Saba teats Bye ses 3: a rend cos SS qa8> Na 1 oe 23 6S AMI SE POTS > Lu o < na O rg =) a > on a W ea iu O WW ng chs 4 ¥ Ane foe, ea hie ‘ ay Digitized by the Internet Archive in 2011 with funding from California Academy of Sciences Library http://www.archive.org/details/transactionsof251836geol i i " ' / 1 y ls Pm Fe F i ¥ ; iia i i ( { ) i iy Opal 4 el yaar a! ae ; a TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. SECOND SERIES. VOLUME V. PART THE FIRST. Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque iis uti, sed ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. Novum Organum, Prefatio. LONDON: PRINTED BY R. AND J. E. TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1837. mae Ethie “or AT aan HOODY faRDLI ONO HHP 40 er it w) ane JEySI rar dauoe ~~ me. o | OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY OF LONDON. 1837. PRESIDENT. Rev. WILLIAM WHEWELL, M.A. F.R.S. VICE-PRESIDENTS. Rev. WILLIAM BUCKLAND, D.D.: F.R.S. F.L.S., Professor of Geology and Mineralogy in the University of Oxford. WILLIAM HENRY FITTON, M.D. F.R.S, F.L.S. GEORGE BELLAS GREENOUGH, Esq. F.R.S. F.L.S. RODERICK IMPEY MURCHISON, Esq. F.R.S. F.L.S. SECRETARIES. ROBERT HUTTON, Esq. M.P. M.R.I. A. JOHN FORBES ROYLE, M.D. F.R.S. F.L.S. Professor of Materia Medica and Therapeutics in King’s College, London. FOREIGN SECRETARY. HENRY THOMAS DE LA BECHE, Esq. F.R.S. F.L.S. TREASURER. JOHN TAYLOR, Esq. F.R.S. COUNCIL. FRANCIS BAILY, Esq. V. P. & Treas. R.S. F.L.S. WILLIAM JOHN BRODERIP, Esq. F.R.S. F.L.S. WILLIAM CLIFT, Esq. F.R.S. Viscount COLE, M.P. D.C.L. F.R.S. CHARLES DARWIN, Esq. CHARLES GILES BRIDLE DAUBENY, M.D. F.R.S. & F.L.S., Regius Professor of Botany, and Aldrich’s Professor of Chemistry in the University of Oxford. Sir PHILIP DE MALPAS GREY EGERTON, Bart. M. P. F.R.S. HENRY HALLAM, Esq. F.R.S. LEONARD HORNER, Esq. F.R.S. L. & E. CHARLES LYELL, Jun., Esq. M.A. F.R.S. & F.L.S. Marquis of NORTHAMPTON, F.R.S. Sir WOODBINE PARISH, K.C.H. F.R.S. Rey. ADAM SEDGWICK, F.R.S. F.L.S., Wood- wardian Professor in the University of Cam- bridge. HENRY WARBURTON, Esq. M.P. F.R.S. & F.L.S. CURATOR ano LIBRARIAN, WILLIAM LONSDALE, Esq. ADVERTISEMENT. THE Editors of the Transactions of the Geological Society are directed to make it known to the Public, that the Authors alone are respon- sible for the facts and opinions, contained in their respective papers. It ts requested that all letters and communications to the Secretaries, and presents to the Society, may be addressed to the Apartments of the Geological Society, Somerset House, London. II. Ill. IV. VI. VIE CONTENTS. PART I. . On the Geological Relations of the South of Ireland. By 'Thomas Weaver, Esq. F.G.S. F.R.S. MRL. A. On the Geological Structure of the North-eastern Part of the County of Antrim. By James Bryce, Jun. M.A. F.G.S. (Member of the Geological Society of Dublin, and of the Natural History Society of Belfast.) . : : : : : : : ‘ 2 pe On the Squaloraia. By H. Riley, M.D. (Communicated by Charles Stokes, Esq. F'.G.S.) < : : : : : : eps Notes on the Geology of the North Coast of the St. Lawrence. By Capt. Bayfield, R.N. F.R.A.S. (Communicated by George Bellas Greenough, Esq. P.G.S.) . ; : 4 j ‘ : ah ot On the Geology of the Bermudas. By Richard J. Nelson, Esq. Lieut. R.E. (Communicated by George Bellas Greenough, Esq. P.G.S.) p. Notes on the Geology of the Brown Clee Hill, in the County of Salop. By Romley Wright, Esq., Employed on the Ordnance Trigono- metrical Survey of England. . : : : : : . Pp. Observations on the Geological Structure of the Neighbourhood of Reading. By J. Rofe, Jun., Esq. (Communicated by Robert Hunter, Esq. F.G.S8.). —. ; : ; ; : : i joe 89 103 VEIT. XI. XII. XIU. XIV. XVI. XVII. XVIII. CONTENTS. Observations on a Well dug on the South side of Hampstead Heath. By Nathaniel Thomas Wetherell, Esq. F'.G.S. p- Observations on the Strata penetrated in sinking a Well at Diss, in Norfolk. By John Taylor, Esq. Treas. G.S. . . On the Structure of the Neighbourhood of Gamrie, Banffshire, par- ticularly on the Deposit containing Ichthyolites. By Joseph p- Prestwich, Jun., Esq. F.G.S. . ‘ : : : ; nine Notices on the Geology of the North Coast of the Counties of Mayo and Sligo in Ireland. By Archdeacon Verschoyle, M.A. (Com- municated by Roderick Impey Murchison, Esq. P.G.S.) Description of some Fossil Crustacea and Radiata, found at Lyme Regis, in Dorsetshire. By William John Broderip, Esg. F.G.S. p- Peek. VPLS. ee | ee On the Bones of Birds discovered in the Strata of Tilgate Forest, in Sussex. By Gideon Mantell, Esq. LL.D. F.RS. . ‘ + Ais On the Syenite Veins which traverse Mica Slate and Chalk at Good- land Cliff and Torr Eskert, to the south of Fair Head, in the County of Antrim. By Richard Griffith, Esg. F.G.S. M.R.LA. P.G.S. of Dublin . : : f 2 : A . . 3 aD . On certain Peculiarities in the Cervical Vertebre of the Ichthyo- saurus, hitherto unnoticed. By Sir Philip Grey Egerton, Bart. MOP PGS. Notes to accompany a Geological Map of the Forest of Dean Coal- field. By Henry Maclauchlan, Esq. F.G.S., Employed on the Ord- nance Trigonometrical Survey . Notice respecting a Piece of recent Wood, partly petrified by Carbon- ate of Lime, with some Remarks on Fossil Woods. By Charles Stokes, Esq. F.G.S. Remarks on a Section of the Upper Lias and Marlstone of Yorkshire, showing the limited Vertical Range of the Species of Ammonites p- p- 131 137 139 149 171 187 . 207 CONTENTS. and other Testacea; with their Value as Geological Tests. Louis Hunton, Esq. (Communicated by J. F. Royle, Esq. F.G.S.) p. By XIX. On the Distribution of Fossil Remains on the Yorkshire Coast, from the Lower Lias to the Bath Oolite inclusive. By W.C. Williamson, Esq., Curator of the Manchester Society of Natural History XX. On the Cretaceous and Tertiary Strata of the Danish Islands of See- land and Moen. By Charles Lyell, Esq. P.G.S. F.R.S. Sc. p- p- XXI. Notices and Extracts from the Minute-Book of the Geological Society . 1. Observations on the Cliffs in the Neighbourhood of Harwich, made in December, 1832. By James Mitchell, LL.D. F.G.S. [Read May 15, 1833.] 2. Notices of the Red Marl and Lias of Worcestershire; of a Fault by which they are affected; and of Fossil freshwater Shells at Shotover Hill. By Hugh Edwin Strickland, Esq. F.G.S. [Read December 4, 1833.] . 3. Notice of the Analysis of a Mineral Water from the Island of St. Paul, in lat. 38° 45’ §., and long. 77° 53! E. By John Bostock, M.D. F.G.S. [Read January 7, 1835.] 4. Notice of Fossils found in the Bognor Rocks. By Woodbine Parish, Jun., Esq., Sec. G.S. {Read January 7, 1835.] 5. Extract from a Letter addressed by Dr. Daubeny to the Cura- tor, on a saline Spring near Oxford. [Read June 10, 1835.] p. 6. Notice of a Letter on the Earthquake in Chili, November 19th, 1822, addressed to Capt. Belcher, R.N. F'.G.S. by H. Cuming, Esq., dated March 5th, 1835. [Read Dec. 2, 1835. ] p- Pp: p- p- p- p- 215 243 259 260 . eaten. te. ed oR, Se © ¥ wo n the : ‘the Blackwater River evtending fiom the Neagles M®on Mac Gillicuddys Recks on the W__Taken trom Drumskeha , about A Miles SW. trom Konturke and 3 Miles North of the Blackwater, : | These tee Views 9 ant & | combined extend through the prinapal Mountain Chain ian the South of Ireland.) . 1 South SW - : : Musherry fice, ‘ eis eH oes tn ae Musheragh — aaah ultaghaneesh The Pape \ ® ry = Mangerton Maw Gillicwddve Rocke . ae ; SECTIONS rHRrovUGH THE SOUTH OF TRELAWND MV! Gallan Fmis a Carboniferous Limestone a, Gurvane Taal 2 Broadtord Kilmeady Hill erboniferons Limestone Ola Red Sandstone me “the roug Countie Greywacke Blackwater R. Trans Gon Lime st Macroom Jineckmildown Mountains a NZ. ye Cashmore (East of Section | Zé = ees O1d Red Sandstone ¥ ay eens ORS coe Pe Oi = as ¥ a ee > Sn = oO 0 Ob { ough fro m uaF, O NE < % N° CO Ke ct Rom wehtough the Dro magi C gael wield Prone eo a + | Scale 80 feet to One Inch | : ’ = & x Del wy t at Grared ) Diluvial Gravel . - Line of Adit’ Level = wee ‘ "Pat = os = es ™ . v's as a, Sa i in a Explanation of the abbreviations __r. stands for compact gritstons or sarutstone rods, sltor slaty rode or shale « =. tar blade shale . sandy slate ar slate day ia OE tee of Merrdcin, aad Bp ranges fom the Mullaghanmely on. the Bast'to' the Cuhirconree on the West__ Talkiy | Clay Slate Sherri?’ Old Red Sandstone Carbonifercns Limestone 2 Old Read Sandstone Lough Slieve Meesh O14 Kel Sandstone Kerry Head O14 Ned Sanderone ferons Limestone Kilmeady Hill 4 Old Red Sand«et one OLA Red Sander Carboniferous Limestone Genter’ a Xx: ETO CECT e TK into Tipperary SMe to Primary Transition Series Carboniférons Series X. Gy ster GrevwackeSlate ke (0 Rat Sandstone Carboniferous Limestone Ee eee GR Zircon mD? (FF) Grtioniterons Limest. RR 01 Birman Distances ¢—— : = f 0 2 Miles: or 10.300 fet t0 an Tne a —— we i 215 Miles on 7020 feet to aT Heiglite j————— a : it Scale of the Sections I to 5. ee CEOMDIEE GEL a Fr om, Sapa h Toa iar Be fala aa {7 ( Scale 80 fect to One Inch ) : esl for slaty rock or shale ; «tor blade shale . sandy slate or state day - ¢.tir coal or cut . . y ye ee Sound pen Bay 8 Sout, ltnare %@ 1 Transition Series & | Grevwacke & Slate &e GEOLOGICAL MAP feo Limestone in DE has wv sda Gurbontterous Sertes SOUTH or IRELAND ame Soe ES arse BY : ss Be: as ; , Ey. Rad Sandstone Lm | eerbematinnes Limestone T. Weaver Esq’ PGS. ERS. MRIA &e. Loop Head, 7 ee “Bihan BR « 0 x J? Tralee Bay 4 . Sinn Blarney Glanmuve) € “yes > ; GEOLOGICAL MAI Tracts im which prevail = ne Cusloe Bay r. ; 2 P 7 ms J f } Ne { de ‘ , ar a amr Eog FOLENS. MRA. Ss ; — ; ' ne . £ | nA J van . | tée = a [FD ror wevete & state cs aca Bak Sandstone Ee] Harboniterous Limestone 01 Fe rmetion Gea a ein BE 2 ee LM. Towns core mucrivel thar © IRELAND hy 1.—On the Geological Relations of the South of Ireland. By THOMAS WEAVER, Esgq., F.G.S., F.R.S., M.R.LA., &c., &e. [Read June 4, 1830, and November 18, 1835.*] CONTENTS. Introduction.—Form of the Surface ........ Re clan re Wea Face Stoo, Geological Relations, and Distribution of the Subject ...... ie Ne Os I.—Transition Series. In Kerry, Cork, and Waterford ; disposition, eran Ts 7 to 33. SEMUCtUTE, GCs este Teidcecie wis EDahat aie svevace Sea Organic remains in the slate,..§§. 12, 19, 24, 26, 30. Ditto in the limestone........ sad afiate §§. 21 to 33. Metalliferous Relations :...06..000seccecese - §§. 34 to 46. In the Greywacke and Slate districts §§, 34 to 41. In the Transition Limestone ...... §§. 42 to 46. * It may be useful to point out in what particulars the present memoir differs from its prede- cessor, which was read June 4, 1830, reference being had to the Table of contents in the Memoir. The delay in finally preparing the paper has arisen from the Author's stay in Mexico and the United States from 1831 to 1834. In §§. 1 to 6, the Introductory part and general distribution of the subject have been remodelled in some respects. In §§. 7 to 20, the disposition, mineral characters, and organic remains of the greywacke and slate series stand nearly as before. In §§. 21 to 33, the details of the disposition, characters, and organic remains of the transition limestone are new for the greater part. In §§. 34 to 46, the metalliferous relations of the transition tract are much condensed, but in other respects as before. In §§. 47 to 68, the detailed disposition, characters, and organic remains of the South Munster carboniferous series are almost entirely new. In §§. 69 to 75, the same may be said of the North Munster carboniferous series, with the ex- ception of the “ coal formation” (§§. 71 to 75.), which stands nearly as before. In §§. 76 to 83, the metalliferous relations of the carboniferous series are mostly new; and partly also §. 84, on segregated metallic deposits in general. In §§. 85 to 89, the notices of Diluvial Action have been amplified to a certain extent, and ren~ dered more general with respect to Ireland. June 8, 1835. T. WEAvER. VOL. V.—SECOND SERIES. B rene en 2 Mr. Weaver on the Geological Relations of the South of Ireland. II.—Carboniferous Series. 1. In South Munster: viz. in Cork, Limerick, and) | Kerry; disposition, characters, and structure . ey §§. 47 to 68. Old red Sandstone, $§. 47 to 50. Carboniferous Limestone, extending in part into Waterford, §§. 51 to 57. Organic Remains, §. 57. 60. Coal formation, §§. 58 to 68. Organic Remains, §. 66. 2. In North Munster : viz. in Clare, extending in part into Galway; disposition, characters, and struc- > §$§. 69 to 75. {UITE. o's eee cceses wins eugie thipia hn elatsitalle ib tia oe Old red Sandstone, §. 69. Carboniferous Limestone. §. 70. Organic Remains, §. 70. Coal formation, §§. 71 to 75. (Note to §. 75, on the carboniferous series of the United States of North America.) Meftalliferous’ Relations : <. o/¢.cjs.ninneimieieinyn,< = (00 0.2.0.0, 070) e0:-70 WO OS, In the old red Sandstone, §. 76. In the carboniferous Limestone, §§. 77. to 82. In the Coal formation, §. 83. General observation on segregated Metallic Deposits........ §. 84 II].—Notices of Diluvial Action eoeereeree eee eee eeeeeeee §§. 85 to 89. In Kerry, §. 87; in Cork, Limerick, and Tipperary, §. 87; in Galway, §. 88; in Ireland generally, §. 89. > Introduction.—Form of the Surface. (1.) IN the following communication [ propose to give a sketch of the mineral constitution of the South of Ireland, including the county of Clare, and extending to the Bay of Galway. Connected with the description which I formerly gave of the Eastern portion of the Island*, the two memoirs will embrace about two thirds of the area comprised in its surface. In this, as in the former account, I shall confine myself to the more striking geological phenomena offered by the tracts described ; presenting occasional details in illustration, but avoiding all theoretical speculation. (2.) The annexed Map (see Plate 1.), with the sections drawn through dif- ferent portions of the tract (see Plate 1. figs. 1 to 5.), and the general views of * Geological Transactions, First Series, vol. v. p. 117 et seq., pl. 6 to 15 inclusive. Mr. Weaver on the Geological Relations of the South of Ireland. 3 the principal chain (see Sketches (a) and (b) in Plate 1.), may serve to illus- trate the general forms, structure, and connection of the mountain and hilly ranges with each other, In determining the geographical limits of the forma- tions I have endeavoured to be exact*. (3.) The Southern and greater portion of our field of inquiry, is composed of a transition tract ; its northern boundary being formed, both in the eastern and western quarters, by carboniferous limestone associated, more or less, with the old red sandstone ; while in the central part of the border, a coal country is found directly conjoining with the transition series. he old red sandstone both on the east and west, as well as in the northern portion of the field, attains to considerable elevation, passing in its descent beneath the more level surface of the carboniferous limestone ; and the limestone here, as in other parts of Ireland, is surmounted by an elevated and extensive tract of coal measures. * See the annexed Geological Map of the South of Ireland (Plate 11.). In this Map I have cor- rected a few particulars in the south-western extremity of my former Map of the East of Ireland. Both are drawn on the same scale. That the geological inquirer may more readily seize the connection between the East and South as well as with the North and West of Ireland, I have added a small skeleton map as an Index to the geology of the whole island (See Plate 1.). In this the principal formations are distributed in groups under the heads of the granite, mica-slate, clay-slate, greywacke and slate tracts, in which these rocks respectively predominate ; but greater detail is given to the carboniferous series, as its members generally appear in a distinct order of succession in the physical structure of Ireland. Then follow the new red sandstone, lias, greensand, and chalk, in one group, succeeded by the overlying trap as the last link of the chain, other formations later than the chalk appearing to be wholly wanting in Ireland. With respect to the North of Ireland, I have availed myself in these outlines, in aid of my own local knowledge, of the excellent memoir on the North-East of Ireland by Dr. Berger, the Rev. W. D. Conybeare, and Professor Buckland! ; and of the valuable Reports on the coal tracts of Connaught and Ulster by Mr. Griffith, to which works it may be sufficient to refer for the requi- site details. All that seems necessary on the present occasion is to indicate the prevailing forma- tions in the primary tracts of the West of Ulster and Connaught. In both of these the chief con- stituents are a base of granite, or syenitic granite, supporting mica-slate and quartz-rock, with pri- mary limestone, greenstone, hornblende-rock, hornblende-slate, and clay-slate. In Galway white imestone occurs in the mica-slate both in its simple form and intermingled with serpentine, in the latter case constituting a beautiful green marble. And in Donegal, in particular, the white limestone approaches to the character of statuary marble, apparently suited to the purposes of the sculptor. The geographical boundaries of the several geological groups will be readily apprehended by comparing the skeleton map with a common Map of Ireland ®. ‘ Geol. Trans., First Series, vol. iii. p. 121 et seq. * Geological and Mining Reports of the Connaught and Ulster coal districts. 3 The Public look with expectation to Mr. Griffith’s promised Geological Map of Ireland. B2 4 Mr. Weaver on the Geological Relations of the South of Ireland. _ (4.) The surface of the transition district consists chiefly of chains of moun- tains and hills, having generally a direction from W. to E.; and the principal, rising in Iveragh, south of Dingle bay, in the county of Kerry, attains its greatest elevation in Mac-Gillicuddy’s Reeks, thence extending eastward through the county of Cork between the rivers Lee and Blackwater*. The less elevated ranges being nearly parallel to this main chain and to each other, longitudinal valleys are inclosed between them, the course of which is indicated by the principal streams ; but as sinuous valleys, dells, and defiles traverse the chains, the region presents on the whole a considerably diversified aspect. (5.) All the elevations given in the following List marked (N.) were ascer- tained by the late Mr. Alexander Nimmof ; those derived from the Trigo- nometrical Survey of Ireland, marked (T.), I owe to the urbanity of Colonel Colby, R. E., by whose directions they were furnished to me by Captain Portlock, R. E. On the north side of Dingle Bay : Above level of sea. The Cahir-conrée and Slieve Meesh range is in the chief points ...... (N.) 2200 feet. But Bartrigoun, the highest point, is according to the Trigon. Survey.. (T.) 2784 While Brandon mountain, standing out on the N.and facing the ia (T.) 3120 tic, is, according to the Trigonometrical Survey ........ cee On the south side of Dingle Bay, in the Iveragh mountains : Knochadubber, facing the Bay.....eescecesecccccceccceseeresssess (N.) 2000 Drung, O,. « «ov pie: ince MARRS ener a cas sis cisisisiin ss 60 6 wen ass )-k ew Oe Bennettee, in the interior ....ccsccccscovccsesccccesccssessscves (N.) 1262 Knockalubrid, do..... sink often iets ate CeEHe cnasot se eeeevtowe wi ins) LOI Cullee, on the east...... oe Sine 6 oat aimtenin rete vastWe wane v's clpesse come (Na) O00 Kniockalin, on ‘the south, «< .o.ce's ce sede one sivicie sb eee a= ovece caer (Ns) 2150 Facing the north side of Kenmare Bay : In the Dunkerrin mountains the highest points vary from 1800 to .... (N.) 2000 The south of the Bay : The chief mountains rise, according to Mr. Nimmo, to a nearly equal DeiGhe fii s'si.'siSis wis wk » «ere pend ae ee er a we fipa nea - In Mac-Gillicuddy’s Reeks, extending toward the Lakes of Killarney : Gurrane Tual, which is the most elevated point, being also the highest land in Ireland, is accotding’'to Mr, Kirwanvidwevcus se cess Ay \ (K.) 5405 Mr.A. Nimmo) 057s ceases (N.) 3410 = the Trigonometiical Survey eee) on0% oo * For a view of this Chain, see Plate 1. Sketches (a) and (6). t+ See Reports to Parliament on the Bogs of Ireland. ¢ Smith in his Natural and Civil History of Kerry, p. 355, states that in the year 1756, at the entrance of Kenmare river, the magnetic variation was 17° W. At Ross Island, in the lower lake of Killarney, I ascertained the magnetic variation in 1829 to be 28° 45! W. Mr. Weaver on the Geological Relations of the South of Ireland. 5 Above level of sea, Purple MOwGtaw cee tcc os swe sna svesssnsecceclnansecses (N.) 2280 Tomies mountain......+e.s. LUSTER EMCO eLGreie ares aie oy shavace “eranelal ost. seve! (N.) 2150 Nes ane ER a SInTT catch roy cual creraiiateuacokcrzudiwreter ovtiacalivier cua bie 1016 «aie 6.0 s.0che (N.) 2090 Thinalk JRO UERLEN Rito Bie SIERELC ERD ICED Rr ORI OCROT CREO ICS eee (N.) 1900 Mangerton, according to Mr. Kirwan......++eeceeeescctenscceeees (K.) 2693 Mr. An. Nimmo. se eis a2 Beatie oi outlsciaisiss (N.) 2550 Beyond the Lakes : RO ACTTELIN AEE) CATIA EV TIAy visas ox cre’ ler kare suc snaneleteranel oie cellutath (a einushayiie) ate eiaifelSrere eisiv (N.) 2175 EAPO MOWBEAIIS:, a 0ie: ois v0. 0:n 9\0 4 0's eeieslae rede neye tet energeaeewsees (N.) 2280 MBrairrsiy Sc TVer en por sye eke ox ci Srers na kanexobokaineseisie Less cabeitewvus yortanoucteiereissue a sseteuad evaleve ane (N.) 2090 Gorfavehy, highest point......ccesscnecsescccencnnsivendiocecveves (N.) 1815 — eaoveny Gore Fone tensiotn aiatete ew) ate carte aainanate s oanera aeeees Mies ae vies (N.) 1500 Ecoereetea ama Gi ol ol diela aie el! oleiie wie el vialelluca aidleisliel oslelad ces sto an wie (N.) 1385 Minskeray, or Musheraghs.. so2.0ss0scccsescccnsebescccsodensces (N.) 1990 Thenceforward, through the Bogra and Neagles mountains, with the Wa- tergrass hills, spreading between the rivers Lee and Blackwater, and extending to the eastward, this principal range declines gradually in elevation. In the Neagles range, Knockbena Skeagh is, according to the Trigonometrical Sur- vey, 1388 feet above the sea. On the south of this main chain, and beyond the river Lee, high land still prevails, yet forming lower ranges, the surface of which is undulated from north to south ; but in the disposition of these ranges a similar declension in altitude from west to east is observable, the principal elevations being found adjacent to the west and south coast. Hungry Hill, on the north side of Bantry Bay, is, according to the Trigonometrical Survey, 2,249 feet above the level of the sea. . North of the parallel of the Lakes of Killarney and the river Blackwater, the coal country of the counties of Kerry, Cork, and Limerick presents more equally flowing outlines in its surface, which may be compared to a series of complex undulations upon a large scale, in which the higher portions vary be- tween 1000 and 700 feet, and the lower between 500 and 300 feet, above the level of the sea; but Tour mountain, situated in this tract north-west of New- market, is according to the Trigonometrical Survey elevated 1329 feet above that level. ~The boggy district between Killarney and Millstreet is, in the central parts, between 500 and 400 feet, and at the eastern and western extremities 300 feet; while the lower lake at Killarney is 50 feet, above the level of the sea, and in its deepest part 190 feet below that level, its extreme depth from the surface be- ing 240 feet. 6 Mr. Weaver on the Geological Relations of the South of Ireland. Proceeding more to the north, the following heights have heen determined by the Trigonometrical Survey of Ireland : Above level of sea. In the Waterford mountains, Monavoullagh (highest point) .......... 2590 feet. In the Knockanafrun, part of the same range..........00. a win ite wis 0 2469 In the Gaultees range, Gaultymore ......eeeeeeeecceee eesibees "5 3000 In the Tipperary mountains, the Keeper..........ccccccccstcccces 2265 the Devil's Bit « viisis.4.5 «/sins oe eee 1572 In the Limestone Plain of Limerick, Knock Dirk .............eseees 477 — ———— Knockfeernagh....... 00.000 0ee . 937 In the'hills of Clare, Craig . 0s av unves0b saw uns= 0 semee ance annwie 1715 Knockaniess sc cges ees ccepenenccce ss seed aning j 1305 —_——_ Callan....... o ccreee idle ev releSwisle css s sciae ae 1297 And in the East of the Island, Mount Leinster in the county of Carlow. . 2604 Geological Relations, and Distribution of the Subject. (6.) In the general relations of the transition tract of the South of Ireland great analogy is found to subsist. 'To prevent repetition, I propose to take a few examples as types, selecting them in the eastern and western extremities of the tract, in which the greater diversity is observable ; namely, in the county of Kerry, the adjacent portions of Cork, and the south coast of the county of Waterford, adding incidentally such further observations as may conduce to the fuller understanding of the whole of the transition field, and which may more particularly appear when I proceed to speak of its metallifer- ous relations. The carboniferous series of Munster, extending from the old red sandstone upward to the coal formation inclusive, may be conveniently considered under two heads: 1. The South Munster, embracing portions of the counties of Cork, Limerick, and Kerry ; and 2. The North Munster, ap- pearing in the county of Clare, and extending thence in part into the county of Galway. But though separated at the surface by the Shannon, these two fields are assuredly connected with each other beneath that river. I. Transition SERIES. In Kerry, Cork, and Waterford. (7.) The county of Kerry comprises rocks of great variety of character, which, though relatively of unequal continuity and distribution, are yet so perfectly inosculated as to constitute a persistent series. Their general range is KE. and W., subject to inflections from that line. The dip is interchange- ably N. or S., the angle of inclination fluctuating from the vertical to the horizontal nearly. From this arrangement arises a succession of ridges and Mr. Weaver on the Geological Relations of the South of Ireland. 7 troughs ; the ridges containing a central axis of vertical beds, from which the lateral strata diminish in elevation on each side, while in the troughs are in- closed other beds which gradually approach to the vertical position in the centre of the trough. These variations in the line of range and dip occupy spaces of greater or less extent ; but independently of this general disposition, involutions and contortions of the strata are also occasionally observable. (8.) Though the rocks of this portion of Ireland present great differences in aspect and structure, the principal masses may, in a great measure, be re- ferred to compounds of quartz and slate variously intermingled and associated. Limestone, another principal mass, also offers considerable varieties, and upon its confines with other rocks, it is found more or less charged with a portion of their ingredients. In generalizing the view, the country may be considered as chiefly composed of greywacke, slate, and limestone. To be more particular, we may designate the whole series as consisting of simple and compound rocks. The simple rocks are clay-slate, quartz-rock, hornstone, lydian-stone, and limestone. The clay-slate is bluish, greenish, seldomer blackish grey, often brownish, reddish or purplish, and glimmering, or glistening, more rarely wholly dull. In some quarters the slate appears as a quartzy clay-slate, and in others as a shivery shale. Quartz-rock, generally of various shades of greyish white, more or less compact and fine splin- tery, or granular ; sometimes also reddish, bluish, or greenish, when coloured by an intimate mix- ture of the substance of clay-slate. Hornstone, or chert, yellowish, reddish, or greyish white, compact, even, and fine splintery. Lydian-stone of its usual aspect, but sometimes passing into flinty slate. Limestone of various shades, from dark to light bluish grey, also pale grey with streaks of reddish and yellowish white, more rarely black ; and in structure varying from compact to sub- lamellar. The limestone in some quarters forms frequent alternations with the lydian-stone, hornstone, and quartz-rock, involving in its substance also shapeless portions of those rocks, for example—in several of the beautiful isles of the Lower Lake at Killarney, in some of which, as in Ross Island, beds of clay-slate are likewise interposed in the series; and in Muckruss peninsula, both on its northern and southern shores, the limestone may be observed alternating with slate and grey- wacke slate, where it borders upon rocks of that description. In other quarters the limestone is less interrupted, appearing in purer beds which afford excellent lime, e. g. in the Drishane quarries near Millstreet, or being deteriorated by a commixture of siliceous particles become less tractable, e.g. in the limestone of the Kenmare district. (9.) The compound rocks may be enumerated under the following heads : clay-slate conglomerate, quartz conglomerate, greywacke, and greywacke slate, sandstone conglomerate, sandstone, and sandstone slate, greenstone, and horn- stone porphyry. Of these the greywacke, greywacke slate, sandstone, and sandstone slate compose the predominant rocks, the coarse conglomerates 8 Mr. Weaver on the Geological Relations of the South of Ireland. being of more casual distribution, for example, the sandstone conglomerate in Dunloe Pass west of the lower lake of Killarney. Greenstone*, and hornstone porphyry, are more local occurrences: the former may be observed in Begnish Isle adjacent to Valentia Island, and the latter within the range of Mac-Gilli- cuddy’s Reeks. In the general series of these rocks, the purer clay-slate, fit for roofing, occurs in beds incidentally distributed and of variable thickness, yet — bearing but a small proportion to the entire mass, e. g. the indifferent, bluish and greenish slates procured from Mangerton and Glen Flesk, and the reddish brown from Dunloe Pass; but in the island of Valentia an excellent roofing- slate is obtained, which may vie with any for firmness and durability, possessing also an agreeable subdued purplish colour. Beds of quartz-rock, hornstone, and lydian-stone, also occur incidentally in the general, compound series ; but the last-named substance is comparatively very rare in the greywacke and slate country, its more usual representative being there a flinty slate. (10.) The common character of the clay-slate conglomerate and greywacke is that of a base of slate or quartzy slate, enveloping rounded and angular fragments of quartz and slate (some- times in the form of considerable pebbles) but very rarely inclosing small portions of felspar also. The greywacke slate is the same rock, of finer grain and fissile structure. Numerous scales of silvery mica enter also more or less largely into the composition of these rocks, as wellas occa- sionally into that of the purer clay-slates. A great variety of these substances, together with some sandstone conglo- merate, may be observed on the coast adjacent to Smerwick harbour, beds of clay-slate also appearing in the association. The beds in this quarter dip 65° to 80° S.; but in traversing the peninsula southward, to the confines of Dingle bay, they gradually acquire a vertical position, then a‘northerly in- clination, and re-assuming a vertical position, they again acquire the southerly dip. In the Cahir-conrée chain a disposition somewhat similar may be observed: thus in the northern face of the eastern quarter, where the Slieve-Meesh range may be said to commence and in which old red sandstone prevails, strata of sandstone appear, including some of conglomerate dipping 50° to 45° to the north ; but on penetrating into the mountains on the south by the valley which runs about two miles and a half in that direction, its mouth fronting Kilgobbin, these sandstone strata may be observed gradually merging into varieties of greywacke and greywacke slate, associated with red, brown and greenish co- loured clay-slate, and with occasional beds of similarly coloured sandstone ; * Namely, true greenstone, a compact, or subcrystalline compound of felspar and hornblende. In Kerry, and generally in the South of Ireland, the rock popularly called greenstone is a grey- wacke, or sandstone, of a greenish hue, and the brownstone of the country consists of the same kind of rock of a brownish or reddish colour. Mr. Weaver on the Geological Relations of the South of Ireland. 