes from the environs of Bonn by, 474, Aketon, notice of carboniferous rocks within area of new red sandstone near, 393. Aldbury, Shropshire, account of section of new red sandstone near, 400. America, deposits in lakes of, compared to the Wealden, 325. Ammonites, fragment of, found in the Weald clay, Isle of Wight, 205. Amygdaloid of the Dukhun described, 423. , remarkable varieties of, 424. Anticlinal lines in Kent and Surrey, 142, 143, and note. in South Wiltshire, 244. - in the vicinity of Bristol, 244, note. Aptychus: see Trigonellites. Aqueous action, degradation by, of the solid por- tions of the earth, in a certain sense constant, 67. Araucaria, cone approaching to, found on the shore of Portland Island, 349. Argillaceous deposits of brown coal formation in the environs of Bonn described, 448. Arkendale and Swaledale, general account of me- talliferous hills between, 94. Arran, observations on red sandstone systems of, 402, Axes of coal fields of Bristol Channel, not parallel, 57. Aylesbury Vale, strata of, 284. B. Babington, Mr., on trap in the Mysore referred to, 429. Bacon-hall, near Lulworth Cove, good section of the lowest Purbeck strata there, 223. Barbon coal-pits, section in shaft of, 76, note. “ Bargate-stone ” of Surrey, a calcareous conglo- merate, 146. Barkin to Casterton High Fell, notice of section from, 95, Barker, Mr., on chalk in Rutlandshire, 308, and note. Barrowmouth, notice of new red sandstone series near, 395, 396; of magnesian conglomerate, 395. Barytes, sulphate of, found near Caxton, 306, note. — in the Fuller’s earth of Nutfield, 141. Basalt of the environs of Bonn described, 443- 445, , age of, with re- ference to the trachyte, 467. , ho fragments of, found in the brown-coal deposit, 468. Dukhun, varieties described, 414— 423, en boules, very generally diffused, 417. » resembles that of the Solfatarra, 417. oe ees a » columnar, 414, » remarkable natural pavement of, at Singhur, &c., 416, ———, compact, of a green colour, 422. —E———————— ——— Statesand other pieces of sculpture formed of it, 422. 3R 484 Basalt of the Dukhun, extraordinary heaps of loose masses of, described, 421. —-— dykes in the Dukhun described, 418. — in general transversely prismatic, ——_——_—-, remarkable one at Hurreechun- durghur described, 418. —_———-—— common in the Siebengebirge, 445. Basterot, M. De, on the vicinity of Folkstone, 106. Baw Fell, notices of structure of, 88, 96. to the Howgill Fells, account of section from, 96. Beaumont, M. Elie de, reference to his memoir on the boundaries of the Paris and London basins, 530. Beck, Dr., of Copenhagen, on a deposit in the Isle of Bornholm containing plants like those of the Wealden, 330. Bedfordshire, beds below the chalk in, 269. —_—_—__-—_____—___,, fossils of, 296, 316. Belemnites, enormous deposits of, in the lias in Dorsetshire, 31. Bell, Thomas, Esq., F.G.S., observations by, on a new fossil species of Chelydra, 379. Bembridge Down, Isle of Wight, section at, 187. Ben How Quarry, notice of, 396. fault by which it is traversed, 396. Benett, Miss, Cycadedidea procured by, from Tisbury, 15. ee » notice of catalogue of Wiltshire fossils by, 255, 256, 257. ——, specimens of gum or resin ob- tained from the gault near Crockerton, 257. Bere Head, Devon, section of the coast at, 234. Berkhampstead, Vale of, its general altitude, 283. Berkshire, beds below the chalk in, 269, 270, &c. Berthier, M., analysis by, of green particles, 109, note. Birds, bones of, found in the Hastings-sand at Tilgate, 180; distinguished from those of Pte- rodactyles, 382*, Bishopstone, near Aylesbury, section at, 287. Black glossy slate of Cumberland contains no organic remains, 48, 66; probable cause of their absence, 66. INDEX. ‘«‘ Black land”, Gault so called, in Surrey, 141. Black limestone group between Kirby Stephen and Penigent described, 73. distinguished by regu- larity of stratification, 73. —— — , organic remains found yields a fine black marble, where found, 73. Blackdown Hills, Devonshire, description of, 235. , fissures from dislocation at,235. ——,, list of quarries , Sithestone pits, section of, 236. , Sithestones, mode of preparing, 2318 Blackdown-sands, list of fossils from, 239. —_—____—__———,, fossils of, well preserved, why, 238. » principally converted into chalcedony, 239, note. Blackgang Chine, Isle of Wight, section at, 194. Blackstone Edge, notice of great saddle of mill- stone grit at, 60. Boblaye, M., notice of his memoir on the beds below the chalk in the North-west of France, 330. Bonn, Leonard Horner, Esq., on the geology of the environs of, 433. , district little known to geologists, 434. , general structure of the environs of, 435. » grauwacke, 436. ——, trachyte, 437. ——, basalt, 443; volcanic eruptions, 446. — —., brown-coal formation, 447, 473. , loess, 447, 469, 474, 479. ——, mineral waters, 403. , relative ages of the sedimentary rocks of, 464. the volcanic, 467. ——_——$<_$—_——___—______ volcanic rocks to each other, 467. , table of heights, 471. ——, Appendix, 472. ————-— to INDEX. Bornholm, Isle of, affords plants like those of the Wealden, 330. Bothenhampton and Bridport Harbour faults, 40. Boughton quarries, in the lower green-sand, 132. » remains of Iguanodon found at, in- cluding new portions of the skeleton, 132, note. Boulonnois, strata connecting the Kimmeridge clay with the Oxford oolite, well disclosed on the coast of, 332. , Portland-stone in, 326. , nodules of grit in the Portland sand, 283. Bowstead, Rev. James, notice of his observations on the north-eastern demarcation of new red sandstone series in Cumberland, 384, note. Bray, Pays de, (near Beauvais, ) equivalent in, of the Wealden, 326. Portland-stone, 328. a of the Portland-sand, 328. Breccia, in Dorsetshire, accumulations of, analo- gous to those of Normandy, 8. of the , tertiary, siliceous accumulations of, in Dorsetshire, described, 5. Bredy, physical features of the Vale of, 32; geo- logical structure of, 32. Bridport, occurrence of oolitic breccia near, 31. —— Harbour and Bothenhampton faults, 40. Brill, Bucks, strata at, 279, 280. Bristol Channel coal fields, axes of, not parallel, Dive , elevation of the car- boniferous system of, less than that of the North, 59. , form and direction of dislocations in the, have little resemblance to those in the North, 58; disturbing action pro- bably not contemporaneous, 58. which gave final configuration to, probably posterior to deposition of lower new red sandstone, 58. ——_—-—., movements Bristol coal-fields, overlying deposits of, analogous to series in the North of England, commencing with magnesian conglomerate, 58. A85 Bristol Institution, collection of Blackdown fossils belonging to, 239. Broadfield, notice of a mass of carboniferous lime- stone within the area of new red sandstone, near the middle of, 391. Brongniart, M. Adolphe, on Cycadedidea, 218. ——_—_—————— on the fossil plants of Hoer in Scania, 330. Brook Chine, Isle of Wight, section at, 194, 200. Brough, account of the fault near, 62. , coal measures near, sometimes resemble new red sandstone in colour, 387, and note. , new red sandstone conglomerate near, described, 385. Brown coal formation of the environs of Bonn, 447. le scription of the argillaceous deposits, 448. ———--——_—— .,, of the siliceous, 448. oo HOt the lignite beds, 449. —-= more recent than the plastic clay, 466. ——_ — — —, its age a criterion of the period of the ejection of the unstratified rocks of the Siebengebirge,466. , thick- os ness of, near Brihl, 458. — —— —— exists extensively in the volcanic region of the Sie- bengebirge, 466. — — » vege- table remains of the, examined by Prof. Lin- dley, 451. > ore ganic remains of described, 450; vegetables, 450-452, 464; fishes, 452; insects, 453; rep- tiles, 453; quadrupeds, 454. eS ee ie see Lignite. Broun, Prof., fossil fishes in the brown-coal for- mation of the environs of Bonn described by, 452. Brown, Robert, Esq., his specimens of vegetable remains from the lignite of Bonn, referred to, 474. 3R2 486 _ INDEX. Brown, Robert, Esq., silicified wood of Portland examined by, 222. , examines a cone approach- ing to an Araucaria, from Portland, 349. —, his observation respecting the Conifer and Cycadee of Portland, 225% Buchanan, Dr., referred to, on various points of Indian geology, 420, 427, 429, 430. Buckinghamshire, beds below the chalk in, 269. , fossils of, 296. Buckland, Rev. Dr., on bones of the Iguanodon near Swanage, 207. , on Cycadee in the Dirt-bed of Portland, 14, 218. , notice of his memoir on the Valley of Elevation in North Wiltshire, 263. Buckland, Rev. Dr., V.P.G.S., and De la Beche, H. T., on the geology of the neighbourhood of Weymouth, 1. , paper referred to, 217, 233. Burrels, notice of new red sandstone conglome- rate near, 386. C. “ Caillard,” or crow-limestone, description of, 74. owes its existence to shells, 75. Caithness schist, proved to belong to the old red sandstone, 402, 406. , ichthyolites of, placed on the pa- rallel of the Herefordshire cornstones, 404. Calcareous grit formation, near Weymouth, 25. Calcareous slate and limestone, band of between the green slate and grauwacke of Cumberland, described, 49; range of, 50. eee , faults which affect it, 50, et seq. Se ——— generally marked by valleys, 52. » Notice of the for- mations associated with, 48. —— ——, order of their succession, 48. Calcareous slate and limestone of Cumberland, order of beds associated with, first determined by Mr. Otley, 48. sometimes passes into strong beds of limestone, containing many fossils, 68*. the limestone breaks with faces parallel to the cleavage of the slates, 68*. exhibits without exception true cleavage planes, 68*. lines of stratification often almost obliterated by the cleavage planes, 68*. , cleavage planes dip N. W., 68*. sometimes strike with the beds, sometimes obliquely, 68*. ——— nowhere coin- cide with the planes of the beds, 68*. rs cut off by Shap granite and por- phyry, near Wastdale Head, 54, 68*. _—— reappear as calcareous conglo- merates imbedded in greywacké, 68*. Calder, Mr., referred to on points of geology of India, 419, 426, 428. Cambridgeshire, beds below the chalk in, 303. $$ —___ _—____. ; fossils of, 316. Cam Dod, top of, a peat moss, 91. Cam Fell, nature of beds forming flanks of, 91. Candern in the Brisgau, marine beds there, sup- posed to be coeval with the Wealden, 330. “Cap”, a remarkable bed in the lower Purbeck strata, so called, 222. , section of, at ‘* Bacon-hall”, 223. Carbonaceous shale and fissile gritstone, group consisting of, described, 75. , subdi- visions of, 75, contains a bed of coal, 75. Carbonate of lime, fibrous, in the Purbeck beds on the coast of Dorset, 11. Carboniferous chains of Cumberland, Professor Sedgwick on the dislocations which have sepa- rated them from the Cumbrian mountains, 47,56. , physical features of, contrasted with those of the slate district, 47. INDEX. 487 Carboniferous formations of the North of En- gland, deposited during a long period of com- parative repose, 56. Sanne succeeded by one distin- guished by remarkable convulsions, 57. effects of, 57. —_—--————— first elevation of, suc- ceeded by the deposition of lowest members of new red sandstone, 58. movements which gave the chief impress to the, anterior to principal dislocations of the south-western coalfields, 58, 59, note. Carboniferous chain between Penigent and Kirby Stephen, Prof. Sedgwick on the, 69. forms a mineralogical link between High Peak of Derbyshire and region of Cross Fell, 69, 98. general section of the forma- tions composing the, 70, 83. contains six bands of lime- stone, 70, 73, 75, 76, 78, 79. ee divisible into three groups, 99. -, lowest, almost identical with mountain limestone of Derbyshire and Bristol, 99. » middle, conforms to portion of Cross Fell carboniferous system, 99. $< —_ —__—______—., third, or millstone grit, common to carboniferous system of England, 99. , conclusions drawn from structure of, 99. between Penigent and Kirby Stephen, causes disturbing the formation of the limestone beds, were in full action in the valley of Tweed, during the whole carboni- ferous period, 99. ————— in York- shire had produced considerable effect before complete development of the formation, 99. in Der- byshire, and the south-western coalfields pro- duced but small modification, 99. Carboniferous chain between Penigent and Kir- by Stephen, beds of, slowly deposited in a sea of considerable depth, 100. contains no freshwater shells, 100. » fossils of distinct species, not confined to particular beds, 100. , sudden change in, accompanied by change in mineral cha- racter, 100. , Trilobites, Ammonites, and Orthocera not found above the scar lime- stone, 100, note. , bottom beds of the calca- reous groups impure, 101. contain few fossils, which are small, 101. do not ge- nerally alternate extensively with shale and sandstone, 101. , top beds of calcareous groups; fossils numerous and large, alter- nate universally with shale and sandstone, 101. —_—___—_—___——_-——, inferences _respect- ing, 101. » grit and sandstone groups of mechanical origin, and less continuous than the limestone, 101. , valleys in the carbonifer- — ous chain are valleys of denudation, 101. group, opinion of the Germans, that it forms only a part of a great system, in- cluding the new and old red sandstones, advo- cated, 401. series, detached masses of, within the area of the new red sandstone in Cumber- land, 391—393. —___- ______——, causes which may account for the appearance of detached portions of, within area of new red sandstone, 391. strata in Cumberland not always distinguishable from the new red sandstone by colour, 387, and note. Carrock Fell syenite, boulders of, on shores of Solway Firth, 388. 488 Carrock Fell syenite, mixed with boulders from Dumfriesshire, 388. “ Carstone” of Norfolk, what; places of its oc- currence, 313. Casterton High Fell, account of beds forming the flank of, 96. oe to Barkin, section from, 95. Caumont, M. de, notice of memoir on beds below the chalk in Normandy, 330. Caxton, sulphate of barytes, found near, 306, note. Central carboniferous chain, account of the dis- locations by which the Cumbrian mountains became separated from the, 56. Chalcedony, veins of, frequent in the sheets of bare rock in the Dukhun, 422. Chalk Beck, notice of mass of carboniferous lime- stone within area of new red sandstone in, 392. Chalk, cavities in, filled with chalk flints, clay, and sand, at White Nore, 6. — and Oxford oolite, general composition of strata between, in the South-east of England, 104. on , arrange- ment and list of, 105. —, decline of its summits from Bedfordshire to Norfolk, 303, &c. -, its thickness in the South-east of En- gland estimated, 318. -, remarks on its distribution and charac- ters in the South-east of England, 322. —, fossils of, in West Norfolk, 312. — —-, inclination of, atthe Hogsback, Surrey,145. — on the coast of Dorsetshire described, 8. — near Dunstable, 293. —-— from Dunstable into Norfolk, 305. , its course through Hertfordshire, 296. ——- cut through at Diss in Norfolk, 311. — at Mildenhall in Suffolk, 310. —- in West Norfolk, 311; Cliff, 314. — in Oxfordshire, 270, 271. -, supposed outlier of in Rutlandshire, 308. at Hunstanton —, the red strata at Speeton, in Yorkshire, referred to it, 315, note. —, red, at Hunstanton Cliff, 314. ———~ in Lincolnshire, 310, note. - on the north-east of Swindon, 264, 270. INDEX. Chalk, fragments of, at Sywell in Northampton- shire, 308. —, lower, near Tetsworth, fossils of, 296. in the Vale of Wardour, 245. — in the Isle of Wight, 182. ** Cheesecakes ”, beds locally so called in Bucks, 289. ; Chelydra Murchisonii, a new fossil species from (Eningen, memoir upon by Thomas Bell, F.G.S. (Pl. XXIV.), 379, ——_—____—___—, detail of its proportions, Serpentaria, comparison of with C. Murchisonii, 380. , its habits described, 380. Chemical combination may be cause of volcanic combustion, 68. » each successive action of, would tend to ultimate quiescence, 68. Chert, concretions of, in sand, of subsequent for- mation, 121. Wi 75 WAU. , in the lower green-sand, -——, following lines of false stra- tification, 120. ,hotice of beds ofshivered, near Weymouth, 7. Chideock Hill, notice of loose breccia in the in- ferior oolite on the summit of, 7. Chichester, earthquake around, in 1834, 155, note. Chicksgrove, in the Vale of Wardour, section at, 251. Clapham to Penigent, notice of a section from, 94. Clay, ferruginous, beneath basalt in the Ghats of the Dukhun described, 419. , remarkably tabulated, in the Dukhun de- scribed, 417. see Gault; Kimmeridge-clay; Oxford- clay; Weald-clay. **Clunch” of Cambridgeshire, what, 305. Coal-formation, resemblance of part of the Weal- den to, 333. Coal, gritstone and shale, group consisting of, near Penigent, described, 79 ; subdivisions of, 79. Coal measures of Whitehaven were disturbed in part anterior to the new red sandstone series, 397. INDEX. Coal seams, persistence of, in the Valley of Dent, 101, note. * Cologne earth” prepared from an earthy lig- nite, 459, note. - -- Combe-Wood, Oxfordshire, oolite containing freshwater shells found there, 275, 276. Composition of strata between the chalk and Ox- ford oolite, general remarks upon, 332, 333. Concretions, formation of, 121. , an accident illustrating, 121, note. of chert, near Sandgate, following lines of false stratification, 120. , coproid, of phosphate of lime, in the Gault, 111, and note. Cone, approaching to an Araucaria, found on the shore at Portland, 349. of an unknown species, from the Hastings- sand, (Plate XXII.-fig. 10.), 181. - —_—_—— from the Isle of Pur- beck, (Plate XXII. fig. 9.), 230. Conglomerate of new red sandstone near Brough, Kirby Stephen, Burrel, &c., described, 385. -— forms lower part of series, 386. not to be distinguished from the dolomitic conglomerate of Mendip Hills, 385, 399. Conglomerates of the lower green-sand in Kent, of what composed, 118. Concan :—see Konkhun. Coniferz, silicified trunks of, found in the “ Dirt- bed” of Portland, 13, 222, 230. es —, wood-cut of a re- markable trunk, found in Portland, 221. , some microscopic characters not con- fined to them, 222. : accompanied in Portland by Cycadez, a nearly related family, 14, 225, 230. at Swindon, above the Portland stone, 269. , petrified, found in the Lower green- sand, 131. 229. Coniston Water Head, account of faults between, and Windermere, 52, 67*. Hastings-sands, A89 Contortions and faults in the Weymouth district, 35. Contraction produced by diminished temperature may explain some of the great parallel corru- gations, 67. Conybeare, Rev. W; D., indicates the group pro- posed to be called Portland-sand, 210. » his account of the Ox- ford oolite referred to, 274. Coprolite, masses resembling, found in the Gault, 111 and note, 368 note. green- sand, over Weald-clay, 181. Copt Point, Kent, its composition, 107. -, view of, from the east, (Pl. X. b. fig. 1.), 106. Coral rag, Professor Sedgwick on the, 26, note, 213, note. Coralline or Oxford-oolite, near Weymouth, de- scribed, 23; its composition, 25; its extent, 27. , very ferruginous cha- racter of the upper beds, near Weymouth, 27. Cordier, M., reference to his notes on the Pays de Bray, 327. Cornbrash, notice of, near Weymouth, 28. ‘© Cornstone” beds, locally so called in Bucks, 288. Coulthard, Capt., referred to, on points of Indian geology, 418, 420, 426, 428. Cowleaze Chine, Isle of Wight, section of the Weald clay at, 197, 198. Crow-limestone, or caillard, description of, 74. -_________...___.___. owes its existence to shells, 75. Craven fault, description of, 90. , under Baw Fell, 97. , at Clapham Beck, 95. , at Short Gill, 96. ——— ———————, near Fhornton Force, 95. 89. , near Wild Boar Fell, , account of effects produced by, 60. , intersection of, with the Cross Fell Fault, 63. 490 Craven fault, notices of Mr. Phillips’s account of, 60, 95, 98. Cross, mountain so called, not to be confounded with Cross Fell, 92, note. Cross Fell, notice of fault near base of, 62. — fault, effects produced by intersection of, with the Craven fault, 63. Crystalline structure of primary slates, not al- ways effect of igneous action, 65. -_——_—— of secondary rocks some- times due to chemical action, unaided by ig- neous cause, 65. —_—____-—__-, instances of, stated, 65. Cumberland, order of beds associated with band of limestone and calcareous slate in, 48. ——, Professor Sedgwick on the new red sandstone series on the north-western coast of, 383. , position and peculiar structure of the schists of, due to causes in action prior to old red sandstone, 49,55, 65. Cumbrian mountains, Professor Sedgwick’s in- troduction to an account of the general struc- ture of the, 47. , parallelism of, to the chains of Cornwall, North Wales, &c., 56. , central portions composed of rocks anterior to the old red sandstone, 47. , outskirts covered by de- posits chiefly of the carboniferous order, 47. » notice of formations consti- tuting the central portion of the, 48. , order of succession of the stratified deposits, 48. — ———~ , first determined by Mr. Otley, 48. , older and newer systems of, entirely unconformable, 55. » no gradations be- tween, but abrupt transitions, 55. —— , Mineral axis consists of un- stratified crystalline rocks, 49. ——_——_—_——__—————__., formations on the sides of, arranged symmetrically, 49. » general strike of formations composing the chain, 49. INDEX. Cumbrian mountains, great dislocations by which they became separated from the central carbo- niferous chain, 50. oe , elevation of the old slates of, produced by protrusion of granite and sy- enite, 67. » elevation, sudden, 55; suc- ceeded by a long period of comparative re- pose, 56. » crystalline slates of, pro- bably owe their structure in part to igneous action, 65. —_—_————,, northern and southern cal- careous zones of, cut off from the central chain, by the same fault, 61. , inferences deduced respect- ing, from the phenomena accompanying the band of limestone and calcareous slate, 54. ——, as concerns the valleys, 54. ———————,, boulders from, occur in South Lancashire, Cheshire, and Denbighshire, 390, note. Cycadez, in the ‘ dirt” above the “Cap” of Port- land, 220, 222. found also in a second bed of dirt, below the “Cap”, 223; a large specimen described, ibid., note. not hitherto found at Chicksgrove or Wockley, 254. Cycadedidez of Dr. Buckland, two species, found in Portland, 230; found by Miss Benett at Tisbury, 15. Cypris Valdensis, (P]. XXI. fig. 1.), why separated from Cypris Faba, 344. , the genus, perhaps not distinguishable, in the fossil state, from Cytherina, 345. , other species of, 177, 260, 345. Cytherina, a marine genus of Crustacea, near to Cypris, 333, note; 345. D. Dangerfield, Capt., on a tradition respecting a shower of earth, by which Oogein was de- stroyed, 428. INDEX. Dangerfield, Capt., on various points of Indian geology, referred to, 410, 414, 416, 418, 420, 424, 425, 426, 428. the great extent of the trap formation in the Peninsula of India, 428. Davy, Dr., notice of a hot spring in Ceylon, 427. , on laterite in Ceylon, 430. Deccan: see Dukhun. De la Beche, H. T., F.G.S., reference to his me- moir on the green-sands of Devonshire, 234. on the coast of Nor- mandy, 330. on marine equivalents of the Wealden, 329. nd er buckland, on the vicinity of Weymouth, 1, 217, Dent, persistence of coal seams in the valley of, 101, note. Denudation producing valleys, account of, in Dor- setshire, 41. Deposits, siliceous, of the brown-coal formation near Bonn, 448. Depressions, geological, in the Weymouth district, 84. Desnoyers, M., notice of memoir on beds below the chalk in the North-west of France, 330. Devakl Unei, hot wells so called in the Konkun, 427. Devonshire, beds below the chalk in, 233, &c. , subdivisions of the green-sand se- ries not discernible in, 233. Diluvium, deposits of,in the vicinity of Weymouth, 44, in the, 44. Dinton, Bucks, quarries at, 285. Dinton, Vale of Wardour, S. Wiltshire, 248. ‘“‘Dirt-bed” near the bottom of the Purbeck series, in the Isle of Portland described, 13, 220. , organic remains occurring of the Isle of Portland affords a mea- sure of the duration of the Portland stone in the state of dry land, 16. , notice of near Upway, 15. Portisham, 15. Thame, 15. VOL. IV.—SECOND SERIES. 