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Books of special value and gift books, when the giver wishes it, are not allowed to circulate. Readers are asked to re- port all cases of books marked or mutilated. a books by marks and writing. Cornell University Library QE 262.S563W89 19lf The geology of the country near Sidmouth 3 1924 004 541 235 Cornell University Library The original of tiiis book is in tine Cornell University Library. There are no known copyright restrictions in the United States on the use of the text. http://www.archive.org/details/cu31924004541235 lEIOIES OF THE eEOLO&ICAL SUEYEY. ENGLAND AND WALES. EXPLANATION OP SHEETS 326 & 340. THE GEOLOGY OF THE COUNTRY NEAR SIDIOIJTH AID LYIB EE&IS. BY H. B. WOODWARD, F.R.S., and W. A. E. USSHER, F.G.S. With Contribations by A. J. Jukbs-Bkownb, B.A., F.R.S. SECOND EDITION. (PUBLISHED BY ORDER OF THE LORDS COMMISSIONBRS OF HIS MAJESTY'S TREASOHY. LONDON: FEINTED FOR HIS MAJESTY'S STATIONERY OFFICE, Rr DARLING & SON, Ltd., 34-40, Bacon Stbbet, E. And to be purchased from E. STANFORD, 12, 13, and 14, LoNd Acre, London ; W. & A. K. JOHNSTON, Ltd., 2, St. Andrew Square, Edinburgh ; _ fiODGES.F3GGI8 & Cq.jGrapton Stre et. D ublin ; w From any Agent (or the sale of Ordnance Survey Maps, or through any Bookseller or from the Director-General, Ordnance Survey Office, Southampton. 1911. Price One Shilling and Sixpence. GEOLOGICAL SURVEY OF ENGLAND AND WALES, AND MUSEUM OF PRACTICAL GEOLOGY. (Office : 28, Jbrmtn Stbeet, London, S.W.) LIST OF PUBLICATIONS. The publications include Maps, Memoira, Museum Catalogues, Catalogue of Photographs, Guides, &c. A complete list can be obtained from the Ordnance Survey Offlce, Southampton, price 8d, The Maps and Memoirs can be obtained from the Ordnance Surrey, or frohi Agents. Museum Catalogues, Guides^ &c„ are sold at the Museum, INDEX MAP OF THE EBITISH ISLES. On the scale of l-25th inch to the mile (1 to 1584000). Price— Coloured, 2«., Uncoloured, Is. Sheet. QUARIEB-INCH MAP OF ENGLAND AND Solid. Drift 1 with 2. (ALNWICK, BEEWICK, &0.) ."!. f CARLISLE and I. OF MAN) .. 4. (NEWCASTLE, STOCKTON, *c.) 5 with 6. (LANCASTER and ISLE OF MAN) 7. (MANCHESTER, LEEDS, &c.) .. 8. (FLAMBORO' HEAD and GRIMSBY) 9 with 10. (HOLYHEAD, SHEEWS- BURY,&c.) H. (STAFFORD, DERBY, LINCOLN, &0.) .. 12. , (LOUTH and YARMOUTH) .. s. d, s, d. 2 6 — 2 6 — 2 6 - 6 — 2 2 2 6 - 2 6 2 6 WALES (i-inch to the mile, or 1 to 253440). Sheet. Solid. Drift. (FISHGUARD, s. d. 8, d. 13 with part of 17. MILFORD) 14. (ABERYSTWYTH. HEREFORD) 2 15. (BIRMINGHAM, OXFORD) .. 2 16. (CAMBRIDGE, IPSWICH) .. 2 18. (BRISTOL, CARDIFF, &o.) .. 2 19. (BATH, GUILDFORD, SOUTH- AMPTON) 2 20 with 24. (LONDON, DOVER, and BRIGHTON) 21 with 25. (FALMOUTH with ISLES OF SCILLY) 2 6- 22. (PLYMOUTH and LYME REGIS) 2 6 - 23. (BOURNEMOUTH to SELSEY BILL) 2 0- 6 - 6 - 6 — 6 2 d 6 — 2 6 2 6 ONE-INCH MAP, NEW SERIES (1 inch to the mile, or 1 to 63360) WITH ACOOMPANriNG MEMOIES. These are published in either a " Solid " or a " Drift " Edition, or in both. The majority of them are fv^iSP^"'^^ ''7 Explanatory Memoirs. New Series Sheets 1 to 73 correspond to the Quarter Sheets of the Old henes Map 91 to 110. Some of (these are now coloui^printed, and are given in the table below ■ the rest are still issued as sheets of the Old Series Map. ' Price of Map. Solid. Drift. Memoir. 33. STOCKTON 34. GUISBROUGH .. 35 and 44. SCALBY and WHITBY 43. EGTON 10 . d. 5 3 5 3 53. PICKERING 54. SCARBOROUGH 55. FLAMBOROUGH 62. HARROGATE .. 63. YORK 64. DRIFFIELD 65. BRIDLINGTON .. 71. SELBY 72. BEVERLEY 73.' HORNSEA 110. MACCLESFIELD, CON- GLETON 123. STOKE-UPON-TRENT 125, DERBY and WIRKS- WORTH 126. NEWARK and NOT- TINGHAM 141. LOUGHBOROUGH and BURTON 142. MELTON MOWBRAY 155. ATHERSTONE and CHARNWOOD.. 166. LEICESTER 187. HUNTINGDON .. 203. BEDFORD 229. CARMARTHEN .. 230. AMMANFORD .. 331. MERTHYR TYDFIL .. 332. ABERGAVENNY 246. WEST GOWER .. 247. SWANSEA 248. PONTYPRIDD .. 249. NEWPORT (MON.) 254. HENLEY-ON-THAMES 261-2. BRIDGEND .. 263. CARDIFF .. 267. HUNGERFORD and NEWBURY .. .. . 268. READING .. .. .. R 282. DEVIZES .. .. 283. ANDOVER 284. BASINGSTOKE .. 295. TAUNTON and BRIDG- WATER .... 298. SALISBURY 209. WINCHESTER .. ' . 300. ALEESFORD .. 9 6 9 1 6 6 16 6 — 2 6 1 6 — 16 3 — 16 2 3- 11 2 2 3 6 2 6 3 — 2 Price of Map. Solid. Drift. Memoir. s. d. s. d, s. A. 1 1 1 1 1 12 1 1 I — 1 — 1 — 1 — 1 9 311. WELLINGTON and CHARD .. .. — 16 314. RING WOOD .. .. - 16 315. SOUTHAMPTON .. - 16 316. HAVANT .. .. — 16 317. CHICHESTER .. .. — 325. EXETER ' — 326 and 340. SIDMOUTH and LYME REGIS.. — 328. DORCHESTER .. — 329. BOURNEMOUTH ..5 3 330. NEW FOREST (pts.), L OF WIGHT (pts.).. 7 6 16 — 331. PORTSMOUTH and L OF WIGHT (pt.).. 5 3 16 - 332. BOGNOR .. ..2 16 6 333. WORTHING and ROTTINGDEAN .. 334. NBWHAVEN and EASTBOURNE 335. TREVOSE HEAD .. 336. CAMELFORD.. 339. NEWTON ABBOT 341. WEST FLEET.. 342. PORTLAND WEYMOUTH 343. SWANAGE 346. NEWQUAY .. 347. BODMIN and ST. AUSTELL 348. PLYMOUTH and LIS- KBARD 349. PLYMOUTH and IVY- BRIDGE .. .. — 14 3 350. TORQUAY .. .. - n 3 351 and 358. LAND'S END DISTRICT .. .. - 2 6 2 3.52. FALMOUTH and TRURO .- 1 353. MEVAGISSEY .. - 1 355. KINGSBRIDGE .. — 5 366. START POINT .. - 3 357 and 360. ISLES OF SCILLY .... - I LONDON (4 Sheets), each — 1 ISLE OF MAN (Sheets 36, T^^t,*^AS8and57) .. .. U 17 9 12 ISLE OF WIGHT (Special Sheet) _ 2 6 8 6 NOTTINGHAM (Special Sheet) _ 16 2 OXFORD (Special Sheet) - 16 2 8 .. - 16) and f .. - 1 6f 1 3 1 1 6 1 2 1 4 6 2 3 10 6 3 4 - 16 — 16 - 16 16 2 6 6 l\ IS 6 1 6 ffn-m"! MiMi-auwiiiipi^ ts ^ o »i no H CD ^ ^ 'm s o 'y 5"o c ?^ PREFACE TO FIRST EDITION. The area referred to in the following pages is of great interest not only on account of its geological history, but also from the fact that it is intimately associated with such notable geologists as Buckland, De la Beche and Conybeare. The original survey on the one-inch scale was made by De la Beche on the old series one-inch maps (21 & 22), but there is some doubt as to the year of publication, for, unfortunately, no dates were affixed to any of the older Geological Survey maps of the south-west of England. Mr. Greenough, in his Presidential Address to the Geological Society in 1834, states that " Mr. De la Beche, one of our Vice- Presidents, acting under the direction of the Board of Ordnance, has produced a geological map of the County of Devon, which, for extent and minuteness of information and beauty of execu- tion, has a very high claim to regard;" from which we may infer, with reasonable probability, that the original map was published in 1833. Some revisions were made at a later date by Mr. H. W. Bristow along the eastern margins of the two sheets ■ (old series) above referred to, and still later, during the years 1873-76, the area was re-surveyed on the old maps, when the subdivisions of the New Red rocks, the Rhsetic beds and the superficial deposits, were surveyed for the first time, and the boundaries of the Cretaceous rocks were revised. The western portion as far as Branscombe, Southleigh, Shute, Dalwood and Stookland was mapped by Mr. Ussher, and the eastern portion mainly by Mr. Woodward, with the help of Mr. Reid, who surveyed the bordering tracts from Lyme Regis to Uplyme and Hawkchurch. In 1884 Mr. Woodward made a special study of the Lias in the neighbourhood of Lyme Regis at the time that he was writing his portion of the Memoir on the Jurassic Rocks of Britain ; and during the years 1894-97 Mr. Jukes-Browne studied the Cretaceous areas with reference to the corresponding Memoir on the Cretaceous Rocks. At the same time the last-mentioned officer made a few additions and some revisions, using the six- inch maps, which were then available. Further additions were made by Mr. Woodward in 1901 when he examined the cuttings on the railway between Axminster and Lyme Regis. Notwith- standing the fact that six-inch maps have been used to some extent during later revisions, it is necessary to remember that the one- inch map as now issued is not based on a recent six-inch survey, but mainly on the re-survey during the years 1873-76. The geological boundaries have been almost wholly transferred from the old to the new one-inch map in the office, and slight errors due to discrepancies between the two editions of the topographical map, must, therefore, inevitably have crept in. But these errors cannot be very serious, and in view of the facts that the new map contains much more information than the old one, and that no (18821—17.) Wt. 35447—9. 750. 7/11. D & S. IT PREFACE. complete re-survey on the six-inch scale of this district can be undertaken for many years, it has been decided to publish this map in its present form. The Memoir has been jointly prepared by Mr. Woodward and Mr. Ussher; the latter being mainly responsible for the chapter on the Kew Red rocks and the former for the parts dealing with the Ehsetic beds and the Lias. The chapters on the Cretaceous rocks have been largely prepared from Mr. Jukes-Browne's obser- vations as recorded in his Memoir on the Cretaceous Rocks of Britain, with aid also from the brilliant zonal work in the Middle and Upper Chalk published by Dr. A. W. Rowe. J. J. H. TEALL, Director. Geological Survey Office, 28, JerTnyn Street, London. 21st March, 1906. PREFACE TO SECOND EDITION. For the preparation of the second edition of this memoir we are indebted to Mr. H. B. Woodward, who has been kind enough to undertake entire responsibility for the work and to carry it outsince his retirement from the Geological Survey. Though no revision of the map has been made, some additional information has been incorporated in the memoir, partly as a result of further visits to Lyme Regis by Mr. Woodward. Some notes and sug- gestions also have been made by Messrs. Ussher and Jukes-Browne in the chapters on the New Red Sandstone Series and Cretaceous Rocks respectively. In the preface to the 1st Edition 1833 was mentioned as the probable date of publication of the Old Series one-inch Sheets 21 and 22, the original Geological Survey Maps of the area. From information since gathered by Mr. Woodward and published m the Summary of Progress for 1907 (p. 159) it is now evident that those maps were not published till 1834. J. J. H. TEALL, Director. Geological Survey Office, 28, Jermyn Street, London. 31st March, 1911. CONTENTS. FAOB. Preface to the 1st Edition, by the Director ... ... iii Pbepacb to the 2nd Edition, by the Director Chapter I. — Introduction Chapter II. — New Red Sandstone Series. Permian and Trias Lower Marls; Pebble Beds; Upper Sandstone; Upper (Keuper) Marls Chapter III. — Trias (continued). Rhffitic Beds; Boring at Lyme Regis 16 Chapter IV. — Lias. Lower Lias; Middle Lias 21 Chapter V. — Cretaceous. Gault and Upper Greensand (Sel- bornian) 42 Chapter VI. — Cretaceous (continued). Chalk 53 Chapter VII. — ^Faults 63 Chapter VIII. — Plateau Deposits. Clay with Flints and Chert (in part Eocene) ... ... ... ... ... ... ... ... 67 Chapter IX. — ^Valley Deposits. Otter Valley; Sid Valley; Axe VaUey; Lym and Char Valleys 72 Chapter X. — Landslips and Coast Erosion 78 Chapter XI. — Economic Geology. Building Stones; Lime and Cement; Marl; Brick Clay; Road Metal; Scythe Stones; Sands; Gun Flints; Gypsum; Pyrites; Soils; Water Supply ... 82 Appendix. — Bibliography. List of principal works on the Geology of the District 92 Index 96 VI LIST OF ILLUSTRATIONS. PAGE. Fig. 1. Geological Map of the Country north of Ottery St. Mary 9 2. Avicula (Pteria) contorta Portl 17 3. Section of the Lias Cliffs from Pinhay Bay, near Lyme Regis, to Golden Cap 22 4. Psilonoticeras planorbis (J. de C. Sow.) 24 5. Lima gigantea J. Sow ••• 25 6. Gryphsea arcuata Lam. ... ... ... .■■ ••• ••• 25 7. Isocrinus (Pentacrinus) basaltiformis (Miller) 25 8. Schlotheimia angulata (Schloth.) 26 9. Scapheus ancylochelis H. Woodw 26 10. Coroniceras bucklandi (J. Sow.) 26 11. Arnioceras semicostatum (Y. (b B.) 26 12. Asteroceras brookei (J. Sow.) 28 13. Asteroceras obtusum (/. Sow.) 28 14. Microderoceras birchii (J. Sow.) ... ... ... ... 28 15. Extraorinus briareus (Miller) 28 16. Oxynotoceras oxynotum (Quenst.) 29 17. Eohioceras raricostatum (Ziet.) 29 18. Deroceras armatum (J. Sow.) ... ... ... ... ... 29 19. Belemnites clavatus Blainv. ... 31 20. Liparoceras striatum (Sein.) 32 21. Liparoceras henleyi (J. Sow.) ... ... ... ... ... 32 22. Deroceras davoei (J. Sow.) ... ... ... ... ... 32 23. Acrodus anningise Ag. ... 33 24. Dapeditis politus De la Heche 34 25. Pholidophorus delabechei Ag 34 26. Section at Weycroft, near Axminster ... ... ... ... 39 27. Section of Whitecliff, west of Seaton ... ... ... ... 43 28. Sections of the Cliffs from High Peak, near Sidmouth, to Beer Head ... ... ... ... ... ... ... 60 29. View of the Cliff on the north side of Beer Harbour ... 58 30. Map of the country near Honiton and Wilmington ... 60 31. Sketch of Quarry north-east of Wilmington 60 32. Section from Honiton to Raymonds Hill, north of Uplyme 64 33. Section from near Broadhembury to Stockland 64 34. Section through Membury 65 35. Section from Westgate Hill to Gittisham Hill 65 36. Section in Railway-cutting east of Combpyne Station ... 68 37. Section of " Pipe " in Greensand on Salcombe Hill ... 71 38. Section south-west of Shook Farm, south of Axminster... 76 39. Section across the Bindon and Dowlands Landslip 79 PLATE. — The Landslip at Bindon and Dowlands, between Lyme Regis and Axmouth Frontispiece. THE GEOLOGY OF THE COUNTRY NEAR SIDMOUTH AND LYME KEGIS. CHAPTER I. INTRODUCTION. The area to be described in this Memoir is included in Sheets 326 and 340 of the Geological Survey Map. Devon claims by far the greater portion, with the market towns of Axminster, Honiton and Ottery St. Mary, and the watering-places of Sid- mouth and Seaton. To Dorset belongs the eastern border, with the seaport of Lyme Regis; while a small portion of Somerset, with the hamlet of Chilson, lies along the right bank of the Axe on the north-eastern margin. The total land-area represented on the map amounts to about 184 square miles, and the coast line extends for about 20 miles, from Otterton Point to Black Yen near Lyme Regis. The area consists of a table-land deeply furrowed by the rivers Axe and Otter and their tributaries. The uplands may be considered as the southern termination of the Blackdown Hills, which rise to heights of from 850 to a little over 1,000 feet between Wellington and Chard on the borders of Devon and Somerset ; and in our present district attain elevations of 885 feet at Hembury Fort, 873 feet at St. Cyres Hill, 812 feet on Gittisham Hill, and 725 feet on Raymond's Hill, descending to from 400 to a little over 500 feet along the sea-borders. The uplift of the higher Blackdown Hills may be said to have directed the courses of the streams, and both the Otter and the Yarty, an important tributary of the Axe, have their sources far away on the southern slopes of the most elevated tract of Black- down, known as Staple Hill, in the vicinity of which there occurs a patch of gravel, probably of Eocene age.^ The general trend of the two main streams in the area is from north-east to south-west with a subsequent bend towards the south, as if to follow the strike of the underlying rocks after leaving the Cretaceous and Tertiary plateau. The Sid which drains the deep valley above Sidmouth flows also to the south-south-west; while the little river Lym, was once probably a tributary of the river Char, which flows from the north-east through the vale of Marsh- wood to the sea at Charmouth, just to the east of our district. ' See TJssher, Quart. Journ. Geol. Soc, xxxiv., 1878, p. 449 ; and " the Country between Wellington and Chard " (^Mem. Geol. Surv.), 1906, p. 48. 2 INTRODUCTION. Along the coast the Sid and the Axe have a perpetual conflict with the sea, the easterly trend of the shingle having a tendency to dam the outlets of the rivers, or to divert them eastward, so that their exits are choked and the river-waters filter through the beach except in times of inland flood. The scenery of the district owes its varied charm to the very irregular manner in which the table-land has been cut back by fluviatile agencies, causing the high land to project in prominent spurs and bluffs that separate numerous small valleys or goyles and dominate the main valleys (see p. 88). The land below the 100-foot contour is of small extent and confined to the river-flats of the main streams and their borders. The barren summits and steep upper slopes of the table-land strongly contrast with the fertility of the lower slopes and broader valleys. The more prominent elevations were utilised in old times for camp or beacon, numerous indications of which are met with in earth-works or place-names in the district. The towns and villages are situated on the porous strata of valley gravel or sandstone, whence a supply of water could readily be obtained by shallow wells ; or they nestle among the combes at a higher level where copious natural springs issue here and there from the hill-sides. The inland population is in the main agricultural, but the famous industry of lace-making occupies many cottagers in Honiton and surrounding villages. Other industries ol lime- burning and quarrying are mentioned in the Chapter on Economic Geology. There are few districts in which natural features are more obviously connected with Geological Structure. The formations represented on the Map are as follows : — Recent and / Alluvium. Pleistocene. \ Valley Gravel. Clay with Flints and Chert, &c. (in part Eocene'). '' Upper Chalk. Middle Chalk. Lower Chalk. Upper Cketaceods. Jurassic ( fiddle Lias. I. Lower Lias. Upper Greensand. 1 r, ,, Gault. jSelborman. Trias and Permian. Rhsetio Beds. Upper (Keuper) Marls. Upper Sandstone. Pebble Beds. Lower Marls. The general arrangement of the strata is shown in the section engraved on the Geological Map. The Lower Marls which appear in faulted tracts to the west of Ottery St. Mary are not exposed in the coast cliffs within the area. Between Budleigh Salterton and Exmouth they are well exhibited and overlie Lower Red Sandstones and Breccias, which westward, lie on an irregular surface of the Palaeozoic Eocks. INTRODUCTION. o At the base of the New Red Rocks there is thus evidence of a great break or unconformity, and as the older rocks were folded and eroded prior to the deposition of the newer, it is impossible to predict the nature of the Palseozoic floor beneath the area. If Coal Measures were reached, they might be of the unprofitable type met with in the Culm Measures of North Devon. The only deep boring in the area was that made a few years ago at Lyme Regis (see p. 20), and this, though carried to a depth of 1,302 feet, was not deep enough to reach even the base of the Keuper Marls. It is doubtful whether Palaeozoic Rocks would be encountered, at this locality, within a further depth of 1,000 feet. Along the western margin of the area the case would be different, as there a boring could be commenced in the Lower Marls and perhaps reach the older rocks within 1,000 feet; but so far as the prospects of workable coal are concerned there is no justification for such an enterprise. The table-land is capped by an accumulation of fiint and chert stones embedded in clay or loam, and co-extensive with the flat summits of the hills. This rests on Cretaceous Rocks, com- prising Upper Greensand, chert, sand and sandstone, underlain in places by Gault clay and locally overlain by Chalk. The chert- beds and the underlying sands form the steeper upper slopes of the table-land. They rest on Keuper Marls from Sidmouth to Seaton and Axminster ; on Rhsetic beds between Culverhole Point and Axminster ; on Lower Lias clays and limestones from the coast west of Lyme Regis to Axminster ; and on the Middle Lias near Hawkchurch and Forde Abbey Farm on 'the north-eastern margin of the area. These facts supply abundant proofs of two peneplains or great plains of denudation. The upper plain is due to the erosion, per- haps mainly subaerial, of the Cretaceous Rocks during the Ter- tiary period ; the lower plain to the denudation of the Jurassic and New Red Rocks by the Cretaceous Sea. The lower plain is marked by the junction of the Cretaceous strata with the under- lying older Secondary rocks, the eroded outcrops of which they successively overlap or overstep from east to west. We may measure the extent to which these underlying rocks were denuded by estimating the thickness of strata from the Middle Lias on which the Cretaceous formations rest in the north-east corner of the area^ to the lowest strata (about 150 feet above the base of the Keuper Marls) on which they rest on the western margin of the table-land. This thickness — judging from actual measure- ments of the Lower Lias, Rhsetic Beds and Keuper Marls would give a total of about 2,000 feet. This is one of the striking facts exemplified in the structure of the district; but whether we look to the succession and arrange- ment of the strata, to the organic remains so abundantly preserved in some of them, or to the effects of faults, folds, and other dis- turbances so clearly depicted along the coast and inland, the district is one which forms an admirable training ground for the geologist. No wonder, then, that it has attracted and inspired many a worker. Fossils were collected during the latter part of the 18th century at Lyme Regis and Charmouth, and were sold 4 INTEODUCTION. as " curiosities " to visitors and to passengers on coaches.* Their scientific importance, however, soon became apparent. Buck- land, who was born at Axminster, gained an interest in geology- early in life by collecting fossils from the Lias quarries near his home. De la Beche as a youth resided at Charmouth and after- wards at Lyme Eegis during the years 1817-21. Influenced no doubt by Buckland, whom he first met at the Assembly Eooms at Lyme Eegis, he devoted himself with great assiduitj to a study of the coast-sections between Sidmouth, Lyme Eegis and Bridport. In a paper read before the Geological Society in 1819 he gave an excellent pictorial section of the cliffs, working out for the first time the sequence of the strata, and the organic remains which characterize the successive groups. He then described the fossil fish Dapedius politus, of which we reproduce a figure, and which happily still retains its original name. In those early days he laboured m association with "VV. D. Conybeare, afterwards Vicar of Axminster (1836-45), and together they published obser- vations on the osteology of the Ichthyosaurus. Conybeare further enriched our knowledge by his description of the Plesiosaurus, which, like that of the Ichthyosaurus, was first brought into notice from Lyme Eegis by the discoveries of that famous fossil-collector, Mary Anning. Buckland, in an early paper " On the Excava- tion of Valleys," noticed how the hills and valleys of this district are abruptly terminated by the sea. He recognized that the sea had no share in shaping them; and, believing that the present streams were inadequate, inferred that diluvial (or, as we should now say, torrential) waters had performed the task of valley-erosion. He then published the first geological sketch-map of the district. Later, Buckland, in conjunction with Conybeare, published a graphic account of the great landslip of Bindon and Dowlands, while De la Beche prepared his one-inch geological map of this and adjoining districts to the north and west, which formed the basis for the establishment of the Geological Survey. Through the labours of these great masters the district " became classic ground for the geological student," and it has attracted and ever will attract a number of workers. Eeferences to later observers are recorded in the text and bibliography. ' W. Gr. Maton, " Observations relative chiefly to the Natural History .... of the Western Counties of England," 1797, vol. i, pp. 75, 76 ; and G. Roberts, •' History and Antiquities of the Borough of Lyme Regis and Charmouth," 1834, p. 286. CHAPTEE II. NEW EED SANDSTONE SEEIES. PEEMIAN AND TEIAS. The rocks grouped as Permian and Trias form the foundation of the entire area, and appear at the surface over a considerable portion of it. In general they are considered to represent con- tinental and desert conditions, with river-deposits, much wind- drifted material and extensive accumulations in inland saline waters. The sequence of these New Eed rocks is admirably displayed in the cliffs from Teignmouth and Dawlish to Exmouth, Budleigh Salterton and Sidmouth, but the lowermost divisions of sand- stone, breccia and conglomerate, if present, nowhere come to the surface in the tract under description. The beds represented are as follows : — ' Ehsetic Beds. New Red Upper Marls Keuper Marls. Sandstone^ Upper Sandstone | Kenper Basement-Beds, j- Trias. <5o ioa ^ Bunter Sandstone. Denes. Pebble Beds Bunter Pebble Beds. J . Lower Marls Permian. This " Eed Sandstone Series," as it was termed by De la Beche, has been repeatedly described, and from the fact that it nowhere exhibits evidence of any marked break, there has been consider- able diversity of opinion on the question of the correlation of the subdivisions with Permian and Trias elsewhere. That the oldest division (Lower Sandstone and Breccia, which occurs beneath the Lower Marls) is equivalent to strata now grouped as Permian, was surmised in 1816 by Conybeare and Buckland, who were struck with the identity of character of the rothe-todte-liegende of the Thuringerwald with the rocks of Heavitree near Exeter*; and in this view Murchison at a subse- quent date entirely agreed.'' On the previous edition of the geological survey map only two divisions were introduced : the New Eed Marl and the New Eed Sandstone, and no definite boundary was drawn between them. The subdivisions adopted during the course of the re-survey, were first described in detail in 1875, and the entire series was then referred to the Trias. ^ In 1888 the Eev. Dr. A. Irving re-opened the question of corre- lation, and strongly urged that the Lower Marls and underlying red rocks should be grouped as Permian; the Budleigh Salterton pebble-bed and the mass of the Upper Sandstone as Bunter.* To him we are specially indebted for the correlation indicated in the preceding Table. Four years later Prof. Hull concurred generally with the views of Dr. Irving, but preferred to group the Lower • " Outlines of the Geology of England and Wales," 1822, p. 313 (footnote). 'See "Siluria," Ed. 5, 1872, p. 333; and A. Geikie, Address, Quart. Journ. Geol. Soc, xlviii., 1892, p. 160 (Proc). ' Ussher, Geul. Mag., 1875, p. 163 ; Quart. Journ. Geol. Soc, xxxii., 1876, p. 377 ; xxxiv., 1878, p. 459. * Qicart. Journ. Geol. Soc, xliv., 1888, p. 149. 6 NEW BED SANDSTONE SERIES. Marls with the Bunter, and to include with the Lower Keuper the calcareous breccias at the mouth of the Sid that had been placed by Dr. Irving with the Bunter.* Subsequently Dr. living accepted the grouping of these breccias with the Keuper base- ment-beds and at the same time Prof. Hull agreed with Dr. irvmg in regarding the Pebble-bed as the true base of the Trias. With regard to the division between Permian and Bunter, the view that the lowest portion of the New Red Sandstone series is Permian, that the Budleigh Salterton pebble-bed and much of the Upper Sandstone should be grouped with the Bunter, and that the Otterton Point and Sidmouth breccias mark the base of the Keuper, may be conceded. The divisions adopted on the map are those employed during the re-survey of the area, and the subject will therefore be treated in accordance with this grouping. In the explanation of the adjacent map, Sheet 325% the lower subdivisions of this series are described, their general relations being shown in a section drawn through Bradninch in a south- easterly direction to the border of the present map near Straight- gate Farm. In that section the Lower Sandstone and Breccia pass beneath a thick series of Marls, called the Lower Marls to dis- tinguish them from the Keuper or Upper Marls which forni so large a part of the surface in the area we have now to describe. These Lower Marls are the oldest rocks superficially present. In the section before mentioned, their broad outcrop rises eastward to form the lower slope of the escarpment made by the over- lying Pebble-beds. From that escarpment the Pebble-beds dip eastward, and at the point where the section is taken, their dip- slope carries them into our present area, west of Ottery St. Mary. To the north of this line of section the Pebble-beds have been denuded, and the escarpment-feature has been in part oblitera- ted. They are shown only on the eastern border of Sheet 325 at Larkbeare, south of Talaton, near Higher Tale, in a large outlier at Clyst William Farm, and in a small one near Woodbeer, further north. These outliers mark the original trend of the Pebble-bed escarpment from Rockbeare Hill, northward; and they are specially mentioned here to accentuate the fact that the absence of the Pebble-beds in Sheet 326 from Payhembury north- ward, is due to faulting and denudation. The Lower Marls are faulted against the Upper Sandstones, so called to distinguish them from the Sandstones underlying the Lower Marls. It may here be mentioned that the Pebble-beds, with their accompanying features, re-appear in the south-west corner of Sheet 311 (the map on the north) toward Keshill. Lower Marls. These comprise dark red green-spotted Marls, with subordi- nate association of sandstones on the coast; and their thickness may be estimated to be at least 500 feet, and possibly a good deal more. ' Quart. Journ. Oeol. Soc, xlviii., 1892, p. 60. ' Ibid., p. 68, and xlix., 1893, p. 79. ' " The Country around Exeter " {Mem. Geol. Surv.), 1902. PERMIAN. I In the small tract (see Pig. 1) which they occupy on the north- west border of the map, these Marls are largely concealed by river gravels. Where this is not the case, although seldom exposed in section, it is easy to distinguish them by their clay soil, from the Upper Sandstones with which they are in faulted contact,' and from the overlying Pebble-beds, where these are present. Pebble Beds. This division consists of 70 or 80 feet of strata, made up of pebbles and occasional subangular stones of quartzite, grit and quartz, in a dark red, or sometimes grey and buff, matrix of sand. Intercalated seams of sand devoid of pebbles are not uncommon. The actual limits of the division are in many places difficult to determine owing to imperfect evidence, and to the resem- blance of some of the superficial deposits of gravel to the Pebble- beds from which they have been locally derived. This is not the place in which to enter on a full account of the Pebble-beds. They occur more prominently in the area to the south-west (Sheet 339). It will be sufficient to mention that fossils were discovered in the quartzite pebbles in 1863 by W. Vicary and described by J. W. Salter;^ that among the species Lingula lesueuri occurs in the Gres Armoricain, and Orthis budleighensis in the Gres de May, of the Ordovician of . N.W. France; and that Devonian pebbles with Spirifer vemeuili and Homalonotus also occur. These fossils have likewise been found in the quartzites of the Bunter pebble-bed in the Midland counties.