9 the series progressively rising ata higher angle until they become vertical, while still further south a successive interchange of dip takes place in these beds, analogous to that already noticed as occurring throughout the transi- tion field. To the eastward, this series is overlaid by the old red sandstone of Slieve Meesh, which forms a flatly arched inflection from north to south; but at its eastern foot the greywacke re-appears adjacent to the river Maine. In various parts of the country, the basis of the fine-grained greywacke is found occasionally to effervesce partially with acids, though no calcareous matter be obvious to the eye. Such, however, does casually appear when approaching the limestone, and sometimes even at the distance of one or more miles, In the quartz conglomerate, the basis being quartz, the ingredients are analogous to those of the clay-slate conglomerate, In the sandstone conglomerate also the larger included portions are essen- tially composed of quartz and slate, the former being usually white or grey, but sometimes tinged reddish or greenish ; while the basis consists of compact, granular or sandy quartz, numerous scales of silvery mica, ard an occasional diffusion of white earth, like that which proceeds from decomposed felspar. From this coarse compound, a gradual transition may be traced to the finer-grained sandstone and sandstone of a slaty structure, and thence, by the greater consolidation of quartzose matter, into quartz-rock itself, This gradation may be seen exemplified in the entrance of Dunloe Pass, where all these rocks possess more or less a reddish or brownish tint, agree- ing in that respect with the neighbouring clay-slate. ‘Those which are first encountered dip at an angle of 60° to the S., which angle they retain until we find a bed of the sandstone conglomerate in juxta-position with a reddish roofing-slate, the latter dipping 63° S. at the point of contact, but ata di- stance from the conglomerate (being about 70 yards thick) gradually assuming the vertical position. Further S. the beds decline to as low angles as 35° and 30°,—then undulate on a small scale for some distance, and subsequently resume the southerly dip at a higher angle. But from Dunloe Pass to Kenmare Bay, though the more general disposition of the strata be to the S., an occasional change of dip toward the N. is also observable, vertical strata in such cases commonly intervening. (11.) J may here remark that in the whole extent of the greywacke and slate country, contemporaneous veins of quartz are more or less common to the seve- ral members of that series, most usually traversing them in the line of the dip. (12.) It will be seen in the Map, that the distribution of the limestone is very unequal in the general expanse of the transition field, the interposed masses not assuming a regular form ; yet the strata are always parallel to those of the rocks with which the limestone is in contact ; and within the limestone ranges, the stratification is occasionally subject to inflections and variations in the line of dip, as well as to contortions, analogous to those within the grey- VOL. V. SECOND SERIES. c 10 Mr. Weaver on the Geological Relations of the South of Ireland. wacke and slate tracts, the scale of these changes of curvature also varying. An example of this kind may be seen, to the best advantage, on the western side of the Isle of Innisfallen, in the Lower Lake of Killarney, when the lake is‘at its lowest level, as well as in some of the adjacent islands. _/(18.) In the series of the greywacke, sandstone, and slate country now de- scribed, I have to notice the organic remains which have occurred to me. Those found in the transition limestone will be afterwards considered under that head. The only quarter in Kerry, in which I discovered numerous organic remains in the greywacke and slaty rocks, is situated on the western coast near Ferriter’s Cove, adjoining Smerwick harbour. They are there distributed in slate and fine-grained greywacke, which occasionally effervesce with acids, though no carbonate of lime be perceptible to the eye ; the petrifactions them- selves appearing either as mere impressions, or as casts of the interior, com- posed of the substance of the rock, namely, of slaty matter, fine-grained grey- wacke, &c. Among these 1 observed the Calymene Blumenbachii (Brongniart, pl. 1. fig. 1.) t{!, and ap- parently also the Asaphus caudatus (Brongniart, pl. 2. fig. 4.) +t, an Orthoceras, Euomphalus, two ‘ The mark f¢ implies that the species occurs in Great Britain or other countries, in the T'ransition System. The mark * that the species occurs in Ireland, in the Carboniferous The mark { —— Great Britain or other countries, System. See further hereon in §§. 33 and 57. Yn Europe the occurrence of the Calymene Blumenbachii and Asaphus caudatus may be ex- emplified in the following manner : Transition. Carboniferous. + Ferriter’s Cove; Dudley; Led- Calymene Blumenbachii .. ‘tan Tortworth; Newton Bushel; +¢ Gottland, A. Eifel ; Scania; Ostrogothia, &c. t Beadnell, Northumber- + Ferriter’s Cove; Bonmahon cst | lan (See Prof. Buckland’s county of Waterford ; Dudley ;Led- ¢ excellent Bridgewater Trea- bury ; Tortworth. { Bred Coalbrook Dale (Mr. Prestwich MS.) Gottland, A. The division of the Gottland limestone marked A, is referred by Mr. Hisinger to the carboni- ferous epoch, but some doubt seems to attach to the correctness of that reference. (See Mr. De la Beche’s Geological Manual, 3rd edition. By some mischance the Asaphus caudatus is omitted in Mr. De la Beche’s list of transition fossils.) On the other hand, in the United States of North America, the Calymene Blumenbachii occurs also both in the transition and carboniferous systems, but the 4saphus caudatus has not yet been met with in the latter: e, g. Asaphus caudatus ...... Transition. Carboniferous. + Glenn’s Falls, upon the Hudson | Ries Trenton Falls, upon he Black Rock on Niagara, Calymene Blumenbachii.. 4 Mohawk River,—both in the State p (see Annals of Lyceum of | of New York; Cincinnati; Louis- | New York, vol. i. part 1. L ville on the Ohio. + Glenn’s Falls upon the Hudson; Cincinnati ; Louisville on the Ohio. (See Dr. Harlan in the Ist vol. of the Transactions of the Geological Society of Pennsylvania ; Asaphus caudatus. ...... Mr. Weaver on the Geological Relations of the South of Ireland. 11 turbinated shells, one being carinated, the other striated, and a Natica; the Producta depressa (Sow. Min. Con. t. 459. fig. 3.) +*{, and other Product ; the Spirifera radiata (olim lineata, Sow. t. 493. fig. 1. 2.), + {, and other Spiriferze; the Terebratula prisca of Schlotheim (Tab. 17. fig. 2.)! considered as identical with Terebratula affinis of Sowerby (t. 324. fig. 2.)+*t, and other Terebratule, as well as a Pentamerus Sow. (t. 28. 29.) +, and other bivalves, besides casts of the interior of Tere- bratule, Spiriferee, and Producte, generally designated by German geologists by the name of hysterolites ; Polyparia, of the genera Cyathophyllum, Turbinolia, and Favosites ; and also crinoidal remains. The Turbinolia appears closely to resemble the 7’. celtica of Lamouroux (Tab. 78. fig. 7.)+, also derived, it seems, from a transition tract °. Several of these casts so perfectly resemble both in the species of the ori- ginal shell and in composition, similar casts occurring in the Tortworth trans- ition district in Gloucestershire, which I formerly described’, that on examin- ing them they might be supposed to have been derived from thence. In both districts the Zurbinolia cellica ? is common. Some of the casts are also identical with fossils figured by Sir Alexander Crichton as occurring in the transition greywacke and slate of the Duchy of Nassau’. In addition to these remains I have to state that the late Mr. Alexander Nimmo found in the slate, adjacent to Dunmore Head, impressions of plants, which, according to his description, would appear to be referable to Calamites. Organic remains are also visible in the greywacke, which protrudes from beneath the old red sandstone at the eastern foot of Slieve Meesh (§ 10), form- ing a low ridge which crosses the river Maine, and extends some distance beyond it. On the right bank of that river, in the lands of Riversville, a quarry, which has been opened eight feet deep, exhibits beds of fine-grained greywacke, from two to six inches thick, with slight layers of slate interposed in the lower part, but alternating in the upper with beds of clay-slate and lime- stone, from four to six or eight inches thick, the whole dipping 12° to 15° to the E. of S. The organic exuvie being closely entangled with the rock, are best discerned where the latter is partially decomposed, and the most common appeared referable to Producte, Spirifere, Terebratule, Favosites, and Cri- noidea. On the eastern side of Ireland, namely, on the banks of the Oom-boy river, and Prof. Eaton, Geological Text-Book, 2nd edition.) I collected specimens myself at Louisville and Cincinnati. From Dr. Harlan’s list it appears that numerous other species of the genera Calymene and Asaphus occur in the transition and carboniferous systems of the United States, but a clear di- vision of them is much wanting. Many of these have not hitherto been noticed in Europe. (See Trans. of Geol. Soc. Pennsylv., vol. i. pp. 99 to 103.) ' Nachtrage zur Petrefactenkunde. * Lamouroux, Exposition methodique des Genres de Polypiers, p. 85. Paris, 1821. ° Geol. Trans. Second Series, vol. i. p. 326—329. * Geol. Trang. Second Series, vol. ii. plate xxxiii. fig. 1, 4, 5. c 2 12 Mr. Weaver on the Geological Relations of the South of Ireland. which flows into Cork harbour, Mr. Nimmo informed me that Orthoceratites and other organic remains are also to be met with in the slate ; and Mr. S. Wright, of Cork, assures me that he has frequently seen small Orthoceratites in the clay-slate near the town of Cove in Cork harbour ; also Spiriferze or Terebratulz in the slate on the Bandon road, five miles south from Cork, but not sufficiently distinct to admit of the identification of species. (14.) In tracing the transition rocks from Kerry into the counties of Cork and Waterford, an analogous structure and composition are everywhere per- ceptible, diversified, however, by numerous varieties ; one member also some- times prevailing more than another in the series. Of this disposition the unequal bands of limestone which pervade the tract, as well as the isolated patches more locally distributed, are sufficient exemplifications. The general observation may also be made, that the conglomerated structure, and the reddish or brownish hue are more particularly developed in the greywacke and slate rocks which occur north of the parallel of the river Lee ; while in the parallel to the south of that river the same class of rocks exhibits commonly a finer structure and a light bluish or greenish grey cast ; but both parallels contain incidentally the other modifications which have been noticed. (15.) The transition rocks on the south coast of the county of Waterford extend from the vicinity of Dungarvan toward Tramore. As they exhibit a series of considerable interest, J shall here subjoin such an account of them as may help to complete our view of the modified structure and association of the general series. Clay-slate.—1. More or less pure, and partly glossy ; blackish, bluish, greenish, or yellowish grey; also reddish brown or purplish. These slates contain more or less numerous scales of sil- very mica disposed parallel to the lamin. The blackish slates are partly aluminous. 2. Quartzy clay-slate containing some crystals of felspar. 3. Quartzy clay-slate containing finely disseminated hornblende, and sometimes also crystals of glassy felspar. 4, Clay-slate very firm, yet fissile, partly porphyritic. Greywacke.—1. Slate enveloping crowded grains of quartz as large as peas, portions of the paste consisting also of green steatite. 2. Slate or quartzy slate inclosing angular and rounded grains of quartz, with small fragments of slate, and numerous scales of silvery mica, and with or without grains of felspar. 3, Greywacke slate, the same rock as the preceding, but of fine grain and slaty structure. 4. A fine-grained base, compounded of slate and quartz, containing isolated, round grains of white quartz, of the size of large peas, the rock at a distance appearing like an amygdaloid. Quartz-rock.—1. In its simple forms. 2. Containing small globules of chlorite, and also particles of hornblende, from the partial decomposition of which it acquires an ochreous aspect. 3. Quartz- rock (sometimes graduating into hornstone, or partially into compact felspar), containing numer- ous reddish and yellowish white crystals of felspar, forming a handsome porphyry ; sometimes containing also particles of hornblende. 4. Quartz-rock (sometimes merging into hornstone), Mr. Weaver on the Geological Relations of the South of Ireland. 13 in which are disseminated crystals of yellowish white felspar, and also crystals and globular portions of brownish grey vitreous quartz, and a few scales of mica. 5. A base of quartz, coloured by clay-slate, and partially also by hornblende or chlorite ; a compact greenish grey, or greyish green rock, containing incidentally particles of hornblende and crystals of glassy felspar, and some- times grains of vitreous quartz. Without attention it may be confounded with greenstone. Hornstone.—1. In its simple forms, splintery or conchoidal. 2. Containing crystals of glassy felspar, or flesh-coloured crystals of felspar, or both conjointly, forming a handsome porphyry. The base is often of a yellowish, and sometimes of a hair-brown colour, and in the base a portion of steatite is sometimes diffused, and the rock then becomes unctuous to the touch. 3. Hornstone forming the base of the compound described under the head of Quartz-rock No. 4. Quartz Conglomerate and Hornstone Conglomerate, coarse- and fine-grained.—A base of quartz or hornstone (or partially of compact felspar), much incorporated with steatite, and thus acquiring a saponaceous feel, and containing crystals both of dull and glassy felspar; as does also the green steatite when appearing in a distinct form, which is frequently the case. This base envelopes nu- merous fragments of quartz, hornstone, and hornstone porphyry, those of the two latter varying sometimes from the smallest size to that of blocks of one and two feet in diameter, Red Conglomerate, Red Sandstone, and Red Sandy Slate——These all contain numerous scales of silvery mica. The conglomerate and sandstone are compounded principally of rounded and angular fragments of quartz and red slate, connected by a basis of similar composition but smaller grain, or by a simple base of quartz or reddish slate. In the mixture some grains of decayed felspar may also be incidentally observed. The compound is sometimes greyish as well as reddish coloured. The ingredients in the conglomerate rarely exceed the size of cherries, but sometimes extend to that of turkey’s eggs, and even a man’s head, in magnitude. When the slaty basis predominates, a sandy slate is formed'. -These beds are sometimes associated with irregular masses and beds of quartz, from an inch to one, two, and three feet wide, which bear a great quantity of beautiful, deep green chlorite. Greenstone and Compact Felspar.—1. Compact greenstone, a base of compact felspar, coloured greenish grey by hornblende, and containing particles or crystals of hornblende, and sometimes also crystals of felspar, thus appearing as a porphyry. The felspar base acquires a white aspect by weathering. 2. Sub-crystalline greenstone, a confused intermixture of greenish grey glassy felspar with hornblende, being also spotted with blackish green hornblende. 3. Compact reddish brown or purplish felspar, partially intermingled with chlorite, or green steatite, and containing also minute crystals of glassy felspar. 4. Greenstone conglomerate, a base of greenstone, enveloping portions of greenstone, mostly of an angular form. The sub-crystalline greenstone seldom occurs in a distinct form on this coast. The compact greenstone, which more generally prevails, exhibits a difference of character according to the state in which the hornblende enters into the composition, the greater or less prevalence of siliceous matter, and the intimate blending of chlorite. Ifthe hornblende be unaltered, the rock is rugged and stony ; if partially decomposed it is saponaceous. It is probably to this unequally affected state of the hornblende that the unequal state of aggregation in the greenstone is partly due; and that one portion consisting of comparatively loose materials is found serving as a base to numerous harder portions which are embodied in it ; a difference ascribable to disturbance during the process ' These rocks, like analogous productions in Kerry, &c., are not to be distinguished by mere mineralogical character from varieties which occur in the old red sandstone of the carboniferous ‘series. 14 Mr. Weaver on the Geological Relations of the South of Ireland. of concretion. In places, the compact greenstone merges into quartz-rock, deeply coloured by chlorite. Red Sandstone Conglomerate, and Greenstone Conglomerate.—When the red sandstone and the greenstone beds come in contact, a gradation may be traced in some places from the one rock to the other, through the medium of a conglomerate, the extreme links of the chain being the follow- ing: 1. A basis of fine-grained red sandstone, enveloping rounded and angular fragments of red conglomerate and sandstone, and of greenstone, the two former exceeding the latter in quantity. 2. A base of compact greenstone, inclosing rounded and angular fragments of greenstone, and of red sandstone, the former predominating. In both conglomerates, the included fragments occur from a small size to that of a child’s head. The crystals noticed in the preceding varieties of clayslate, quartz-rock, hornstone, greenstone, and compact felspar, appear to be of contemporaneous formation with the rock itself, possessing angles sharp and well defined. (16.) The rocks thus described form beds intimately connected with each other by direct association, gradations, and repeated alternations, but without any specific order of succession or continuity. Their range is east and west yet subject to inflections from the line, while the dip changes from the north to the south, the beds being commonly at an angle approaching the vertical; but in the most eastern part of this coast, trending toward Tramore bay, they are inflected to a much greater extent, and partially disposed at a low angle of inclination. Between the river Bonmahon and the bay of Ballydoan situated two miles west, there are fewer varieties of rock exhibited than occur more west and north of that bay. In the bay itself, the immediate association of the red sandstone and greenstone beds is well exemplified, in double alternation ; and in the line of contact between the two rocks may be observed those gradua- tions from the one into the other, through the medium of the compound con- glomerates, which I have just described. North of these beds varieties of slate are found, alternately’with greywacke, quartz-rock, hhornstone, red sand- stone, and conglomerate, and containing subordinate beds of greenstone, with the porphyritic varieties of the rocks which I have described. This arrange- ment is well exposed, in the western continuation of this coast, extending to- ward Dungarvan. ‘To the eastward of the river Bonmahon the composition is analogous, with this exception, that no red conglomerate appears on that part of the coast, forming a portion of this transition series ; it probably, how- ever, occurs inland, as indications of red slate are there observable. More east upon this coast, the steatitic varieties of hornstone and conglomerate are, in particular, well displayed near Annestown, to the east of Kean Head. (17.) Disseminated iron pyrites is not uncommon in the transition rocks of this coast, particu- larly in the blackish and bluish slates, which, by mutual decomposition, form sulphates of alumine Mr. Weaver on the Geological Relations of the South of Ireland. 15 and iron, giving rise to extended exudations, which spread over the face of the cliffs in dirty brown yellow, and white streaks. It rarely occurs, however, in the red conglomerate and red sandstone. - These are more especially distinguished by the diffusion of the red and yellow oxides of iron, which substances frequently occupy their interstices. (18.) Numerous veins of quartz are found in all the rocks of the transition series on this coast, and of calcareous spar in most of them. They are, however, least frequent in the red conglo- merate and red sandstone. Veins of hornstone also often traverse several of the rocks, in some places pursuing a very tortuous course. All these veins vary from a thread to four, six, or eight inches in width, and rarely exceed a breadth of one or two feet, frequently ramifying, and termi- nating in filaments. Many of them are wholly barren and discontinuous; but others, whether consisting simply of quartz, or of calcareous spar, or a compound of both, bear copper and lead ores, either separately or conjointly ; those bearing copper ores separately being the most common. Where these ores occur, the face of the cliffs is generally stained with blue and green streaks, ari- sing from the decomposition of the sulphurets of copper. (19.) In one portion of this district I met with organic remains, namely, immediately eastward of the Bonmahon river, both upon the coast and inland, disposed in fine-grained greywacke and greywacke slate. In the former quarter they appear in the face of a cliff, which consists of coarse slate, the cleavage planes of which are nearly vertical ; but the organic remains form a number of parallel lines, arranged in an horizontal position, thus traversing: the fissile structure of the rock, and constituting so many layers, at the distance of three to six inches apart, a disposition which might give rise to some curious specula- tion. This deposit occupies a considerable portion of the face of the cliff upward, though in length it extends only about twelve fathoms. I must remark, however, that the organic remains are not wholly confined to these parallel lines, occurring also scattered through the mass of the rock. They here consist of three or four species of Polyparia, several bivalves, and a 'Turbo ; but inland I found, in addition to these, the Asaphus caudatus, and the whole may bear a strict comparison with similar remains in Kerry, Gloucestershire, &c., hy- sterolites, or the casts of bivalves, also appearing among the number, and closely resembling those figured by Messrs. Phillips and Woods as occurring at the summit of Snowdon!, (20.) Generally speaking, this transition series is connected, on the north, by insensible gradations with the great body of clay-slate which prevails in that part of the county of Waterford, the whole sustaining, upon the higher lands, unconformably, extended overlying masses and caps of the old red sandstone?, ' Annals of Philosophy : December 1822. * The horizontal position of the old red sandstone formation in the Monavoullagh range is well marked in a drawing representing the precipice in that formation, which overhangs the Lake of Coumshenane 1100 feet in height. (See Dublin Penny Journal of Oct. 20, 1832.) 16 Mr. Weaver on the Geological Relations of the South of Ireland. and on the flanks partial borders of the same formation, the latter supporting the carboniferous limestone in conformable position in those quarters. (21.) Turning now our attention to the bands and isolated masses of lime- _ stone which are included in the transition tract, I may remark, that the greater part of these limestones are continuous in the mass, yet appear interlaminated or interstratified with the slaty rocks wherever exposed on their confines with the latter. A remarkable feature attending most of these bands of lime- stones is, that they occupy the line of valleys or dells, being flanked on each side by elevated ranges of greywacke and slaty rocks. ‘They seem to belong to some of the oldest of the transition class, the species of organic remains which they contain being, so far as my experience extends, not many in num- ber, and being also sparingly and partially distributed. ‘The close researches of Mr. S. Wright in the Cork limestones lead to the same conclusion, as will fully appear in the sequel. (22.) To the north of the road between Skibbereen and Ross is a calcareous district, extending about three miles in length and one to one and a half miles in width, consisting of isolated elliptical masses of bluish grey limestone, ar- ranged in somewhat of an echelon order in grey clay-slate, the latter being also partly calcareous when adjoining the limestone. An analogous deposit exists also on the western side of Courtmacsherry bay; in these I observed only crinoidal remains and a few bivalves. About three miles north of Bantry town, and adjacent to the narrow inlet from the sea, called Reenadunagan Lake, is a band of grey limestone, about one quarter of a mile wide, which has been traced upon the range some little distance to the eastward. It lies in pale bluish-grey, glossy clay-slate, arranged in strata from one to one and a half feet thick where continuous ; but on its confines with the slate on the south, it is interlaminated with the latter in layers only a few inches thick, all dipping 45° to the south at the point of contact ; while in receding, both north and south, the beds gradually acquire a higher inclination, The thinner layers of limestone are usually compact, and the thicker granularly foliated, the latter appearing compounded of the com- minuted fragments of crinoidal remains. I did not observe any bivalve. (23.) At the head of the bay of Kenmare is a limestone district, which ex- tends to the east and west of the town of Kenmare, being about ten miles long, and from a half to a quarter of a mile broad, and confined to the right bank of the river Rought and the bay of Kenmare. At its western extremity, on the townland of Reens, it gradually narrows tv a point on the north shore of the bay, yet extends through the adjacent islands of Cappanacus and Dunkerrin. The limestone strata appear continuous throughout, and nearly rectilinear in FS AG, Mr. Weaver on the Geological Relations of the South of Ireland. 17 their course, with a dip uniformly to the southward at angles from 75° to 80°, except on the northern side of the western extremity, where they partially dip to the north, but at the same high angle, vertical strata probably intervening. In the adjoining slate and greywacke country, both on the northern and southern sides of the limestone, analogous, corresponding variations in the dip are like- wise to be observed. In this limestone, organic exuviz are very sparingly dis- tributed, consisting of a few bivalves with some crinoidal remains. (24.) In the Killarney limestone district, the southern and eastern parts of Muckruss peninsula, consist of blue limestone in nearly continuous strata. North and west of the continuous band, the limestone alternates with thin layers of slate and greywacke slate, and still further north, where beds of com- pact, fine-grained, greywacke predominate, the beds of limestone gradually disappear. In the region of Muckruss mine, the limestone strata dip about 70° to the southward, but further south they gradually acquire as low an angle as 30°. Bivalves and fragments of Crinoidea occur in the Muckruss limestone, and in the adjacent slate and greywacke slate, but they are confined to a few species. ‘They are incidentally met with also in the limestone of the vicinage of Killarney, being, however, rare in proportion to the greater quantity of siliceous matter in that rock. Indeed, in those parts where the calcareous repeatedly alternate with the siliceous beds, scarcely the vestige of a shell is to be seen ; for example, in the greater part of Ross Island and in some of the adjacent islands. (25.) It is not improbable that a connexion subsists between the Killarney transition limestone and that which appears in the Drishane quarries near Millstreet, traces of limestone having been observed in the boggy tract which intervenes. The Millstreet band ranges south of the Blackwater river, past Clonemeen to the east of Roskeen bridge, terminating at a short distance from the latter in the greywacke and slate country. In most places it is amorphous, but where the strata are distinctly developed, they dip to the south, at angles varying from 45° to 70°, yet subject to curvatures, corresponding with those in the adjacent greywacke and slaty rocks. This limestone is generally of a light colour, and it exhibits few distinct organic reliquiz, the chief or most charac- teristic being a species of Avicula, assembled casually in interlaced groups, forming a thin separate layer. (26.) The band of light-coloured limestone which ranges from the east of Aglish past Tallow to Castle Lyons on the west, may be seen adjacent to the first-named village, reposing on and alternating with clay-slate, both forma- tions, where in contact, dipping to the southward at an angle of 45°, and con- taining the Producta depressa, some Spirifere, Polyparia, and crinoidal re- VOL, V.