491 “ Dirt-bed ”, silicified coniferous trunks found in, 13, 218, 220. , Cycadez found in, 14, 224. , notice of, in the Boulonnois, 15, note. » a second and lower bed of, also con- tains Cycadez, 223. “Dirt, black,” on the Dorsetshire coast, what, 287. “Dirt, black and grey,” clays, so called in Bucks, 290. Dislocations in the coal-fields of Bristol Channel, little resemblance of, to those in the North, 58. , disturbing action probably not contemporaneous with that of the North, 58. , Prof. Sedgwick on the, which have separated the Cumbrian Mountains from the neighbouring carboniferous chains, 47, 56. Diss, Norfolk, section quite through the chalk at, 311. Distribution, local, of the strata between the chalk and the Oxford oolite, in the South-east of England, 321. Disturbances of strata in Buckinghamshire, 285. near Hazeley, Oxfordshire, 286: see “Gulls”. in Portland, 218. near Sevenoaks in Kent, 134, 135. Disturbing forces, their effects, on the coast of Dorsetshire, 32. Dolphin Sty, notice of fault at, 90. Dorking, and Leith Hill, Surrey, tract between described, 143. Dorsetshire, Mr. Webster on, referred to, 1, 206. coast, fossils of, 228. , enumeration of authors on the coast of, 1. , geology of the coast of, 1, 206. eee , the subdivisions of the green-sand strata seen in Hants, Sussex and Kent, not re- cognisable in, 9. , description of tertiary deposits of the coast of, 4. , description of puddingstone in, re- sembling that of Hertfordshire, 5. 358 492 Dorsetshire, greensand formation of, 9. , Hastings sand on the coast of, 11. , Purbeck beds on the coast of, 11. , description of inferior oolite in, 30. —_— —., succession of changes in the coast of, 45. Down Cliff, notice of a conglomerate in the infe- rior oolite, formed of fragments of that rock, $1. Duddon, notice of a fault in valley of the, 51. Dufrénoy, M., notice of his memoirs on the beds below the chalk in the South-west of France, 330. Dukhun, portion of, described by Lieut.-Col. Sykes, 409. ; it sboundanes 1400: —_—_—_——_—_—_ —_—_—. , Stratification of, 410. Ss therGhats orale , the valleys of, 412. ———_—_——_—_—__—_——_——,, not produced by rivers, 413. — eee , terraces, 413. po te eee ee , escarpments of the Ghats in, described, 414, , columnar basalt a great geo- logical feature in, 414. , basaltic and amygdaloidal columns in, 415. , places of their occurrence, 415, 416. , schistose, indurated clay as- sociated with basalt, 417. , basalt en boules (or nodular basalt) of, 417; its localities, 2b. , basaltic dykes of, 418 ; their localities, 2b. , prismatic character of, 418. , ferruginous clay associated with basalt described, 419; its localities, 2b. ——_—_———-——, limestone, three forms of, 419, ——_——__—_——_—_—_—,, pulverulent, 419; its localities, 420. —_—_—__—_———_—,, nodular, 420; its great abundance in certain localities, 420, 430. , crystalline of, 421. INDEX. Dukhun, portions of, limestone, specimen of com- pact found by Colonel Sykes in, 421. , loose basaltic stones occur in immense quantities, 421. » heaps of rocks and stones in the, 421. — , occurrence of sheets of rock in the, 422 ; description of them, 2b. ; their loca- lities, 2b. —, structure and mineral com- position of the trap rocks of, 422. —, a variety of green compact basalt found in, 422; description of it, 423. , prevalence of amygdaloids in certain localities in, 423. -—- ———_--—— , amygdaloid with vermicular stilbite, 424. ————-_—-—-—,, minerals found in the trap rocks of, 424; their localities, 425. ——_ natural saltssoimA2ommanens localities, 425, 426. ———, ores of, 426. a , No organic remains met with by Colonel Sykes, 426. ——_—— —_ ——_—_— , the absence of remarkable, —_———, great extent of the trap re- gion in, 428. , absence of volcanic products ——., age of the trap formation of, ———— —— lateritesolm4oOnmitsmlaea= lities, ib. —_____—_—__——_., granite of, 431. —_____—_—_——,, sedimentary rocks of, 431. » mode of determination of the elevations of, 432. ——, explanation of the sections accompanying Col. Sykes’s paper on, 432, Dunnose, in the Isle of Wight, its true position, 191, note. Dunscombe Hill, notice of pits in the chalk of, filled with flints, 6. Dunstable, Bedfordshire, section through, 292. Dunton, Bucks, quarries of Portland stone at,272. INDEX. Dykes, basaltic, in the Dukhun described, 418. , aremarkable one at Hurreechun- durghur, 418. -, of the Siebengebirge, 445. E. Earthquake around Chichester, in 1834. 155, note. Eden, account of cleft, called Span of, 385. , description of a longitudinal section from Penigent to the plains of the, 84. ——, Professor Sedgwick on the new red sand- stone series in the basin of the, 383, et seq. —-, sterile sandstone in valley of, the parallel of forest sand of Nottinghamshire, 387. Elevation, effects and phenomena of, in the neighbourhood of Weymouth, 32—34. of the northern carboniferous chain, dislocations produced by, 59. marked by asystem of longitudinal faults, 59. —, great changes of level among the strata during, 63. —_—_—__—________—_—, fractures produced by, sometimes inclined to each other, 63. probably produced by protrusion of the Cheviot porphyries, the Charnwood syenite, &c., acted on by volcanic agents, 63, 64. ——_—__—____————— produced by vio- lent action, and of short duration, 64. Elephants’ teeth, occurrence of, in the diluvium of Dorsetshire, 44. Elie de Beaumont, his theory of epochs of ele- vation supported by position of the older for- mations in British Isles, 56, 65. ——, coal-fields of Bristol Channel, exceptions to, 57. Endogenites erosa, found in the Hastings-sand near Hastings and St. Leonard’s, 167, 168. —, its external forms, (Plates XIX. and XX.,) 172; internal structure, 175. England, general comparison of the red sandstone series of, with that of Scotland, 402. —, probable appearance of, if laid dry im- mediately after the carboniferous period, 56. 3f 493 England, South-east of, Dr. Fitton on the strata between the chalk and Oxford oolite in, 103, et seq. , succession of geological events in, 45, 320. Eruptions, volcanic, of the Siebengebirge, 468 ; of the Roderberg, 2b. Everest, Rev. Robert, on trap between Calcutta and Ghazipoor, referred to, 429. Exeter conglomerate may be equivalent of upper part of lower red sandstone of Yorkshire,403. Exogyra (Gryphza) virgula, found in the Kim- meridge-clay of Buckinghamshire, 273. F. Farlton Knot, dislocation near, not leading branch of Craven fault, 60. Farnham, Surrey, section near, 144, Faults, account of, on coast between Parton and St. Bees Head, 393, et seq. at Bothenhampton and Bridport Harbour, 40. — and contortions in the Weymouth di- strict, 35. — at Osmington and Ringstead Bay, 39. , notice of, respecting the band of lime- stone and calcareous slate of Cumberland, 50, et seq. ——_—_—_————_——— generally marked by valleys, 52. Felspar, glassy, resembling Cleavelandite, in amy-~ gdaloid, in the Dukhun, 424. Fenny Stratford, section through, 292. Firestone, (Upper green-sand,) section of, near Godstone, 137. near Merstham, 140. at Reigate, 137. First millstone grit, description of, between Peni- gent and Kirkby Stephen, 81. Fishes, fossil, of the Gault, 203, 259. Weald clay, 180, 206. examined by —— M. Agassiz, 180. ~ Hastings sand, 180, 206. Purbeck strata, 230, 260, 298. 352 AO Fishes, fossil, of the Portland stone, 261, 300. Portland sand, 231. Kimmeridge clay, 232, 303. Fissile gritstone and carbonaceous shale, descrip- tion of beds of, between Strong Post and Mosdale limestones, 75. ——_—, Mosdale Moor and Four-fathom limestones, 77. , most important of the groups al- ternating with the limestone series, near Pe- nigent, 77. E —, subdivisions of, 77. —______-—_—, used as roofing-slate, 78. —_——,, contains two beds of coal, 78. Fitton, William Henry, M.D. P.G.S., “ On Strata between the Chalk and Oxford-oolite in the South-East of England,” 103. ——_—__—___—_—__——__——__, objects and plan of his paper, 104, 105. , table of its contents, 384*. —___________._______ finds the “ dirt-bed” of Portland in the Boulonnois, 15, note. Fitton, W. J., remarkable specimen of Ammonites found by, 152. Flints, accumulations of, due to the action of water, 6. Flinty slate, fragments of, in the conglomerates of the Lower green-sand, 117. Flookborough Spaw, conglomerate of new red sandstone unconformable to mountain limestone near, 589. Flora of the lignite of Bonn, not yet explored, 451, 464. Fog, remarkable appearance in, from the Hogs- back, Surrey, 149, note. Foliated-sand, and clay, remarkable alternation of, 168. Folkstone, vicinity of, strata described, 105. » coast near, view of, (Plate VIII.), 106. Forest marble, description of, in the Vale of Wey- mouth, 28; fossils of, 29; its extent, 29. and cornbrash closely united in the Weymouth district, 3, note. INDEX. Fossils of strata from chalk to Oxford-oolite, lists of explained, 112, note. —_-—_—_—_—_, local distribution of: see the Names of Counties,— Kent, Surrey, Sussex, &c. oe ,- scribed in Dr. Fitton’s paper, deposited in the Geological Society’s Museum, 334, note. » new species of, (Plates XI.to XXIII.), Mr. Sowerby’s descriptive notes upon, 375. » col- of, general inferences not safely deducible from, 334. , Varia- tion of, within short distances, 334. , syste- matic and stratigraphical Tables of, 351—368. , explanation of the Tables, 350. Fossil remains of the Loess of Bonn, 461, 462. Fossil trees in the Isle of Portland, 13,217, et seq. Foundations of geology, are accurate mineralogi- cal distinctions, and order of superposition, 67. Four-fathom limestone, description of, 78. —_—_—___—_—_— variable in thickness, 78. ———__—_—__—___—_— abounds in. encrinital —_—_—__—__—____—_—,, some cherty beds of, con- tain casts similar to the screwstones of Derby- shire, 78. Fovant, Vale of Wardour, section at, 246. Franklin, Major, referred to, on points of geology of India, 418, 420, 426, 428, 429, 431. Fraser, Mr. on the extent of trap in India, 429. Freshwater deposits in England, publications upon, 324, note. , limestone, beds resembling, at the top of the Portland strata; but including marine shells, 333. shells, in oolite, at the bottom of the Purbeck series, in Oxfordshire, 275—276. Fuller’s-earth near Aylesbury, 287. ——_——-— of Bedfordshire, described by Hol- loway, in 1723, 295. INDEX. Fuller’s-earth at Nutfield, Surrey, 141, includes sulphate of barytes, 141. — near Woburn, section of a pit, 294, —————_ , grey clay on the coast of Dorsetshire, probably the equivalent of the, near Bath, 29. G. “ Gault,” a local term in Cambridgeshire ; its meaning, 306. Gault, general remarks on the distribution and. characters of, in the South-east of England, 323. ———, its thickness estimated, 319. , its constancy remarkable, 323. incloses nodules containing phosphate of lime, 111, and note. , bed supposed to resemble, in the Lower green-sand, 142, note. , the red beds at Hunstanton supposed to represent, 312; doubtful, 365, note. , coproid masses found in, examined by Dr. Prout, 111, note. near Aix-la-Chapelle, 323. in Berkshire and Oxfordshire, 271. in the Lower Boulonnois, 323. in Buckinghamshire, 291, note. near Cambridge, its general relations, 306. — not found onthe coast west of Weymouth, on the coast of Kent, described, 109. near Liege, 323. near Leighton and Wing, 294. in Norfolk, 312. ———— near Swindon, 265. near Thame, 279. in the Vale of Wardour, 247. in the Isle of Wight, 184. , fossils of, in Bedfordshire, 296. in Cambridgeshire and Norfolk, 316. ———— on the Dorsetshire coast, 228. near Folkstone, 112. in the interior of Kent and part of Surrey, 152. in the Isle of Wight, 203. in South Wiltshire, 258. 495 Garsington, Oxfordshire, stratification at, 270. » quarries of Portland- Strata at, 277. Geology, foundations of, are accurate mineralogi- cal distinctions, and order of superposition, 67. Germany, central, proofs of identity of new red sandstone system of, with that of England, 399. Ghats, true meaning of the term explained, 409. ~ of the Dukhun, general description of, 411. , escarpments of described, 414, —, sections respecting, (Plate XXVIII.) ex- plained, 432; have a slightly perspective cha- racter, ib. -, some heights in, determined by boiling point of water, 432. Glaisher & M’Lauchlan, Messrs., heights in Cambridgeshire ascertained by, 370. Glennie, Rev. J. D., drawing by, of the coast near Hythe, (Plate VIII.) 106. , drawing by, of Copt Point, from the east, (Plate X. b. fig. 1.) 106. Godalming, Surrey, section at, 146. Godstone, Surrey, section through, (Pl. X. a. No. 2.), 137. —, sectional list of firestone pits near, 137. Goldfuss, Prof., remains of insects in the brown- coal formation of Bonn have been described by, 453. , fossil remains of reptiles in the environs of Bonn described by, 453. Goodhall, H. H. Esq. (deceased), a fossil species, of Nerinea named after, 348. Grauwacke of the environs of Bonn, 436; its lo- calities and extent, 2b. Granite and gneiss regions, in the Peninsula of India, of amazing extent, 428, 431, , its great extent in India mentioned by Dr. Voysey, 431. ———, fragments of, found in the gravel at Muswell Hill, Middlesex, 293, note. of Skiddaw Forest overlaid by crystalline slates, 48. Gravel, angular, account of beds of, near Wey- mouth, 7; referred to the tertiary period, 6, 496 INDEX. Gravel, containing chalk flints, over green-sand, within the Wealden tracts, 153. , remarkable accumulation of, at Muswell Hill near Highgate, Middlesex, 293, note. , superficial, in Bedfordshire, a very exten- sive deposit, 293. ——— of Bucks and Bedfordshire, some fossils of, 296. of Cambridgeshire, of two kinds, 304, note. much conceals the strata in the eastern counties, 304-805. ———., mass of, over the brown-coal formation, in the environs of Bonn, 455. Graystone House, account of the limestone near, 50, and note. Graves, M., “Marbre a Paludines”, in the Pays de Bray, 328. Great Colm (in Cumberland), enumerationof beds composing sides of, 87. — to Ingleton, notice of a section from, 95. Great Ridgeway fault (in Dorsetshire), descrip- tion of the, 36. Great scar limestone, description of, 70; full of fissures, 71. —-—_ ——__ —_—__.-_—_——_ caverns, 71. , not formed by the mere long continued action of water, 71. — SS ,» how some were probably formed, 71. ———— between Penigent and Kirkby Stephen, contains no bands of coal, 72. —, beds of reddish sandstone alternate with, in the lower part, 72. passes upwards by alter- nations into a group of sandstone and shale, 72. Great upper shale, description of, between Peni- gent and Kirkby Stephen, 81. Green matter of the Lower green-sand, analysed by M. Berthier, 108, 109, note. of the green-sands, analysis of, by Dr. Turner, 108, and note. — the same in several different strata, of sand, 108. of the beds above the chalk, 333. Green matter of the Portland-sand, 108. Greenock, Lord, fossils of the Kentish coast col- lected by, 112. Green quartzose slate of Cumberland, notices of, 48. dislocated, but not contorted, 55; and why, 55. Green quartzose slate of Cumberland, contains no organic remains, 48. continuous bed of limestone, 48. —_—_——--——,, supposed origin of the, 55. Green-sand, the term objectionable; but adopted ; why, 105, note. 822. in Devonshire, no subdivisions, 233, ——,, list of fossils, 239. in Dorsetshire, described, 9. —_—______—__—_ reposes_ successively on the Purbeck beds, Portland stone, Kimme- ridge clay, Oxford clay, inferior oolite, lias and red marl, 10. ——_—__—__———___-_-—— in Normandy, on Kimmeridge clay, coral rag, and Oxford clay, 11. Green-sand, Lower, mineralogical nature of the pebbles composing the conglomerate beds, 116, Mr 117, 118. ———___————— easily removed by water, 197, note. includes concretions of chert, , eroded cavities on its surface, containing gravel, 144. , chalk-flint gravel on its sur- face, within the Wealden denudation, 153. , general remarks on its cha- racters and distribution in the South-east of England, 323. a , in contact with Kimmeridge- clay at Little Brick Hill, Bedfordshire, 295. with sand of the Portland strata, at Swindon, 265. , its thickness in the South-. east of England estimated, 319. INDEX. A97 Green-sand, Lower, near Folkstone, subdivided into three, 115. a » Ast, or up- per subdivision described, 116, 118. Bo eee » 2nd, or middle subdivision, 121 ; detail of beds, 123. —__—_—__—__,, 3rd, or low- est, subdivision, 124, 125; contains beds of limestone, 126, 127. » subdivisions of, near God- stone, 137. subdivisions of, near Pulbo- rough, like those of Folkstone, 155. , ridges of, between Seven- oaks and Godstone, 133. near Aylesbury, 285. — in Oxfordshire and Bedford- shire, 271. —_—. in the east of Bedfordshire, 295; subdivisions probably exist there, 295. at Brill, 280. ————— in Cambridgeshire and Nor- folk, 306. at Long Crendon, 282. near Farnham, its thickness and probable subdivision, 145. at Hunstanton, 314. near Leighton, 294. ——_—__—_—_—_—_—_—_——— near Merstham, 141. in Norfolk, 313. in the Pays de Bray, 327. at Quainton, 289. in Surrey, advances by pa- rallel steps, or ranges, 143. near Swindon, in contact with sand of the Portland strata, (wood-cut), 265. near Thame, 279. at Tilburstow Hill, near Godstone, (wood-cut), 138. at Whitchurch, 291. in the Vale of Wardour, 248. in the Isle of Wight, 184, 188, TOT 19552005 » fossils of, in Bedfordshire, 297. Green-sand, Lower, fossils of, near Folkstone, OK in the interior of Kent and Surrey, 152. ae in Hampshire, 157. in Norfolk, 317. —_—_——_—____—— inthe Isleof Wight, in North Wiltshire, 268. — in Oxfordshire and Bucks, 297. Green-sand, Upper, remarks on its distribution, and characters in different places in the South- east of England, 322. ; , its thickness estimated, 318. not prominent between the coast and Godstone, 131. , the firestone beds near God- stone, a part of, 137. in Cambridgeshire, 306. near Folkstone, 107. near Godstone, 137. in Hampshire, 154. at Hunstanton, 314. m1 in West Norfolk, 312. in Oxfordshire, 270. in the Pays de Bray, 327. in the Vale of Wardour, 246. , fossils of, in Dorsetshire, near Folkstone, 108. in Hampshire, 156. in Oxfordshire, 296. in Western Sussex, 156. in the Isle of Wight, 202. in South Wiltshire, 257. in North Wiltshire, 267. Greenstone, large masses of, found on the sur- face near Hunstanton, 314, note. , worn fragments of, in the superficial | gravel of Cambridgeshire, 304. ‘“*Greenstone,” beds locally so called in Bucks, 288. Greywacke of Cumberland contains beds of im- pure limestone full of organic remains, 48. 498 Greywacke of North Devon and part of South Wales, probably elevated after completion of carboniferous series, 57; does not conform to the range of other greywacke chains, 7b. Gritstone shale and coal, description of a group of beds of, between the first and second mill- stone grits, 82. —., between the twelve-and four-fathom limestones, 79. , between the second and upper millstone grits, described, 82. Growth of plants, on former surfaces of the globe, limitation of inferences from, 321, note. Grypheea Virgula—(see Exogyra,) 273. Guildford, Surrey, description of Upper green- sand, &c., near, 144. “Gulls” (or Gullies), cavities so called, in the Portland strata at Great Hazeley, 276. , wood-cut of one, 276. evidently the effect of disturbance, 276. , surface over, not irregular, 276. analogous to cavities in the lower Pur- beck strata, in Portland, and Buckinghamshire, 286; and in the Pays de Bray, 328. Gypseous marls of central England, wanting almost entirely in new red sandstone of valley of the Eden, 387. H. Hailstone, Rev. Mr., on the vicinity of Cambridge, 303, 304, notes. Hamites, remarks on a spiral portion of, by the Rev. Gerard E. Smith, 337. Hampshire, geological features of part of, 153. ** Hardstone,” bed locally so called in Bucks, 290. — contains Paludine, 290. Harter Fell to Wild Boar Fell, account of a sec- tion from, (Plate VI. fig.9.), 97. ** Hassock” of the Kentish quarries, what, 127. Hastings, view of cliffs on the east of, by Mr. Webster, (Geol. Trans. 2nd Ser. ii. Pl. V.), 163. —, cliffs on the west of, great recent altera- tions in, 165, &c. 382*. ————, sectional sketch of (Plate X. b. fig. 3.), 164, INDEX. Hastings, ledges of rock on the coast near, 168, and note. —, great disturbance of the strata near, 169, note. Hastings-sand, a member of the Wealden group, 103. , Junction of, with the Purbeck strata, 208. , ledges of, in the sea, in the Isle of Wight, 186; and near Hastings, 168, note. a , probable outliers of, in Bedford- shire and Bucks, 294, and note. fossils of, (supposed,) in Bucking- hamshire, 297. in Kent, Surrey, Sussex, and Hampshire, 176. near Hastings, contains numer- ous specimens of Endogenites erosa, 172. ,cone of unknown species found in, 181. in Kent, Surrey, Sussex, and Hampshire, 176. on the Dorsetshire coast, 11, 229. in the Vale of Wardour, 248. Haute Sadne, a marine deposit coeval with the Wealden occurs there, 329, 330. ** Hazel-mould,” soil over upper green-sand so called in Surrey, 141. Hazeley, Great, Oxfordshire, quarries at, 276. Headington, Oxfordshire, section at, 278, 279. ‘* Heath,” beds locally so called in Bucks, 289, 296. Heaps of rock, remarkable, in the Dukhun, de- cribed, 421. —, places of their occurrence, 421. Height of the surface of the Rhine at Bonn, 472. Heights, in the Ghats of the Dukhun, (Section, Plate XX VIII.), 411,432; some determined by boiling point of water, 432. —, in the environs of Bonn, table of, 471. in the South-east of England, many well determined by the recent levelling for railroads, 375. , list of, in the South-east of England, 3871—381*. explanation of, and reference to authorities for, 369—371. INDEX. Helsingburg, in Scania, probable existence there, of a deposit analogous to the Wealden, 330. Hematite of Mahabuleshwur in the Dukhun pro- duces the Wootz steel, 426. Henslow, Rev. Prof., his observations on the strata containing stratified trunks in Portland, 16, note; referred to, 218, 220. , notice of the temperature of springs in the neighbourhood of Weymouth, 44, note. Herschel, Sir John, examines the colouring mat- ter of the green sands, 109. —, sectional drawings, and lists by, of the strata on the south of the Isle of Wight, referred to, 186. High Pike to the top of Great Colm, notice of the beds from, 87. Hill forts in the Dukhun, their great strength due to trap, 414. Hills, Mr. of Court-at-Street, Kent, numerous fossils collected by, 112, 127, note, 128, 339. Hindhead, Surrey, stratification at, 144. , sands near, described, 147. Hockliffe, in Bedfordshire, section through, 292. Hoer, in Scania, fossil plants there analogous to those of the Wealden, but probably belonging to the oolite series, 330. Hog’s-back, Surrey, a ridge of chalk strata highly inclined, 145. Hole Beck near Stank, beds of cellular magnesian limestone, form base of red sandstone, 389. Hollows, which may have been craters, in the Vindhya range, mentioned, 428. Holworth Cliff, notice of the spontaneous com- bustion of the Kimmeridge clay in, 23. Horner, Leonard, Esq., on the geology of the environs of Bonn, 433. —_—_—_—_—_—_.— geological specimens de- posited by him in the museum of the Society, 454. —_—————-—., his coloured map of the environs of Bonn, 434. , his notice of Mr. Ly- ell’s observations on the loess, 475, 476. , modification of his opi- nions respecting the history of the loess, 479. VOL. IV.—SECOND SERIES. 499 Hot springs of the trap mountains of Rajmahl, 427. Howgill Fells to Baw Fell, account of a section from the, 96. Hunstanton Cliff, Norfolk, sectional lists of strata at, 313, 314. , Sections of, by different geologists compared, 315, note. —___—_——_—__. » red stratum between the chalk and the Lower green-sand there, 314, 315, note. Hunter, Rev. Joseph, notes by, on the word Hurst, 162, note, Huntingdonshire, not yet described geologically, 303, note. Hurreechundurghur, hill fort of, its situation de- scribed, 411. , remarkable basaltic dyke at, 418. , glassy felspar, resembling Cleavelandite, found there in amygdaloid, 424. “ Hurst”, the word of frequent occurrence in the names of placesin Kent, Sussex, and Surrey,161, note. , Its meaning explained, 162, note. Hyleosaurus, a new fossil of the Wealden, dis- covered and described by Mr. Mantell, 179. i Ichthyophthalmite in the amygdaloid of the Dukhun, 424. at Poona, 425. Ichthyosiagones, a name given to a species of Trigonellites, by Dr. Riippell, 348. Iguanodon, new portions of the skeleton found near Maidstone, in the Lower green-sand, 132, , splendid specimens of, found note. India, age of the trap formation of, undetermi- nable, 429. , Peninsula of, its characteristic geological features recapitulated, 431. » granite, its basis, 431. Indus, mouth of the, phenomena there like those which produced the strata in Portland, 226. aT 500 Inferior oolite, description of, on the coast of Dor- setshire, 30. Ingleborough, succession of beds on the flanks of, Sor Ingleton to Great Colm, notice of a section from, (Pl. VI. fig. 6.) 