^ Attention may, however, be directed to a recent paper by Mr. H. H. Thomas* in which he describes the minute mineral composition of the sands at intervals along the outcrop, and finds a decrease in the percentage of heavy minerals from the coast northwards. This fact accords with the view of the drift of the pebbles long ago advocated from their size and distribution.' The Pebble-"beds are represented by the easterly continuation of portions in the adjacent area (see p. 6), and by patches on the Lower Marls at their faulted junction with the Upper Sandstones near Sidmouth Junction and Fairmile. At Fairmile Inn the Pebble-beds were exposed to a depth of about 30 feet. To the south-west of Ottery St. Mary and west of Bishops Court the most southerly tract of Pebble-beds is cut through in a stream- valley in which Lower Marls are exposed, both bein^ cut off by fault against Upper Sandstones on the east. The lower beds of the Upper Sandstones here pass into the area of Sheet 325, of which they form the south-eastern corner. The above details are given in order to connect the geology of Sheet 325 with that ' Near Sherwood Farm, west of Peniton, the indication of the faulted junction by a, white line has been accidentally omitted on the map. » Quart. Journ. Geol. Soc, xx., 1864, p. 283. ' Lapworth, Proc. Geol Assoc, xv., 1898, p. 382. * Quart. Journ. Geol. Soc, Iviii., 1902, p. 620. ' Ussher, Hid., xxxiv., 1878, p. 461, 8 NEW BED SANDSTONE SERIES. of the area under description in which we find the upward con- tinuation of the series. If these maps are joined it will be seen that the occurrences of Lower Marls and Pebble-beds along their borders are accompanied by an irregular line of disturbance ; the dislocations, shown by the abrupt termination of rocks litho- logically so distinct, amounting to as much as 200 feet or more. This line of disturbance enters Sheet 325 west of Bishops Court, and continues southward toward Budleigh Salterton. It has an important bearing on the geological structure of the entire area. The map (Fig. 1, p. 9) on which the superficial deposits are omitted, shows the faults and more especially the explanation adopted in regard to the strip of country north of Escot on the west of the Tale. The Pebble-heds of Blue Anchor Inn are assumed to dip eastward beneath the Upper Sand- stones, both being cut off on the west against Lower Marls, by a fault which, traced southward, throws the Sandstones against a patch of Pebble- beds (covered by gravel), north of the railway, near Lashbrook Farm, south-west of Talewater ; and again west of Escot. The Upper Sandstones on the south-east of Escot overlie Pebble-beds (a small patch), both being cut off by fault against Lower Marls, which are overlain by Pebble-bed patches, here, at Fairmile, and (under gravel) south-east of Colesworthy. These patches are in each case in faulted contact with Upper Sandstones. The fault on the south-east of Escot seems to turn northward before reaching Clapperentale Farm. At any rate, a fault (concealed by alluvium or by the gravel tracts on its eastern border) has necessarily to be assumed along the Tale Valley, in order to separate the sands (attributed to the Upper Sandstones) on the western slopes, from the Lower Marls on the east. This fault is assumed to cross the road north of Tuokmill Farm, and to join another, taken as the northern boundary of the Blue Anchor Pebble-beds. Further north this dislocation should unite with the Payhembury fault, and continue toward Crammer Barton. On this assumption the occurrence of Pebble-beds under the alluvium of the Tale at Talewater Mill is highly probable, as we were informed that from 30 to 40 feet of hard cemented (ferruginous) gravel had been encountered in sinking on the south of the houses near the mill-stream. IJppEH Sandstone. This division consists of rather fine-grained sands and soft sandstones, mostly red, but sometimes bright yellow, buff, grey, or white in colour. False-bedding is well exhibited in many sections; there are occasional seams and lenticular beds of red, greenish and mottled clay or marl, the results of local deposition, and also pellets of clay such as would result from contem- poraneous erosion. In the railway-cuttings south-east of Sidmouth Junction, by Harpford Wood and near Bulverton, lenticular masses and intercalated bands of clay were exposed in the sands and sandstones. Some of the beds of sandstone are calcareous, and calcareous nodules are of frequent occurrence. Concretionary iron-stone, or pan, is occasionally found in the lower beds. The sands are usually more or less micaceous. The total thickness of the group may exceed 400 feet. In the boring at Dotton Lane, Colaton Raleigh, nearly 300 feet of the strata were proved. (See p. 90.) Lateral changes in the characters of the beds are not unfrequent. Occasional pebbles occur (near Talaton), also small pieces of shale and fragments of murchis- onite* (near Escot). ' A variety of orthoclase, possibly derived from the Dartmoor Granite. TRIAS. Fig. 1. INDEX Upper Grtjervaarvat.,h la'Val PdlUBe^.f^ ESJ LoitrcrMarlse^ dH Geological Map of the Country north of Ottery St. Mary. By W. A. E. UssHET?. Scale — One iuch to a mile. jy NEW KEP SANDSTONE SERIES. In a lane-section near Northmostoyn several ^^ecciated beds were noticed, and compared with fl^^^ «^7^;f^ ,f i^^^^ltT- Point, a view subsequently confirmed by ^r- Jrvmg s identitca tinn of brecciated beds in several places between Utterton ana Pa^saford' Their occurrence further north was also detected m the neigbbourhood of Harpford and in the rarlway-cuttmg near Tipton St. John's. -r^ tj j. These breccias, which are now regarded as ^euper Basemen Beds (see p. 6), were not separated from the Upper Sandstones during the re-survey of the area. -^ , „ • It is with the two upper subdivisions of the New Eed Series name V the Upper Sandstones and Keuper (or Upper) Marls ?hS ie have chiefly to deal. Both these subdivisions are well exposed in the coast-section between Otterton Point and the Mouth of the Axe; but the lower part of the Upper Sandstones west of Otterton Point, is included m the area of sheet 66^, and may attain a thickness of 100 to 150 feet. In the examination o the coast-sections between Sidmouth and Otterton Point strict attention must be paid to the tides, as at high water many por- tions of the beach are impassable, and -the great arch at Ladram Bay can only be passed through on foot at low-water spring-tides, once a fortnight.^ In the north-western part of our area the outcrop of the Upper Sandstones is irregularly restricted by the faults already men- tioned (p. 8), but south of Ottery St. Mary this is not the case. The relations of the Upper Sandstones to the Keuper Marls are not only conformable, but in places so intimate as to suggest the local horizontal passage of sandy marls into sandstones, _ or vice versa. This occasions a difficulty in estimating the position of brecciated beds in the Sandstones with reference to their junction with the Marls above. Otterton Point consists of red sandstones exhibiting a con- glomeratic character near the base of the cliff. As described by Dr. Irving in 1888 "An irregular band of breccia occurs inter- calated with the sandstones, just above high-water mark. . . ^. Nearly all the fragments appear to be slightly subangular." Amongst them he noticed "slate slightly cleaved," also "vein- quartz, trap (various), reddish granite (the felspar slightly kaolinized), an older grit containing felspathic fragments, quartzite (dark grey, red and yellow). The few pebbles which formed the exceptions to the rule were composed of either trap,, quartz or quartzite." A second breccia occurs hereabouts, in which all the contained fragments are of hard red marl. The matrix of both these breccias is fairly hard, owing to calcareous cementation.' In his investigations of the petrography of the Upper Sand- stone and Marls, Mr. Thomas has found that all the mineral species, with the exception of staurolite, that occur in the finer ^ Quart. Journ. Geol. Soc, xlix., 1893, p. 80. 2 P. 0. Hutchinson, " Guide to Sidmouth," 1875, p. 53. ' Quart. Journ. Geol. Soc, xliv., 1888, p. 153. TRIAS. 11 New Eed deposits " could be supplied by tlie older rocks of the West of England." The staurolite-bearing rocks "probably lay to the south of the present coast-line."^ In September, 1868, Mr. Whitaker discovered the jaw of the lacertian reptile Hyperoda'pedon, " on the left bank of the Otter, just above its moutli, where the sandstone is somewhat breccii- form. The specimen was in a large block which had fallen from the low cliff that bounds the estuary."^ The late Dr. H. J. Carter, of Budleigh Salterton, also found many traces of osseous structure at this locality. This brecciated horizon was traced in 1874 at some feet above high-water mark from Otterton Point to 370 yards from the southern promontory at Ladram Bay. The upward extension of the brecciation is very irregular, and facilities for observation depend on the scour of beach-materials from the foot of the cliffs. In this distance of more than a mile and a half, the stony breccia was less frequently seen than the concretionary type, which forms irregular nodular calcareous beds in the sandstone, and contains sandy pellets cemented by fine white calcspar. Within a quarter of a mile from Otterton Point four small faults are visible, but they have an inappreciable effect on the brecciated beds. At about three-quarters of a mile from Otterton Point the section consists of red sandstones with corrugated calcareous bands weathered out in relief, and very irregular near the top of the cliff. In the lower part the brecciated beds occur ; they are much false-bedded, and exhibit signs of disturbance, as if turned up on the north at a crack, or small fault, which hades in a south-westerly direction from the top of the cliff, at an angle of 20°. At Brandy Head, a mile from Otterton Point, the cliff is about 160 feet in height; corrugated breccio-conglomerate was exposed at its base, and for fifteen feet upward from the beach lenticular impersistent bands of worn stones were noticed, along lines of current-bedding in the red sandstones; and, just above them, a lenticular patch of dark red clay. Near this, on the north, the sandstone cliff attains 200 feet in height, and is capped by from 8 to 12 feet of flint and chert gravel which extends northwards to about a quarter of a mile from Ladram Bay. From Otterton Point to Ladram Bay calcareous matter is most irregularly distributed in the sandstones, and the bedding is not sharply defined. The red sand-rock, or sandstone, is partly intersected by an irregular network of calcareous concretionary veins, partly intercalated with irregular calcareous beds, and it occasionally exhibits false-bedding. The calcareous matter is absent in places, and the rock consists of thick-bedded, homogeneous, and comparatively soft red sandstone. Lenticular bands and small patches of dark red clay are noticeable in the sandstones in the lower part of the cliff, a little north of the last exposure of the brecciated beds. Near the southern horn of Ladram Bay the cliff attains a height of about 160 feet, and exhibits similar characters; the ' Quart. Journ. Geol. Soc, Ixv., 1909, p. 241. ' Bid. xxv., 1869, p. 156. 1S82I B 12 NEW RED SANDSTONE SERIES. thick even-bedded sandstones giving place to an irregular net- work of calcareous concretions which obscure the bedding from top to base. The cliff is here capped by a thin layer of Keuper Marl under gravelly soil, the base of the large outlier which extends to Otterton. The southern boundary of this outlier trends westward, a phenomenon which may be due to horizontal bedding, or to a local change in strike. From Otterton Point to the disappearance of the brecciated horizon, near Ladram Bay, the sandstones are practically hori- zontal. Dips of from 1° to 5° are locally present, and where not due to current-bedding may be ascribed to slight undulations. The brecciated horizon is about 180 feet or so from the top of the sandstones, and its disappearance may be due to slight synclinal undulation, as, if we remember rightly, it reappears in the beach reefs in the south part of Ladram Bay. The basement-beds of the Keuper Marls are let down by a nearly vertical fault at a quarter of a mile north of the road to Ladram Bay. This fault has, we believe, a downthrow to the south of from 90 to 100 feet. Traced westward it forms the northern boundary of the Otterton Keuper Marl outlier. The Marls let down by it are 15 to 20 feet in thickness, and they are further shifted by two small but well- marked faults on either side of Hern Rock Point. At Conger Pool the Otterton Point brercias reappear on the north side of the main fault. From here to Lade Rock^ the brecciated beds are continuously present at the base of the cliffs. These beds were not detected in the coast exposures of the Upper Sandstones to the east of Lade Rock. The outcrop of the Upper Sandstones at the base of the cliff naturally depends upon the scour of the shingle beach. They were found to dip beneath sandy Marls at somewhat less than half a mile west of the Chit Rocks. The Sandstones crop out on the cliff, on the slope of High Peak hill (513 feet) at between 200 and 300 yards from the fault at Conger Pool. They are overlain by red sandy marls, mottled greenish, and containing buff, grey, and greenish bands of laminated sandstone, often with ripple-marked surfaces, and with occasional pseudomorphs after rock salt. Between High Peak and Peak Hills the cliff is known as Wind- gate or Windygate. It is much obscured by slips and debris, and furrowed by rain channels, but by a path to the summit the basement beds of the Keuper Marls may be examined at intervals in vertical section. In 1875 Dr. Johnston-Lavis^ discovered the remains of Laby- rinthodon Javisi Seeley, below the western slope of High Peak hill at Picket Rock Cove, in fallen blocks and debris from several beds in the cliff "situated about 10 feet from the top of the sandstone." In this talus Dr. Carter subsequently obtained bone structures of Labyrinthoclont affinities, and a fragment of jaw-bone, with teeth. In ■ As shown on the new series maps, a quarter of a mile nearer Sidmouth than on old one-mch map. Dr. Irving, Quart. Journ. Geol. Soc, xliv., 1888, p. 152, applies this name to the Ladram Arch promontory, about half-a-mile S.W. of Lade rock on the old map. ^■Quart. Jnurn. Geol. Soc, xxxii., 1870, p. 274, with olifE-seotion by Hutchinson. TRIAS. 13 1882 Mr. A. T. Metoalfe^ visited the spot and also found osseous structures. He locates the talus on the beach, in which these remains were found, as directly under " a stile on the brink of the cliff, whence a stratum in the sandstones, somewhat lighter in colour than the rest, may be seen dipping to the east. This stratum is very near the junction with the Upper Marls." Mr. Metcalfe was of opinion that the talus with osseous struc- tures had fallen from this lighter coloured bed, but adds that the late P. O. Hutchinson had assigned a lower horizon. The diagram mentioned by Mr. Metcalfe is no doubt a replica of a careful coloured section by Mr. Hutchinson, of the Sidmouth coast, dated Oct. 8, 1878, that has been recently presented to the British Association Trias Committee. In this section the Lahyrinthodont bed is placed at 100 feet above the talus on the beach, and about 50 feet below the base of the Keuper Marls. Two white bands are shown in the uppermost beds of the Sandstone, and above them, at the base of the Marls, a band containing plant-remains. In talus from this band, at Windygate, Hutchinson obtained a plant stem^ in May, 1878. Dr. Johnston-Lavis described the ossiferous zone as " nearly hard enough in some places for building purposes, containing here and there masses of marl varying in size from that of a pea to that of a hen's egg." " In these beds," he adds, " ripple marks are very plentiful." For 40 or 50 feet above the plant-bed at Windygate, Hutchinson's section shows lines of geodes in the marls, containing calcspar crystals, and in one of the lower bands crystals of celestine (sulphate of strontium) had formed on them. Above these he placed the band in which pseudomorphs after rock sEilt had been found. These latter, however, occur also higher up in thin bands which often display ripple marks. The Sandstones were seen to pass under the Marls of Windy- gate, but near Chit Rocks they assume a contrary dip, being thrown into a syncline by a composite fault which brings up the sandstones on the north side of the Rocks (see section on map). The section is now obscured by talus, but the westerly downthrow is about 60 or 70 feet (less than originally estimated), and as it does not appear to have appreciably affected the Cretaceous strata, it may be of pre-Cretaceous age. In 1875, tributary dis- locations, probably due to the subsidence of the marls, were clearly distinguishable. By these dislocations a mass of broken sandstones is cut off from the Sandstones of the Chit Rocks on the east, and from the Marls (in which a bed of sandstone was seen to dip west) on the west. In this faulted mass of sandstone fragments of bone were found by the Rev. S. H. Cook.' The Chit Rock sandstones are in very thick beds, with calcareous concretions sometimes in lines, and are false bedded. The Upper Sandstones are concealed by the gravels of the Sid, in Sidmouth, but their outcrop in the cliff on the east, at the mouth of the Sid, has been described in detail by Dr. Irving, and figured by Prof. Hull. The former mentions 50 feet of thick-bedded coarse sandstones, current- bedded and slightly brecciated, and toward their base current- bedded breccias (mostly of fragments of indurated marl in a marly matrix) intercalated with, but quite subordinate to, them. These rocks are exposed for 300 yards by the Sid escarpment, and on the coast they pass under massive beds of finer-textured sandstones, with feeble traces of current-bedding, and associated ' Quart. Journ. Geol. Soc, xl., 1884, p. 257. ^ Figured and described in Trans. Devon. Assoc, xi., 1879, p. 383. '■> Quart. Journ. Oeol. Soc, xxxii., 1876, p. 277, The spot is marked on Hutchinson's section. J8821 B 2 14 NEW RED SANDSTONE SERIES. with beds of marl increasing in importance upward. Above these Dr Irving records massive hard well-bedded marls, with sub- cuboidal structure, characterized through a range of 150 feet by the presence of numerous calcareous concretions and geodes, lined with crystals of calcite. „„..,, ^ n During the re-survey of the district in 1874-5 the outcrop of the Upper Sandstones on the beach was taken at about 80 yards east of the mouth of the Sid, and in the clifi at about 50 feet above the beach. The Manor House, on the north side of Sidmouth, stands on the upper beds of the Sandstones, which are here brought against the basement-beds of the Keuper Marls on the east by the Chit Rock fault. This reversal of downthrow, from the west side to the east, is partly due to the undulations by which the presence of the Upper Sandstones, seen in junction with the basement- beds of the Marls at Sidmouth Station and at Bulverton, is accounted for. If, as Dr. Irving suggests, and this is highly probable, the breccia by the Sid is on the same general horizon as the Otterton Point breccias, it seems likely that these beds may be below the Chit Rocks. At any rate the appearance of the Upper Sandstones in the Sid valley seems to be due primarily to an anticlinal undulation accompanied, or subsequently compli- cated, by faulting. Upper (Keuper) Marls. This most persistent division of the New Red series extends over a large area, but it is much concealed by Cretaceous strata, debris from which likewise obscures its outcrop on the slopes and lower lands. The lower part of the Keuper Marls, for perhaps 200 feet, from Sidmouth to Weston Mouth, consists of hard red marl passing insensibly into sandy marl, and effervesces but feebly with hydro- chloric acid. It also contains intercalations of hard sandy marls, which sometimes occur in nodular bands, and include geodes lined with calcspar. In this lower portion bands of shaly, red, green, and grey sandstone may be taken as the representatives of the Waterstones of the Midlands. As a whole the structure of the Marls is cuboidal, but this is seldom exhibited by the harder, marly beds, and is less perfectly developed in the basement-beds. Celestine, barytes, and gypsum locally occur, and pseudomorphs after rock-salt have been found at Salcombe Mouth. Mr. H. H. Thomas notes that both barytes and celestine occur in the New Red rocks as cementing materials — the former mineral was found in the Red Marls of the Lyme Regis boring, the latter was recorded from the Marls of Peak Hill and Salcombe by Mr. S. G. Perceval.' The gypsiferous Marls do not extend to the west of Salcombe Mouth, and thence upward, the character of the division may best be gathered from Mr. Jukes-Browne's detailed description of the beds encountered in the boring near Lyme Regis, where the thickness was proved to a depth of 1,130 feet, and may attain ' Quart. Jouni. Oeol Soc, Ixv., 1909, p. 234. TRIAS. 15 as much as 1,300 feet. {See p. 20.) The Keuper Marls are mottled with greenish and bluish-grey bands and patches, the latter tint, as pointed out by Pengelly, prevails in the upper part of the series. Toward Weston Mouth, hard greenish bands occur, and gypsum appears in the Marls, intersecting them in a network of selenite veins. Mr. Hutchinson fixed the lower limit of the gypseous marls at Hook Ebb reef. At about 200 yards east of Littlecombe Shoot gypsum has been worked. The filamentous veins are noticeable from here to Branscombe Mouth at intervals.^ A hard greenish band is conspicuous in the Marls between Weston Mouth and a ravine to the westward (half a mile west of Littlecombe Shoot). East of Branscombe Mouth the Creta- ceous rocks descend to the sea-level (see coast-section on map), and the Marls pass beneath them under the beach on the west of Beer Head, reappearing at White Cliff (Seaton Hole), where they are brought up by a great fault with a downthrow to the west of 200 or 300 feet. The low cliff at Seaton is capped by old river-gravel beneath which red rock-sand occurs for 15 feet, apparently merging into the Red Marl below. The Red and Variegated Marls, with traces of gypsum, are again seen beneath the Cretaceous rocks of Haven Cliff to the east of Seaton, where the easterly dip soon brings on the succeeding Grey Marls (passage-beds) and overlying strata of the Rhsetic formation. Between Haven Cliff and Culverhole Point frag- ments, and sometimes large masses, of Marl fall from the cliffs. See De la Beche, Trans. Geol. Soc, ser. 2, vol. ii., 1826, p. 30. 16 CHAPTEE III. TRIAS — {continued). Rh^tic Beds. Coast Sections. These strata are exposed at several places along the coast between Axmouth and Lyme Regis. The most complete and accessible section from the Red Marls to the White Lias is at Culverhole below the Bindon Cliffs, a little west of Culverhole Point ; but the full thickness of the White Lias is better seen at Charton Bay, and the junction with the Blue Lias at Pinhay Bay. In passing eastwards along the shore from Axmouth Harbour, we find the Chalk and Greensand resting on a foundation of the red and variegated Keuper Marls. The marls are bent into gentle undulations, and they are displaced by several faults which cut the cliffs obliquely and sometimes nearly parallel with the coast. Towards the top of the red marls there is a layer of hard pale-grey or buff banded marl with dark clayey streaks, and this marks the commencement of the sedimentary conditions which characterize the succeeding Rhtetic formation. The strata dip eastwards at an angle of about 5°, and within a short distance the main mass of the Rhtetic series is exposed, here and there displaced by slight faults, some of which, however, may be due to land-slipping. The following section at Culverhole was noted in 1884, but some additions to the list of fossils were made during the visit of the Geologists' Association in 1899,^ and four other species [noted in square brackets] have since been recorded by Mr. L. Richardson^ : — Ft. In. f (Top beds, about 10 feet, obscured.) Thin-bedded white limestones, here and there I wedge-bedded, and with concretions or pebbles White Lias \ of compact limestone in the lower part : Area, I Modiola minima ... ... ... ... about 15 I Impersistent masses of rudely arborescent Land- L scape Stone or Gotham Marble about 8 f Black shales, with ArAcula (Pteria) contorta, Anatina prmcursor, Cardium {Protocardium) I rhaiticum, Ilinnites, Modiola, Pecten valoniensin, [Pleai-ophoruH elongatus. Placunopsis alpiita, Black ' ''^!^i/ophoria emmriclii, Schizodus ewaldi], and Avicula- ' occasional thin lamins of micaceous sandstone conturta "^ ""'^^^ Pidlastra arenicola : at the base a bone- Shales ' ''"^'^ (black calcareous grit with small pebbles of quartz) yielding an occasional reptilian bone, I also numerous fish-remains, including Acrodus minimus, Gyrolepis alberti, Hyhodus cloacinus, I Lepidotus, Saurichthys acuminaius, Sargodon (, tomicus and coprolites about 18 n H Proc. Geol. Assoc, xvi., 1899, p. 135 ; x., 1887-8, p. 531. The species here mentioned were mostly identified by Mr. E. T. Newton. ' Proc. Geol. Assoc, xix., 1906, p. 406. pi § Grey Marls Keuper Marls. RHiETIC BEDS. 17 Ft. lu. 'Green marl : the surface cracks infilled with fish- remains 10 ^ Jj •j (Passage ■{ Alternations of pale greenish and cream-coloured 3 g I Beds). I marls, with hard bands of marly limestone and W L dark grey and black clays 20 Dark, light-grey, green and red cuboidal marls ... ) Hard layer of pale-grey or buff banded marl > 15 with dark clayey streaks j Green, grey and red marls. , Red and variegated marls. In the boring at Lyme Regis a greater thickness was assigned to the Black Shales, but the record was not precise. Mr. Richardson's measurement Frf "'' of the strata at Culverhole agrees practically with ' ~" ours, but he groups some shales with the " Upper Rhsetic," which we place with the Black Shales — — a matter of no importance. Mr. W. H. Wickes ''■4J'5k> has pointed out that the pebbles found in the Rhsetic Bone-beds may have been derived from \^ materials swallowed by fishes and saurians.^ With regard to the so-called "Tea-green marls," we omit to use the name, as it was originally Avicula (Pteria) applied by R. Etheridge to the alternations of contorta Portl. green and red (Keuper) marls, below the Grey Marls.2 In De la Beche's original description of the strata along this coast the Grey Marls, beneath the Black Shales, were grouped with the Lias, but they were later on assigned to the " Upper part of the Variegated Marls. "^ For many years afterwards " the Bone Bed " was regarded as the base of the Lias. In 1841, however. Sir Philip Egerton drew prominent attention to the Bone Bed at Axmouth, comparing it with the well-known and richly fossiliferous bed at Aust Cliff in Gloucestershire. He then remarked, " A thin stratum replete with remains of saurians and ichthyolites occupies a similar stratigraphioal position near Axmouth; and Prof. Agassiz, during his visit to England in the autumn of 1840, identified in a series of specimens obtained by Mary Anning, one Placoid, two Lepidoid, and one Sauroid fish, with well-known muschelkalk species." The following were the species: — Hybodus plicatilis [prob. S. cloacinus], Gyrolepis alberti, G. tenuistriatus [G. alberti] and Saurichthys apicalis.'' The Bone-bed, with the zone of Avicula contorta, was placed in the Keuper by Oppel,^ while the White Lias was grouped by him in the Lower Lias, zone of Ammonites planorbis. In 1861 the Rhtetio Beds were first clearly distinguished in this country through the researches of Charles Moore, the White Lias and Black Shales being included as Rhsetic, and the Grey Marls generally being grouped with the Keuper. In 1864 when the mapping of the Rhsetic Beds came first to be under- taken by the Geological Survey, H. W. Bristow and R. Etheridge visited many of the principal sections, and concluded that " The lower portion of the Rhaetic strata consists of alternations of hard and soft marls, passing gradually into the red and green marls of the Keuper formation, upon which they are based. "° The higher portion was taken to include the Black Shales and White Lias. The survey of the Rhsetic Beds in the area of the present map was carried out on this principle during the years 1873-74; whereas in the ■ Proc. Bristol Nat. Soc, ser. 2, x., 1904, p. 213. - Proc. Cotteswold Nat. Club, iii., 1864, p. 220. ' "Report on the Geology of Cornwall, Devon, and West Somerset," {Men. Geol. Surv.), 1839, p. 223 ; see also Conybeare and Phillips, " Outlines of the Geology of England and Wales," 1822, p. 262. ' Proc. Geol. Soc, iii., 1841, p. 409. 5 " Die Juraformation," 1856-58, Tab. 64. " Bristow, Geol. Mag., 1864, p. 238. 18 TKIAS. recent one-inch maps of South Wales, Monmouthshire, and Nottingham- shire the base of the Rhietic Beds has been taken below the Black »hales and on top of the Grey Marls, as being the most definite boundary that could be surveyed. There is much to be said locally for either view of the grouping. In an interesting paper on the Rhsetic Beds of Glamorganshire, Mr. L. Richardson has classed with this formation some portion of the Grey Marls (the " Sully Beds") that underlie the Black Shales^ ; but this grouping has been opposed by Dr. Strahan. Mr. Jukes-Browne in his record of the boring at Lyme Regis (see p. 20) groups 39 feet of Grey Marls with the Rh^tic Beds, an arrangement which coincides with the grouping on the geological map. We may agree with Edward Forbes, who after a visit to Lyme Regis in 1847 broached the notion to De la Beche, " that the red marls were formed in a great salt inland sea (a sort of Aralo-Caspian), during the last state of which the white lias was formed. "2 No doubt influxes of the open sea gradually brought in the Rhsetic fauna, while the Liassic fauna overspread the area during subsequent depression. The Rha;tic Beds thus mark the commencement of the physical changes which terminated the continental conditions of the Trias, and ushered in the marine conditions of the Jurassic, changes that evidently were not brought about uniformly over the British area. Some of the harder bands in the Grey Marl series appear to be detrital limestones. 3 Microscopically examined by Dr. Teall a sample of Grey Marl from the base of the series at Culverhole was found to be " Com- posed of excessively fine-grained granular calcareous matter." At Cliarton Bay we find the nest good section of the Rhsetic Beds, and the entire sequence can be seen, when not masked in places by the numerous slips of strata. The locality is accessible (by permission) through the grounds of Rousdon, or it may be reached by footpath through the Pinhay underclifEs, and across the broken ground of Humble Green. The beds are bent into a gentle anticline at the base of which traces of grey marls with reddish tinges may be detected. Above come the Grey Marls, as noted at Culverhole, a series comprising in descending order : grey marls, alternations of hard grey marls and black cuboidal shaly beds, hard pale marls of tufaceous appearance, with inter- banded greenish marls and laminated mudstones, altogether about 35 feet thick. The Black Shales were greatly obscured at the times of our visits, but masses of mammillated Landscape Stone 3 inches thick, were obtained near the base of the over- lying White Lias. Ledges of the White Lias may be traced on the foreshore a little further east, and then they disappear beneath a mass of Lower Lias. The full thickness of the White Lias at Charton Bay, has been estimated at 25 feet by Mr. Richardson, and he records from it Ostrea liassica, Modiola minima, PUcatula (Dimyodon) intusstriata, ;ind Protocarclium} At Pinhay or Pinney Bay the White Lias again appears, being upraised by a fault with a westerly downthrow. (See p. 24.) The full thickness of this division is not seen, and the beds soon descend eastwards beneath the blue limestones and shales of the Lower Lias. On the foreshore the Black Shales, with Avicula contorta, Cardiuni rhceticum, and Pecten valoniensis, ' Quart. Journ. Geol. Soc, Ixi., 1905, p. 386. See also A. Strahan, Jubilee vol. of Geol. Assoc, 1910, p. 846. - " Memoir of Edward Forbes," by G. Wilson and A. Geikie, 1861, p. 418. ' See H. B. Woodward, " Jurassic Rocks of Britain," (Mem. Geol. Surv.), vol. iii., 1893, pp. 29-32. J> ^ * Proc. Geol. Assoc, xix., 1906, p. 406. RHJiTIC BEDS. 19 were observed during an excursion of the Geologists' Association in 1906. The White Lias is remarkable for containing many " pebble-like concretions,"' which stand out in relief on its weathered faces. These lumps are composed of hard white or pale-grey limestone, very similar to the matrix. Sir Archibald Geikie, who, in 1885, paid a visit of inspection to the coast, suggested that during the accumulation of the strata the cal- careous mud may have been from time to time exposed to the sun's rays, so that films of the deposit curled up, and these, if subsequently rolled by the waters of the inland sea, would be shaped into the lumps which form so conspicuous a feature in the rocks.