—SECOND SERIES. D 18 Mr. Weaver on the Geological Relations of the South of Ireland. mains. The broken portions of Crinoidea are very frequent in the limestone. The general range of the conjoining slaty and other rocks on the northern side dip to the south, and on the southern side to the north, commonly at high angles, to which the limestone appears to conform, its more central strata approaching the vertical position, as may be observed in the Tallow district. On the northern side of this limestone band, in the range of hills which ex- tends eastward to the southern part of Dungarvan harbour, may be observed numerous varieties of greywacke, sandstone, quartz-rock, and slate, frequently of a reddish brown hue, also of a yellowish or whitish cast, the sandstone and greywacke affording, in some places, tolerable freestone for building purposes. Many coarse conglomerates occur also in the series, containing fragments and pebbles of considerable size. (27.) Proceeding S. from Aglish to Clashmore, a distance of about five miles, the slaty rocks undergo interchanges of the dip from N. to S., and again to the N., vertical strata intervening. Between Clashmore and Ballyhenny we cross a band of limestone about half a mile wide, which ranges nearly two miles E. and W., included in clay-slate, these rocks all dipping in conformity 75° to the N. The slate is partly interlaminated with the limestone, where it underlies the latter. Lydian-stone occurs occasionally in the limestone, in layers a few inches thick, and also in interspersed portions. The latter rock is mostly dark bluish grey, containing chiefly small fragments of crinoidal remains and of some few bivalves. At a little distance S.E. of Ballyhenny limestone quarry, roofing-slate is raised. (28.) To the N. of the town of Youghall is a band of light-coloured lime- stone, which, proceeding from the vicinity of Clasheen on the W. past Kil- natoara Castle and river, seems to cross the harbour, reappearing on the E. in Pilltown, and extending thence to the small bay of the sea situated to the N. of Ardmore Head. It may average half a mile in width, and both at Pill- town and Kilnatoara Castle quarries the strata dip 80° to 85° to the N., or approach the vertical. The slaty rocks immediately north of this limestone dip south, and on the south to the north, but in both cases at high angles ; while still further north and south the dips are interchangeable, so that the general series may be considered as nearly vertical. In the Pilltown lime- stone are few well-marked organic remains, and they are chiefly crinoidal, as also in that of Kilnatoara. In the latter I did not observe a single bivalve, but I obtained a broken portion of what appears to be a Goniatite of Von Buch. (29.) South of Youghall we enter upon the principal band of limestone contained in the transition tract, extending from Youghall Bay on the east, Mr. Weaver on the Geological Relations of the South of Ireland. 19 past Carrigtohill and Cork to Castlemore on the west. In this range the lime- stone, after reaching the upper part of Cork harbour, occupies the smaller islands in that quarter, together with the northern points of Cove Island, thence pursues its western course on the south side of the Lee to the confluence of that river with the Bride, then lines both banks of the latter stream for a short distance, while the remainder of its course is confined to the right bank, ter- minating at about a quarter of a mile to the west of Castlemore Castle, or nearly fifteen miles west from Cork. This band in its broadest part, on the east, is between four and five miles wide, while at Castlemore, on the west, it is reduced to about halfa mile in breadth. Flanked throughout by hilly ranges of slaty and greywacke rocks, the general dip is to the south, varying chiefly between angles of 70° and 80°, yet often approaching the vertical, and in some parts exhibiting a counterdip to the north. These relations may be distinctly observed, in traversing the bounding slaty rocks and the limestone from north to south, in different portions of the range, both to the east and the west of Cork harbour. The limestone is generally light-coloured and continuous, free from foreign beds, and the few organic remains I have seen in it were chiefly crinoidal. (30.) A similar arrangement is observable in the parallel band of limestone, which, proceeding from the sea on the east, passes through the vale of Cloyne to Cork harbour, where itoccupies the northern part of Spike Island, the south- western point of Cove Island, the whole of Rocky Island, and the isles of Haul- bowline and Rinniskiddy ; thence passing to the main land, it composes the projecting points of the coast as well as the strand of Rinniskiddy village, and proceeding west, it passes by Shanavally and Hawksglen to Shannon Park*. The interlamination of this band of limestone on its southern side, with the adjacent clayslate of Rinniskiddy hill, is distinctly seen in the rocks upon the strand, all approaching the vertical position, yet dipping south. The great body of Rinniskiddy hill is composed of clayslate, corresponding with the southern part of Spike Island; but in passing round the former along the strand, we find toward its southern side, the slate containing, at considerable intervals, discontinuous layers of limestone, each a quarter or half an inch wide. Further south these beds become more frequent and thicker, until they exceed those of the clayslate in dimensions and number, and in the more southern portion of the hill are nearly continuous. We have thus entered upon another parallel band of limestone, which ascends about halfway up the southern face of Rinniskiddy hill, and occupies the flat of the inlet below, ranging to the westward by Coolmore to Carrigoline; and to the eastward it * The scale of the Map does not permit the whole of these places to be laid down. D2 20 Mr. Weaver on the Geological Relations of the South of Ireland. apparently passes under the sea to Corkabeg, terminating there in a low promontory, which extends from the mainland on the eastern side of the lower harbour, being situated to the north of Carlisle Fort. The clayslate, interlaminated with the limestone both on the northern and southern sides of Rinniskiddy hill, contains the same organic remains as the latter rock, and the series of strata deserves strict examination from those, whose local residence may afford the requisite leisure and opportunity. The fossils I met with were mostly indistinct. All these rocks dip conformably to the south. (31.) In the ranges of clayslate hills which occupy the district on the south of the limestone of the vale of Cloyne, is an isolated but parallel band of lime- stone, situated about half a mile south of that of the Cloyne valley. It ranges in a dell from east to west nearly two miles, being about one eighth of a mile in thickness; and, as exposed in the principal quarries of Carrigacrump and Ballyfin, its strata appear on the northern side, dipping 70° to the south, cor- responding in that respect with the adjacent clayslate on the north; but in proceeding south the limestone approaches to the vertical position. (32.) I have yet to notice two small isolated bands of limestone in the grey- wacke and slate series, the one situated at Blarney, north of the river Lee, the other adjacent to that river and south of Macroom. At Blarney the limestone forms a ridge of slight elevation, about two miles inlength, ranging east and west, in strata apparently nearly vertical. Blarney Castle is situated about midway between the two extremities of the ridge, which becomes narrow toward the east, but widens toward the west ; its greatest width being nearly half a mile. The red slate and greywacke rocks which bound this limestone on the north and south, approach the vertical po- sition, yet with a prevailing dip toward the south, though the northerly dip also occurs. High, hilly ground, about two miles wide, intervenes between the Blarney limestone and the river Lee. The band of limestone south of Macroom, stretches along the right bank of the river Lee to an extent of two miles, but in its progress west it crosses that river, proceeding about half a mile further. It nowhere appears to exceed half a mile in width, and its general position may be considered as vertical, the slaty and greywacke rocks by which it is bounded, being on the south either vertical, or inclined north, and on the north inclined south, yet nearly vertical ; while still more north and south the dip becomes interchangeable, high angles in these cases always prevailing. In the hills flanking this limestone, and also in the defiles which lead toward the Castlemore limestone in the valley of the Bride (§. 29), may be observed many varieties of greywacke, quartz-rock, and slate, of varying shades of blue, green, brown, red, and grey. “Mr. Weaver on the Geological Relations of the South of Ireland. 21 In the limestones mentioned in §§. 31 and 32 organic reliquie appear very sparingly. (33.) In addition to the organic remains noticed by me in the transition limestone in the preceding §§. 21 to 32, I here subjoin a list of those observed by Mr. S. Wright in the Cork limestones, for which list and their localities I am indebted to that gentleman, almost all the species having been determined by Mr. James de Carle Sowerby. The locality given as Cork, implies that the species were derived from quarries near that city, in the direction of the vil- lage of Evergreen ; while that of Ballinlough denotes a position nearly half way between the city and the extremity of the peninsula of Black Rock. To the localities of those species which have been found also in the transition tracts of Great Britain or other countries I have affixed the mark +; to those occur- ring also in the carboniferous limestone of Ireland, the mark * ; and to such as have been met with likewise in the carboniferous limestone of Great Britain or other countries, the mark}. From this list it will be obvious that many species of Producte, Spiriferee, and Terebratule, in particular, are common to both the transition and carboniferous epochs. For many of the distinct localities of these and other organic remains specified, reference may be further had to Sowerby’s Mineral Conchology ; the 3rd edition of Mr. De la Beche’s Geological Manual, 1833; the German modified translation of the 2nd edition of the same work by M. von Dechen, 1832, and the French translation of the 2nd edition of same work by M. Brochant de Villiers, 1833 (the latter being distinguished by very useful references to the published figures of fossils, as well as by other additional matter); also the excellent work on Geology in the Encyclopedia Metropolitana by Professor Phillips ; and to other authors'!. = ee ; Localities in L n other ; South of Ireland. — Transition Tracts. Two species of Trilobite, undetermined .... Black Rock. The tuberculated species of Asaphus, figured by Brongniart, PlateIV. fig. 12. (Asaphus gemmuliferus of Professor Phillips) ...... * t Cork. Cephalopoda polythalamia. Malmoe ; Christiania; Orthoceras striatum, (Sow. T. 58.) ........ * Black Rock. +4 Teena aie (New ork. Orpreyni, (sow. 1. 60, fig. 5.) ..60.sls. = Ditto. 1 This list may serve to clear up some doubts expressed by Professor Phillips in the Encyclo- pedia Metropolitana, art. Grotocy, pp. 577 and 578, as to the occurrence of certain fossils in the transition limestone of the South of Ireland. Compare also with pp. 572 to 576, and pp. 579 to 581 of the same work, which have reference to the fossils of transition tracts in general. With the view of drawing the attention of geologists further to this subject and exciting inquiry, I have appended a note to each of the lists of the Productz, Spiriferee, and Terebratule, found in the Cork limestones, showing what other species of these genera are stated to have been discovered both in the transition and carboniferous systems of other countries. 22 Mr. Weaver on the Geological Relations of the South of Ireland. Localities in In other South of Ireland. Transition Tracts. Orthoceras fusiforme, (Sow. T. 588, fig. 1,2.) *t Black Rock. Nautilus globatus, (Sow. T. 481.).......... *f Ditto. + Trenton Falls. N. multicarinatus, (Sow. T. 482. figs.1,2.).. *t Ditto. N. cariniferus, (Sow. T. 482, fig. 3,4.).... f Ditto. N. sulcatus, (Sow. T. 571, fig. 1,2.)...... * $ Middleton. N. Wrightii(Fleming), considered as identical with N. globatus..ceseceseserceces Black Rock. N. ovatus, (Ellipsolites of Sow. T. 37.).... * Ditto. + Hof; Schleitz. N. funatus, (Ditto, Sow. T. 32.) ........ - Ditto. N. compressus, (Ditto, Sow. T. 38.) ..... Ditto, Gasteropoda. Euomphalus triangularis, (Wright.) ........ Cork. E. ovalis, (Wright.) ..csccosteccccsces Ditto. E. pentangulatus, (Sow. T. 45, fig. 1,2.).. *} Ditto. + Dudley. E. catillus, (Sow. T. 45, fig. 3, 4.) ..... - *}{ Black Rock. + Dudley; Blankenheim. Pileopsis vetusta, (Sow. T.607, fig. 1,to3.).. *} peed t ieiline: ey Ampullaria helicoides, (Sow. T. 522, fig. 2.) * { Cork. A; ovalis;, (Wright.) .....cccssceccsses Black Rock. Solarium, (Wright.) ......cccccsssccesce Ditto and Cork. Nerita spirata, (Sow. T. 463, fig. 1,2.) .... | $~ Black Rock. + Plymouth. Conchifera. Producta Scotica, (Sow. T. 69, fig. 3.) .... *{ Black Rock. + Isle of Man; Eifel: P. Martini, (Sow. T. 317, fig. 2,3, 4.).... *} Ditto. P. concinna, (Sow. T. 318, fig. 1.) ...... *t Cork. P. lobata, (Sow. T. 318, fig. 2 to 6.).... *} Black Rock. P. punctata, (Sow. T. 323.) ....-000- - *+t Ballinlough. P. antiquata, (Sow. T. 317, fig. 1, 5,6.). *{ Black Rock. P. plicatilis, (Sow. T. 459, fig. 2...00+.. ¢ Ditto.! 1 Of the above species of Producte, the Producta Scotica alone appears to have been hitherto noticed in the transition series of other countries; but the following species of Product are enu- merated as having been found both in the transition and carboniferous systems : Transition. Carboniferous. Producta depressa, (Sow. T. 459, fig. 3.).. ‘ie ar os aa 42 he Fermanagh}; Liege. t Z + Eifel; Albany; + Ratingen ; Liege. P. hemispheerica, (Sow. T. 328.) ...... { (New York.) y \ 5 13 Baie (Wright.) P. longispina, (Sow. T. 68. fig. 1.) .... + Blankenheim ........ + Linlithgow. P, sulcata, (Sow. T. 319, fig. 2.) ...... + Catskill Mountains ....+ Derbyshire; Visé; Liege. Panomala, (Sow. MS.) 21.02. .0.05- fo EeyMienth |. Jefe owt « + Preston. P. sarcinulata, (Goldfuss) ......... Jy a gee a t Visé. (See the French translatiom of Mr. De la Beche’s Geol. Manual. The Producta depressa in Fermanagh was discovered by Prof. Phillips.) : : t Derbyshire ; Liege; PrgcaprcoiasneOWs P69.) seccessces f Etele. cuss e cose 4 Visé (Von Dechen). Mr. Weaver on the Geological Relations of the South of Ireland. 23 In other Transition Tracis. Spirifera cuspidata, (Sow. T. 120.)........ * Black Rock. + iyeataeh 5 dels Cob- S. distans, (Sow. T. 494, fig. 3.).....00. * + Plymouth. Localities in (Conchifera.—continued.) South of Ireland. Ditto. Sobpiaia, (Sow. Ly 268). .c 2s eeccees, “FT Ditto. + Norway. S. trigonalis, (Sow. T..265.).....00.5.. “f° Ditto. S. radiata, (Sow. T. 493, fig. 1,2.) .... + Cork. ¢ Dudley. S. striata, (Sow. T. 270.) ......+e+--- *f Ballinlough. tT Dudley. S. pinguis, (Sow. T. 271), considered by Von Dechen as identical with S. le- vicosta of Goldfuss bade Sale consis wise wav) id Ditto. + Eifel; Coblentz; Bensberg. S. octoplicata, (Sow. T. 562, fig. 2 to4.).- *t ees sland, - ae ene Eifel ; S. resupinata, (Terebratula, Sow. T. 325.) *% Ballinlough. S. rotundata, (Sow. T. 461, fig. 1.) .... *+t Cork.! + Newton Bushel. Terebratulacrumena, (Sow. T. 83, fig. 2,3.) *+ Black Rock. f Eifel; Lindlar. T. hastata, (Sow. T. 446, fig. 2,3.) .... *t Ditto. T. sacculus, (Sow. T. 446, fig. 1.)...... *t Ditto and Middleton. + Blankenheim. T. lateralis, (Sow. T. 83, fig.1.) ...... *t+ Black Rock. + Eifel; Blankenheim. T. cordiformis, (Sow. T. 495, fig.2,4.).. * Ditto. T. levigata, (Schlot. T. 18, fig. 1.) Spiri- fera, considered by Von Dechen as identical with S. oblata of Sowerby T. pugnus, (Sow. T. 497.) T. reniformis, (Sow. T. 496, fig. 1 to 4.) T. acuminata, (Sow. T. 324, fig. 1.) .... e©eo0eeeeeeee Isocardia oblonga, (Sow. T. 491, fig. 2.) .. *¢ Ballinlough. + Norway. * + Black Rock. f P cnet ieee *t — Ditto.2 { Ballinloughs. + Eifel. Black Rock and Little Island in the South of Ireland. ' Of other Spiriferze occurring both in the transition and carboniferous series, Prof. Phillips enumerates the following species, (see Encyclopedia Metropolitana, art. Grozoey, pp. 576 and 605.) Transition. + Plymouth + Eifel; Coblentz .. + Blankenheim .... Spirifera glabra & obtusa, (Sow. T. 269.) S. attenuata, (Sow. T. 493, fig. 3, 4, 5.) S. ambigua, (Sow. T. 376.)......., Carboniferous. Derbyshire; Ratingen; Liege. Dublin ; ¢ Liege. t Derbyshire. Ratingen. eeeee0e0 Be % + S. reticulata, (Sow. MS.).......... + Plymouth ...... * Treland. S. decurrens, (Sow.)......+ seeeeee +t Newton Bushel .. } (De ie Paes pinay: + Eifel; Bensberg ; S. striatula, (Goldfuss)........... : Christiania; Tren- >{ Ratingen, (Von Dechen.) ton Falls. * Both Von Buch and Sowerby consider 7’. reniformis and T’. lateralis as varieties of 7’. pugnus. See “ Ueber die Terebrateln, mit einem Versuche, sie zu classificiren und zu beschreiben, von Leopold von Buch. Berlin, 1834.” p. 34. * Of other Terebratula met with both in the transition and carboniferous systems, Professor 24 Mr. Weaver onthe Geological Relations of the South of Ireland. é : Localities in In other (Conchifera—continued) South of Ireland. Transition Series. Cardium hibernicum, (Sow. T. 82, fig. 1,3.) er 1 Piurorigicue Mierninsot Sallge ote eee Ts Polyparia. Cyathophyllum ......seeeesscevesencs Cork. Favositesic.s oe sjsicis ccs 0000.00 semen mas cls Little Island. Retepora .seces..cevccccceserevecaces Black Rock and Cork. near Coutances; Cat- skill Mountains, (New + Eifel; Mont Chatou Amplexus coralloides, (Sow. T. 72.) ...... *} Cork. | L York.) Crinoidea. The Actinocrinites 30-dactylus.....++++. *f + Eifel. And many other crinoidal remains occur in fragments in the ....eeeeeeevcseeeees Cork limestones generally. To this list I have to add that casts, apparently derived from the concavity of vertebre of fish, have also occurred in the Cork limestone ; and which were, I believe, first recognised as such by the late Mr. J. S. Miller. METALLIFEROUS RELATIONS OF THE TRANSITION TRACT®. (a.) In the greywacke and slate districts. (34.) The metalliferous indications appearing on a part of the Waterford south coast, lying immediately east and west of the Bonmahon river (§. 18.) have Phillips gives the following list. (See Encyclopedia Metropolitana, art. GroLocy, pp. 577 and 605.) Transition. Carboniferous. Terebratula Mantiz, (Sow. T. 277, fig. 1.) + Ems; Blankenheim.. * Ireland. T. platyloba, (Sow. T. 496, fig. 5,6.).. + Plymouth ......... - + Clithero. T. plicatella,(Dalman)...........- « + Plymouth; Gottland.. { Ratingen, (Von Dechen. T. diodonta, (Dalman) ............ -. + Eifel; Gottland...... { Ratingen, ‘Ctien Dechen.) (Sow. T. 324, fig. 3,) T. prisca, (Schlot. ley; Plymouth; Eifel;< Liege; also* But- T. 17, figadewina cis secves orcs sqcune Bensberg ; Gottland.. tevant, ( Wright.) 1 This is not now considered a Cardium. Professor Phillips brings it under a new genus, named by him, as above, Pleurorhynchus. The common form in which this shell appears is as figured by Sowerby; but in three instances I have found attached to the broader end of the shell a flattened rim round its border, while from the projecting part of the broad end proceeds a long tubular spi- nous process. Viscount Cole informs me he has seen this process in a large individual, extending to the length of three or four inches. 2 [ have long been persuaded of the importance of placing upon record an account of the geo- logical circumstances of mines, for independently of the light they assist in throwing on the phy- sical structure of the earth, they afford practical information to the miner and the landed proprietor, and may often prevent a wasteful application of capital. This latter evil might be remedied to a certain extent, if a legislative enactment were made, And according to Von Dechen, T. sit} South of Ireland; Dud- i Derbyshire ; Mr. Weaver on the Geological Relations of the South of Ireland. 25 given rise to mining operations at different periods, which seem in general to have been attended with little advantage. The greater part of the workings were shallow. To the westward of the river such operations were conducted upon fifteen different veins in the face of the cliffs, three being worked for lead, and the remainder for copper. Latterly, re- searches have been extended more inland, upon some old workings at Monachoe, to a depth ex- ceeding fifty fathoms, but they yielded only a small quantity of copper ore, the vein not = improved in depth. On the other hand, on the east of the river, a vein of copper ore discovered more recently at Ballinasisla, yielded valuable returns to a considerable depth, but latterly it has become nearly barren. On this part of the coast the old trials were conducted on seven veins for copper, and two veins for lead. These metalliferous veins affect, for the most part, a nearly north and south course, the dip being to the east or west, or to both in the same vein at different depths, They, however, frequently ramify both on the line of range and dip. (35.) The metalliferous relations in the county of Cork, refer chiefly to the lead mines of Ringabella and Doneen, and to the copper mines of Audley, Ballydehob, and Allihies. (36.) In the small inlet of Ringabella, on the western side of the entrance to Cork harbour, the slate, which is displayed on both banks, ranges east and west, and dips 80° south, and on the south side of the inlet rises a small low hill, in which is situated the Ringabella lead mine. This undertaking is conducted on a bed in the slate, composed of quartz and sparry iron ore with in- terlaminated slate, which contains galena, pyrites of copper and iron, and some calcareous spar. It is irregular in form, varying from a few inches to one and a half feet in width. The two first- mentioned substances predominate, the sparry iron ore often forming a drusy assemblage of cry- stals. Te lead ore appears in bunches, the copper ore is sparingly disseminated, while the iron pyrites is more abundant. I am informed that the trial has not been conducted to a greater depth than twenty fathoms*. (37.) In the southern cliffs of Doneen Inlet, on the western side of Clonekilty Bay, are the remains of old works, close to the sea, conducted, as reported, to the depth of thirty or forty fathoms. Judging by those remains, the object of research would appear to have been a bed in the slate, between one and two feet wide, composed of sparry iron ore and quartz, with dissemf- nated galena, and pyrites of copper and iron, and hence, in formation, bearing considerable arialogy to that noticed in the Ringabella mine. The range of the slate on this part of the coast is generally east and west, the strata being nearly vertical, or inclined at a high angle to the south. Upon the strand below the northern cliffs of Doneen, are displayed beds of sulphate of barytes, with intervening strata of slate, the former being mostly compact, or minutely granular-foliated, with some appearances also of the large lamellar structure. There are three of these beds, the obliging all adventurers in mines to lodge among the records of the county, in which any such mine was situated, a plan and section of the mine when abandoned, together with a report of its then state and circumstances, and the cause of its abandonment. _ * It is in the slate of Spring Hill, situated on the northern side and near the western extremity of Ringabella inlet, that the fine specimens of the Cork wavellite have been obtained. VOL. V.—SECOND SERIES. 10) 26 Mr. Weaver on the Geological Relations of the South of Ireland. northern being one and a half to two feet wide, the middle one about four feet, and the southern six or eight inches ; the interval of slate between the first and second beds being three to five feet, and between the second and third, twenty feet. These beds contain only a few specks of pyrites of iron and copper, and some galena sparingly disseminated. In their arrangement they are nearly rectilinear; but about ten fathoms north of the northern bed of sulphate of barytes, the slate forms acute-angled inflections, which are exhibited in a horizontal section. (38.) In the Audley mines, which are situated about ten miles south-west of Skibbereen, the metalliferous deposits are also contemporaneous with the rock, which consists of slate more or less quartzose, and passing into quartz-rock. The principal workings are on the town-land of Cappagh, conducted on a metalliferous bed, the inclination of the strata being at an angle of 80° to the south. The bed generally consists of quartz, accompanied by purple and green copper ores, but sometimes the quartz disappears, and the metalliferous deposit is confined to the slate alone, appearing in strings and flakes. The bed has varied in its course from an inch and less to two feet and a half in width, forming separate bunches connected by a leader ; and it is occasionally joined and traversed by contemporaneous veins of quartz, most of which are barren, but some contain also interspersed specks of purple and green copper ores. North of this bed is a second of a similar nature, which being only at a short distance, is wrought at the same time. These workings have been extended upwards of seventy fathoms in depth*. South of Cappagh mine the slate, after having become vertical, gradually acquires the northerly dip, which prevails also throughout Horse Island, adjacent on the south, varying here from 45° to 60° above the horizon. Here also may be occasionally observed a thin layer of slate (commonly varying from a line to three or four inches in width), which is penetrated with cupreous particles, namely, slight flakes of green carbonate of copper scattered between the lamine and in the fissures of the rock, accompanied by disseminated purple copper ore; and a similar layer some- times contains also quartz and a small portion of calcareous spar. Quartz veins likewise fre- quently traverse the rock, mostly ranging in the direction of the dip of the slate, and varying from a line to two, three, or four inches wide; but they often terminate at the distance of two or three feet. They are mostly barren, yet some contain slight flakes of the green carbonate, and specks of the purple sulphuret of copper; chlorite also is not uncommon. In the vicinity of these veins the slate is very quartziferous, and in some of the layers may be incidentally observed, interspersed particles of pyrites of copper and iron. A similar diffusion of metallic particles occurs in the slate of the townlands of Filemuck and Ballycomisk, which flank Cappagh on the north; seven discontinuous layers being dis- posed there, somewhat in an echelon order, and having given rise to as many different trials. The greater part of these trials extended only about ten feet, while one of them was 24 feet in depth ; but the principal, called Ballycomisk mine, was carried down to the depth of 20 fathoms, yet the working in the bottom seldom exceeded six fathoms in length, being that of the main bearing of ore. This was conducted on a bed of quartz mixed with slate, about two feet wide, containing yellow copper ore, specular and micaceous iron ore, some sulphate of barytes, iron pyrites, and a little purple copper ore. The cupreous deposits in some of these trials, have extended occasionally to the width of three or four feet in the rock. (39.) Analogous relations to those now described (§.38), occurred at the Ballydehob mine on *The Cappagh purple copper ore is sometimes accompanied with bismuth. An intermixture of these substances, analysed by Mr. Edmund Davy, Professor of Chemistry, Royal Dublin So- ciety, yielded 45 per cent. of copper, and 20 per cent. of bismuth. Mr. Weaver on the Geological Relations of the South of Ireland. 27 Mr. Swanton’s estate, situated about one and a half mile north of Cappagh. The works here ex- tended about 20 fathoms in depth. Some similar indications of ore occur on Lord Audley’s property adjoining the Ballydehob mine ; also on Mr. Becher’s estate, lying about one mile and a half to the north-west; also, one mile and a half further in the same direction, on Mr. Teulon’s land in Gurtinakilly. A similar occur- rence is to be observed about two miles south of Skibbereen on the townland of Moneyvolan, Co- lonel Townsend’s property ; and again in Hare Island, south-east of Horse Island. This diffusion of cupreous particles through a portion of the county of Cork is remarkable ; and it is to be hoped that the indications may lead to the discovery of some valuable deposit. (40.) Cupriferous peat-bog. In the year 1812 there existed on the eastern side of Glandore harbour, a peat-bog occupying a small dell, and extending over a very few acres, which was found charged with copper. The peat was in consequence cut out, burnt, and the copper thus be- came concentrated in the ashes. Forty or fifty tons of the dry peat produced about one ton of cupriferous ashes, which were sufficiently rich to yield a remunerating price when sold. Some of the ashes are said to have contained as much as 10 or 15 per cent. of copper. This discovery led to some trials in the vicinity with a view to find the source of the saline impregnation. In these researches, however, there were met with in the soil, only detached portions of iron ore and manganese, partly blended with quartz and sulphate of barytes. It seems not improbable that this deposition of copper in the bog, originated in the decomposition of some of the sulphurets of copper, contained in the vicinage, either in a metalliferous bed, or partially disseminated in the rock ; both of which cases, we have shown, are not of uncommon occurrence in this part of the island. Quarries of roofing-slate are worked near Glandore harbour, and other parts adjacent to the south coast; and of this slate considerable use is made in the country. But it cannot vie either with the Welsh or the Valentia slate. (41.) One of the most valuable copper mines in Ireland is that of Allihies, situated in the south-western extremity of the county of Cork, facing the entrance of Kenmare bay. It was dis- covered by a Wicklow miner in the year 1812, and it has been since wrought with great success, having yielded upon an average more than two thousand tons of merchantable ore per annum, which has been sold in the Swansea market, in general, at the rate of about £10 per ton. This body of ore has been derived from a powerful vein of quartz, which is of variable dimensions, but has in some parts been found enlarged to the breadth of thirty feet. The principal deposits of ore have occurred adjacent to the walls. The vein ranges in general in a north and south direction, intersecting the slaty rocks of the country, but in a part of its course it also runs parallel with the slate. The chief workings have been extended to adepth exceeding fifty fathoms, the prevailing ore being copper pyrites. (b.) In the Transition Limestone. (42,) The transition limestone of the South of Ireland has hitherto been found productive of metal in the county of Kerry alone ; viz., in the lead mines of Kenmare, and in the copper mines of Muckruss, Ross Island, and Crow Island. E 2 28 Mr. Weaver on the Geological Relations of the South of Ireland. (48.) The Kenmare limestone field (§ 23.) extends from west to east, through the following properties, opposite to which are placed the indications of metals observed in each respectively. TOWNLAND*, PROPRIETOR. INDICATIONS. Reens..........-+ Mr. Langford. Galena, copper pyrites, and blue and green car- bonates of copper, with calcareous spar. Dunkerrin.......- Dr. Thos. Taylor. Galena. Tibburid.......... Rev. Mr. Mahony. \ Iron ochre, galena, and iron pyrites, with cal- Gurtamullin ...... Ditto. careous spar. Kenmare town..... Marq. of Lansdowne. Galena with calcareous spar. Killowen......-+- Ditto. Galena, blende, iron pyrites, and iron ochre, with quartz and calcareous spar. Gurtagass & Cleady, Trinity College, Dublin. None observed. West Cahir ....... Marg. of Lansdowne. Iron ochre, blende, galena, iron pyrites, and green carbonate of copper, with calc. spar. East Cahir....