90% Insects, fossil, of the environs of Bonn, notice of Prof. Goldfuss’s description, 453. Iron ore, hematite, of the Dukhun produces the Wootz steel, 426. — SS fragments of, found in the Lower green-sand, 117. , pisolitic, found in the Hastings-sand near Hastings, 166, and note. probably not confined to Hastings, 335. , found on the Continent, in ma- rine deposits supposed to be coeval with the Wealden, 329, 330. , titaniferous, at Hunstanton, Norfolk, 313. K. Kankar: see Kunkur, 431. Kent, coast of, beds below the chalk on, described, 105. : see Copt Point, Folkstone, Sand- gate, Hythe, &c. , ancient cliffs of, now separated from the sea by Romney Marsh, 161. , general section of (Plate X. a. No. 6.), 163, and note. , another section, on the true scale of height and distance, (Plate X. a. No. 6. lower line), 163, note. , near Folkstone, view of, by the Rev. J. D. Glennie (Plate VIII.). , East, Packe’s Map of, 1743, 106. , interior of: see Boughton, Maidstone, &c. Kimmeridge Bay, described, 21, 212. Kimmeridge clay and Weymouth beds, in the Isle of Purbeck, 212. ee —— pass insen- sibly into Oxford oolite, 331. ——_____—___, its thickness in the South-east of England, estimated, 320. INDEX. Kimmeridge clay, the substratum of the Isle of Portland, 22. near Aylesbury, 292. at Little Brickhill, in contact with Lower green-sand, 293. in Cambridgeshire, 307. at Headington, Oxfordshire, 278. near Muswell Hill, 283. in Oxfordshire and Bucks, 273. —__—___—, a portion of, wanting near Ox- ford, 274. near Swindon, 267. in West Norfolk, 315. near Weymouth, 21. ——— at Whitchurch, 291. , fossils of, in Bedfordshire,Cam- bridgeshire, and Norfolk, 317. in Dorsetshire, 231. in Oxfordshire and —— ——— ——— —— Bucks, 302. ——_—— the marly sandstone of, in Ringstead Bay, 21. at Swindon, 269. ———, notice of its occurrence in France, 22. — —=— ——-—, spontaneous combustion in, at Holworth Cliff, near Weymouth, Dorset, 23. Kirkby Lonsdale, dislocation near, not the leading branch of the Craven fault, 60. Kirkby Stephen and Penigent, Prof. Sedgwick on the carboniferous chain between, 69. , description of a longitudinal sec- tion from Penigent to the plains of the Eden near, 84, , new red sandstone conglomerate, near, described, 385. Konkun, (East Indies), general description of, 411, , thermal springs of, 427 ; their localities, 2b. ——_———, widely diffused there, 427. Kunkur, (nodular limestone), signification of the word, 420, 430. , its characters in the Dukhun de- scribed, 420. INDEX. Kunkur, analysis of by Mr. Prinsep stated, 431. , not the cornbrash of England, 431, L. Lancashire, Prof. Sedgwick on the new red sand- stone series on the north-western coast of, 883. Langcombe, Oxfordshire, section at, 278. Laterite of a portion of Dukhun, described, 430, , places of its occurrence, 430, associated with hematite, said to occur at the source of the Krishna river, 430. ——— region, in the Peninsula of India, of very great extent, 428. ——.— passes into Ceylon, 430. Leighton Buzzard, vicinity of, 293, Leith Hill, Surrey, 142, 143, “ Lets,” eroded cavities in the strata, so called, at Tisbury, 255: (see ‘“ Gulls.”) Lias formation of Dorset, 31; enormous depo- sits of Belemnites in, 31, Lignite: see Brown-coal. deposit of Bonn superior to the chalk,465. —— » no remains of mollus- cous animals to be found in, 465. , only two species of fish hitherto met with in, 474. Lime, phosphate of, coproid masses composed of, frequent in the Gault, 111, note, examined by Dr. Prout, 111, noée. Limestone, three states of, in the Dukhun, 419. , crystalline, in amygdaloids, of the Duk- hun trap, described, 421. , nodular, (Kunkur) of the Dukhun, de- scribed, 420. ——_—_—___—_—_——- occurs very exten- sively in India, 430. — — , analysis of by Mr, Prinsep stated, 431. , pulverulent in the Ghats of the Duk- hun, described, 419. —————, description of the bed called ‘ Strong Posto. 501 Limestone, range of the bed called “ Strong Post,” (ie and calcareous slate, account of a band of,in Cumberland, between green slate and grey- wacke, 49. —_—__—_—_———— full of organic remains, separated by enormous masses from other calcareous strata, 49. ——, most western appear- ance of, at Beck, 49. » great faults which af- fect the band, 50, et seq. ————_—_--—-——_————— generally ———— — ————_—_—_——., exception at Pool Beck Scar, 52. » notice of the forma- tions associated with, 48. , order of their suc- cession, 48. SERRE » first esta- blished by Mr. Otley, 48, and note. ———_—— —, cut off by the Shap granite of Wastdale Head, 54. —, reappears beyond the granite, 68*, Lincolnshire Wolds, structure of, 310, note. Lindley, Prof., examination by, of specimens of the vegetable remains of the brown-coal forma- tion near Bonn, 451. Loess of the environs of Bonn, description of, 460; its localities, 460, 461 ; its composition, 460, 461; fossil remains of, 461 ; its greatest elevation, 461. absence of vegeta- ble remains in, 462. — — around the Roderberg, 474, 475, —-— intermixed with volcanic products, in ex- cavations near the Roderberg, 475. , hotice of Mr. Lyell’s writings on the, 475, 480, 481. , terrestrial shells greatly predominate over aquatic in the, 475. —— absorbs water with great avidity, 475. , modification of Mr. Horner’s opinions re- specting its history, 479-481. 372 502 Loess, relative age of the, 469. . probably the production of some vast flood, 469. Lonchopteris Mantelli, said to have been found at Wansford in Northamptonshire, 309; doubtful, 383*. Lonsdale, William, F.G.S., notice of his examina- tion of the Oolitic series, near Bath, 261. —— , lines of sections by, in Geol. Trans. 2nd Series, vol. ili.; Map, Plate IX., 261, note. near ee , sections by, Calne, Plate X. a. No. 15 and 16, 261. Lower new red sandstone, overlying Whitehaven coal-field, compared with that of the Yorkshire and Durham coal-fields, 397. ——_——,, of Yorkshire and Dur- ham, in some places conformable, in some un- conformable to coal measures, 397, 401. —, near Whitehaven, ex- cavated prior to the deposition of the magne- sian conglomerate, 398. ——- conformable to the coal measures on the coast; unconform- able in the interior, 397. Lulworth Cove, section of, east side, 216. —, inclined strata near, 14. ——, inference from, — respecting the trees of the dirt-bed, 15. Lunn, Francis, Esq., on the confines of part of Huntingdonshire and Cambridgeshire, 303, note. Lydden Spout, near Folkstone, Kent, issues from the lowest chalk, 106. Lyell, Charles, Esq., P.G.S., observations by, on the effect of earthquakes at the mouth of the Indus, 226. ——— ——__—_-_—_______, observations on the loess in the higher parts of the valley of the Rhine, 475, 477. Lynn, West Norfolk, deep well at, in the Kim- meridge and Oxford clays, 310. M. M’Lauchlan, Mr., observations by, on the chalk of Bedfordshire and Cambridgeshire, 303, 304. INDEX. M’Lauchlan, and Glaisher, Messrs., list of heights by, in Cambridgeshire, 370. Magnesian conglomerate and limestone, descrip- tion of near Barrowmouth, 395. ————— ————— of the coast near White- haven compared with that of Nottinghamshire, Yorkshire, and Durham, 398. of Bristol coal-field equi- valent of magnesian limestone and not of rothe todte liegende, 399, 400. Mahr, in the Konkun, hot springs at, 427. Maidstone, remains of Tguanodon found near, 132, note. , large Scaphites found near, 339. “Malm,” a mass so called at Garsington, Oxford- shire, belonging to the Purbeck series, 277. “ Malm-land”, and “ malm-rock”, in Surrey, what, 154, note. rock”, in Hampshire, supposed to be di- stinguished by its fossils, 154. Man-of-War Cove, section at, 217. Mantell, Gideon, F.G.S., Hyleosaurus, a new genus of reptiles, discovered by, 179. , his observations on remains of the Iguanodon found near Maid- stone, 132, note. ascertains that bones of birds exist in the Hastings-sand, 382*. Mantell, Mr. Walter, anew fossil species of Unio found by, 179. Marshes of Huntingdonshire and Cambridgeshire, remarks upon, 304. Martin, P. I., F.G.S. The term ‘ Wealden” proposed by, 103. , his observations on West- ern Sussex, 155. —_— on the drainage of the Wealden Valleys, 150. , beds subordinate to the Weald clay carefully traced by, 160. , section by, through West Sussex (Plate X. a. No. 5.), 155. Maryport to St. Bees Head, country almost wholly composed of coal measures, 388. Menzalé, description of the lake of, 12, note. Merian, M., marine deposit of pisolitic iron ore, INDEX. 503 described by, supposed to be coeval with the Wealden, 330. Merstham, Surrey, section at, 140. Mesotype in the amygdaloid of the Dukhun, 424. , great masses of, found at Aklapoor in the Dukhun, 425. Meyer, M. Von, on Aptychus, referred to, 348. Miller, Mr., late of Bristol, (deceased, ) his collection of Blackdown fossils, 239. , a fossil species of Pecten, named after, 342. Millstone grit, description of the group called the first millstone grit between Penigent and Kirkby Stephen, 81. , called the second millstone grit, 82. - upper mill- stone grit, 82. Mineral, new, green, breaking into ‘‘ Rhombs,” found at Gorgaon in the Dukhun, 425. Minerals in amygdaloid, ofthe Dukhun, mentioned, 425. Mineral axis of Cumberland mountains, unstra- tified crystalline rocks, 49. formations on the sides of, arranged sym- metrically, 49. —-—_—_———, general strike of, 49. Mineral waters of the environs of Bonn, 463; analysis of, 7b. Mineralogical] distinctions, and order of superpo- sition, the foundations of geology, 67. Mosdale, notice of the beds in, 93. Mosdale moor or wold limestone described, 76; range of, 2b. Mota River, the valley of, on the south of Poona, exceedingly narrow, 412. Murchison, R. I., F.G.S., his observations on part of Hants referred to, 153, 156. ee sketch and description by, of Hunstanton Cliff, (Pl. X. b. fig. 12. b.,) 313. description by, of the geological place of a new species of Chelydra, referred to, 380. Murchison, Mrs., fossils of the Green-sands of Hampshire, collected by, 156. Muswell Hill, Bucks, section at, 279. Muswell Hill, near Highgate, Herts, superficial deposit there, containing fragments of several different strata, 293. N. Nautilus plicatus, wood-cut of, 129. New red sandstone series, Prof. Sedgwick on the, in the basin of the Eden, and on the north- western coasts of Cumberland and Lancashire, 383. ———, geographical distribu- tion of in Cumberland, and part of Lancashire, 384, 405. employed in Westmore- land and Dumfriesshire for roofing-slate, 386. connected with the car- boniferous rocks in Cumberland by a lower red sandstone, 387, 4.00. ——, great degradation of, 388, 389. of Cumberland differs from that of the Bristol and South Wales coal-field, by passing into the coal measure through an in- termediate sandstone, 391. in some parts of Cumberland is concealed by enormous masses of drifted materials, 388, 389. » probable extension of, at a former period from the coast of Cumberland, to Cheshire, 389. at Hole Beck, base of, is cellular magnesian limestone, 389. , the gypseous marls of central England wanting almost entirely in the, of the valley of the Eden, 387. , carboniferous beds some- times resemble it in colour, 387, and note. , conglomerates of, near Brough and Kirkby Stephen, described, 385. , not to be di- stinguished from the dolomitic conglomerates of the Mendip Hills, 385, 399. of England, proofs of the identity of, with that of central Germany, 399. 504 New red sandstone series,description of the suc- cessive deposits which compose the, from Par- ton to St. Bees Head, 393. , lowest member of, in the North of England, probably produced by the dislocations which immediately followed the carboniferous period, 58. » deposition of, followed by movements of elevation anterior to the magnesian limestone, 58. , once extended in Cum- berland over a greater surface than at present, 389, —_—_____—_—__,, perfectly analogous to the corresponding series of Yorkshire and Dur- ham, 399. ———__-———., section of, near Ald- bury, 400, ——_—_— ——_—_—-——,, though sometimes con- formable to the carboniferous system in Cum- berland, is not conformable on a great scale, 387, 388. unconformable among last ramifications of the Eden, 390, — Furness, 391, in Low , near Ros- ley, 387, note. between Appleby and Maryport, generally conformable to carbonifer- ous series, 391. near St. Bees Head, both conformable, and unconformable, 391. Nicol, Mr., of Edinburgh, slices of fossil wood prepared by, 222, note. Nilsson, Professor, of Lund, his Petrifacta Sue- cana referred to, 350. —— , observations by,on a deposit resembling the Wealden at Helsing- burg, in Scania, 330. Nodular limestone, (Kunkur,) forms a remarkable feature in the geology of India, 430. ——— , organic remains in, belong to living species, 431. — region of, in the Peninsula of India, of very great extent, 428. INDEX, Noggerath, Prof., bed of silicified wood at Bruch near Ober Cassel, examined by, 451. , fossil remains of quadrupeds in the environs of Bonn, mentioned by, 454. —, on the shells of the brown-coal formation of the environs of Bonn, 473. Nomenclature of strata, notto be taken from mere external character, 105, note. Norfolk, West, general sketch of the geology of, 309. , fossils of, in beds below the chalk, 316, &e. North Devon and part of South Wales, grey- wacke series of, elevated probably after com- pletion of carboniferous series, 57. , axes of, parallel, 57. , North Wales, no obvious centre of dislocation in, 67. , Strata thrown into vast parallel un- dulations, 67. —, probably not produced by shocks succeeding after long intervals, 67. Northern carboniferous chain, account of the ef- fects produced by the elevation of, 59, ————— marked by a system of longitudinal faults, 59. Nutfield, Surrey, Fuller’s earth pits there, 141. contain sul- phate of barytes, 141. O. (Eningen, new fossil species of Chelydra from, described by Thomas Bell, F.G.S., 379. Old red sandstone conglomerates of, North of England, often havea much newer appearance than those of the new red sandstone, 390, note. —__—_—__—_—__—_—_———~— in Westmoreland occur at several points where the carboniferous chain is in contact with greywacke, 69. —— -_ —_—____———__ near Hebblethwaite Hall Gill, 97. ——, peculiarities of structure and position of the schistose rocks of Cumber- land originated in causes anterior to existence of the, 49, 55. INDEX. Oogein, city of, said to have been estroyed bya shower of earth, 428. Oolite, containing freshwater shells, in the Pur- beck bed, at Combe Wood, Oxfordshire, 275. -, Oxford, phenomena presented by, at junction with the Kimmeridge clay, near Ox- ford, 274. its thickness, in the South-east of England, estimated, 320. at Blackthorn hill, Bucks, 274. beyond Haddenham, Cambridge- shire, 507. - at Headington, 279. , at Upware on the Cam, 307. , fossils of, in Cambridgeshire, 316. near Oxford, some fossils of, 303. Oolitic stone, at the top of the Portland series ; somewhat like that of Bermuda, 224. Opal, milk, found at Oondurgaon in the Dukhun, 425, Order of superposition and accurate mineralogical distinctions, foundations of geology, 67. Organic remains help to unite disconnected base lines, 67. » none found in the Dukhun, 426. Osmington and Ringstead Bay, Dorsetshire, faults at, 39. Otley, Mr., order of stratified deposits of central Cumbrian mountains, first determined by, 48. Oxford clay, in West Norfolk, places of its oc- currence doubtful, 316. in Dorsetshire, 28. _ Oxford oolite, or coralline, near Weymouth, de- scribed, 23; its extent, 27. , difference of characters of, in Ox- fordshire and Dorsetshire, 26 and note, 27. Oxfordshire, beds below the chalk in, 269. » fossils of, 296. Oysters, their occurrence a proof of the presence of salt water, 321 note. P. Packe, Christopher, M.D., his map and memoir on East Kent, (1743); 106 and note. 505 Paludine, found in the “ hard stone” of Quainton, Bucks, 290. Papierkohle in the environs of Bonn, frogs and insects found in, 466. Parkinson, Mr., his name Trigonellites, retained, 348. Parton and St. Bees Head, account of the coast section between, 393. ne , faults by which it is affected, 394, et seq. Passy, M., notice of his work on the structure of the Pays de Bray, 327, 331. “Pendle,” fissile freshwater limestone so called, in Bucks, 287, 289, 290. Penigent and Clapham, notice of the country be- tween, 94. - to Stags Fell near Hawes, account of a section from, 91. - to the plains of the Eden, near Kirkby Stephen, description of a longitudinal section from, 84. -, account of the beds composing the sum- mit of, 84, Peppingford, in Ashdown Forest, Sussex, fossil Cone found at, 181. Petersfield, fossils from neighbourhood of, 156. Petrifactions, siliceous, amidst calcareous frag- ments, 332. of trees and Cycadez in Portland, 225, 332. ——— of shells at Blackdown in siliceous sand, 332. Pewsey, Vale of, stratification described, 262. ———, Dr. Buckland upon, referred to, 263; a “valley of elevation,” 263. Phillips, John, F.G.S., notices of his account of the Craven fault, 60, 95, 98. et —— paper ona group of slate rocks between the rivers Lune and Warfe, referred to, 95, 98. —, on Belemnites Listeri, in red chalk, 315, note. —_——-, his Geology of York- shire, referred to, 214. Phillips, William, F.G.S., on the chalk near Dover, referred to, 107. 506 Pisolitic iron ore, in the Hastings sand, near Hastings, 166. , probably not confined to Hast- ings, 353. on the Continent, in deposits supposed to be coeval with the Wealden, 329, 330. Plastic clay, description of, near Weymouth, 5. Farnham, 190. Pleurotomaria (Trochus), note upon, 153, Poland, marine deposits in, supposed to be coeval with the Wealden, 329. Pool Beck Scar, fault at, not marked by a valley; 52. Poorundhur, glassy felspar found at, in amygda- loid, 424. Pope, Rev. W. L., a new species of Sphenopteris found by, in the Hastings sand, 181. Portland Ferry and Weymouth Harbour, com- position of the cliffs between, 24. — formation, its interrupted deposition in England, 19. Portland, Isle of, summary of publications on, 217%. ——— | int-bed ofthe lis. , detailed section of upper beds in, 219. , fossil trunks of Co- niferee and Cycadee in, 13, 225. , phenomena of, analogous to those produced by earthquakes at the mouth of the Indus, 226. —$—— , hypothesis, explaining them, 226. , quarries of, ought to be fre- quently examined, 227. , Strata pervaded by fissures, proving disturbance, 218. , strike of the strata well ascer- tained, 214, note. Portland Sand, group of strata proposed to be so called, 20, 210. —-— abounds in green particles, 210. a stage of transition, from the Kemendoe clay to the Portland stone, 21, 331. INDEX the Portland stone, throughout the coast of Dorset, 19. » concretional nodules in, near Thame, (wood-cut,); 283; at Shotover, 273, 278; at Swindon, 273; Portland Sand, coextensive with in the Boulonnois, 273, 328. designated by Mr. Conybeare, 210. , importance of distinguishing it, $3. , probable occurrence of, at Shot- over Hill, near Oxford, 21. , notice of, at Whitchurch, 21. , notice of, at Swindon, 21. in the Boulonnois, 21. , thickness of, in the South-east of England estimated, 320. near Aylesbury, 291, ——_—_——_——-. at Brill, 280. ———__———— at Long Crendon, 282, ——— at Emmet’s Hill, Isle of Purbeck, ———— at Muswell Hill, Bucks, 283. —_—_————_ in Oxfordshire and Bucks, 273. ———_-———_— in the Pays de Bray, 328. ————_————_ in the Isle of Purbeck, 210. ——__-_— at Swindon, 266, 267. ———_—_——__ near Stewkley, 292. ———_———-_ near Thame, 282. —_—_—_-—+_——. Vale of Wardour, 255. at Whitchurch, 291. , fossils of, in Dorsetshire, 20, 231. at Swindon, 269. in Oxfordshire and Buckinghamshire, 301. in the Vale of War- dour, 261. Portland stone, its thickness in the South-east of England estimated, 320. , passing into sand, in contact with Lower green-sand, 265. near Aylesbury, 286. in the Lower Boulonnois, 328. at Great Hazeley in Oxfordshire, 276. in Oxfordshire and Bucks, 272. INDEX. Portland stone in the Isle of Purbeck and Dor- setshire, 17, 210. at Quainton, Bucks, 290. —____—_—_—— near Stewkley, 291 and note. —_—_—_————- at Swindon, 265. —_____—_——_ in the Vale of Wardour, 254. in the Pays de Bray, 328; in Burgundy and the vicinity of Angoulesme, 19. in other parts of France, 330, 331. , fossils of, in Dorsetshire, 260. in Oxfordshire and Buckinghamshire, 299. at Swindon, 268. in the Vale of Wardour, 260. Portland strata, remarks on their distribution and characters in the South-east of England, 331. , their junction with the Purbeck strata, a point of great geological interest, 331. , less extensive at present than the Kimmeridge clay, 332. , their equivalents in France, 19, 227; and on the Continent in general, 222. Prestwich, Joseph, F.G.S., on alternations of marine and freshwater remains, 321, note. Prevost, Constant M., observations by, on the Isle of Wight, 185 note. ———— —— notice of his memoir on the coast of Normandy, 331. Primary and secondary stratified rocks, broad mineralogical distinction between, 66. tertiary stratified rocks, a_ still broader distinction, 67. Prout, Dr., coproid masses from the Gault, examined by, 111, note. finds the petrified trunks of Portland, and of the Vale of Wardour, to be almost wholly siliceous, 225, 254, note. Pudding-stone, numerous large blocks of, like that of Hertfordshire, occur in some of the chalk combs, Dorsetshire, 5. Pulborough, vicinity of, subdivisions of the Lower green-sand in, 155. , derangement of strata near, 155. Purbeck beds on the coast of Dorset, notice of, 11; occurrence of an oyster bed in, 12. VOL. IV.—SECOND SERIES. 507 Purbeck Isle, distant view of, 206, note. , east coast of, section, 206. -, general view of the south coast of, 212. , general view of the coast west of, 215; numerous sections of beds below the chalk, 215, and note. Purbeck strata, their junction with the Hastings sands, in the Isle of Purbeck, 208. Portland formation, very remarkable, 225, 331, near Aylesbury, 287. at Combe Wood, in Oxfordshire, in part oolitic, 275. at Long Crendon, 2&2. at Dinton, Bucks, 285. at Garsington, Oxfordshire, 277; there called ‘* Malm,” 277. in the Isle of Portland, 218. in the Isle of Purbeck, 208, 209. at Swindon, N. Wilts, 266. in the Vale of Wardour, 249, PHOS ——_—— ~—— near Whitchurch, Bucks, 289. —_——— ——,, fossils of, in Dorsetshire, 229. a in Oxfordshire and Bucks, 297. —_—__.__—___.._-___.. jn the Vale of Wardour, 259. Pusch, M., notice of his memoir on the beds below the chalk, in Poland and Silesia, 329. Putzberg, near Bonn, section of the beds at, 456. Q. Quadrupeds, fossil remains of, in the environs of Bonn, mentioned by Prof. Noggerath, 454. Quartz (Amethyst), in the trap rocks of the Dukhun, 424. , varieties of, in the trap rocks of the Dukhun described, 424. , forms a large portion of the Lower green- sand conglomerates in Kent, 116. Quartzose green slate of Cumberland, notices of the, 48. 3 U 508 INDEX. R. Radipole Barracks, Weymouth, notice of the Ox- ford clay near, 28. “Rag,” Kentish, described, 117. Rail-roads in England have determined the heights of numerous points of small elevation, 375. , list of heights derived from the sections of, 375—381*. Raven Crag, notice of a fault at, 51. Ravenglass, coarse red gravel of the cliffs south of, consists apparently of debris of new red sandstone, 389. Ravenstone Dale, account of the dislocations in the calcareous hills of, 61. Red marl and gypsum of St. Bees Head, very nearly on parallel of the lower red marl and gypsum of Yorkshire, 398, and note. Red sandstone of St. Bees Head, exact equiva- lent of upper red sandstone of Yorkshire, 398. series of Scotland and England, general comparison of, 402. Reigate, Surrey, section at, 142. Remarks, general, on the strata between the chalk and Oxford oolite, 318. Reptiles, fossil remains of, in the environs of Bonn, described by Prof. Goldfuss, 453. , of the Lower green-sand, 153. Weald clay, 179. Hastings sand, 179, 206, —_______..._——.. Purbeck strata, 230, 298. = Portland=stone 30. — Portland sand, 269. — Kimmeridge clay, 303. ————-— Oxford oolite; 16; Resemblance, notice respecting the, of deposits of different epochs, 333. Rhine, height of its surface at Bonn, 433, 472. -, Valley of the, physical features of, 462. Rhinoceros tichorinus, tooth of, found by Mr. Horner in a gravel pit near Bonn, 478. Ridge, Vale of Wardour, section at, 247. Ridges, anticlinal, of curved strata, near Seven- oaks, Kent, described, 133, and note. of small extent, supposed mode of their formation, 136. Ridges, another hypothesis explaining, 136, note. Ridgeway fault, in Dorsetshire, description of the great, 36. —, no indications of ruin and violence throughout its line, 42. Ringstead Bay and Osmington faults, 39. Risell, notice of beds on sides of, 87. River gorges, of the Wealden, remarkable, 151. Rivers, their mode of egress from the Wealden tract wi32s , their course transverse to the chalk, fa- voured by the stratification, 151. Rock, extensive sheets of bare, frequent in the Ghats of the Dukhun, 422. Rocks, sedimentary, of Bonn, relative ages of, 464—466. , of the Dukhun, remarks on , volcanic, of the environs of Bonn, 467; their ages in relation to each other, and to the sedimentary rocks, 467. Roderberg, an eruption from, subsequently to the commencement of the deposit of the loess, 478. -————., alternation of volcanic ejections with the loess near, 475. —, recommendation by Mr. Horner of a recently published account of the, by M. Carl Thomae, 472. —, voleanic eruption of the, 447, 468. Rose, R. C. Esy., of Swaffham, his account of West Norfolk, referred to, 309. , section by, from Swaffham to Lynn, (Plate X. a. No. 25); 510. Rosley, new red sandstone not conformable to coal strata near, 387, note. Rothe todte liegende of Germany, not repre- sented by the magnesian conglomerates near Bristol, 400, 403. Riippell, Dr., on Ichthyosiagones, referred to, 348. So “ Salt Brook,” stones in a rivulet so called, in- crusted with common salt and carbonate of lime, 425. dk ee INDEX. Saltom, notice of faults at, 395. Saltpetre in the Dukhun, manufactured from scrapings of old walls, 426. ; Sand: see Bagshot-sand ; Green-sand ; Hastings- sand ; Portland-sand. and clay, foliated, in very thin beds, re- markable alternation of, 168. Le 45 Le ehy- pothesis to explain it, 168. , white and green, remarkably disposed, at Tilburstow in Surrey, and other places, 139. Sandgate, coast near, view of, (Plate VIII.) 106. —, indications of disturbance near, 124, 126. Sandown Bay, Isle of Wight, 187. Sandstone, new red, immediately below the green- sands of Blackdown, 238. resemblance of to the Weal- den, 333. of the valley of the Eden, the parallel of forest sand of Nottinghamshire, 387. been ex- posed to great denudation, 387. and shale, lowest group of, between Penigent and Kirby Stephen, described, 72. , subdivisions of, 72. , Shale, and calcareous grit group be- tween second and Strong Post limestones, de- scribed, 74. stinguished by beds of calciferous grit, 74. , lead- ing subdivisions of, 74. , fissile gritstone, and shale, between Mosdale Moor and Four Fathoms, described, tho ——_——_______—_—_—_—__ ——_,, most re- markable of groups alternating with limestone of Cumberland carboniferous system, 77. , contains two beds of coal, 78. ee — ——— ’ subdi- ———_—__—__—__—_—_————_,, the grit- stone used for roofing-slate, 78. Sadne Haute, equivalent of the Portland strata and Wealden found in, 329, 330. 