^ Inland Sections. In 1884 the White Lias was exposed to a depth of 23 feet in the quarries at TJplyme where an inlier of Rhsetic Beds is shown on the map. Here several bands of the Lower Lias are so pale in colour that they may readily be mistaken for the true White Lias which occurs below. On this account Dr. Wright was led in 1860 to group the White Lias in the zone of Ammonites planorhis; but in a later article he modified his views, and conceded that " the series included light-coloured limestones belonging to two distinct zones of life."' He first drew attention to the occurrence in this district of the Landscape Stone or Gotham Marble, the bed being 9 inches in thickness. At TJplyme, as at Pinhay Bay, the White Lias contains here and there throughout its mass nodules or pebbles of compact limestone, that stand out conspicuously on the weathered surfaces. The beds were exposed in 1904 at the Yawl limekilns. Tubiform borings occur in the White Lias here, as in so many other localities. They are conspicuous in the top hard layer, extending to a depth of 4 or 5 inches : the rock is a compact pinkish-brown limestone with irregular surface like the Sun bed of Somerset. Nodular white lias occurs below, and rests on alternating bands of white limestone and marl, which contain a good deal of selenite. (See p. 39.) From the White Lias were obtained Cardium rhcsticum, Modiola minima, Ostrea liassica, Pteromya, Pecten pollux and P. valo- niensis. In other inland parts of our area, as in the neighbourhood of Axminster, there were no noteworthy sections of the Rheetic Beds. At Hood, north-west of Musbury Castle, and in the valley to the east of the castle, the Grey Marls were exposed, but it was difficult to say whether or not they occur at other points, owing to the debris of Green- sand that occurs on the slopes and in the valleys. The Rhtetic Beds were exposed in places along the Axminster and Lyme Regis railway to the south-east of Trill, and here again the boundary is indefinite owing to local slips and talus.* Information was obtained in 1873 that the White Lias had been reached in the large quarry north of Weycroft, at a depth of 5 feet beneath the water-level, and proved to a depth of 15 feet. (See p. 83.) Where the reck appears at the surface by the railway-cutting to the south-west, the beds are much broken and probably faulted. A well that was being made in 1904 to the south of the Axe, and not far from the high road west of Weycroft Manor House, was sunk through 7 feet of gravel into the Grey Marls. ' Noticed by T. Hawkins in his " Memoirs on Ichthyosauri," &c., p. 7. ^ Proc. Gfeol. Assoc, xi., 1889, p. xxx. ' Quart. Journ. Geol. Soc, xvi., 1860, p. 396 ; Geol. Mag., 1864, p. 290. * " Summary of Progress " for 1901, (Mem. Geol. Surv.), 1902, p. 55, 20 TRIAS. Inlying tracts of White Lias, the upper layer of which is locally termed the " White Rock," were observed by Mr. 0. Reid between Greatwood and Chapplecroft Farms, the top-bed exhibiting evidence of borings. The junction of White Lias and Lower Lias was shown in a quarry between Tolcis and Hasland Farms, to the south of Membury. At Gtreendown south-east of Membury, the Rhsetic beds were exposed, and the White Lias could be traced here and there on the ridge to the west. An inlier of Keuper Marl is here met with, indicating an anticline, the product no doubt of the Membury fault; and the disturbance is con- tinued in the inliers of RhEetic beds at Sarte and Greatwood. To the west of Membury the exposures of Rhsetio Beds were of Grey Marls, and this was the case again to the north at Furley. There is much debris of Greensand along the slopes south of Yarty Farm west of Membury. At Dane's Hill, Dalwood, the Greensand rests on an outlier of the Khaetic Beds, overlapping them in places; they consist mainly of the Grey Marls, but traces of the Black Shales were observed on the eastern slopes of Harner Hill, above Lower Farm. SECTION OF BORING M.VDE AT LYME REGIS. The following' particulars of a Boring in search of Coal at Lyme lieg'is are of importance with reference to the thicknesses of the Rhaetic Beds and Keuper Marls. As remarked by Mr. Jukes- Browne, it was an " endeavour to find coal at a place where no geologist would have recommended the attempt." The boring was made by Messrs. Vivian, in 1901, to the west of Colway Manor House, and about half-way between Horn Tavern and Middle Mill Farm, on the left bank of the Lym. The height above Ordnance Datum is about 90 feet. The full particulars, so far as they could be obtained, were published by Mr. Jukes-Browne (see Bibliography). Records and samples of the strata were sent to him by A. C. Pass and George Haycraft; and H. B. Woodward personally examined the cores that had been placed in a shed near the boring, and contributed some notes. The cores, however, had not been carefully arranged. The following- is an abstract of the record : — Thickness. Ft. In. D^rift / Soil, gravel, and flints 10 8 Blue shales and pale grey earthy limestones, some beds resembling White Lias (see p. 19) about 62 4 r White limestones with shaly layers ... ... 22 1 Grey and greenish marl 6 2 Dark shales and occasional bands of limestone, Avicula coniorta, Cardium {Protocardium) rli(Bticum, Pecten valoniensis, and Schizodics ^ cloacinus... ... ... ... ... ... 32 5 Ph Blue, grey, and green shales and marls, hard [ and soft bands (Passage Beds) f' Green marl ... Red and green marls ... Red and green marls with veins of gypsum ... Red and green marls with beds of gypsum up to 16 in. thick 3]3 jq Red and green gypsiferous marls with 3 bands of calcareous sandstone 134 Hard red and bluish clays and marls with gypsum 297 7 Hard red and bluish silty and micaceous clays with some gypsum UU 5 1,302 Lower Lias. 13 .2 { M L Depth. Ft. 111. 10 8 73 95 101 133 39 1 172 9 42 1 214 10 82 6 297 4 118 10 416 2 730 864 1,161 21 CHAPTEE IV. LIAS. In uo other part of the country cau the Lias, as a whole, be so well seen as on the coast from Axmouth to Lyme Regis and Eype, near Bridport. The connection with the Eeuper Marls, through the Rhsetic Beds, can be studied near Culverhole Point and Charton Bay ; while from Pinhay Bay eastwards the several divi- sions of the Lias can be traced in sequence through Lyme Regis until, near Bridport, we reach the Midford Sands that form the passage-beds between the Upper Lias and Inferior Oolite. Attention is now specially directed to the area which extends from Lyme Regis to Black Ven, but in order to gain a knowledge of the full sequence of the Lower and Middle Lias as developed inland, it is needful to examine the cliffs to the east of Lyme Regis as far as Seatowu, near Golden Cap. Before studying the beds in detail, it is a good plan to obtain a general view of the cliffs from a boat at a short distance from the shore. From the base of the Lower Lias to the Middle Lias all the beds can be examined and measured in detail, their continuity being only interrupted here and there by faults, of which the amount of displacement can be estimated with no great difficulty. Landslips, indeed, mask the beds in many places, but not so as to interfere with the complete exposure of the series at one point or another. The thickness of the Middle and Lower Lias amounts to about 830 feet, the Middle Lias being about 345 feet, and the Lower Lias about 485 feet. Notwithstanding the faults, which, having downthrows on the east, tend to carry the beds below the sea-level sooner than would otherwise have been the case, there are opportunities of measuring the larger divisions at different points. Comparing results it will be found that the measurements of the subdivisions differ to the extent of from 5 to 15 feet in sundry places. This may be due to original variations in the thickness of the strata, but it may also to some extent be attributed to a difference in pressure, the strata irt some places being overlain by thick and heavy accumulations, while in others they are at or near the surface. Prom Pinhay Bay to near Black Ven the cliffs are mostly vertical, or nearly so, and they are more or less dangerous to those who walk along the beach, on account of the crumbling of the cliffs and the loose fragments of rock that frequently fall. Attention must also be paid to the state of the tide, as at high-water the beds are inaccessible between Pinhay Bay and the West Cliff, Lyme Regis, and between Lyme Regis and Black Ven. The Liassic strata everywhere in the district indicate marine conditions, with waters more or less muddy, of no great depth, and not far distant from land. LowEB, Lias. Coast Sections. The Lower Lias is exposed in the cliffs between Culverhole Point and Golden Cap, where the strata admit of the following divisions : — AiM.MON'iTE Zones. Ft. 4 Wear Cliff or " Green Ammonite " Beds. f Liparoceras capricornus. Bluish-grey clays 105 \ Liparoceras henleyi. 3. Stonebarrow or " Belemnite " Beds. / Uptonia jamesoni. Pale-grey marls 80 I Deroceras armatum. .1 T>, 1 -IT T. J a T>i 1 Ti/r i" TEchioceras raricostatum. 2. Bkok Ven Beds or Black Marl. J Oxynotoceras oxynotum. Dark shales and cement stones: ... 195] ^^^^^^^^^^ ^^^^^^^ {Arnioceras semicostatum. Coroniceras bucklandi. Schlotheimia angulata. Psilonotioeras planorbis 485 22 LIAS. bo a CJ .S ej ^ -M TJ o o ,5 ^ 00 'nSB 'I' 4 -3 0? SI •Si 13 i^ ;^ o rr^ .^"g s CO « 2 § o ~^ <>J Si l> CM so ,Q oJ Q rai^m O to s s s s ^ s ^ T|H CO (N 1-i fa LOWER LIAS. 23 The generic names into which the old and comprehensive genus Ammo- nites has been split, cannot be said at present to be in a stable condition. We give what appear to be the latest names in use, some have been altered since our former edition was published, and, indeed, during the past twenty years there have been so many changes that student and teacher, amateur and professional, have been alike bewildered. Topographic names have been introduced for the' main sub-divisions of the Lower Lias as the terms Black Marl, Green Ammonite Beds, &c., are not very appropriate. ^ The term Black Ven Beds was used by Meyer {Geol. Mag., 1866, Plate II.) for the local Cretaceous beds, but the group- ing he then adopted has since been abandoned ; and the term strictly applies to the Lower Lias clays. The term Charmouthian, introduced by Mayer-Eymar, has been used to include the whole of the Middle Lias, and part of the Lower Lias by de Lapparent and Sir A. Geikie. It is prac- tically equivalent to the Pleinsbachian of Oppel, a term now more generally used, and in a chronological sense. Mr. S. S. Buckman includes in -Char- mouthian the Ammonite zones from niricostatum to capricornus, but this is not convenient from a stratigraphical point of view. The earliest geological description of the Lias along this coast was by De la Beche, who noted the leading lithological divisions in the strata and their organic remains, and gave an excellent pictorial diagram of the cliff-sections.^ The next important description of the Liassic strata and of the successive groups of fossils was given by Albert Oppel, who, in- spired by Quenstedt, introduced into this country the zonal divisions, most of which have been adopted.' Subsequently the Lower Lias beds were described in detail by Thomas Wright, while the subdivisions of the Middle and Upper Lias were investigated very carefully by E. C. H. Day, who was aided largely by li. Etheridge.* These observers have furnished the greater part of our knowledge con- cerning the distribution of the organic remains, but the help of local workers is of the utmost importance to those who can spend but a few weeks in a district. Much of our knowledge of the horizons of fossils is due to the labours of fossil-collectors, especially to Samuel Clark and Robert and Isaac Hunter, of Charmouth, no longer living. To the late .J. W. Mw-der, of Lyme Regis, we are likewise indebted for the recogni- tion and preservation of many important fossils. I. Lyme Regis Beds or Blue Lias. — Ammonite Zones : Psilono- ticeras planorbis,. SchlotheiTnia angulata, Coroniceras hucklandi and Arnioceras semicontatvm. This division comprises alternating bands of limestone and clay or marl, to which, as elsewhere, the term " Blue Lias " is confined. The beds appear by the shore to the east of Culverhole Point, and extend higher up in the cliffs about as far west as Dowlands and Bindon, but they are much tumbled and obscured by land- slips. Eastwards, gentle undulations bring the strata to a higher ' See Proc. Geol. Assoc, xix., 1906, p. 325. 2 Trans. Geol. Soc, ser. 2, vol. i., 1822, pp. 40-47, and Plate VIII. ; vol. ii., 1826, pp. 21-30, and Plate III. ; and " Report on the Geology of Cornwall, Devon, and West Somerset " (ifem. Geol. Surv.), 1839, pp. 222-235. ' P. A. Quenstedt, " Das Flozgebirge Wiirtembergs," 1843 ; Oppel, " Die Juraformation Englands, Prankreichs und des Siidwestlichen Deutschlands," 1856-58. ^ See Bibliography. 24 LIAS. level in Cliarton Bay, where the underlying Rhsetic series may be observed. It is not until Pinhay Bay is reached that the Lower Lias is seen to advantage. A ravine and watercourse here coincide with a fault, that throws down the Blue Lias limestones some 40 feet on the west (see Fig. 3) ; a dislocation depicted by De la Beche. On the east, the lowest beds of the Lias are seen resting on the White Lias, and in marked contrast as to colour. Thence the upward succession can be traced, and eaeJi band of limestone can be examined. The thickness of the main mass of stone-beds may be reckoned at 70 feet on the eastern side of Pinhay Bay, but detailed measure- ments made at different points on the coast to Black Ven, indicate that -the thickness increases to 80 or 85 feet. About 16 feet above the main mass of limestones, and separated from them by clays or shales, there is a conspicuous band of in- durated grey marl known as the Hard Marl or Table Ledge, and this is a useful guide in tracing the succession of strata. Taking the beds from the top of the White Lias up to the Table Ledge we have a full thickness of about 105 feet. Owing to the easterly dip of the beds, the lower portions, about 40 feet in thickness, are exposed only in the cliffs immediately east of Pinhay Bay. They do not reappear further on in the West Cliff, nor do they rise again in the Church Cliffs. ,The lowest zone in the Lias must thus be looked for as we pass eastwards from Culverhole Point and Charton Bay, and again eastwards from Pinhay Bay. At and near the base of the Lower Lias there occur thin laminated shales or paper-shales. Where exposed on the fore- shore some of the beds are seen to be crowded with spines of Echinoderms, whose tests also are occasionally pre- served. Among the species Dr. Wright recognized Cidaris edioardsi, F seudodiadema lobatum, Hemi- pedina hechei, and H. boiverbanJci. The associated limestones yield Ostrea liassica, Modiola minima. Area lycetti, Gervillia, and Pleuro- mya crowcomheia. The Ammonites Psilonoticeras planorhis and Calo- ceras johnstoni have been found at Pinhay Bay. There is no evidence whereby the zone of Psilonoticeras ■planorhis can be definitely marked off from the zones succeeding, but it includes about 20 feet of strata. Continuing eastwards by Seven Eock Point, we traverse ledges formed by the successive bands of limestone. Gryphcea arcuatn and Lima gig antea become more abundant. Some layers are crowded with Rhynchonella calcicosta (R. variabilis of Wrio-ht) and in others we find shoals of Pentacrinites (Isocrinus). Here and there Schlotheimia angulata may be observed, and further on many specimens of Nautilvs and Coroniceras hucklandi. Fig. 4. Psilonoticeras planorbis {J. de C. Sow.). LOWER LIAS. 25 Partly owing to the curvature of the coast, the beds in the West Cliff present a gentle synclinal followed by an anticlinal struc- ture. Moreover, below the Esplanade the beds sink again, so that the Cobb is based on the surface of the main mass of stone-beds, which appear on the foreshore, and here at low water the ledges stand out in graceful curves that mark the synclinal structure. Some of the ledges that occurred here, as elsewhere, have been broken up and removed by the hand of man, and among them portions of the " Table-rock " were formerly exposed near the eastern jetty. ^ The Table Ledge may be traced from the bank above the Esplanade to the Gun Cliff, and thence it is well seen in Church Cliffs. At the base of the Church Cliffs, the artificial removal of the ledges has largely aided the natural destruction of the cliffs, and the foreshore being full of muddy holes, affords at times a treacherous route for the traveller. Slabs of rock within recent years have been torn from the foreshore. (See p. 80.) In these cliffs the beds are somewhat disturbed by small faults and slips, and these dislocations give rise to many cracks or " vents " in the strata. The stone-beds with the Table Ledge dip gently towards Black Ven, and gradually disappear beneath the mass of the " Black Marl." They belong mainly to the zone of Coroniceras bucJclandi, but include the upper portion of the zone of Schloihevmia angulata, the lower portion of which has been previously traversed. The succession of the zones is as well-marked as could be expected, albeit there is no reason to point to any particular layer to indicate a separating plane. The Ammonites S. angulata and C. huch- landi have been found together at this locality. Fig. 5. Fig. 6. Fig. 7. Lima gigantea J. Sovk Gryphsea arcuata Lam. Isocrinus (Pentacrinus) basaltiformis {Miller). Schlotheimia oharmassei occurs as high up as the " Best Bed." (See p. 37.) Large specimens of Coroniceras bucMandi and • See (t. Roberts, " History and Antiquities of the Borough of Lyme Regis and Oharmouth," 1834, pp. 214, &c. 26 LIAS. Lima gigantea are common, and Nautilus striafMS and Isocrinus hasaltiformis, of which the joints (see Fig. 7) are known as " Tucks," may usually be found. Fig. 8. Fig. 9. Soapheus anoylochelis H. Wondv). Schlotheimia angulata {SMoth.). Arnioceras semicostatmn occurs near the top of the stone-beds at Lyme Eegis, as well as in the Hard Marl or Table Ledge above ; beds which were grouped by Dr. Wright in the zone of Arietites turneri. It occasionally occurs at higher horizons. V ermiceras bonnardi, recognized by Messrs. Sharman and Newton from this locality, is a form that somewhat resembles A. turne.ri, but it has been regarded as identical with V. conybearei. Specimens of these Ammonites are frequently enveloped or partly replaced by iron-pyrites ; and most of them have been found on the beach or among the fallen blocks near the northern end of the Church CliflFs. A block of limestone pur- chased from the late Mrs. Dollin, of Lyme Regis, contains V. honnardi and A. turneri. Another form, Asteroceras brookei, occurs in a higher horizon, in the zone of A. ohtusum: It is best to I'egard the upper portion of this Blue Lias series rather as the zone of Arnioceras semi- costatum than of Arietites turneri, because the former species is found in abundance on the same approximate horizon in other parts of England and has more generally been adopted as the zonal Ammonite. ^ Fig. 10. Fig. 11. Arnioceras semicostatum (Y. & B.). Coroniceras bncklandi (J. Sow.). The Blue Lias series of Lyme Regis thus includes the zones of the Ammonite species planorbis, angulatum, buchlandi, and Uasher, "The Country around Lincoln" {Mem. Oeol. Surv.), 1888, p. 16. LOWER LIAS. 27 semicostatum ; an arrangement that fits in well witli other parts of England, as it includes the main mass of the Lower Lias limestones, where these are well-developed. The limestones appear to have been largely detrital, derived not mainly from the grinding up or decay of the organic remains of the period, but also from the waste of Limestone cliffs that bordered the Liassic seas. It is interesting also to observe the varying nature of certain layers; some known as " skulls " mimicking chalk -flints in the irregular character of the nodular bands, while in other cases there occur smooth lenticular or ovoid masses of limestone. This process of segregation of the more calcareous matter from the mud might have varied according to the pressure to which the bands were subjected by overlying deposits during consolidation. 2. Black Ven Beds oe Black Mael.— Ammonite Zones : Astero- ceras ohtusum, Oxynotoceras oxynotum, and Echioceras raricostatum. The dark shales that overlie the " Table Ledge " are locally known as the " Black Marl." They appear above the West Cliff, but the slopes are difiB.cult of access and more or less obscured by slips. The lower beds are seen in places above the Esplanade, but the finest sections are those east of Lyme Regis, where their appearance well accounts for the name of Black Ven. In this cliff the entire division can be studied. The higher part of the upland, known as Timber Hill, is formed by Chert gravel, Upper Green- sand, and Grault. The base of the Gault is marked by a thin pebbly layer or grit, but the formation itself, as observed by the Rev. W. Downes, is pervious to such an extent that springs are thrown out by the Lias clay beneath.* It is well, moreover, to bear in mind that the fossils of the Gault and Lower Lias are commingled on the slopes. Further east the Black Marl forms the base of Stonebarrow, where its dark clay is surmounted by the grey clay of the Belem- nite Beds ; the whole being capped by the yellow Greensand, por- tions of which are washed down over the face of the clay-cliffs. The Lias of Black Yen is exposed in three terraces that form the lower portions of the cliff beneath the Cretaceous rocks. The uppermost of these is formed for the most part of pale grey marls, known as the " Belemnite Beds " (to be described further on). The terraces below are formed by the much darker shales, clays, and marls, which are noted in detail (p. 35). Near the top of the lowest terrace a band of Firestone Nodules is conspicuous, and it is slightly faulted at one point with a down- throw of 5 or 10 feet on the west. (See Fig. 3.) It is not, how- ever, shown in the cliffs east of Charmouth, as a more important fault traversing the valley throws down the beds about 50 feet on the east. The band of cement-stones or " Firestone Nodules "" is known as the Birchii Bed," from the occurrence of Microderoceras hircTiii. The specimens are familar to collectors as the " Tortoise Ammonites," and also as " White Ammonites " from the white ' Quart. Journ. Geol. Soc, xli., 1885, p. 23. ^ Some of the nodules were formerly used for fires, as fire-balls. 18821 C 28 LIAS. calc-spar that often fills the chambers of the shells. The band was most accessible in the western part of Black Ven towards the Church ClifPs. Fine specimens of Asteroceras ohtusum occur here and there in the clays and nodular limestones between the Table Ledge and the Coin Stone Bed ; and Polymorphites trivialis and other small and juvenile Ammonites, most of them replaced by piyrites, may be picked up on the slopes. Blocks of limestone, crowded with small ammonites, and resembling the famous Ammonite Marble of Marston Magna, which is on the same geological horizon, occur beneath the Penta- crinite Bed, and may be found on the clay-slopes or on the beach. Fig. 12, Fig. 13. Asteroceras brookei (J. Sow.). Asteroceras obtusum (J. Sow.). Not far below the Coin Stone Bed (see p. 35) is the layer known as the Pentacrinite Bed, which has yielded many fine specimens, mostly coated or replaced by _ iron-pyrites, of the " Briarean ^^^- ^^• Encrinite " Ecctracrinus hriar- (Fig. 15). Being often with lignite, by Buckland itself in large of floating ' eus found associated it was thought to have attached groups to wood. masses Fig. 14. Microderoceras birchii {J. Sow.). Extracrinus briareus {Miller). ' Bridge-water Treatise, 1836, p. 437. LOWER LIAS. 29 The Coin Stone Bed is the name applied to the upper portion of a band of large cement-stones, which form two and sometimes three layers, high above the Firestone Nodules, and in the upper portion of the darker shales. The cement-stones occur in the top of the middle clay-terrace of Black Ven, and form a noticeable band, about 40 feet beneath the pale-grey Belemnite Beds, in the cliffs of Stonebarrow to the east of Charmouth. Immediately above these beds we enter the zone of Oxynotoceras oxynotum, specimens of which are prevalent in the dark pyritic shales and clays about 10 feet above the Coin Stone Bed. The variety of this species known as lymensis, and Microceras densinodum likewise occur. Fig. 16. iiJ.4 l^:'\ rl'"'"/" Oxynotoceras oxynotum {Quenst.). Still higher in the same set of shales Deroceras armatum and fine examples of Echioceras raricostatum occur, but there is no- thing to indicate any plane of demarcation between the zones. E. raricostatum extends upwards into the Belemnite Beds, which are grouped in part with the zone of D. armatum. Large Fig. 17. Fig Echioceras raricostatum {Ziet.). 18821 Deroceras armatum (/. Sow.). C 2 30 LIAS. examples of this Ammonite with prominent spines have been obtained from the neighbourhood of Lyme Eegis, mostly from fallen blocks below Black Yen. Their particular horizon requires investigation. The series now under notice extends to the base ot the upper terrace under Black Yen, where two or three bands of limestone occur at the junction with the Belemnite Beds. These bands were mostly obscured in Black Yen by talus (in 1884), but were shown in the cliffs of Stonebarrow in the east. The Black Marl thus includes the zones of the Ammonite species obtusum, oxynotum, and raricostatum, which here and elsewhere may be conveniently linked together. 3. Stonebakuow or Belemnite Beds.— Ammonite Zones: Deroceras armatum and Uptonia jamesoni. This division occupies the higher portions of the clay-cliffs at Black Yen, forming the third terrace. It appears as a well- marked light-grey band here, and again in Stonebarrow, where the easterly dip brings it nearer and nearer to the sea-level {see Fig. 3, p. 22). It disappears abruptly, west of St. Gabriel's Water, Golden Cap, owing to a fault with a downthrow of about 40 feet on the east. Lenticular masses of lignite, approaching jet in character, occur in places. The central portion of this division is formed by a band of harder pale grey marls, but to the upper portion most interest attaches : in it there occurs a band of dark shaly marls, rich in fossils, covered by a thin layer of pale marly lime- stone, known as the " Belemnite Stone," and also very fossili- ferous. Black Yen is not the most convenient place to examine these beds, as the platform at their foot is exceedingly wet and boggy, springs being thrown out at the junction with the denser clays and shales below. Good sections are exposed in some of the gullies in Stonebarrow Cliff, and here their fossil treasures may readily be obtained.^ The finest exposures of the beds, however, are on the foreshore below Golden Cap, for tlie strata which were thrown down by a fault west of St. Gabriel's Water, re-appear owing to gentle anticlines, and they are usually well exposed both on the west of the loftiest portion of the cliffs, where they rise for two or three feet above the shingle, and on the east between Golden Cap and Seatown, where they appear 7 feet above the beach. In this latter exposure there is evidence of slight faulting. The fore- shore along which the beds are shown at low-tide is rather to the west of this exposure, and there a grand exhibition of Belemnites and other fossils is to be seen, some in the Belemnite Stone, others in still greater profusion in different layers of the dark shaly marls beneath. The long pencil-like forms of Belemnites longissimus are conspicuous, but difficult to extract, ' In his section, Trans. Geol. Soc, ser. 2, vol. i., 1822, Plate viii., De la Beche marked Stonebarrow Cliff as " Shorne Cliff," but the latter is the name applied to the higher portion of the clifE at Golden Cap. LOWER LIAS. 31 while B. elongatus, B. clavatus, and B. pollex are not uncommon. A large number of species have been identified.^ Among the Ammonites, Lytoceras fimbriaium and Liparoceras striatum may be found in the Belemnite Stone. Among the Belemnites and allied forms of fossil cuttle-fishes that have been found at or near Lyme Regis, it may be mentioned that specimens oiGeoteuthis, with, the ink-bag well preserved, were obtained by Mary Anning and described by Buckland in 1826. Samples of the fossil ink were submitted to Sir r IG. 19. Francis Chantrey, who had a drawing prepared with the sepia, which was pronounced to be of excellent quality.^ Remains of Xiphoteuthis have been obtained from the Belemnite Beds ; and Prof. Huxley has described two species of Belemnites — B. elongatus and B. hruguierianus — with the ink-bags preserved, both obtained from the zone of Asteroceras ohtusum.^ The dark shaly . marl especially, yields a number of small pyritic Ammonites, which may be found in the Stonebarrow cliffs, and are collected at Black Ven for sale. These are cut and polished for brooches, the species being Microceras subplanicosta, and Amblycoceras Belemnites clavatus planicosta : the last named being also recorded Blainv. from beds at a lower horizon. 4. Wbae Cliff oe Geeen Ammonite Beds — Ammonite Zones : Liparoceras henleyi and L. capricomus. Above the Belemnite Beds come the Wear Cliff Beds, a series of bluish-grey micaceous marly clays, with occasional indurated bands, nodules of hard grey limestone, and ferruginous layers, altogether about 105 feet thick. Towards the lower part of the series the limestone-nodules are most abundant and frequently contain specimens of Androgynoceras lataicosta (Sow). These when cut and polished are sold under the name of " Green Ammonites " because the spar filling the chambers is often of a green colour. The same Ammonite is abundant in the marly beds, but usually in a fragmentary state. Hence the name " Green Ammonite Beds," adopted by E. C. H. Day, has been used as a general term for the marls between the Belemnite Stone and the Three Tiers.' (See p. 40.) Traces of these beds first appear in the eastern part of Black Ven, although on account of the slips and the diflSculty of getting at the strata, they cannot be well examined. Mr. W. D. Lang has, however, obtained A. latcecosta and Rhacoceras loscombei, as well as several species of Straparollus, including ;S'. aratus Tate, from this locality.' ' See J. Phillips, Monograph on Belemnites {Palceontograph. Soc). 2 Proc. Geol. Soc, vol. i., 1828-9, p. 97 ; Bridgewater treatise, 1836, p. 305. ' Monograph on the Belemnitidse (Mem. Geol. Surv.), 1864 ; see also Gr. C. Crick, Froc. Malaeol. Soc, v. 1902, p. 13. ' Day, Quart. Journ. Geol. Soc, xix., 1868, p. 278. * Proc Geol. Assoc, xix., 1906, p. 324. 32 LIAS. Eastwards the Wear Cliff Beds occur above the Belemnite Beds in Stonebarrow Cliff, and although traces of the Tiers are found m places, showing that the entire thickness of the beds is there represented, only the lower portion is well exposed. The beds, however, are clearly shown beneath the Three Tiers in Golden Cap. Commencing east of St. Gabriel's Water, they are exposed along the base of the cliffs, above the Belemnite Beds (which appear here and there), as far as the Coast-guard station at Seatown, where about 70 feet of the beds, including the upper portion, may be seen. These beds do not appear east of Seatown, being let down on that side of the valley, below the sea-level, by a fault (noticed by Mr. Day), which has a downthrow of from 190 to 200 feet. Under the coast-guard station the beds are much disturbed and even contorted, features partly due to the fault and partly to landslips. {See Fig 3.) Fig. 20. Fig. 21. Liparoceras striatum {Rein.). Liparoceras henleyi {J. Sow.). Oppel grouped part of this series as the " Davoi-hett," cliaracterized by the Ammonites now known as Deroceras davcei, Liparoceras capricornus, L. henleyi, and Lytoceras- fimhriatum. Dr. Wright, who referred to the beds as the Davcei zone, placed them in the zone of Henleyi, but extended the zone above the Three Tiers, as high as the Starfish-bed, whereby he included a series of marls that are characterized by Amaltheus mar- garitatus.