-.. Ditto. None observed. Clontua.........+. Mr. J. Dillon Croker. Galena, blende, iron pyrites, yellow, grey, and purple sulphurets of copper, with blue and green carbonates, and calcareous spar. Ardtully Proper.... Ditto. Iron ochre, and copper pyrites, with calc. spar. Kilpadder.......-- Mr. Townsend Orpen. Copper pyrites, with calcareous spar, In the slate, adjoining the limestone on the north, are also the following indications. In East Cahir sips occa secs es cr ececeere Compact indurated oxide of iron. In Clontua.csccccceccccvecsevcccssces Green carbonate, grey and purple sulphurets of copper, and indurated oxide of iron. The above-mentioned metalliferous indications appeared for the most part of a confined, local character, bespeaking no permanent extension : yet, some seeming to deserve research by actual working, trials were made in Killowen in separate places to the respective depths of 42, 33, and 15 feet; in West Cahir to the depths of 45, 46, and 25 feet; and in Ardtully Proper to the depth of 15 feet. But in all these cases, however promising the appearances at the surface, the mineral deposits proved discontinuous, dividing and contracting so as finally to disappear, and thus penetrating the rock only to a small extent either in length or depth; yet in their position they were always nearly parallel to the range and dip of the bed in which they were included. The same results clearly followed the researches of former adventurers, made on the lands of Reens and Kilpadder, extending only a few fathoms in depth. The most extensive of the old trials were made in Clontua in the form of four open-casts, respectively 60, 80, 28, and 10 fathoms in length, two being on the same range, and two parallel to each other. The deepest did not ex- ceed 6 or 7 fathoms in depth, while none of the others penetrated beyond 10 feet. In these trials, as in others already mentioned, were chiefly found layers of calcareous spar of uncertain continuity, and bearing ore more or less sparingly. Researches were also made in the slate, north of the limestone, in East Cahir and in Clontua. In the former, the old adventurers had made an extensive open-cast and sunk some pits; but no ore appeared at the surface beside indurated oxide of iron. Workings, more recently instituted, * The scale of the map does not permit the position of the townlands to be laid down. Mr. Weaver on the Geological Relations of the South of Ireland. 29 traversed merely diluvial matter, among which was found only the same indurated oxide of iron. This mineral therefore was probably the object sought with a view to the manufacture of iron, at a time when the superabundant forests of the country were made applicable to that purpose *. In Clontua, adjacent to the limestone, five shafts had been sunk in the slate upon an E, and W. line, apparently 9 or 10 fathoms deep. New workings, conducted to the depth of 13 fathoms, discovered in the slate only a few strings of quartz with lenticular nodules of calcareous spar, ‘containing grey and yellow copper ores in filaments or minutely disseminated, which on being pursued disappeared altogether. (44.) The Muckruss mine consists of two works, an eastern and a western, conducted appa- rently (as indicated in the annexed plan and section), in the same bed of slate, included in the limestone adjacent to Turk Lake (§. 24.), and from one to three feet wide. Plan and Section of Muckruss Mine. Ww. wy, * Work — Sf ae oe Pay ry 8 SSSR Ero 74. of Outeyo, E. Work =| 3 =a LS Water S, a) SSS Water 5. ay ————————— es Turk Lake Scale,—Twenty fathoms to one inch, Eastern Work Both the eastern and western works were undertaken about the middle of the last century. In the latter rich yellow and grey sulphurets of copper prevailed, while in the former the ores con- sisted chiefly of copper pyrites accompanied by much iron pyrites. In the western work was found also a layer of arsenical cobalt ore from half an inch to two inches wide, and more or less inter- mingled with the copper ores. The cupriferous bed of slate is represented as interwoven with layers and laminz of limestone, and layers and veins of calcareous spar, in which the copper ores were contained in layers, strings, and disseminated ; but the ends of the workings having become narrower and less productive, the mine was abandoned fT. The eastern work was resumed in 1785, and again in 1801, but not continued. The bottoms were then stated to be 22 fathoms deep. The western was resumed in the year 1795, and again reopened in 1818, when on the examination of an able Cornish miner it was reported to be poor and unpromising. The bottoms are said to be 28 to 30 fathoms deep from the surface. a * The former excavations may have been made by the English colony planted at Killowen in the year 1670 by Sir William Petty, as it is stated that these people were employed in zron norks and a fishery.—See Smith’s History of Kerry, p. 317. y + According to Smith’s History of Kerry, p. 125, the Muckruss mines yielded in one year, after the works commenced, $75 tons of copper ore, which produced 26% per cent. of copper. 30 Mr. Weaver on the Geological Relations of the South of Treland. The outcrop of this bed at the surface appears in the form of iron ochre, which in the western part contains some intermingled portions of galena. (45.) The earliest working of the Ross Island mine, is ascribed to the times of the Danish in- roads; and the shallow parts above the level of the lake were evidently wrought by fire, being composed of chambers ofa rudely vaulted form. The works have been resumed at various periods ; one of the latest was in the year 1804, from which time the operations were continued until 1810. In this interval 3220 tons of ore were raised, the sale of which amounted to 69,487/., being on an average about 2117. per ton; and the standard price of copper during those years having averaged 1351. per ton, the ores appear to have yielded 174 per cent. of copper. In the year 1825 my attention was drawn to this mine, then filled with water, the level of which corresponded with that of the lake. The mine had been represented by some as a metalliferous bed, dipping to the south at an angle of 16° from the horizon, yet partially connected with irregular contemporaneous veins; while by others it was considered as a rake vein. In reference to what follows, the annexed plan and section of Ross Island mine will be found serviceable. They repre- sent the state in which the mine was left in the summer of 1829. Plan of Ross Island Mine with the Embankment. iy 5 Cilia py S “y e q Explanation ~ = Shafts Dy rae K Seale of feet ++ Bore holes : TT 300 400 Galleries and drifts. Deep level. Section of Ross Island Mine and Embankment from S. to N. on the line A—B. 5 2 Se LO aes ; 2 o¢ eS aa & s & § 2 = B = Ss Q il S S rr s ov & 2 § = $ s & Ru HighLevi 3 5 S Bore holes ~ of Low Level of Lake C2 a= Z Natural Clay = ae bottom only 50 Faths long from E. to W. => >> ia Mr. Weaver on the Geological Relations of the South of Ireland. 31 To redeem this mine I devised the following plan: 1. To form an efficient embankment, drawn from the west to the east through the deep water on the south, thus gaining a considerable portion of land from the lake: 2. To sink a new engine-shaft south of the old mine, intercepting in greater depth the metalliferous bearing, and forming there new workings: 3. To drain, in the mean while, the old mine by horizontal rods extending from the new engine-house to the old engine-shaft : 4. and lastly, By connecting the new with the old workings, to render the new engine-shaft the central point of drainage. The preliminary works having been completed in sixteen months, the drainage was effected in May 1827. The succeeding operations showed that the real geological circumstances of this mine had never been clearly understood. They proved, in fact, that the mine was not wrought upon a metalliferous bed, nor upon any real rake vein or true lode ; but that the metallic deposits formed a portion of, and were contemporaneous with the rock mass itself; being most unequally and irregularly distributed in the form of isolated portions, branches, strings, and particles of ore minutely disseminated, in a manner quite analogous to the strings, filaments, and other portions of calcareous spar which are also embodied in the substance of the limestone mass. Though thus irre- gularly incorporated with the rock, the general disposition of the metalliferous ground assumed an east and west range with a southerly dip, but without any wall or decided line of partition, so that the form of the excavation, made in any case, depended wholly on the extent to which the ore was disseminated, laterally as well as longitudinally, and deserved extraction. In the plan the shaded space indicates the extent of the excavations upon ground productive of ore, its northern extremity showing the actual outcrop at the surface upon an inflected line from east to west, and its southern extremity denoting the irregular limits of the metallic deposits in their “inclination to the southward. The dip of the excavations thus formed, is exhibited in the section. The northern (ore-grownd) inclines in general at an angle of 16° from the horizon, and the southern (ore-ground) at an angle of 35°; but to the westward they collapse, run together, and are finally attenuated in the form of a thin wedge, On the other hand, to the eastward, the southern body of ore-ground extends only a short distance beyond the meridian of the New Engine Shaft, while the northern body becomes in the eastern direction gradually more and more contracted in its dimensions, terminating, beyond the excavation called the Blue Hole, in occasional slight fila- ments and particles of ore, dispersed through the rock, unworthy of pursuit. The workings in the Blue Hole itself were conducted in the northern part on discontinuous branches and strings of yellow copper ore; and in the southern part chiefly on irregular masses imbedded in the rock, which consisted of an unprofitable compound of blende, galena, and iron pyrites, with a slight intermixture of copper ore. Yet considerably to the westward, adjacent to the Cliff shaft, an isolated, profitable bearing of good yellow ore was met with, but this did not ascend to the surface. In short, Ross Island consists for the greater part of what may briefly be called the siliceous limestone, namely, a series of thin, alternating beds of lime- stone, hornstone, quartz, and lydian stone, with some few of clay-slate inter- posed. This series supports, at the southern angle of the isle, continuous, thick strata of blue limestone, which form a body, in its highest part, from ten to twelve fathoms in thickness, and, in its lowest part, about six fathoms. The blue limestone rests in a perfectly conformable position upon the siliceous lime- stone, the inflection of the two kinds of rock corresponding throughout, rising 32 Mr. Weaver on the Geological Relations of the South of Ireland. and outcropping to the north at an angle of 40° to 45°, but in descending to the south, gradually flattening to an angle of 6° or 7°, and on approaching the lake becoming absolutely horizontal. The line of division thus marked in the section, between the two descriptions of limestone, serves to indicate correctly their coinciding stratification ; and by the miner it is familiarly termed the flat bed. ‘The juxtaposition of the two rocks is, in most cases, so close as scarcely to admit the blade of a knife ; but in some places the line of separation is expanded to a few inches, and, though very rarely, even to two or three feet ; the interval being occupied by clay, either wholly barren, or containing occa- sionally iron pyrites, or disseminated particles of copper ore, derived from the deposits above. The metallic deposits, thus described, occur in the blue limestone mass, and terminate in their descent to the southward on reaching the flat bed, never penetrating into the subjacent, silice- ous limestone. The galleries, drifts, and sinkings proved this fact. The two former (distinguished in the plan and section by narrow lines) are wholly driven in the blue limestone, the siliceous,lime- stone forming their floor; and in the deep level (marked by broader lines) the siliceous limestone is chiefly cutinto. The new engine shaft penetrated 44 feet into the siliceous limestone, and a bore- hole from its bottom went 314 feet deeper; and a cross-cut was driven from Cock’s shaft wholly in the siliceous limestone under the Blue Hole, and connected therewith by a bore-hole ; yet by none of these operations was a particle of ore found in this rock, The experience thus gained prognosticated an early termination to this mining adventuré, un- less further discoveries could be made either within or beyond the then existing excavations. With the former view, drifts were opened from the Cliff shaft to the north-east and east ; and by eight bore-holes the ground was also searched in the south-eastern quarter; but by neither operation was any discovery effected. Galleries were likewise extended to the westward, and by one of these, productive ground was laid open, which led to the excavation of a whole mass of rock, containing disseminated ore, from the flat bed up to the very surface, as indicated by the darker-coloured, triangular space marked on the plan. To try the ground effectually to the north of the mine, both in the blue limestone and the sub- jacent siliceous limestone, the following measures were adopted: (See Section.) 1st, A cross- cut was driven twenty fathoms north from No. 8 shaft in the blue limestone, and a winze or pit was then sunk in the siliceous limestone five fathoms deep, from which a bore-hole went five fathoms deeper. 2nd, Another cross-cut went north-west nineteen fathoms, being fifteen fathoms beyond the ore ground, and a bore-hole was put down beyond it. 3rd, A series of bore-holes, thirty in number, were distributed over the north ground, descending in all cases through the blue lime- stone into the siliceous limestone, and in a few instances perforating the latter rock to the depth of five fathoms. 4th, Trenches were cut down to the blue limestone rock, and extended to the north nearly to the siliceous limestone, which crops out there at the surface. By none of these re- searches was any discovery made. I must here observe that had any true lode or rake vein, upon whatever range, existed within the precincts of the mine, it must have been discovered in the course of working; and the same assertion holds good with respect to any vein which might have ranged north and south in the ground, north of the mine; and with regard to any vein upon an east and west range in the north ground, the trenches would have made its discovery. Again, had any irregular metallic deposit, Mr. Weaver on the Geological Relations of the South of Ireland. 33 analogous to those occurring in the existing mine, been contained in the north ground, it must have been detected either by the bore-holes distributed over that surface, or by the trenches. The preceding details, which may perhaps more immediately interest professed miners, are yet important, since they establish the geological relations of this mine both in a positive and negative manner; and they may thus prove useful to future inquirers in researches of a similar nature. During the course of operations between May 1827 and May 1829 inclusive, 15294 tons of ore were raised, averaging in produce 132 per cent. of copper, the sale of which amounted to 18,0901. 18s. 9d., being equal to 11/. 16s. 6Zd. per ton; the average standard price of copper during that time having been about 108/. per ton. In the earlier part of this undertaking the ore raised, amounted sometimes to nearly 100 tons per month; but the last month’s work yielded only 29 tons, the main deposits of ore having, in fact, been worked out. These ores consisted chiefly of grey, yellow, and purple sulphurets. Green and blue carbonates and tile copper ores, with small portions of native copper and crystallized red copper ore, occurred much more rarely, having been chiefly found in the part of the blue lime- stone immediately over the flat bed. Intermingled particles of galena were likewise incidentally met with, as well as blende and iron pyrites more in mass. This remarkable metallic deposit, coeval in its origin with the limestone rock itself, must have yielded, from first to last, a produce exceeding in value 100,000/. sterling. As dependent on the structure and condition of the limestone rock, I think it necessary to add a few words on the water of this mine. When full access had been obtained to the interior, fissures were found, in general nearly vertical, some upon a north and south, and others upon an east and west range, which, in the course of their extent, varied from the tenth of an inch to four or five feet in breadth, the expansions being sudden, irregular, and of comparatively short continuance. These fissures and cavities are commonly filled with a closely compacted mass of pebbles, gravel, and sand, imbedded in clay, and, when persistent, generally impervious to water; but unoccupied intervals occurring in some places, it is easy to conceive that upon such fissures passing outwardly to the lake, those spaces would become gradually enlarged by the fretting of the lake water, and the feeders of the mine be proportionately increased. Nor was this the only source of the water flowing into the mine. From the horizontal disposition of the flat bed in its direction to the south- ward, ascertained by the cutting of the deep level, it became evident that the flat bed must run into the lake at the distance of about twenty fathoms from the embankment in the deep water, opposite to Dyer’s shaft, the bottom of the lake deepening in that quarter rapidly to the south*. And the surge of the lake, which in a storm is like a tempestuous sea, could not but press its waters with an increased impetus, fretting, by the line of the flat bed, into the mine. And such was found to be the case in the progress of the deep level to the westward, Thus the discharge of water, from a depth of 95 fathoms, was, from May to December 1827, 32 to 4 tons per minute; and afterwards from a depth of 103 fathoms, between December 1827 and April 1828, 4 to 5£ tons per minute, and in June 64 tons per minute ; but after the deep level had passed Spillane’s shaft, it increased progressively to 8, 9,10, and 114 tons per minute. This was caused by the deep level cutting a vertical fissure four inches wide, and by the opening of the flat space between the blue and siliceous limestone, to the height of nine inches. By the latter line great quantities of pebbles were washed into the mine. As a check to the influx of water, dams * At the distance of 200 fathoms from the embankment, south of Dyer’s shaft, the lake has, in fact, acquired the depth of 35 fathoms, which it retains to a considerable extent, the deepest point being 40 fathoms, whence the bottom rises gradually to the opposite shore. VOL. V.~—-SECOND SERIES. F 34 Mr. Weaver on the Geological Relations of the South of Ireland. were fixed in the level ; but from thenceforward, namely, to May 1829, the average discharge from the mine was 8 or 9 tons per minute. When required, the steam engine (of 36-inches cylinder, working single,) has been made to throw out 133 tons of water per minute, or nearly 20,000 tons in 24 hours. (46.) In Crow Island, which is situated about half a mile to the eastward of Ross Island, and is of small extent, being only about twenty fathoms in breadth, the mine is said to have yielded about 100 tons of coppersore of inferior quality. This was obtained from slight, contem- poraneous strings, isolated portions and particles of ore, of uncertain distribution in the blue lime- stone rock, and blended more or less with calcareous spar, and partially contaminated by an inter- mixture of blende, iron pyrites, and galena; the formation being analogous to that prevailing in the vicinage of the Blue Hole at Ross Island, was poor and unpromising. The principal working was about fifteen fathoms long and six fathoms deep, the line of excavation ranging 30° west of north and.east of south, with an inclination of 65° to the south of west. II.—Carponirerous SERIEs. I. In South Munster, viz., in Cork, Limerick, and Kerry. Old Red Sandstone*. (A7.) In the eastern quarter of our field, I have first to notice the old red sandstone of Kilworth mountain and the adjacent hills, on the north of the * I may here remark, that tracts of transition rocks analogous to those described in this paper, (in which conglomerates, sandstone, and quartz-rock, are of such common occurrence,) appear in many cases to have yielded a large proportion of the materials of which the old red sandstone of British geologists is composed. And that the great carboniferous order, or series, forms, in gene- ral, an independent and consistent group, appears proved,—1. by the predominant unconformity of its position, in relation both to subjacent and superjacent systems; 2. by the general absence of organic remains in the old red sandstone; 3. by the organic reliquiz peculiar to the carbo- niferous limestone and the coal formation; and 4. by the not unfrequent interstratification of these three members in the order of succession. Several organic exuvize, however, being common both to the transition and carboniferous orders, while many are peculiar to either series, affinity as well as difference is thus indicated; but the discordant position of the two systems appears conclusive as to their different eras of production. Some of the foregoing positions I find entertained also by M. Hoffmann in his General View of the Geological Relations of the North West of Germany, 1830. (vid. Uebersicht 2te A btheilung, pp- 503, 504, and 589 ;—positions which I advanced and partly developed between the years 1818 and 1824 in the Geological Transactions and Annals of Philosophy. See in particular the Annals of Philosophy for the years 1821, 1822, 1823, and 1824. But I differ from that author in not including, as he does, in the carboniferous series, the red sandstone that is interposed be- tween the coal measures and the magnesian limestone (Zechstein). In this, however, he is not singular, as German geologists in general had, to that date, done the same, comprehending with him under the head of rothe-todte-liegende the whole of the carboniferous series, together with the red sandstone subjacent to the magnesian limestone. If the use of the term rothe-todte-liegende be still continued, it may be well to restrict it to this red sandstone, lying between the coal forma- Mr. Weaver on the Geological Relations of the South of Ireland. 35 river Blackwater. Furrowed by defiles and ravines whose course is toward the vale of the Blackwater, the subjacent clayslate is exposed to our view, in strata nearly vertica!, supporting the sandstone formation in unconformed posi- tion. The formation, as here exhibited, may be taken as a good example of the old red sandstone of Ireland, and it will bear a close comparison with that of England, to which it is quite analogous, presenting the same varieties in colour and composition, and consisting of compact and slaty beds of firm sand- stone, associated with others of a looser texture, with sandstone conglomerate, and with beds of indurated clay and slaty clay ; the reddish brown colour pre- dominating in the series. (48.) Within the ranges of the Gaultees, Slievenamuck, Slieve Riagh, and Seefin mountains, clay-slate and greywacke rocks (partially traversed by small veins of calcareous spar) form their foundation, in a position nearly vertical, ranging from the glen of Aharlow to the westward, and upholding on each side unconformable, continuous mountain masses and isolated caps of the old red sandstone formation. An expansion of this sandstone spreads, on the north, into the plains of Limerick, extending westward to, and constituting the substance of, the three ranges of hills called Knockfeernagh, Kilcruaig, with Knockaderry, and Kilmeady ; yet excepting the knoll of Knockfeernagh, which consists of greywacke, and greywacke slate. The sandstone of the plain is generally fine-grained, and yields good flagstones in the quarries adjacent to the road between Kilmallock and Bruff, where it is about three miles wide, nearly horizontal, or gently undulated on the large scale, sup- porting the carboniferous limestone in conformable position both on its northern and southern sides, and dipping in the former 10° to the north, and in the latter 20° to the south. In the ranges of Knockfeernagh, Kilcruaig, and Kilmeady, the sandstone is generally composed of granular quartz, with interstices partly filled with white or yellowish earth (like decomposed felspar) or yellow or brown oxide of iron, scales of silvery mica being sparingly scattered through the mass. When the mica is more abundant, the rock takes a coarse slaty structure. When con- sisting of nearly pure grains of quartz, closely compacted, it approaches to the character of quartz- rock. Though associated with beds of red, indurated clay, and slaty clay, its general colour is yellowish or greyish white ; but where a greater diffusion of iron oxide takes place, it acquires a brownish or reddish tinge. Each range is formed of strata nearly horizontal on the top, tion and the magnesian limestone, as is the practice with English geologists, so as to avoid the con- fusion which has arisen from its extended German signification. On the geological relations of the magnesian limestone, and the subjacent red sandstone in the North of England, compared with their equivalents in Germany, a clear light has been thrown by Professor Sedgwick in his admirable Memoir, published in the Third Volume of the Geological Transactions, Second Series, 1829. F2 36 Mr. Weaver on the Geological Relations of the South of Ireland. but which on the sides decline toward the limestone plain, under angles varying successively in different quarters from 60° to 40°, 30°, 20°, and even as low as 15° and 10°. The superposition of the limestone to the sandstone may be traced in some places, as at the western ends of the ranges of Kilmeady and Knockaderry ; and near the points of contact the limestone is sandy. Looking to the composition and structure of Knockfeernagh, it may be presumed, that all the three ranges derive their forms from subjacent ridges of greywacke and slate, the sandstone conforming to their surface. In the pro- truding knoll of Knockfeernagh, the greywacke and slate range to the east and west, dipping 85° to the north ; but in the defile below, which traverses the range from north to south, on the east of the knoll, there exposing those rocks, they dip 80° to 85° to the south ; the opposite dips doubtless arising from a flexure of the strata in their descent. They are here surmounted by beds of sandstone and red slate-clay in nearly horizontal position. The projecting knoll above is surrounded by the sandstone on every side, and the greywacke and slate which compose it may be described as follows. A base of clay-slate more or less incorporated with mica, or chlorite, or quartz, and enveloping rounded or angular fragments of hornstone, quartz, and slate; usually containing also, scattered through the mass, scales of silvery mica, particles of vitreous quartz, and more rarely fragments of felspar. Calcareous spar, more or less disseminated, is also not an uncommon ingredient. When in a state of disintegration, the exhibition of yellow and brown oxides of iron becomes very abundant. The same rocks, in the defile below, partake more of the character of a compact clay-slate or nova- culite, enveloping some of the other ingredients mentioned. These include a bed of stratified quartz rock, about ten fathoms thick, consisting almost wholly of simple granular quartz-rock, closely consolidated, and exhibiting a small splintery fracture. (49.) I have already remarked (§. 10. and §. 13.) that in the western quar- ter of our field, the old red sandstone of Slieve Meesh overlies the transition rocks of Cahirconrée in their range to the eastward ; and that they reappear more east from beneath the old red sandstone, forming a low ridge of grey- wacke, which crosses the river Maine near its head: partly separating the vale of the latter from that of Castle Island, and supporting there, on each side, the carboniferous limestone. The old red sandstone of Slieve Meesh may be best studied from the north- ern side, where it is penetrated by deep sinuous glens and ravines. The southern side of the range being little interrupted, does not present the same facilities for observation. Between three and four miles to the south-west of Tralee is the mouth of Curahene glen. At two and four miles east of this, respectively, are the two mouths of Blennerhasset’s glen, the more distant being adjacent to the old road leading from Tralee across Slieve Meesh to Castlemaine. Two miles still further east, are ravines adjoining the old road Mr. Weaver on the Geological Relations of the South of Ireland. 37 from Tralee to Killarney. In the last-mentioned locality may be observed alter- nating beds of red sandstone, red and mottled indurated clay, and red, mica- ceous, slaty clay. These beds, where exposed in the higher lands, are nearly horizontal, or incline gently to the north ; but in descending toward the carbo- niferous limestone of the vale of Tralee, they successively dip 20°, 15° and 10° north. At the eastern mouth of Blennerhasset’s glen are similar beds, inclined 25° tothe north. They repose on continuous strata of solid red sandstone, reaching nearly one mile up the glen; but the sandstone gradually loses the intense red colour, becoming generally of a brownish grey hue. The lowest angle observed in the dip of the beds in this glen, was 15° to the north. The approach to Curahene glen is rendered very striking by the immense accumulation of blocks and boulders of red sandstone and sandstone conglo- merate, which form a kind of promontory, proceeding from the mouth of the glen to the plain below, and expanding there to the east and west. Through this accumulation, the stream which issues from the glen, winds its way, having high banks on both sides. In the glen upward, the banks also are composed of similar debris, and the firm rock is first displayed, in any continuity, in the brows overhanging the northern entrance of the glen, where sandstone and sandstone conglomerate dip 30° to the north. Further up the glen these rocks approach nearer to the horizontal position ; and still more south, a reversed inclination toward the south becomes perceptible. The sandstone of this glen, whether in situ or detached, is remarkable for its uniform red or purplish colour, with little difference in the shade. It is commonly of a rather coarse structure, and some varieties of the conglomerate contain rounded and angular frag- ments, chiefly composed of quartz, as large as turkey’s eggs. The beds of red clay and slaty clay, associated with the red sandstone in the northern confines of the formation, appear to decline in their progress west- ward into the vale, and they probably pass into the sea to the south of Blen- nerville. (50.) To the north of Tralee bay, the old red sandstone reappears, forming Kerry Head, and arranged in strata nearly horizontal on the higher lands, but declining thence, on every side, at angles as low as 15° to 10°. In the cliffs along the shore, extending from Ballyheige castle to the westward, and round the Head to the north side, the rocks are well exposed, showing beds of firm sand- stone of brown, red, grey, bluish and greenish colours, associated occasionally with beds of red, indurated clay and slaty clay, both simple and micaceous ; sandstone conglomerate also occurring in the series. 