509 Satpoora Hills, Col, Briggs’s description of hot springs of, 427, Scaphites Hillsii, specimens of, from the Lower green-sand near Maidstone, (Pl. XV. f. 5), 128, 339. Schistose deposits, remarks on their ancient se- paration into two groups, the upper containing organic remains, the lower none, 66. , line of separation difficult to determine, 66. rocks of Cumberland owe their pecu- liarities of structure and position to causes in action anterior to the existence of the old red sandstone, 49. Scotland, general comparison of red sandstone series of, with that of England, 402. —, red sandstone and conglomerates of, assigned principally to old red sandstone, 402. Second millstone grit, description of, between Penigent and Kirkby Stephen, 82, or black limestone group, between Kirkby Stephen and Penigent, described, 73. Secondary rocks, from the south coast to latitude of Derby, have a direction parallel to grey- wacke chains, 59; reasons why, 59. beyond Derby, the direction is parallel to great central carboniferous chain of the North, 59. and primary stratified rocks, broad mi- neralogical distinction between, 66. Sedgwick, Professor, F.G.S., description of a se- ries of longitudinal and transverse sections through a part of the carboniferous chain be- tween Penigent and Kirkby Stephen, 69. , Introduction to an account of the general structure of the Cum- brian mountains, 47. ‘ ———_—_______1____, hissection between Portland Ferry and Weymouth Harbour, 24. , on the coral rag, 26, note. ———_____—_—__—___—1_——-,, on the vicinity of Weymouth, 24, 213, note. reference to his ac- count of the Kimmeridge strata near Scarbo- rough, 214, 3u 2 510 Sedgwick, Professor, F.G.S., notes by, on the geology of Cambridgeshire, 303, note. , on the new red sandstone in the Basin of Eden, and the coasts of Cumberland and Lancashire, 383. Sedimentary rocks of Bonn, relative ages of, 464— 466. , stated not to exist in Western India, South of Baroach, 431. Serroor, inthe Dukhun, glassy felspar found near, in amygdaloid, in the bed of the Goreh river, 424, , occurrence at, of carbo- nate of soda, 426. Shale, carbonaceous and fissile gritstone, group of, between the Strong Post and Mosdale Moor limestones, described, 75. ——————_— — —_ —___—________--, most im- portant bed of the group is the coal in the shale, 7K fc. —, gritstone and coal, group of, between the four and twelve fathom limestones de- scribed, 79. — and sandstone, lowest group of, between Penigent and Kirkby Stephen, described, 72. — sandstone, and calcareous grit, group of, between the second and Strong Post limestones, described, 74. -——, calcareous grits the characteristic beds of the group, 74. —-—-, sandstone, and fissile gritstone, group of between Mosdale Moor and four fathom lime- stones, described, 77. -, most re- markable of the groups alternating with the limestone series near Penigent, 77. ——-, a system of, wanting at bottom of lime- stone series in Cumberland, 71. Shanklin Chine, Isle of Wight, numerous fossils found near, 192. Shap granite, boulders of, in detritus of new red sandstone of the valley of the Eden, 388. of Wasdale Head, cuts through the band of limestone and calcareous slate, 54, 68*. assumed its present position after the formation of transition limestone, 54. INDEX. Shap granite, veins of, penetrate greywacke near Wasdale Head Farm, 68*. Shap Wells, mineral waters of, spring from a cal- careous conglomerate, 68*. Shells, list of, found in the loess of Bonn, 462. —, fossil, from the beds between the chalk and Oxford oolite, Systematic Tables of, 350— 364. , descriptive notes of new species, by Mr. J. De Carle Sowerby, 335—348. , alphabetical list of; Upper green- sand, 108, 156, 202, 228, 257, 267, 296. —— Gault, 112, 152, 203, 228, 258, 296, 316. of the sands of Blackdown, De- — von, 229. , of the Lower green-sand, 127, 152; 157, 204, 268, 297, 317. ———.-— Weald clay, 176, 228. Hastings sand, 176, 228, 297. Purbeck strata, 228, 259, 297. 260, 268, 299. ——_____._—.— Portland sand, 231,261, 269, —-- Portland stone, 230, —— Kimmeridge clay, 231, 261, 269, 302, 317. —— ——— Oxford oolite, 817. Shotover Hill, Oxfordshire, section at, 274. 232, 503, Shropshire, account of a section of new red sand- stone near Aldbury in, 400. , continuity between the coal measures and red sandstone series of, effected by lower red sandstone, 401. Shunner Fell, account of the beds composing the flanks of, 93. , description of a section from Whern- side to, 92. Siebengebirge, description of, by Mr.Horner, 453. , basalt dykes frequent in the, 445; their localities, 445. , brown-coal formation of the, 447. , crystalline volcanic rocks of the, 439, note. ee INDEX. 511 Siebengebirge, different in structure from other groups in Germany, except one in Nassau, and another near Montabaur, 435. , absence in, of substances which in Hungary and Central France accompany trachyte, 440. , Mon-occurrence of basalt frag- ments in the trachyte tuff of the, 441. , notice of a geological map of, 472. , notice of authors who have de- scribed the, 433. , the, the nearest point to En- gland where volcanic phenomena nearly re- sembling those of modern eruptions are to be seen, 434. , trachyte tuff of the, (wood-cut), 440—443; its localities and characteristics, 441, 442. , volcanic eruptions of, 468. Silesia, Prof. Pusch on the beds below the chalk in, 329. Siliceous deposits of the brown-coal formation in the environs of Bonn, 448. Siliceous stone in sand, concretion of, formed sub- sequent to deposition of the sand, 232. , white, containing casts of shells and vegetable stems, occurrence of, at Marien- forst in the environs of Bonn, 454. Similarity of deposits of different epochs ;— of Wealden, to new red sandstone, and to beds above, and below, the chalk, 333;—of green- sand, above, and below, the chalk, to that of the Portland series, 333; of part of the Wealden to the coal formations, 333. , inference from this similarity, 333. Sithe-stones, mode of preparing at Blackdown, 237. , workmen said to be consumptive, 238. Skiddaw Forest, granite of, overlaid by crystal- line slates, 48. -, slates of, probably owe their structure to action from below, 65. S'ate, siliceous, pebbles of, in the Lower green- sand conglomerate of Kent, 117. Smith, Rev. Gerard E., fossils of Kent, collected and drawn by, 112. Smith, Rev. Gerard, E., examines the Wealden cliffs in Kent, 161. -, remarks by, on the spiral termination of certain Hamites, 337. Smith, William, his map of Kent referred to, 107. —— , his statement respecting “sand in- “cluding the Portland-stone,” explained, 265, note. Soda, carbonate of, at Serroor in the Dukhun, its form and mode of occurrence described, 426. and at other places, 426. ——, muriate of, impregnates many of the wells at Ahmednugeur, 425. Samia also a rivulet called the Salt Brook at Ahmednug- gur, 425. , streams impregnated with, at other places described, 426. Solway Firth, boulders of Carrock Fell syenite, on the shores of, 388. South Wales and North Devon, greywacke series of, probably elevated after completion of car- boniferous:series, 57. - does not conform, in direction, to other greywacke chains, 57. axis of, parallel to that of the coal basin of South Wales, 57. South Western coal, notice of total break between coal measures and red sandstone series of the, 401. Sowerby, James, F.LL.S. (deceased), observations by, (1812), on the probable existence of fresh- water formations, 324, note. Sowerby, James De Carle, F.L.S., fossils of beds between the chalk and Oxford oolite, drawn and engraved by, 105. ——_-—_____.__ , descriptive notes by, on the shells figured in Plates XI. to XXIII. of this volume, 335—348. Sphenopteris gracilis, a new species of fern from the Wealden, (wood-cut,) 181. Springs near Weymouth, temperatures of, 44, note. 512 Springs, thermal, in the Konkun, described, 427. Spurs of the Ghats in the Dukhun described, 412. Stags Fell near Hawes, account of the structure of, 91. —, section from Penigent to, 91. Stainmoor, Craven-fault stops near the mountain pass of, 61. St. Bees Head, account of the coast section be- tween, and Parton, 593. , comparison of strata of, with new red sandstone series of Yorkshire, 398. , faults by which it is affected, 393, et seq. , red sandstone of, dips conform- ably to the coal measures, 388. 0 separated from coal measures by intermediate sandstone, mag- nesian limestone and conglomerate, 388. , notice of structure of, 396. -—— to Maryport, coast almost wholly composed of coal measures, 388. Stilbite and other zeolites, found at Ahmednuggur in the Dukhun, 424, 425. ——.-, great masses of, found in amygdaloid, at Brahmunwareh, in the Dukhun, 425. Stirling, Mr. on Cuttaek in India, referred to, 431. St. Leonard’s, near Hastings, detailed account of the cliffS and strata, 163, 165, 169, 171. Stone, village of, (Bucks,) pits of Lower green- sand, at, 285. Stone, formation of, amidst deposits originally consisting of sand and gravel, 332. Stourhead (South Wiltshire), section at, 256. Strata below the chalk, their variation of cha- racter in different parts of the South-east of England, 322. Stratification, false, near Folkestone, 120. -———-, fissures of, adopted by masses of chert of subsequent formation to the sand which includes them, 120. Strombeck, M. Von, his account of beds sunk through at Utweiler, in the environs of Bonn, 457. Strong Post limestone, description of, 75. , range of, 75. INDEX. Stutchbury, Mr. Samuel, a fossil species of Pec- ten named after, 342, 360. Summary of observations on the strata below the chalk in the South-east of England, 318, &c. Superficial deposits of Cambridgeshire, extensive and important; their contents, 304; of two kinds, ‘‘ white” and “red” gravel, 304, note.— (see Gravel.) — —-————— _ resemble those of Bedfordshire, and the East of En- gland generally, 305. Surrey: see Godstone; Reigate; Hind-Head ; Leith-Hill; Guildford, &c. , strata below the chalk in, described, 137. Sussex, Western, strata of, described, 153. Swanage, remarkable appearances on the shore near, 209, note. Swath Fell, structure of the top of, 89. Sweden, marine deposits coeval with the Wealden in, 330, Swindon (North Wiltshire), stratification at de- tailed, 264--267. ———___ — , fossils of, 267. , nodules in the Portland sand at, 267. Sykes, Lt.-Col. W. H., F.G.S., on a portion of the Dukhun in the East Indies, 409. —__—-—__—_—_—_——,, recapitulation of the characteristic geological features of the peninsula of India, 431. -————___—___—___—__—— — , explanationof the sections accompanying his paper on the Duk- hun, 432. 408 Table of heights in the environs of Bonn, 470. 3039; Taylor, R.C., F.G.S., his section at Hunstanton, and publications on Norfolk, referred to, 315, note. -—— South-east of England, Temperature, diminution of in the earth, may ac- count for some of the great parallel corruga- tions, 67. Terraces of the Dukhun described, 413. Tertiary deposits of the coast of Dorset de- scribed, 4. INDEX. Thame, Oxfordshire, strata there, 279, 282. Thermal springs of Konkun in the East Indies, 427, Thirria, M., on beds below the chalk in the De- partment of the Haute Sadne, 330. Thomae, M. Carl, on the lava of the Roderberg, 473; on the loess around the Roderberg, 475, 476. Tilburstow Hill, Surrey, list and sketch of beds composing the section, (wood-cut,) 138, 139. Tisbury, Vale of Wardour, quarries at, 255. Titaniferous iron ore, found in the Lower green- sand at Hunstanton, 313. Tonbridge Wells, strata there resembling those of the coast near Hastings, 170, note. Trachyte and basalt of the environs of Bonn, age of, 467. and grauwacke, instance of a junction of, in the neighbourhood of Bonn, 440. of the environs of Bonn, 437 ; its loca- lities and varieties, 437, 438. Trachyte, its affinity with the trap family, 438. Trachytic tuff, its correspondence in composition with adjacent trachyte nearest to it, 442. of the Siebengebirge, 440-443 ; its localities and characteristics, 441, 442. , the oldest of the volcanic pro- ducts of the environs of Bonn, 467. Trap region, in the Peninsula of India, of amaz- ing extent, 428. , extent not yet appreciated, 409. , authorities upon its stratification referred to, 410, note. its age uncertain, 420; probably not identical with that of the new red sandstone, 429. rocks in the Ghats of the Dukhun, charac- ters of described, 422. Tree, fossil, a remarkable specimen of, found in clay at Brill, 280. Trees, coniferous, silicified found at Portland, 13, BOA: —____1+—_————,, ascertained by Dr. Prout to be almost wholly siliceous, 225. in the lowest Purbeck strata of the Vale of Wardour, 256. —— i —— 518 Trees, coniferous, silicified, wood-cut of a re- markable specimen, 221. Trigonellites of Parkinson (Pl. XXIII. f. 2.), the name retained, why, 348. found in the Kimmeridge clay in Cambridgeshire, 273; and near Aylesbury, Bucks, 292. Troutbeck, account of fault in the valley of, 53. Tucksbury Hill, (or Farnham Beacon,) near Farnham, Surrey, section through, 149. Tuff of Siegburg, its great resemblance to that of the Phlegraean Fields and Ischia, 446. Turner, Edward, M.D., Sec. G.S., analysis by, of the green matter of green-sands, 108, note. Turna Fell coal works, section of beds at the, 93, note. Twelve-fathom limestone, description of, 79; abounds with encrinital remains, 80. U. Upper millstone grit, description of, between Pe- nigent and Kirkby Stephen, 82. Upware, on the river Cam, quarries there of the Oxford oolite, 307 ; fossils obtained there, 317. Vi Vale of Bredy, geological formations of the, 32. Wardour, geological structure of, 244. Weymouth, physical features of the, 3. Valley, remarkably narrow, on the Mota river, south of Bonn, 412. Valleys in the limestone band of the Cumbrian mountains, scooped out upon lines of fracture, 52, O4, in Dorsetshire produced by denudation, 41. of the Dukhun in India described, 412. Vegetable remains of the environs of Bonn, ex- amined by Professor Lindley, 451. —____\___—,, absence of, in the loess of Bonn, 462. Vegetables, fossil, of the Upper green-sand, 157, 203. Gault, 115. Lower green-sand, 131, 153, 514 Vegetables, fossil, of the Weald clay, 181, 228. ——_ _.__— Hastingsisand ld lenote, 725 US 2068229- SE = Punbeckstratawlone2 il, 230, 298. Portland stone, 269. Portland sand, 269. Kimmeridge clay, 269. | Volcanic action, cause of, not known, 64. not reducible to laws of any con- stant force as respects its effects, 65, 67. may be an effect of chemical combination, 68. ———.-, produced by the penetration of water to highly heated matter, 68. must diminish in force by the earth’s refrigeration, 68. Se ee and by each successive chemical combination, 68. has not acted during all geologi- cal periods with equal intensity, 65. -——, no indications of its recent oc- currence in the Dukhun, 428. Volcanic craters, none seen in the Dukhun, 428. — eruptions in the neighbourhood of Bonn, 446, 447. ——-— eruptions of the Siebengebirge, 46S. took place during the deposition of the brown-coal beds, 468. Roder- berg, 447, 468. Volcanic forces, provision for an eternal and uniform circulation of, not compatible with known laws of chemical action, 67. have modified the earth in two ways, 68. —— by violent paroxysms, producing lines of volcanic vent, 68. —— - os by local action producing volcanic cones, &c., 68. ——— rocks of the environs of Bonn, their ages relative to each other and to the sedimentary rocks, 467. INDEX. Voysey, Dr., on various points of Indian Geo- logy, referred to, 410, note, 412, 417, and note, 418, 426, 428, 431. W. Wardour, Vale of, general structure of, 244; strata described, 244; Chalk, 245; Upper green- sand, 246; Gault, 247; Lower green-sand, 248; Wealden, 249-254; Portland stone, 254; Portland sand, 255; Kimmeridge clay, 256. —-——————., anticlinal line of, 244. —_—_— , fossils of, 257—261. Warminster, Vale of, described, 257. ————., fossils of, 257, Wasdale Head Farm, granite veins penetrate the greywacke near, 68*. ——, the Shap granite of, cuts through band of limestone and calcareous slate, 54, 68*. , limestone and slate reappear beyond the granite, 68*. Water Blain limestone, notices of, 50, and note. Waters, mineral, of the environs of Bonn, 463; analysis of, 463. Weald clay, a member of the Wealden group, 103. earefully traced in W. Sussex by Mr. Martin, 160. ——_——-—_,, beds of sand and stone subordinate to, in Sussex, 159; in Surrey, 160; and in Kent, 161. , Cavities in, at its junction with the Lower green-sand in W. Sussex, 156. near Guildford, 148. near Hindhead, Surrey, 148. in the Isle of Wight, 185; detail of its beds near Cowleaze Chine, 198. » fossils of, in Kent and Surrey, Sus- sex and Hampshire, 176. in the Isle of Wight, on the Dorsetshire coast, Wealden, adopted as the general name of the strata between the Lower green-sand and the Portland stone, 103, INDEX. Wealden, acceptation of the term extended, why, 159. ——_—— characterized by its fossils, 104. probably the deposit of an estuary, 104, 324. —_— —, resemblance of part of, to the New red sand-stone; to some of the beds above the chalk ; and to the coal formation, 333. , sudden change from marine fossils, beneath it, and above, 324. , its stratification conformable to the for- mations above and below, 324. , formations immediately below it much connected, 331. , theory of its formation, 324. , analogy of, to deposits now in pro- gress, 325; as in the lakes of North America, 325. , its distribution and general characters in the South-east of England, 323, and note. , its original and remaining extent in England, undetermined, 324. , junction of, with the Lower green-sand, in the Isle of Wight, 189; in Western Sussex, remarkable, 156. , thickness of, in the South-east of En- gland, estimated, 319. not found beyond the limits of the Port- land formation, 332. in Buckinghamshire, indications of, 288, 289, 290. on the Kentish coast, described, 161. in Kent, Surrey, and Sussex, 159, et seq. in Oxfordshire, traces of, 272. at Shotover Hill, Oxfordshire, 274. in the Vale of Wardour, 249. , supposed indications of, at Wansford, in Northamptonshire, 309 ; doubtful, 383*. in the Isle of Wight, 184, 190. , deposits of the same date and character in other districts, 326 ; in Scotland, 326; in the Lower Boulonnois, 326; Pays de Bray, 326. equivalents of, in the Isle of Bornholm, and near Helsingburg, in Sweden, 330; in Poland, Switzerland, and France, 326, 330, 331. VOL. IV.—SECOND SERIES, 515 Wealden, marine deposits coeval with, probable @ priori, 329. , consequences of their existence, 329. not to be expected, ge- nerally, in England, $29. , places in which they have been found, 329, 330. -—_———,, remains of plants in, 181. » fossil shells of, in Kent, Surrey, Hants, and Western Sussex, 176. in the Isle of Wight, 205. » reptiles of the, 179. ————, fishes of, examined by M. Agassiz, 180; list of them, 367, 368. Wealds, Valley of the, in Kent, Surrey, and Sus- sex, 160. , drainage of, on the north- west, remarkable, 150. —_———_——,, tortuous course of rivers in, 150; hypothesis thence deduced, 150. ee » section across, from West Sussex to Surrey, (Plate X. a. No. 6); 155. Webster, Thomas, F.G.S., his work on the Isle of Wight, referred to, 8, 182. ——___—. on fossil trees in Port~ land, 13, 217. on the Purbeck and Portland strata, 11, 206, 210. , view by, of the coast near Hastings, 163. on freshwater shells in the Hastings and Purbeck strata, 324, note. Well, 600 feet in depth, at Lynn, Norfolk, 320. Wells, hot, called Devakl Unei, 50 miles south- east of Surat, 427. Wendover hill, its height, 284. Wey river, its course near Farnham in Hamp- shire, and in Surrey, 151. Weymouth, Dr. Buckland and De la Beche, H.T., on the geology of the neighbourhood of, 1. — district, an important geological tract, , the general physical features of, 2. —, physical features of the Vale of, 3. 3x 516 Weymouth strata form the transition from the Kimmeridge clay to the Oxford oolite, 331, 332. —-——— at Langcombe, Oxfordshire, 278. vary, much in different places, 332. , well seen in the Boulonnois, 332. : see Kimmeridge clay. Whernside, description of a section from, to Shunner Fel], 92. , notice of beds forming the flanks of, 85, 86. Whewell, Rev. W., sketch by, of part of Hun- stanton Cliff, (Plate X. b. fig. 12, ¢.); 313. Whitehaven coal-field, notice on, 293. , faults affecting, on the coast, 393, et seq. White Nore, Dorsetshire, pits in the chalk, at, filled with flints, 6. -, chalk cliffs of, 8, 9. White-rock, Hastings, section at, 168. recently destroyed or re- moved, 165, note, 382*. Wight, Isle of: see Blackgang, Shanklin, Cow- leaze, &c. , proofs of its repeated submersion and elevation, 185, » resemblance in, between the beds above and below the chalk, 185. » general structure of, 182. , south coast, sectional sketches of, by Sir John Herschel, 186. , sectional list of strata, from Bem- bridge Down to Sandown Bay, 187. —_ -——_——___——_——— from Bon- church Cove to Sandown Bay, 191, &c. —.—_— from Black- gang-chine to Brook-chine, 194. INDEX. Wight, Isle of, sectional list of strata, from the shore under Afton-down to Brook-chine, 200. , fossils of the beds below the chalk in, 202. Wild Boar Fell, structure of, 89, 98. - to Harter Fell, account of a sec- tion from, 97. Wiltshire, North: see Swindon. —, South: see Vale of Wardour, and of Warminster. Windermere, valley of, scooped out upon a line of fracture, 52. and Coniston Head, notices respect- ing faults between, 67 *. Woburn, section through, 292. —, Fuller’s earth pit, near, 294. Wockley-quarry, Vale of Wardour, section of, Dole Wold or Mosdale Moor limestone, described, 76; range of, 76. Wood, fossil, lignitized, a remarkable specimen found in clay, at Brill, 280. , coniferous, silicified, found in the “Dirt Beds,” in the Isle of Portland, 13, 217, 221, 222; in the Vale of Wardour, 254; at Swindon, 269. , silicified, bed of, in the environs of Bonn, 451; examined by Professor Noggerath and M, B. 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Deux Promenades au Mont Dore pour I’Etude de la Question des Cratéres de Soulévement, formant la 1ére livraison de la 4éme Série d’Itinéraires du Cours com- plet d’Etudes Géologiques par des Lecons et par des Voyages, par M. Nérée Boubée, 18mo. Paris, 1833. Nixus Plantarum. Auctore Johanni Lindley, 8vo. Lon- dini, 1833. Notice sur le Bradford-clay de Bouxwiller et de Bavil- lers, par M. P. L. Voltz, 4to, Extrait des Mémoires de la Société d’Histoire Naturelle de Strasbourg. Mémoire sur les Groupes du Cantal, du Mont Dore, et sur les Soulévemens auxquels ces Montagnes doivent leur Relief actuel, par MM. Dufrénoy et Elie de Beau- mont, 8vo. Paris, 1833. Extrait des Annales des Mines, 8éme Série, tome 3. Transactions of the Zoological Society of London, vol. 1, part 1, 4to. London, 1833. Proceedings of the Royal Society of Edinburgh, No. 2, April and May 1833. Mémoires de l’Académie Royale des Sciences de 1’In- stitut de France, tome 12éme, 4to. Paris, 1833. DONORS. Dr. Cooper. Messrs. 