^ (See p. 41.) Fig, 22. Deroceras davoei (/. Sow.) Androgynoceras latcecosta is unques- tionably the most characteristic fossil, and this species was regarded by Oppel as a Capricorn - Ammonite." Some specimens of A. latcecosta are regarded by Mr. E. T. Newton as very near to Liparoceras capricornus, which has been recorded from the Dorset coast. There is therefore good reason to classify the beds with the zones of L. henleyi and L. capricornus, although the " Henleyi Ammonites " appear in the upper part of the preceding division. ' Wright, " Lias Ammonites," Falceontograph. Soc, 1878-86, pp. 89, 420. ' "Die Juraformation," 1856-58, pp. 155, 157. LOWElt LIAS. 33 Among the species collected during the Geological Survey are Liparoceras bechei, L. henleyi, L. striatum, Deroceras davcei, and Rhacoceras loscombei. R. loscomhei appears to be most abundant in the upper part of the Wear Cliff or Green Ammonite Beds,^ but specimens occur in the same block with A. latcecosta. Fig. 23. OTHEE FOSSILS FEOM LYME EEGIS. Of the MoUusca, attention has been drawn to the prevalent forms, but it may be mentioned that many of the species figured by Sowerby were obtained from Lyme Regis and the neighbourhood. Among these were the species of Ammonites named Bechei (after De la Beche), Birchii (after Col. Birch, a great frequenter of Lyme), Brookei (after H. J. Brooke), Davcei (after Sir H. Davy), Henleyi (after H. H. Henley, the Lord of the Manor), and Loscomhei (after C. W. Loscombe), together with Fim- iriatus, Latcecosta, Stellaris, and Striatus. Among Crustacea a fine example of Bryan antiquus (Broderip) was figured and described by Dr. H. Woodward (Geol. Mag. 1888, p. 433). Concerning the Saurians, for which Lyme Regis is noted, most- of the remains have been found in the Blue Lias series of the West Cliff and of the Church Cliffs, and in the overlying dark shales and cement-stones of Black Ven. The species are thus for the most part preserved at higher horizons than is the case with the noted locality of Street in Somer- setshire. Remains of Ichthyosaurus from the Blue Lias are found generally in layers between the stone-beds, and a fine specimen of Plesio- saurus was obtained from these beds (zone of Coroniceras hucklandi) by Mr. Day.^ Although for more than 120 years the fossils of Lyme Regis and its neighbourhood have been collected for sale, it was not until 1811 that Mary Anning, the most noted of the early fossil- collectors, obtained her first specimen of Ichthyo- saurus which was described by Sir Everard Home in 1819 under the name Proteo-saurus^ ; but in the previous year Koenig had applied the name Ichthyosaurus to remains of the Saurian, and hence that name became adopted. Examples 24 feet in length have been obtained. In 1821 Mary Anning discovered remains of another Saurian, described by Conybeare under the name Plesiosaurus ,* and in 1828 she pro- cured (for the first time in this country) the Pterodactyl, of which the species described by Buckland is now known as Dimorphodon macronyx. Another noteworthy form is the Scelidosaurus harrisoni, a Dinosaur obtained from Charmouth by James Harrison. This like many of the other fine Saurians was obtained piece-meal and at intervals. Many species of Fishes have been obtained from the Lower Lias of Lyme Regis, and to a large extent through the personal exertions of the third Earl of Enniskillen and Sir Philip Egerton. Little, however, is known of the special horizons of these fossils, although some, such as Chondrosteus and Bapedius {Mchmodus) are assigned to the zone of Asteroceras ohtusum. Other genera such as Acrodus, Eugnathus, Hyhodus, and ' See also Day, Quart. Journ. Geol. Soc, xix., 1863, p. 291. 2 Geol. Mag., 1864, p. 47. ' See papers by Home, Phil. Trans., 1814-1820. * Trans. Geol. Soc, ser. 1, vol. v., 1821, p. 559 ; ser. 2, i.,pp. 103, 381 ; see also Buckland, "Geology and Mineralogy" (Bridgewater Treatise), i., ed. 3, 1858, p. 198. Acrodus anningise Ag. (Brit. Mus.) 34 LIAS. FKolidophorus, together with Bapedius have been obtained from the stone- beds below.i (See Figs. 24 and 25.) The Coprolites originally described by Buckland were found in the same set of beds. There are few records of any vertebrate remains from the Belemnite Beds and higher stages of the Lower Lias of Dorsetshire. Two examples of Cycadean stems have also been recorded from the " Lias " of Lyme Regis, under the names of Cycadeoidea (Yatesm) gracilis and 0. pygmma.' /^ j-j j Other cycad-remains under the names of Pagiophyllum, tycadites, and Otozamites (OtopUris), and the ferns Thinnfeldia and Ctenopteris, have been recorded from the Lower Lias of Lyme Regis, Axminster and Membury. Fig. 24. Dapedius politus De la Beche, Lyme Regis. (Brit. Mus.) Fig. 25. Pholidophorus delabechei Ag., Lyme Regis. (Brit. Mus.) Notwithstanding all that has been done in the matter of collecting fossils from the Lower Lias at Lyme Regis, there is yet a great deal to be ascertained with regard to the precise horizons and ranges of many of the species, whether of vertebrate or invertebrate animals or plants. Too often the specimens in museums have been gathered on the slopes, and even when obtained in situ the exact position has not always been recorded. To investigate the distribution of the fossils in the detail ' See lists by Bgerton in De la Beche's Report, p. 225 ; Wright, Lias Ammonites, Palceontograph. Soc, p. 61. Recent particulars will be found in Dr. A. Smith Woodward's " Catalogue of the Fossil Fishes in the British Museum (Natural History)," 1889-1901. ' Oarruthers, Trans. Linn. Soc, xxvi., 1870, pp. 689, 703. See also A. C. Seward, Cat. Mesozoic Plants, Brit. Mus., Jurassic Flora, II., 1904. LOWER LIAS. 35 required for modern biological study would necessitate researches extend- ing over two or three years, and these should be carried out in a thoroughly independent manner. It is hoped that the particulars of the strata here given may prove of some service in further and more detailed work. The details of the Lower Lias are as follows : — ■ Weak Cliff or Green Ammonite Beds. Zones of Liparoceras capricomus and L. henleyi. About 105 feet. Seen in clifis from eastern end of Black Ven to base of Golden Cap. Stonebareow or Belemnite Beds. Zones of Uptonia jamesoni and Deroceras armatum. About 80 feet. Seen in Black Ven, Stone- barrow and Westhay Olifes. Z) Black Ven Beds or Black Marl. Zone of Echioceras raricostatum. About 15 feet. Zone of Oxynotoceras oxynotum. About 15 feet. Three Tiers (base of Middle Lias.) ' Sandy and ferruginous clay passing down into ] bluish-grey micaceous marly clay with iron- ( stone nodules and iron -stained limestone 1 nodules ' Flaggy bed of sandy calcareous rock Bluish-grey micaceous marly clay with ferru ginous band. Bhacoceras loscomhei Occasional bands of indurated marl or limestone Bluish-grey marly clays with nodules of hard grey limestone and ferruginous bands. Andro- gynoceras latxcosta, Liparoceras bechei, L. [_ striatum, Inoceramus ventricosus Belemnite Stone. Hard pale-grey uneven marly limestone ... Dark shaly marls with much iron-pyrites, and' pyritic fossils ; Microceras subplanicosta, Ino- ceramus, Waldheimia numismalis, &c., with nodules and impersistent masses of hard grey limestone Pale grey marls with Belemnites milleri, B. eom- pressus, &c. Hard marly limestone and hard pale and dark grey marls, forming ledges in the gullies of Stonebarrow Cliff over which springs fall. Thickness variable Grey shaly and micaceous marls with Belem- nites (as above) Marly limestones and shales >- Shales Ft. In 12 1 38 54 6 toO 8 6 35 6 30 1 1 Grey earthy limestones with shales. Watch- \ STONE Beds with Ech. raricostatum, Belem- j- y nites ... ... ... ... ... ... -" I Dark shaly marl with D. armatum : including \ Metal Bed with much iron-pyrites J 3 10 to 15 0. ^ nd y Zone of Asteroceras obtusum. About 170 feet. Dark shaly pyritic marl with 0. oxynotum, 0. lymense and Microceras densinodum, found 10 feet above Coin Stone Coin Stone Bed (Corn Stone Ledge of Dr. Wright). Cement-stone bed, in impersi^tent nodular masses that form a prominent band in Stonebarrow Cliff. Fish-remains Dark and rusty shales with nodules of limestone Ferruginous and marly cement-stone in two bands. Large specimens of Ast. stellare in sparry and septarian nodules ; also A. broolcei [Wright] Dark shaly marls with Pentacrinite Bed, • yielding Extracrinus briareus ; and below, impersistent layers of limestone (like Ammon- ite Marble) with many small Ammonites, A. obtusum, Amblycoceras planicosta, &c. Dark slightly micaceous and calcareous paper- shales with flattened Ammonites ■ 15 10 25 36 LIAS. Black Yen Beds or Black Makl — cont. Zone of Asteroceras obtusum. About 170 feet — cont. The above beds of Black Marl seen in upper part of West Cliff, in Black Ten and West part of base of Stonebarrow OlifE. Ft. 1 ;;} Lyme Regis Beds or Blue Lias.' Zone of Arnioceras semicostatum. Seen in Church ClifE, West Cliff, and Pinhay Bay. ' Band of irregular indurated marl Dark shaly marl and shale with nodules of lime- 1 stone ) Upper Cement Bed. Hard iron-stained Cement- j stone, an irregular and conspicuous band seen I in central part of clay-cliff of Black Yen, and j in lower part of cliff east of Charmouth ... ) Nodular and impersistent limestones with Saurian "j remains ... ... ... ••• ••• ■•• f Shaly marls Thin band of limestone Marls Lower Cement Bed. Hard irregular iron- stained marly limestone or cement stone : seen near base of cliff East of Charmouth. This termed the West Kock in West Cliff and the bed a few feet above, are known as the " Two Cement Beds " Shaly marls, yielding fine specimens of Ast. \ 30 brookd sometimes enveloped in pyrites ... -' to 40 Firestone Noddles or Birchii Bed. Hard irregular and nodular limestone or Cement- stone ("nuts"), with shell of "beef" above and below. It forms one or two beds with iron-stained joints and is a prominent band in the lower part of Black Yen, inclined towards Charmouth, and terminating in the low cliff near the Coast Guard Station. Microderoceras birchii and clusters of small Ammonites Dark shales with band of thin shaly limestone, and occasional nodules of limestone Lenticular but persistent band of grey limestone, " with " beef " Dark shales with thin band of limestone in places Interrupted band of limestone with " beef " and pyrites : not very conspicuous ... Dark shales and paper-shales, slightly calcareous and micaceous, with indurated bands and seams of "beef." [Saurian remains.] Marly cement-stone bed Marly shales with iron-pyrites, and thin con- spicuous layer in the West Cliff known as the Black Bear : seen in ClifE above Esplanade, and in East ClifE 'Hard Marl or Table Lbdhe. (" Indurated ~ Marl," of De la Beche.) Well seen in West Cliff, above Esplanade, in Gun ClifE, and in Church Cliffs ; it descends to beach at foot of Black Ven. Grey marl that becomes in- durated on the sea-front by the Esplanade, A. semicostatum, \_Arietites turneri'], Avicula incequivalvis, lihynchonella calcicosta {= vari- abilis of Wright) ... Saurian Bed. Shale. \_Ichtliyosaurus communis, \ I. platyodon A. semicostatum, Rh. calcicosta'^ ... J Split Ledge or Fish Bed. Shaly limestone, -v breaking into pencil-like slabs. \_Ariet. turneril, !■ In. 3 1 3 9 6 1 1 6 10 15 25 3 6 to 12 Am. semicostatum . Marl and shale with limestone-nodules 3 8 ' A detailed section was published by Dr. Wright, Quart. Journ. Geol. Soc. xvi., 1860, pp. 401, &c. The species included in square brackets are given on his authority, but it is not possible to correlate all the particular beds he enumerates, with those above noted. LOWEB LIAS. 37 Lyme Beois Beds or Blue Lias — cont. Zone of Coroniceras hucklandi (in part). Seen in Church Cliff, West Cliff, and Pinhay Bay. Even band of grey ' Saurian remains ... Zone of C. huchlandi. Seen in Church Cliffs and West Cliff. fGKEY Ledge.' Grey earthy limestone with fucoidal markings. C. huchlandi, A. semi- costatum, Lima gigantea, Avicula, \_Lima anti- quata, Rh. calcicostal Shale. \_PlesioBaurus rostratus] Glass Bottle. Irregular and lenticular grey limestone. Ijarge C. bucMandi on under sur- face. ILima gigantea, L. antiquata, Rh. calci- costa'} Shale Top or 1st Quick Ledge. limestone. C hucklandi. Marly Shale Venty Bed. Even band of grey limestone, marly at base Shale and marl with occasional nodules of lime- stone Best Bed. Even bed of limestone. Large Lima gigantea, Schlotheimia charmassei Shale Second Bed. Even bed of limestone : seen at base of Church Cliff, under wall. Nautilus, Isocrinus ... Dark shales ... ... ... ... ... ... Rattle. Impersistent limestone passing into marl. Ammonites. Seen at base of Church Cliff, under wall Dark shales with a few impersistent layers of limestone ... Middle or 2nd Quick Ledge. Smooth band of grey limestone : well marked in cliff, and one of the highest beds that comes to the shore in ledges near Devonshire Point. Seen under termination of wall , in Church Cliff, and it descends to beach on eastern side of gentle anticline. Isocrinus ... Shale (impersistent) Gumption. Thin band of grey limestone. Fish- remains Grey marl and shale with " beef " (fibrous car- bonate of lime), pyritic layers, and occasional lenticular masses or nodules of limestone. Extends in broad shelf below the projecting portion of Church Cliff. Isocrinus Under or 3rd Quick Ledge. Grey shelly lime- stone. Nautilus, Ostrea ... Shale with thin seams of " beef " ... Top Tape. Grey shelly limestone fucoidal in places, and splitting into two layers with lig- nite. C. hucklandi, Isocrinus, Scaplieus ancy- lochelis (Fig. 9, p. 26) described by Dr. H. Woodward from " Tape Ledge " Shale with lignite Under or 2nd Tape. Grey limestone with fucoidal markings. Gryphcea arcuata abun- dant, C. huchlandi Top Copper. Dark limestone with veins of calc spar and iron-pyrites ' '- Dark shale. Gry. arcuata, Rhynch. calcicosta ... Ft. In. 3 6 3 3 5 9 9 8 1 to 1 3 5 1 6 3 6 3 3 2 3 ' The "Grey Ledge" was misplaced in Dr. Wright's section. It forms the top of the main mass of stone-beds, and is probably the same as the Broad Ledge, a platform of rocks exposed at low-tide at some distance from the eastern jetty, south-east of the Church Cliffs. 38 LIAS. Lyme Regis Beds or Blue Lias — cont. Zone of C. huchlandi — cont. Zone of Schlotheimia angulata. Seen in Pinhay - Bay, West CM, and the base of Church Clifes. Zone of Psilonoticeras planoriis and perhaps a part of that of S. angulata. Seen in Pinhay Bay. Rhsetic Beds. f Mongrel. Irregular pale grey limestone with hummocky surface and fucoidal markings. Bh. calcicosta abundant in clusters : Ammonites ... Shale and shaly marl with impersistent mottled limestone, 2nd Mongrel or Skull. Gry. arcuata, Vermiceras conybearei ••• Specketty Bed. Grey limestone, Kh. calcicosta Dark shales. G. arcuata Upper White Bed or 3rd Tape. Limestone, G. arcuata, Lima gigantea ... ... _•.• Skulls. Layers of pale grey irregular and im- persistent limestone and clay. Schlotheimia angulata Iron Ledge. Grey limestone. Rh. calcicosta, Gryphma arcuata. This is the lowest bed worked in the clifE west of Lyme Regis Dark shale . ••• Under Copper. Irregular grey and sparry lime- stone with "mundic" (iron-pyrites). Lima gigantea, Rh. calcicosta ... ... ••• ••• ' Dark shales and grey limestones, very little hard rock : seen in reefs on shore below Church ClifE. S. angulata, Lima gigantea Under White Bed. Sparry limestone. Lima gigantea, G. arcuata Skulls. Pale grey nodular limestones with very j irregular surfaces, and very little shale. Large I Lima gigantea. L. hermanni. These are the j lowest beds seen in Church ClifE ' Dark shales Irregular limestones and shales with Lower' Venty Bed, Pig's Diet or Sorx Bed, and Brick Ledge. Ammonites, Ostrea. These are the lowest beds worked on the foreshore below West ClifE and Church Cliff Shale with bands and nodules of limestone : G. arcuatq^ Grey limestone Dark shale and shaly marl with 7 bands of even and irregular limestone Grey shelly limestone Shale Shales with 5 beds of even-bedded limestone. Lima gigantea &hTmia,'D.i ... Shales with 5 irregular bands of limestone. Pholadomya, Ammonites Compact limestone with marly base, weathering "j white and forming a conspicuous ledge near j- Pinhay Bay -' Shale Limestone with large Ostrea, G. arcuata, Lima gigantea Shales with 3 bands of limestone ... Limestone with Modiola, Ostrea Uassica, G. arcu- ata, small forms of Lima gigantea Shale and 8 bands of shelly limestone, Ostrea' Uassica, spines of Bchinoids Irregular bed of limestone, disturbed in places, the lower part ferruginous and shelly. Ostrea Uassica Brown laminated paper shales with films of lime- \ stone ... / White Lias. Ft. In. 2 8 ne. \ J 13 2 9 3 6 to 5 1 6 3 5 9 12 1 1 6 3 3 3 1 3 1 6 6 5 6 1 LOWER LIAS. 39 Inland Sections, At Uplyme and near Axminster there is sometimes a difficulty in readily determining the junction between the Lower Lias and White Lias. Among the Lower Lias limestones there are beds of pale marly limestone and compact limestone that much resemble beds of White Lias. (See pp. 19, 83.) Numerous old quarries occur in the neighbourhood of Uplyme, and the beds are now worked about a quarter of a mile north of Uplyme MiU, and at the Yawl limekilns to the north-west of the village. At Yawl, imme- diately above the "White Rock" or top of the White Lias (see p. l9), is a band of brown laminated shales 1 foot thick, and this is succeeded by bands of tough ferruginous and sandy limestones, slabs of which are crowded with Ostrea liassica and small examples of Lima gigantea; Modiola and Pleuromya occur, and spines of Echinoids are abundant. These strata are succeeded by upwards of 20 feet of limestones and shales, the limestones being some of them pale grey and compact like beds in the White Lias. In the lower beds Psilonoticeras planorhis and Caloceras johnstoni have been found, as well as Gryphcea arcuata and Lima gigantea. The higher beds contain Vermiceras conyhearei and include a portion of the zone of Schlotheimia angulata. From them Dr. Wright recorded Lima antiquata Sow. ( = L. suecinda Schloth.)i In this tract where the Rhaetic Beds appear as an inlier there is evidence of local displacement of the beds by faulting. This is the case also near Axminster : subsidiary dislocations occur in proximity to the principal faults. The limestones are quarried by the railway north of Weycroft, and there a broken anticline was exposed, the effects of which diminished in depth, showing that the feature was due to local thrusting. (See Fig 26.) Fig. 26. Gravel, 3 feet. -^o„' -s' Clays, 10 feet. , -^^ o Limestones and Clays, 25 feet. Section at Weycroft, near Axminster. (H. B. W.) We have no records near Axminster of the full thickness of the Blue Lias series, but the quarries show about 30 feet of stone-beds. (See p. 83.) Judging from the evidence obtainable, there is reason for believing that the stone-beds of Lyme Regis diminish in thickness towards the north, a large part of the zone of Coroniceras huchlandi being represented by clays with subordinate bands of stone. The Lower Lias clays occur over much of the country east of Weycroft, near Hawkchurch and Chard junction in the Axe Valley, and in the valley by Chardstock; but there are few openings of any kind to reveal the > Quart. Journ. Geol. Soc., xvi., 1860, p. 396 ; Geol. Mag., 1864, p. 291 ; and " Lias Ammonites," Pal. Soc, 1878-86, p. 21. 40 LIAS. zones, and the brickyards formerly in work in the valley below Tuck Mill and north-west of Castle Inn, near Hawkchuroh, have long been abandoned. Near Axminster the lias clay " is so bituminous in some places, that it has been sunk through in search of coal."i Middle Eias. This division is not exposed in the cliffs of the area represented on the map, but portions of it appear inland, where unfortunately there are no sections that clearly exhibit the characters of the strata. An examination of the ground from Thistle Hill to Champernhayes Farm, and again between Hawkchurch and Forde Abbey, failed to yield any definite information. A great deal of Greensand detritus is spread over the slopes, while, unfortunately for the geologist, several brickyards that formerly existed have been abandoned. In an old clay-pit west of Forde Abbey Farm, in 1904, a fragment was obtained of an Ammonite most nearly resembling Liparoceras caprieomus. This occurred in the lower part of the pit, and tended to confirm the boundary-line drawn on the map between Lower and Middle Lias. It is desirable, therefore, to give such particulars of the strata as are obtainable from the cliffs that extend eastwards to Char- mouth, Golden Cap, and Thorncombe Beacon. In passing eastwards from Lyme Eegis, we find traces of the lower beds of the Middle Lias in Stonebarrow and Westhay Cliffs. Tumbled blocks of the Three Tiers may be observed here and there above the platform formed by the "Wear Cliff or " Green Ammonite " Beds and by the Stonebarrow or " Belemnite " Beds, but the strata are much obscured by a wreck of Cretaceous material. Better sections are to be seen at Golden Cap, which rises to 619 feet, and owes its name to the sands of Upper Green- sand age that form its summit; for these are " gilded " on a sunny day, and appear in marked contrast with the dark Liassic clays beneath. Beneath Golden Cap there are without doubt the grandest series of Lias cliffs in Dorsetshire. Their outlines are very varied, the precipices and slopes being scarred by deep channels and chines, separated by irregular peaks of Lias clay; while the thick bands of calcareous sandstone, known as the " Three Tiers," which constitute the base of the Middle Lias, form great buttresses along the lower portions of the cliffs, about 80 feet from the base. They stand out prominently above the Wear Cliff Beds, and form ledges over which several springs fall after traversing gullies in the overlying clay. Large tumbled blocks of these Tiers and other rocks protect the base of the cliffs and form a small headland. (See Fig. 3.) The highest beds of Middle Lias seen in Golden Cap belong to our group of " Laminated Beds," zone of Amaltheus margari- tatus. To gather details of the entire series we have to proceed ' Conybeare & Phillips, " Outlines of the Geology of England and Wales,'' 1822, p. 264 (footnote). MIDDLE LIAS. 41 eastwards to Down Cliff and Thorncombe Beacon. The following are the sub-divisions of the Middle Lias : — TTDDer ( ■'^'"^ micaceous sandy shales. Lias. 1 ^°™P*°t P^Je yellow and pink limestone, joined to the layer below, (. and forming a Junction-bed. Sh ^" 11. Brown and greenish-grey conglomeratic and iron-shot limestone Pleurotomaria, flO.. Ft. In. 9 s o o _ QQ n 1 30 G-rey marly and sandy clays with indu rated bands 10 9. Yellow and brown micaceous sands, with huge indurated masses or Doggers, Pal- topleuroceras spinatum 50 8. Bluish-brown micaceous sandy clays ... 16 7. Hard blue and brown ferruginous sandy limestone, Am. margaritaius, Rhyncho- nella tetrahedra ... 6. Blue and grey laminated micaceous sands and clays, with nodules and bands of hard flaggy micaceous sandstone 5. Hard bluish-grey shelly and sandy lime- stones, with Pentacrinites, Gryphaa ^ cymbium, Pecten mquivalvis ... 1 5 to 2 3 Middle J ■» g 4. Blue and brown micaceous sands, clays, Lias. ' § h^ and sandy marls with ferruginous layers, ironstone nodules, and occasional nodules or lenticular beds of blue lime- stone 40 3. Starfish-Bed. Hard greenish-grey mi- caceous and calcareous sandstone, with Ophioderma egertoni, and 0. tenuibra- chiata ... ... ... ... ... 4 6 2. Bluish-grey micaceous marl and clay, with occasional indurated bands, and small irregular nodules of grey earthy limestone, ironstone nodules, and iron- pyrites, Am. margaritatus, Leda gra- phica 155 6 1. Three Tiers. Three thick bands of fissile micaceous and calcareous sand- stone, separated by micaceous sandy clay with concretionary masses of cal- careous sandstone 35 Lower Lias. Wear Cliff or Green Ammonite Beds. 3 s 345 Note. — The fossils figured in the previous pages are mostly reproduced from the Geological Survey Memoir on " The Jurassic Rocks of Britain," vol. III., in which the sources of the figures are acknowledged. The illustrations of fishes were kindly supplied from the British Museum (Natural History). Figs. H, 12, and 14 (after Dr. T. Wright) are new. 42 CHAPTEE V. CEETACEOUS. Upper Geeensand and Gactlt. (Selboenian.) The bold uplands of East Devon and the borders of Dorset are formed mainly of the Upper Greensand, capped by irregular accumulations of flint and chert gravel, and underlain in places by Gault clay. The best sections are undoubtedly exhibited in the clifis from Lyme Regis to Sidmouth, and they early attracted the attention of De la Beche who, in 1826, described the following subdivisions near Lyme Regis and Seaton in the " Sands and Sandstones beneath the Chalk usually termed Green-sand "*: — Chert Beds. Foxmould (Yellowish brown sand). Oowstone Beds (Sands with indurated nodules). This series was taken to represent a thickness of about 200 feet and the estimate has since been confirmed. No portion of the Gault was then recognized, but ten years later Fitton considered that the series might include representatives of both Lower and Upper Greensand, observing that " 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."' Godwin- Austen, in 1843, expressed the view that the lower beds of the Greensand in Dorset and Devon were a sandy^ condition of the Gault' ; and this conclusion has been established by subsequent observers. Mr. A. J. Jukes-Browne, in 1900, introduced the appropriate term Selbornian to include the Upper Greensand and Gault. He then published a full account of the strata and their fossils, and to his observations and records our information is largely due. The strata are wholly marine, the clays indicating deeper water, and the shelly sands, as near Sidmouth, indicating depths of 40 to 100 fathoms with land not far away.* The general section of the Upper Greensand and Gault is as follows ; — ■ Feet. 6 to 10 Upper Greensand. Gault. Zones. Pecten asper. Schloen- baehia rostraia. HopUtea interruptus. 5. Calcareous grit or sandstone 4. Buff and green sands and sandstone, with layers and nodules of chert irregularly developed, and occa- sional nodular masses of calcareous sandstone : (Chert Beds) ... 3. Green, grey, yellow and white sands, weathering brown and red, with greenish -grey calcareous concre- tions: (Foxmould) 2. Sands (15 to 20 feet thick) : with locally three bands of lenticular concretionary masses of hard cal- careous sandstone (Cowstones) ... . 1. Dark glauconitic and micaceous loamy sands and clays, with nodules of iron-pyrites ; and pebbly layer in places at base 50 to 70 100 to 150. 20 to 45 ■ Trans. Geol. Soc, ser. 2, vol. ii., 1826, p. 113 ; see also " Report on the Geology of Cornwall, Devon, and West Somerset " (Mem. Geol. Surv.), 1839 p 235 ' Trans. Geol. Soc, ser. 2, vol. iv., 1836, p. 233. ' ' Proc. Geol. Soc, iv., 1876, p. 197, and Trans. Geol. Soc, ser. 2, vol. vi. 1840, p. 449 ; see also Quart. Journ. Geol. Soc, vi., 1850, p. 472 ; D Sharup JhiA x 1 854, p. 186 ; and Meyer, Geol. Mag., 1866, p. 13. ' ^ ' ' • "Cretaceous Books of Britain," vol.i. (Mem. Geol. Surv.), 1900, pp. 182-215 404. UPPER GREENSAND AND GAULT. 43 O I M & Co I 6 Em i •; r. ^ '.-.Ir.: ^v •.'.■AV ■,'.\^ ?r^\ m ' 'U ' -^m (iioM'^ .+;: o o 3 o K a tS S s o p. p< OQ 9 " W ft %/^ o'o a t ■" 13 CSrtfq 53 w=? PS )> K o o o S>s Cu a PI ri ",^0 o o OPtSJtqtq 9 rC3 «H aj'd 18821 44 CRETACEOUS. The total thickness, as estimated by Mr. Jukes-Browne, is from 170 to 230 feet, and this inchides the local development of the Gault clay. Bed 1, which is local, represents the more clayey conditions of the Ganlt. It has been observed along the coast near Lyme Regis, and inland in the railway-cutting east of Honiton. It belongs to the zone of the Ammonite Hoplitex interruptvs. Beds 2 and 3 include the Cowstones and Foxmould of De la Beohe, and yield the fossils of the Blaokdown Beds of the area to the north. They represent the zone of the Ammonite Schloenhachia rostrata. The Cowstones derive their name locally, from the fancied resemblance to cattle of the fallen blocks on the slopes bordering the coast. They consist of flattish masses of calcareous sandstone, from 6 to 12 inches in thickness, and 3 or 4 feet in diameter. The Foxmould is also a local term. The Chert Beds (4) form the scarps of the bold hills which are the prominent features in the district. The Calcareous Grit (5) .often stands out in relief, forming conspicuous ridges along which the rocks sometimes appear at the surface bare of soil. They weather in cavernous form. These beds (4 and 5) belong to the zone of Pecten asper. The following lists include the more abundant and characteristic fossils that have been recorded from the district by C .1. A. Meyer, C. E. De Ranee, W. Downes, Dr. A. Strahan, Mr. Jukes-Browne,' Mr. W. D. Lang,2 and Mr. H. A. Allen': — Gault. Zone of Hoplites intemiptus- Dark green loam (Top of Serpula concava (J. Sow.). Lingula subovalis Dav. Cuoullsea (Grammatodon) carinata (J. Sow.). Gervillia linguloides Forbes. Inoceramus concentricus Park. Lima gaultina Woods* Modiola albensis cV Orb. Nuoula pectinata J. Sow. Pecten orbicularis /. Sow. Black Yen, Ware, &c.). Pecten (Neithea) quadricostatus J. Sow. Pinna robinaldina (T Orb.'' Thracia sancta-crucis Pict. and Camp. Aporrhais retusa (J. de C. Soio.). Avellana inflata d' Orb. Natica genti (J. Soio.). Turritella vibrayeana d' Orb. Hoplites interruptus (Brug.). splendens (J. Soid.). Discoidea subuculus (Klein.). Holaster Isevis de Luc Salenia gibba Ag. Rhynchonella dimidiata (J. Sow.). Upper Gbeensand. Zone of Pecten asper. Calcareous Sandstone. (Bindon, &c.) Rhynchonella schloenbachi Dav. Terebratella pectita {J. Sow.). Terebrirostra lyra (J. Sow.). Exogyra conica J. de C. Sow. Cliert Beds. (Seaton, &c.) Exogyra digitata (J. Sov).). Ostrea ( .^lectryonia) frons Parle. Pecten (Neithea) quadricostatus J. Sow. qninqueeostatus /. Soil). Sponge spicules. Orbitolina concava Lam. Serpula (Vermicularia) concava (./. Sow.). Exogyra columba Lam. conica J. de C. Sow. iQi'i^s^^on^""^ ^°^^^ °* Britain," vol. i. {Mem. Geol. Surv.), 1900, pp. 185-188, J-I/'t, li7o, ZU4. ' Geol. Maff., 1903, p. 391 ; 1904, p, 129 ; Proc. Geol. A.9soc., xix., 1906, pp. 323, ^ Geol. Mag., 1909, p. 170. " Hitherto recorded as Lima parallela d'Orb. (fide Lang and H. Woods). ■ Hitherto recorded as Pinna tetragona Sow. (fide Lang and H. Woods). UPPER GREENSAND AND GAULT. 45 Upper Geeensand — cont. ■Zone of Schloenbachia rostrata. roxmoiild (Charmouth, with overlying calcareous and glauconitic sandstone at Whitecliffi, Beer and Sidmouth). Grervillia solenoides Defr. Lima semisulcata J. de C. ., Ostrea frons Park. Pecten orbicularis /. Sow. (Neithea) quadricostatus J. Sov!. Pectunoulus umbonatus {J. Soio.). Trigonia alif ormis Park. Turritella granulata /. de C. Sow. Serpula concava (J. Sow.). filif ormis J. de C. Sow. Entalophora ramosissima d' Orb. Cardium hillanum J. Soio. CucuUsea glabra Park. Cyprina cuneata, J. de C. Soio. Dosiniopsis caperata (J. de C. &i«.)- Bxogyra columba Lam. couica J. de C. Sow. Sow. Siphonia sp. Serpula concava (/. Sow.). Enallaster (Hemipneustes) greenovi (Forbes). Hoploparia longimana (J. Sow.). Necrocarcinus tricarinatus Bell. Avieula pectinata J. de C. Soio. Aucellina gryphseoides (J. de C. Soir.). Cucullsea carinata (J. Sow.). glabra Park. Exogyra conica J. de C. Soio. Cowsioiiess. (Charmouth to Seaton.) Grryphaea vesiculosa J. Sow. Inoceramus concentricus Park. sulcatus Park. Lima tombeckiana d' Orb. Pecten orbicularis J. Sow. Pectunculus umbonatus (/. Sow.). Trigonia aliformis Park. vicaryana Lye. Turritella granulata J. de C. Sow. Hoplites splendens {J. Sow.). Orioceras. Coast Sections. As remarked by Mr. Jukes-Browne : — " Wherever the capping of Chalk has been completely removed from the tracts of Upper Greensand, the Chert-beds seem to have yielded very rapidly to the disintegrative effects of rain, frost, and percolating water." East of Lyme Regis " the quarries on Hardown Hill show layers of chert which seem to have settled down in mass, while much of the intervening sand has been carried away ; probably it has been gradually washed out by the soakage of rain and the suck of the springs which issue at various points round the hill."^ The decomposition of the beds, as shown in a chert-pit to the east of the Charmouth road-cutting, has given rise to a clayey kind of residue, which is made up largely of powdery chert, and it is probable that much of this material enters into the matrix of the superficial accumulation of clay with flints and chert. (See p. 69.) The high ground above Black Ven is capped with the broken remnants of the Chert-beds, and the ' following section at this locality was noted by Mr. Clement Reid in 1875 : — Drift. Upper Greensand. / Brown loam with quartz grains and unworn chalk \ flints about Chert- beds, much shattered ... Rusty sand with glauconite and many broken shells of Pecten Ft. In. 5 20 2 o a o Brown and grey sand ; the lower part rather loamy and containing glauconite and numerous irregular concretions. Few fossils 74 • " Cretaceous Rocks of Britain," vol. i. (Mem. Geol. Surv.), 1900, p. 191. 