38 Mr.Weaver on the Geological Relations of the South of Ireland. Carboniferous Limestone. (51.) This formation is found both in the western and eastern portions of our field, reposing either directly and unconformably on the transition series, or conformably on the old red sandstone, when the latter intervenes. Thus in the west, at the junction of the valleys of the Laune and the Maine, the limestone rests on the transition rocks ; but in its circuitous course eastward up the latter valley, across that of the Brown Flesk, and around, past Castle Island, westward to Tralee bay, it reposes chiefly on the old red sandstone of Slieve Meesh, while to the east it appears resting on the greywacke projection which forms the eastern foot of that range, already noticed in §. 49. North of Slieve Meesh, and south of Tralee, the limestone is slightly inclined to the north, yet gently undulated. North of that town, the strata are more nearly horizontal ; but about midway between it and Castle Island, they dip 60° to 65° to the north, forming protruding knolls on a line three miles in ex- tent. Further east, and to the south of Castle Island, and around the grey- wacke which projects into the vales of the Brown Flesk and the Maine, the limestone is nearly horizontal, yet subject to undulations, as it also is in its further progress down the valley of the Maine, the latter variations in the dip being from north to south ; while in the line of contact with the old red sand- stone on the south side of Slieve Meesh, the general dip, as exhibited in the quarries, is 20° to 25° to the south. Again, to the north of Ardfert the lime- stone reposes on the old red sandstone of Kerry Head, while both are over- laid in that quarter by an outlying portion of the coal measures. It will be hereafter seen, that the limestone of this district, which in its de- vious course is continued from Tralee bay to Listowel on the north-east, and thence to the mouth of the river Shannon on the north-west, is in conformable position with the superincumbent coal measures, wherever denudation affords an opportunity of observation. (52.) In the eastern quarter, the carboniferous limestone first appears on the south of the Blackwater in Dromaneen townland, about four miles west from Mallow ; and in the Marble-hill quarry the stratification is well displayed, thin beds of black limestone and grey and black slate-clay alternating with each other, the whole dipping 10° to the north; while the greywacke, sandstone, and slate series, which form its southern and western boundary, dip to the south. West of Dromaneen, the greywacke country extends about six miles, before we reach the transition limestone near Roskeen Bridge. Following the line of the Blackwater to the east, the limestone is found in some parts occupying both banks, and in others confined to one bank of the Mr. Weaver on the Geological Relations of the South of Ireland. 39 river, as may be seen in the map; but the stratification is often ill developed. On the east of Mallow there appears a disposition to the northerly dip. Ap- proaching Fermoy the strata imcline toward the south, conformably with the old red sandstone in Kilworth mountain, in which quarter, viz. in the defile called Araglen, may be remarked an outlying portion of the carboniferous limestone, about two miles in extent, the connexion of which with the same formation in the vale of the Blackwater, appears to have been interrupted by denuding causes. Near Lismore the dip is also to the south; but between Cappoquin and Dungarvan bay the strata appear to form an arched inflection from north to south, abrupted at the surface, and hence showing a northern and southern dip on the sides, with nearly vertical strata intervening. In Ballynacourty Point, which forms the northern side of Dungarvan bay, and in the ledge of rocks stretching out eastward into the sea, the limestone strata are arranged according to a semicircular flexure, the dip being successively to the north, the-east, and the south. The limestone alternates in some parts with slate clay. On the other hand, the greywacke and slate ranges, which immediately flank on the north and the south, the vale of Dungarvan, and the line of the Blackwater higher up to the west, generally dip 70° to 75° toward the south. (53.) In the northern and more central portion of our field, the limestone is supported by the old red sandstone, being inclined, where contiguous to that formation ; but-in the plains it more nearly approaches to the horizontal position, as at Ballydaniel, two miles north of Broadford, and at Newcastle, in the line of the river Arrow, yet it is subject to local inflections at higher angles, arising from undulations in the strata. The same appearances are observable in pro- ceeding further north toward the Shannon, and north-east toward Limerick. (54.) The limestone of our tract is frequently continuous over a large area ; but, as already shown, it occasionally alternates with slate-clay or shale, as in the central part of the district, at the Broadford quarries, two miles west from Drumcullaghar. | It is also associated with lydian stone, hornstone, black car- bonaceous shale, trap, and porphyry. Its association with lydian stone is well developed in the hilly ground ad- jacent to the south side of the Guestin river, above its confluence with the Laune, containing, as in the Listry quarry, beds of that substance, from a few inches to three and four feet thick. . The dip is to the north, while on the opposite side or right bank of the stream, as at Lisinvane, the dip is to the south, the beds consisting chiefly of brown shale, lydian stone, and horn- stone, with others of black limestone. This part of the stream appears to run in a concavity formed by an undulation of the strata. 40 Mr. Weaver on the Geological Relations of the South of Ireland. (55.) The association of the limestone with black carbonaceous shale, may be observed to advantage both in the west and east of the field. In the west, these rocks appear on the coast to the north of the Cashen or Feale river, extending nearly two miles between Ballybunnian and Lick Castle, alternating both in thin and very thick beds, whose general inclination is to- ward the north-east, yet undulated on the large scale, commonly under an angle of 25° to 30°, but in some places they are at high angles, and even ver- tical. These great undulations have been broken in upon, by inroads of the sea in a direction from west to east, forming six or seven inlets or coves, in which, by abruption and perforation, the rocks have been wrought intoa variety of fantastic forms, with archways and caverns winding into the interior. In the black shale, iron pyrites being incidentally disseminated, and mutual de- composition taking place, alum, hydrate of iron, &c. are produced, and the face of the rock becomes stained with white, yellow, brown, and reddish depositions. These substances penetrate also into the fissures of the rock, in which wavellite likewise is found. In the east we may notice that portion of the carboniferous limestone which is adjacent to the angular boundary, formed by the conjunction of the counties of Cork, Limerick, and Tipperary. It there contains massy beds, both of grey slate-clay and black carbonaceous shale, in the latter of which iron py- rites is not unfrequently distributed. The appearance of this black shale gave rise to trials for coal about forty years since, several pits having been sunk for that purpose, but without any success. (56.) The association of the carboniferous limestone with trap and porphyry, has been treated by me, at some length, in my Memoir on the East of Ireland*, and I therein indicated (§. 178.) that the distribution of those rocks in the lime- stone, was probably more extensive than I had then an opportunity of ascer- taining. The subject has since been resumed, both by Dr. Apjohn+ and Mr. Ainsworth {, and to the respective memoirs of those gentlemen I beg to refer for the details of their extended researches. With Captain Sabine, R.A., and Mr. Ainsworth, I have since had the satisfaction of visiting part of the ground formerly left by me unexplored ; and in the map I have introduced the range of the trappean and porphyritic series determined by the latter. Of that portion of the district which lies to the west and north-west of the field for- merly examined by me, a general view may be obtained from the hill of Car- rig Parsons, situated about midway between Limerick and Pallis Hill, over- looking the vale which extends to the foot of the Bilboa mountains on the north. * Geol. Trans., First Series, Vol. 5. + Journal of the Geological Society of Dublin, No. 1. + Ibid:; No. 2. Mr. Weaver on the Geological Relations of the South of Ireland. Al The hill is composed of limestone, and the strata are curved from south to north, but the crown of the arch is ruptured, the line of fracture being from south-west to north-east, and the beds basset out on the opposite sides of the rupture under an angle of 30°, in the western part of the hill dipping toward the vale, and in the eastern from the yale. The strata in the eastern part of the rupture present a bluff toward the valley, which is on a line with the bluff of Knockeen limestone hill, distant a few miles on the east, while still further east, on the same line, appears the trap bluff or precipice of Pallis Hill, im- pending over Linfield. As viewed from the summit of Carrig Parsons, the trap ranges are most prominent on the south-east near Pallis Hill; thence re- ceding toward the south and west, through the Cahirconlish, Carrigfeoch, Bal- lochbega, Ballinaguard, Knocknea, and Cahirnarry ranges ; while to the north- west, and more insulated, rise the trap hills of Carrig O’Gunnel, adjacent to the Shannon ; and to the west of north appears the insulated trap range of New- castle, which, in its extension west, approaches within a short distance of the artillery barracks at Limerick. In the series of such of these trap and por- phyry rocks as have come under my view, I have not succeeded in finding the stilbite, mesotype, and olivine, which Mr. Ainsworth states he had noticed. I shall here merely add a few remarks on the trap formation at Carrig O’Gunnel, Knocknea, Cahirnarry, and the porphyry south of Lough Gur. The castle of Carrig O’Gunnel is built on a protruding mass of trap con- glomerate, amorphous, and irregularly traversed by fissures. The paste of the conglomerate is chiefly compact felspar, variously coloured, and sometimes mot- tled, but most commonly of a reddish hue, apparently much charged with iron; but in some places it consists of very fine-grained, compact greenstone. The base envelopes fragments of limestone, mostly angular, sometimes as large as the head, and even larger, also fragments of trap corre- sponding more or less in composition with the paste. Among these may be noticed also basalt with shining facets of small and minute grain. In the trap, calcareous spar appears as the most common ingredient, and portions of green earth are also incidentally diffused. Where the calcareous spar has decayed, the rock is porous and vesicular. To the north of Castle Carrig O’Gunnel hill, is a lower hill, which consists of calcareous conglomerate, a base of limestone with some green earth diffused, inclosing numerous fragments of trap. In these conglomerates occur numerous crinoidal remains ; also broken bivalves; and I noticed one specimen of Cyathophyllum. The trap conglomerate of Knocknea resembles in many respects that of Carrig O’Gunnel, but it is disposed in tabular masses, nearly horizontal, dip- ping only a few degrees to the north-east. A defile separates this hill from that of Cahirnarry, on the north. The latter consists of compact basaltic greenstone, containing acicular crystals of glassy felspar, and grains of horn- blende or augite, and it is disposed in a rudely thick, columnar form, without distinct sides. To the north-east of Cahirnarry is a lower hill, which appears VOL. V.—SECOND SERIES, G 42 Mr.Weaver on the Geological Relations of the South of Ireland. chiefly composed of flat tabular masses of trap conglomerate (enveloping, as usual, fragments of limestone), and generally of a greenish colour, from the intimate diffusion of green earth in its composition. To the east of this, and about one mile from Cahirnarry trap hill, is the limestone hill of Carrig Par- sons, which I have already mentioned. There are few parts of the trap district in which the red felspar porphyry, is better developed than in a hill called Knock Derg, situated to the south of Lough Gur. The basis is chiefly a finely granular or compact felspar, containing crystals of glassy felspar ; the whole being, where the rock is fresh or not weathered, of a deep flesh colour or reddish brown, or of a brownish red cast. When much disintegrated, the stone, at the first glance, looks like a dirty or brick-red sandstone. The porphyry, however, is not uniformly red or brown, being in some places striped or mottled with disseminated portions of green earth. The mass of the rock is formed occasionally of spheroidal or ovoidal concretions, which separate by atmospheric influences into concentric layers. Toward the northern foot of the hill green-coloured trap conglomerate also occurs. It is much to be wished that some one, possessed of the necessary leisure and gifted with sufficient devotion, would construct an exact topographical map of the Limerick district occupied by trap and porphyry, showing in all cases, by the aid of sections, the precise relations of these rocks to the limestone with which they are there associated. (57.) Large tracts of the limestone field may be traversed without encoun- tering more than a few, thinly scattered, organic remains. It is from local de- posits met with incidentally, that they are chiefly to be procured. One of the most productive is in the valley of the Maine, in the Ardconnaught quarries, and adjacent to Castlemaine mine. The following is a list of those I procured in that quarter ; and the fossilist will readily notice that while most of the or- ganic remains enumerated, are of common occurrence in the carboniferous limestone of other countries, several are also found in transition tracts, some of which have hitherto been considered as distinctive of the transition period : to these I have prefixed the mark, § . But to such as have hitherto been noticed only in the Cork transition lime- stone, and not in other transition tracts, I have affixed the mark (c.) The signs {| { have the same import as was explained in §§. 13 and 33. Crustacea : § Calymene concinna, (Dalman, ‘Tab. I. fig. 5.)!, besides fragments of one or two indeterminate species of Trilobite. 1 Om Paleeaderna eller de si kallade Trilobiterna af J. W. Dalman. Ur K. Vet. Acad. Hand- lingar, 1826, Stockholm, 1827. Mr. Weaver on the Geological Relations of the South of Ireland. 43 Cephalopoda polythalamia : § Orthoceras striatum, (Sow. T. 58.) t- O. undulatum, (Sow. T. 59.) t. O. unguis {, (Phillips, Plate X XI. fig. 2.) ! Nautilus globatus, (Sow. T. 481.) tf. N. multicarinatus, (Sow. T. 482. fig. 1, 2.) c. t. N. ovatus, (Ellipsolites of Sow. T. 37.) t. A Goniatite also occurs. The Orthoceras striatum appears very frequently, sometimes exceed- ing two feet in length, and five and a half inches in diameter at the larger end. : Cephalopoda monothalamia : Bellerophon tenuifascia, (Sow. T. 470. fig. 2, 3.) +}. Gasteropoda : Euomphalus catillus, (Sow. T. 45. fig. 3. 4.) +f. Pileopsis vetusta, (Sow. T. 607. fig. 1 to 3.) +}. Ampullaria helicoides, (Sow. T. 522. fig. 2.) c.f. Cirrus acutus, (Sow. T. 141.) tf. Melania constricta (Sow. T. 218. fig. 2, and Phil., P]. XVI. fig. 1.) t. M. tumida, (Phil., Pl. XVI. fig. 2.)t, and another species of Melania or Turritella unde- termined. Natica ampliata, (Phil., Pl. XIV. fig. 21 and 24.) {, and one other turbinated shell less distinct. Conchifera : The prevailing species are referable to the genera Producta, Spirifera, and Terebratula: viz. Producta scotica, (Sow. T. 69. fig. 3.) Tt. P. Martini, (Sow. T. 317. fig. 2, 3,4.) ¢.f. P. concinna, (Sow. T. 318. fig. 1.) c.f. P. lobata, (Sow. T. 318. fig. 2 to 6.) c.f. P. punctata, (Sow. T. 323.) c.f. P. fimbriata, (Sow. T. 459.) t. P. analoga, (Phil., Pl. VII. fig. 10.) {, and two other species of Producta not yet named. Spirifera cuspidata, (Sow. T. 120.) +f. S. striata, (Sow. T. 270.) +f. S. pinguis, (Sow. T. 271.) tt. S. octoplicata, (Sow. T. 562. fig. 2 to 4.) tt. S. resupinata, (Terebratula, Sow. T. 325.) c.f. S. glabra, (Sow. T. 269. fig. 1.) tf. S. obtusa, (Sow. T. 269. fig. 2.) Tf. S. attenuata, (Sow. T. 493.) +t. S. bisulcata, (Sow. T. 494. fig. 1, 2.) f. S. squamosa, (Phil., Pl. X. fig. 21.) f. S. semicircularis, (Phil., Pl. IX. fig. 15, 16.) j. S. glabristria, (Phil., Pl. X. fig. 19.) t. S. expansa, (Phil., Pl. X. fig. 18.) t. \ considered as one species by Professor Phillips. ‘ See the very valuable and elaborate Illustrations of the Geology of Yorkshire, by Professor Phillips, Part II. Mountain Limestone District. G2 A4 Mr.Weaver on the Geological Relations of the South of Ireland. Conchifera : (continued) Spirifera rhomboidea, (Phil., Pl. IX. fig. 8, 9.) f. S. insculpta, (Phil., Pl. IX. fig. 2, 3.) t, besides three species of Spirifera not yet named. Terebratula crumena, (Sow. T. 83. fig. 2, 3.) +f. T. cordiformis, (Sow. 495. fig. 2, 4.) c. T. pugnus, (Sow. 497.) +f. T. pleurodon, (Phil., Pl. XII. fig. 25, 26, 27.) {. T. radialis, (Phil., Plate XII. fig. 40, 41.) t; besides several other Terebratulz, some of which appear referable to— T. elongata, (Schlotheim ,T. 20. fig. 2.) t..) Considered as the same species by Von Buch. T. lata, (Schlot. T. 20. fig. 3.) t. (See p. 100, iiber die Terebrateln.) T. rostrata? (Schlot. T. 16. fig. 4.) +, Spirifera. T. levigata, (Schlot. T. 18. fig. 1.) +}, Spirifera; seems more nearly allied to Spirifera glabra than to S. oblata of Sowerby. But these are severally given by that author as derived from transition tracts on the Continent’. Among the Bivalves are also to be noticed, Isocardia vetusta (Phillips), the upper valve of a Posidonia (Phillips). Pleurorhynchus elongatus, (Phil., Pl. V. fig. 28. Cardium, Sow. T. 82. fig. 2.) }. P. hibernicus (Phil. Cardium hibernicum, Sow. T. 82. fig. 1. 3.) c.f. Pecten plicatus (Sow. T. 574. fig. 3. and Phil., Pl. VI. fig. 21.). P. dissimilis (Phil., Pl. VI. fig. 19.) {, and three other species of Pecten not yet named, besides an Avicula, and some other bivalves as yet undetermined. Of Polyparia, remains chiefly referable to the genera Retepora, Cyathophyllum, Favosites, Turbinolia, and Astrea. But the Amplexus coralloides is not of uncommon occurrence. The Re- tepora membranacea (Phil., P]. I. fig. 1 to 6) is also common, spread in wide sheets through the rock. Of Crinoidea, the remains which have principally occurred to me belong to portions of vertebral columns, which appear referable to— § Actinocrinites moniliformis, A. triaconta-dactylus, Cyathocrinites tuberculatus, and Platyeri- nites laevis. (See Miller’s Crinoidea. ) Some of the preceding organic exuvie I have noticed also in the quarries adjacent to Castle Island, associated with others not remarked on the line of the Maine, e. g. Orthoceras striatum, Nautilus ovatus ; Euomphalus catillus ; Melania constricta ; Producta Martini, P. punctata ; Spi- rifera imbricata (Tereb., Sow. T. 334. fig. 3, 4.) }, S. lineata (Tereb., Sow. T. 334. fig. 1, 2.) f, S. striata, S. obtusa, S. attenuata ; Terebratula hastata (Sow. T. 446. fig. 2, 3.) c.f, T. pugnus, T. pleurodon ; Plewrorhynchus elongatus, Pleurotomaria carinata? (Phil., Pl. XV. fig. 1. Helix, Sow. T. 10.) }, and an Orbicula? Amplecxus coralloides, Favosites, and Retepora; and also a frag- ment of the abdomen of a Trilobite. Several of these remains I have observed likewise in the carbo- niferous limestone adjacent to Newcastle, on the north-eastern side of the South Munster coal tract. In further illustration of this subject, I here add a list of the species remarked by Mr. S. Wright in the carboniferous limestone, with which he has favoured me, mostly determined by Mr. Sowerby. Locality. Nautilus biangulatus, (Sow. T. 458. fig. 2.){.... Buttevant, and Glen of Ballybeg, in the county of Cork. ' Nachtrage zur Petrefactenkunde. Mr. Weaver on the Geological Relations of the South of Ireland. 45 Locality. Nautilus sulcatus? ......00+eeeeseeeseeeeeee Buttevant, and Glen of Ballybeg, in the county of Cork. N. a large species undetermined .......... Castle Connell, co. of Limerick. Bellerophon, a large species undetermined ...... County of Clare, north of Limerick city. Euomphalus pentangulatus, (Sow. T. 45. fig. 1, 2.) { Castle Connell. E. catillus, (Sow. T. 45. figs. 3,4.)f{...... ditto. Ampullaria nobilis, (Sow. T. 522. fig. 1.) {...... ditto. A. helicoides, (Sow. T. 522. fig. 2.) c.}..... Buttevant. Producta hemispherica, (Sow. T. 328.) ti ...... ditto. Spirifera bisulcata, (Sow. T. 494. fig. 1, 2.)}.... ditto. si glabra, (Sow. T. 269. fiz. 1.) scsaccese Vy ee Gail + * S. obtusa, (Sow. T. 269. fig. 2.) .......6. Sroblata, (Sow: Ts 268.) fe fwd esis csctaate ditto. S. lineata, (Terebratula, Sow. T. 334. fig. 1, 2.) t ditto. S. imbricata, (Tereb. Sow. T. 334. fig. 3, 4.) t ditto, S. trigonalis, (Sow. T. 265.) c.f ......+--.- Clonmell. S. attenuata, (Sow. T. 493.) Tt .....eseee ditto. § Terebratula affinis, (Sow. T. 324. fig. 3.)...... iE prisea, (Schlot. T. 17. fig. 2:)ccc0cecies hag paerent T. sacculus, (Sow. T. 446. fig. 1.) tf ...... Castle Connell. ma ouenus, (Sow... 49%.) T Live aagn conto ditto. i. niplicata, (Sow. 1. 437. fig. 2,8.) 2.000. ditto. T. indentata (Sow. T. 445. fig. 2.)$.......0. ditto. Pleurorhynchus hibernicus .....ccccsccoccsee ditto. Cyathophyllum and Tubipora ........ sla doveste ditto. I learn also from Lieut. Weller and Capt. Sheppard, of the R.A., that they have found the following organic remains in the carboniferous limestone of the county of Clare, namely, north of the Shannon, at the distance of three and five miles respectively from the city of Limerick: _Trilobites, Orthoceratites, Pleurorhynchus hibernicus, Spiriferee, Productee, Euomphalus, and Re- tepora, with several species of Crinoidea, the Ampullaria helicoides, and a Natica; and in the lime- stone south of the Shannon, near Limerick, also a few specimens of univalve shells. Of the Trilo- bites, the post-abdominal portions of six individuals only were met with, which belong to two spe- cies; one of which appears to be new or undescribed, and the other to bear some affinity to the Trilobite figured by Martin under the name of Entomolithus oniscites, in tab. 45 *, fig. 1.! Coal Formation. (58.) The South Munster coal tract occupies a large area, computed to contain nearly one thousand square miles ; yet the seams of coal which have been met with, are comparatively few in- number and importance. Nor is it likely that many exist, for the elevated position of the coal-field above the ' See Petrificata Derbiensia. 46 Mr, Weaver on the Geological Relations of the South of Ireland. adjacent limestone plains; the rivers which intersect it east, south, and west ; the. roads which traverse it in various directions; the ravines which furrow its escarpments, and the limestone knolls which protrude within its area, afford such means of observation that many valuable beds of coal could scarcely have escaped detection. In fact, the more important appear confined to a small district lying north of the river Blackwater and south-west of Kanturk. I propose, in the first place, to trace the contact of the limestone with the coal rocks around the border and in the interior, and then to give a general view of the position of the coal measures in different parts of the tract; con- cluding with further notices of their composition and structure, and of the coal mines hitherto wrought. (59.) In making the circuit of the South Munster coal tract, the carboni- ferous limestone, wherever apparent, is almost invariably found following the foot of the hills, seldom rising up a small portion of the escarpment; and when it does, the position appears to proceed from an undulation in the beds. The following observations show the corresponding dips of the limestone and the superjacent coal measures, on the western and eastern sides of this coal-field. In the West, on the Ballybunian coast (§. 55.), the ascending order of suc- cession is from limestone to shale, and from shale to sandstone. The shale first intercepts, at intervals, a solitary bed of sandstone; but in proceeding north-east sandstone gradually becomes predominant, as in the headland at Lick Castle, where these beds, with slight interposed layers of shale, dip 30° to the north-east ; and this arrangement is traceable in ravines to the hilly range of Knockanore, on the east’. In proceeding, however, further east toward Listowel, the beds, both of the limestone and the coal rocks, approach the horizontal position, e. g. in the banks of the river Feale to the east of that town, dipping there only 5° to the south-east. pping y The limestone and coal measures In the northern side of the ridge, on the south-west dip of Ardfert, and within three miles of the town .. 20° to 25° to the southward. While in the southern side of that ridge and north of Tralee they incline gently to the...... eoeces northward. North-eastward of Castle Island ,.......esseeees 30° north-eastward. East ;of; ditt0\.claisteieieisyeiriersieletwisleleiviays . horizontal or 10° to 15° eastward. South of ditto, at Dicksgrove, beyond the Brown Bleskesicie\e'e eye slets pinpecosetat fete pine ictal eats cteléipte.0.0 40° to 50° southward. * From this headland we perceive with the naked eye that the position of the coal rocks near Kilcordan lighthouse, on the opposite coast, in the county of Clare, corresponds with that of the beds under Lick Castle, dipping likewise to the north-east. Mr. Weaver on the Geological Relations of the South of Ireland: 47% The limestone and coal measures dip In the quarries extending toward Milltown on. the SOME =WEStire wplom saiepincicnceesccnaccencsdbaes 20° to 40° southward. Between the valleys of the Maine and the Guestin, : _ undulated from north to south and from horizontal to 40° and 50° _ north and south. On the East of the coal tract, and proceeding from north to south. At Parkmore and Shrewlana, north of Shanagolden.. 10° to 15° north-west. At Drumruagh, about five miles south of Newcastle 10° to 15° south-west. At Broadford, two miles west from Drumcullagbar.. S59 south-west. In the line of the Awenbeg river at Liscarol, the lime- stone forms an inlet, an arched inflection from south to north, abrupted at the surface, bounded by and supporting the coal measures on the north, west, and south, in conformable position, under angles varying from horizontal..........eeeeeeeeeee to 40° and 50° north,west, & south. In the escarpment toward Kanturk, successively.... 50°, 45°, 20° south. Garthe east: Of Kanturk 54.5 a cncjcseencasdas coves 30° south-west. North of the tongue of coal measures stretching east toward Doneraile the stratification of the limestone is not well displayed ; but the coal measures there visible form an arched curvature from north to south, abrupted at the surface, beyond which inflec- tion, proceeding toward Mallow, their general dip EGE sila bi=Maeldiopne +0 o)stm 0 sida wslaa steine oe Awe tor 20° south. (60.) Within the interior of the coal tract the carboniferous limestone ap- pears in knolls, protruding through the coal measures at Maaling, Tour and Skull, and at Carrigdulkeen. At Maaling, situated near the left bank of one of the tributaries of the river Allow, and north-east from Newmarket, the limestone rises to the surface in two places on the higher grounds, disposed in strata flatly undulated from north to south, and supporting the coal rocks in corresponding position. It is traceable to the left bank of the river, and again in the more elevated lands about two miles to the westward. At Maaling the limestone, where quarried, is continuous, and of a black colour, containing courses of nodules of lydian stone which extend about twenty feet in depth, but from which the subjacent strata are free. In the latter is a bed one foot thick, almost composed of litho- dendra. Tour Hill lies about six miles west from Maaling, and to the north-west of Newmarket, forming high ground, 1329 feet above the sea. The limestone here rises in dome-shaped strata, supporting the coal rocks, which latter con- stitute the summit of the hill in the form of a cap, as well as the external border of the limestone, all being in conformable position. The limestone 48 Mr. Weaver on the Geological Relations of the South of Ireland. strata are continuous, 2 to 33 feet thick, bluish or blackish grey, dipping to all points of the compass 25° to 30°, and containing lydian stone in beds, veins, and intermingled portions. The limestone reappears in the vale at the eastern foot of Tour Hill, and again at Skull, beyond the vale, about one mile distant, in a direction to the north of east, and in strata nearly horizontal. In these lower positions the limestone is purer, being less contaminated with siliceous matter. In the Tour limestone organic remains are sparingly found, being chiefly fragments of Crinoidea and Producta Martini, but the Sanguinolaria concentrica (Phillips) also occurs. Another outbreak of the limestone occurs at Carrigdulkeen, about ten miles to the south-east of Castle Island, and within two miles of the right bank of the river Blackwater. The deeper strata appear to be nearly horizontal, but in the higher grounds the dip is 20° to 30° to the south, and the nearest su- perjacent coal rocks dip in the same manner. This limestone is nearly in an alignment with that of the Guestin stream situated to the west. (61.) The coal rocks vary in position in different portions of the tract. On the north coast, extending toward Shanagolden and Fynes Island, they may be considered as mainly undulated from the north-east or easterly incli- nation to the south-west or westerly, both the convex and concave portions being nearly horizontal where perfect, while the ascending or descending beds rarely attain an elevation exceeding 40° or 50°. But all these beds are com- monly more or less abrupted at the surface, as well as in other portions of the tract. The undulated structure is also apparent on the line between Newcastle and Castle Island, passing through Abbeyfeale; the coal rocks dipping in the northern escarpment 40°to 20° to the south-west, and in the southern 30° to 10° to the north-east. The arrangement between Broadford and Kanturk, passing through Free- mount and Newmarket, is analogous, the prevailing undulations being from north to south, yet in some cases attaining as high an angle as 80°. In penetrating from the westward, from Castle Island to Carrigdulkeen, we find the coal measures, where in contact with the limestone at the foot of the escarpment, slightly inclining to the south-east, but in the interior becoming gradually elevated to an angle of 45°, dipping south-east, as at Scartaglen, adjoining the Brown Flesk. Beyond that river they become nearly horizon- tal, then gently undulated, and at Carrigdulkeen they correspond in position with the subjacent limestone. In crossing from the valley of the Maine to the river Guestin in Barry’s glen, the dip is first successively 40° and 60° south; it then gradually declines to Mr. Weaver on the Geological Relations of the South of Ireland. 