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Résumé Préliminaire de ’Ouvrage sur la Théorie des Volcans, par le Comte de Bylandt, 8vo. Naples, 1833. Memorie sopra due casi di Alienazione Mentale osser- yati nel R. Stabilimento de’ Matti di questa citta, composte da Giovanni Silvestri, 8vo. Palermo, 1833. General Observations upon, and Sailing Directions for, the English and Irish Channels and Channel Islands by Capt. Martin White, R.N. Descriptions of the Inferior Maxillary Bones of Masto- dons in the Cabinet of the American Philosophical Society, with Remarks on the Genus Tetracaulodon, &c., by Isaac Hays, M.D. Extracted from the Trans- actions of the American Philosophical Society, vol. 4. New Series, 4to. Philadelphia, 1833. A Catalogue of a valuable Collection of Books, in the French, Spanish, Portuguese and Italian Languages, on sale by John Bohn, 8vo. London, 1833. Verhandlungen der Gesellschaft des Vaterlindischen Museums in Bohmen in der eilften allgemeinen Ver- sammlung am 10 April 1833, 8vo. Prag, 1833. . Journal of the Franklin Institute of the State of Penn- sylvania, devoted to the Mechanic Arts, Manufac- tures, General Science, and the recording of American and other patented Inventions, edited by Thomas P. Jones, M.D. New Series, vol. 10, Aug. 1832, No. 2, 8vo. Philadelphia, 1832. Proceedings of the Royal Society of London, No. 13, 1832-1833. A descriptive Catalogue of the Minerals, and Fossil Or- ganic Remains of Scarborough and the Vicinity, inclu- ding the Line of Coast from Hornsea to Mulgrave, and extending into the Interior as far as Malton, 8vo. Scar- borough, 1816. Memoirs of the Royal Astronomical Society of London, vol. 6, 4to. London, 1833. DONORS. Henry Brookes, Esq. F.G.S. L’ Administration des Mines. The Author. The Author. Comte de Bylandt. The Lords Commissioners of the Admiralty. The Author. Mr. Bohn. Count Sternberg. Petty Vaughan, Esq. The Royal Society. John Willimott, Esq.F.G.S. The Royal Astronomical Society. 1833. Nov. 22. Dec. 3. 16. 20. List of Donations. BOOKS. Experimental Researches in Electricity, (Fourth Series, ) by Michael Faraday, D.C.L. F.G.S. From the Phi- losophical Transactions, 4to. London, 1833. The Horticultural Register and General Magazine of all useful and interesting Discoveries connected with Na- tural History and Rural Subjects, conducted by Joseph Paxton, for the year 1833. The London and Edinburgh Philosophical Magazine and Journal of Science, conducted by Sir David Brewster, K.H. LL.D. F.G.S. &c., Richard Taylor, Esq. F.G.S. &c., and Richard Phillips, Esq. F.G.S., for the year 1833. The Magazine of Natural History and Journal of Zoo- logy, Botany, Mineralogy, Geology and Meteorology, conducted by J. C. Loudon, Esq. F.G.S. &c., for the year 1833. The Penny Cyclopeedia of the Society for the Diffusion of Useful Knowledge, vol. 1,A—Andes, 8vo. London, 1833. Catalogue of Fellows, Candidates and Licentiates of the Royal College of Physicians, 8vo. London, 1833. Observations of Nebulze and Clusters of Stars made at Slough, with a twenty-feet Refiector, between the Years 1825 and 1833, by Sir J. F. W. Herschel, Knt. Guelp. F.G.S. From the Philosophical Transactions. 4to. London, 1833. On the Absorption of Light by coloured Media, viewed in Connexion with the Undulatory Theory, by Sir J. F. W. Herschel, K.H. From the London and Edinburgh Philosophical Magazine and Journal of Science, December 1833. Etablissement Géographique de Bruxelles. Annuaire Industriel et Administratif de la Belgique, Année 1833, 2éme Année, 8vo. Bruxelles, 1833. Dictionnaire Géographique de la Province de Namur, 8vo. Bruxelles, 1832. Dictionnaire Géographique de la Province de Hainaut. 8vo. Bruxelles, 1833. Mémorial de l’Etablissement Géographique de Bruxelles, fondé par Ph. Vander Maelen, 8vo. Bruxelles, 1831. Recueil de Documens Statistiques. Belgique, 8vo. Brux- elles, 1833. Journal of the Geological Society of Dublin, vol. 1, part 1, Dublin, 1833. An Encyclopedia of Gardening, containing the Theory and Practice of Horticulture, Floriculture, Arboricul- ture, Landscape Gardening, &c., conducted by J. C. Loudon, Esq. F.G.S., Specimen Number, 8vo. Lon- don, 1833. DONORS. The Author. The Conductor. The Conductors. The Conductor. Mr. Knight. The Royal College of Phy- sicians. The Author. The Author. M. Ph. Vander Maelen, Fon- deur de 1’Etablissement. CC ee ee ereseeesneseeeoe eens The Geological Society of Dublin. The Conductor. 10. 14, List of Donations. BOOKS. . M.A. Nattali’s Catalogue of a Collection of Books in General Literature, English and foreign, 8vo. Lon- don, 1834. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D. vol. 24, No.2. and vol. 25, No. 1. 8vo. New Haven, 1833. . The Nautical Almanac and Astronomical Ephemeris for the Years 1834 and 1835, published by Order of the Lords Commissioners of the Admiralty, 2 vols. 8vo. London, 1833. Address delivered at the Anniversary Meeting of the Royal Society on Saturday, November 30th, 1833, by His Royal Highness the Duke of Sussex, K.G. &c., The President, 4to. London, 1833. Descriptive and illustrated Catalogue of the Physiolo- gical Series of Comparative Anatomy, contained in the Museum of the Royal College of Surgeons in London, vol. 1, including the Organs of Motion and Digestion, 4to. London, 1833. Bulletin de la Société Géologique de France, tome 4éme, feuilles 1-5, Paris, 1833. Proceedings of the Royal Society of Literature, vol. 1, No. 4, 1833. Histoire des Végétaux Fossiles, ou Recherches Bota- niques et Géologiques sur les Végétaux renfermés dans les diverses Couches du Globe, par M. Adolphe Brong- niart, Séme livraison, 4to. Paris. A New System of Mineralogy in the Form of Catalogue, by William Babington, M.D. . Experimental Researches in Electricity, (Fifth Series,) by Michael Faraday, Esq. F.G.S. From the Philo- sophical Transactions, 4to. London, 1833. Transactions of the Society instituted at London for the Encouragement of Arts, Manufactures and Commerce, with the Premiums offered for the Years 1832-1833 and 1833-1834, vol. 49, London, 1833. . Studien des g®ottingischen Vereins, Bergmannischer Freunde, im Namen desselben herausgegeben, von Joh. Friedr. Ludw. Hausmann, 3ter band, 8vo. Got- _ tingen, 1833. Eloge de M. le Baron Cuvier, par. C. L. Laurillard. Discours couronné par l’Académie des Sciences, Belles Lettres et Arts de Besancon dans sa Séance du 24 éme, Aott 1833, 8vo. Paris, 1833. Proceedings of the Royal Asiatic Society, December 1833, and January 1834, 8vo. Manvel Géologique par Henri T. De la Beche. Traduc. tion Frangaise, revue et publiée par A. J. M. Brochant de Villiers, 8vo. Paris, 1833. DONORS, M. A. Nattali. The Conductor. W.S. Stratford, Esq. The Royal Society of Lon- don. The Royal College of Sur- geons. The Geological Society of France. The Royal Society of Lite- rature. Frederick Page, Esq. F.G.S. B. G. Babington, M.D. F.G.S. The Author. The Society of Arts. M. F. L. Hausmann. The Author. The Royal Asiatic Society. Henry T. De la Beche, Esq. F.G.S. — 1834. Jan. 25. 28. ole Feb. 4 io. 20 cr List of Donations. BOOKS. A Catalogue of Modern and Standard Works, principally of the Duplicates of Hookham’s Library, 8vo. 1834. Tide Tables for Plymouth, Portsmouth, Ramsgate, Sheer- ness, and London for the Year 1834, 8vo. London, 1834. A descriptive Catalogue of the Collection illustrative of Geology and Fossil Comparative Anatomy in the Museum of Gideon Mantell, Esq. F.G.S. 8vo. Lon- don, 1834. Proceedings of the Royal Society, No. 14, November 1832. Philosophical Transactions of the Royal Society of Lon- don, for the Year 1833, part 2. London, 1833. On the Former Extent of the Persian Gulf, and on the comparatively recent Union of the Tigris and Euphra- tes, by Charles T. Beke, Esq. 8vo. From the London and Edinburgh Philosophical Magazine and Journal. Messrs, Black, Young, and Young’s Catalogue of German Books and Maps which have been published from July to December 1833, 18mo. Mémoires de la Société Géologique de France, tome lére, lére partie, 4to. Paris, 1833. Contributions to Geology, by Isaac Lea, Esq. 8vo. Philadelphia, 1833. Report of the Scarborough Philosophical Society, for 1833. . Proceedings of the Royal Asiatic Society, January 4th, 1834. . The Architectural Magazine and Journal of Improvement in Architecture, Building and Furnishing, and in the va- rious Arts and Trades connected therewith, conducted by J. C. Loudon, Esq. F.G.S. vol. 1, No. 1, March 1834, . Aide-Mémoire du Voyageur, ou Questions relatives a la Géographie Physique et Politique, 4 l’ Industrie et aux Beaux-arts, &c., a Usage des Personnes qui veulent utiliser leurs Voyages, ou acquérir la Connoisance exacte du Pays qu’elles habitent, 12mo. Paris, 1834. . Sketches in Spain during the Years 1829, 1830, 1831 and 1832, containing Notices on some Districts very little known; of the Manners of the People, Govern- ment, recent Changes, Commerce, Fine Arts, and Natural History, by Capt. S. E. Cook, R.N. K.T.S. F.G.S. 2 vols. 8vo. London, 1834. Entomological Magazine, vol. 1. . Journal of the Royal Geographical Society of London, vol. 3, part 2. Des Causes de la plus Grande Taille des Espéces fossiles et humatiles comparées aux Espéces vivantes, par M. Marcel de Serres. Extrait de la Revue Encyclo- pédique, Avril—Mai 1833, 8vo. DONORS. Mr. Hookham. The Hon. The Court cf Di- rectors of the East India Company. Gideon Mantell, Esq. F.G.S. The Royal Society. The Author. Messrs. Black, Young, and Young. The Geological Society of France. The Author. The Scarborough Philoso- phical Society. The Royal Asiatic Society. The Conductor. Colonel Jackson. The Author. F. Walker, Esq. F.G.S. The Royal Geographical So- ciety. The Author. 8 List of Donations. 1834. BOOKS. Mar. 13. De la Simultanéité des Terrains de Sédiment Supérieur, par M. Marcel de Serres. Extrait du tome 5éme de la Géographie Physique de I’Encyclopédie Méthodique, Ato. Paris, 1830. April 3. Considérations sur les Ossemens Fossiles la plipart in- connus, trouvés et observés dans les Bassins de |’Au- vergne, par M. Geoffroy St. Hilaire. 8. Report on the Geology, Mineralogy, Botany, and Zoo- logy of Massachusetts; made and published by Order of the Government of that State, with a descriptive List of the Specimens of Rocks and Minerals collected for the Government, by Edward Hitchcock, 8vo. Am- herst, 1833. 14. Thirteenth Report of the Council of the Leeds Philoso- phical and Literary Society, at the close of the Session 1832-1833. Bulletin de la Société Géologique de France, tome 4€me, feuilles 6-9, 8vo. Paris, 1833. Proceedings of the Royal Society of Literature, vol. 1, No. 5, January to March 1834. Proceedings of the Royal Society, No. 15, December 1833, to March 1834. Lettre sur le Déluge de la Samothrace 4 M. A. M. Létronne, par M. Théodore Virlet, 8vo. Notes Géologiques sur les Isles du Nord de la Gréce, et en particulier, sur un Terrain de Calcaire d’ Eau douce a Lignites, par M. Théodore Virlet. Extrait des Annales des Sciences Naturelles, tome 30éme, 8vo. Asiatic Researches. Transactions of the Physical Class of the Asiatic Society of Bengal, part 2, 4to. Calcutta, 1833. 16. Proceedings of the Committee of Science and Correspon- dence of the Zoological Society, for May, June, July, August, September, October, November and Decem- ber 1833, with a List of Contributors. Prospectus of a Joint Stock Company for the Improve- ment of Ireland, 8vo. London, 1834. Gedrangte Uebersicht der Ergebnisse einer geogno- stischen Erforschung des Odenwaldes und einiger an- grenzenden Gegenden, mit besonderer Riicksicht auf Andeutung der Verbreitungsgebiete der Formationen, von Dr. A. Klipstein, 4to. Heidelberg, 1829. History of the Berwickshire Naturalists’ Club, instituted Sept. 22nd, 1831, 8vo. Edinburgh, 1834, 25. The History of the Royal Society of London for the Im- proving of Natural Knowledge, by Thomas Sprat, 4to. London, 1667. Transactions of the Royal Society of Edinburgh, vol. 12, part 2, 4to. Edinburgh, 1834. DONORS. The Author. The Author. The Author. The Leeds Philosophical and Literary Society. The Geological Society of France. The Royal Society of Lite- rature. The Royal Society. The Author. eeeeeeeeee The Asiatic Society of Ben- gal. The Zoological Society. Lt.-Col. Colebrooke, F.G.S. The Author. The Berwickshire Natura- lists’ Club. Roderick I. Murchison, Esq. V.P.G.S. The Royal Society of Edin- burgh. 1834. April 25 26 29. May 4% 8. 10. 14, 16. June . List of Donations. BOOKS. Proceedings of the Royal Society of Edinburgh, Nos. 1 and 2, December 1832 to May 1833, and No. 3, De- cember 1833 to January 1834. Catalogue des Livres de la Bibliotheque de Feu M, T* **** *, 8vo. Paris, 1834. M. A. Nattali’s Catalogue of Books, for May 1834. The Transactions of the Linnean Society of London, vol. 17, part 1, 4to. London, 1834. Mr. T. Rodd’s Catalogue of Works on Arts and Sciences, and Natural History. Studi Geologici sulla Toscana del Professore Paolo Savi, 8vo. Pisa, 1833. An Inaugural Lecture on the Study of Botany, read in the Library of the Botanic Garden, Oxford, May 1st, 1834, by Charles Daubeny, M.D. F.G.S. Professor of Chemistry and Botany in the University of Oxford, 8vo. Oxford, 1834. Annual Report of the Council of the Yorkshire Philo- sophical Society, for 1833, presented to the Annual Meeting, February 4th, 1834, 8vo. York, 1834. Outline of the Geology of the Neighbourhood of Chelten- ham, by Roderick Impey Murchison, Esq. V.P.G.S. &c. 8vo. Cheltenham, 1834. Annual Report of the Committee of the Athenzeum for the Year 1833, dated May 12th, 1834. An Account of the Caves of Ballybunian, County of Kerry, with some Mineralogical Details, by William Ainsworth, Esq. 8vo. Dublin, 1834. - Memoirs of the Royal Astronomical Society, vol. 7, 4to. London, 1834. . Origines Biblicz, or Researches in Primeval History, by Charles Tilstone Beke, Esq. vol. 1st, 8vo. London, 1834. - Note ona Paper by Dr. John Davy, entitled, ‘‘ Notice on the Remains of the recent Volcano in the Mediterra- nean,” by Charles Daubeny, M.D. F.G.S. From the Philosophical Transactions for 1833, 4to. London, 1833. On the Quantity and Quality of the Gases disengaged from the Thermal Spring which supplies the King’s Bath in the City of Bath, by Charles Daubeny, M.D. F.G.S. From the Philosophical Transactions for 1834, 4to. London, 1834. Hoéhen Messungen inund um Thiringen, Gesammelt, Verglichen und mit einigen Bemerkungen begleitet, von K. E. A. von Hoff, 4to. Gotha, 1833. Proceedings of the Royal Society, No. 16, April and May 1834. 3. Bulletin de la Société Géologique de France, tome 4éme, feuilles 10-14, 8vo. Paris, 1833. 9 DONORS. The Royal Society of Edin- burgh. M. Silvestre. Mr. Nattali. The Linnean Society. Mr. T. Rodd. The Author. The Author. The Yorkshire Philosophical Society. The Author. The Committee of the Athe- nzeum. The Author. The Royal Society. Astronomical The Author, The Author. The Author. The Royal Society. The Geological Society of France. Last of Donations. BOOKS. . Table des Matiéres et des Auteurs pour le troisiéme Volume du Bulletinde la Société Geologique de France, par M. Clément-Mullet. Researches in Theoretical Geology, by Henry T. de la Beche, Esq. V.P.G.S. 12mo. London, 1834. . M. A. Nattali’s Catalogue of Books, for June 1834. Magazin for Naturvidenskaberne. Udgives af den phy- siographiske Forening i Christiania, Anden Reekkes, Iste Binds, 2det Hefte, 8vo. Christiania, 1833. . Journal of the Royal Geographical Society of London, vol. 4, part 1, 1834, . Transactions of the Cambridge Philosophical Society, vol. 5, part 2, 4to. Cambridge, 1834. . Experimental Researches in Electricity (Sixthand Seventh Series), by Michael Faraday, Esq. D.C.L. F.G.S. From the Philosophical Transactions for 1834, 4to. London, 1834. - . The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D. vol. 26, No. 1, 8vo. New Haven, 1834. . Descriptions of some new Species of Cuvier’s Family of Brachiopoda, by W. J. Broderip, Esq. V.P.G.S. Ato. From the Transactions of the Zoological Society, vol. 1, part 2, 1834. On the Anatomy of the Brachiopoda of Cuvier, and more especially of the Genera Terebratula and Orbicula, by Richard Owen, Esq. Assistant Conservator of the Museum of the Royal College of Surgeons in London, 4to. From the Transactions of the Zoological Society, vol. 1, part 2, 1834. . An Address delivered at the third Annual Meeting of the Geological Society of Dublin, on the 13th of Fe- bruary 1834, by the Rev. Bartholomew Lloyd, D.D. President of the Society ; to which is subjoined the Annual Report, &c. 8vo. Dublin, 1834. Journal of the Geological Society of Dublin, vol. 1, part 2, 8vo. Dublin, 1834. . Premiums of the Society for the Encouragement of Arts, Manufactures, and Commerce, for the Sessions 1834— 1835, 1835-1836, 8vo. London, 1834. Annalesdes Mines, ou Recueil de Mémoires sur l’Exploi- tation des Mines, et sur les Sciences et les Arts qui s’y rapportent, rédigées par les Ingénieurs des Mines, et publiées sous }’ Autorisation du Conseiller d’Etat, Direc- teur Général des Ponts et Chaussées et des Mines, 3eme Série, tome 6, 4éme livraison, 1834, 8vo. Paris, 1834. 9. The Athenaum Journal of English and foreign Litera- ture, Science and Fine Arts, from January to June 1834, 4to. London, 1834. DONORS, The Geological Society of France. The Author, Mr. Nattali. H. C. Strém, Esq. The Royal Geographical Society. The Cambridge Philosophi- cal Society, The Author. The Conductor. The Author. Wm. J. Broderip, Esq. V.P.G.S. The Geological Society of Dublin. The Society of Arts. L’ Administrationdes Mines. The Editor. 1834. July 11. 13 17. 19. List of Donations. BOOKS. Transactions of the Royal Asiatic Society of Great Britain and Ireland, vol. 3, part 3, 4to. London, 1834. The Journal of the Royal Asiatic Society of Great Bri- tain and Ireland, No. 1, 8vo. London, 1834. Notice of Fossil Bones found in the Tertiary Formation of the State of Louisiana, by Richard Harlan, M.D. Read October 19th 1832. From the Transactions of the American Philosophical Society held at Philadel- phia, vol. 4. Annales des Mines, ou Recueil de Mémoires sur l’Ex- ploitation des Mines et sur les Sciences qui s’y rap- portent, rédigées par les Ingénieurs des Mines, et publiées sous ]’Autorisation du Conseiller d’Etat, Di- recteur Général des Ponts et Chaussées et des Mines, 3éme Série, tome 5éme, 11éme livraison de 1834, 8vo. Paris, 1834. Report of the Third Meeting of the British Association for the Advancement of Science, held at Cambridge in 1833, 8vo. London, 1834. . Philosophical Transactions of the Royal Society of Lon- don, for the Year 1834, part 1, 4to. London, 1834. . A Manual of Mineralogy, comprehending the more re- cent Discoveries in the Mineral Kingdom, by Robert Allan, Esq. F.G.S. 8vo. Edinburgh, 1834. Mémoire sur la Position Géologique des Principales Mines de Fer de la Partie Orientale des Pyrénées ; accompagné de Considérations sur Epoque du Sou- lévement du Canigou, et sur la Nature du Calcaire de Rancié, par M. Dufrénoy. Extrait des Annales des Mines, 3éme Série, tome 5éme, 8vo. Paris, 1834. ° Transactions of the Zoological Society of London, vol. 1, part 2, 4to. London, 1834. . Quelques Observations de Physique Terrestre, par MM. Auguste de la Rive et F. Marcet, 4to. . Bulletin de la Société Géologique de France, tome 4éme, feuilles 15-19, 8vo. Paris, 1834. . Mémoire sur la Formation Jurassique dans le Nord de la France, par M. E. Puillon Boblaye. Extrait des Annales des Sciences Naturelles, Mai 1829, 8vo. Paris, 1829. Recherches sur les Roches designées par les Anciens sous les Noms de Marbre Lacedemonien et d’Ophites, par M. E. P. Boblaye, folio. . Bulletin dela Société Géologique de France, tome 4éme, feuilles 20-24, 8vo. Paris, 1834. Verhandlungen der Gesellschaft des vaterlandischen Mu- seums in Bohmen in der zwélften allgemeinen Ver- sammlung, am 2 April, 1834, 8vo. Prag, 1834, 11 DONORS. The Royal Asiatic Society of Great Britain & Ireland. The Author. L’ Administration des Mines. The British Association. The Royal Society. The Author. The Author. The Zoological Society. The Authors. The Geological Society France. The Author. The Geological Society of France. The President of the Mu- seu of Prague. 12 1834. Aug. 14 18. 30. Sept. 1. 18. 20 Oct. 16. 24 Nov. 95. List of Donations. BOOKS. . Nautical and Hydraulic Experiments, with numerous Scientific Miscellanies, by Colonel Mark Beaufoy, F.R.S. vol. 1, 4to. London, 1834. Résumé des Progrés des Sciences Géologiques pendant V’Année 1833, par M. Ami Boué. Lu aux Séances des17et 24 Février, et 7 Avril 1834, tome 5éme du Bulletin de la Société Géologique de France, 8vo. Pa- ris, 1834, Contents of parts 2 and 3 of the Proceedings of the Royal Society of London, 1831-1833. Black, Young and Young’s Catalogue of German Books and Maps which have been published from January to June 1834, 12mo. Abhandlungen der Kéniglichen Akademie der Wissen- schaften zu Berlin, aus dem Jahre 1832 nebst der Ge- schichte der Akademie in diesem Zeitraum, 4to. Ber- lin, 1834. Principles of Geology, being an Inquiry how far the former Changes of the Earth’s Surface are referable to Causes now in Operation, by Charles Lyell, Esq. For. Sec. G.S. 3rd Edition, in four volumes, 12mo. Lon- don, 1834. Transactions of the American Philosophical Society, held at Philadelphia, for promoting Useful Know- ledge. New Series, vol. 4, part 3, 4to. Philadelphia, 1834. . ACollection of Geological Facts and practical Observa- tions intended to elucidate the Formation of the Ashby Coal Field, by Edward Mammatt, Esq. F.G.S. 4to. Ashby-de-la-Zouch, 1854. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D. For. Mem. G.S. vol. 26, No. 2, July 1834, 8vo. New Haven, 1834. . Memorie della Societa Italiana delle Scienze residente in Modena, tomo 20, fascicolo secondo delle Memorie di Fisica, 4to. Sul Problema dell’ Equilibrio delle Volte. Memoria del Signor Dottore Vincenzo Amici, Coronata dalla Societa Italiana delle Scienze residente in Modena, 4to. Mo- dena, 1833. A Treatise on the Epidemic Cholera; containing its Hi- story, Symptoms, Autopsy, Etiology, Causes and Treatment, by Alexander Turnbull Christie, M.D. 8vo. London, 1833. Elements of Chemistry, including the recent Disco- veries and Doctrines of the Science, by Edward Turner, M.D. Sec.G.S. Fifth Edition, 8vo. London, 1834. DONORS. Henry Beaufoy, Esq. F.R.S. The Author. The Royal Society. Messrs. Black, Young and Young. The Berlin Academy. The Author. The American Philosophi- cal Society. The Author. The Conductor. The Society. The Author. . George Turnbull, Esq. The Author. 14, 18. ale List of Donations. BOOKS. . Observations on the Genus Unio, together with Descrip- tions of new Genera and Species in the Families Naiades, Conche, Colimacea, Lymnzana, Melaniana and Peristomiana ; consisting of Four Memoirs read before the American Philosophical Society, from 1827 to 1834, and originally published in their Transac- tions, by Isaac Lea, Esq. 4to. Philadelphia, 1834. Recherches sur les Ossemens Fossiles, découverts dans les Cavernes de Ja Province de Liége, par le Docteur P. C. Schmerling, 2éme partie, complétant le premier volume, 4to. Liége, 1833. Mémoires de la Société de Physique et d’Histoire Na- turelle de Genéve, tome 6éme, parties 1 et 2, 4to. Ge- neve, 1833. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D. LL.D. vol. 27, No. 1, Oct. 8vo. New Haven, 1834. The Fourteenth Report of the Council of the Leeds Phi- losophical and Literary Society, at the close of the Session 1833-1834, 8vo. Leeds, 1834. A Catalogue of the Fellows, Candidates and Licentiates of the Royal College of Physicians, 8vo. London, 1834. . Nouveaux Mémoires de la Société Impériale des Natu- ralistes de Moscou, dédiés 4 S. M. l’Empereur Ni- cholas I. tome 3, 4to. Moscou, 1834. Bulletin de la Société Impériale des Naturalistes de Mos- cou, tome 6, 8vo. Moscou, 1833. A Treatise on Nautical Surveying: containing an Out- line of the Duties of the Naval Surveyor ; with Cases applied to naval Evolutions and miscellaneous Rules and Tables useful to the Seaman or Traveller, by Com- mander Edward Belcher, R.N. 8vo. London, 1835. . Observations Géologiques sur les deux Isles Baleares, Majorque et Minorque, par le Chevalier Albert de la Marmora, 4to. Turin, 1834. Transactions of the Geological Society of Pennsylvania, vol. 1, part 1, 8vo. Philadelphia, 1834. A descriptive Catalogue of the Collection illustrative of Geology and Fossil Comparative Anatomy, in the Museum of Gideon Mantell, LL.D. F.G.S. 3rd Edi- tion, 8vo. London, 1834. The Magazine of Natural History and Journal of Zo- ology, Botany, Mineralogy, Geology and Meteorology, conducted by J. C. Loudon, Esq. F.G.S. &c., for the Year 1834, 8vo. The London and Edinburgh Philosophical Magazine and Journal of Science, conducted by Sir David Brewster, K.H. LL.D. F.G.S. &c., Richard Taylor, Esq. F.G.S. &c.,and R. Phillips, Esq. F.G.S. &c., for the Year 1834. 