18821 D 3 46 CRETACEOUS. Upper Greensand — cont. Ft. In 1 12 10 5 Gault. 7 1 6 9 6 6 Cowstones (3rd bed) Grey sand Cowstones (2nd bed) ^ , Rather loamy grey sand ■• ^ I Cowstones (1st bed)— tough oval concretions of O I sandstone, about 4 ft. long : with many fossils, ^ including Crustacea ... ... ••• ■•• 1 " Brown loamy sand, with clay-galls and Serpula ( FwmicMto'Ja) in lower part Dark blue loam Hard band •" Dark blue micaceous loam with many fossils : nodules of pyrites in lower part Dark blue loam and glauconitic sand Clay with derived Liassic fossils, and small pebbles of quartz, jasper, grit, vesicular trap, &c. ... 5 Disturbed Lias clay (loam containing numerous worm tubes) about 6 The sands are well shown on the borders of the road between Timber Hill and Charmouth, and some of the lower beds appear when seen at a distance almost as white as Chalk. They are surmounted by brown and green sands and chert-beds that may be seen in a pit on the western side of Timber Hill. Mr. Reid's section of the Greensand at Black Yen agrees well with the latest published record, that by Mr. W. D. Lang, who drew special attention to a fossiliferous bed beneath the Cherty division, evidently on the horizon noted by Mr. Eeid. Mr. Lang mentions that Pecten quadrico status and Exogyra conica are by far the commonest shells ; all " are siliceous, many, especially the fiat fragments of Pecten, showing the curious concentric structure peculiar to Beekite."^ This silicification, as in the case of the fossils in the Blackdown Beds, is no doubt due to the decay of overlying cTiert-beds and the transmission by percolating water of soluble silica that replaced the calcareous shells. The evidence here and elsewhere indicates that shells are locally preserved at various horizons in the sandy series. The Rev. W. Downes had previously described " a nest of fragmentary fossils silicified, and altogether resembling very poor Blackdown speci- mens "^ among which he recorded as abundant, Cyprina cuneata and GervilUa rostrata. This bed occurred about 100 feet above the Gault clay. Gault fossils were recorded in 1865 from Lyme Regis by the Geological Survey," but our present knowledge of the formation is due to the labours of C. E. De Ranee, the Rev. W. Downes, Mr. Jukes-Browne and Mr. Lang. From evidence obtained in two exposures on Black Ven Mr. Lang has estimated the full thickness of the Gault (zone of Hop- lites intemiptus) at about 38 feet. It is somewhat thicker at Ware. (See p. 89.) He observed that the basement pebbly bed occurred in pockets, and was impersistent ; and that the junction ' Geol. Mag., 1903, pp. 388-392 ; see also Jukes-Browne, " Cretaceous Rocks of Britain," vol. i. (Hem. Geol. Surv.), 1900, p. 187. ' Quart. Journ. Geol. Soc, xli.. 1885, p. 24. ' Catalogue of Fossils in the Museum of Practical Geology," by T. H. Huxley r.tid R. Etheridge (Mem. Geol. Surv.), 1865, p. 275; also '" Catalogue of Cretaceous Fossils" (Mem. Geol. Surv.), 1878. UPPER GREENSAND AND GAULT. 4< of Lias and Gault appeared in the cliff at a height of about 315 feet above sea-level. He remarked that the pebbly layer and overlying unfossiliferous loamy sand, which he reckoned to be about 14 feet thick, " may represent the zone of Acanthoceras TnaTn-millatum, but there is not a particle of fossil evidence to justify the assertion."^ As remarked by Mr. Jukes-Browne, the pebbly basement-bed of the Gault no doubt gave rise to the sup- position that a representative of the " Carstone " or Lower Greensand occurred at Black Ven.^ In passing westwards from Lyme Regis through the region of landslips, we encounter numerous sections of the Upper Green- sand, notably of the chert-beds and associated beds of sandstone which form the brown and rugged cliffs beneath the Chalk. One of the finest sections may be seen in the great landslip of Bindon and Dowlands, details of which are given by Mr. Jukes- Browne. He mentions that " Lenticular layers of hard water- worn pebbles of glauconitic sandstone mingled with broken Exogyra shells occur at several horizons ' ' ; the pebbles seem to be portions of the harder sandstones " rolled and worn in situ by the action of strong currents on the sea floor."' The Foxmould and Cowstone Beds may be noticed here and there amid the debris of the lower slopes between Lyme Regis and Axmouth. Gault clay was observed by De Ranee at Pinhay ; by Mr. Jukes- Browne in 1895 on the shore in front of Humble Green below Whitlands Cliff, where it occurred as a slipped mass, and also to the west of Culverhole Point, above the Rhaetic Beds. It is in- teresting to note that Conybeare had in 1840 referred to a possible trace of Gault near Culverhole.* Beyond Culverhole the Gault has not been observed westwards along the coast, but, as remarked hj Mr. Jukes-Browne, it is no doubt represented in the lowermost glauconitic sands in the cliffs west of Seaton. There, as he points out, the most complete and accessible section of the Upper Greensand is that of Whitecliff, between Seaton and Beer {see Fig. 27). The Keuper Marl which forms the cliff at Seaton ends abruptly above the little bay called Seaton Hole, and the Greensand is brought in by a fault which strikes nearly north and south. " From this line of fault the dip is south-west at about 7° or 8°, and the component beds of the Greensand are successively brought down to the shore." This classic section was noted in detail in 1825 by Fitton,^ and subsequently by C. J. A. Meyer, and other observers. The Greensand is here conspicuously divided into an upper cherty series, and a lower series of green sands which yield many of the fossils of the Blackdown Beds (zone of Schloenbachia rostrata). 1 Geol. Mag., 1904, p. 131 ; 1907, p. 156. * See Btheridge, Quart. Journ. Geol. Soc, xxxviii., 1882, p. 93, xli., 1885, p. 26. ^ " Cretaceous Rocks of Britain," vol. i. (Mem. Geol. Surv.), 1900, p. 192. ■• On p. 2 (footnote) in the volume of Ten Plates referred to on p. 92. 'i Trans. Geol. Soc, ser. 2, iv., 1836, p. 234. Upper Greensand. 48 CRETACEOUS. Summarized, tlie strata seeu below tlie Chalk at Whitecliff are as follows^ : — Feet. f Nodular calcareous sandstone 8 Grey and yellow sands and sandstones, glauconitic and calcareous, with nodules and masses of chert, and nodules and occasional pebbles of sandstone (Chert Beds) 60 Calcareous sandstone with many fossils 2i Soft grey and greenish grey sands with layers or burrs of calcareous sandstone (Foxmould) ... ... ... 50 Dark greenish sand with Cowstones 15 Gault. Dark greenish and argillaceous sand, about ... ... 20 Here the lowest bed was regarded by Meyer as the equivalent of the Gault clay ; and it is interesting to learn that he observed " near its base a g-rit-bed of minute subangular pebbles, or frag- ments of the underlying rocks. "^ (See p. 46.) The Chert Beds are to be seen at Little Beach below Beer Head, where they attain a thickness, estimated by Mr. Jukes-Browne at about 64 feet; but they contain chert only in the lower part. Further on the Upper Greensand is exposed in the cliffs at Brans- combe, and westwards to the neighbourhood of Sidmouth. Pebbly layers with water-worn sandstone pebbles occur at different horizons in the Chert Beds, also a whitish calcareous sandstone, which forms a conspicuous band in the cliffs at Branscombe and onwards to Dunscombe. At the base of this group there is the same fossil-bed that was observed by Mr. Jukes-Browne at White- cliff. The total thickness of the Greensand is here about 170 feet. The Chert Beds form a fine cliff at the Eempstone Rocks near Dunscombe, where Mr. Jukes-Browne noted that some of the sandstone pebbles were bored by Litliodonnus.^ Silicified examples of Exogyra conica occur in the strata, but the chert is developed mainly in the lower beds. (Fig. 28). Further west in Dunscombe Cliff the lower sandy series includes large doggers and lenticular layers of fine grey calcareous sand- stone, that may represent the Cowstones. Mr. Jukes-Browne notes that the same set of beds can be seen in Salcombe Cliff, where about 100 feet of sands come in below the flint-gravel which caps the hill. In the lower 30 feet of these Meyer found Serpula coiwava, E.fogyra conica, and Cyprina cuneata; and Dr. A. Strahan obtained Trigonia aliformis, Dos- iiiiopsis (Cytherea) caperata and Turritella granulata} Godwin-Austen drew attention to the occurrence of a conglo- meratic bed in the lower part of the Greensand on Salcombe Hill : * the pebbles consist of glauconitic sandstone, due, no doubt, to contemporary erosion. The last prominent cliff' of Upper Greensand is that of Peak Hill, west of Sidmouth, where the thickness, dependent on the 1 Jukes-Browne, " Cretaceous Rocks of Britain," vol. i. {Mem. Geol. Surv.), 1900, pp. 197, 205. 2 Quart. Jouni. Geol. Soc, xxx., 1874, p. 370. ' " Cretaceous Rooks of Britain," vol. i. (Mem. Geol. Suro.), 1900, pp. 202-210. * Trans. Geol. Soc, ser. 2, vi., 1840, p. 449 ; Proc. Geol. Soc, iv., 1876, p. 197 . UPPER GKEENSAND AND GAULT. 49 irregular capping of gravelly beds, was reckoned at from 80 to 100 feet by Mr. Ussher. In the eastern end of this cliff Mr. Jukes- Browne observed the following succession : — Upper Greensand. Keuper. Flint and chert gravel, and disturbed sand... ... about Clean buff sand „ Buffi sand with small irregular siliceous concretions and thin layer of siliceous stone ... ... ... „ Greyish sand with a layer of friable sandy nodular concretions, containing fossils with silicified shells „ Glean light-grey sand weathering yellowish ... 30 to Eed Marl. Feet 20 10 12 10 35 He remarks that " if the sands with siliceous concretions are the same as those seen at Dunscombe cliff the beds below are 20 feet thinner, the sand with large doggers having quite thinned out." Dr. Strahan obtained two of the concretions many years ago, and from them Mr. Jukes-Browne extracted upwards of 60 speci- mens belonging to 28 species, among which C'jicuUcsa glabra and Lucina pisum are the most abundant. In the same horizon at the western end of the hill Meyer found many fossils. The fauna is that of the Blackdown Beds. On Bulverton Hill, near the northern end of the Peak Hill tract of Greensand, and on the western slope, a little south-west of the point known as Salter's Cross, is a sand-pit, from which Dr. Straha-n " obtained a similar assemblage of fossils, but in a less friable condition, and still more like those of Blackdown." The following are among the species determined by Mr. Jukes- Browne^ : — Schloenbachia rostrata (J. Sow.). Hysteroceras varicosum (■/. de C. Sow.). Aporrhais calcarata /. Sow. Natica genti (J. Sow.). Turritella granulata J. de C. Sow. Cardium hillanum J. Sow. Oorbula elegans J. de C. Sov:. Cucullsea carinata {J. Sow.). glabra Park. Exogyra conioa J. de C. Sow. Inoceramus concentricus Park. Lucina pisum J. de C. Sov). Nucula antiquata J. de C. Sow. Nuculana lineata (J. de C. Sow.). Pecten orbicularis J. 8oii\ Trigonia aliformis Parh. scabricola Lijc. Serpula concava {J. Sow.). Inland Sections. With regard to the inland sections it is unnecessary to give many details. It is, however, interesting to find that the Gault extends some miles distant from Lyme Regis , Thus in 1874 Mr. C. Reid observed the following beds in the banks of the stream north of Highgate, about three miles east-south-east of Axminster : — upper I Mottled green and orange sand. TBlue micaceous loamy clay, full of fossils like those in the G-ault. < Gault of Black Yen. (^ Olive-green sand. Lower Lias. Stiff blue clay. The beds were not exposed with sufficient clearness to allow of their being measured, but he estimated the thickness of the Gault clay to be " Cretaceous Rocks of Britain," vol. i. {Mem. Geol. Surv.), 1900, pp. 202-204. 50 mil nil ««5; I O M cq I CO H M & 1-3 o ;zi w ■< tl5 a 53 g cc tn ^ 00 I i 11 i!!,!i S ifi I ! li P ! Jlli lllf..... Ill ;vf;< iiifc liii::;-: iilfoHa llllll-^:;;:! Cc f^ \\ {lllllll •■ III (^ "9 1- ^^ ^;?J «5 t ^m fi& o 52 CRETACEOUS. 10 to 12 feet. The same bed.s are cut through by seveial of the streams which rise in Wyld Warren, and Mr. Reid found the clay was everywhere underlain by a thin bed of green sand. The scarp of Greensand as shown on the map at Cuthays, between Axminster and Hawkchurch, appears to have been carried too low, as the farm is situated on yellow clay, while black earthy and stony soil, and fox- mould occur on the higher slopes. Gault may, however, occur there. Occasional sections of the calcareous sandstone, chert beds, and under- lying sands, with here and there a shelly bed, are met with, between Chardstock and Membury, and again at Dalwood. In the railway-cutting at the eastern end of the Honiton tunnel, north-west of Wilmington, Mr. Ussher in 1874 observed " clayey beds at the base of the Greensand which seem to be referable to the Gault. "^ No fossils were at that time obtained, but the clays were mapped as Gault. It was not until 1886 that the Rev. W. Downes made a careful search in the clays (believing them at first to be Ehsetic)), and he obtained the following fossils, in black marly clay^ : — Actseon affinis /. de C. Siiir. I Mytilus. Exogyra. i Pecten quadricostatus /. Soiv. Inoceramus concentricus Pari: '. Pectunculus. Modiola. I Tellina. Mr. Downes published a section of the tunnel and cuttings from data communicated by the engineer of the railway, and in this the sequence of the strata in the hill was at one point shown as follows : — Feet. Clay with chert ... ... ... ... ... ...)-, Upper rCherty greensand ... ! / Greensand. j^'^^y«^°'^-V - , 81 (^ Yellow sand, very wet 18 !Dark grey marl and black clay (with fossils) ... 6 ^1^"^^^'''^, 44 White sand 1 Rreenish sandy clay ... 10 Keuper. Red Marl. Mr. Jukes-Browne visited the locality in 1897 and published further par- ticulars and a larger diagram-section of the strata proved in the tunnel and cuttings. 3 He drew attention to the fact " that the surface of the Red Marl is uneven, and that the thickness of the dark sandy beds increases from about 37 feet at the eastern end to over 60 feet in the central part, thinning again to 55 feet at the western end." Mr. A. W. Clayden has since referred to these features as affording evidence of the old land surface prior to the Cretaceous overlap, and of the waters of the Gault sea having filled ancient valleys here and there with sediment; an explanation which might to some extent account for the local distribution of the Gault.* ' H. B. Woodward, "Geology of England and Wales," 1876, p. 237. ' Geol. Mag., 1886, p. 309. ' " Cretaceous Rocks of Britain," vol. i. (Mem. Geol. Surv.), 1900, p. 212. * " History of Devonshire Scenery," 1906, p. 125. 53 CHAPTEE VI. CRETACEOUS— coT-^MwetZ. Chalk. In 1826 De la Beehe gave the first particular description of the Chalk near Lyme Regis, and he then divided the formation as follows' : — Feet. Chalk with flints ... ... ... ... ... ... about 150 Chalk without flints 30 or 40 Chalk with quartz-grains ... ... ... 20 or 30 He further noticed the presence in the basement-bed, about ■3 feet thick, of numerous organic remains. The above divisions are those that may be recognized readily in the cliffs, and De la Beche, acting in accordance with the methods of William Smith, marked out the main stratigraphical divisions in the formation, and carefully recorded their fossils. Our knowledge of the succession of the organic remains and of the correlation with beds in other areas has enormously in- creased owing to the painstaking work of C. J. A. Meyer, ^ fol- lowed by that of Dr. Charles Barrois,' Mr. A. J. Jukes-Browne,* and Dr. Arthur W. Rowe.' The zones being divisions based on the occurrence of certain as- semblages of fossils, are naturally independent of the purely strati- graphical divisions. The fossils taken to characterize the several zones are not necessarily confined to these particular stages ; in fact, some of them come in below and range above the limits assigned to a zone. Taken, however, in conjunction with other fossils, and allowing for the natural variations in geographical distribution, the succession of zones in the Middle and Upper Chalk has not only been determined by Dr. Rowe in more detail than had hitherto been attempted, but with an enthusiasm unsur- passed. Anyone wishing to follow his divisions must do so with his paper in hand. Among the noteworthy conclusions arrived at by Dr. Rowe, who was aided by Mr. C. D. Sherborn, is the re- markable variation in the thicknesses of the strata assigned to some of the zones, and especially to that of TerebratuUna. The Chalk was a purely marine formation, for the most part of organic origin, and the strata, as pointed out by Mr. Jukes- Browne, were accumulated generally under deepening conditions, which finally extended to a depth of about 700 fathoms. 1 Trans. Geol. Soc, ser. 2. ii., 1826, p. 110. '' Quart. Joum. Geol. Soc, xxx., 1874, p. 369. ' " Recherches sur le Terrain Cretac6 Superieur," 1876, p. 71. * " Cretaceous Rocks of Britain," ii. and iii. (Mem. Geol. Sun.), 1903-4 ; Jukes-Browne and Hill, Quart. Joum. Geol. Soc, Iii., 1896, p. 99. ' Proc Geol. Assoc, xviii., 1903, p. 1. ■ 54 CRETACEOUS. The following tabular statement and lists of fossils are mainly based on tlie researches of Dr. Rowe and Mr. Jukes-Browne : DIVISIONS OF THE CHALK BETWEEN LYME REGIS AND SIDMOUTH. Chief Stratigraphical Divisions. Zones. Brans- combe and Beer. White- cliff. Pin- hay. Upper J Chalk. ] Chalk with flints. Chalk with flints and phosphatio nodules. Mioraster cor-testudinarium. Holaster planus. Feet. 30 60 Feet. 20-f- 34 Feet. 40 Chalk with flints. Terebratulina. 90 to 156 70 72 Middle Chalk. " Hard and soft nodular chalk, with flints locally in upper part. Beer Stone, and hard quartziferous chalk. Rhynchonella cuvieri. 20 to 80 28 60 Lower Chalk. ■ Calcareous sandstone and arenaceous chalk, with quartz' grains. Holaster subgloho- sus and Ammo- nites (Schloen- bachia) varians. 'Actinocamax ple- nus. Ammonites (Acan- thoceras) man- telli, with sub- zone of Stauronema car- ter! (doubtfully ^ represented). 14 to 80 2 to 3 Lower Chalk. Zone of Schloenhachia varians. Lamna appendiculata Ag. Oxyrhina mantelli Ag. Ptychodus decurrens Ag. Calycoceras navicularis Mant. Mantelliceras mantelli (J. Sow.). Metacanthoplites rotomagensis (Defr.). Schloenbachia coupei {Brongn.). — ^ varians (J. Sov}.). Scaphites aequalis J. Sow. Turrilites morrisi Sliarpe wiesti Sharps Nautilus expansus J. de C. Sow. fleuriausianus d'Orb. largilliertianus d'Orb. Avellana cassis d'Orb. Pleurotomaria cassisiana d'Orb. Cucullsea mailleana d'Orb. Lima ornata d'Orb. Peoten asper Lam. (Neithea) aequicostatus d'Orb. Thracia carinifera d'Orb. Trigonia affinis J. Sow. meyeri Lye. Rhynchonella dimidiata J. Sow. grasiana d'Orb. Terebratella pectita (J. Sow.). Terebratula biplicata J. Soto. semiglobosa J. Sow. Ceriopora ramulosa {Mich.). Catopygus columbarius (Lam.). Discoidea subuculus (Leske). Holaster subglobosus (Leshe). Pseudodiadema ornatum (Gold/.). Salenia petalifera Ag. Zone of Actinocamax plenus. Pseudaspidoceraseuomphalus(S7ia)'^e). Actinocamax plenus Blainv. Scaphites sequalis J. Sow. Avellana cassis d'Orb. Rhynchonella wiesti Quenst. Discoidea cylindrica {Lam.). Galerites subrotundus Mant. CHALK. 55 Middle Chalk. Zone of Rhynchonella cuvieri. Lamna appendiculata Ag. Ptychodus mammillaris Ag. Pachydiscus peramplus (Mant.) Inoceramus mytiloides Mant. Terebratula aemiglobosa J. Sow. Cardiaster cretsiceus Sorig. pygmseus Forbes Cidaris hirudo Sorig. Cyphosoma radiatum Sorig. Discoidea dixoni Forbes Galerites (Echinoconus) castanea (Bi-ongn.). subrotundus Mant. Grlyphocyphus radiatus Hcen. Hemiaster minimus Ag. Salenia granulosa Forbes Pentacrinus agassizi Hag. Serpula avita J. de C. Sovj. Cyphosoma radiatum Sorig. Discoidea dixoni Forbes Galerites subrotundus Mant. Hemiaster minimus Ag. Holaster planus {Mant.). Micraster cor-bovis Forbes Pentacrinus. Zone of Terebratulina. Lamna appendiculata Ag. Pachydiscus peramplus {Mant.). Inoceramus lamarcki Park. Spondylus spinosus J. Sow. Rhynchonella cuvieri d'Orb. Terebratulina. Cardiaster cretaceus Sorig. Cidaris hirudo Sorig. Mr. E. T. Newton has explained that the so-called " Terebratulina gracilis-zone " could no longer be called by that name, because the small Brachiopod there found was not the true Terehratulina gracilis, but another form; the true T. gracilis only having been met with in the higher beds of the Chalk at Trimmingham, in Norfolk. The TerebratnJina found in the Middle Chalk seemed to be the form named Ter. lata by Etheridge, but this required further examination. It was best, for the present, therefore, to call this zone of the Middle Chalk simply the " TereJiratidijM-zone."'^ Upper Chalk. Zone of Holaster planus. Pleurotomaria perspectiva Mant. Solariella gemmata {J. de C. Sow.). Inoceramus brongniarti .7. de C. Son:. Plicatula barroisi Peron Spondylus spinosus J. Sow. Terebratula carnea J. Sow. semiglobosa /. Sow. Rhynchonella plicatilis J. Sow. reedensis Eih. Eschara acis d'Orb. Cardiaster cotteauanus d'Orb. Cidaris serrifera Forbes Cyphosoma radiatum Sorig. Echinocorys scutatus Lesl-c Holaster placenta Ag. planus {Maut.). Micraster leskei Desm. (M. breviporus Ag.). praecursor Rowe (Special group form).^ Pentacrinus. Serpula ilium J. de C. Sow. Ptychodus mammillaris Ag. Plicatula barroisi Peron Terebratula carnea J. Sow. semiglobosa J. Sow. Terebratulina striata Wahl. Rhynchonella reedensis Etli. Cardiaster cotteauanus d'Orb Zone of Micraster cor-testudinarium. Cidaris serrifera Forbes Echinocorys scutatus Leshe Holaster placenta Ag. Micraster prEecursor Rowe (Special group form).' Serpula ilium J. de C. Sow. Mr. Jukes-Browne has remarked tliat the zones of Micraster cor-anguinum and Marsupites testudinavius " originally extended over Devonshire, is proved both by the flints and flint fossils which are found in the gravels capping the higher plateaux. ' Proc. Geol. Assoc, xix., 1906, p. 337. « See " Analysis of the Genus Micraster," by Dr. A. W. Rowe, Quart. Journ, Geol. Soc, Iv., 1899, p. 494. 56 CRETACEOUS, These include casts of Micraster cor-anguinum, of Galerites alhogalerus, and of ilfarswprfe.s-plates, and the flints are of three sorts, some cavernous with branching cavities enclosing remains of Dory derma ramosum ; some solid and translucent with a milky- white band near the periphery, and thirdly flints which are solid and light grey throughout." Coast Sections. The Chalk is exposed between Lyme Eegis and Axmouth, in cliffs named for the most part according to the adjacent home- steads : thus proceeding westwards there are the Ware (400 feet), Pinhay (500) west of Pinhay Bay, Whitlands and Charton (500) west of Whitlands ravine, Eousdon (480), Dowlands (400), Bindon, and Haven Cliffs (300 and more). The Upper Chalk occurs in the clifEs from Ware to Pinhay, at Whitecliff and Beer Head. As remarked by Mr. G. W. Young, " The first available ex- posures of Chalk, the Pinhay Cliff and Chapel Eock, are situated in the grounds of Pinhay (formerly known as Clevelands).'" Permission is therefore required to examine the sections. The higher portion of the cliff is formed of hard nodular chalk with flints belonging to the zone of Micraster cor-testudinarium ; below comes the zone of Holaster planus, yellowish nodular chalk, reckoned by Mr. Jukes-Browne to be about 40 feet thick, and to include in the lower 14 feet, nodular rocky chalk with brown phos- phatic matter that is equivalent to the Chalk Rock. The Middle Chalk is seen in the Ware and Pinhay Cliffs and onwards to the Haven Cliffs. The Terehratulina zone is well seen at Pinhay, and below the Whitlands Coastguard Station ; thence it forms the summit of the cliffs to the neigh- bourhood of Dowlands, and the basement portions have been observed by Dr. Rowe further west in the Haven Cliffs. In a quarry by the old lime-kiln north of Haven Cliff, Dr. Rowe obtained Inoceramus mytiloides, Shynchonella cuvieri, Terehratula semiglobosa, Holaster planus, and other fossils, which he regards as belonging to the base of the above zone.^ The Bhynchonella cuvieri zone can be examined at intervals from Pinhay to the clijfs at the Bindon landslip, where it is well exposed : it occurs also in Haven Cliff. The Lower Chalk consists very largely of chalk with quartz grains, green-coated nodules and a few phosphatic nodules. It belongs in the main to the zone of the Ammonite Mantelliceras mantelli, including at its base in some places, as at Beer Head, a band a foot or two in thickness, which may represent the Chloritic Marl, or sub-zone of Stauronema carteri, although at present that species has not been discovered in the district. Locally the Lower Chalk also includes in its upper part, the Belemnite Marl or siib- zone of Actinocaw,ax plenus, a band that does not exceed 2 feet in thickness. The Lower Chalk has been exposed at intervals along the lower cliffs from Pinhay westwards, but there is evidence of considerable irregularity and overlap. Thus Mr. Jukes-Browne finds that above Charton Bay the band 1 Proc. Geol. Assoc., xix., 1906, p. 335. ^ Ibid, xviij,, 1.903, p. 11. CHALK. 57 of Actinocamax plenus rests directly on a phosphatised surface of Upper Greensand, while a little further west and for a short distance only, the Lower Chalk is absent and the Middle Chalk rests, with a glauoonitic base- ment-bed, on the Upper Greensand. There is, moreover, evidence of local erosion and reconstruction in the beds themselves, the top band (zone of Act. plenus) containing casts of phosphatised fossils. Taken as a whole, Mr. Jukes-Browne and Mr. W. Hill find a strong Chalk-marl element in the fauna, and a large proportion of species that occur in the Cenomanian of Western France.^ The Lower Chalk appears to attain its greatest thickness in the district at Wilmington, where it is probably more than 40 feet. (See p. 61.) From a quarry near the Coastguard Station on Haven Cliff the following species, collected during an excursion of the Geologists' Association, were identified by Mr. E. T. Newton^: — Galycoceras navicularis (Mant.). Mantelliceras mantelli (J. Sow.). Metacanthoplites rotomagensis (Defr.). Nautilus. Exogyra. Pecten asper Lam. (Neithea) quinquecostatus J. Sow. Lima hoperi (./. Sow.). Rhynchonella dimidiata (J. Sow.). Disooidea subuculus {Leske). In the grand headland at WhiteclifE, between Seaton and Beer, a fine sequence of Chalk may be observed. In the bluff known as Annis' Knob (see Fig. 29) the Upper Chalk may be conveniently studied. Here the formation is remarkably nodular, the nodules being some of flint with thick white siliceous crust and a tiny nucleus of black flint, while a large number are composed of more or less siliceous chalk. A prominent band of black flints near the middle of the bluff was taken by Mr. Jukes-Browne as a con- venient divisional plane between the zones of Micraster cor-testu- dinariuin and Holaster planus, but Dr. Rowe takes the limit 10 feet higher. At a lower level in the cliff which forms the northern side of Beer Harbour {see Fig. 29), the best section in Devon of the Middle Chalk is exposed. The upper part belongs to the zone of Terebratulina, about 90 feet ; and the lower part bordering the shingle beach, about 30 or 40 feet, to the zone of Rhynchonella cuvieri. In this latter zone, which extends to the natural arch- way further east, is included the representative of the Beer Stone, noted by Mr. Jukes-Browne as consisting of two layers of some- what nodular chalk about 5 feet thick. Reefs of the Lower Chalk a few feet thick occur beneath, resting on a floor of Upper Greensand. The large quarries to the west of Beer exhibit fine sections of the two zones of the Middle Chalk. (See p. 82.) The Beer Stone yields few fossils, fortunately for its reputation as a free- stone; they include Nautilus, Inoccramus mytiloides, Bhynchonella cuvieri, Terehratula semiglohosa, Galerites svhrotvndus, Ptychodus mammillaris, and Lamna appendiculata, identified by Mr. E. T. Newton.' In other quarries north-west of Beer, about 20 or 30 feet of Upper Chalk was seen above nearly 60 feet of Middle Chalk, zone of Terehratulina. On approaching Beer Head, the Lower Chalk, as observed by Mr. Jukes-Browne, thickens considerably, the upper part of the ' "Cretaceous Rocks of Britain," vol. ii. (Mem. Geol. Surv.), 1903, pp. 125, 131, 132, 434 ; Quart. Journ. Geol. Sac., lii., 1896, p. 99. 2 Proc. Geol. Assoc, xvi., 1899, p. 138. ^ Ibid. p. 140. 58 CRETACEOUS. zone of Mantelliceras mantdli remaining fairly constant and from IJ to 2 feet thick, while the lower part increases to 12 feet. The bed attains a thickness of nearly 30 feet at Hooken Cliff, but the sub-zone of Actinocamax plenus appears (only locally) to be represented by about 6 feet of glauconitic sand which merges upwards into the hard nodular Middle Chalk. The hard chalk of the zone of Rhynchonella cuvieri forms the buttresses of the caves near Pounds Pool on the eastern side of Beer Head, and the beds appear in the Pinnacles below Hooken Cliff, a part of the landslip of 1790. The zone of Terehratidina CHALK. 59 occurs towards the. upper part of the cliffs at Beer Head and ex- tends westwards ; and there is about 50 feet of Upper Chalk pre- sent, being the last portion of this division that is seen on the coast. West of Hooken Cliff there is the remarkable overlap of the Chalk with Flints, to which attention was directed in 1871 by Mr. Whitaker.^ The chalk of the Terehratvlina zone, as pointed out by Mr. Jukes-Browne, overlaps the rough nodular chalk of the Rhynchonella cuvieri zone and rests on a thin representative of the Lower Chalk. The Lower Chalk, variable as before, is seen on the western side of Branscombe Valley, and above it about 25 feet of the zone of Rhynchonella cuvieri reappears, and this zone becomes thicker as it is traced further west.'' As pointed out by Mr. Jukes-Browne, the lower beds of the Terehratulina zone appear west of Branscombe Mouth, more than a mile from the Coastguard Station. They consist of soft white chalk with frequent flints, both scattered and in layers, and in no place are more than 30 feet thick. They, are covered and deeply trenched by hollows filled with chert gravel, and clay with flints. Beyond Berry Cliff no Chalk higher than the zone of Rhyncho- nella cuvieri has been seen. Along this portion of the cliffs the Chalk is rarely accessible, but at the Kempstone Rocks the Lower Chalk (calcareous grit and shelly limestone) may be examined, and the beds were ex- posed in an old quarry east of Dunscombe Farm, where squared blocks of shelly limestone have been used for building-stone. At the eastern end of Higher Dunscombe Cliff the junction of the Middle and Lower Chalk can be seen, and the Lower beds, 4 or 5 feet thick, were exposed above massive calcareous sand- stone, in an old quarry. This is the most westerly tract of Chalk in England, and it includes about 10 feet of nodular chalk belong- ing to the zone of Rhynchonella ouvieri? (See Fig. 28, p. 50.) Inland Sections. Inland the Lower and Middle Chalk are found in the faulted tract between Offwell and Widworthy east of Honiton, there partially concealed beneath a covering of clay with flints and chert; and they occur also at Membury and to the north-east of Chardstock. On the colour-printed map the boundary-line for the " Clay with flints and Chert " above Sutton quarry has unfortunately been omitted, and the exposed chalk in consequence has been coloured with the superficial drift. Elsewhere the Lower Chalk, where at the surface in the adjacent valley and at Wilmington, has not been distinguished by tint from the Green- sand. The following notes on the Lower and Middle Chalk of Wilmington and Widworthy are by Mr. Jukes-Browne.* ' Quart. Journ. Geol. Soc, xxvii., 1871, p. 97. ^ Jukes-Browne, " Cretaceous Rocks of Britain,'' vol. ii., {Mem. Geol. Surv.), 1903-4, pp. .134, 140, 436, 440, &c., vol. iii., pp. 129, &c. ' " Cretaceous Rocks of Britain," vol. ii., (Mem. Geol. Surv.), 1903, pp. 142, 143, 444, 448. * Jukes-Browne, Quart. Journ. Geol. Soc., liv., 1898, p. 339 ; and " Cretaceous Rocks of Britain," vol. ii,, (Mem. Geol. Surv.), 1903, pp. 126, 4,30, J8821 E 60 CRETACEOUS. The occurrence of hard calcareous sandstone, locally known as " grizzle," was mentioned by Fitton, who observed that " In a large pit or quarry at the bottom of the chalk, near Sutton and Widworthy, a stone, called Grizzle by the quarrymen, is dug in the situation of the firestone [of Surrey]. The '^^Cenomaniari Sands b^j-BC^w Greenland ^ 1 flTg w Jtcct Mart ^ Position b/ Pits ^ Quarri^ Fig. 30. — Map of the country near Honiton and Wilmington, By A. J. Jukes-Browne.