49 the horizontal, and is afterwards 8° or 10° to the north; while further on in Barry’s glen, the southerly dip is resumed at angles between 40° and 20°. But in the range of hills lying between that glen and Killarney the inter- changeable dip is repeated, at high angles, vertical beds intervening. A similar structure is observable, in the same parallel, in the eastern portion of the tract. Thus, immediately north and west of Kanturk, the beds undu- late from north to south, their curvature seldom reaching to a high angle; but between the Brogeen stream (which joins the Allow river from the west, near to Kanturk) and the Blackwater on the south, the coal rocks are generally in a position approaching to the vertical, with dips interchangeable north and south. The southern portion of our coal-field, is thus marked by a range of nearly vertical beds, extending from the northern side of the Laune and Killarney on the west, to the banks of the river Allow on the east. On the south, this range immediately conjoins with the transition rocks, and it is remarkable that on the greater part of this line, namely, by the course of the Blackwater, the two series are found, the former on the left and the latter on the right bank of that river, both dipping to the southward, and at angles nearly correspond- ing, viz. between 75° and 45° south, which led me in the first instance, com- bined with other considerations, to conceive the formations contemporaneous; but this idea was dispelled on finding the coal measures in the western and eastern portions of the tract directly incumbent on the carboniferous lime- stone, and the latter in the west reposing, in part, on the old red sandstone. (62.) The rocks of the South Munster coal-field consist chiefly of varieties of sandstone or gritstone, and slate or shale, alternating with each other. In this series, I have not met with coarse conglomerates ; and the slaty micaceous sandstone or flagstone, which is extensively developed in the coal formation of the county of Clare (as well as in parts of that of Leinster), appears generally deficient in the tract, south of the Shannon. In the line of contact with the subjacent limestone, brown, yellow, grey, and black shales are the more common rocks. When firm and intermingled with quartzose and micaceous matter, they partly resemble some kinds of greywacke slate. The line of cleavage in the shales commonly forms a highly oblique angle with the plane of stratification; and on exposure to meteoric influ- ences, the stone generally shivers into long splinters or spicular fragments. In some of the beds may also be observed a tendency to spheroidal concretions, composed of concentric lamelle, formed of very fine-grained, micaceous gritstone cemented by ferruginous shale. Portions of the black shales are in some places employed as black chalk. The gritstones are most commonly of brownish or greyish hues, seldomer greenish, and are more or less argillaceous or siliceous, as slaty or quartzose matter prevails in the composition, being also more or less micaceous. Some of the argillaceous gritstones, when containing small scaly frag- VOL. V.—SECOND SERIES. H 50 Mr. Weaver on the Geological Relations of the South of Ireland. ments of slate interspersed, resemble some, kinds of greywacke; and the purer quartzose varieties approach, in places, to the character of granular and splintery quartz rock. The gritstones generally form hard compact rocks of fine grain, quartz with more or less mica being the principal consti- tuents, and the eementing matter forming the least proportion. (63.) The coal of Munster, as of Leinster, is wholly anthracitous. In the field under consider- ation, it is found in beds either of pure anthracite, possessing a strong lustre and a conchoidal frac- ture, and is easily frangible; or in thin slaty, tender, and flaky layers, generally associated with black carbonaceous shale. A portion of a bed of the latter, is sometimes so strongly charged with carbon, as to burn limestone very well; though in the fracture, the grain of the shale appears wholly dull and earthy; e. g. at Tullig culm pits, situated to the north of Abbey-feale. But in no part of the tract, have I seen coal so firm and solid, as that which occurs in the Leinster districts, where it is raised in blocks, hard and tenacious. In South Munster it is generally fragile, and hence brought to the surface in the form of small coal, bearing the common name of culm. The coal is also usually much contaminated with iron pyrites, though beds do occur, comparatively free from that substance, being then denominated sweet coal. (64.) With the exception of the small district on the south-west of Kanturk, the beds of coal met with throughout the tract are unimportant, their average thickness varying from less than one foot to between one and two feet, in- cluding the black shale with which the coal is partially interlaminated, and which in some places constitutes the greater portion. Coal thus interlaminated with shale, has been met with in the hills north of Killarney and Tralee, but in no case was it found worthy of pursuit. The grey shale which there accom- panies the coal, contains in some places small, isolated, elliptical nodules of clay ironstone. Culm is raised from analogous beds at Loughill, nine miles north-east of Tarbert, on the left bank of the Shannon, and also three or four miles to the north of Abbeyfeale. At Tullig the slaty culm seam, is fifteen to twenty-four inches thick, the floor being black shale, and the roof gritstone, all dipping about 30° to the south-west. In Barna or Sugar Hill, which is situated nearer to the north-eastern escarpment of the coal country, is a bed of good flaky anthracite, from nine to twelve inches thick. In a more central portion of the tract, Mr. Griffith, in the year 1833 or 1834, discovered a bed of culm, in forming the new line of road from Newmarket to Castle Island, through the Crown lands of Pobble O’Keefe. A culm bed is said to have been found likewise toward the south-western escarpment, about three miles to the north of Castle Island. Slight indications of culm have been noticed also in other portions of the tract; as in the tongue of coal rocks which extend from the west and north of Mallow toward Doneraile ; but the trials were not pro- ductive. (65.) The district which claims our chief attention, extends between seven and eight miles in an eastern and western direction, with an extreme breadth Mr. Weaver on the Geological Relations of the South of Ireland. 51 of four to five miles, and is situated south-west of Kanturk and north of the Blackwater, its eastern extremity being about one mile west of the river Allow. The northern boundary may be considered as ranging from the town- land of Garrevasogue, on the east, to that of Cullen, on the west, while the southern boundary passes through the townland of Drumshecan. The an- nexed diagram will convey a general idea of the relative position of the pro- perties through which this coal deposit is distributed. The general range of the beds is east and west. 3S North. = Cullen. e < Duargan. : Coolclough. IN Kill or Coal Pits Clonbannin, or Garrevasogu ~ 2 Clumbane. Dromenagh. G Buc: > . ortine. 5 Cooleen. Coolbeg. Ea ak of Bciwaiahae Dromagh. _ Dysart. oghill, West. : Gutrane. East. Keale. Blackwater Drumshecan. —_ River. South, On the west the townlands of Cullen, Duargan, and Kil belong to Coun- sellor N. P. Leader, as also on the east those of Cooleen, Dromagh, Dysart, Coolbeg, Gortine, and Garrevasogue. To Major Freeman belong Clonbannin and Island of Doghill; to Mr. John Leader, Keale ; to Mr. Broderick, Drum- shecan ; to Mr. Wallis, Gurrane ; to Mr. Dennis O’Callaghan, Drumskeha ; to Mr. Morrison, Dromenagh ; and to Mr. Walcot, Coolclough. The more valuable portion of the district appears to be that which ranges from Gortine on the east, through Dromagh, into Drumskeha on the west, being that in which the main, or bulk beds, as they are termed, are particu- larly found. In the other collieries the culm seams are, with few exceptions from twelve to eighteen inches only in thickness, and I have been informed most of the parties engaged in working these small seams, have derived little advantage, while others have lost by the enterprise. The field has been chiefly opened, in the eastern quarter, by three levels, one of which is con- ducted into Coolclough, from the south to the north, about eight hundred yards in length, cutting the coal at the depth of forty yards, which there consists of three seams, all dipping south, the two northern at a high angle, the southern at one rather lower. The distance between the northern and middie seam, is twenty-seven yards, and between the latter and the southern, sixty yards. In all three the floor or seat is gritstone, and the roof shale, and the coal is commonly two to three feet thick, but in some places compressed to eighteen inches, and in others enlarged to fifteen feet. H 2 52 Mr. Weaver on the Geological Relations of the South of Ireland. Another level was brought up from south to north, namely, from the vicinity of the Blackwater into the western part of Dromagh, being about one mile in length. The beds thus cut through, show repeated interchanges of dip from south to north, with vertical strata intervening between each change of dip, the coal seams conforming to this arrangement, as illustrated in Section No. 6. Piate I. ‘This section was constructed for the service of Mr. Leader by Mr. Griffith, and for a copy of it, I am indebted to the former gentleman. On the south, the beds dip about 45° to the southward, but in proceeding northward, they gradually become vertical, then incline northward, are again vertical, and afterwards the southerly dip is resumed. This succession is re- peated in the more northern part of the section. It will be seen, that in the line of this level, eighteen small seams of culm were intersected before the four main or bulk beds, and the four other seams north of them, were met with. It will also be observed, that in the northern part of the section, the flexure of one coal bed is perfect in its changeable dip from south to north ; from which consideration, and the general structure of the country, it might be inferred, that many of the coal beds may converge in depth, thus reducing considerably the actual number of the seams. It must be left to future expe- rience, however, to determine, whether these beds are generally continuous in depth. I observed in one part of the field a thin bed of black shale dipping 80° north, which in its ascent thinned out, and did not reach the surface ; and a similar discontinuance might occur to a bed in its descent. The bulk beds of culm extend in width from two or three feet, to ten, fifteen, and twenty feet, according as the walls are expanded or contracted ; but the bulks occur only at intervals, there being intervening distances void of culm, in which the walls of the bed are drawn nearly close together. These bulks, therefore, are arranged somewhat in the form of parallel pipes, descend- ing into the earth ; and yet in this descent, they are subject to contractions also. This level has been extended to the eastward on the main beds, namely, those called the bulk, the rock, and the coal veins, about two miles in length, obtaining at the eastern extremity a depth of forty yards below the surface. ‘The workings on coal are conducted above that level, and it is only in a few places, that trials on the coal have been made forty yards deeper, Mr. Leader leaving all below that level, as a reserve for a future period, when, with the aid of deeper shafts and of steam engines, his collieries may be wrought on a more extended scale. Faults occasionally traverse the coal-field, ranging north and south, shifting the beds to the north three or four yards, and in some places as much as four- teen or fifteen yards. Of the greater dislocations, three or four parallel ones occur in Dromagh and Gortine. In the Dromagh section, it may be seen, that in the great majority of instances, Mr. Weaver on the Geological Relations of the South of Ireland. 53 the floor of the coal is black shale, and the roof slate-clay or sandy slate ; but there are a few cases in which the floor is slate-clay or sandy slate, and the roof is either black shale or gritstone. A third level was brought up, also from the south, into Dromenagh, about seven hundred yards in length, cutting the coal at the depth of thirty yards from the surface. Here are four coal seams, each about one foot thick, composed of conchoidal anthracite, the intervening coal measures being respectively sixty to seventy yards thick, and all dipping about 60° to the south. The floor of all these seams is black shale, and the roof gritstone. The beds of coal wrought in Clonbannin and Kil, are said to be the western extension of those of Drome- nagh. 'To the north of Dromenagh, approaching the Brogeen river, the grit- stone dips 80° to the south. In the Island of Doghill the floor of the coal also is black shale, and the roof gritstone, and the dip south. In Gurrane the coal seam is one to two feet thick, the floor being gritstone, and the roof black shale two feet thick, over which lie grey sandy slate three feet, gritstone two feet; then slate again, &c., all dipping 70° to the south. In the shale of this district may occasionally be observed small nodules, and even thin discontinuous layers of clay ironstone ; but the ore does not appear to be at all abundantly distributed, either in this or any cther portion of the South Munster coal tract. The preceding notices may suffice to convey an idea of the general structure of this field, in which no excavations have hitherto been made to a'greater depth than eighty yards from the swr- face. (66.) Theconsiderable quantities of iron pyrites which sometimes accompany the coal, are in places impressed with plants, and the coal itself seems, in a great measure, composed of a congeries of vegetables. ‘The impressions occur also both in the dark and light-coloured shales, and in the clay-ironstone. The vegetable remains to be obtained from the refuse of the coal-pits, appear chiefly assignable to Equiseta, Calamites, Filices, Lepidodendra, Stigmarie, and Si- gillariz, besides numerous impressions of indistinct reed-like plants and grasses. Compressed stems of Stigmariz ten or twelve yards in length sometimes occur in the black shale, also partially flattened trunks of Calamites. Of the latter, ‘I have a fragment, measuring in the transverse section, eleven inches by eight inches; but the colliers assured me, they were sometimes found as large as eighteen inches by twelve inches. In the Stigmarie, Sigillarie, and Cala- mites, the external coating consists of coaly matter, while the interior is fine- grained gritstone. 54 Mr. Weaver on the Geological Relations of the South of Ireland. In Jooking over, with Professor Phillips, such specimens as [ was able to pro- cure and bring away with me, the most distinct appeared referable to Two species appa- } by Sternberg, (Flora der Vormelt); Ad. Brongniart, (Vézé- Pecopteris. rently undescri- | taux Fossiles); or Lindley and Hutton, (Fossil Flora of bed Great Britain.) Lepidodendron erosum. Lindley and Hutton, PI. 7. fig. 1. Impressions of Lepidodendra and their leaves. Asterophyllites longifolia. Lindley and Hutton, PI. 18. Stigmaria ficoides. Ibid., Pl. 31 to 36. Sigillaria, apparently undescribed. Bechera grandis? PI. 19. fig. 1. Lindley and Hutton. Sphenophyllum Schlotheimii. Pl. 27. Ditto. The colliers stated also, that in a few places shells have been found in the shale, but that, from their perishable nature, they soon wasted away on expo- sure to the atmosphere. 'Twosuch bedsare indicated in the Dromagh section, (Plate. I. fig. 6.) under the name of “ muscle slate.” I had not, however, the good fortune to find any of these shells, as few pits were at work during my different visits to this district. But in the black shale of Ardnagragh, si- tuated about three miles east of Castle Island, and near to the subjacent limestone, I found impressions of small indistinct bivalves, and of convoluted shells, the latter resembling in form small Goniatites*, together with some impressions of plants. This shale is partly employed as black chalk. . (67.) The anthracitous coal of the Kanturk district, is so ill adapted to culinary purposes, that English or Welsh bituminous coal, is consumed in preference, even so near as in the town of Mal- low. The native coal is employed chiefly in burning limestone to provide manure for land, and especially in the reclaiming of waste land, in which application it has rendered most important ser- vice to the agricultural interests of the neighbourhood. But as upon these demands, which fluc- tuate according to circumstances, the supply of the coal necessarily depends, so the quantity annually raised, has varied considerably. During the last war, when a great impulse was given to agriculture, the quantity disposed of from the Dromagh collieries alone, which are the principal, amounted to as much as 25,000 tons per annum. The culm sells at the pit mouth, according to its quality, at an average from ten to fifteen shillings per ton. The collieries of this district are chiefly wrought during the summer months, when labourers can be best spared from agriculture, and the works are least heavily watered. (68.) A large portion of the South Munster coal tract, is covered with peaty soil ; but it may be remarked, that wherever limestone is adjacent, and a facility of intercourse is secured by the construction of good lines of road, the conver- sion of waste land into productive soil is progressive * Bearing some affinity perhaps to the Goniatites sphericus or G. striatus, discovered by Sir Philip de Malpas Grey Egerton, Bart., and Viscount Cole, in the carboniferous shale of the county of Fermanagh. (Geological Proceedings, No. 32. 12th June, 1833.) Mr. Weaver on the Geological Relations of the South of Ireland. 55 11. Carsonirerous Series 1n Nortu Munster. In Clare, and extending into Galway. Old Red Sandstone. (69.) This formation, in the district under consideration, is quite analogous in composition, structure, and position, to that observed by me in other quar- ters of Ireland. Its chief mass extends from Derrybryan mountain, on the north, to Lough Derg on the south-east ; but from near Lake Youlky on the west, it is continued to the south and east in a narrow belt, encircling the clayslate mountains, and reposing, wherever the contact is observable, in un- conformable position ; in the higher grounds, in nearly horizontal strata, but on the flanks declining according to the declivity. This may be conveniently observed in the hills lying north of Limerick ; and at six miles from the city on the road leading both to Broadford and Killaloe, where the sandstone rests in horizontal strata on the vertical edges of clayslate (the latter ranging east and west), but nearer the vale, the former rock dips toward the south, under angles of 25° and 20°, and the succeeding limestone is in cor- responding position, yet in receding, approaches to an horizontal arrange- ment. ‘These relations are also observable in the strata extending to the west past Croghanambrydy mountain. To the north, Derrybryan moun- tain, consisting wholly of this formation, exhibits horizontal beds in the higher lands, but inclined on the flanks. Thus, in proceeding west toward Gort, the sandstone strata are inclined 30° and 25° westward, and the succeeding limestone, where first apparent, is in conformable position, but more west it gradually becomes horizontal. In Derrybryan mountain may be found all the common varieties incident to the old red sandstone, including beds of red, in- durated clay, and sandstone conglomerate. The latter rock appears occasion- ally in considerable force, containing, in places, rounded and angular ingre- dients as darge as turkey’s eggs; and from its mottled aspect, resembles strongly the sandstone conglomerate north of Waterford bridge, and of the Drumdowney quarries adjoining the Barrow and the Suire*. Carboniferous Limestone. (70.) The general tendency of this formation to a nearly perfect, horizontal arrangement, as extending from the county of Galway into and through that of Clare, is remarkable, the deflections from that position being only inci- dental and seldom important. Undulations on a very large scale occur, yet rarely varying more than a few degrees from the horizon. The chief lines of elevation are adjacent to the old red sandstone. This disposition is well de- * Geological Transactions, First Series, vol. 5; Memoir on the East of Ireland, §. 149. 56 Mr. Weaver on the Geological Relations of the South of Ireland. veloped, in passing from the western declivity of Derrybryan mountain through Gort (§. 69), across the plains to the limestone hills on the west, which there form the bounding line between Galway and Clare. Near Kilmacduagh Abbey and Rockfield, a few miles west of Gort, are broad sheets of bare limestone rock, extending repeatedly over many acres, and separated from each other, only by small green patches of herbage or pools of water. The eye thus ranges over large fields of naked rock in nearly hori- zontal strata, but fissured at the surface into quadrangular masses. This desolate scene is continued to the limestone hills on the west, where the same horizontal arrangement prevails, as may be noticed in their escarp- ments, which being in many places divested of all vegetation, the eye traces with facility the corresponding strata from hill to hill. In the projecting and partially isolated hills, this disposition is very striking, as in those adjacent to Glancolmkill, where terraces of horizontal strata, receding one above another, present the stair-like form, so characteristic of many trap districts. The Clare limestone is distinguished by the general continuity of its strata. The organic re- mains which have incidentally appeared to me, correspond generally with those derived from other portions of our field. Ihave already adverted (§. 57.) to the fossils noticed adjacent to the Shannon by Messrs. Weller, Sheppard, and Wright ; and I shall merely add, that in the limestone of the peninsula of Renville, on the south side of the bay of Galway, I met with two species of Pen- tremites, which appear to be undescribed. Coal Formation. (71.) This formation in Clare, as in other parts of Ireland, forms hills of greater or less magnitude, planted upon the carboniferous limestone in con- formable position ; the latter being at the foot of, or rising only a certain di- stance up, the escarpment on its northern and eastern sides. Viewed on the large scale, the entire coal-field may be described as a nearly uniform plane, corresponding to that of the subjacent limestone, the angle of inclination seldom deviating more than a few degrees from the horizon, and the prevailing dip being from the east of north to the west of south. The highest portion of this area is the district of Mount Callan, which rising some hundred feet above the general level of that part of the coal coun- try which is situated further north, is still more elevated above the southern portion of the tract; the surface of the latter gradually declining in that di- rection nearly to the level of the sea. In the higher grounds, however, as well as in the southern, or lower parts of the field, the coal measures may be oc- casionally observed, disposed in a gently undulated form. The general arrangement thus described, may be traced along the eastern Mr. Weaver on the Geological Relations of the South of Ireland. 57 and northern flanks of the coal-field, as well as in the interior; but still more clearly in the mural precipices of the western coast, the natural sections of which, gradually decline in elevation in proceeding from north to south. (72.) At the northern extremity, at Doolan and the village of Roadford, the limestone is at the foot of the escarpment, and the calcareous base with the superimposed coal measures, may be seen in juxtaposition. The lime- stone appears also on the beach, and forms the low point of Ballylaline. To the south of the place, where the two formations are seen in conjunction, we look along a range of cliffs facing the Atlantic as far as Luagh Point; and if we afterwards proceed to Ballyelaw Point, still more south, we obtain, in reverse position, a view to the north, extending also to Luagh Point ; thus comprising in these two views, the whole of that part of the coast, a range of seven or eight miles in extent. The cliffs are nearly mural throughout, varying generally in elevation perhaps from 200 to 300 feet. In the first and lowest part of the coal measures, displayed in these cliffs, the shales predo- minate, in which clay ironstone occasionally appears, and also gritstone in thin, subordinate beds; but higher up in the series the gritstones acquire greater magnitude and strength. In no part of this portion of the coast, has any coal been discovered ; but excellent flagstones might he raised from the slaty, micaceous gritstone, to any extent and of the largest dimensions. (73.) On the other hand, if from Ballyelaw Point, or from Liscanon asy- lum harbour, situated on the east, we cross Malbay to the opposite coast, on the south-east, we find coal in the cliff at Raneen, about five miles from Ennistymond. This is the lowest coal hitherto met with in the whole tract. It is aseam of flaky, tender anthracite, much contaminated with iron pyrites, and averaging about eighteen inches in thickness, the roof being shale, and the floor gritstone flag. It has been wrought to a very trifling extent only, for the purpose of burning limestone, brought from the south islands of Arran ; and the furthest drift inland, does not exceed fifty yards in length. ‘The mine is situated about twenty feet above high water-mark, but the seam may be traced on its line of dip along the foot of the cliff to the south, until it sinks below the level of the sea. Above this seam is a second, perhaps 80 or 100 yards higher in the series; it does not, however, appear in the face of the cliffs, which, upon this part of the coast, scarcely attain 200 feet in height. The second seam, which does not exceed eight or nine inches in thickness, consists of solid anthracite, good “sweet” coal, the roof being shale, and the floor fire-clay, having beneath it gritstone flag. This coal was discovered about forty years ago by some Kilkenny colliers; it has been worked to a small extent only. VOL. V.—SECOND SERIES. I 58 Mr. Weaver on the Geological Relations of the South of Ireland. (74.) Hence along the coast to the southward, no coal has been found, until we reach the vicinity of Seafield, situated about fourteen miles from Ennistymond, and nine miles from Raneen. Culm has been met with on the townland of Cahirush, about one mile north of Seafield, and it is said to be twelve inches thick, but it has not been worked: and culm was formerly raised on the townland of Clahaininch, distant two miles south-west from Sea- field. Pits were there sunk through the sand hillocks of the coast to the culm, which however was only six or seven inches thick, and of bad quality. No coal has been discovered further south than this spot. My own observations have not extended along this coast beyond the parallel of Kilrush, but Iam assured by different authorities, that the coal measures occupy the whole in- terval to Loop Head, though coal itself be wanting in that part of the series. On the south coast of this tract, viz. at Labasheda on the right bank of the Shannon, culm has been also worked on a small scale and only to a slight depth, the pits being soon troubled with water. (75.) The general view which I have given of the North Munster coal-field, would appear to exhibit no very favourable prospect of its productive power. To the instances of coal having been met with, I have, however, to add the fact that in times of heavy rains, coal has been washed down the ravines on the northern side of Mount Callan (in which direction the coal measures crop out), and in particular on the townland of Sileshawn, part of that of Ballylea, and at a place known by the name of Morrison’s Mill. From the paucity of coal appearing on this line of coast, in which the general flatness of the coal measures is so well displayed, it would seem that the lower part of the series contains very little coal. Hence, the best chance of discovery appears to lie in the more elevated region of the Mount Callan district, in which the coal measures are accumulated in greater mass; and as they there apparently retain their small deviation from the horizontal position, an opportunity might perhaps be afforded, should valuable seams of coal be laid open, of working the whole of that portion of the coal tract level free, a circumstance of material importance to the operative miner, as well as to the proprietor of the soil*. * This advantage is enjoyed to a considerable extent, in the vast expanse of the coal tracts of the United States of North America. In my route from the Gulf of Mexico up the Mississippi and Ohio rivers to Pittsburgh, and thence overland to Lake Erie and through the State of New York in the year 1834, I was very forcibly struck by the nearly perfect horizontality of the strata throughout; from the first visible rocks of carboniferous limestone and their occasional associates of shale and sandstone, adjacent to the Mississippi and Ohio rivers, to the continuous coal-bearing measures, which come in force near the influx of the Great Kanawha into the latter river, extend- ing thence westward into the state of Ohio, and northward through the Virginia, Pennsylvania, and New York States to lake Erie; the prevailing deviation from that position being a slight inclina- tion to the southward, subject, however, to gentle undulations upon a large scale. The carboniferous series of the United States, admits of a close comparison with that of the British Isles; and the following view may serve to show their agreement. This view I give as Mr. Weaver on the Geological Relations of the South of Ireland. 