15 DONORS. The Author The Author. The Society of Natural Hi- story of Geneva. The Conductor. The Leeds Philosophical and Literary Society. The Royal College of Phy- sicians. The Imperial Society of Na- turalists of Moscow. The Author. The Author. The Geological Society of Pennsylvania. Gideon Mantell, LL.D F.G.S. The Conductor. The Conductors. Whe 12. 17. List_ of Donations. BOOKS. _ The Horticultural Register and General Magazine of all useful and interesting Discoveries connected with Natural History and Rural Subjects, conducted by Joseph Paxton, for the Year 1834. . A Guide to Geology, by John Phillips, Esq. F.G.S. Professor of Geology in King’s College, London, 12mo. London, 1834. Transactions of the American Philosophical Society held at Philadelphia, for promoting Useful Knowledge, vol. 3, part 2. New Series, 4to. Philadelphia, 1834. Rules and Regulations for the Government of the Athe- neum, with an Alphabetical List of the Members, &c. 12mo. London, 1834. Transactions of the Medico-Botanical Society of London, for 1832 and 1833, 8vo. London, 1834. Experimental Researches in Electricity (Eighth Series), by Michael Faraday, Esq. F.G.S. &c. From the Philoso- phical Transactions, part 2, for 1834, 4to. London, 1834. A Journey from Sydney to the Australian Alps, by Dr. John Lhotsky. Geschichte der durch tberlieferung nachgewiesenen na- tiirlichen Veranderungen der Erdoberflache ein Ver- such, von Karl E.A. von Hoff, 3te Theil, 8vo. Gotha, 1834. Lethza Geognostica, oder Abbildung und Beschreibung der fir die Gebirgs-Formationen bezeichnendsten Versteinerungen, von Dr. H. G. Bronn, 1ster Lie- ferung, Stuttgart, 1834. Canal de Jonction entre le Rhin et le Danube, par Ch. Th. Kleinschrod. Traduit de |’Allemand, 8vo. Munich, 1834. Bulletin de la Société Géologique de France, tome 4éme, feuilles 28 et 29, 8vo. Paris, 1834. The Philosophical Transactions of the Royal Society of London, for the Year 1834, part 2, 4to. London, 1834. Proceedings of the Royal Society of London, No. 17, May and June 1834, 8vo. The Repertory of Patent Inventions, and other Disco- veries and Improvements in Arts, Manufactures and Agriculture. New Series, for the Year 1834, 8vo. Lon- don, 1834. Annales des Mines, ou Recueil de Mémoires sur l’Ex- ploitation des Mines, et sur les Sciences et les Arts qui s’y rapportent, rédigées par les Ingénieurs des Mines, et publiées sous ]’Autorisation du Conseiller d’Etat, Directeur Général des Ponts et Chaussées et des Mines, 3eme Série, tome 6, 5éme livraison, 8vo. Paris, 1834. DONORS. The Conductor. The Author. The American Philosophi- cal Society. The Committee of the Athe- nzeum. The Medico-Botanical So- ciety. The Author. The Author. The Author. The Author. The Author. The Geological Society of France. The Royal Society. The Editor. L’ Administration des Mines. 1835. Jan. | 3: 9. 26. Feb. 1 List of Donations. BOOKS. M.A. Nattali’s Catalogue of Books in various Languages, for the Year 1835, 8vo. London, 1834. T. Rodd’s Catalogue of Books for the year 1835, 8vo. Descriptive and illustrated Catalogue of the Physiologi- cal Series of Comparative Anatomy contained in the Museum of the Royal College of Surgeons in London, vol. 2, including the Absorbment, Circulating, Respi- ratory, and Urinary Systems, 4to. London, 1834. Transactions of the Society for the Encouragement of Arts, Manufactures and Commerce, for the Session 1833-1834, being part 1 of vol. 50, 8vo. London, 1834. Records of General Science, by Robert D. Thomson, M.D. with the Assistance of Thomas Thomson, M.D. F.G.S. Regius Professor of Chemistry in the Univer- sity of Glasgow, No. 2, February 1835, 8vo. London, 1835. On the Structure of the Teeth, in the “ Edentata,” fossil and recent, by Richard Harlan, M.D. Read April 28th, 1834. From the Transactions of the Geological So- ciety of Pennsyivania, vol. 1. Critical Notices of various organic Remains hitherto discovered in North America, by Richard Harlan, M.D. Read May 21st, 1834. From the Transactions of the Geological Society of Pennsylvania, vol. 1. Bohn’s Catalogue of Ancient and Modern Books in all Classes of Natural History, Agriculture, Gardening, Mining, Hunting, Hawking, Fishing, &c. 8vo. Lon- don, 1835. Arboretum Britannicum ; or the Hardy Trees of Britain, native and foreign, pictorially and botanically deli- neated, and scientifically and popularly described, &c., by J.C. Loudon, Esq. F.G.S. Nos. 1 and 2, 8vo. Lon- don, 1835. Dictionnaire Géographique de la Province d’Anvers, et Dictionnaire Géographique de la Province de la Flan- dre Orientale, par M. Ph. Vander Maelen, 2 vols. 8vo. Bruxelles, 1834. Proceedings of the Royal Society of London, No. 18, Nov. 1834. Journal of the Royal Geographical Society, vol. 4, part 2, 8vo. London, 1835. A Letter to James Jameson, Esq., by Charles Waterton, Esq. of Walton Hall, 8vo. Wakefield, 1835. On the Freshwater Limestone of Burdiehouse, in the Neighbourhood of Edinburgh; with Supplementary Notes on other Freshwater Limestones, by Samuel Hibbert, M.D. F.G.S. From the Transactions of the Royal Society of Edinburgh, vol. 13, part 1, 4to. Edinburgh, 1835. 15 DONORS. Mr. M. A. Nattali. Mr. T. Rodd. The Royal College of Sur- geons. The Society of Arts. The Editor. The Author. eeeeeeeeee Mr. John Bohn. The Author. M. Ph. Vander Maelen. The Royal Society. The Royal Geographical So- ciety. The Author. The Author. 16 1835. List of Donations. BOOKS. Feb. 1. The Analyst, a monthly Journal of Science, Literature Mar. and the Fine Arts, No. 7, February 1835, 8vo. London, 1835. Asecond Copy of the same Number was presented by the Editor, March 7th. Analysis of Coprolites and other organic Remains im- bedded in the Limestone of Burdiehouse, near Edin- burgh, by Arthur Connell, Esq. From the Transac- tions of the Royal Society of Edinburgh, vol. 15, 4to. Edinburgh, 1835. On the Satellites of Uranus, by Sir J. F. W. Herschel, Knt. Guelp. F.G.S. From the Memoirs of the Royal Astronomical Society, vol. 8, 4to. London, 1834, A List of Test Objects, principally double Stars, arranged in Classes, for the trial of Telescopes in various Re- spects, as to Light, Distinctness, &c., by Sir J. F. W. Herschel, Knt. Guelp. F.G.S. From the Memoirs of the Royal Astronomical Society, vol. 8, 4to. Lon- don, 1834. A Second Series of Micrometrical Measures of double Stars, chiefly performed with the seven-feet equatorial, at Slough, in the Years 1831, 1832 and 1833, by Sir J. F. W. Herschel, Knt. Guelp. F.G.S. From the Memoirs of the Royal Astronomical Society, vol. 8, 4to, London, 1834. Transactions of the American Philosophical Society, held at Philadelphia, for promoting Useful Knowledge,vol.5. New Series, part 1, 4to. Philadelphia, 1834. Bulletin de la Société Géologique de France, tome 6, feuilles 1-4, 8vo. Paris, 1835. Raccolta di Osservazioni Cliniche sull’ Uso dell’ Acqua Termo-Minerale Vesuviana-Nunziante, Fatte da varii Professori del 1832, fascicolo primo, 8vo. Napoli, 1833. Raccolta di Osservazioni intorno gli Effetti Terapeutici e le Cure per Acqua Termo-Minerale Vesuviana- Nunziante corrente l’Anno 1833. Preceduta da una Memoria scritta dal Professore Guiseppe Ricci, fasci- colo secondo, 8vo. Napoli, 1834. . A History of British Fishes, by William Yarrell, F.L.S. part J, 8vo. London, 1835. 3. The West of England Journal of Science and Literature, edited by George T. Clark, No. 1, January 1835, 8vo. Bristol, 1835. Journal of the Academy of Natural Sciences of Philadel- phia, vol. 7, part 1, 8vo. Philadelphia, 1834. List of the Members of the Zoological Society of London, June Ist, 1833, 8vo. London, 1833. DONORS. Hugh E. Strickland, Esq. F.G.S. The Author. The Author. The Author. enreeseeeee The American Philosophical Society. The Geological Society of France. Charles Daubeny, M.D. F.G.S. ee eeee reese ae ee eter oeee The Author. The Editor. The Academy of Natural Sciences of Philadelphia. The Zoological Society. 1835. Mar. 7. 26. April 3. 6. List of Donations. BOOKS. Supplement to the List of the Members of the Zoologi- cal Society, June 1834. List of the Members of the Royal Asiatic Society of Great Britain and Ireland, 1834. 8vo. List of the Members of the Royal Society of London, Ist Dec. 1834, 4to. Report on the Adjudication of the Copley, Rumford, and Royal Medals; and appointment to the Bakerian, Croonian, and Fairchild Lectures. 4to. London, 1834. List of the Members of the Society of Antiquaries of London. 4to. 1834. List of the Members of the Linnean Society of London. 4to. 1834. List of the Members of the Horticultural Society of Lon- don. 4to. 1834. . The American Journal of Science and Arts, conducted by Benjamin Silliman M.D. LL.D., vol. 27, No, 2. 8vo. New Haven, 1835. Transactions of the Royal Society of Edinburgh, vol. 13, part 1. 4to. Edinburgh, 1835. Proceedings of the Royal Society of Edinburgh, No, 4, January to April, 1834. 8vo. 23, Bibliographia Paleonthologica Animalium systematica. Auctore Gotthelf Fischer de Waldheim. Editio altera, aucta, jussu Societatis Czesareze Nature Scrutatorum impressa. 8vo. Mosque, 1834. The Journal of the Royal Asiatic Society of Great Bri- tain and Ireland, No. 2. 8vo. London, 1834. Voyage dans ]’Amérique Méridionale commengant par Buénos Ayres et Potosi jusqu’a Lima, par Antoine- Zachaire Helms, traduit de l’Anglais. 8vo, Paris, 1815. The Entomological Magazine, Nos. 6-9 for January to October 1834, and Nos. 10 and 11 for January and April 1835. 8vo. London. Illustrations of the Botany and other Branches of the Natural History of the Himalayan Mountains, and of the Flora of Cashmere; by J. Forbes Royle, Esq., F.G.S., &c. parts 1 to 5. fol. London, 1834, 1835, Memoirs of Ichthyosauri and Plesiosauri, extinct Mon- sters of the Ancient Earth; by Thomas Hawkins, Esq. F.G.S. fol. London, 1834. Transactions of the Zoological Society of London, vol. 1, part 3, 4to. London, 1835. A memoir on Clavagella; by W. J. Broderip, Esq., V.P.G.S. From the Transactions of the Zoological Society, vol. 1. 4to. Descriptions of some New Species of Calyptreide; by W. J. Broderip, Esq., V.P.G.S. From the Transac- tions of the Zoological Society, vol. 1. 4to. 17 DONORS. The Zoological Society. The Royal Asiatic Society. The Royal Society. The Society of Antiquaries. The Linnean Society. The Horticultural Society. The Conductor. The Royal Society of Edin- burgh. The Author. The Royal Asiatic Society of Great Britain and Ireland. John Willimott, Esq. F.G.S. F. Walker, Esq. F.G.S. The Author. The Author. The Zoological Society. The Author. eseeeeee00 is List of Donations. 1835. BOOKS. DONORS. April 27. Views in Ethnography, the Classification of Languages, the Progress of Civilization, and the Natural History of Man; by Charles T. Beke, Esq. From the Edin- burgh New Philosophical Journal for April 1835. 8vo. The Author. Report of the Directors of the Manchester Mechanics’ Institution, and Proceedings at the Annual Meeting of the Members held in the Theatre of the Institution |The Manchester Mechanics’ on Thursday, 26th February, 1835. 8vo. Institution. A Catalogue of the Library of the Manchester Mechanics’ Institution, with the Rules anda Sketch of the Objects and Advantages of the Institution. 8vo. Manchester, 1834. 28. The Chemical Catechism, by the late Samuel Parkes, F.G.S. &c. &c. Thirteenth Edition; revised and adapted to the present state of Chemical Science by E. W. Brayley, Jun. 8vo. London, 1834. The Editor. 29. Illustrations on the Botany and other Branches of the Natural History of the Himalayan Mountains and of the Flora of Cashmere; by John Forbes Royle, Esq. F.G.S. &c. part 6. folio. London, 1825. (he Authoe: Proceedings of the Royal Society of London, No. 19 December 1834 to March 1835. 8vo. May 1. Experimental Researches in Electricity (Ninth Series) ; by Michael Faraday, Esq. D.C.L. F.G.S. &c. From the Philosophical Transactions, part 1. for 1835, 4to. London, 1835. Arboretum Britannicum, or, the Hardy Trees of Britain Native and Foreign, pictorially and botanically deli- neated, and scientifically and popularly described ; by J.C. Loudon, Esq. F.G.S. No. 5, May. 8vo. London, 1835. The Author. Ueber Terebrateln mit einem Versuch, sie zu classificiren und zu beschreiben; von Leopold von Buch, Eine in der K6niglichen Akademie der Wissenschaften gele- sene Abhandlung. fol. Berlin, 1834. The Author. Nouvelles Annales du Muséum d’Histoire Naturelle, ou Recueil de Mémoires publiés par les Professeurs de cet Etablissement et par d’autres Naturalistes sur L’Administration du Mu- The Royal Society. The Author. V'Histoire Naturelle, Anatomie, et la Chimie, tomes séum d’ Histoire Naturelle 143. 4to. Paris, 1832-1834. de Paris. 4. Mr. M. A. Nattali’s Catalogue of Books for May 1835. 8vo. Mr. Nattali. A Guide to Geology; by John Phillips, Esq. F.G.S. Professor of Geology in King’s College, London. 2nd Edition. 12mo. London, 1835. The Author. Sketch of the Geology and Mineralogy of New London and Windham Counties in Connecticut ; by Wm. W. Mather. 8vo. Norwich, U.S., 1834. The Author. Fast of Donations. 19 1835. BOOKS. DONORS. May 12. An Address delivered at the Fourth Annual Meeting of the Geological Society of Dublin, on the 11th of Fe- bruary, 1835, by Richard Griffith, Esq. F.G.S. Pre- sident of the Society: to which is subjoined the Annual T. H. Holdsworth, Esq. Report, &c. &c. 8vo. Dublin, 1835. F.G.S. Notice as to the supposed Identity of the large Mass of Meteoric Iron now in the British Museum, with the celebrated Otumpa Iron described by Rubin de Celis in the Philosophical Transactions for 1786 ; by Wood- bine Parish, Jun., Esq. F.G.S. From the Philoso- phical Transactions, part 1. for 1834. 4to. London, 1834. The Author, 21. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D. LL.D. vol. 28, No. 1, April, 1835. 8vo. New Haven, 1835. The Conductor. 27. Notices on the Bolivian Andes, and Southern Affluents of the Amazons, communicated to the Royal Geogra- phical Society by J. B. Pentland, Esq. and Woodbine Parish, Jun. Esq. F.G.S. From the Journal of the Royal Geographical Society. 8vo. 1835. The Communicators. * How to Observe” Geology; by H. T. De la Beche, Esq. For, Sec. G.S. 8vo. London, 1835. The Author. 20. Synopsis of the Organic Remains of the Cretaceous Group of the United States; by Samuel George Morton, M.D. 8vo. Philadelphia, 1834. The Author. The Repertory of Patent Inventions, and other Disco- veries and Improvements in Arts, Manufactures and Agriculture. New Series for the Year 1835. 8vo. London, 1835. The Editor. June 2. Revelation and Science: the Substance of a Discourse delivered before the University of Oxford at St. Mary’s, March 8th, 1829, with some additional Remarks oc- casioned by the publication of the Bampton Lectures for 1833 and other recent Works; by the Rev. Baden Powell, M.A. Savilian Professor of Geometry inthe The Rev. James Yates, University of Oxford. 8vo. Oxford, 1833. F.G.S. 4. Instructions for making and registering Meteorological The South African Literary Observations in Southern Africa, and other countries and Philosophical Institu- in the South Seas, as also at Sea. 8vo. tion. The Cyclopedia of Anatomy and Physiology; edited by Robert B. Todd, M.B. part 1, published by Sherwood and Co. 8vo. London, 1835. The Publishers. 5. Arboretum Britannicum, or, the Hardy Trees of Britain, Native and Foreign, pictorially and botanically deli- neated, and scientifically and popularly described, by J. €. Loudon, No. 6, June. 8vo. London, 1835. The Conductor. Volcanic Geology, by Professor Daubeny, M.D. F.G.S, From the Encyclopedia Metropolitana 4to. The Author. 1834. Jan. Mar. 25 April 14 Nov. 5 14 25. List of Donations. BOOKS. . Revue Critique des Poissons Fossiles figurés dans !’Ittio- litologia Véronese ; Rapport sur les Poissons Fossiles decouverts en Angleterre; par M. L. Agassiz. The Horticultural Register and General Magazine of all Useful and Interesting Discoveries connected with Natural History and Rural Subjects ; conducted by Joseph Paxton, from January to June 1835. 8vo, London, 1835. The Magazine of Natural History and Journal of Zoo- logy, Botany, Mineralogy, Geology and Meteorology ; conducted by J. C. Loudon, Esq. F.G.S. From January to June 1835. 8vo, London, 1835. DONORS. The Author. The Conductor. The Conductor. II. Donations to the Collections of Maps, Drawings, &c MAPS, &c. . Carte de I’Ile et Dé partement de la Corse, et une Carte et Plan de Constantinople et du Canal du Bosphore. 2 sheets. An Impression of the engraved Portrait of the Rev. Prof. Sedgwick. Series of Charts containing Surveys mostly executed in the Indian Seas by Officers in the East India Com- pany’s Marine Service. Sheet No. 45 of the Ordnance Map in continuation of the Trigonometrical Survey of Great Britain. Sixteen Charts of part of the Mediterranean, the Coast of Portugal, &c. . Head of an Ichthyosaurus, painted with Fossil Sepia. » Sheet No. 62 of the Ordnance Map in continuation of the Trigonometrical Survey of Great Britain. - Sheets Nos. 53 and 57 of the Ordnance Map, in con- tinuation of the Trigonometrical Survey of Great Britain. . Copy of the Lithographic Plate accompanying M. Jules de Christol’s “Recherches sur les Caractéres des Grandes Espéces de Rhinoceros Fossiles.” 19, The Ordnance Townland Survey of the County of 1835. Mar. 31 Tyrone. - An Impression of a Lithographic Drawing of Calymene arachnoides. DONORS. M. Donati. Thomas Phillips, Esq. R.A. The Hon. the Court of Di- rectors of the East India Company. The Master-general and Board of Ordnance. Capt. Beaufort, R.N. Hon. Mem.G.S., by orderof the Lords Commissioners of the Admiralty. H. T. De la Beche, Esq. F.G.S. The Master-general Board of Ordnance. and M. Jules de Christol. Lieut.-Col. Colby, by order of His Excellency the Lord Lieutenant of Ire- land. M. F. Wm. Hoeninghaus. 1835. ad 13. 19; 21. 1833. July 1 Sept. 19. 30. List of Donations. MAPS, &c. An Outline Map of the World on Mercator’s Projection, drawn by C. Bradbury. No. 46 of the Ordnance Map in continuation of the Trigonometrical Survey of Great Britain, Ordnance Townland Survey of the County of Down, in 59 sheets. The N.E. quarter sheet of the 63rd sheet of the Ordnance Survey, coloured geologically by H. Still, Esq. em- ployed in the Ordnance Survey. 21 DONORS. Mr. Bradbury. The Master-general Board of Ordnance. Lieut.-Col. Colby, by order of his Excellency the Lord Lieutenant of Ire- land. and Henry Still, Esq. III. Donations to the Cabinet of Minerals. SPECIMENS. Agate Nodules from the Magnesian Limestone, Mendip Hills. Copper Slags from Swansea. Specimens from the Mountain Limestone in the neigh- bourhood of Tenby. Bones of the Elephant, Rhinoceros, and Ox, from the gravel, Brockhall Lawford. Fossils from the Cliffs at Hastings and St. Leonards, and a Tree from the Submarine Forest near St. Leonards. Specimens of Endogenites erosa from St. Leonards. Specimens from the Submarine Forest near Hastings. Specimens of Wood perforated by a Pholas. Specimen of Thorit. . Three Fishes from the Magnesian Limestone, Thickley. Specimens of Cyrtoceratitis costatus from Gerolstein. . A series of specimens from the North Shore of the River St. Lawrence. Specimens of Lead Ore, from Gador, South of Spain. Specimen of Fossil Wood perforated by Teredina per- sonata. Specimens from Vesuvius, Calabria, Sicily and Mount St. Gothard, &c. A Specimen of Marble perforated by Lithodomi obtained from a Ship sunk in the Leghorn Roads in the year 1750. A specimen of rock salt from Huamanga between Huan- cavelica and Cusco. A collection of specimens made in the crater of Vesu- vius, . Chromate of Lead from Siberia. . Specimens from Malta. A specimen of the Hastings sandstone. DONORS. The Rev. Prof. Buckland, D.D. F.G.S, eeeeeeeeoeneee eres eoseeee The Rev. T. Salway. The Rev. Wm. Thornton. Woodbine Parish, Jun. Esq. F.G.S. Wm. Henry Fitton, M.D. VEG, Robert Wrench, Esq. Capt. Belcher, R.N. F.G.S Prof. Esmark, For. Mem. G.S. Wm. P. Cumby, Esq. M. J. W. Hoeninghaus. Capt. Bayfield, R.N. John Willimot, Esq. F.G.S. Henry C. White, Esq.F.G.S. Count Bylandt. W. Richardson, Esq.F.G.S J. M. Maclean, Esq. John Auldjo, Esq. F.G.S. Mons. Donati. J. W. Collings, Esq. Charles, Babbage, Esq. 22 1833. Dee. 18. 1834. Jan. 8 22 Feb. 5. 26 Mar. 12 95 April 9. List of Donations. SPECIMENS. Specimens of Asbestus. Specimens from the Azores. Specimens in illustration of Capt. Burnes’s Memoir on the Geology of the Banks of the Indus, the Indian Caucasus, and the Plains of Tartary to the Shores of the Caspian. Specimens from Jersey. . Specimens from the Old Red Sandstone of South Wales. . Casts of perforations by T'eredina personata from the Plastic Clay, Hengisbury, Hants. Suite of rocks and fossils to illustrate Mr. Murchison’s paper on “ Herefordshire, Shropshire, and parts of Wales.” Specimens from Australia. Casts of the Bones of the Megatherium from Buenos Ayres, brought home by Woodbine Parish, Jun. Esq. F.G.S. Casts of the Inferior and Maxillary Bones of the Mas- todon and Tetracaulodon. Specimens from the Coal-Field of Wyre Forest. . Fossils from the Plastic Clay near Reading. Specimens from the Islot of Alcatraz on the West Coast of Africa, and from Gibraltar and Keith’s Reef between Sicily and the coast of Africa. Fossil Plants, Insects and Fishes from Aix in Provence. Specimens of Lignite from Leira. 2. Specimens from France. Corals from Aymestry. . Cast of an Ophiura ; from the Lias, banks of the Severn. Specimens of plants from the Greensand Formation of Niedershona near Freyberg. An Hippurite from Sicily. Additional specimens from the Eifel. Specimens of the Southstone Roche near Tenbury, Wor- cestershire. Specimens from the Mountain Limestone and Greensand of England. Fossil Fishes from Monte Bolca. Specimens from Port Macquarie. Selenite from the London Clay near Herne Bay. . Portions of Septaria from the London Clay at Brixton, and Fossil Wood perforated by Teredina personata. . Native Iron from the Mass in the British Museum from Otumpa in the Chaco, South America. . Specimens from the Tertiary Formations of Murcia. . Specimens of Pentamerus oblongus. DONORS. Richard Knight, Esq.F.G.S: The Rev. J. H. Simpson. Capt. Alexander Burnes. Ashurst Magendie, Esq. F.G.S. Roderick I. Murchison, Esq. F.G.S. The Rev. Prof. Buckland, D.D. F.G.S. R.1I. Murchison, Esq.F.G.S. Capt. H. Smyth, 39th Regt. The Royal College of Sur- geons. The American Philosophi- cal Society. The Rev. Thos. England, F.G.S. John Rofe, Jun. Esq. Capt. Belcher, R.N. F.G.S. Geo. Bentham, Esq. F.G.S. Richard Hollier,Esq.F.G.S. R. I. Murchison, Esq. V.P.G.S. The Rev. T. T. Lewis. Mathew Wright,Esq.F.G.S. M. Felipe Bauza, Jun. M. le Comte Duchatel. LeonardHorner,Esq.F.G.S. R. I. Murchison, Esq. V.P.G.S. eoeereereeeeoere esses eoese Capt. H. Smyth, 39th Regt. W. Richardson, Esq. F.G.S. The Rev. Prof. Buckland, D.D. F.G.S. Woodbine Parish, Jun. Esq. F.G.S. Chas. Silvertop, Esq. F.G.S. Mr. Rees. 1834. April 25. Fossils of the Grauwacke Series of Shropshire. May July Aug. Nov. 21. 3. List of Donations. SPECIMENS. Fossils from the Grauwacke of the neighbourhood of Llandovery. A large specimen of the polished Limestone found near Gwinfe in Caermarthenshire. . Cast of a Palatal Bone from the Chalk. Specimens of Rowley Rag, unaltered, decomposed and fused. . Lava from Graham’s Island. . Specimens of Greenstone, Porphyry and Sienite from the Border Counties of England and Wales. . Specimens from the Hastings sand. Specimens from Spain. Slickensides, from Cornwall. . Fish from the Magnesian Limestone. . Specimens from the Mines of Konigsberg, Norway. A specimen of artificial cupriferous Iron Pyrites. Fish from Monte Bolca. Carbonate of Strontia with calcareous Spar and Brown Iron Ore, Forest of Dean. Minerals from the Trap of Scotland. Corals from the Shale beds of the Mountain Limestone, County of Fermanagh. Casts of the Remains of Felis spelea and Gulo speleus from Gailenreuth. Magnetic Iron Ore from Sierra Leone. Specimens from Tampico. Specimens taken from the crater of the Water Volcano near Guatemala. A Fossil Crab from India (Gonoplax Latreillii), 7. Fossils from the neighbourhood of St. Ives. 20. Specimens from the London Clay at Hornsey. 14. 12. 13. Specimens from the Channel Islands. Cast of a claw-bone of a Crocodile, and of an Iguanodon from Tilgate Forest. . Cast of a Palatal Tooth from the Chalk of Dorsetshire. Specimens from the Loam of Muswell Hill; and addi- tional specimens from a well at Hornsey. Remains of Anthracothertum Velaunum, Myoxus and Cro- codile from Puy en Velay. 