^ Scale one inch to a mile. beds are altogether about 5 feet in thickness." He further noted that the grizzle contains green particles, and does not burn to lime.^ Good speci- mens of Inoceramus striatvs can be obtained from the exposures now open at Wilmington, to the north of the old Sutton quarries. At Wilmington there are two sand pits opened in the zone of Blantel- liceras mantelli, for though the rook is a hard calcareous grit when covered by some thickness of Chalk, it is otherwise where it crops out to the surface, Fig. 31, — Sketch of Quarry north-east of Wilmington. (A. J. J-B.) being so decalcified and decomposed that most of it can be easily removed by pick and shovel. The coarse sand so obtained is valued for rough- casting, and for other purposes. • From Quart. Journ. Geol. Soc, liv., 1898, p. 240. The Turonian in the map represents the Middle Chalk, and the Cenomanian the Lower Chalk ■- Trans. Geol Snc, ser. 2, iv., 1836, p. 234, CHALK. 61 The pit in a field to the north-east of Wilmington, near the lane to Hayne Farm, shows the junction of the calcareous sandstone with the over- lying Middle Chalk, and the following succession was observed in 1897: — Vegetable soil and flints. Ft. In. •5. Soft bedded white chalk, up to 2 6 4. Rubbly glauconitic chalk with scattered quartz Middle grains, and a layer of very hard chalk with Chalk. green-coated nodules at the top, Innceramua my- tiloides ... 2 6 ^ 3. Soft glauconitic marly chalk 9 ' 2. Hard glauconitic and quartziferous limestone, with worn and phosphatised surface at top, but the Lower base not well marked ; some fossils ; about ... 2 Chalk, j 1. Rough yellowish calcareous sandstone with many I fossils ; weathering into sand with lumps and blocks of sandstone 6 The above measurement was taken on the downthrow side of the fault, shown in Fig. 31 : the throw cannot be more than 9 or 10 feet. The other quarry is on the south side of the road at the western end of Wilmington. The face of this quarry is over 30 feet deep, but does not show the base of the calcareous sand. In the soil at the top are loose lumps of the quartziferous limestone and large blocks of hard calcareous sandstone (grizzle) ; below these are 3 or 4 feet of soft sandstone, with harder lumpy portions, and in this part fossils are very abundant. The rest of the sand contains only a few fossils, and it cuts with an even face, being chopped out with the broad end of a pick. It is traversed by three layers of siliceous concretionSj the highest consisting of large flattish or lenticular masses, white or pink outside, and containing u nucleus of brown chalcedonic chert. The lower layers are of small irregular concre- tions. They contain sponge spicules, and seem to be sponges more or less filled with sand and cemented by chalcedonic silica. AVishing, if possible, to find the base of this sand, we had a hole dug in the floor of the quarry, but at a depth of about 12 inches the workman reached a hard rocky sandstone, with large sand grains and some small pebbles, the whole being indurated and compacted by a hard stalagmitic kind of calcic carbonate. The workman stated that a hole had been dug in the orchard outside the pit, traversing 6 or 7 feet of such lock without reaching its base. The total thickness of this calcareous sandstone seems, therefore, to be about 40 feet. Pebbles also occur occasionally in the mass of the sand. Most of them consist of rough vein-quartz, and one measured about I5 x 1 x IJ inches ; another is a flat pebble of a greenish micaceous sandstone 2 J inches long. [Mr. Jukes-Browne records a long list of fossils obtained mostly from the Lower Chalk (zone of Mantelliceras mantelli) at Wilmington.] There are some old chalk quarries in the park east of Widworthy Court, and Mr. A. Marwood Elton, of the Court, informed us that freestone was quarried from them as well as from the Sutton quarries half a mile further south. This freestone is a bed in the lowest part of the Middle Chalk, and is apparently identical in character and position with that occurring at Beer, near the coast, and known as Beer Stone. It consists principally of small fragments of shell set in a chalky matrix, and cemented by calcite into a hard, gritty stone, which cuts freely in any direction when freshly quarried. Dr. G. J. Hinde kindly made slides from samples of the Beer Stone and Sutton Stone sent to him, and informed us that the two stones have the same microscopic structure. No exposure of the freestone was visible at Widworthy in 1897, but a mason (Mr. D. Hooper) who had worked in the large Sutton quarries stated that the succession of beds there was as follows : — Feet. Flint rubble at the top 4-6 Soft white chalk 10-30 Hard chalk about 20 Freestone ■•■ ■•■ ,, 5 Soft chalk with green grains ,, 5 Hard cockly chalk ,, 2 Grizzle at the bottom (see p. 60). 18821 E 2 62 CRETACEOUS. A foot of two of the soft white chalk which could be seen near the top of the quarry above the limekiln, had the character of the chalk of the Tere- bratulina zone. We had the talus cleared away from the lowest face of the quarry by the side of the limekiln, and disclosed about 18 feet of rather hard chalk, lumpy in places and containing Inoceramiis mytiloides, mostly as broken shells; this evidently belonged to the zone of Bhynchonella cuvieri, and in another part of the quarry, from similar chalk, Mr. John Rhodes obtained that species with Innceramus mytiloides. The base of this hard chalk was not reached, as a large block of inferior freestone, a hard, shelly chalk, lay below ; but this and the better freestone were probably in place near by. There are several quarries in the Membury outlier, and as the Middle Chalk comes in as well as the Lower, the locality is an interesting one. The numerous faults make it difficult to estimate thicknesses, but that of the Lower Chalk was judged to be about 50 or 60 feet. At the time of our visit in 1892 the church was being restored, and the chalk thrown out from the foundations was a peculiar soft grey granular chalk. This is about 60 feet below the level of an exposure of Melbourn Rock in the lane to the west. North of the village there is a series of old chalk quarries; the first of these by the lane leading to Furley is in Middle Chalk, but all the others appear to be in Lower Chalk. In the lane west of the church and in the bank of a little garden, hard nodular chalk, like Melbourn Rock, was seen, and just beyond is a quarry in the Middle Chalk containing Shynchonella cuvieri, Terebratula semi- globosa, and many fragments of Inoceramus. By the next lane running north-west toward Furley there is an old quarry, at the top of which a few feet of rubbly chalk was exposed, contain- ing Inoceramus mytiloides and Bhynchonella- cuvieri. The quarries at Chardstock, three miles south-west of Chard, are now abandoned and overgrown. There is, however, a small exposure in a quarry half a mile north of Tytherleigh and east of the old quarries. A. J. J.-B. On Storridge Hill, north-east of Chardstock, the following section was noted in 1874 by H. B. Woodward : — ( Even-bedded white chalk, passing down into chalk with Lower 3 glauconite and quartz grains. Chalk, "j Nodular bed full of fossils, Nautilus and many echino- ^ 10 ( derms (" Chloritic Marl "). feet. Upper / Sandy beds, green at top. Grreensand. \ Chert beds. The nodular fossil-bed was also observed by Mr. Reid in the road leading to Brimscombe Farm, west of Chardstock Church. This fossil-bed, known in the Chard district as the Chloritic Marl, is regarded by Mr. Jukes- Browne " as u, condensed representative of the lower part of the Chalk Marl." 63 CHAPTEE VII. FAULTS. We may uow draw atteutiou to the principal faults tliat have affected the strata, aud although some of them displace the Plateau Deposits, yet a consideration of the later dislocations may he appropriate hefore we describe those mixed accumulations on the uplands. The faults in the area may be divided into three classes. (1) Those that cannot be proved to affect the Cretaceous rocks. (2) Those that affect the Cretaceous rocks without interfering with the Tertiary plain or table-land surface. (3) Those that affect the level of the Cretaceous plain and the continuity of the Plateau Deposits of Clay with flints and chert. The first class includes the faults which displace the New Red subdivisions in districts from which the Cretaceous rocks have been entirely denuded. These faults run in different directions along a general north and south zone of dislocation, which extends for 15 miles, from Stowford in sheet 325, by Payhembury and CoUiton to Uffculm. The general tendency is equivalent to a great north and south fault throwing the higher beds down on the east, in places to the extent of 300 feet or more. Of the second class, the fault east of Offwell, which throws down Chalk on the west, with a displacement of 200 feet or more, with- out affecting the level of the tableland, is the most notable example. (See pp. 59-61.) The third class, as will be seen by the accompanying sections, is well represented. The most westerly example is furnished, near Combe House, south-east of Gittisham, by a north and south fault with a downthrow to the west of between two and three hundred feet, bringing clay with flints and underlying Greensand in contact with Keuper Marls. Followed southward it appears to cut off Greensand against clay with flints at Wolvers- leigh Farm and cannot be traced further. The most important fault of this class is the dislocation which, running irregularly northward from Northleigh by Widworthy, throws down the Greensand and clay with flints on the west against Keuper Marls on the east, lowering the summit of the tableland 200 feet or more in places. This fault may have shifted the dislocation that lets down the Chalk, and coalesces with it at Slade. If so, its shifted prolongation may have cut off the small patch of Greensand east of Northleigh, on the west. The fault which brings the Keuper Marls of Dalwood and Shute against clay with flints and Greensand, has a westerly downthrow of from 100 to 200 feet. The section near the northern margin of the map exhibits examples of the three classes of faults, and of the great effect the faults of the third class have had in dislocating the Tertiary plain, and so influencing the direction of the drainage systems, and affording facilities for fluviatile denudation. (Figs. 33 and 34.) FAULTS. i-t u ^ u .CO .B ^- . 3 ^ ■§r3 c >2 FAULTS, 65 De la Beclie drew attention to the prevalence in the eastern part of the district and in that to the north, of faults taking a northerly and southerly direction; and he pointed out how, in certain instances, the valleys had originated along the lines of dislocation. As he remarked, some of the faults which traverse the valleys extend also through the uplands, and the influence which they exerted would appear to be local rather than general, for they only in places coincide with the present main lines of drainage. W 6 M a o =« ai Hi o O .=^ 3 o C3 I to :§ !«■■ "^i m H\i ^i \fiA ^W:M ■m -InfiVJ -< ''>» I S: !^ t^ Si Ji ^ M Em Q"* Tratia. Geol. Sue, ser. 2, vol. vi., 1840, p. 448. PLATEAU DEPOSITS. 71 of red and greenish-grey sand. Several shallow pipes close by were filled with sand only. The following is the section : — Fig. 37. — Section of " Pipe " in Greensand on Salcombe Hill. (W. A. E. U.) te 33EnEn CXSI^a: •CEaCEPC:^; Wi ,^ti^!<>^5A;■^(^fe»M■tf^»iat^d^ m-mwM:^ Ft. In. 10 Greenish-grey sand, with hard nodu- lar bands of fine whitish calcareous sandstone. 2 Hard whitish calcareous sandstone. 2 Orange-stained sand. - 6 Fossiliferous band with pisolitic iron-ore grains. 1 6 Grey sand with few iron-shot grains. - 6 Sand full of fragments of Ostrea. 1 6 Grey compact sand. 1 2 Hard rubbly nodular fossiliferous sandstone. 2 Compact greenish-grey sand. The materials in the pipe consist of : — X. Brown clay with broken unworn chalk flints; y. Brown sand; z. Red and greenish sand. On Peak Hill many excavations have been made, the accu- mulation consisting of clay, and reddish sandy loam with pockets of greenish grey sand, angular fragments of flint and chert, broken unworn flints, with occasional large boulders of flint-breccia and worn blocks of coarse brown grit (grey wethers). Some portions of this mixed accumulation near Lyme Regis are simply disintegrated masses of the bands of chert and sands belonging to the Upper Greensand, which have slipped from higher levels. Indeed the upper slopes of Shapwick Hill on the borders of the railway, north of Combpyne station ; the slopes of Penn and Thistle Hills, two miles north of Lyme Regis; and numerous other localities, are covered with angular chert-detritus or " run of the hill." Elsewhere the clay with flints and chert is not uncommonly exposed to a depth of 20 or 30 feet at the heads of the small valleys or goyles. Thence by various stages we pass downwards from the more or less rolled, into the definitely rolled, detritus due to the action of the present streams and rivers. To sum up. Between the original plateau drifts and the present valley deposits, there is a break marked by some earth- movements accompanied by faulting ; but the distinction between the accumulations is largely effaced by the effects of down- washes and slips that have occiirred at various periods. 72 CHAPTEE IX. VALLEY DEPOSITS. Ottee Valley. Along the valley of the Otter there are considerable tracts of valley gravel whicli descend from an elevation of upwards of 400 feet above Honiton, to 142 feet near the mouth of the river on the headland of Otterton. Where the gravels rest on the Triassic Pebble-beds it is not always easy to discriminate between them; although the gravels as a rule are paler in colour and their sandy matrix is less pure. As they are traced eastwards from the area of Straightway Head (in Sheet 325)^ and come to rest on the Upper Sandstone, the pebbles from the older rocks are associated with chert stones and no difficulty arises. The gravel occurs on various divisions of the ISTew Red rocks in the area of our present map, and it consists of the hard Budleigh Salterton pebbles and chert stones in a clayey, loamy, or sandy matrix. The thickness varies from a few feet to 12 or more feet. Newton Poppleford takes its name from the pebbles or " popples " derived from the old Pebble-bed that are found along the course of the river. The washing or re-assortment of Pebble-bed materials in the direction of their dip-slope eastward, and the commingling of stones of Cretaceous derivation in that direction, is just what we should expect to have taken place at a time when the Pebble- bed escarpment was continuous, and the Cretaceous rocks of Blackdown extended somewhat further than their present limits. It is indeed impossible to say to what extent the removal of the Pebble-beds from their escarpment, and the consequent alterations in drainage sources, may have affected the present watershed boundary between the basins of the Clyst, Culm, and Otter ; but it is highly probable that the Tale (the chief tributary of the Otter) may have been formerly of more importance than the Otter above their confluence. In any case, although they may in part date to an old line of drainage, there is nothing in the appearance of these gravels, or in their position and surroundings, to connect them with Tertiary deposition, and they may be classed with the deposits of the Otter Valley as a higher terrace. This view is borne out by the mode of occurrence of the old Otter Gravels. A well-marked lower terrace slopes toward the Alluvium from about 50 feet above it, between Fairmile and Salston House. The gravel terrace between the Otter and the Tale rises to 50 feet or more above the Alluvium. A chain of gravel patches at heights of 100 feet or more above the Alluvium seems to show the continuation of the higher terraces southward to the coast near the mouth of the Otter. The gravel patches at and near Honiton formed part of a continuous terrace which, in the town itself, seems to have been partly mixed with a slip from the Green sand. Owing to rainwash it was often difficult to separate these patches from a lower gravel terrace bordering the Alluvium ; and at Monkton Barton, and at Hamlet south-west of Honiton, the higher ' Ussher, "The Country around Exeter" {Mem. Geol. Snri\), 1902, p. 50. VALLEY DEPOSITS. 73 and lower gravels cannot be separated. The gravel patches between Ottery St. Mary and Tipton St. John's, in addition to worn and angular chert stones in brown loamy sand, contain pebbles of quartz, quartzite, and grit derived from the Pebble-beds. The gravel patch which partly conceals the Keuper Marl outlier near Otterton, and the larger patch to the south which caps the cliffs up to the 200 foot contour line, are composed of worn chert stones. The larger patch is 12 feet or more in thickness, in places. These Otterton gravels are probably the oldest traces of Pleistocene fluviatile deposition in the area, and carry us back to a, time when the coast line was some miles seaward of its present position. The Alluvium of the Otter and Tale consists of reddish-brown loam and grey and brown clay, with subangular and rounded chert stones and Triassic pebbles. The mouth of the Otter valley is flat alluvial land, completely covered in times of flood. It is barred from the sea by a pebble beach about 15 feet above high water at top; through this the river has made an outlet by Otterton Point. Sid Valley. The Sid deserves the title " river " only through having given names to Sidmouth, Sidford, and Sidbury. Its sources are in the Upper Green- sand, near Wolversleigh farm, about 6 miles from its mouth. Except during, or after, heavy rains the stream filters through the beach across its mouth.i At the bridge where the road to Salcombe crosses it. Upper Sandstones were exposed in the bed of the Sid in 1875. The late P. O. Hutchinson then informed us that two or three years previously the river bed contained from 2 to 3 feet of gravel, which was swept away, during a severe storm, by floods which nearly undermined the Coastguard Station, owing to the excavation of a new channel by the stream through the shingle at its mouth. The gravel patches near the base of the Greensand, near Mincombe farm ; east of Sidbury ; near Buckley farm ; at, and north of, Harcombe; east of Griggs; east of Burscombe; and at Core Hill House, are all the results of rainwash from above, which at Sidbury and near Burscombe may mask, or partly obscure, terrace gravels. At Sandecombe farm the patch coloured as gravel, is a landslip of Greensand and clay with flints, making subsidiary features. A slipped mass of Greensand, not shown on the map, forms a small hill feature below the wood (Core Copse) north of Path Hill and south-west of Plyford farm. At Sidford and east of Woolbrook the valley gravel of the Sid is bounded by gentle slopes, probably composed of redeposited materials, which (the evidence being deemed in- sufficient) are not indicated on the map. At the foot of Trow Hill east of Sidford, the gravel makes a low terrace sloping toward the stream. It was exposed to a depth of four and a half feet in a pit section, and con- sisted of broken flint and chert stones and subangular pieces of hard greensand (rag) in brown sand and loam. At Sidmouth the river gravel consists of angular and subangular flint and chert stones with occasional seams of brown loam, and it appears to be banked against a low terrace of redeposited marl and loam. In 1881 P. O. Hutchinson found a portion of the antler of a stag about 9 inches in length, in clean red sand and loam in " Back Fort Field, Sidmouth." A well was sunk at " Old Chancel," formerly Mr. Hutchinson's house, which save the following descending section : — * Ft. In. Loam passing into clay ... 4 Coarse subangular chert gravel in clay 5 Fine gravel ... ... - 9 Coarse gravel with a very little clay in the upper part ... 2 Thin seam of peat or mould ... - 2 Gravel (without clay, stones subangular,) in which water ' See P. O. Hutchinson, " Guide to Sidmouth," 1875, pp. 20-22. 74 VALLEY DEPOSITS. Teeth of Mammoth (Elephas primigenius) were found in the , bed of the Sid half a mile from its mouth ; two teeth of Mammoth were also found in clay under Sidmouth beach by Hutchinson, who presented them to the Exeter Museum. Godwin-Austen^ stated that in all the South Devon valleys, from the Exe to Lyme Eegis, tusks, bones, and teeth of elephant and rhinoceros were furnished by gravels and sands, horizontally arranged in low situations ; and they proved, in his opinion, that the excavation of the valleys to their present depth took place before the occupation of the country by those animals. The probability of the remains of the extinct mammalia having been derived from older gravels or ancient screes, and incor- porated in more recent deposits as the excavation of the valleys proceeded, especially in the Sid valley, is much too strong, how- ever, to be overlooked. The valleys of Salcombe Mouth, Weston Mouth, Branscombe, and Beer may formerly, when the coast line extended seaward, have been drained by tributaries of the Sid in the two former, and of the Axe in the latter cases. The stream-gorge at Weston Mouth showed 30 to 40 feet of clay with broken flint and chert stones. This is evidently debris from clay with flints carried down the steep slopes of the valley, the friable Greensand having been washed away. Hutchinson noted traces of submerged vegetation after heavy gales on the foreshore at Sidmouth, opposite the Fort field on the west of the river mouth. Stumps of trees (apparently recent) were found at 8 feet below high water mark. The rapid wear of the coast before the construction of the sea-wall might be held sufficient to account for this without invoking change of level, but the presence of blue clay under the shingle beach (at about high water mark) renders it probable that there are here proofs of tree-growth at the mouth of tlie Sid valley. On this blue clay Mammoth teeth were found, derived no doubt from older gravels. Hutchinson gave reasons for believing that subsidence was taking place on this coast at the rate of about 10 inches in 100 years.' This, however, is very questionable.' Axe Vai.ley. The eastern part of the area is drained mainly by the river Axe and its tributaries. This river rises in the Dorsetshire Downs near Axnoller farms, between Cheddington and Beaminster. It enters the area a little south of Chard Junction, and follows a meandering course along an alluvial tract that extends in a fairly direct line to the south-west. It is joined on the right by the Yarty, which also follows a very direct course, and by the Coly with its tribiitary the Umborne Brook. Erom the bordering heights of Hawkchurch and other places, fine views of the valley are to be obtained, and the spectator is impressed with the extent of the erosion. ' Trans. Geol. Soc, ser. 2, vol. vi., 1840, p. 443. " Trans. Devon Assoc, vi., 1873, p. 232 ; and Rep. Brit. Assoc, for 1885, p. 422, ' See Report Roy. Oomm. on Coast Erosion, vol. i. 1907, p. 125, VALLKY DBP08IT8. 75 The slopes of these steep hills are strewn with detritus from the plateau-drifts and from the scarps of cherty rocks, and this angular detritus passes in places insensibly into the rolled material of the river gravels. ' The term valley gravel is therefore appropriately employed for all the accumulations in the valley that could be readily mapped, but it must be borne in mind that over a considerable portion of the area the soil is exceedingly stony. The principal tracts of valley gravel occur near the junctions of the tributaries, as noticeable in the neighbourhood of Colytou and Kilmington, at Wadbrook and Broom north-west of Hawk- church. The gravel descends from an elevation of about 300 feet at Kilmington and 200 feet at Broom to 100 feet near Seaton. Mr. Reid noted a pit half a mile to the west of Chard Junction, where 10 feet of sand was seen resting on the Lower Lias clay : it was then used in the brick-works. Between Broadbridge and Westford farms (Higher Bathams on the old series map) 50 or 60 feet of gravel was proved in a well. This thickness is not surprising, as a little further south in the great ballast pit of Broom north of Wadbrook in the parish of Hawkchurch, gravel and sand have been worlied to a depth of more than 35 feet, and have been proved to a further depth of 10 feet without reaching the base. The gravel is worked to near the water-level. It includes loamy and clayey layers, with lenticular seams of grey and brown sand, and consists chiefly of Greensand chert, flint, and quartz, with occasional dark grit and black chert. Dr. A. E. Salter noted pebbles of schorl-rook.' From this pit Mr. W. S. M. D'TJrban', then Curator of the Exeter Museum, obtained, in 1877, a fine series of PalEeolithic Implements made from the Greensand chert.'' Dr. Salter observes that " Roughly shaped chert implements are abundant, mostly in the bottom layers," but we were not successful in finding any examples during the progress of the Geological Survey, nor on a subsequent visit. In a shallow cutting by the main line of railway near Axminster station, valley gravel was seen to rest irregularly on the Keuper Marl. The gravel consists for the most part of rough flint and chert stones, with pebbles of quartz and dark grit. Stones occur some way down in the Keuper Marl, having probably descended through cracks formed in dry weather ; but here and farther along the branch railway to Lyme Regis, there are evidences of considerable soil-movements and small landslips which have led to the inoor^ poration of gravel with Ved marl . Thus by the orchard south-west of Shools Farm there was an interesting section of the valley drift, a good deal disturbed, and showing gravel with patches and bands of red Keuper Marl, which in the re-arranged condition showed little or no variegation. (Fig. 38.) Below the railway by Abbey Gate Bridge the road-cutting showed pockets of gravel in the red and variegated Keuper Marl, a feature perhaps due to the effects of subterranean stream erosion.^ Gravel has been worked at Weycroft north of Axminster, to the north of Musbury, and at Hampton south of Kilmington. In the gravel of Kilmington which extends tq below 80 feet, Dr. A. E. Salter states, " Rudely chipped cherts also occui- here, large blocks of chert up to 10 X 8 in., schorl rock, etc."* The valleys of Offwell, so>ith-east of Honiton, are for the most part covered with dense wood, scrub and morass, but in two places, above ' Proc. Geol. Assoc, vol. xv., 1898, p. 282. ' Geol. Mag., 1878, p. 37. ' H. B. Woodward in Summary of Progress for 1901, (Mem. Geol. Surv.), 1902, p. 54. ' Proc. Geol. Assoc, vol. xv., 1898, p. 282, \SH2l F 76 VALLEY DEPOSITS. Aplins Common and at the mouth of Oflfwell Valley, the Trias was shown in artificial excavations ; elsewhere it is concealed by extensive slips and rain- washes made up of sand and clay, together with flint and chert stones. Fig. 38. — Section south-west of Shook Farm, south of Axminster. (H. B.W.) 4. Soil and sandy loam. 2. Red marl with stones. V 8 to 3. Gravel with patch of red marl. 1. Clayey gravel. | 9 feet. In the valley of the Coly near Northleigh an(^ Farway Street, there is also much detritus and gravel, the latter sometimes obscured by a soil of red clay with stones. The gravel, moreover, is not always clearly separable from the Alluvium. Thus north of Bonehayne the banks of the river exhibit loam resting on gravel, and on the right bank, about half a mile east of Bonehayne, about 25 feet of gravel was seen resting on Keuper Marl. Near Southleigh gravelly soil is met with, notably to the north-east of Morganhayes ; and between Bolshayne and Colyf ord, which lies to the south-east, the plateau drift merges into the valley gravel across a line of fault. Mr. Reid observed that about half a mile north of Chappie- croft Farm, east of Membury, the stream disappeared into a fissure in the Lias; and at the junction of the streams above Greatwood Farm the main brook sinks in the same way as at Chapplecroft, and the tributary throws down a deposit of pink calcareous tufa. The Alluvium displayed in the river-banks consists of loam, with here and there shoals of gravel, or of loam with partially rounded blocks of flint and chert. Much of the ground between Axminster and Colyf ord is very uneven, and there is seldom a very definite boundary between the Alluvium and the bordering strata. The Axe, as remarked by De la Beche in 1830, " is deflected from its course by the pebble bank thrown up from W. to E. by the prevalent W. and S.W. winds, which here afford the heaviest breakers, and it escapes into the sea by supporting itself against Axmouth cliff; the sea, however, is constantly endeavouring to bar up its passage.'" This easterly trend of the beach' was the means of choking the harbour of what was once the flourishing little fishing town of Axmouth. Salt-pans then existed. At the close of the 18th century a large tract of Salt-marshes extended over the area of ' Phil. Mag., ser. 2. vii., 1830, p. 169. VALLEY DEPOSITS. ( / the old harbour, the sea was eventually excluded, and the area has been drained to the advantage of the neighbourhood. Salt was an article of trade at Lyme Regis in the 14th century. Lym and Chae Valleys. Remains of the Mammoth (Elephas primigenius) and of Rhinoceros have been recorded from the gravel of Charmouth, and the " diluvium " above the church cliffs at Lyme Regis.^ One tusk of the Elephant 9 ft. 8 in. long was obtained by De la Beche. The gravel at Charmouth is well exposed near the mouth of the little river. T. Hawkins mentioned a bed of gravel concealing the blue lias marl east of the borough of Lyme.'' This has now gone owing to encroachments of the coast, but probably it was an extension of the higher valley gravel of the Char, on the lower part of Church Cliffs, before the land had been washed away so far. De la Beche stated that there were slight remains of a sub- merged forest at the mouth of the Char. Along the Lym (or Buddie) Valley above Lyme Regis we find a little rough chert gravel here and there at various levels — it was proved in the trial-boring for coal (see p. 20) ; but there are no conspicuous tracts of Alluvium, partly owing to the slipping here and there of bordering tracts of Lias Clay, whereby the stream-course has been narrowed. To the west of Holcombe between TJplyme and Combpyne an unusually deep and dry gully was to be seen in 1906. The channel had evidently been scoured out by a tumultuous flow of water — the ploughed field was strewn with blocks of chert, and at the bottom of the slope there was a considerable accumulation of them. During a visit of the Geologists' Association Mr. A. W. Clayden suggested that the phenomenon might have been pro- duced by one of those heavy local falls of rain known as " cloud- bursts," and he subsequently ascertained from Mr. C. W. Grover, of the Observatory at Rousdon, that this was the case. Mr. Grover had entered the following statement in his Records for 1886: " The heaviest gale and rainfall known in this district for many years occurred on December 26th. Rain was falling at 9 a.m. and continued moderate till about 4 p.m., when it descended in torrents, making with the wind a most deafening roar, everything being quickly flooded. The roads in many places were washed away, numerous trees of great age and size were uprooted and chasms were washed out, some of which were measured and found to be 10 ft. in depth. Many hundreds of tons of earth, chalk, and rock were washed down towards the sea. The total rainfall of the day was 2"65 ins." Mr. Grover added that the gully in question was one of those referred to in the foregoing passage.' • De la Beche, Trans. Geol. Soc, ser. 2, vol. i., 1822, p. 421, " Report on Geology of Cornwall, Devon, and West Somerset " (Mem. Geol. Surv.), 1839, pp. 412, 417 ; Buckland, " Reliquias Diluvianas," p. 174, and Trajis. Geol. Soc, ser. 2, vol. i., 1822, p. 102. 