59 These views may prove useful, whenever the exploring of this hitherto untrodden region shall be undertaken in a systematic and economical manner ; a period, however, which might perhaps appear far distant, if we looked merely to a supply of fuel for local consumption, since the vast tract of peat-bog covering the greater part of the coal-field, and extending from Mount Callan to Loop Head, is provided with a store of that useful combustible which seems almost inexhaustible. the general result of the observations which I had an opportunity of making during my travels through those States, compared with the great body of valuable information which has been con- tributed on this subject by other observers; especially in Professor Silliman’s American Journal of Science, the works of Professor Eaton, the distinct publications of our countrymen Messrs. G. W. Featherstonhaugh and R. C. Taylor, and the Transactions of the Geological Society of Penn- sylvania'. In the State of New York, the carboniferous limestone reposes partly on old red sandstone, partly on transition rocks. At the northern extremity, the old red sandstone which lines the south coast of Lake Ontario, from the west of the Niagara to the east of the Oswego river, distinctly underlies the limestone-shale, and limestone from Queenstown, by the gorge of the river Niagara upward to within two hundred yards of the ferry below the Falls of Niagara, having a gentle dip throughout to the southward. The same relative position is observable west of Lockport, in proceeding east from Lewistown by the line of road leading to Rochester; also in the Genesee river north of the latter town, and in the course of the Oswego river. ‘To the east of the Oswego, the old red sand- stone reposes on transition rocks, and, being deflected to the south-east, on approaching the Helderberg mountains, it appears to be overlapped and concealed by the carboniferous limestone, the latter then coming in contact with the transition rocks on the east, which range from Canada to the southward: while still more south, in Pennsylvania, the coal measures appear to overlap the carboniferous limestone on the east, and to come also in direct contact with the transition rocks. In tracing, from north to south, the order of succession, from the carboniferous limestone to the superincumbent coal measures, the same low angle of inclination to the south is observable from Niagara in the direction of Buffalo, and thence along part of the south-east coast of Lake Erie. The same disposition is likewise to be remarked, in passing south by the lakes of Cayuga, Seneca, &c., whose waters find a common outlet on the north by the river Oswego. South of those lakes, the land rises rapidly by an accumulation of coal measures, forming the northern aspect of the Alleghany mountains, and the southerly dip is still observable. These beds form an alternating series, distinguished by the prevalence of red shales and red sandstones with beds of sandstone conglomerate and limestone interposed, but in which coal has hitherto been rarely met with; while in the higher regions this series supports and includes the abundant deposits of coal which occur on the northern confines of Pennsylvania, in the anthracitous coal-field of Carbondale and ' See in particular— In the American Journal of Science: Z. Cist, in vol. iv. J. Pierce, in vols. vi. and xii. Pro- fessor Silliman and D. Thomas, in vols. xviii. and xix. A Naturalist in Ohio, in vol. xxv. Dr. Hildreth in vol. xxix. (from 1822 to 1835.) Professor Eaton, Geological Text-book, 2nd edition (1832), and in the American Journal of Science, vol. xix. (1831), and vol. xxiii. (1833). Mr. G. W. Featherstonhaugh, Geological Report made to both Houses of Congress, (1835.) Mr. R. C. Taylor, in Loudon’s Magazine of Natural History, (Oct. 1835). In the first volume of the Transactions of the Geological Society of Pennsylvania (1835): Mr. R. C. Taylor, three papers, pp. 177, 204, 275; Professor Troost, four papers, pp. 224, 232, 244, 248; Dr. Harlan, two papers, pp. 256, 260; Mr. E. Miller, p. 251; and Mr, T. Conrad, p. 267. 12 60 Mr. Weaver on the Geological Relations of the South of Ireland. Metalliferous Relations of the Carboniferous Series. (76.) In the Old Red Sandstone—The only spot in which I have met with metal in any material quantity in this rock in Ireland, is in the northern face Lackawanna and Wyoming, on the Susquehanna, and the bituminous coal-fields of Bradford, Tioga, Lycoming, and Clearfield. The main body of carboniferous limestone, which thus underlies the series just noticed, extends from Lake Erie in an easterly direction through the State of New York to the Helderberg moun- tain, situated about 20 miles S.W. of Albany. Here its course is inflected to the south and south- west, and from the Helderberg mountain it has been traced 120 miles upon that line, extending into Pennsylvania on the right bank of the Delaware river, and flanked throughout on the east by transition rocks'. It thus supports the bituminous coal measure series of the Alleghany and Catskill mountains on the north and the east, and incloses and supports on the east also the anthra- citous deposits of Carbondale, Lackawanna, and Wyoming, as above stated®. The southern border of the carboniferous limestone, intersects in its range, the lakes Seneca and Cayuga, and near the heads of those lakes, on the south, thin layers of bituminous coal have been found in the coal measures ; and again further east in Otsego county, in the shale lying above the limestone’. In like manner, narrow seams of bituminous coal have been met with in the Catskill range bordering on the river Schoharrie ; and again in the southern part of the same range in Ulster county, varying from eight to twenty-two inches in thickness, the beds being here in some places horizontal, but in general slightly inclined to the westward*. To what extent other seams of coal may occur in the higher accumulation of these coal measures, subjacent to the great anthracitous and bituminous deposits of Pennsylvania above noticed, remains yet to be proved®. In the Alleghany ranges, and thence to the west in particular, in the conterminous regions of Prof. Eaton, Geol. Text Book, pp. 66, 67, 2nd edition. ® Ibid., pp. 90, 121, 124. Ibid., pp. 79, 110, 121. 1 3 4 American Journal of Science vol. vi. p. 94 to 96. 5 It may be useful to consider, in this place, the distribution of the Trilobite family in the State of New York, in reference to the transition and carboniferous systems respectively. In the Transition series are found, Localities. Calymene Blumenbachii ............... At Watertown near Sackett’s Harbour; Glenn’s Falls; Trenton Falls. RPCIEMIE CERNE Tinie io% 0'0)4.0.0 09 0 0''s.0. 010 05 New York State. KS, TOACTOPEUNAINA sce ces ccc came scene Ulster County. MD AGUOMEGCEEAIA Ts sjo\e's'e\s's 15% NGO \ ae Fi, Pe citadel. a... Granite \Peaghan’ fi = Anock-laye Hill } 4 WES \ \ } } jes] Trap - i 4 jushl wale Brish-adhu Hee | Lorphyry Pra, | trap - Cushendn Sy SZ Cushendun Bav 3 oo q » mt Vinegar , Bally Knock 7. A ; “aa /, shendall R. palleask R. f CUSHENDALL BAY Corkey y f Mountains > —— ltabuliadh JCorlane IBAS Teavemuitle™ Trostan THO 69 11.—On the Geological Structure of the North-eastern Part of the County of Antrim. By JAMES BRYCE, Jun., M.A., F.GS., (MEMBER OF THE GEOLOGICAL SOCIETY OF DUBLIN, AND OF THE NATURAL HISTORY SOCIETY OF BELFAST.) [Read May 2, 1832. | (1.) THE Third Volume of the First Series of the Society’s Transac- tions, contains a Memoir by Dr. Berger on the Geological Features of the North-eastern Counties of Ireland. It is preceded by an Introduction from the pen of Mr. Conybeare, and is followed by a Supplement, the joint production of that gentleman and Dr. Buckland. The views of the structure of the country given by these authors are, gene- rally speaking, correct ; in many of the details, however, there are errors con- cerning those portions whose structure is anomalous or complex, and are such as strangers might be expected to fall into, who took a rapid survey of the district. Having had opportunities, from my local situation, of ex- amining the North of Ireland leisurely and repeatedly, it was easy for me to become acquainted with the details of its structure ; I propose, therefore, to lay before the Society, in the following brief memoir, the result of my ob- servations. As the remarks will be entirely supplementary, it is unnecessary to repeat anything contained in the memoirs referred to. My attention was first called to the peculiarities of this district by Dr. Mac Donnell of Belfast, to whom, previous writers on the North of Ireland, have been largely indebted, and to whom I am anxious to acknowledge my obli- gations. (2.) The district I propose to describe, is the north-east corner of Antrim, between Kenbane Head on the north-west, and Garron Point on the south- east ; being about eleven Irish miles long, with an average breadth of ten miles. It is traversed in a north-west direction by the Aura Mountains, a portion of the great chain which runs parallel to the sea-coast through the whole length of the county, and in this part of its course contains several mountains, varying from one thousand to nearly two thousand feet in height. The principal are, Trostan 1810, Sleiveanee 1782, Knocklayd 1685, Sleive an Orra 1676, and 70 Mr. Bryce on the Geological Structure of Ben-cruachan about 1500. From the main body of the chain project, in the southern part of the district, several long ridges, with flat, broad summits and precipitous sides. They reach almost to the sea-shore, and are separated by deep and narrow gilens, which extend far into the interior ; the principal being Glenariff, Glenaan, and Glendun. Through these glens flow rivers of the same name; the waters of which are scanty in summer, but in winter are swelled by many tributaries, from the upland bogs ; and tumbling over the cliffs, excavate deep and wide channels, which present to the geologist perfect sections of the strata. In the northern part of the district, or that which has Glendun for its southern boundary, the surface of the country is occupied, at intervals, by considerable hills, which are detached from the main chain and from one another, but have a northerly direction, parallel to the principal chain. Those which deserve mention are Glenmackeeran, 1321 feet; Ballypatrick and Brishadhu, about 1100; and Carnanmore and Carnlea, 1250 each. They are of an elongated, narrow form, and in general slope gradually; but the eastern sides of those next the sea, shelve down to the shore in abrupt and rugged terraces. The direction of these hills determines that of the valleys and river courses. The valleys have a north and south direction, and open into a principal one running east and west to the south of the elevated ridge which forms the coast from Fair Head to Ballycastle. The rivers flowing through these valleys turn westward, and pour their united waters into the sea at Ballycastle. On the western part of the district, the principal chain of mountain descends, in a succession of undulating hills, into the low country, which extends at their base from Corkey by Armoy to Ballycastle. (3.) The following are the principal formations which occur in the district : mica slate, old red sandstone, porphyry, carboniferous limestone, coal with its accompanying strata, new red sandstone and conglomerate, lias, mulatto, chalk, and trap. Granite, primitive limestone, and porphyry occur as subordinate rocks. Mica Slate. (4.) This formation in the north-east of Antrim, does not vary from its ordi- nary character in the North of Ireland, as described by Dr. Berger. It occa- sionally passes into gneiss, and by the insulation of the crystals of felspar assumes a porphyritic aspect. It contains crystals of quartz and, rarely, of common schorl, also amorphous quartz, accompanied by chlorite. Mica slate occupies the greater part of the area under consideration. Its boundary in the south- eastern part of the district is a line ranging, in an irregular north-east direction, from the eastern the North-eastern Part of the County of Antrim. 71 ‘point of Teavemuile, a mountain forming the highest part of the ridge which bounds Ballyeemin Glen on the north, across the head of the glen in which Cushendall is situated ; and along the north- west declivity of Cross-slieve, to the mouth of Glendun river'. From this point it occupies the coast as far as Murlogh Bay. From the base of Tibuliadh near Teavemuile it ranges north-west, conforming in its direction to the eastern escarpments of the Aura Mountains, and constituting their inferior regions ; sweeping round the northern front of Bencruachan, which terminates the chain, it turns southwards and composes the lower part of all the mountains as far as Corkey, the whole of the low country which extends from Corkey by Loughguile and Armoy to Ballycastle, and the half of Knocklayd, in which it rises to the height of 800 feet. From Ballycastle its line of junction with the secondary strata trends eastward up the valley of the Carey, and with the stream of which its boundary nearly coincides, then turns northward until it finally dips under a narrow band of secondary rocks to the south-east of Fairhead, and is thus connected with its north-eastern ter- mination in Murlogh Bay. Over all this area the general dip of the strata is south-east at a high angle; but there are frequent irregularities in the dip and inclination, and the strata are often much contorted. (5.) Other primary rocks occur abundantly, subordinate to the mica slate. Primary limestone is found at Torr Point, and on the declivities of Knocklayd, and in the townland of Ballynagard, near Ballycastle. Beds of felspar, por- phyry, hornblende rock, and hornblende slate occur in several places. These have all been described by Dr. Berger. Granite is found near the village of Ardsillach on the road from Cushendun to Torr. It occurs in the face of a hill called Deaghan, which overhangs the road; the bed is conformable to the mica slate ; it is several yards wide, and is probably connected with a subja- cent body of the same rock. It is composed of red felspar, which is the pre- dominating ingredient, of minute portions of vitreous quartz, and of small cry- stals of brown mica. Old Red Sandstone. This rock has little of the conglomerate structure ; being most commonly a coarse-grained whitish sandstone, with a little admixture of argillaceous and calcareous matter. It contains some fragments of other rocks, but in very small proportion to the mass. The fragments are water-worn masses of resinous quartz, varying in mag- nitude from the smallest particle to the size of a man’s head ; also several va- rieties of porphyry, many of them the same as those of Kilnadore and the Knockans, afterwards to be described ; but many of them have no resem- blance to those porphyries, subordinate to the mica slate, or to any other por- phyry known by me zm sztw in the North of Ireland. Some of the imbedded masses are the same as the base itself, showing either that parts of the rock have been derived from preexisting portions being worn 1 See after Article 7. ¥2 Mr. Bryce on the Geological Structure of down and afterwards recomposed ; or that a preexisting rock of very similar structure has been entirely worn away in supplying materials for this great mechanical deposit. I have observed no pebbles of granite or mica slate. The largest of the fragments are identical with the base itself, while those of quartz are by far the most numerous. In most of the strata the fragments are few: they are rare in those adjoining the mica slate, while they occur in greater quantity and variety in those in contact with the newer conglomerate. Many of the strata, however, include no fragments, and in others they are col- lected into distinct groups in different parts of the same stratum, the remaining portion being quite free from them. The rock, moreover, often loses its coarse- grained gritty structure, and assumes a fine-grained sandy texture, like a grey freestone ; but by far the greater part possesses the appearance and structure formerly described. A sandstone occurs under low-water mark, in advance of the cliffs near the collieries at Bonnycastle. It is overlaid by the carboni- ferous limestone, and must therefore be the old red sandstone. (7.) This rock extends from Cushendun to the head of Ballyeemin glen, occupying the greater part of Cross-slieve, the upper portion of the glen in which Cushendall is situated, the lower part of the southern side and the greater portion of the bottom of Ballyeemin glen, also the whole southern declivity and half the table-land of the summit of the ridge which forms the northern side of that glen; the rest of the summit and the whole northern front being composed of mica slate, which seems to constitute the greater part of the ridge, as the covering of sandstone is very thin along the southern side. In the eastern face of this ridge, in the town-land of Tavnagharry, the mica slate protrudes from beneath the sandstone and occupies a small gulf-shaped area, sur- rounded by the sandstone on all sides except the north, where it is joined by a narrow neck, or isthmus, to the great body of the same rock. The Ballyeemin river crosses the southern part of this area; and the mica slate is seen in the bed of the river, overlaid, on the left bank, by the sand- stone. In the bed and banks of the same river, near the head of the glen, two isolated patches of mica slate are met with, separated from one another by beds of sandstone of small extent, and are probably portions of the rock elevated above the general level, and from which the sandstone, having nearly thinned out in this part, has been worn away. The intervening beds of sandstone seem to occupy a trough or basin between these two projecting peaks or spires of mica slate. The newer conglomerate, which will be immediately described, and which here contains enormous masses of mica slate, reposes immediately on the mica slate forming the upper of these two iso- lated portions, the old red sandstone being most probably overlapped, or having thinned out. (8.) Over all the area occupied by the old red sandstone, the strata dip uni- formly to the east. The angle of inclination, however, varies, being generally about 40°, and rarely less than 25°. Near the mica slate it is high and con- formable to that rock, while at points remote from the schist it is less. the North-eastern Part of the County of Antrim. 73 Porphyry. There are several varieties of this rock. The most common is a clay por- phyry, of red, grey, brown, reddish grey, and bluish red colours, irregularly intermixed in every possible manner. It contains crystals of glassy felspar, vitreous quartz, and calcareous spar, and small crystals of brown mica!. The crystals often disappear, and the rock passes into a claystone, or into an argillaceous sandstone, closely resembling the base of the finer varieties of the old red sandstone. Another variety is a clinkstone porphyry, of a bluish or greenish colour, which seems to pass, in some instances, into a close-grained greenstone. The area occupied by the porphyry is an irregular triangle, extending from Cushendall on the north to a little beyond the Knockans on the sauth-west: its eastern boundary being the sea between the mouths of the Cushendall and Balleask rivers. Within these limits the porphyry is continuous, and does not crop out in independent masses, as stated by Dr. Berger ®. The strata of old red sandstone which are interposed on its western bound- ary between the mica slate and the porpbyry, preserving their usually high inclination, dip uniformly eastwards, so as to pass under the porphyry. The summit of Court McMartin, a hill immediately adjoining Cushendall, is com- posed of porphyry, but the old red sandstone appears in its lower part. The isolated hill Teavaragh, behind Cushendall church, has also a base of old red sandstone. Strata of clinkstone porphyry crop out in its middle, while its summit is composed of a disintegrating green-stone. Further, the newer conglomerate on the shore covers the porphyry. It would appear from these facts, that the porphyry overlies the old red sandstone, through which it has been most probably erupted, and that it is covered by the new conglomerate. Few’ junctions being visible, there is little opportunity of observing altera- tions such as igneous rocks usually produce upon the sedimentary deposits ; two instances, however, occur. At the mouth of the Cushendall river the strata of the newer conglomerate are tilted by the porphyry from their usually low inclination to a nearly vertical position ; but, as the contact of the two rocks is concealed, it cannot be determined whether any change of structure is in- duced upon the conglomerate. At the base of Teavaragh the old red sand- stone is considerably indurated by the contact of the clinkstone porphyry which overlies it. ' Masses of jasper also occur. * See Dr. Berger’s Paper, Geol. Trans., 1st Series, vol. iii, p. 201. ’ The following paragraph was added by the author, in April, 1836. VOL. V.—SECOND SERIES, L 74 Mr. Bryce on the Geological Structure of (10.) Mr. Conybeare noticed a bed of clay porphyry on the west side of Fairhead, under the level of the coal formation ; it is probably contained in the old red sandstone mentioned as occurring there. If so, the analogy be- tween its position and that of the Cushendall porphyry is striking and illustra- tive. The rock in both localities would thus be contained in the old red sandstone, and the new conglomerate which covers the porphyry at Cushen- dall overlies the coal formation in Murlogh Bay. (See after, art. 16.) Other points, near Cushendun, at which porphyry occurs, are noticed in the map. Carboniferous Limestone. (11.) This rock is fully described by Dr. Berger. It appears on the shore near the Collieries, under the coal-field ; but is of very small extent, and does not occur in any other part of the district. Coal Formation. (12.) The coal measures exhibit the usual alternations of coal, sandstone, slate clay, and bituminous shale. To the accounts of it by various authors, I shall add only a few observations on its superficial extent. It has been stated, (p. 72) that the formation reposes at its northern ex- tremity upon the carboniferous limestone, underlaid by old red sandstone ; on its southern boundary it rests immediately on mica slate!. The sea is the northern boundary of the coal-field from Ballycastle on the west to the south-east corner of Murlogh Bay on the east ; its southern boundary almost coincides with the Carey river from Ballycastle to the townland of Drumnakeel, where that river turns westward into the valley before mentioned. * Here its boundary turns north-east and passing through Drumadoon, ranges by the trap of Fairhead ; and then extends eastward in a narrow zone between the trap and the mica slate, and, passing afterwards under the chalk, finally expands into a deposit of considerable importance in Murlogh Bay. The coal strata thus emerge on all sides from beneath the basaltic mass of Fair Head, which is by this means isolated. The usual alternations of sand-stone with slate clay and bituminous shale appear in many places; but are exhibited beautifully in a section on the banks of the Carey river. (13.) In Murlogh Bay the beds are precisely similar to those in other parts of the field. A sandstone cementing small quartz pebbles occupies the shore, and is well seen near the great dyke. Mr. Conybeare thinks it identical with ' See particularly the very valuable ‘‘ Geological and Mining Survey of the Antrim Coal Di- strict,” by Richard Griffiths, Esq.; in which an accurate account is given of the various beds of this formation. the North-eastern Part of the County of Antrim. 15 the Cushendall conglomerate. It is undoubtedly much older, as I shall pre- sently show. The same rock, though less gritty in structure, extends to a considerable elevation in the bay, and alternates with beds of slate clay, and a dark blue, bituminous shale, as in the cliffs west of Fairhead. There also adits were made into the sandstone, and a considerable quantity of coal was obtained, but the workings are now abandoned. Fairhead reposes upon the coal formation. At the south-western termi- nation of the area, near Maghera and Cairnlogher, in the county of Derry, a small coal formation occurs, resting upon carboniferous limestone and old red sandstone on the one side, and upon mica slate on the other, thus afford- ing a complete analogy with the Ballycastle district. New Red Sandstone and Conglomerate. (14.) The conglomerate of this formation has been fully described by Dr. Berger and Mr. Conybeare. In addition to the fragments observed by them, I noticed a few small round pieces of red granite, which would seem to have been derived from the beds of that rock, subordinate to the mica slate. This conglomerate passes (apparently) into old red sandstone on the one hand, and into red marl on the other. It lines the coast from Cushendun Bay to the commencement of the porphyry, at the mouth of Cushendall river, and ex- tends a short distance from the shore into Cross-slieve. At Cushendall caves, the red sandstone alternates with the conglomerate ; but is so free from fragments, that it is quarried in considerable quantity and shipped for Belfast. The cement of the conglomerate also often passes from its ordinary coarse, reddish, and highly quartzose state into a finer and white sandstone, indicating a passage from the one rock into the other. Jn- deed so close is the connexion in mineral structure, that it seems almost im- possible to draw a precise line between them. On the shore near Port Vinegar, the masses of porphyry imbedded in the conglomerate, are more numerous than ai any other place, and are all identical with the adjoining rock; and as almost every variety is found in rolled and angular pieces, a great part of the conglomerate at this point, has been pro- duced, apparently by the wearing down of the porphyry. At the southern termination of the porphyry the conglomerate is resumed, and extends to the mouth of Glenariff river. A change there takes place in the base of the conglomerate,—it first passes into a coarse red sand, containing the usual fragments ; then into a fine stratified red sand, in which the frag- ments are loosely imbedded, adhering neither to the base nor to one another. These fragments gradually diminish in size and in quantity, until they ulti- L2 76 Mr. Bryce on the Geological Structure of mately disappear and the rock becomes a fine marl. Thus the conglomerate, with its enormous, imbedded masses, graduates so imperceptibly into a fine red sandstone, that it is altogether impossible to separate them in nature. The strata of the conglomerate on the shore, have an inclination conform- able to the old red sandstone on which they repose; but near Red Bay castle, where the conglomerate graduates into red marl, its strata gradually pass from their usually inclined to a horizontal position, which the red marl afterwards preserves. The strata of the conglomerate are also horizontal along the front and north side of Lurgeidan mountain; and they are never found inclined in the in- terior. The conglomerate does not extend further south than the opening of Glen- ariff-glen. It rises to a considerable height on the eastern front of Lurgeidan Mountain, and stretches in a narrow zone around its northern base to the head of Ballyeemin-glen ; but the whole stratum soon after thins entirely out in the eastern face of Teavemuile, in the upper part of Corlane. Its pre- vailing character in the first part of its course is that of a siliceo-argillaceous base of a reddish grey colour, including numerous round and angular frag- ments of various sizes of quartz and mica slate, with smaller of red granite. Here also it rests in nearly horizontal strata upon the edges of the highly inclined beds of mica slate and old red sandstone, and when near the mica slate its base is often very micaceous. (15.) The red marl occupies the bottom and sides of Glenariff to a con- siderable height; and its uppermost strata, next the mulatto or green sand, are highly argillaceous, but never contain gypsum. That substance does not appear until after turning the point of Garron, where it is found in the ar- gillaceous marl, subordinate to the sandstone. White and blue clay-galls also, are not unfrequent in the red sandstone of Glenariff. From Glenariff the red marl ranges round the front of Lurgeidan Mountain, overlying the conglomerate, but in a narrower zone, and turning westward along: its northern side, runs out in the townland of Cuilags, a considerable distance east of the termination of the conglomerate. The same gradation between these two deposits, which I have described in Red Bay, is everywhere ob- servable. In Mullach-fin-ooar, between Ardsillach and Torr, a patch of red conglomerate is interposed between the mica slate and the chalk; it includes loosely imbedded fragments of mica slate and quartz, and is very like the conglomerate of the caves in Red Bay. It extends along the south-east face of the hill fronting the sea. (16.) he red sandstone and its conglomerate are fully developed in Mur- the North-eastern Part of the County of Antrim. TE logh Bay, and present the same structure and the same gradations which have been already described (14, 15). The conglomerate covers the coal sand- stone, and is identical with the less coarse varieties of the Cushendall con- glomerate, particularly those of the cliffs in Red Bay, the fragments being: as usual quartz and mica slate of various sizes, imbedded in a coarse sandstone of a reddish colour. Both the conglomerate and red sandstone terminate abruptly against the mica slate in the southern corner of the bay. On the northern side, the conglomerate extends under the greenstone of Fairhead, the red sand having previously thinned out. To what distance it ranges in this direction it is impossible to determine, the strata are so completely hidden by subsidences; but it is possible that it soon terminates, since it appears from sections exposed in other places, that the Fairhead greenstone reposes upon the coal sandstone itself. (17.) Jt has been thought that the trap and sandstone alternate here. I could detect no such alternation; and the mistake arose from “ viewing the conglomerate in relation to some subsided masses of greenstone,” been well remarked by Mr. Conybeare. (18.) It may be questioned whether the rock which I have called new con- glomerate, should be separated from the old red sandstone. The facts surely warrant such a separation ; and it may be well to recapitulate them. In our old red sandstone granite or mica slate pebbles never occur, while both are as has found, the latter most abundantly, in the conglomerate. The conglomerate covers the mica slate and old red sandstone unconformably. The porphyry overlies the old red sandstone, but is covered by the conglomerate : besides, in Red Bay and Murlogh Bay, there is a clear gradation from the congio- merate into the new red sandstone. (19.) This whole series of mechanical deposits with the intrusive rocks, 1s analogous, in many respects, to the conglomerate and accompanying rocks which occur in South Devon, the theory of whose origin is so well given by Mr. De la Beche in his Geological Manual (pp. 400, 405. 2nd edit.).* Laas. (20.) Upon turning the Point of Garron and advancing towards the opening * In Dr. Berger’s Map, the greater part of our district is coloured as composed of new red sandstone, whereas that formation is of very trifling extent, the mica slate occupying by far the greater portion of the area. In the notes to the coast sections, similar mistakes continually occur. Tea-bulioah and several other mountains are said to “ exhibit basalt, chalk, and red sand,” while not a particle of red sand is to be met with beyond the limits described. This will appear sufficiently from the details already given. (1836.) 