23 DONORS. W. Williams, Esq. Prof. Miller, F.G.S. The Rev. T. T. Lewis. Nathaniel Wetherell, Esq. F.G.S. John Corrie, M.D. F.G.S. Capt. Stewart. R. I. Murchison, V.P.G.S. Baden Powell, Esq. F.G.S. Capt. Cook, R.N. F.G.S. R. Taylor, Esq. F.G.S. of Perran, Arworthal. J. W. Colling, Esq. H.C. Strom, Esq. Engineer of Mines. Esq. ae L. Pratt Esq. F. G. S. Capt. Yorke, R.N. G. B. Greenough, Esq. Pres.G.S. Viscount Cole, M.P.F.G.S. and Sir Philip Egerton, Bart. F.G.S. oe eee eee esos eeeeeeroeee David Bastiat Esq. H.M. G.S. Thos. Weaver, Esq. F.G.S. Col. Galindo. The Right Hon. the Earl of Cawdor, F.G.S. J.R.Wright, Esq. F.G.S, and H. Machlauchlan, Esq. F.G.S. N. T.Wetherell, Esq. F.G.S. W.C. Trevelyan, Esq.F.G.S. Gideon Mantell, Esq. F.G.S. The Rev. Prof. Buckland, D.D. F.G.S. N.T. Wetherell,Esq. F.G.S. M. Bertrand de Doue, For. Mem. G.S. ro) List of Donations. SPECIMENS. . Fossils from Bognor and the Chalk near Felpham. Palatal Teeth of an Eagle Ray, (Myliobatis, Cuv.) from Bermuda. Specimens of recent Coral from the Straits of Sunda. Specimens from the Big Bend on the Missouri. Tertiary Shells from the United States. Specimens from the Ancient Beach at Hope’s Nose near Babbacombe and from the Watcomb Fault, Devon- shire. . Specimens from China. Specimens of Granite traversed by veins, from Dartmoor. Vegetable Remains from the Anthracite of North De- von. Specimens from Australia. . Anthracite from the Lehigh Coal Mine, Pennsylvania. Palatal Tooth of a Fish from the Chalk. Fossils from the Greensand near Lyme. Hippurite from Untersberg. Cast of a Molar Tooth of Mastodon angustidens from the Crag, Suffolk. . Shells from the Loam and Gravel near Cropthorne, Wor- cestershire. 2, Fossils from the neighbourhood of Ilfracombe. Specimens from the Coal of the South of Ireland. . Fossils from the Calcaire Grossiere of France. Casts from Flambro’ Head of Spongeous Zoophites. Shells and Bones of Mammalia from Stutton, Suffolk, and a Specimen of the Calcareous Nodules accompanying the Shells. Specimens of Lias from Cloverly and of the New Red Sandstone Series of Shropshire. . Porcelain Jasper from the Junction of the Sandstone and Trap Rock of Stirling Castle. Flexible Magnesian Limestone from Sunderland, and Fossils from the Lower Greensand, Kent. A Specimenof Franklinite from New Jersey, and of Shelly Ironstone from Lake Mollor between Hamburgh and Lubeck. Fossils from the Greensand, Blackdown. . Casts of bones of the Megalonya laqueatus from Big-bone Cave in Tennessee, DONORS. Woodbine Parish, Jun. Esq. F.G.S. LeonardS.Coxe,Esq.F.G.S. Woodbine Parish, Jun. Esq. F.G.S. HenryD.Rogers,Esq.F.6.S. e@eeerereeene ese eeoeeeesrenees Robert A. Austen, Esq. F.G.S. John R. Reeves, Esq. J. H. Deacon, Esq. F.G.S. Henry T. De la Beche, Esq. F.G.S. A. Cunningham, Esq. F. Lambert, Esq. John Dickinson, Esq. F.G.S. Viscount Cole, M.P. F.G.S. and Sir Philip Egerton, Bart. F.G.S. R. I. Murchison, V.P.G.S. Hugh E. Strickland, Esq. F.G.S. Esq. Col. Harding. Thomas Weaver, Esq.F.G.S. J. Prestwich, Jun. Esq. F.G.S. — Leigh, Esq. Edward Charlesworth, Esq. R. I. Murchison, Esq. V.P.G.S. Richard Knight, Esq. F.G.S. John Willimott, Esq. F.G.S. eoceesre ee eeeee Viscount Cole, M.P. F.G.S. and Sir Philip Egerton, Bart. M.P. F.G.S. Richard Harlan, M.D. 29. 14. June 10. 1833. Aug. 1834. Feb. 5. June 4. Dec. 6. List of Donations. SPECIMENS. : Specimens from the Silverdale Mines, Staffordshire. Shells of existing species from the Newer Pliocene De- posits in the Baltic. Specimens from the Isle of Portland. Specimens from Chili, Peru and the Island of Juan Fer- nandez. Specimens of British and Foreign Minerals. Specimens from the Island of Ascension, the Mauritius, &e. Specimens from the Pennant Grit and Dolomitic Conglo- merate near Bristol. Silicified Wood from the Portland Stone at Chicksgrove, Wilts. A Stalactite from Ingleborough Cave, Yorkshire. A specimen of Shale with impressions of Fern Leaves from the Grit Formation near Wodwowitz, Prussia. A Fish from the Purbeck beds, in the Vale of Wardour. Minerals and Rock Specimens from Norway. Casts of an Occipital Bone, and the anterior Cervical Ver- tebre of the Ichthyosaurus lately found near Lyme Regis. Specimens from the Mountain Limestone near Frome. Specimens of Fossils from the Coal Strata near Keighley, in Yorkshire. Specimens from the Diluvium at Lawfurd. Specimens of Spirolinites in Chalk Flints from Stoke, near Chichester. A set of Teeth of the Gangetic Crocodile. Specimens from the Arigna Mines. Specimen of a Trilobite from Dudley. IV. Miscellaneous. MISCELLANEOUS, Glass Models to promote the study of Crystallography. A Medal of Berzelius in Selenium. A Silver and a Bronze Medal of Count Casparus Stern- berg. ‘ Specimens of Iron Tubes from a Steam Boiler, Cornwall. Deposits on the vertical walls of the Boiler of a Steam- boat. 25 DONORS. Sir Philip Egerton, Bart. M.P. F.G.S. Charles Lyell, Esq. P.G.S. W. H. Fitton, M.D. F.G.S. H. Cuming, Esq. T. H. Holdsworth, Esq. F.G.S. The Rev. W. P. Hennah. George Cumberland, Esq. Hon. Mem. G.S. Miss Benett, of Norton House. Woodbine Parish, Jun. Esq. F.G.S. M. John Prague. Miss Benett. M. H. C. Strom. B. Batka, of H. Warburton, Esq. M.P. F.G.S. Miss Benett. The Rev. Theodore Dury. The Rev. Wm. Thornton, F.G.S. The Marquis of Northamp- ton, F.G.S. N.T. Wetherell, Esq.F.G.S. John Rofe, Jun. Esq. F.G.S. — Rofe, Esq. DONORS. M. J. B. Batka. Count Sternberg, For. Mem, G.S. JohnTaylor,Esq.Treas.G.S, Charles Lyell, Esq. For. Sec. G.S. nani’ ian : F re YA Fe: a)uaie. Sales? ‘a hateoe'p Fs = eS Fe oh a 3h & 3's ft tk scat] Panes on iS + -Bad i > ; | on ape’ Ted, f Aree SSE) wa . : S ive . S J : j é 7 “ ‘ . . rt. a f 7 = ¢ i _¥ F : ‘ 6 < “ : j ’ ’ are 2 s ‘ 7 > ‘ - = be -~ os i ee E : ji5 [3 PLATES AND MAPS IN ILLUSTRATION OF VOLUME IV. SECOND SERIES, OF THE TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. LONDON: PRINTED BY RICHARD TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. ———= 1837. EXPLANATION OF THE PLATES. Pirates I., II. & III. Illustrate Dr. Buckland and Mr. De la Beche’s paper on the Geology of the neighbour- hood of Weymouth and the adjacent parts of the coast of Dorset. Prate I. Geological Map of the neighbourhood of Weymouth and the adjacent parts of the coast of Dorset. The reader is requested to take notice that the authors do not profess to mark the exact limits of the lower Purbeck Beds in Portland, but merely to indicate their presence as the uppermost formation in the north end of that island. Pratt II. Series of Sections.—Colours the same as in the Map. Fig. 1. Section from the Great fault near Upway to the Bill of Portland*. Fig. 2. Section from the Great fault near Moigne’s Down Farm to Ringstead Bay. Fig. 3. Section from the Great fault near Poxwell to the signal station near Osmington Mills. Fig. 4. Section from the Great fault near Sutton to the Sea at Ham Cliff. Fig. 5. Section from the Great fault near Sutton to Jordon Hill in Weymouth Bay. Fig. 6. Section from Abbotsbury Common over Linton Hill. Fig. 7. Section from Abbotsbury Castle to Abbotsbury Swanery, showing the continua- tion of the Great fault. Fig. 8. Coast section from Jordon Hill to near Boat Cove. the Oxford Clay and other strata at the east end of this section arises from an inden- tation of the coast: the strata have an E. and W. direction throughout, and dip rapidly N., and have not the bend here represented, by throwing the curves of the The apparent curvature in coast into a straight line. 9. Coast section from near the termination of fig. 8 to Ringstead Bay. As the coast ranges along the line of direction of the strata, its indentations give these strata a false appearance of dipping in different directions: they form a small arch at Osmington Mills. * The Scale (in length) of fig. 1. is one inch to the mile; of fig. 2. to 10. inclusive, two inches to the mile: figs. 11. to 13. inclusive are on a larger scale, and fig. 14. two inches to the mile. Fig. Fig Fig Fig. EXPLANATION OF THE PLATES. . 10. Coast section near White Nore. . 11. Fault in the Cliffs, a little W. of White Nore. 12. Theoretical diagram representing the manner in which different rocks may be seen in contact, in consequence of various degrees of denudation, on the same fault. II- lustrations of this may be found in Sutton Valley ;—where there is little or no denu- dation, the Portland Stone and Chalk are in contact at the surface; where a denuda- tion occurs to the depth of the curved line a a, the Portland Stone and Green Sand are in contact, on opposites sides of the fault; at the depth dd, the Portland Sand and green sand touch each other; and at the depth c c, the Kimmeridge clay touches green sand. @. 13. Fault in the cliff west of Bridport Harbour. . 13 a. Eastern termination of the Bridport Harbour fault. . 14. Section from the cliff west of Bridport Harbour to Askerswell. Prare III. . 1. Tabular and proportional view of the strata in the Weymouth district. . Angular flints and plastic clay. . Chalk. . Chalk interspersed with grains of green earth (Craie chloritée). . Indurated green sand, with quartz grains and quartzose sandstone. . Greenish brown sands with indurated concretions. > Light brown sands. Fox mould. - Green sandy marl beds, with nodules similar to the cow-stone at Lyme Regis. . Purbeck beds. . Dirt bed, above the Portland beds, frequently contains rolled calcareous pebbles, and fossil silicified trunks of large coniferous trees, and of Cyca- deoidez. k. Best beds of the Portland Stone. 7. Compact light-coloured limestone, with beds, seams, and nodules of chert. m. Grey shelly beds, the base of the Portland Stone. n. Green, brown, and grey sands and sandstones. 0. Brown and grey sandy marls, with indurated nodules. p- Kimmeridge clay, contains an abundance of deltoid oysters. qg. Clay ironstone in the lower part of the Kimmeridge clay. r. Upper grit beds, containing deltoid oysters: these beds are most fully deve- loped near Sandfoot Castle. - Oolite differently developed in different places. . Brown sands, containing indurated nodules of calcareous sandstone. . (Grey clay.” mos SL SS x, =< & ws w . Larger deposit of calcareous grit, containing Gryphea dilatata. ww. Oxford clay, grey marl, abounding in Gryphea dilatata. - Rubbly and slaty Cornbrash limestones, alternating with clays and marls. y. Slaty and shelly grey and brown limestones, containing Apiocrinites rotundus, lignite, broken shells, &c. 8 EXPLANATION OF THE PLATES. z. Grey marl, with marlstone in its lowest region. aa. Coarse granular limestone, loaded with grains and veins of hydrate of iron. 6 b. Light brown and yellow calcareo-siliceous sands and sandstones, often highly micaceous. Fig. 2. Section showing details of the Oxford oolite near the east extremity of Weymouth Bay. Fig.3. Detailed section of the strata that occur in the Isle of Portland. Note.—Since the paper was printed to which these sections refer, a notice has appeared in the London and Edinburgh Philosophical Magazine, August 1, 1833, p.158, by Mr. R. Phillips, containing a minute analysis of the water of two sulphureous springs of similar quality near Wey- mouth, both of which issue from near the junction of the lower beds of the Oxford clay with the cornbrash or upper beds of the Forest Marble Formation. One is situated at Nottington, about three miles on the North of Weymouth, and was described by Dr. Pickford in a small treatise printed at Weymouth in 1821. The other rises at Radipole, about one mile from Weymouth, and was discovered but a short time ago. The most important of the ingredients of these mineral waters is sulphuretted hydrogen, which is derived from the passage of the water through strata that contain iron pyrites in a state of decomposition. Mr. Phillips remarks that “ the saline con- tents of these waters are so small in quantity, that they must be considered as quite inert, and therefore those who wish to avail themselves merely of the sulphuretted hydrogen, may take them in larger quantity than if they were active in other respects. Pruates 1V. & V. Illustrate Professor Sedgwick’s paper introductory to the General Structure of the Cum- brian Mountains, with a description of the great dislocations by which they have been separated from the neighbouring carboniferous chains: p. 47. Prate IV. Map exhibiting the geological structure of the district, and the range of the band of lime- stone and calcareous slate between the quartzose green slate and the greywacké slate. Piate V. Sections exhibiting some of the great dislocations produced by the elevation of the northern carboniferous chain: p. 59. Prate VI. Illustrates Professor Sedgwick’s paper on a Series of longitudinal and transverse sections through a portion of the carboniferous chain between Penigent and Kirkby Stephen: p. 69. EXPLANATION OF THE PLATES. Puares VII. tro XXIII. Illustrate Dr. Fitton’s paper **On some of the strata between the Chalk and the Oxford ‘‘ Oolite, in the South-east of England”: p. 103, to 378. Prate VII. Contains small portions of the Maps of Kent, Surrey, and Wiltshire, reduced to half the scale of the Ordnance Survey. Fig.1. Part of the Coast of Kent: p.105—119. Fig.2. Part of Surrey: p.137—142. Fig. 3. The Vale of Wardour, South Wiltshire: p. 245—254. Prate VIII. A Sketch of part of the Coast of Kent, from Hythe to Folkstone Hill; reduced from a drawing by the Rev. J. D. Glennie: p. 108—127. Puate IX. Map of part of the South East of England, and of the opposite Coast of France, on the same scale with Mr. Gardner’s reduced Geological Map of England; about 18 miles to an inch. ‘The space occupied by strata above the chalk is taken from Mr. Greenough’s Map. ‘The divisions below the chalk are inserted from the information stated in the present paper, and will be given on a larger scale in the new edition of Mr. Greenough’s Geological Map. The continuous red lines, numbered 1. to 25., refer to the sections described in this paper, and represented in Plate X.a. The dotted lines adjacent to Nos. 15. and 16. represent the course of Mr. Lonsdale’s sections, (Geol. Trans. 2nd Series, vol. ili. pl. 32.) ; and those adjoining Nos. 18 and 21, are ¢ransverse sections in Oxfordshire and Bucks. The blue lines denote some of the anticlinal lines; those in the vicinity of Bristol are from Messrs. Buck- land and Conybeare’s map, (Geol. Trans. 2nd Series, vol. i. pl. 38.) ; the rest from the statements of the present paper. On the French coast, from Calais to Treport, the colours are inserted from the manuscript notes of the author: In the Pays de Bray, and thence to the mouth of the Seine and coast of Normandy, they are taken principally from M. Passy’s map of the Depart- ment of the Lower Seine, with some additions by Mr. De la Beche: thence to Cherbourg, from the maps annexed to the papers of M. Desnoyers and M. Con- stant Prevost, in the Annales des Sciences Naturelles, tome iv. 1825; and. of the former, in the Mémoires de la Société d@ Histoire Naturelle de Paris, tome ii. 1825. The depths of water in the English Channel are taken from the Admiralty Chart. The lines under the figures were intended to represent the form of the bottom; but the depths are so enormously exaggerated, that without explanation they would convey a very erroneous impression. Mr. De la Beche’s section of the channel between Portland and Cape La Hogue *, on the true relative scale of depths and horizontal distance, and more than five times as long as in this map, is scarcely different from an uniform line ruled with a common pen. * Sections and Views,” &e. 4to, 1830. Plate II. fig. 2. > 2 ee ee eee vv ee ee ee ee EXPLANATION OF THE PLATES. Puate X. a. Contains a series of sections, at right angles to the range of the chalk, on the lines marked in the map, Pl. [X., Nos. 1. to 25. The series begins on the coast north of Folkstone, and follows the outcrop of the chalk, round the Weald denudation of Kent and Surrey, &c.; thence along the coast, to Devonshire; and in the interior, from the Blackdown Hills to Norfolk. These sections are all drawn to the scale of the Ordnance maps, one inch toa mile. The heights are of necessity much exaggerated ; but additional lines are given below Nos. 6. and 7. in the true proportion of height and distance. No.1. Section from Folkstone Hill to Copt Point, Kent: p. 104.—(See the Map, Pl. VII. fig. 1.; and Sectional Sketch; Pl. X. b. fig. 1.). No.2. Through Tilburstow Hill and Godstone, Surrey: p. 137.—(See the Map, Pl. VII. fig. 2.) No. 3. Through Nuffield and Merstham, Surrey: p.137—141.—(See the Map, Pl. VII. fig, 2.) No. 4. From Hindhead, Surrey, through Tucksbury Hill, near Farnham: p. 144—149. No. 5. Section across the Wealds, from the South Downs at Duncton-Beacon, through Floxham Park, Plaistow, and Aldfold, to the North Downs at Netley Heath; ‘principally from Mr. Martin’s MSS.: p. 155—160. No.6. The Coast of Sussex and Kent, from Beachy Head to Folkstone Hill;—part of which is given in greater detail in Pl. X. b. fig. 3. The lower line of this figure re- presents the cliffs on the true relative scale of height and horizontal extent: p. 161 —164. No.7. Part of the South Coast of the Isle of Wight; from Afton-Down to Rocken-End, and from Dunnose to Bembridge Down:—(See also the transverse Section Pl. X. b. fig. 4.). In the lower line of this figure, the heights are in the true proportion to the horizontal distances.—p. 182—202. No.8. From Durlstone Head, through Swanage, to Ballard Down, Dorsetshire: p. 206 —215. No. 9. From Broadbench, in Kimmeridge Bay, Isle of Purbeck, to the Chalk-hills: p. 206 —215.—(See Pl. X. b. figs. 5. and 6.). No. 10. Section at Lulworth Cove, Dorsetshire: p. 215—216.—(See Pl. X. b. fig. 7.) No. 10’. Section at Man of War Cove, west of Lulworth, Dorsetshire: p.215—217.— (See Pl. X. b. fig. 8.) No. 11. Coast near Bere, Devonshire: p. 234.—(See Pl. X. b. fig. 9.). No. 12. Blackdown Hill, Devonshire: p. 238. No. 13. Sections of the Vale of Wardour, in South Wiltshire: p. 245—255.—(See the Map, PI. VII. fig. 3.). — — on the anticlinal line, A. B. —— on the transverse line, C. D. —— on the transverse line, E. F. —— on the transverse line, G, H. No. 14. Vale of Warminster, South Wilts: p. 257. EXPLANATION OF THE PLATES. No. 15. Poulshot-Green to Etchilhampton Down, North Wilts; drawn by Mr. Lonsdale : p: 261, 262. No. 16. Sandridge Hill to Beacon-Down Hill, North Wilts ; Mr. Lonsdale: p. 262—-266. (The dotted red lines adjacent to Nos. 15. and 16. in the map PI. IX. denote the course of the Sections connected with Mr. Lonsdale’s Paper in the Geol. Trans., Qnd Series, Vol. iii.; Pl. 32, figs. 1, 4, and 6.] No. 17. Swindon to Liddington Castle Hill, North Wilts: p. 264—266. No. 18. Oxford, through Shotover Hill, and Great Hazeley, to the chalk range, south- west of Stokenchurch Hill: p. 270—274. The flap, No. 18/., gives the section, on a line nearly parallel to No. 18., along the main road from Oxford to London, through Wheatley and Tetsworth: p.271— 279.—(See the transverse section Pl. X.b. fig. 10.) No.19. From Blackthorn-Hill, in Oxfordshire, through Muswell-Hill, Brill, and Thame, to the chalk near Bledlow ridge: p. 270—-279. No.20. From the north-west of Whitchurch, through Aylesbury, Bucks, to Wendover Hill, Berkshire: p. 270—284.—(See the transverse section, Pl. X. b. fig. 11.) No. 21. Through Woburn, Hockliffe, and Dunstable, Bedfordshire: p.270—293. The flap, No.21'., is the Section from Fenny Stratford, through Little Brick-Hill, to Hockliffe: p. 270—293. No. 22. From Caxton Gibbet, Huntingdonshire, through Cambridge, to Balsham: p. 305—308. No. 23. Haddenham, through Denny Abbey, to Bottisham, Cambridgeshire: p. 305. No. 24. Through Upware on the Cam, to Swaffham Prior, Cambridgeshire: p. 305. No. 25. Through Lynn, to Swaffham, West Norfolk; by Mr. C. B. Rose: p. 310—312. No. 26. Hunstanton Cliff; Norfolk: p. 310—313. (See Plate X.b. fig. 12, a. b. and c.) Prate X. b.* This Plate contains miscellaneous Views and Sections, on different scales, illustrating the country represented in some of the sections of Pl. X.a. 1. A sketch of part of the Coast near Folkstone, not visible in the direct line from the sea: p.106—108. Reduced from a drawing by the Rev. C. D. Glennie.—(See Plate X. a. No. 1. Fig. 2. Section on the west of Pulborough, in Western Sussex, showing the subdivisions of the Lower Greensand: Mr. Martin’s MSS.: p. 155. fig. 3. Enlarged Section, on the same scale of height and distance, of part of the coast near Hastings and St. Leonard’s, Sussex: p. 164.—(See Pl. X.a. No.6.). Fig. 4. Transverse Section, from Brook Point to Shalcomb Down, Isle of Wight: p. 200. —(See Pl. X.a. No. 7.) Fig. 5. Enlarged Section at Emme?’s Hill, Isle of Purbeck: p. 211.—(See Pl. X.a. No. 8.) Fig. 6. Ideal Section, from S¢. Alban’s Head to Worbarrow knob, in the Isle of Purbeck : page 211, 212.—(See Pl. X.a. No. 9.) yy ° 5° * This Plate is subsidiary to Plate X. a. ; but is placed before it in binding, that both may fold out and be consulted at the same time. EXPLANATION OF THE PLATES. Fig. 7. East side of Lulworth Cove, Dorsetshire: p.216.—(See Pl. X. a. No. 10.) Fig. 8. Plan of Durdile, and Man-of-War Coves, and Section of the latter: p. 215—217. (See Pl. X.a. No. 10/.) Fig.9. Enlarged Section of part of the coast of Devonshire, from Seaton to Branscomb Mouth: p.234.—(See Plate X. a. N.11.) Fig. 10. Transverse Section through Garsington and Wheatley, in Oxfordshire: p. 273. —(See Pl. X. a. No. 18’.) Fig. 11. Transverse Section through Quainton and Whitchurch, Bucks: p. 271.—(See Pl. X. a. No. 20.) Fig.12. a.b.and c. Hunstanton Cliff; Norfolk. Fig. 12. a. Map of part of the north-west Coast of Norfolk; from the Ordnance Survey, and on the same scale,—one inch to the mile: p..310—313. Fig. 12.6. Enlarged Section of Hunstanton Cliff; by Mr. Murchison: p. 310.— (See Plate X. a. No. 26.) Fig.12.c. View of Hunstanton Cliff; from the point « of the preceding figure; from a sketch by the Rev. W. Whewell: p. 310. Fig.13. Abstract Section, representing the whole series of strata illustrated in Plates X.a. and X.b.: p. 318, &c. Prates XI tro XXIII. These Plates contain figures of the new and more remarkable fossils, obtained from the tract described in Dr. Fitton’s paper. The details are explained in Mr. Sowerby’s descriptive notes; Appendix A.—p. 335—348. Pirate XI.f FOSSILS OF THE UPPER GREEN-SAND AND GAULT. CHALK MARL. Fig. 6. Pollicipes radiatus. (Low- | Fig. 14. Solarium conoideum. Fig. 1. Tornatella elongata. er green-sand, p. 130.) 15. Pyrula Smithii. 6*, ———— rigidus. 16. Rostellaria elongata. LIES EUS 2 SNL 7. Venus? tenera. 17, ————— buccinoides. 2. Lucina? globosa. 7*.Venericardia tenuicosta. 18, ————— marginata. 3. Avicula grypheoides. 8. Nucula bivirgata. 19, —————-- carinata. 9. Modiola bella. 20. Ammonites circularis. GAULT. 10. Lima semisulcata, 21, —————- symmetricus. 4. Pentacrinites. 11. Auricula inflata. 22, ——- crenatus. 5. Pollicipes levis. 12. Natica canaliculata. 23, ———- cristatus. 5*, ——--_~ unguls. 13, Solarium ornatum. Pirate XII. FOSSILS OF THE GAULT (continued), Fig. 1, 2. Hamites rotundus. | Fig. 3. Hamites attenuatus. | Fig.4. Hamites spiniger. Prate XIII. FOSSILS OF THE LOWER GREEN-SAND. Fig. 1. Echinus? arenosus. Fig. 3. Trigonia spinosa (var.). Fig. 4. Diceras Lonsdalii. 2. Panopea rotundata. + In the following lists of names, the mew species are in Roman characters; those previously figured, in Italics. EXPLANATION OF THE PLATES. Puate XIV. FOSSILS OF THE LOWER GREEN-SAND, (continued). Pholas giganteus. . Modiola \ineata. . Avicula pectinata. . Ostrea retusa. . Anomia radiata. levigata. Fig. Dow Wt Fig. 7. Anomia convexa. 8. Zerebratula Tamarindus. oP quadrata. 10. —— Faba. 11. ——_-—— elegans. 12. ——— conyexa. Puate XV. Fig. 18. Yerebratula parvirostris. 14. prelonga. 15. Lingula truncata. 16. Pleurotomaria striata. 17. Ammonites furcatus. FOSSILS OF THE LOWER GREEN-SAND, (continued). Scaphites Hillsii; the detail of the figures is explained at p. 339. Puate XV. a. FOSSILS OF THE GREEN-SAND OF BLACKDOWN, Siphonia pyriformis ; the figures are explained in detail at p. 340. Puiate XVI. FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued). Fig. 1. Pollicipes levis. . Serpula filiformis. Tuba. Vermes. . Panopea ovalis. . Mya leviuscula. . Amphidesma tenuistriatum. MIO COR ot Fig. 8. Corbula truncata. 9. Mactra? angulata. 10. Petricola nuciformis. 11, ———— canaliculata. 12. Psammobia? gracilis. 138. Lucina orbicularis. Pisum. Pirate XVII. Fig. 15. Astarte concinna. 16. formosa. Uf multistriata. 18. impolita. 19. Cyprina cuneata. FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued). Fig. 1. Cyprina rostrata. . Cytherea subrotunda +. . Venus? truncata. submersa. sublzevis. immersa. . Cucullea formosa. NOOB Owe Fig. 8. Arca rotundata. 9. Nucula lineata. apiculata. ; obtusa. 12. Trigonia quadrata. 13. Modiola reversa. 14. Mytilus tridens. Pirate XVIII. Fig. 15. Mytilus prelongus. ineequivalvis. 17. Perna rostrata. 18. Avicula anomala. 19. Pecten Millerii. , - compositus. 21. Lima subovalis. FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued). . Pecten Stutchburiensis. . Terebratula dilatata. megatrema. . Dentalium medium. . Litorina pungens. . Natica canaliculata. granosa. ? carinata. . Tornatella affinis. CONaonpwNhe Fig. 10. Vermetus concavus. 