2 " Memoirs of Ichthyosauri . . . ," 1834, p. 12. ' Proc. Geol. Assoc., xix., 1906, p. 332 and Plate VI. 18821 F 2 78 CHAPTEli X. LANDSLIPS AND COAST EEOSION. Landslips. Among the attractions of Lyme Regis is the great series of land- slips that fringe the coast westwards to within a couple of miles of the mouth of the Axe. The margin of the uplands is from 300 to a little over 500 feet in elevation, and it consists of the brown sands, chert-beds, and calcareous sandstone of the Upper Green- sand, surmounted by the white Chalk, and by irregular cappings of flint and chert detritus. This mass of strata rests on the Gault, Lower Lias clays and limestones, the Ehsetic limestones and shales, and on the Keuper Marls, which, taken together, form a generally impervious and slippery foundation. The Cretaceous strata, though fairly flat, have a slight seaward inclination, and this has been accentuated in places by the under- mining action of springs in carrying away the loose sands at the base of the Greensand. Thus an inclination of 5° S. 20° E. was noted in the cliff at Bindon. Hence we have the most favourable conditions for the produc- tion of landslides, and they have occurred at intervals all along the coast from time immemorial.^ To this cause are due the inflnite variety and picturesqueness of this broken coast-line. The ordinary slipping of a great clay bank is evident on the slopes both east and west of Lyme Eegis, but it is not until we get under the brow of the Ware Cliffs that we enter the region of the great landslips. The ground is made up of the greater and smaller slipped masses — huge blocks and masses that form under- cliffs, intermingled with tracts of greensward, scrub and thicket, rough stony places and quagmires. Here and there detached pinnacles, as the Chimney liock (formed of the higher beds of Upper Greensand) under Ware Cliffs appear below the main Chalk cliffs. Below the Pinhay Cliffs to the south-east of Whitlands is the " Chapel Rock," described by Mr. Jukes-Browne as a large mass of Upper and Middle Chalk, forming a bluff between 120 and 130 feet high. An excellent photo- graph of it has been published by Dr. Rowe, and with regard to the date of these slipped rocks he mentions, on the authority of Miss Helen Allhusen, " the belief that they were formed before the 16th century, as tradition says that they were used as a place for seci'et worship during the religious persecutions in the reigns of Mary and James. "^ Further west on the borders of the Whitlands ravine is a deep fissure known as the " Great Cleft," running parallel to the face of the cliff, thus cutting off a thick slice of rock. The crack first started in 1886, had gradually widened year by year, but rather more rapidly of late than at first. The base is cut in Upper Greensand, the cherty nature of which was well displayed.' An important founder is stated to have occurred in 1765, when the underolift at Whitlands was formed : in 1840 another landslip took place there. ' De la Beohe mentioned that 7 miles south of Lyme Cobb, chalk rocks occurred at a depth of about 15 fathoms : these are no doubt relics of the waste of the coast. Trans. Ge.ol. Soc, ser. 2, 1822, vol. i., p. 41. " Prnc. Geol. Assoc, vol. xviii., 1903, pp. 5, 8, and Plate I. ' G. W. Young, Ibid, xix., 1906, p. 3,S6. LANDSLIPS. 79 0(1, .a, <^ "« S I S s =5 t; a -^ o ^ „ ,2 OS OQ CO 05 -+J o w o fe a 3 .-.r^ a o ■ The most extensive landslip, however, that occurred in this country during the last century- happened in December, 1839, in the cliffs of Bindon and Dow- lands, north of Culverhole Point. The summer and autumn months had been ex- tremely wet, and for more than a week prior to the founder great cracks or clefts had been observed along the brow of the cliffs. The slipping began early on Christmas morning, but the main mass subsided on the following day, when about 4U acres broke away from the clitf , and foundered towards the sea. The result was a chasm from 200 to 400 feet broad, from 130 to 210 feet deep, and about half a mile long, and in the midst there was a sunken belt of broken ground. It was esti- mated that about eight million tons of rock subsided. The pressure of the foundering strata upheaved the sea-bottom adjoining the coast, producing a reef, nearly three-quarters of a mile long and 40 feet high in places, and this was covered at the time with marine organisms. The consternation in the neighbourhood was great, many persons attributing the occur- rence to an earthquake; indeed, " A brief account of the Earth- quake " was published in Lon- don. This inference is interest- ing, as there is a record of an earthquake having happened at Lyme Kegis in 1689 ; and we are thus warned not to place implicit reliance on such re- cords, although a slight earth- quake disturbance might well set in motion strata prepared to founder. At the time of the great land- slip Buckland was staying at Lyme Regis, and Conybeare was in his vicarage at Ax- 80 LANDSLIBS. minster. To them and to W. Dawson, Civil Engineer of Exeter, we are indebted for full particulars of the phenomena; while a more handy guide was published in 1840 by George Eoberts (the historian of Lyme Regis), and this reached five editions during the year.' A good general view of the landslip is shown in the Frontispiece, and the structure of the ground, practically the same as that represented by Conybeare and Dawson, is given in Fig. 39, drawn by Mr. Jukes-Browne. Another important landslip was that of Hooken Cliflf, between Beer Head and Branscombe, which took place in March, 1790. Roberts states that two years before a fine stream of water ceased to flow, and that cracks appeared long prior to the catastrophe. Among the minor slips it may be mentioned that about 2^ years after the deep cutting for the new road was made (in 1825) above Black Ven, between Lyme Regis and Charmouth, the ground slipped down from 20 feet at the western end to 8 feet at the eastern, towards the sea. This road forms a hollow-way known as the " Devil's Bellows," from its exposure to winds The bordering high grounds afford evidence of three amphitheatre- like hollows produced by great slips, and the intermediate hollow is close to the margin of the road. The Rev. W. Downes noted that a further landslip in 1880 necessitated the reconstruction of the high road.' Roberts mentions that in 30 years between 1803 and 1834, 90 feet in breadth of the Church Cliffs were lost, in this case " without any great slide, but by a gradual mouldering, slippingand crumbling." He estimated the loss east and west of the town at from 1 to 3 feet per annum. Never- theless, man has not been free from blame in the actual destruction of the cliffs, for the same writer informs us of the serious injury that has arisen from the removal of the ledges of Lias limestone that served to protect the coast.^ There was formerly a lane to Charmouth, which, as noted by Roberts, commenced by the Alms Houses in Church Street. The position of St. Michael's Church, Lyme Regis, has for many years caused anxiety, but we learn from Mr. A. C. G. Cameron that steps have now been taken to protect the adjacent cliff from further waste, as the church is only 80 feet distant, and a portion of the churchyard has broken away. On June 10, 1908, a series of small landslips took place in the clay-cliffs east of Spittles Lane, Lyme Regis, along a tract about 500 yards in length. Coast Eeosion. The coast is subject to waste from the combined action of sea and springs, together with frost and other subaerial agents. The relatively harder rocks of the Upper Sandstones of Otterton Point naturally withstand the ravages of the sea better than the Red Marls of Sidmouth and Branscombe ; and they present a bold front with rocky platforms, diversified, however, by small and picturesque bays, with isolated stacks of rock and arches, due to the erosive action of the sea along planes of jointing and less indurated portions of the strata. Again, a syncline has lowered the Chalk to Sea-level so as to form the prominent feature of Beer Head, while the fault on the oast of WhiteclifE has brought the Red Marls into abrupt contact with the Greensand and facilitated the erosion of Seaton Bay. Eastwards the cliffs and ledges of White Lias and Lower Lias ' See Titles in Bibliography, p. 92. ' Quart. Journ. Geol. Soc, xli., 1885, p. 23. '■' History of Lyme Regis, 1834, pp. 194, 214-217. COAST EEOSION. 81 limestones form minor headlands or points, and at low tide exten- sive platforms of the strata are exposed, until, east of Lyme Regis, the limestones dip below the level of low water and the sea has direct access to the Lower Lias clays. Erosion has, therefore, been more rapid, and this has been aided by previous fluviatile action when the Char Valley .extended further south. From the foot of Peak Hill to Branscombe there is a shingle beach made up mostly of chert and flint pebbles with sand in places at low tide, and there the loss of land was estimated by Hutchinson at'p.n inch a year, or about 8 feet in a century. Rather finer shingle and sand extend along the shore of Seaton Bay to Culverhole Point, beyond which the beach is more inter- mingled with tumbled blocks from the cliffs. iWest of Lyme Regis the shingle has been carted away from time to time for economic purposes — a proceeding which cannot be commended on a coast which requires protection, and more especially as so much limestone is taken from the cliffs for the manufacture of lime and cement. 82 CHAPTER XI. ECONOMIC GEOLOGY. Building Stones. The stone obtained from the extensive quarries to the west of Beer has long been employed for building purposes, and was used in the interior of Exeter Cathedral in Norman and later times. The Beer Stone belongs to the Middle Chalk, and it consists of limestone composed almost entirely of coarse shell- fragments. It has been opened up in an immense quarry on the north side of Quarry Lane, about a mile west of Beer, and worked both above and below ground. The tunnels whence the freestone has been obtained extend a long way underground both to the north and south of Quarry Lane ; and they are supported by masses of the freestone, aided here and there by timber. The stone is sawn out in situ, and blocks from six to eight tons are obtained. It is comparatively soft when taken from the workings, but hardens on exposure. It is estimated to bear a stress of 2,106 lbs. per square inch.' From its uniform texture and close grain it is admirably adapted for carving, and especially for inside decora- tive work. It has, however, been used with success for outside as well as inside work in many of the neighbouring churches, at Ottery St. Mary, Honiton, Axminster, &c., and has even been sent as far as Norwich for use in the Roman Catholic Cathedral in that city. The total thickness of the freestone is 12 or 13 feet, but it appears to be somewhat locally developed.^ De la Beclie mentions that " A shaft was formerly sunk, and a level driven into the hill, between Beer Head and Branscombe, in order to obtain a continuation of the same beds, but the work does not appear to have been profitable, as it is now abandoned."^ Mr. Jukes-Browne notes that near the Pinnacles in Hooken Cliff, dressed blocks of stone still lie about on the slopes.^ The Beer Stone was not identified as a freestone in Beer Head. (See p. 61.) Mr. Jukes-Browne considers that the Beer Stone is represented by 5 feet of freestone which has been worked in the Sutton Quarries, south-west of AVidworthy." Freestone was also worked in the Lower Chalk at Wilming- ton, and at Dunscombe. (See p. 59.) The Lower Lias limestones at Lyme Regis, Uplyme and Axminster have been quarried for building-blocks, paving-stone and lime-burning. The following section, recorded in 1822 by Buckland, is of interest in showing the local "names applied to the strata; it iias " taken from u, series of lias quarries on the two opposite sides of the valley of the Axe near Axminster."^ ' P. B. Masey, " Observations on Beer Stone," Exeter, 1882. ^ See Jukes-Browne, " Cretaceous Rocks of Britain," vol. ii., {Mem. Geol. Surv.), 1903-4, p. 506, vol. iii., p. 379. ' Report on Geology of Cornwall, Devon, and West Somerset {Mem. Geol. Surv.), 1839, pp. 240, 487. ' " Cretaceous Rocks of Britain," vol. ii., {Mem. Geul. Surv.), 1903, p. 440. " Quart. Journ. Geol. Soc, vol. liv., 1898, p. 241. « Trans. Geol. Soc, ser. 2, vol. i., 1822, p. 98 ; " Reliqui* Diluvianae,'' ed. 2, 1824, p. 242. BUILDING STONES. 83 Lower Lias. ' White Lias — Slaty and fissile, used for flooring Clay. Burrs — Eough building-stone , Clay. Cockles — Shelly stone, used for building Clay. Anvils — Blue building-stone, forming a bed of irregu- lar anvil-shaped blocks Clay. Gaze Burrs — Good blue building-stone Clay. Fire Stone — White building-stone, used also for forming the arch-work of lime-pits Clay. Half -foot bed — Flagstone, the best for paving Clay. Foot Stone — Blue paving and building-stone Clay. Red Size — White Lias inclining to grey, used for paving and building Clay. Under bed — Blue building-stone, used for paving and for steps Clay. White Rock — White Lias. Ft. 2 10 10 1 10 1 6 6 8 Rhsetic Beds. The local names of the beds here and at Uplymei are applied to the cjiaracter and uses of the beds and without respect to the relative horizon. The Lower Lias has been opened up in several quarries in the neighbour- hood of Uplyme (see p. 39), and the beds are now worked at Wey croft, near Axminster (see also p. 19). The quarrying of stone at Lyme, Regis, especially the removal of the ledges of rock on the foreshore has for many years been a source of some anxiety to those interested in the protection of the coast; but as a building stone, De la Beehe states : " When taken from the sea-side, as near Lyme Regis, where it has become impregnated with saline water, it is notoriously bad."2 Blocks of cement-stones from the cliffs or beach near Charmouth have, in old times, been utilised for paving-stone or pitching. The indurated nodules in the Upper Greensand known as Cow- stones have been employed (together with Portland " roach ") in the construction of the Cobb at Lyme Regis. The date of its first erection is not known, but its present form is said to have been in part as old as the fourteenth century, but the main mass was reconstructed and completed in 1826, after damage by a great storm in November, 1824. Elsewhere the chert-beds of the Greensand, and chert and flint from the gravel-beds, have been locally used in building cottages and walls. On Shute Hill the chert has been largely worked for paving bowling alleys and yards, for which pur- poses it has been sent to various parts of South Devon. The calcareous sandstones of the Greensand at Dunscombe and Sal- combe were formerly quarried for building-stone, but most of the pits are now overgrown. Lime and Cement.^ Lyme Regis has for many years been celebrated for its hydraulic lime and cement. ■ See Wright, Quart. Joum. Geol. Soc, xvi., 1860, p. 397. ' Report on Geology of Cornwall, Devon, and West Somerset {Mem. Geol. Surv.), 1839, p. 488. ' See H. B. Woodward, " Jurassic Rocks of Britain," vol. iii., (Mem. Geol. Surv.), 1893, pp. 288-293, 84 ECONOMIC GEOLOGY. The Blue Lias limestones of tlie West Cliff and some of the Cement-stones in the clays above have been utilized for this pur- pose. A good deal of the material has been shipped in the raw- state, about 120 tons a week, while much of it is prepared for lime and cement at the adjoining kilns. Analyses, by Mr. John Spiller (1870), of cement made from the limestones and cement-stones, showed that the latter contained a slightly larger proportion of soluble silica and alumina, whereby the cement sets somewhat harder and exhibits a greater density. The stone is collected from the tumbled masses on the beach, and when these have been removed the stone in the cliffs is blasted. Each layer has its distinctive name as elsewhere noted (p. 37), the same names being applied as far as possible to the layers in the West and Church Cliffs. The Hard Marl and the West Rock (an iron-stained cement-stone that occurs at a higher level in the clays of the West Cliff), are said when mixed together to make a superfine cement. Some of the cement-stones in the cliffs near Charmouth, especially the " two cement-hands," have been employed in old times for making cement, and remains of a disused cement-mill still stand near the sea-shore. (See P- 36.) At the Yawl Lime-kilns at Uplyme the Lower Lias and also the White Lias are used in the preparation of lime. Near Weycroft, Axminster, at the Dorset Blue Lias Lime and Cement Works, both lime and cement were formerly made from the Lower Lias limestones, but, in 1904, lime only was prepared. It is said that the paler beds of Lower Lias and the White Lias make the better lime for plastering and indoor work. Chalk has been burnt for lime in many localities, and at the famous Beer quarries the beds above the Beer stone are so utilized. Occasionally the top highly calcareous rock of the Greensand has been burnt for lime near Chardstock. Maul. In old times, and for the most part prior to the 19th century, the Marls or red clays of the Trias were extensively dug for top- dressing of the land. The old pits afford no sections worthy of record, but many of them occur in the Sid and Branscombe valleys. North of Great Trill beds of greenish-yellow marl streaked with red were formerly dug for agricultural purposes. Bkick Clay. The Lower Maris have been worked for brick-making on the eastern side of the Tale valley near Talewater. Pits were opened in the Keuper Marls for the same purpose, in the lower beds — at Sidmouth station ; on the east of the high road south of Sidford ; east of Manston Farm, in red, rather loamy clay, with a green band ; in the Otterton outlier (by the high road east BRICK (JLAY. 85 of the village) ; near their junction with the sandstones east of Ottery St. Mary ; by the railway (a large pit) on the west side of the tributary valley, west of Honiton Station ; also at Couchill, north-west of Seaton. About a quarter of a mile south-east of Fordhayes, north of Kilmington, there was formerly a pottery where whitish clay was dug beneath gravel. The Lower Lias clays have been worked for brick-making on the western side of Lyme Regis, and in a number of localities bordering the Axe above Axminister, as near Hawkchurch south- west of Forde Abbey. Nearly all these small brickyards are now closed, partly because good facing bricks are to be more cheaply obtained from larger works, such as those of Pinhoe, near Exeter. Road Metal. The chief local road-materials are those derived from the Triassic pebble-beds, the Greensand chert, the plateau accumula- tions of chert and flint, and the valley gravels. Scythe Stones. Broadhembury on the northern margin of the area has been noted for the Scythe Stones manufactured from siliceous or cherty concretions in the Upper Greensand. The strata from which the material was obtained, lie to the north, in the area of sheet 311, but the manufacture of Scythe Stones or " Devonshire batts " formerly gave employment to many persons in the villages of Broadhembury and Payhembury. Sands. Sands for rough-casting have been obtained from the Green- sand at Wilmington. (See also pp. 60, 75.) Gtjn Flints. On the undercliff to the west of Beer Head a manufactory of Gun-flints formerly existed, as recorded by P. 0. Hutchinson.' The work was abandoned in the early part of the 19th century. Gypsum. Gypsum occurs in the Keuper Marls at Branscombe, and it was at one time worked between Branscombe Valley and Weston Mouth (see p. 15). Vancouver mentions that it used to be sold at 2s. Qd. per hundredweight.^ In the boring near Lyme Regis many bands of gypsum, up to 16 inches in thickness, were penetrated (see p. 20). 1 See Skertchly, Manufacture of Gun-flints, (Mem. Geol. Surv.), 1879, p. 14. 2 C. Vancouver, " Agriculture of Devon," 1808. 86 ECONOMIC GEOLOGY. Pyrites. The Lower Lias sliales of Black Veil are more or less impreg- nated with iron-pyrites, but in the upper part of the dark shales or Black Marl there is a band known as the " Metal Bed," and from this at one time, during the winter months, much pyrites was obtained for the manufacture of sulphuric acid. Examples of marcasite (rhombic iron-pyrites) have been sold to visitors at Lyme Regis as " angels' wings." The presence of so much pyrites in the cliifs occasionally leads to " spontaneous combustion." In August, 1751, after very hot weather, followed by sudden rains, the Lias cliffs near Charmouth (probably Black Ven) began to smoke, and at times to burn with a visible flame.* Some of the shales at this locality are highly bituminous. On the 19th January, 1908, many of the inhabitants of Lyme Regis were alarmed by the announcement that a " volcanic eruption " had taken place, as smoke was seen to issue from a mound of Lias shale and clay on the cliffs about half a mile north-east of St. Michael's Church. The mound was portion of a mass of Lias clay and shale that had some time previously slipped from the higher cliffs, and the "eruption" was due, as in the former case, to the decomposition of iron-pyrites and the conse- quent production of sufficient heat to ignite portions of the bituminous shales. Explanations of the phenomena were com- municated to the local newspapers by Mr. A. C. G. Cameron, and full particulars were afterwards published by Mr. Jukes-Browne.'' Soils. One of the old agricultural writers divided the county of Dorset into Felix, Petrcea and Veserta — the fruitful vales, the stony uplands, and the heaths.^ This general division would apply not only to the portions of Dorset included in our area, but also to the larger tracts of Devon. The Lias, the Keuper Marls, and the other Red rocks, together with the Alluvial deposits, form the fruitful vales, with much rich meadow and grazing land, and many orchards. The lighter tracts lie along the Tale valley and the Otter below Ottery St. Mary, where the New Red Sandstone and pebble-beds are developed; but, as before mentioned, the stift'er soils of the Keuper Marls and Lias Clays are very largely modi- fied by down-washes of sand and chert-detritus from the stony uplands. The soil on these uplands is a variable stony loam and clay, better for tillage than pasture; but much of the land, spoken of ' J. Stephens, Phil. Trans., lii., 17,62, p. 119. ' Proc. Dorset Nat. Hist. Club, xxix., 1908, p. 155. " L. H. Ruegg, Jourti. Bath & W. of Eiig. Soc, ser. 3, viii., 1897, p. 180. See also C. Vancouver, " Agriculture of Devon," 1808. SOILS. 87 as " Deserta" consists of picturesque heath, common, and wood- land, " waste-land " only from an agricultural point of view. During recent years the Dorset County Council has initiated researches on the soils of the county, and these have been carried on in the Agricultural Department of University College, Eeading. In the vale of Marshwood, the western portion of which appears by Westover Farm, N.B. of Lyme Regis, the soil, where not affected by down- washes of Upper Greensand, is " a very stiff clay, about six inches in depth, the arable land being very difficult to work in either wet or dry weather. As a rule the crops produced are light, although wheat is sometimes a heavy crop. Much of the land has now been laid down to pasture, and dairy farming is now very general in the district, "i The region is famed for Dorset butter and blue cheese. Analysis shows that the low-lying soil is poor in lime. " The peculiar sticky, impervious character of these clay soils is due to the high proportion of very fine particles which they contain."' There is naturally much downwash from the Greensand Hills, over the slopes and undulating tracts of Middle Lias. Near Forde Abbey " The farming of the district is of a mixed character, being chiefly sheep and corn, with some dairying. The soil is of a gravelly loam about a foot deep, lying on a rather stiff gravelly subsoil reddish in colour. "^ Water Supply. Water is to be obtained in shallow wells from the various valley gravels, and sometimes from the plateau deposits when these are based on a clayey substratum. In most cases the village-supplies from valley gravels have become polluted. A well at Chard Road Hotel, on the north confines of the map, by the railway-station, was carried to a depth of 12 feet in the alluvial gravel. It not improbably receives from the adjacent river Axe an accession of water which would filter through the gravel. The Chalk itself is practically porous through its mass, there being no lower division of marly or clayey chalk. The water supply from the Chalk and Upper Greensand is, therefore, not disconnected as a rule, unless by any local bands of flint, or by hard rock-beds at the junction of Chalk and Greensand. In consequence, along the upland range between Lyme Regis and Axmouth, " Wells have been dug to a depth of between two and three hundred feet before any water could be procured."* The Greensand is the most important source of water in the district. In villages situated directly on it, the supply from wells is apt to be polluted, and a more distant source, free from con- tamination, is, in many cases, greatly needed. Numerous springs, and all those of a permanent character, are given out at or near the base of the Greensand, being thrown ' First Annual Report on the Soils of Dorset. Suppt. VIII. to the Journal of the Reading College, by D. A. Gilchrist and C. M. Luxmoore, 1899, p. 37. " Report on the Soils of Dorset, by John Percival. Univ. Coll. Reading, 1906, p. 19 ; and Final Report, by C. M. Luxmoore, 1907. ' D. A. Gilchrist and C. M. Luxmoore. Second Ann. Rep. on the Soils of Dorset. Suppt. X. to Journ. Reading Coll., 1900. ' G. Roberts, " Account of, and Guide to the Mighty Land-slip of Dowlands and Bindon," Ed. 5, 1840, p. 13. 88 ECONOMIC GEOLOGY. out locally by the Gault clay, and elsewhere by the clayey Lias, RhEetic Beds, and Keuper Marls. In times of much ram, springs issue from higher levels, and brooks flow from the Plateau Drift and course down the steep slopes of the Greensand. Thus, the stream which flows northward to Honiton from the valley between Gittisham and Farway Hills, takes its rise, at times, from an oval swamp on the Plateau Drift, known as " Eing-in-the-Mire."i The slight south-easterly dip of the Cretaceous strata has influenced the direction of outflow of the main springs along the Greensand scarps ; and there is, consequently, a marked increase in the number and importance of springs along the slopes facing east and south-east, as compared with those along the slopes facing west and north-west. The relative erosive influence of the springs is manifest in the amount of irregularity along the different scarps. Sidmouth is supplied by springs from two sources : one on Mutter's Moor, on Peak Hill, and the other from Finn Hill, between Sidbury and Honiton. The water is derived from the Greensand, and is filtered and stored in reservoirs on the slopes of Peak Hill. It is a soft water containing less than six grains of mineral water per gallon. ^ Honiton derives its supply from the Greensand on the eastern slope of St. Gyres Hill. The main source is on the 700 foot contour near Hutching- hayes, whence collecting pipes convey the water to two open storage- reservoirs situated nearly half a mile west of Combe Baleigh. The water is conveyed to the town in a 4-inoh supply main. Springfield service reser- voir is on the eastern side of the town. Sand filters are used. Messrs. Beesley, Son & Nichols kindly supplied the information. Lyme Regis is supplied from a spring that issues from the Greensand at Hollow Grove, east of Hole Farm, on the north of Dragon Hill, and about Ij miles north of the town. Uplyme is supplied from the Greensand on the southern side of the village; and Charmouth derives a supply from springs below Fern Hill, north-west of the village. Axminster has been supplied from springs that issue from the Greensand at Furzeley to the south and south-east of the town. In one case " the overflows of several springs unite to form a brook known as the ' Town Lake,' " a conduit that flows through the town — and has been used. The chief supply is taken from a reservoir about a mile from the town on the Lyme Regis road. This is fed by streams from the same district of Green- sand, but in dry seasons the supply has proved insufficient. Colyton receives a good and abundant supply from springs in a combe on the side of a hill near Ridge way farm. The water is conducted to two reservoirs, and thence by gravitation to the town. Many wells remained in use (in 1899). Their depth does not exceed 50 feet, and they would derive water from the valley gravels. The village of Beer is partly supplied from springs at Couchill, the water being brought through a tunnel in the hill. This is the best supply. There are also local wells and springs, not as a rule free from sources of contamination.' ' Hutchinson, " Guide to Sidmouth," 1875, p. 64. ' Dr. A. Macindoe, '■ Sidmouth as a Health Resort and Place of Residence." 8vo., Bristol, 1900, pp. 36-38. ' For information relating to Uplyme, Axminster, Colyton, and Beer, we are indebted to a Report on the Axminster Rural District, by Dr. P. St. George Mivart, Loc. Gov. Board, No. 142, 1899. WATER SUPPLY. 89 Seaton is also supplied from the springs at Couchill : these issue from the Greensand. The well at Rousdon was carried to a depth of 207 feet, through Chalk into Greensand. Information supplied by Mr. C. W. Grover. The following records give details of the strata : — Ware House, Devon, about a mile west of Lyme Regis. Surface of ground about 395 feet above Ordnance Datum. Shaft 48 feet ; the rest bored. From particulars obtained by Mr. A. C. G. Cameron, 1909. About 2,000 gallons of water a day obtained from the shaft. Foxmould sand Cowstone Grey sand with small concretionary stones Light green sand, with hard stone, 2 ft. 5 in. Schloenbachia rostrata Light green sticky sand ... Hard coarse sand Grey sandstone concretion Sand... Grey sandstone concretion Sand Dark sandstone Sandy micaceous clay Dark loamy clay ... Greenish loamy clay Lighter-coloured sandy clay Dark loamy clay Brownish sandy clay Upper Greensand. Gault. Zone of Schloen- bachia rostrata. Zone of HopUten interrup- ius. Thickness. Depth. Ft. In. Ft. In 21 21 2 23 5 28 [ 20 48 10 58 3 61 9 61 9 1 3 63 4 63 4 7 8 71 1 6 72 6 6 10 79 4 9 88 4 10 98 4 15 113 4 2 115 4 2 117 4 CoTLEiGH, Devon, (Lady Ashburton's house), about 3 miles N.E. of Honiton. Details from Mr. Crawford communicated by Mr. W. Whitaker. Surface of ground rather more than 500 feet above Ordnance Datum. Water level 22^ feet down. Yield 7^ gallons a minute. Dug well (the rest bored) Loam and flints Clay with Flints and Chert. Upper Greensand. Gault ? Flints Flints and loam White sandstone Sandy clay and stone White flints [chert J Sand White flints Green and yellow sandy clay Dead grey sand Blue stone Dead green sand Blue clayey sand ... Dead grey sand and shells... Dead grey sand Grey sand Sandy blue clay Grey stone Pyrites [and ?olay] Hard grey stone lick ness. Depth. Ft. In. Ft. In _ _ 10 9 6 19 6 2 21 6 6 22 5 6 27 6 2 29 6 16 45 6 1 46 6 2 7 49 1 3 8 52 9 29 81 9 2 6 84 3 2 6 86 9 5 91 9 4 6 96 3 5 6 101 9 3 104 9 5 6 110 3 3 6 113 9 3 6 117 3 3 117 6 90 ECONOMIC GEOLOGY. The Lower Lias limestones and White Lias (Rhisetic) yield springs and limited supplies of water in wells, near the outcrop of the strata, as exemplified by the following record. Waterside, about a quarter of a mile E.S.E. of Uplyme Church, Devon. Surface of ground 225 feet above Ordnance Datum. Old shaft 95 feet; the rest bored by Messrs. Tilley in 1908. The shaft yielded about 300 gallons of water a day; the boring yielded more than twice that amount. Communicated by Mr. A. C. G. Cameron. Rhsetic. Lower Lias and / Shaft (no details of strata) ... White Lias. \ White rock [limestone] Dark clays and shales with thin Black Shales. -J bands of stone, and selenite in bottom layer Greenish tinted clay or marl ... Dark grey marl or clay and some hard lumps Thickness. Ft. In. 95 (I 2 9 Grey Marls (Passage Beds). 23 3 3 Depth. Ft. In. 95 97 9 121 1 124 1 127 1 The extra amount of water must probably have come from the basement-bed of the White Lias. Limited supplies of water may sometimes be obtained from the Keuper Marls when they contain bands of sandy rock. A boring at Coi-yton Park, west of Axminster, was in 1903 carried through about 30 feet of cherty gravel, and through 138J feet of Red Marl to Rock Marl — the total depth reached being 169 feet. Water was obtained, and this stood at a level of 85 feet below the surface of the ground. A boring at Lady Ashburton's house at Seaton was in 1869 carried from the base of a well 107 feet deep through " red loam " and hard rock bands to a further depth of 37 feet. No useful amount of water was obtained. Next in importance to the Greensand are the Upper Sand- stones and Pebble Beds from which good supplies of water are to be e:!gpected in favourable situations. West of Ottery St. Mary by the road to Exeter two wells were sunk ; one (Mr. Campion's) on the southern side of the road, near the margin of the map, was said to have been sunk to a depth of 52 feet through gravel (pebble-beds), sand, and a la3'er of clay. At a cottage by a bye-road not far to the east, a well had been sunk in gravel to a depth of 30 feet. The upper portions of the strata passed through were probably re-deposited materials.! A well at Blue Anchor Inn, west of Payhembury (see Fig. 1), was sunk through 30 or 40 feet of gravel (pebble-beds), apparently overlain by several feet of gravel, clay, and sand, probably re-deposited material. DoTTON L.\NE, about 1 mile north of Golaton Raleigh Church, Devon. For Exmouth Urban District Council Waterworks. From particulars communicated by Messrs. 6. H. Hill & Sons (1908-9) to Mr. W. A. E. Ussher. Supply abundant. Ussher, " The Country around Exeter " {Mem. Geol. Snrr.), 1902, p. 50, WATEB SUPPLY. 91 Surface of ground 77 feet above O.D. Dug well to 28 feet 9 inches, at which depth water came too fast for the excavation to be continued, and a boring 2 feet 4 inches in diameter was commenced. Superficial Deposits. Top soil Pebbles and sand Sand and shingle Hard red sand ... Upper Sandstone. (Concretionary Beds.) Upper Sandstone (seldom Concre- tionary). Upper Sandstone i a j^j. j j i. (probably Keuper \ |°*V sandstone Basement Beds) Hard sand, yellow tinge, mixed with ' I pebbles ... ' Sandstone rock Thin layers of sandstone Hard sandstone and thin layers of mottled clay Hard red sand Hard sandy marl Hard coarse sand Sand and sandstone fragments Sandy marl , Sand and sandstone fragments ' Sandy marl and sandstone Sand and sandstone fragments Soft sand and layers of soft sandstone Bed sand and layers of sandstone Sand of yellow tinge and sandstone (at 121 feet) Coarse red sand Bed sand... Bed sandatone and fragments. Bed sand, band of marl and two bands of sandstone Coarse red sand Bed sand with band of sandstone Bed marl \ Sandstone / Bed sand Bed marl with grey streaks and sand- stone (6 inch band) Coarse red sand Sand of lighter tinge and finer texture Bed marl with grey streaks \ Sandstone / Sand of lighter tinge Dark red sand Sandstone Dark red marly sand Yellowish buff sand mixed with marl L Bunning sand Pebble beds Calcareous or "petrifying" springs were observed by P. 0. Hutchinson to the east of Salcombe Mouth, and at Little "Weston, a hollow in Dunscombe ClifEs.^ (See also p. 76.) No noteworthy Mineral Springs have been met with, and no " Spas " have anywhere been established in the district. ' " Guide to Sidmouth," 1875, pp. 48, 49. Thickness Depth. Ft. In. Ft. In 2 2 1 6 3 6 3 6 6 3 9 6 4 IB 6 8 6 22 9 22 9 4 3 27 1 9 28 9 5 33 9 1 34 9 2 6 37 3 6 43 3 2 6 45 9 3 9 49 6 2 6 52 24 6 76 6 9 9 86 3 33 6 119 9 8 3 128 23 151 2 3 153 3 9 154 3 157 5 162 8 7 170 7 1 11 172 6 6 178 6 5 3 183 9 13 9 197 6 5 6 203 4 6 207 6 3 6 211 22 5 233 5 7 234 35 269 22 9 291 9 10 7 302 4 35 8 338 18821 92 APPENDIX. List of Principal "Woeks on t:^e Geology of the District. [For references to special Palseontological Books and Papers, see Biblio- graphies in " Jurassic Rocks of Britain," vol. v., and in " Cretaceous Rocks of Britain," vol. iii., Mem. Oeol. Surv. See also W. Whitaker, " List of Works on the Geology, Mineralogy and Paleeontology of Devon- shire," Trans. Devon As.wc., vol iv., 1870, p. 330; vol. v., 1872, p. 404; and W. Whitaker and A. Strahan, " List of Books, Papers, Maps, &c.,onthe Geology, Mineralogy, and Palaeontology of Dorset," in Geology of the Isle of Purheck and Weymouth," by A. Strahan, Mem. Geol. Surv., 1898, p. 241.] 1822. De la Beche, H. T. Remarks on the Geology of the South Coast of England, from Bridport Harbour, Dorset, to Babbacombe Bay, Devon. Trans. Geol. Soc, ser. 2, vol. i., pp. 40-47. BucKLAND, Rev. W. On the Excavation of Valleys by Diluvian Action, as illustrated by a Succession of Valleys which intersect the South Coast of Dorset and Devon. Trans. Geol. Soc, ser. 2, vol. i., pp. 95-102. 1826. Db liA Beohe, H. T. On the Lias of the Coast in the Vicinity of Lyme Regis. Trans. Geol. Soc, ser. 2, vol. ii., pp. 21-30. De la Beche, H. T. On the Chalk and Sands beneath it (usually termed Green-sand) in the Vicinity of Lyme Regis, Dorset, and Beer, Devon. Trans. Geol. Soc, ser. 2, vol. ii., pp. 109-118. 1829. BuoKLAND, Rev. W. On the Discovery of Coprolites, or Fossil Fseces, in the Lias at Lyme Regis, and in other Formations. Proc Geol. Soc, vol. i., pp. 96-98; Trans. Geol. Soc, ser. 2, vol. iii., pp. 217-222. 1834. Roberts, G. The History and Antiquities of the Borough of Lyme Regis and Charmouth. 8vo. London. 1839. De la Beohe, H. T. Report on the Geology of Cornwall, Devon, and West Somerset. Mem. Geol. Surv. 8vo., London. 1840. CoNTBEAEB, Rev. W. D. Extraordinary Landslip and Great Convul- sion of the Coast of Culverhole Point, near Axmouth. Edin. New. Phil. Journ., vol. xxix., p. 160. CoNTBBEARE, Rev. W. D., and others. Ten Plates, comprising a plan, sections, and views, representing the changes produced on the Coast of East Devon, between Axmouth and Lyme Regis by the Subsidence of the Land and Elevation of the bottom of the Sea, on the 26th December, 1839, and 3rd of February, 1840. From Drawings by W. Dawson, the Rev. W. D. Conybeare and Mrs. Buokland. With Geological Memoir and Sections, by the Rev. W. D. Conybeare. The whole revised by Prof. Buckland. Ohlong, London. [Godwin-] Atjsten, R. A. C. On the Geology of the South-east of Devonshire. Trans. Geol. Soc, ser. 2, vol. vi., pp. 433-489. Roberts, G. An Account of, and Guide to, the Mighty Land-slip of Dowlands and Bindon, in the Parish of Axmouth, near Lyme Regis, December 25th, 1839 (5 Editions in 1840). 8vo. Lyme Regis. 1843. Hutchinson, P. O. The Geology of Sidmouth and of South-Eastern Devon. 12mo. Sidmouth. 1856-8. Oppel, Dr. A. Die Juraformation Englands, Frankreichs, und des Siidwestlichen Deutschlands. 8vo. Stuttgart. BIBLIOGEAPHT. 93 1860. Wright, Dr. T. On the Zone of Avicula contorta, and the Lower Lias of the South of England. Quart. Journ. Geol. Soc, vol. xvi., pp. 374-411. 1862-65. Penqbllt, W. The Red Sandstones and Conglomerates of Devon- shire. Trans. Plymouth Inst. 1863. Day, E. C. H. On the Middle and Upper Lias of the Dorsetshire Coast. Quart. Journ. Oeol. Soc, vol. xix., pp. 278-297. 1864. Wright, Dr. T. On the White Lias of Dorsetshire. Geol. Mag., vol. i., pp. 290-292; Bep. Brit. Assoc, for 1864, p. 75. 1865. Dat, E. 0. H. On the Lower Lias of Lj-me Regis. Geol. Mag., pp. 518-519. 1869. Whitaker, W. On the Succession of Beds in the " New Red " on the South Coast of Devon, and on the Locality of a New Speci- men of Syperodapedon. Quart. Journ. Geol. Soc, vol. xxv., pp. 152-157. 1871. Whitaker, W. On the Chalk of the Southern Part of Dorset and Devon. Quart. Journ. Geol. Soc, vol. xxvii., pp. 93-100. 1873. Hutchinson, P. 0. Submerged Eorest and Mammoth Teeth at Sidmouth. Trans. Devon Assoc, vol. vi., p. 232. 1874. De Range, C. E. On the Physical Changes preceding the Deposition of the Cretaceous strata in the South-west of England. Geol. Mag., pp. 246-253. Meter, 0. J. A. On the Cretaceous Rocks of Beer Head and the adjacent Clifl-sections, and on the Relative Horizons therein of the Warminster and Blackdown Fossiliferous Deposits. Quart. Journ. Geol. Soc, vol. xxx., pp. 369-393. Woodward, H. B. Remarks upon the Relations and Grouping of the Permian and Triassic Rocks. Geol. Mag., pp. 385-390. [Devon Coast Section, pp. 388, 389.] 1875. Ussher, W. a. E. On the Sub-divisions of the Triassic Rocks, between the Coast of West Somerset and the South Coast of Devon. Geol. Mag., pp. 163-168. 1876. B.ARROis, Dr. C. Recherches sur le Terrain Cretace Superieur de I'Angleterre et de I'lrlande. Mem. Soc. Geol. du Nord, Lille. (Devonshire, pp. 68-76, reprint.) Johnston-Lavis, Db. H. J. On the Triassic Strata which are ex- posed in the Cliff-sections near Sidmouth, and a Note on the Occurrence of an Ossiferous Zone containing Bones of a Labyrinthodon . Quart. Journ. Geol. Soc, vol. xxxii., pp. 274-277. TJssHER, W. A. E. On the Triassic Rocks of Somerset and Devon. Quart. Journ. Geol. Soc, vol. xxxii., pp. 367-394. 1878. D'Urban, W. S. M. Paleeolithic Implements from the Valley of the Axe. Geol. Mag., pp. 37, 38. Evans, Sir J. On some Palseolithic Implements found in the Axe Valley. Sep. Brit. Assoc for 1877, p. 116. UssHBR, W. A. E. The Chronological Value of the Pleistocene Deposits of Devon. Quart. Journ. Geol. Soc, vol. xxxiv., pp. 449-468. 1878' Ussher, W. A. E. On the Chronological Value of the Triassic Strata of the South-western Counties. Quart. Journ. Geol. Soc, vol. xxxiv., pp. 459-470. 1878-86. Wright, Dr. T. Monograph on the Lias Ammonites of the British Islands. Palceontograph. Soc. 1882. Whitley, N. On Supposed Paleolithic Implements of the Valley of the Axe. Journ. Vict. Inst., vol. xvi., pp. 35-57. 94 APPENDIX. 1884. Metcalfe, A. T. On Further Biscoveries of Vertebrate Remains in the Triassio Strata of the South Coast of Devonshire, between Budleigh Salterton and Sidmouth. Quart. Journ. Qeol. Soc, vol. xl., pp. 257-262. Parfitt, E. On Palseolithic Implements and Roman Coin found at Broom in the Valley of the Axe. Trans. Bevon Assoc, vol. xvi., pp. 501-504. 1885. DowNES, Rev. W. The Cretaceous Beds at Black Ven, near Lyme Regis, with some Supplementary Remarks on the Blackdown Beds. Quart. Journ. Geol. Soc, vol. xli., pp. 23-26. DowNES, Rev. W. Geological Notes upon the Honiton District. Trans. Devon Assoc, vol. xvii., pp. 240-245. 1886. DowNES, Rev. W. On the Tunnel Section near Honiton, Devon. Geol. Mag., pp. 308-311. Hutchinson, P. O. Report on the Rate of Erosion of the Sea-coasts — Sidmouth. Bep. Brit. Assoc for 1885, pp. 417-422. WoODWABD, H. B. Report on Erosion of Sea-coasts — Axmouth to Eype, &c. Bep. Brit. Assoc for 1885, pp. 423-426. 1888. Irving, Rev. De. A. The Red-Rock Series of the Devon Coast- section. Quart. Journ. Geol. Soc, vol. xliv., pp. 149-163. 1889. Woodward, H. B. Excursion to Lyme Regis. Proc. Oeol. Assoc, vol. xi., pp. xxvi-xlix. 1892. Hull, Prof. E. A Comparison of the Red Rocks of the South Devon Coast with those of the Midland and Western Counties. Quart. Journ. Geol. Soc, vol. xlviii., pp. 60-68. Irving, Rev. Dr. A. Supplementary Note to the Paper on the " Red Rocks of the Devon Coast-section." Quart. Journ. Geol. Soc, vol. xlviii., pp. 68-77. UssHER, W. A. E. Permian in Devonshire. Geol. Mag., pp. 247-250. 1893. Irving, Rev. Dr. A. The Base of the Keuper Formation in Devon. Quart. Journ, Geol. Soc, vol. xlix., pp. 79-83. Woodward, H. B. The Jurassic Rocks of Britain. Vol. III. The Lias of England and Wales (Yorkshire excepted). Mem. Geol. Surv. 8vo., London. 1896. Jukes-Brownb, A. J., and W. Hill. A Delimitation of the Ceno- manian : being a Comparison of the Corresponding Beds in South-western England and Western France. Quart. Journ. Geol. Soc, vol. lii., pp. 99-178. 1897. Jukes-Browne, A. J. The Origin of the Vale of Marshwood and of the Greensand Hills of West Dorset. Proc Dorset Nat. Hist. Club, vol. xviii., pp. 174-184. 1898. Jukes-Browne, A. J. On an Outlier of Cenomanian and Turonian [equivalent to Lower and Middle Chalk] near Honiton. Quart. Journ. Geol. Soc, vol. liv., pp. 239-250. Salter, A. E. Pebbly and other Gravels in Southern England. Proc Geol. Assoc vol. xv., pp. 280-283. 1899. Woodward, H. B., and W. A. E. Usshbr. Excursion to Seaton, Sidmouth, Budleigh Salterton, and Exeter. Proc Geol. Assoc, vol. xvi., pp. 133-153. 1900-1904. Jukes-Bbowne, A. J., and W. Hill. The Cretaceous Rocks of Britain. Mem. Geol. Surv. 3 vols., 8vo., London. 1902. Jukes-Bbowne, A. J. On a Deep Boring at Lyme Regis. Quart. Journ. Geol. Soc, vol. Iviii., pp. 279-289. Thomas, H. H. The Mineralogical Constitution of the Finer Material of the Bunter Pebble Bed in the West of England. Quart. Journ. Oeol. Soc, vol. Iviii., pp. 620-632. Usshbr, W. A. E. The Geology of the Country around Exeter. Mem. Geol. Surv. 8vo., London. BIBLIOGRAPHY. 95 1902. Woodward, H. B. Notes on a New Railway in course of construction between Axminster and Lyme Regis. Summary of Progress for 1901, Mem. Geol. Surv., pp. 53-59. WooDWABD, H. B. Note oii the Occurrence of Bagshot Beds at Combe Pyne, near Lyme Regis. Geol. Mag., pp. 515, 516. Bep. Brit. Assoc, for 1902, pp. 601, 602. 1903. Jukes-Browne, A. J. Devonshire in the time of the Lower Chalk. Trans. Devon Assoc, vol. xxxv., pp. 787-799. Lang, W. D, On a Fossiliferous Bed in the Selbornian of Charmouth. Geol. Mag., pp. 888-392. ■ROWE, Dr. a. W. The. Zones of the White Chalk of the English Coast. III. Devon. The Cliff-sections, by C. D. Sherborn. Proc. Geol. Assoc, vol. xviii., pp. 1-52. SoMERVAlL, A. On the Base of the Keuper in South Devon. Geol. Mag., pp. 460-462; Ibid. 1904, p. 283. ■ Bep. Brit. Assoc for 1903, pp. 665, 666. SoMBRVAiii, A. The Red Rocks of the South Devon Coast. Trans. Devon Assoc, vol. xxxv., pp. 617-630. 1904. Irving, Rev. Dr. A. Further Notes on the Trias of Devonshire, with Special Reference to the Divisional Line betwen the Bunter and the Keuper in that region. Geol. Mag., pp. 166-172. Lang, W. D. The Zone of Soplites interruptus (Bruguiere) at Black Ven, Charmouth. Geol. Mag., pp. 124-131. 1905. Solly, Rev. H. S. The Landslip, Lyme Regis. Proc Dorset Nat. Hist. Club, vol. xxvi., pp. 182-186; 1906. Clayden, a. W. The History of Devonshire Scenery. 8vo., Exeter and London. Richardson, L. On the Rhsetic and Contiguous deposits of Devon and Dorset. Proc. Geol. Assoc, vol. xix., pp. 401-409. UssHER, W. A. E. The Geology of the Country between Wellington and Chard. Mem. Geol. Surv. 8vo., London. Woodward, H. B., and G. W. Young. Excursion to Lyme Regis. Proc Geol. Assoc, vol. xix,, pp. 320-340, 1907. L\NG, W. D. The Selbornian of Stonebarrow Cliff, Charmouth. Geol. Mag., pp. 150-156. 1908. Jukes-Browne, A. J. The Burning Cliff and the Landslip at Lyme Regis. Proc Dorset Nat. Hist. Club, vol. xxix., pp. 153-160. 1909. Cameron, A. C. G. On a Well-section at Ware House, near Lyme Regis, and the Fossils obtained therefrom. Geol. Mag., pp. 169-171, Thomas, H. H. A Contribution to the Petrography of the New Red Sandstone in. the West of England. Quart. Journ. Geol. Soc, vol. Ixv., pp. 229-245. 1910. MoNCKTON, H. W. The Dorset Coast In " Geology in the Field " : the Jubilee vol. of Geol. Assoc [Lyme Regis, pp. 382-389.] 96 INDEX. Abbey Gate Bridge, 75. Acanthoceras mammillatum, 47. Agassiz, Prof. L., 17. Agriculture, 86. Allen, H. A., 44. AUhusen, Miss H., 78. Alluvium, 72-74, 76, 77. Ammonite Marble, 28, 35. Ammonites, Names of, 23, 33. See also Zones. , Polished, 31. Angular detritus, 75. Anning, Mary, 4, 17, 31, 33. Annis' Knob, 57, 58. Anticlines, 14, 18, 20, 25, 30, 39, 66. Aplins Common, 76. Arches, Natural, 10, 12, 57, 80. Area, Character of, 1. Avicula contorta, 16, 17. Axe, River, 1, 2. 10, 64, 65, 74, 76, 78, 87. Valley, 39, 74-77. Axminster, 1, 3, 4, 19, 34, 39, 40, 49, 52, 66, 68, 69, 75, 76, 82-84, 88. Axmouth, 16, 17, 21, 47, 56, 76, 87. Bagshot Beds, 68. Barrels, Dr. C, 53, 93. Barytes, 14. Beaches, 2, 73, 76, 81. Beacons, 2. Beaminster, 74. Beef, 36, 37. Beekite, 40. Beer, 43, 45, 47, 54. 57, 66, 70, 74, 82, 84, 88. Head, 15, 48, 51, 56, 58, 59, 80, 82, 85. Stone, 54, 57, 61, 82. Beesley, Son and Nichols, 88. Belemnite Beds, 21, 22, 30, 35. Marl, 56. Stone, 30, 35. Berry Clifl, 51, 59. Bibliography, 4, 92. Bindon, 4, 23, 44, 47, 56. Landslip. 78, 79. Birchii-hei, 27, 36. Bishops Court, 7, 8. Bituminous Shales, 40, 86. Black Down, Portesham, 68, 69. Blackdown Beds, 4*, 46, 47, 49. Blackdown Hills, 1, 70, 72. Black Marl, 21, 22, 27, 35, 36. Black Shales, 16-18, 20. Black Yen, 21, 24, 27, 28, 29, 30, 31, 35, 36, 44, 45, 46, 47, 49, 80, 86. Beds, 21-23, 27, 35, 36. Blue Anchor Inn, 8, 9. Blue Lias, 21-23, 36-38. —— Lime and Cement, 83. Bolshayne, 76. Bone-bed in Upper Sandstone, 11-13 ; in Rhsetic, 16, 17. Bonehayne, 76. Boring at Lyme Eegis, 14, 20. See also Wells. Borings, Tubiform, 19, 20, 46. Bournemouth, 68. Bovey, near Beer, Well at, 70. Tracey, 68. Bradninch, 6. Brandy Head, 11. Branscombe, 48, 51, 54, 70, 74, 80-82, 85. Mouth, 15. Valley, 59, 84, 85. Breccia, Permian, 5. Siliceous, 67. Brecciated beds in Trias, 6, 10-12. Briarean Encrinite, 28. Brick Clay, 84. Brickyards, 40, 66. Bridport, 21. Brimscombe Farm, 62. Bristow, H. W., 17. Broadbridge Farm, Well near, 75. Broadhembury, 64, 85. Broad Ledge, 37. Broom, 75. ClifE, 22. Buckland, Rev. W., 4, 5, 28, 31, 33, 34, 67, 77, 79, 82, 92. Mrs., 92. Buckley Farm, 73. Buckman, S. S. 23. Buddie Valley, 77. Budleigh Salterton, 2, 5, 6, 8, 72. Building Stones, 59, 82. Bulverton, 8, 14. Hill, 49. Bunter, 5-14. Burning Cliff, 86. Burscombe, 73. Butter, Dorset, 87. Cain's Folly, 22. Calcareous springs, 76, 91. Cameron, A. C. G., 80, 86, 89, 90, 95. Carruthers, W., 34. Carstone, 47. Carter, Dr. H. J., 11, 12. Caves, 58. Cavities in Chalk and Greensand, 70. Celestine, 13, 14. Cement, 83. Stones, 29, 36, 83, 84. Cenomanian, 57, 60. INDEX. 97 Chalk, 53. ClifEs, 56. Marl, 57, 62. Rock, 56. Champernhayes Farm, 40. Chantrey, Sir Francis, 31. Chapel Rock, 56, 78. Chapplecroft Farm, 20, 76. Chard, 39, 70. Junction, 74, 75. Road, Well at, 87. Chardstock, 39, 52, 59, 62, 84. Charmouth, 3, 4, 22, 25, 27, 29, 33, 36, 45, 46, 69, 77, 80, 83, 84, 86, 88. Valley, 66. Charmouthian, 23. Charton Bay, 18, 21, 24. Clifes, 56.- Char Valley, 1, 77, 81. Cheddington, 74. Cheese, Dorset, 87. Chert, 61. Beds, 42, 44, 45, 69, 83. Implements, 75. Cbilson, 1. Chimney Rock, 78. Chit Rocks, 12, 13, 50. Chloritic Marl, 56, 62. Church ClifEs, Lyme Regis, 22, 24, 25, 28, 36-38, 80, 84. Clapperentale Farm, 8, 9. Clark, S., 23. Clay pellets, 8. Clay with Flints and Chert, 45, 63, 67, 70. Clayden, A. W., 52, 70, 77, 95. Clevelands. 56. Cliff-sections, 22, 50. Cloud-burst, 77. Clyst basin, 72. • William Farm, 6. Coal, Borings in search of, 3, 20, 40. Coast Erosion, 74, 77, 80. Cobb, the, Lyme Regis, 78, 83. Colaton Raleigh, Well at, 8, 90. Colliton, 63, 64. Colway Manor House, 20. Coly, River, 74, 76. Colyford, 76. Colyton, 75, 88. Combe Raleigh, 88. Wood, 70. Combpyne, 68, 69, 71, 77. Concretions, 8, 13, 14, 16, 19. See also Nodules. Conger Pool, 12. Conglomeratic bed in Upper Green- sand, 47, 48. See also Pebbles and Pebble Beds. Conybeare, Rev. W. D., 4, 5, 17, 33, 40, 47, 79, 80, 92. Cook, Rev. S. H., 13. Coprolites, 16, 34. See also Phos- phatic Nodules. Core Hill House, 73. Coryton Park, Boring at, 90. Gotham Marble, 16, 18, 19. Cotleigh, Well at, 89. Couchill, 66, 85, 88, 89. Cowstones, 42, 44-46, 83. Coxe's Cliff, 51. Crammer Barton, 8. Crawford, Mr., 89. Cretaceous, 2, 42, 53. Plain, 2, 63. Crick, G. C, 31. Culm basin, 72. Measures, 3. Culverhole Point, 15, 16, 18, 21, 23, 24, 47, 79, 80. Cuthays, 52. Cycad-remains, 34. Dairy Farms, 87. Dalwood, 20, 52, 63, 66. Dane's Hill, 20. Dapedius, 4, 34. Dartmoor, 69. Davcsi zone, 32. Dawlish, 5. Dawson, W., 80, 92. Day, B. C. H., 23, 31-33, 93. De la Beche, Sir H. T., 4, 5, 15, 17, 23, 24, 30, 34, 36, 42, 44, 53, 65, 66, 68, 70, 76-78, 82, 83, 92. Denudation, 3, 4, 74, 80. De Ranee, C. B., 44, 46, 47, 93. Devil's Bellows, 80. Devon, 1. Devonian fossils, 7. Devonshire Batts, 85. Point, 37. Diluvial action, 4. Diluvium, 77. Doggers, 41, 48, 49. DoUin, Mrs., 26. Dorset, 1. Dotton Lane, Boring at, 8, 90-91. Dowlands, 4, 23, 47, 56. Landslip, 79. Down Cliff, 41. Downes, Rev. W., 27, 44, 46, 52, 80 94. Downwash, 71-73, 75, 76, 86, 87. Dragon Hill, 88. Drift deposits, 67, 72. Dumpton Hill, 64. Dunscombe, 48-50, 82, 83, 91. Dunscombe Farm, 59. D'Urban, W. S. M., 75, 93. Earthquake, Supposed, 79. Echinoderm Spines, 24, 38. Economic Geology, 82. Bgerton, Sir P., 17, 33, 34. Elephant remains, 74, 77. Elton, A. M., 61. Enniskillen, Earl of, 33. 98 INDEX. Eocene, 1, 2, 67-69. Erosion of Coast, 80. See also Denu- dation. Eryon, 33. Esoot, 8. Esplanade, Lyme Regis, 25, 36. Etheridge, R., 17, 23, 46, 47. Evans, Sir J., 93. Exe River, 74. Exeter, 5. Exmouth, Eype, 21. PairmUe, 7, 8, 72. Farway Hills, 88. Street, 76. Faults, 63 ; in Cretaceous, 15, 47, 60-62 ; in Lias and Rhsetic, 16, 18, 20, 22, 24, 27, 30, 32, 39 ; in Trias and Permian, 6-15. Feniton, 7. Fern Hill, 88. Firestone, 60. Nodules, 27, 36. Fishes, 16, 17, 33. Fitton, Dr. W. H., 42, 47, 60. Flagstone, 83. Flint fossils, 55. Floods, 73. Forbes, E., 18. Porde Abbey, 40, 85, 87. Farm, 3. Fordhayes, 85. Formations, Table of, 2. Fossil Collectors, 3, 23. Fossils in Bunter pebbles, 7 ; in Upper Sandstone, 11-13 ; in Rhsetio, 16- 20 ; in Lias, 21-41 ; in Greensand and aault, 42-49, 52 ; in Chalk, 53-62 ; in Valley Drift, 74, 77. Freestone, 61, 62, 82. Pounders, 78. Poxmould, 42, 44, 45, 47, 48. Furley, 20, 62. Purzeley, 88. Gault, 42, 44, 46, 47, 49, 52. Geikie, Sir A., 5, 18, 19, 23. Geodes, 13, 14. Geological Survey, 4. Geoteuthis, 31. Gilchrist, D. A., 87. Gittisham, 1, 63, 65, 88. Hill, 65. Glacial Period, 70. Glauconitic Beds, 42, 45, 57, 58, 61. Godwin-Austen, R. A. C, 42, 48, 67, 70 74 92. Golden Cap,' 21', 22, 30, 32, 35, 40. - Goyles, 2, 71. Gravels, Plateau, 67 ; Flint fossils in, 55. Valley, 72. Great Cleft, 78. Great Trill, 84. Greatwood Farm, 20, 16. Green Ammonite Beds, 21, 22, 31, 35. Greendown, 20. Greensand, 42. Grey Ledge, 37. Marls, 17-20. Greywethers, 67, 71. Griggs, 73. Grizzle, 60, 61. Grover, C. W., 77, 89. Gully, Rain, 77. Gun Clife, 25, 36. Gun Flints, 85. Gypsum, 14, 15, 20, 85. Haldon, 68. Hamlet, 72. Hampton, 75. Haroombe, 73. Hard Marl, 24, 36, 84. Hardown Hill, 45, 69. Harner Hill, 20. Harpford, 8, 10. Harrison, J., 33. Hasland Farm, 20. Haven Clife, 15, 56, 57. Hawkchurch, 3, 39, 40, 52, 74, 75, 85. Hawkms, T., 19, 77. Hayoraft, G., 20. Heavitree, 5. Heights, 1. Hembury Port Hill, 1, 64. Hern Rock Point, 12. Higher Bathams, 75. Dunscombe ClifE, 50, 59. Tale, 6. Highgate, 49. High Peak, 12, 50. Hill & Sons, G. H., 90. Hill, W., 53, 57, 94. Hinde, Dr. G. J., 61. Hinxman, L. W., 69. Hole, 70. Farm, 88. Holcombe, 77. Hollow Grove, 88. Home, Sir E., 33. Honiton, 44, 59, 60, 64, 72, 75, 85, 88, 89. tunnel, 52. Hood, 19. Hook Ebb, 14. Hooken Cliffs, 51, 58, 59, 80, 82. Hooper, D., 61. Hull, Prof. E., 5, 6, 13, 94. Humble Green, 18, 47. Hunter, L, 23. R., 23. Hutchinghayes, 88. Hutchinson, P. 0., 10, 12, 13, 14, 73, 74, 81, 85, 88, 91-94. Huxley, Prof. T. H., 31, 46. Hyperodapedon, 11, INDEX. 99 Ichthyosaurus, 4, 33. Industries, 2. Ink-bag, Fossil, 31. Inliers of Rhsstic Beds, &c., 19, 20, 39. Iron-shot Greensand, 71. Ironstone, 8, 41. Irving, Eev. Dr. A., 5, 6, 10, 13, 14, 94, 95. Jet, 30. Johnston-Lavis, Dr. H. J., 12, 93. Jukes-Browne, A. J., 14, 18, 20, 42, 44, 46-50, 52-57, 59, 61, 62, 67, 70, 78, 80, 82, 86, 94, 95. Jurassic, 2, 21. Kempstone Rocks, 48, 59. Keshill, 6. Keuper, 2, 5, 14. Basement-beds, 6, 12, 14. Kilmington, 75. Koenig, C, 33. Lahyrinthodon, 12, 13. Lace-making, 2. Lade Rock, 12. Ladram Arch, 10, 12. Bay, 10-12. Laminated Beds, 22, 41. Landscape Stone, 16, 18. Landslips, 58, 73, 75, 76, 78. Lang, W. D., 31, 44, 46, 95. Lapparent, A. de, 23. Lapworth, Prof. C, 7. Larkbeare, 6 Lashbrook Farm, 8. Lias, 21, 82. Lignite, 28, 30, 37. Lime-burning, 82-84. Limestones, Detrital, 18, 27. Lithodomus, 48. Little Beach, 48. Littlecombe Hollow, 51. Shoot, 15. Little Weston, 91. Loam, 73, 76. Lower Chalk, 54. Dunscombe Olifl, 50. Greensand, 42, 47. Lias, 21. Marls, 6. Sandstone and Breccia, 5, 6. Luxmoore, Dr. C. M., 87. Lyme Cobb, 78, 83. Regis, 3, 4, 14, 16-18, 20-22, 25- 27, 80, 31, 33, 34, 38-40, 42, 44-47, 49,53, 56, 68,70,71, 74,75,77-83, 85-89. Beds, 21-23, 36-38. Lym Valley, 1, 77. 18821 Macindoe, Dr. A., 88. Mammoth, 74, 77. Manganese-ore, 68, 69. Manston Farm, 84. Maroasite, 86. Marder, J. W., 23. Market-towns, 1. Marl, 84. Marls, Permian and Triassic, 5. Marlstone, 41. Marsh wood, Yale of, 1, 87. Marston Magna, 28. Marsupites, Zone of, 55. Masey, P. B., 82. Maton, W. G., 4. Melbourn Rock, 62. Membury, 20, 34, 52, 59, 62, 65, 76. Metal Bed, 35, 86. Metcalfe, A. T., 13, 94. Meyer, C. J. A., 23, 42, 44, 47-49, 53, 93. Micraster, Zones of, 55. Middle Chalk, 54, 55. Lias, 21, 40. Midford Sands, 21. Mincombe Farm, 73. Minerals, 7, 8, 10-15, 20, G8, 69. Mineral springs, 76, 91. Miocene, 68. Mivart, Dr. F. St. G., 88. Monckton, H. W., 95. Monkton Barton, 72. Moore, C, 17. Murchison, Sir R. I., 5. Murchisonite, 8. Musbury, 75. Castle, 19. Mutter's Moor, 88. New Red Sandstone Series, 5. Newton, E. T., 16, 26, 32, 55, 57. Newton Abbot, 68. Poppleford, 72. Nodules, 8, 13, 14, 27, 42, 54, 57 ; Green-coated, 56, 61. See also Con- cretions. Northleigh, 63, 76. Northmostown, 10. Ofiwell, 59, 63, 64, 75-76. Oligocene, 68. Ophioderma, 41. Oppel, Dr. A., 17, 23, 32, 92. Orchards, 86. Ordovician fossils, 7. Otter, River, 11. valley, 72-73. Otterton, 72, 73, 84. Point, 6, 10-12, 73. Ottery St, Mary, 2, 6, 7, 9, 10, 73, 85, 86 ; Wells near, 90. Overlap and Overstep, 3, 59, H 100 INDEX. Palaeolithic Implements, 75. Palaeozoic, 2, 3. Pan, 8. Paper-shales, 24. Parfitt, E , 94. Pass, A. C, 20. Passaford, 10. Passage-beds, 15, 17, 20, 21. Path Hill, 73. Paving-stone, 82, 83. Payhembury, 6, 9, 63, 85, 90. Peak Hill, 14, 48-50, 71, 81, 88. Peat, 73. Pebble-bed at base of G-ault, 46-48. Pebble Beds (Trias), 7. Pebbles in Chalk, 53, 54, 56, 61 ; in Upper Greensand, 47, 48 ; in White Lias, 16, 19. Peneplains, 3. Pengelly, W., 15, 93. Pentacrinite Bed, 28, 35. Pentacrinites, 24, 25, 41. Penn Hill, 71. Perceval, S. G., 14. Peroival, Prof. J., 87. Permian, 2, 5. Petrifying springs, 76, 91. Phillips, Prof. J., 31. W., 17, 40. Phosphatic nodules and fossils, 16, 34, 54, 56, 57. Picket Rock Cove, 12. Pinhay Bays 16, 18, 19, 21, 22, 24, 36-38, 47, 56. ClifPs, 54, 56, 78. Pinhoe, 85. Pinnacles, 58, 78, 82. Pinney Bay, 18. Pinn Hill, 88. Pipe-clay, 68. Pipes in Chalk and Greensand, 70, 71. Pisolitic iron-ore, 71. Plains of Denudation, 3. Plant remains in Trias, 13 ; in Lias, 34. Plastic Clay formation, 67, 68. Plateau deposits and faults, 3, 63, 67. Pleinsbaohian, 23. Pleistocene, 2, 67, 72. Plesiosaurus, 4, 33. Plyford Farm, 73. Poole, 68. Popples, 72. Population, 2. Portesham, 68, 69. Pottery, 85. Pounds Pool, 53. Pterodactyl, 33. Pyrites, 35, 86. Pyritic fossils, 26, 28, 31. Quartz grains in Chalk, 53, 54, 56. Quartz pebbles, 61, 67. Quartzite pebbles, 7, 67. Quenstedt, F. A., 23. Railway-cuttings, Axminster and Lyme Regis, 19, 68, 75, 76 ; Honiton, 52 ; Sidmouth, 8, 10. Rainfall, Destructive effects of, 77. Rainwash. See Downwash. Raymonds Hill, 64. Recent, 2, 72-77. Red clays, 68, 70, 75, 76. Reid, C, 20, 45, 46, 49, 52, 62, 68, 69, 75, 76. Mrs., 68. Rhgetic, 16. Rhinoceros, 74, 77. Rhodes, J., 62. Richardson, L., 16-18, 95. Ridge Cliff, 22. Ring-in-the-Mire, 88. Ripple-marks, 12, 13. River Gravels, 72. Rivers, 1, 2, 72-77. Road, Lyme and Charmouth, 80. Road Metal, 85. Roberts, G., 4, 25, 70, 80, 87, 92. Rockbeare Hill, 6. Rock-salt, Pseudomorphs of, 12-14. Bothe-todte-liegende, 5. Rousdon, 18, 56, 77 ; "Well at, 89. Rowe, Dr. A. W., 53-57, 78, 95. Ruegg, L. H., 86. St. Cyres Hill, 1, 64, 88. Gabriel's Water, 30, 32. Salcombe, 50, 73, 83. Cliff, 48. Hill, 50, 67, 70, 71. Mouth, 14, 74, 91. Salston House, 72. Salter. Dr., A. E., 75, 94. J. W., 7. Salter's Cross, 49. Salt-marshes, 76. pans, 76. Sandeoombe, 73. Sands, Economic uses of, 60, 61, 75, 85. Sarte, 20. Saurians, 33. Scapheus, 26, 37. Scenery, 1-3, 74, 78. Schorl-rock, 75. Scythe-stones, 85. Seaton, 3, 15, 21, 42-45, 47, 57, 66, 75, 89 ; Boring at, 90. Bay, 80. Hole, 47. Seatown, 30, 32. Selbornian, 2, 42. Selenite, 15, 19. Sepia, Fossil, 31. Seven Rock Point, 24. INDEX. 10] Seward, Prof. A. C, 34. Shapwick Hill, 71. Sharman, G., 26. Sharpe, D., 42. Sherborn, 0. D., 53, 95. Sherwood Farm, 7. Shingle, 81. See also Beaches. Shools Farm, 75, 76. Shorne Cliff, 22, 30. Shute, 63. Hill, 64, 69, 83. Sidbury, 73, 88. Sidford, 73, 84. Sidmouth, 3, 5-8, 13, 14, 42, 45, 48, 50, 67, 70, 73, 74, 80, 84 ; Wells and Water-supply of, 73, 88. Pebbles, 67. Sid, River, 1, 13, 14, 50, 73-74, 84. Siliceous breccia, 67. nodules, 57. Silicified fossils, 46, 48, 49. Skertchly, S. B. J., 85. Slade, 63. Smith, W., 53. Soil-movements, 75. See also Down- wash. Soils, 86. Solly, Rev. H. S., 95. Somerset, 1. Somervail, A., 95. Southleigh, 76. Sowerby, 33. Spiller, J., 84. Sponge -spicules, 61. Spontaneous Combustion, 86. Springfield, 88. Springs, 27, 76, 87, 88, 91. Stacks, 80. Staple Hill, 1. Starfish Bed, 41. Staurolite, 10, 11. Stauronema, 54, 56. Stephens, J., 86. Stookland Hill, 64. Stonebarrow Beds, 21. 22, 30, 35. Cliff, 27, 29-32, 35, 36, 40. Stone-beds, Names of, 35-38, 83. Storridge Hill, 62. Stowford, 63. Strahan, Dr. A., 18, 44, 48, 49, 50, 92. Straightgate Farm, 6. Straightway Head, 72. Streams, Disappearance of, 76. Subaerial Erosion, 69, 77, 80. Submerged Forest, 74, 77. Subsidence, Recent, 74. Subterranean Erosion, 75, 78. Sully Beds, 18. Sun Bed, 19. Sutton quarries, 59-61, 82. Synclines, 13, 25, 43, 66, 80. Table of Formations, 2. Table Land, 1, 3, 63. 67. Table Ledge, 24, 25, 36. Talaton, 6, 8. Tale, River, 72, 73. valley, 8, 86. Talewater, 84 ; Well at, 8. Tea-green Marls, 17. Teall, Dr. J. J. H., 18. Teignmouth, 5. Tertiary, 67, 68. Plain, 3, 63, 69. Thistle Hill, 40, 71. Thomas, H. H., 7, 10, 14, 69, 94, 95. Thorncombe Beacon, 40, 41. Three Tiers, 22, 40, 41. Tilley, Messrs., 90. Timber Hill, 22, 27, 46. Tipton St. John's, 10, 73. Tolcis Farm, 20. Tortoise Ammonites, 27. Towns and villages, 1, 2. Trias, 2, 5. Trill, 19, 84. Trow Hill, 73. Tucks, 26. Tufa, 76. Turonian, 60. Tytherleigh, 62. Uffculm, 63. Umborne Brook, 64, 74. Unconformities, 3. Undercliffs, 78. Uplyme, 19, 39, 64, 66, 77, 82-84, 88 ; Well at, 90. Upper Chalk, 54, 55. Greensand, 42, 44, 45. Lias, 41. Marls, 2, 5, 14. Sandstone, 2, 5, 8. Ussher, W. A. E., 5, 7, 9, 26, 49, 52, 64, 65, 70-72, 90, 93-95. Vale of Marshwood, 1, 87. Valley Deposits, 72. Valleys, Origin of, 4, 65. Vancouver, C, 85, 86. Variegated Marls, 14, 16. Vicary, W., 7. Vivian, Messrs., 20. Volcanic eruption. Supposed, 86. Wadbrook, 75. Wambrook, 66. Ware Cliffs, 22, 44, 46, 56, 78. , Well at, 89. Watch-stone Beds, 35. Waterside, 90. Waterstones, 14. Water Supply, 87. Wear Cliff Beds, 21, 22, 31, 35. 102 INDEX. Wells and Borings, 87-91 ; see uho 8, 19 70 75 87. West Cliff, 21, 25, 27, 33, 36-38, 84. Westford Farm, 75. Westgate Hill, 65. Westhay Cliff, 22, 35, 40. Weston Mouth, 14, 15, 51, 74, 85. Westover Farm, 87. Weycroft, 39, 75, 83, 84 ; Well at, 19. Whitaker, W., 11, 59, 68, 89, 92, 93. White Ammonites, 27. White clay, 68. Whitecliff, 15, 43, 45, 48, 54, 57. White Lias, 16-20, 83, 84. White limestones in Lower Lias, 19, 39. White Rock, 20, 39, 83. Whitlands, 47, 56, 78. Whitley, N., 93. Wickes, W. H., 17. Widworthy, 59-61, 63, 64, 82. Wilmington, 52, 57, 59-61, 67, 82, 85. Wilson, G., 18. Windgate (Windygate), 12, 13. Wolversleigh Farm, 63, 73. Woodbeer, 6. Woods, H., 44. Woodward, Dr. A. S., 34. Dr. H , 33, 37. Woolbrook, 73. Worm-tubes, 46. Wright, Dr. T., 19, 23, 24, 26, 32, 35- 37, 39, 41, 83, 93. Wyld Warren 52. Xiphoteuthia, 31. Yarty, River, 1, 74. valley, 65, 66. Yawl limekilns, 19, 39, 84. Young, G. W., 56, 78, 95. Zone of Actinocamax plenus, 54. the Ammonite species : angulata, 21, 23, 38 ; armatum, 21, 30, 35 ; huchlandi, 21, 23, 37, 38 ; capricornus, 21, 31, 35 ; davcei, 32 ; henleyi, 21 , 31, 35 ; interruptus, 42, 44 ; jamesoiii, 21, 30, 35 ; mammillatum, 47 ; mantelli, 54 ; margaritaius, 41 ; oltusum, 21, 27, 35, 36 ; oxynotum, 21, 27, 35 ; planorbis, 21, 23, 38 ; raricosiatum, 21, 27, 35 ; rostrata, 42, 45 ; semi- eostatitm, 21, 23, 36 ; spinatum, 41 ; turneri, 26 ; varians, 54. Avicula {Pteria) contorta, 16, 17. Holaster planus, 54, 55. H. subglobosus, 54. Mlarsupites, 55. Micraster, 54, 55. Pecten asper, 42, 44. • Rhynchoiiella cuvieri, 54, 55. Terebratulina, 54, 55. Stauronema carteri, 54. Zones in Chalk, 53-55. Greensand and Gault, 42, 44. Lower Lias, 21. — — Middle Lias, 41. ONE-INCH MAP, OLD SERIES (Itach to the mile, or 1 to 63360). 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