11. Scalaria pulchra. 12. Litorina gracilis. 13. Phasianella pusilla. 14. ——————_ formosa. 15. striata. 16. Fusus rigidus. 17. quadratus. 18. —— rusticus. Puate XIX. FOSSILS OF THE WEALDEN,. Fig. 19. Fusus clathratus. 20. Pyrula depressa. 21. Brightii. 22. Rostellaria retusa. 23. —————- macrostoma. 24, ———_——- Parkinsonii. 25. Nassa lineata. 26. costellata. 27. Ammonites triserialis. External forms of Endogenites erosa: the details are explained at p. 173—175. + In the Table at p. 355, Cytherea subrotunda is erroneously referred to Plate XXII. fig. 2. EXPLANATION OF THE PLATES. Pirate XX. FOSSILS OF THE WEALDEN (continued). Illustrates the internal structure of Endogenites erosa ; the details are given at pp. 175, 176. Puate X XI. FOSSILS OF THE WEALDEN (continued), Fig. 1. Cypris Valdensis. Fig. 7. Cyclas parva. Fig. 13. Cyclas major. Zz. —— tuberculata. 8. subquadrata. 14, Unio Mantellii. 3. spinigera. 9. —— elongata. 15. subtruncatus, 4. granulosa. 10. —— media. 16. Gualterii. 5. Corbula alata. 11. -—— , (var.) ; Wie Martinii. 6. Psammobia tellinoides. 12. —— angulata. 18. Mytilus Lyellii. Pirate XXII. FOSSILS OF THE WEALDEN AND PORTLAND-STONE. Fig. 6. Paludina Sussexiensis. Fig. 11. An unknown body from VEREPEM, 7. Neritina Fittonii. Quainton; (p. 349.) Fig. 1. Exogyra Bulla. 8. Tornatella Popii. 2. Ostrea distorta. 9. A Conefrom the Isle of Pur- EE TE ANDES TONES 3. Bulla Mantelliana. beck; (p. 349.) 12. Lucina Portlandica. 4. Melanopsis? tricarinata, 10. A Cone from Sussex; (p. 13. Cytherea rugosa. 5. — attenuata. 349.) 14. Trigonia incurva. Prate XXIII. FOSSILS OF THE PORTLAND-STONE, KIMMERIDGE-CLAY, AND OXFORD-OOLITE. PORTLAND-STONE (continued). Fig. 6. Terebra Portlandica. Fig. 10. Exogyra Virgula. Fig. 1. Ostrea falcata. 11. Trigonellites latus. 2. Nerita angulata. KIMMERIDGE & WEYMOUTH STRATA. 3. Natica elegans. 7. Serpula variabilis. cca peas aes 4. Buccinum naticoide. triserrata. 12. Nerinea Goodhallii. 5. ————— angulatum. 9. Panopea depressa. Pirate XXIV. I}lustrates Mr. Bell’s Memoir “On a new fossil species of Chelydra”: p. 379—381. Piate X XV. Illustrates Professor Sedgwick’s memoir ‘‘ On the new red sandstone series, in the basin ‘‘ of the Eden and north-western coasts of Cumberland”: p. 383—407. Fig. 1. Section on the coast of Cumberland, between Parton and St. Bee’s Head: p. 391 —393. Fig. 2. Section from the mountains east of Mollerstang, to the overlying conglomerates in the valley of the Eden above Kirkby Stephen; showing the great fault and the breaks in the carboniferous series; p. 383—390. Fig. 3. Section from the greywacké mountains of Westmorland, through Orton Scar and Burrels, to the Eden; p. 386. Fig. 4. Section exposed in Ben How quarry, between St. Bees and Whitehaven: p. 388. Fig. 5. Section from the mountains of Copeland Forest, through Cold Fell, to the sea north of the river Calder: p. 389—391. EXPLANATION OF THE PLATES. Fig.6. Section from Corney Fell to the sea-coast west of Bootle: p. 389—399. Fig. 7. Section from the Mountain Limestone Hills at Low Furnace, to Salt-Coats oppo- site the Island of Barrow: p. 389. Puates XXVI. tro XXVIII. Illustrate Col. Sykes’s memoirs “On a portion of the Dukhun in the East Indies”: p. 409—432. Puate XXVI. Map of the Dukhun. Puate X XVII. Panoramic Sketches. No. 1. is a distant view of the mountains, on which are situated the celebrated /ill Sorts of Jewdun, &c. It is taken from the hill N. of the town of Goreh: p. 432. No. 2. A view of the hills, to the North and East, as seen from Lakungaon in the flat broad valley of Jooneir (Sewneir). No. 2*. is a continuation of the view No. 2. from the North round to the West. No. 3. A sketch of the Azlls to the North and East, as seen from the summit of the armoury, in the fort of Ahmednuggur. No. 4. A sketch of the northern flank of the Plateau on which the city of Ahmed- nuggur stands ; as seen from Wamooree, in the plain of the Godavery river. Prate XXVIII. Fig. 1. Elevation and declination of the country above the Ghats, between 73° 35! and 74° 49' East Longitude, and 18° 50! and 19° 10! 3" North Latitude: p. 411—418, 432. Fig. 2+. Elevation and declination of the country above the Ghats, between 17° 35! and 74° 49' Kast Longitude, and 18° 28! and 18° 50! North Latitude: p. 424—432. These Sections are fully explained at p. 432. Prate XXIX. Illustrates Mr. Horner’s paper “On the Environs of Bonn”; p. 433—481. The principal division of the plate is a Map of the Environs of Bonn; described at p- 434. Beneath is a panoramic view of the Hills on the East of the Rhine, as seen from the Coblentz Gate of Bonn. The remaining division of the Plate represents the vertebra of a Fish, probably, of the genus Zamna, found in the loess near Basle; the smaller figures are of the natural size; pp. 476, 480. + In the engraving of fig. 2., the names Moteh and Mota are confounded. Mota is the name of the River, Moteh that of the Town. + ad Geel. Trane, Lerten, Voi tv. Plate 1 POARTLAN D laridsfoot Castle ROAD Bottom of Kimmeridge Clay tland Nore Cay he Vly, LPAIR I of , ‘ f fr Suse Castle AB line cf Section Prats 2. ID © ik, S 1; a ‘S| Jef It ik Te, 5 [.K.Line of Section. Place 2. CD). Lane of Section 1, M Line of / = KF. Line of Section sat J Gt Line of Section Se ~ 4 % rave Hole y ce f £ h 1 Green Sand. Purbeck Stone Portland Stone Pavrtllaned Sand & Sandstone KinmerifgeClay xt Colite b: Catrarenus (eit Oxford Clay Cornbrash &Forest Marble Inferior Oolite Blocks of Silicasus Ficlding Stone BILL of LORTLAND Scale of Statute Miles | as eee eee eee : Ls ea es “ortiand Rae Fairings Lithey fae _ OpQQTVT SPLOT QI) STOMP TIED i * s@uayspun sy ¥ ; " ; " sprT “PRO LOL4UT PP etiey “Avy, 2) PLOZLO yy 77°O PAO “AP}D Li lel Ps Pee, (eat es audigy (Beal a PURS YPAQMNT png wad YIP? me T J P 5 “AbD App "YN O() LOYUT pay sory edd} —— . ag VIAN h ; nD -aygnyy asatog yroaucg AbPD i ted | Mi daa Any Lodpingy : aon 7 "OGLE ALOT: MII M, MOLT POTPIAT uomag wads (any mp se Od) pp hh LT KS ON YWPU? “yyou? “pimg Uarty Aoy) Uy LL punodua) sz aoe UPL YPPUD BQO IS ALOT: PUI TT UH, Cue a ‘24ON RUA M weroy 6 . 61 Se or Ot aby) PLpxo ADZD PtIXO “gue OTR) R10 PEED ‘BH Mpsor Ang poasbuny agian Owe oa ft gar M Aare Amgsyoqqy ‘ iat “ ay Aang: cows phn th opsny Amngswoqqe (ID) "9 hr LT uounue) rae yt s N- Ss N i ee wn wey DH WORST gee AY fey fst e (xT Gbiy ~ (Ho) pO 3 sng, poapobuny ~ ee 4 a . ae e ype aa eae veya Ud? “snot To a eae yy 1 unops seu yg nopseube. uli WH und) s rao/ bry K er noe Of yey 24 Ay - N General Section of the Strata in the Weymouth District, Angalar Fhiuts and Plastic Clay. Green Sand. Purbeck Beds. Portland. Stone. Portland Sand. Kinmeridge Clay. Upper Calcareons Grit. Oxford Oolite. Lower Calcareous Grit. Forest Marble. Tnferior Oolite. ~. WT de la Beche. del Fig.1. 20. 100. 4°. 70. 80. 300 4oo. zZ. aa, 300. bb. Geol Trans. 2° Series Vol .N PLB. Fig. 2. Section between Ringstead Bay & Osmmington Mills. Kimmeridge Clay. Bed of Cay Ironstone. Upper alcareous Grit. Bubbly Linestone. Oolite. Gray Marl. Grit Beds, marl partings. . Light brown sand | with concretions Oxford Oolite. Gray Marl. Lower Qlcareous Grit. [__— Fig.d. Section of the Chffof Black Nore W. side of Portland. laleareous Slate, Dirthed Fossil Trees, Cycadeoidex. Top lap. q Roach. Good Stone. Gompact & Chalhy limestone with chert. Portland Stone. Tubbly beds with chert. Sandy limestone with chert. Shelly gray linestone. Gray & Brown Sandy Mart & Sandstones. Dark Sandy Marl with Sandstone concretions Portland Sand. Fallen Masses of Kock. -_— 4, 7) \ i tain westone Ki ff § a S, = 7 Li Geol.Trans. 2° Series, Val IV-PL4 - Z = g ES) . S N ANY ) = f NS So eeZ : r SNPs AD RW SS = 4 = eee 8 BS ry Ss “Ss VL OY ij PAN iy 87 g % S S | s§ as QN | x 8 ~~ a& N S eS ~~ eS QR as es SS % iB = SS § 2 : S Fig . (p.3g) Geol. Trans. 2? Series Vol A PLS. Leak of Derbyshire Derbyshire Coal Fig. 2. /p.60) Lancashire Coal Blackstone Edge Fork sit re Coal Fig. 3. (pp. 60.62) Ingleborough TIT raeerrry Ganbrian Mountains Fig. 6. (p.62/ Goss Fell Chain 7) Fig.7. (pp. 61.63) < N. Swaledale Head Brough Scar Wi Bar ae Sy tones Wew Red agnesian Gal Millstone Limestone. Shale, Sear Old Red Grouwadee Sandstone. Limestone. Measures. Grit. & Sandstone. Limestone. Sandstone. Fig 1. GENERAL SECTION oF THE CARBONIFEROUS LIMESTONE SERIES &.MILLSTONE GRIT. (See p.70) Thin bands of Coal. Coal seam of Turna Fellmuch worked. \ Thin band of Coal worked to the north of the line of Section. Numerous Clagstone quarries, Longitudinal and Our. | in alee co Trace of Goal at Rawthay Gill. — \ Silicoous Flagstone used for rooting slate. Barton Coal seam, much worked . Fis epetem ie PARSE SCONE A thin Coal band.not now worked. Trials for Gat. Blask marble Group. Carbonaceous shale, F: lig. 2, LONGITUDINAL SECTION 7 SSE. aco Moulton Fell Baw Fell oor” Risell Uiduale ceeecond Millstone V5). Swath Fell Garsdale Fig. 3. LONGITUDINAL SECTION FROM THE TOP OF PENIGENT 10 THE TOP OF STAGS FELL NEAR "oC S'- Ws tone Cam Doa Penigent . yo" pimest uw. nw Fart of NYU &NN3. Second Milletone Grit, V5) Shale, Grit & Coral, and first Millstone V3) « River Ribble SERIES OF TRANSVERSE : SWhy We Fig. 5. TRANSVERSE SECTION. Se p94) Moughton Fell Clapham Clapham Beck Horton Why N. : Eby 8. Barki Cr r my Ca sterton figh Pell Ww. Fig. 7. TRANSVERSE SECTION | ‘00 p95! Howgill Fells Short Gill VGITUDINAL. SECTION THROUGH THE CARBONIFEROUS CHAIN FROM PENIGENT TO THE PLAINS OF THE EDEN NEAR KIRKBY STEPHEN | (5 p00 WW. Whernside &. Simon Fell 3 ee ‘ 5) ea Great Colm Clas — as a eet wocot Secundt Millstone V9) Groups ot ’ : ye i: pala Shale, Grit. foul IA\First Millatone Grit V3). ’ ap immeatone D* Piet wh Combe 2 — _—kittle Colon State Quarries Be - Chapel le Dale - = § ibd The line trom Whernside : A to Great Colm deflects ni im ec ££ C*eh oe . due west acroes Deepdale. Fg. 2. CONTINUE D. © DS : Dolphin Sty got! aciteeen. Wild Boar Fell coal pass metal Send Sioa p ‘ weail oat vet * . oe a net there Kirkby Stephen River Eden e s t ° n © a : : Greate S c @F Zameen ; one "Conglomerate of New Red Sandstone oo OF ST. AGS FELL NEAR HAWES. (Se p91 Fig. 4. LONGITUDINAL SECTION FROM THE TOP OF WHERNSIDE TO THE TOP OF SHUNNER FELL AT SWALEDALE HEAD «©: Sepi92 NINE. oS = | a> = WE. | Stags Fell Whernside ie Cross Cotter Fell Shunner Fell | Mosdale Mill. grit representing all i Cha grome Ton i 13" groups F to inclusive. hudtihy S84 813. HUES OF TRANSIERSE SECTIONS CONNECTING THE LONGITUDINAL SECTIONS WITH THE GREYWACKE CHAINS OF WESTMORLAND. — os AS ag abs)? rea . Fig. 6. TRANSVERSE SECTION, (5ap95) : Trace or Second Miltstone Vs) penraie: . pate Sear Limestone \V. ESE. Wey : ; Harter Fell Fig. 9, TRANSVERSE SECTION, | 5ep.97/ Wild Boer Fell Millstone Grit ke V5 to V3. Clouds Ravenstonedale reywacké pik ; 2 es Geol. Lrans. 2 Serves Vol. LV, Ft. VIL. Mole F. Uprcoldhame FOLESTONE PART OF THE COAST OF KENT. Fig 2 Tothiunst PART oF SURREY. Gmpton ' . a Hut d pr oe ‘ “tt Ebbeshorne c - yA Wak ‘Alvediston VALE oF WARDOUR, WILTSHIRE, : = : Kinuneridge Clay Hastings Sand & inferior beds ee Purbeck Strata Lines of Section Portland awe Anticlinal line Fig 3.AB + dechcontbe —) CSS Lower Greensand ——— ee di a Lower Greensand Fig.3 { I | Stone t Weald Clay Fight 2.” a sand! Scale 1 % 0 1 2 3 Miles * o < ] Sheth of Tart of the Coast of Kint, fiom Hy the to hotkstone Milt Gaol Teac By Saree OEY Bt r“Quarrver » Lolsferd: Hla + Sadtwood Castle ~ v feachboro Summer House * Gucarrves bi fiat v4 Meal Down J24 ject Hythe wdourt £08) feet Seabrook ~ * Paracre Wood: ovKickmond Shaw ~>~+Dentons Pinel ~ Cherctor Church Bocsags i ¥ £69 feee ‘Prospect Place te dir ce 2 ~ Artillery Barracks ; ~ Castle ~ Chapel Sandgate A range of Rocks, of the lower Greengandab low water mark . 3 ; 5 ; ~ Castle Hill . Cliff Oop abou 199 feet Spring breades cme ~ Sagar Tioef Fide ere area Lit MAT x Lower H23. thf Marielle DW. 251 fiat : Folkestone Copt Point. Tower. 1427" . 132 feetr — *Palkavtone Mild 257 fie fea ciaz Upper Greensand I Lower Greensand Weald Clay Frnedl by Clhslimaandtel Gale = ‘ Redivced from wv Steetch by the Rev *1D Glennae - The Hughes are taken prom the mean bored of the Sea Bo eae ag) Me ra Nh ae i Geol Thins 2% Serves Vol I PLE ; te ae —__——— - ———_——_—— SSS f. ' i \ ~ I MAP A A atore econ | aaa of part of the : oy aa. SOUTH EAST or ENGLAND, ; pera — and of the EE (eet et OPPOSITE COAST , j K B y oF FRANCE, a) Bett de. a ae eee Se ee 2 sR) frtind stone & sand. DR Birvneridoe 8 Wesnoth bets, ese | ston! Oolite & beds beneath. a —_—$—<_ lines of Section. N°1 to 26. Anticlinal Lines. The Depths of the Sea. at low wirter; are expressed in tithome, —YouTH or Mo TU Ty Mes. WN. Foreland Ken = Adenge Baer Lew De Brightovi Bowing deat — ; we Wesrthing x Sabra Bill oNeufchatel « Guillefontaine lite an Bayinenion: sph eek ee Bhi i Ene hi tS. # Ov THE {scan ia) i OF << Lute’; | Ss ia daa sae (CAS Ss (day ay EX ._ pit. Fog HASTING s 7 shale Chanare iy direction wt E nee One Enitogenites ; pep : ; , Warriors Gate op ort - Catle Rock Rast : S' Leonards a : 2 — sina sor oo wa08 Fiices Fotkstoane, from the Eas t pe Fig. 4 | Fig. 8 x a ; Downy, j tf owe ata West of PULBOROUGH, Susy 60 piss. — Dar dia Cowie: | wt a Fig. 2 Brook Point to Shalcomb Down. / % Isle of Wight. p200. / 4 : rst a = ne zs wn aie pe ~ o at . Por, ms 2 - wobittig ee? si ; —=2== = = Fae = a ee eae. > i= wy T Mile deat Section ss EAD. Li of Parte ch .per X be \ 2 ‘ : Fig 6 \ ' gt cel wil sills a / Man of War Cove ’ se! we poll ww | t PY otto! : ( Tet Mage 202) io SMbans Head y PSE eS tte 1) Ose ea aI ONT, Tie EC VO) ae { = a © Fig. 7 290 sous foot (see text page 216) 4 a See 4 N. S a : =f Frente Carpmune Poot —— pa 20 TSA et #4 ~ indies = —— ee J n — . Part of the N.W. of fo lle. 2 , FEE VES Ta ONE DO! BF CLIF F, Norfo && .-pan. BERE HEAD, Devonshirey ps. “ x a stall Siptiheices | Fiy 12 bs. Fig, 12. ©. and WHITCHURCH, Bucks. p27. Whitchurch Seale of Miles TUE WEALDEN e 10. u ABSTRACT SECTION ot the Sertes: of Strata represented m this Plate.and in PlateX.a- Superficial Greevel Bagehot Sard Londen Cay. Vlastic Tay: alk: = Weald Gaye Hastings Sant Aster Oolite. Qurend Gay _ hae Yowale of Keestwater Ce a - — > test Mindhead V3. MER een, SULTON. plo : na) yw ° : : Wd HInnpnHeEAD fro TeceKsS BURY A | ; Aldershot = . Nuttlotd ie | Merstham eine yw ~~» ~ x” ca | core, “2 a ee Birewk i i] V = ‘s 4 " } oe : ‘ eit 2 = naa Pi = Fersham Common Parclight Down 1 woe o e ‘ NT 6.5 P t Pevensey gi Z ‘ exh . ‘soaps en a ah PO by hE ¢ wher -s < aii we ov es hy = Se aa ee ae tere ag au as Oo. Ty aE Di hie I Pa O F W IDG A 47 R piss. S* Gtherenes Dowe 830 18 SEhensifasce Deowes Shanklin Down Bee AT SwavnaGe BAK” 2 A space of about four miles emitted here ix eanpicd - - pte. by @ eoncinuution of the sume Strats. 5 AWD Oo. Wr BAY, p87 14, SS or at oo ot amt e - om ° ~ Qa Red Clitr : V° ss. Through Powrsuor GREEN: Vorth Wilts. 1 ene Ee Py es. Or Ten oe D iO Ir oR Wilts. p.246-256 = p2ee. ( VOU. VALE OF WARMINS VELES..p 287, ton Mit Vlate VU fig. 3. Brimtock Lown é 7. 2. MI TER, Welts. p27. —_ ra rs This Deverill ‘dl Fs i Warminster ng brie farmin: oo OP ee \ sSivele wf Distewwrs. Otwe Trach te «4 Mile. ? SO0Oa TH DOWNS, WES TBR N Ss U AY S fieuks fo the OR RE ALE £L S.-pis. New thls pliscw the Carnal falls by The spene here cosignal 0 the Waskd Cpr is rack anayrervtnd. in consnywerice the Oily of the Section te the Line of Dip Bleck saiey ters 0 fe The Summit level of the Surrey & Sussex Coral wheat ue yo Cowntodd 2 wile distant ix HOS thet above the Seer act Love Wester Aldfold Spur Wo Phistow Aahrin ee Pa oe I Dallinglurst The eights, thom Qitk ond t0 the East ot Uvthe, which appear w have firmed the trast at some remote ported .are now sapsirated trom the Soa bo the artensive Mint of Remagy Marshes. Denge Nes, the South eastern extremity of this low tracttt HW Miles sistant from Applatore ol Ke ingto Warehor r a i aay on m nasi Panchey Down WW, COAST near BERE, Devon. p.23#, N° it. BLACKDPOWN, Devon. s ap -258 _ Ye Ww = =: a Soe ex | WHEATLEY through TET § WOR T M pp2mes. Shot 3097! _tarspath, con Wheatley Silisacast L) Y t ‘moe aan Oo rays 4 a 40 Se a ce ges ~ Tr = thei a tel a SWINDON through LIDPDINGTO Pade’ 97/3 ‘Svindon _ pp. 264. NW Ontton Park Through Chilton LOW G=-C REN Long Crendon DON and T H A M £E.-p.279. iio Fowersey OT — Blackthorn Hill Easington ition ‘ - “> = Thame ti PO BAL S H A MH. .p.30b. Whitehnech oy 20. FROM WHITCHURCH, through AYLESBURY, to WENDOVER-~HILE._p203. Halsham eros Stone Pits Sule Mandeville "eg Nem Fulbenurne —t Road w Newmarker . — -— &d Mbilex roan Lesradirn Aslesbury or ESE rs see __ncalhe oa — 2M F EN: -SvRATEORD through HOCKLIFF Bedfordshire. p-20s Bom Briobhiit , a = “ = eae cas 270.2 ZL. Brickhill Drertieg wo? Mocktife ) 5 . hi P on ¢ ~ ate . ——_ NE ar tem ys ow — a PS | Walon _p3o5- Swattham Poor pit Fancy — qn bee! Beets ee Fenny Stratford Gingl 24008 = £26. HUNSTANTON CLIFF, Norfolk. Pecan SRST nt SNR we x ‘ Spe CHALK-MARL. ge SUS ~ } ae 4 es 4 é 2 § pfeve {9% Ceol. Trans, 22 Serves Vol VELL UPPER GREENSAND. LOWER GS. JD.C. Sowerby fecit, a ae ne ed er ae al. Trans. 20 Series Fol. LVLLXL. 0 G AUL T_( continued.) G - Geol. Trans, 22 Series Vol IV Pt. £1, LOWER GREENSAND. a) 2) WIG? B9gN99 0 4o4 pi mE iS rn, F Ky \ SSH PE { Wik ANN “te Qe iW ieee TDC. Sowerby Lect. LOWER. GREENS AND_(continued) Geol Drans. 2] Series, Vol IV EL. ALV = SSS SSS NSS Uy, Geol. Trans. 20 Series, Vol LV PL AV. LOWER GREENS AND_(continued.) JD.C. Sowerby fecit Geol. Trans. 2 Series Vol IVPULXV. a. GREEN SAND (of Blackdown, Devonsh re.) Geol. Trans, 2¢ Series, Vol IV PLA, GREEN SAN D- (ol Blackdown.) continued Ceol. Dpans. 27 Series Vol. IVIL. XVIT, fot Blackdown) continued REE NS AVD- G TD.C. Sowerby teert. CLDrans Ze Series Vol LVPTAVIM. Geo REEN SAND (ot Blackdown) continued. ’ G <=" = JD.C Sowerby fecit. WHALDEN, LnAOGEHITES COSA. Cool. Trans. 4 Bee Sertes VoOLLV Plt. X1LX.~ 2. Feet TC. Of the natural size JD.C.Sowerly fecit magnets ed & times. WHALDEN, Lndogenttes CPrOStH. these two Ligures are magnitied 4 times Geol.Trans. 20 Series Vol lV. Pt, XX. ‘ magnitted 8 mes PUNO WEHEALDEN, (continued) Geol. Trans. 22 Series, Vol. LV PL, XAG. TD.C. Sowerby fect Geol. Trans. 2© Series Vol LV. PLAZTL, WEHEALDEWN- (continucd) J.D.C.Sowerby fe Geol Trans, 20 Series, Val. LV. PU. AXTIT. PORTLAND _ (continued) JD.C. Sowerby fe cit anadosryatnpy Miphzey) POVILDULY AZT 1) PDP MMIAT 77 WT DAG PQA boy2y Jvpos o VE LOTATIY PUOE PULRL SUNY. 7 °°D : a Mee “it vias wae ; OE eed be * Geol Tron. 26 Sor VOL PL AE ‘ | ’ < HGL SECTION on tip COAST oF CUMBERLAND BETWEEN PARTON uno S’ BEES HEAD, p. 391.39, ; Fig 4p. 366. Ben How Quarry, near 8! Bow. : fa Fig.? p. 383. 390. we fie Fig. 3.p. 586. il i Fig 5.p. 389. ID. ig Fort Fig. Cp. 569 5A 1 5 WwW. soot uf in flows” LI ~ os 4 or | a ——a7= = : ( Z Sa = — S = sa - ’ | / Green Slate & Torplyay Upper Slate Group. Old red Sandstone Gurboniterons Limestone Garboniterons Limestone Coal Measures Lower New Red Magnestan Limestone. New Red Sundstone (middle series) & conglomerate. ‘lower davaston) i upper division | Sarudstone. revting ane Heisei ITN Tah Mr bt iti } Fal de {sith IN iti ee Ai yl Wey Geol Trans. 2"4 Series, Vol IV. PL XVI. oS me i P ae 4 4 <4) os Begaghiua®, A ie | : 7 Aseer (| Amba. EX 5 “ herald Springs s | + F Copla, ° Sind duar °o Arrawud. B null diet 0) VY Tapheir Ghar Springs BOORHANPOOR fa = fxg | oF 2 OY Se ze . U Wewul or Vera s OME ~ Nussleerabad ° D ° ° —| 21 fi Thamal Springs " warungaon a hoolia (| | ag Galna Jauamner ° | Movtier Burygaon | Bhund 2. | Malligagf Z epee “a Adyuntah o > a —, c handore | of 2 . Peegnidner LA Wianeir Unkey | Ral ae ad MA. P & = Vinchoor oti Ellora . of ; °. 20 = Tealeh Aurungabad = = | }° : oo DUKHUN Mees ~ s Zopayaor id Lhooltambis er a he DD) Te Bes 8 fahatao Toe by Li Col! W. H. Sykes | re : 6 Vewassa PSs LGaS. | Hurreechundurgheun, ae - a | - eo - - g. oSomace a Malse Chit * g Sewgaon Seale #8 Miles to an lich Naneh Ghat © | ee es J, digg, Phonan Wareh. We ra ocleesgaon 0 72 4 36°°~«@f8 anes oon Alla. 4 Kuzjoon AI ° 4 = ¢) £0 Ahopeh 6 Grup, Bo Fe eee heor Ng B ee Nod ne ee . YeAHMBDNUGGUR anwor 19 ae i more SS li ° | a ~ a S Anko alia in: 19| hae ican er | Kundalldie ~% ¥ meyvon °)Sambcheir | Sy Log ae ¢ wa | 5 ‘Sew , ohiada | J Teckonehn aya c sa ve Bhoom ( | ' 2 oDhokeh Sgagaon Pada | & Purrunayo ofuugree Kull eoWangee oKumlapoor | Thermal Springs aes Rarhlonee 8 les 3 é soorne Oondaxgaon olyapoor ForuVictod Wahbuleshyiiire é | - onk cto £ Sour o Kurlumbh - 2 BSC Gi “pu” | Bhosah oWohol| 4 Main | ae Ge, SHOLAPOOR | uttao aS Lodiy Antalkcowteh i R TUAMACOWTN or \ Booshunghur sa Brum poor. B,.. eMindroop ° Koo: > 6 Hulsingeéo ; ‘ Kanapgor, Cherdee Manowr a i md A bdulpoor WP Z4JOL lee = Yasgaon d Tutt } ‘ dimilla : . Be 6 Tamba 7 r io) : A " liv B A ae) te eee fh Bhorgaon vtheecanent tae (ES a Ookileé ° 2 ° | Kolapoor a ya Ze: Kolutnoor Mungolee loomgee OD fagul S i ° f RS 5 B ecedree ‘Begehwarree s cS) A de ae alk, een Wepance meas Beelgel oumulgee = Y Jao , ~ ° Dowleshwuro “Yoodul Muchutw ‘ar faput Malwant Southern linit | Yardwa ~4 KP aus oft Trap in iojtaka Dudhee 5 ce BAGULKOT 7 Bu ° Gokauk > 16 2 ba < iw Toragul , PAZ LOOT" _ | al i 1G , & Munolee, B adam te Reduced trom a Map by Cap? a ee et Samuduttee ° Safihal ° Sopp Dep © Survevor Gen Lof SB oor Jim MEP OOT? “Sangolee on; pee ama yeas . Miers ZA India excepting places tn the SS Beamguah rere ae Ros ° ~ Koran, which are inserted SI Wi Nundigurh Bs ok al ~ ¥ ° 5 a tiem Arrowsmith Map. = Eiupheeree' D HARWAR BEACH | ° | ° 5 The Country described vs the ele auuel Hulliyal hoya Ql? portion of the Map. = Misrikota a at Boni: oSUu77Us ‘onignitel 2 Liichmeshwur } Sawapo° 15 v 15 7\3 7\4 75 WAH. Sylees Feeit. # a\ i ; : 7 a f a : {NENG ROMY Duras ‘ am ss aye, hy = me ’ sheng od” cc - Oe nl ~~ te a Pt > ues = ll = & é : al oat Yosh. here ee a Re roa SEY ws tt a on wa a ta yw h * % . - a 4d sal © vere navy + i PRPS * . ds r - ns bs We tenth: heth ye si a Pb err ae gate fy RR Yar ’ : a - me a sd / aR taka a —b ~~ — on PANORAMIC SIKETCIRUES. Geol. Trans.2™ Sep VOLIV-PL.AXVH. RANGE OF HILLS N AND W. OF JOONUR FROM THE SUMMIT OF A HILL N. oF THE TOWN OF GOREH. i 2 iS & ” Samanmnyamne Gh tae AL\ Hill Fort of Hurreectuimndurghur N T0 E. RANGE oF HILLS AS SEEN FROM LAKUNGAOWN IN THE VALLEY OF JOONUR. HILLS TO THE NE. AND E. AS SEEN FROM THE ARMOURY IV THE FORT OF AHMEDNUGGTUR. > § & Sulahut Pdihans Tomb NORTHERN FLANK OF THE PLATEAU ON WHICH ,THE CITY OF AHMEDNCUGGUR STANDS AS SEEN FROM WAMOOREE. 4 Dongurgunge ‘ Thre Z/ Sas Shetchad by LS Fidler INATION of tur COUNTRY ABOVE tk GHATS, BETWEEN 73. 35.4ND 74£49. EAST LONGITUDE, ANp THE PARALLELS OF 18°50. AND 1990.31. NORTHMATITUDE: SHEWING THE GEOLOGICAL STRUCTUR E, OFTHE’ SAME. sg 3 ‘ i ¢ ; ) i 3 = i: ; 3 i : : | ; 2 H a uns ¥ s s i : ee ty : fa ¥ i er me : A i Se oye i 3 : = ‘ d . . * : . isce | i3 i ot ane aa ] a) eg 2 i i { fred i Level whe Coreh River — SS = : = Level of the Sea CLINATION oF tu COUNTRY ABOVE tr GHATS, BETWEEN 73°35.4ND TH49 EAST LONGITUDE, ANDTHE PARALLELS OF 18°28. 4xD 18°50. NORTH LATITUDE: §HEWYN G 1 me: GEOLOGICAL STRUCTURE or me SAME. ss 8 3 S . ‘ RS i gE. ; i ; i = : ; ae itchy = 4 : i 4 i 3 hs ene 3 a ka = = . 4 ali Tt, 4 y , ‘ a lie : SRS fy af ary z ws < £ 5 es = a ¥ a3t i ison 3 3 ae ‘ é t a! add Hil i s $ s g # i a d ' a Wee ers Camper NO Fort W. Level ofthe Inderane« ud Powna Ri Level of the Sea- The strata of the darker hue are Basalt of various kindle; those colored grey-green are vurietice of Anwodaloid, quarts, zeolite, red evllulan &eke The lanes following the rusnbers subjoined. to the names of Places,denote the mode in hich the heighte huore. be obtained, signifies Barometric mearurenvent. Wauleulation trom the temperature of boiling Weter: teal. Trans 2° Series VOLT: Plate NATE, Caudal Endenih 0 . ENVIRONS oF BONN “Do Meckenheim ; » | * \vaale of English Mites INDEX (Not a Section) OF THE MINERAL | STRUCTURE as seen fiom the top of the Coblent: gate Bonn. 5 the Siebengebirge ——— ee as. a. & | ee syRé ab p Pee iii ig] 46) 4 - a i hee ianh os Soe eae ae fy : i S S45 ES aR es S | © 3 : ae e€ aycanee § 4 7s a a8 4 adel 4 4 Vertebra: belonginy te the Shark Family t S © e a _. » as de _ probably the Genus Lamna. cre : as he oe -tivm the Loess near Basle. wade > CD otanis sue CBM ceate a ) a i . i a , wa ey ose eee 3 ba : Sy, — a - oe . ¢ P S 8 v eS 7 ? ™ “ae, me rt ‘ . > —— oe Ce lee NE wing he —_ 3 a ain! V> © LAP oe a —— ay lah beth ee ee ee x - er : a ae b ~~ J sata eine : ht = genge i =" a a * . 4 j > <= - —— . a —— a a “ -. & ? a pe * : i - FR, So, cep } C : * — Z : . 5 i ; ; a : ; ; - Qs ' 3 f poe : A aah ag Mae : ely * Fale itigs pes, din youn Megpslteeth. i POL oon — as) ange ate AS RSD, > ne A Say ta ies = oe AN Ay, il 04 | 10004 55 | | ii | EN | Cl | | OFS 3 1853 AD fete Sh ae aR TS iil) | | “ itt oe tees af : ee & ~- sy ; gs ~ =f chieat Src ae a } : + = z > s :