78 Mr. Bryce on the Geological Structure of of Glenariff-glen, the lias which extends almost without interruption from Larne, again appears from beneath masses of fallen rocks, which strew the whole space between the shore and the cliffs: the only stratum visible is the slate clay ; no limestone having been detected. The thickness of the deposit is here greater than on any other part of the coast, except at the little deer park of Glenarm ; but it cannot be accurately determined. The slate clay is well seen on the road-side, a little west of Cloch-a-stukan ; and the soft sub- stratum having given way, the road has sunk considerably. It terminates before entering Glenariff, the mulatto from this point resting on the sand- stone, until near Ballintoy at the extreme north-western corner of the district, where the lias reappears. Mulatto or Green Sand. (21.) Dr. Berger noticed, that the upper beds of this rock are of a homo- geneous sandstone, while the lower frequently include quartz pebbles, and thus assume the conglomerate structure. ‘These two varieties are constant in their character and relative position, from the Point of Garron to the eastern flank of Lurgeidan Mountain ; where the sandstone thins out, and the mulatto for the remainder of its range is a conglomerate. Under this form it con- tinues its course between the chalk and the newer red conglomerate as far as the eastern part of Teabuliadh, where it ultimately disappears, extending some distance beyond the termination of the red conglomerate, and thus reposing on the mica slate. From the point where the mulatto sandstone ends, the mulatto conglomerate begins to contain fragments of mica slate in addition to the quartz pebbles, which alone had entered into its composition before ; and they become much more numerous from the point where it begins to repose upon the new red conglomerate. It never contains the red granite found in the conglomerate ; but fragments of a white carbonate of lime, like an indurated chalk, are not unfrequent. It is difficult to say whence this limestone was derived. The existence of beds of mulatto near Armoy, on the western edge of the district, seems indicated by loose masses strewing the surface ; but as no section is exposed, the mulatto, on this part of the map, is marked as doubtful. Where the stratum is fully developed, in the first part of its course, its thickness varies from six to ten feet, the conglomerate bed forming about one third of the whole. In the latter part of its range, where the brecciated bed alone occurs, the thickness varies from nine inches to three feet. the North-eastern Part of the County of Antrim. 79 In Farous-glen, on the south side of Glenariff, in the bed of a river which exposes a vertical section, the red sandstone is succeeded by a bed of blue argillaceous marl two or three feet thick, similar to that, which, in most places, forms the upper member of the sandstone series. On this marl the mulatto conglomerate rests, and is interstratified with a few thin seams of the ar- gillaceous marl. That part of the marl which is interstratified with the mulatto, and the overlying portion to the thickness of six inches, contain very few pebbles; while the superior portion includes them in great numbers. In the north-east face of Lurgeidan Mountain, veins of mulatto, not exceeding two inches in thickness, pass irregularly to the depth of from five to fourteen inches through the upper beds of the new red sandstone, which are here a fine red sand. ‘The sandstone between the seams is charged with calcareous grains ; and the regular stratum of mulatto conglomerate, which is here about one foot thick, is arenaceous in its lower part. ‘This may be regarded as a rudimentary formation of the lower greensand, which attains a full develop- ment in other places, beyond the limits of our district. Both these instances of interstratification, are unexampled among the upper secondary deposits of the North of Ireland. A brecciated mulatto inclosing quartz pebbles only, and about three feet thick, underlies the chalk in Murlogh Bay, terminating against the mica slate in the south-western corner of the bay. Chalk. (22.) The chalk having ranged round the sides and across the lands of all the glens from the Point of Garron to Teabuliadh, continues its course in a north-west direction, along the eastern declivity of the principal chain, then turning round the northern front of Bencruachan, takes a southerly direction along the western escarpment as far as Corkey. Here, after a short sweep to the west, it turns again northward, and continues in that direction by Ballyknock, Armoy, and Balleeny, to Ballycastle, where turning again westward, it forms the coast by Kenbane and Ballintoy towards the Causeway. In the interior of the country, the chalk con- stitutes part of the four isolated hills, Knocklayd, Ballypatrick, Carnanmore, and Mullach-fin- ooar, all ranging in a north and south direction, and lying in the same parallel of latitude. In the three former it is covered by a thick cap of trap; but in the latter it is uncovered. It is also uncovered by trap in the northern part of Carnanmore, and extends thence in a zone of considerable breadth through Coolnagoppoge and Ballynean, to the cliffs above Murlogh, where it abuts abruptly against the greenstone of the Fairhead. This zone presents the greatest surface of chalk uncovered by trap in the North of Ireland ; and it is here only that the peculiar vegetation of the chalk is exhibited. The soil is a light dry mould, covered by an intensely green turf, which is bespangled with myriads of daisies. (23.) We have seen, that the upper beds of new red sandstone in Glenariff pass into an argillaceous marl, which, however, does not contain any veins of . ch a Na * . - « : es | - e 4e a 7 > . ; maby ia > ra . d —_ , a ; « , . iy » #4 ay : z A ‘i 7 a” 1 ; é c a , ae aX Py ad gs ie by Alar Rare ba ; ie il ‘iti “a “ ai - caidurly a : . asta? Ai, *. pe Se oo eae ae oe A en , F ee ’ SS a car iia yea eel Bee Yaad dn selon oh ieee me ue ¥ Py he aaa i POULSIART BT, eine, 4 > ; - in, wo » . . \ a em é rs a : | a a g i q ‘Z ‘ 3 ; “ ; 1 é 4 Csr i Sra n 7 ) , ro ay: f was : a iy flay — > Py: rap i? i ee abe no Ay 1 ae ee | 7 > : > | a A “awl ai whyere Be Ae: . i ; i " a mh me ‘ane nh, mi pipe on: a eo ane |e qe ane ene aby b : ne eae ae % z. " ae ay a qi asa _ {hh to eae Biss ar noe re — p iy » 1 . a eal Trans 2 Servis, Val V Ft 4 Prnbed by CHallenonséel: SQUALORAIA. (p- 63) Ss pantie rend eee on : a Yl MT a Aas eh Spies Hoe Dae eK Vee oy ays Fa hn HOE. OC Nchovf abhog [ 83 } III. —On the Squaloraa. ~ ‘ By H. RILEY, M.D. Communicated by Cuarzes Stokes, Esq., F.G.S. [Read May 15, 1833.] Tuis interesting animal, of which Plate IV. is an accurate representation *, was discovered in the lias of Lyme Regis in 1831 by Miss Anning, associated with the Saurian and other remains, for which that place has become so cele- brated. It was purchased by John Naish Sanders, Esq., and deposited by him at the Bristol Institution, where it now constitutes a part of that valuable and improving collection. The form of this animal is so striking and peculiar, that the majority of ob- servers have disagreed not only as to its genus, but even as to its class: for by the generality it has been pronounced a Saurian, and by a few even a bird. Those who advocate the former of these opinions, are led to do so from the form of its parietal bone and its elongated jaws. The latter character was likewise the reason for supposing it to be a bird. But the absence of alveoli and teeth, and of respiratory openings ; the form and number of the vertebra ; the form of the thoracic and pelvic regions, with their attached members, render the former opinion but little probable. The other supposition is so at variance with all the anatomical details of the fossil, that we shall not trouble our readers with its discussion. For our own part, we cannot avoid concluding that it is a cartilaginous fish, having many points of resemblance to some of the Rays, but differing from them in several important characters. The entire length from the end of the lower jaw to the fractured extremity of the tail is 175 inches. The greatest length of the head, 73 inches. Breadth across the orbits, 34 inches. Length of the remains of the vertebral column, 10 inchest. Extreme width, 5} inches. * Copied by permission of M. Agassiz from Plate XLII., vol. 3. of Les Recherches sur les Poissons fossiles. + Nearly the whole of the remainder of the tail has been subsequently found, and measures * rather more than ten inches, including about 240 vertebrae; and is in the possession of Miss Philpott. M 2 84 Dr. H. Ritey on the Squaloraia. The animal is imbedded in the lias with its belly downwards ; whilst, there- fore, we have an excellent view of the whole of its superior surface, we have no means of observing its inferior or abdominal. It has, however, on the most superficial inspection, a strong resemblance to the flat cartilaginous fishes ; and this is not confined to the form alone, for there are distributed all over its surface an immense number of ‘spines with radiated bases, (Plate IV. Fig. 1—3.) the remains of its dermoid apparatus. They are best seen around the head, and on each side of the terminal pieces of the head. These spines are identical with those of the Rays. . In studying the head (Plate IV.) we can distinctly observe at its posterior face or boundary, two processes projecting backwards, flattened laterally, and bounding the occipital hole ; being evidently the remains of occipital con- dyles. Allowing for the process of flattening, the forms of this region are not unlike those of the Rays. Superiorly, and on the median line corresponding to the occiput, the bone or cartilage has been greatly defaced ; but the parts between the orbits are in excellent preservation. They are much depressed on the median line, but rise in elevation as their lateral portions form the internal boundaries of the orbits. This space in form and position, and indeed in all its characters, has a very close resemblance to the same region in the Rays. In them the cartilage corresponding to this space, becomes a mere membrane, and is termed the “ fontanelle.”’ The depression and flattening in our specimen might have depended on the same modification *. | In front of the “ fontanelle” are two terminal prolongations. The superior has been fractured at its posterior extremity, and thrust backwards as far as the anterior edge of the orbits. It has likewise been broken in two other places near the middle. It is elongated, conical, flattened posteriorly and superiorly, but becomes more rounded towards its anterior extremity. Firmly attached to its superior surface, are many of the small spines already noticed. In its displacement it has been moved obliquely back- wards, so that we are unable to observe the superior surface of the inferior prolongation. This prolongation is likewise elongated and conical; its length was pro- bably greater than the preceding, for its anterior extremity is broken and * This appearance of the interorbital region, has led the majority of observers to consider the animal in question a Saurian: we trust, however, the arguments we have advanced are sufficient to show the contrary to be the case. Dr. H. Riney on the Squaloraia. 85 has been lost. The superior surface instead of being convex like the former has a very wide and superficial groove, the boundaries of which are the edges on ‘each side, elevated into a corresponding ridge. These ridges are higher and wider posteriorly than anteriorly. The form of these terminal cartilages in the Rhinobatis is, in their essen- tials, like that of our specimen. In studying the lateral regions of the head, and proceeding from behind forwards, we find the parts posterior to the orbits much injured ; portions, however, of bone or cartilage may be seen on the posterior edge of the left orbit, extending downwards and forwards, so as to constitute its lateral and external boundary. From the position, form, and direction of these frag- ments, supposing the fish to be a cartilaginous one, we think they are probably the remains of the os quadratum. 'The orbits themselves are of large size, and well defined, particularly the left. In front of the orbits is, on each side, a large elliptical mass. In form and position it resembles those swellings of the cartilage which in the Plagiostomes, and the Skates in particular, con- * stitute the seat of the organs of olfaction. These olfactive cavities are much compressed vertically *. These spaces have on both sides a number of pieces or parts more or less _ connected with them; but having evidently undergone great mutilation, their determination becomes a matter of some difficulty. We cannot trace any connexion between them and the anterior extremities of the thoracic members, which in many cartilaginous fishes are prolonged as far as this point. Are they feelers? or, are they bones or cartilages extending from the upper to the lower jaw ? * Since the above memoir was written, this country has been honoured by the presence of Dr. Agassiz of Neuchatel, and gladly did we avail ourselves of the opportunity, during a transient visit he made to the city of Bristol, of laying before him our very interesting fossil: we now with much pleasure acknowledge that to his keen observation and perfect acquaintance with the science of Ichthyology, we are indebted for some determinations which had escaped us. On removing with his penknife some fragments of shale, he discovered several minute teeth along the line separating the elliptical masses or olfactive cavities from each orbit: therefore these portions must be considered as the olfactive cavities pressed closely against the maxillary bones; and in the line of their contact, and consequently along the anterior edge of the orbit, would be situated the teeth attached to the superior maxillary bone having its usual position. A reference to these parts in the common Skate will render this very evident. The overlooking this circumstance in our determination of these parts, and the rectifying of our error by Dr. Agassiz, lead us to withdraw the specific name of Dolicognathus as being no longer applicable : we hope ere long to have the pleasure of seeing Professor Agassiz’s views regarding this very curious fish, registered in his Poissons Fossiles. 86 Dr. H. Ritey on the Squaloraia. The anterior piece on the right side, is evidently continuous with the cranium ; the middle one on the left presents the appearance of a joint: but we do not recollect to have seen jointed feelers. In the common Skate are two small bones in this position, and in the Squalus Squatina, the only specimen of a Squale in our possession, are three large bones or pieces extending from the upper to the lower jaw, and placed considerably anterior to the temporo- maxillary articulation. 'T'wo of these pieces are articulated with the upper jaw at one end, and by the other with the third piece, which extends itself to the lower jaw. Although these analogies are very imperfect, we cannot help thinking that if more extensive means of comparison were in our possession, we should find that they belonged to the latter category. Behind the cranium in the cervical region, are several detached elongated pieces, which we are inclined to. consider as remains of the branchial appa- ratus ; on the left behind the orbit, is a portion lying at right angles with the vertebral column, another is parallel, a third is to be seen to the right. What remains of the vertebral column, is less injured than the other parts. The processes of the vertebre have disappeared, leaving the bodies which are circular very perfect. They are concave anteriorly as well as posteriorly, as may be seen at the places where they have been fractured. This column, or the cycleal elements of it are cylindrical, its transverse diameter seems rather to increase towards the posterior extremity. The vertebra are extremely numerous, and are injured in a few places, which prevents our counting them very accurately. There are about 260 in the whole, of which 28 are cervical, counting as far back as the middle of the transverse piece, corresponding to the scapular region; 143 dorsal, counting to the middle of the pelvis; and the remainder, 90, belong to what remains of the tail. Their transverse diameter is six times more than their antero-posterior diameter. In the Rays the cervical portion is consolidated inferiorly into one entire piece,—in the Squales it consists of distinct vertebrz ; indeed the analogies of form in this column with that of the Squales, are much closer than with any other genus with which we are acquainted; for in the Squales, as in the common Shark for instance, the cycleal elements of the vertebre or the bodies are quite round. In them the vertebral canal can hardly be said to be formed at the expense of the bodies, which present a very superficial groove only, at their superior surfaces for the reception of the spinal marrow, the canal being principally made up by the epial elements, in other words, by the plates and spinous processes, which in many of this genus are very easily detached. This canal is more deeply grooved in the bodies of the vertebre of the Rays, whilst the plate and spinous processes are in general wider and stronger, and more firmly attached. Dr. H. Rizey on the Squaloraia. 87 On casting the eye along the upper surface of the column of the fossil, it is easy to recognise traces of the spinal canal in the form of a very superficial groove ; which is more evident in the posterior than in the anterior half. From the above details we should be inclined to consider this animal as having a column resembling that of the Squales. The thoracic and pelvic members are next to be considered. They are greatly injured, hardly an entire piece remaining, and it is evident that with the view of rendering the form of these parts more clear and decided, great liberties have been taken with the specimen. The scapule have disappeared, but we can make out the remains of pieces corresponding to a sternum and pelvis. We can likewise recognise the radiated form of the thorditic and pelvic members, and can easily trace the anterior member backwards as far as the pelvis, circumscribing an oval space, with the vertebral column running through its centre. This space would correspond to the seat of the alimentary canal and organs of generation. It is dotted with an immense number of small spines, of the same form with those so often alluded to, but seems to have suffered from the measures resorted to for an advantageous display of the vertebral column. Those parts, which in the fossil put on the appearance of radii, belonging to the thoracic member, are distinct from each other, but do not present any traces of joints, a character in which they differ greatly from the Rays, whose radii are jointed. The spaces between these radii have been apparently cut into grooves by a knife, which has injured them. The forms and arrangement of the pelvic radii are by no means dissimilar from those of the Rays. There are no signs of the powerful claspers to be found in the males of this family. We are not able, for want of a greater number of skeletons, to determine the original form of the transverse piece in the region of the scapule. The portion which must have passed over the vertebra, corresponding to the scapulz, has been destroyed, whilst the part which is to be seen lying under them remains, but has been greatly mutilated. This portion in the Rays would correspond to that transverse cartilage, which connects the thoracic members with each other under the bodies of the vertebre. By its position and flattened form, increasing in width at each extremity, it resembles the piece occupying the same position in the Rays, and would correspond to the sternum. But the form ot this region in the fossil differs from that of the same region 88 Dr. H. Ritey on the Squaloraia. in the Rays, since in the latter the vertebrz are consolidated into a single piece, and are continuous with, and firmly united to, the two pieces of car- tilage or scapule meeting on the median line above them. The right side of the pelvis is less injured than the left, and resembles that of several of the more common species of the Rays. From these details we trust it will be clear, that the specimen must have belonged to the cartilaginous fishes; that it has many points of resemblance with the Squales, but still more with the Rays ; but that it differs from both of these families by its peculiarly elongated head. So far as our own limited means of observation and comparison will allow, we cannot ‘help thinking that it will be considered a new genus by those who make Ichthyology a distinct study ; and as its generic characters would ' be founded on parts belonging to the Squales and the Rays, we shall venture to propose the name of Squatorasa. Mingen L* ia abrado, ) ) ea a ptaas ; SMP ‘ irene er en nen ne epee eR RE | | Ie z | CSthonf Ui ang Trnteadiiey C Exillmam. Natwel Columns of Lanestore on the Last Stale of Neapwscalstand one of the Mingan stands Peer} IV.—Notes on the Geology of the North Coast of the St. Lawrence. By Caper, BAYFIELD, R.N. F.R.A:S. Communicated by G. B. Greenoven, Esq. P.G.S. [Read Nov. 20th, 1833.] 1. ON presenting a suite of specimens to the Geological Society from a long line of coast, which is scarcely more known in Canada than in Europe, being seldom visited except by fur traders and fishermen, I hope a few remarks upon the structure of the country, will not be deemed devoid of interest, though my official duties did not allow of a minute investigation. The district between Quebec and the river Saguenay, particularly about Murray Bay, has been examined by Dr. Bigsby. The late William Green, Esq. has most ably described the vicinity of Montmorency* ; and Lieut. Baddeley of the Royal Engineers, St. Paul’s bay and the Saguenay river+ with a minuteness and ability which leave me nothing to add. I shall there- fore commence my account at the Saguenay, and proceeding eastward, de- scribe the coast of the river and Gulf of St. Lawrence.{ 2. From the Saguenay to Pointe de Monts, a distance of 130 nautical miles §, the hills forming the coast are composed, for the greater part, of varieties of syenitic granite ; and the country inland as far as the Falls of the Bersimis river, about 40 miles from the St. Lawrence, in a direction parallel, or nearly so, to the course of the Saguenay, consists of the same formation. All the valleys and basins between the granitic hills are filled with horizon- tally stratified deposits of clay, sand and gravel, sometimes 200 or 300 feet thick ; the clay being invariably next the granite, and the gravel generally on the surface. No organic remains having been found, it is difficult to assign to these deposits any relative age; but as the rivers, tributary both to the St. Lawrence and the Saguenay, have cut sections through them, future investi- * Transactions of Literary and Historical Society of Quebec, vol. i. p. 181. + Ibid. vol. i. p. 79. vol. ii. p. 76. { Plate V. fig. 1. § The distances in this memoir always mean nautical miles. { Shells of species, existing at present in the estuary of the St. Lawrence, have been found in banks of similar sand and clay, as will be noticed hereafter (p. 96.). VOL. V.—SECOND SERIES. N 6 eee me soa = ar 3S Bs Sz a srt] er one Sa ee et ENE ee PESTS 9 En on ne 90 Capt. Bayrietp’s Notes on gations may lead, by the discovery of fossils, to their true history and relative age. I am, however, averse from applying to them the term diluvial, because the regularity of their stratification would seem to be due to a cause less violent and longer continued, than is consistent with our ideas of diluvial aetion. These immense deposits abound on all parts of the north coast of the St. Lawrence, which we have visited; nor are they wanting on the south coast. The soil which they supply is by no means good, but is sufficient for the growth of large pines, and may be not altogether unsusceptible of cultivation. These formations must not, however, be confounded with the alluvial de- posits at the mouths of the rivers, the latter being chiefly due to the currents undermining the soft banks, composed of the former. Alluvial accumulations of this description, occur extensively at Pointe Mille Vaches and Port Neuf, as well as at the entrance of the Bersimis, Outard, Manicouagan, and other rivers. The extensive Manicouagan shoals have doubtlessly been formed by the two last rivers, especially the Outard, whose course for eight or nine miles, from the falls to the sea, is through the soft strata just mentioned. On approaching Outard bay after the time of high water, the sea was of the colour of sand, and had it not been previously ascertained that there were nearly 100 fathoms of water, we should have supposed that a sand bank existed close to the surface of the sea. When the vessel sailed into the discoloured water the effect was very remarkable. She cut through and displaced the thin stratum of comparatively fresh and discoloured water, displaying the clear blue sea beneath, and left a blue line wherever she passed. The discoloured water was ascertained to be derived from the Outard river, charged with sedimentary matter ; and was so widely diffused as to cover the whole bay, and the sea for several miles. 3. The same granitic rocks, with stratified deposits in the valleys, and allu- vial formations at the entrances of the rivers, compose the coast and country, from Pointe de Monts to the Seven Islands, a distance of 60 miles. The rocks constituting the Seven Islands abound with hornblende. In the bay of the Seven Islands is a very extensive alluvial formation, ele- vated only a few feet above the present level of the sea at high water. Walking inland from the sandy beach, which extends for many miles to the eastward, I counted seven parallel sand ridges in a distance of about a mile ; evidently ancient beaches which formed, at different successive epochs, the margin of the sea. The number of these beaches and the nature of the wood which covers them, would seem to show, that those furthest inland are very ancient. On removing the thin covering of vegetable matter, I found in several of the ridges, clam shells perfectly similar to those which abound on the present shore. That the beaches were formed by the combined action of the sea and adjacent rivers, continued during an immense period of time, there can be no doubt ; and on comparing Des Barres’ plan of this bay with our survey, no appre- the Geology of the North Coast of the St. Lawrence. 91 ciable change appears to have taken place in the last 70 years. Whenever excavations have been made in the sand, sufficiently deep to reach below the level of the sea at low water, clay has been met with. In this respect, therefore, these undoubtedly alluvial formations bear a strong resem- blance to the deposits in the valleys, basins, and hollows of the granitic hills previously mentioned, and seem to differ from them principally in being much thinner, and in occupying lower levels. The sandy country continues from the Seven Islands to the river Moisic, a large stream which is fullof sand banks, and deposits extensive sandy shoals near its mouth. It is about five leagues from the Seven Islands. About three leagues further eastward, the granitic hills, which to the westward range several miles in rear of the coast, and opposite the islands attain an elevation of 1700 feet, again approach the sea, and form the coast to the Magpie river, a distance of 60 miles. 4, The unstratified rocks of this long line of coast are arranged irregularly, in round-backed hills and ridges, often studded thickly with round knolls. Their elevation above the sea seldom exceeds 1000 feet, being about the same as that of the coast westward of Pointe de Monts. There is a much greater variety in the primitive rocks in this part of the north coast, than in any other further to the westward. Besides the genuine granite, composed of quartz, felspar, and mica, and considered comparatively rare in Canada, there is a peculiar kind of glassy felspar*, not met with by us elsewhere, which forms considerable hills and the coast for many miles. Porphyry was found at the falls of the Manitou river, and I believe this is the only locality yet ob- served in, Lower Canada: it passes into syenite. Magnetic iron ore occurs abundantly in veins and beds, associated with the felspar rocks. 5. From the Magpie river to Mingan, the coast is formed of the stratified, argillaceous, and arenaceous deposits, and of the alluvion of the river St. John. The soil is poor, loose, and sandy, but covered with a dense forest of spruce, with a few birch and aspen trees. Near the river St. John, resting on the clay, is a semi-indurated sandstone in process of forming, by the percolation through the sand, of water strongly impregnated with red oxide of iron. As my remarks have arrived near the western extremity of the Mingan islands, I shall make a few observations upon the coast which has passed in such brief review. Our boats visited every part, and ascended the rivers to their falls, yet no rocks of the transition or secondary classes were observed im situ. Magnetic iron ore is largely and generally disseminated, although * T do not affirm that this is the glassy felspar of mineralogists ; but its cross fracture is highly vitreous. Its laminz are frequently striated,—a character common in the felspars of the St. Lawrence. + Most of the specimens in this section of the coast, were collected by my assistants Lieutenant Collins and Mr. Bowen. wn 2 92 Capt. Bayrretp’s Notes on we observed it in the greatest quantity in the portion of the coast which I have last described. When not seen, its existence at no great distance, was indicated by the large quantity of magnetic iron-sand on the beach, and by its effects upon the instruments, used on shore in the survey of the coast. The compass needles were frequently and powerfully disturbed all along the north coast of the St. Lawrence, not only within the limits which I have mentioned, but from Cap Tourment eastward, to the eastern extremity of the Esquimaux islands, and perhaps to the longitude of 60° west. I must not be understood as confirming the vulgar opinion, that the compasses of vessels sailing up the St. Lawrence, are affected ; on the contrary, we observed, that the needles on board the Gulnare, were visibly disturbed in one or two instances only, when the vessel was not more than a mile or a mile and a half from the shore. The strongest case was off Port Neuf, where the beach contains large quantities of magnetic iron sand, and we were not more distant than 14 miles, yet even there the disturbance did not exceed four or five degrees ; and at double the distance it became insensible. From the Magpie river to Mingan, the granitic rocks are hid by the alluvion and the superincumbent soft strata. They pierce, however, through the sand at the entrance of the Mingan river ; and afterwards appear frequently at the margin of the sea, within the Mingan and Esquimaux islands, affording op- portunities, occasionally, of observing their junction with the limestone of which those islands are formed. 6. The Mingan and Esquimaux islands, 29 in number, are situated just to the northward of the 50° of latitude, and between the 643° and 632° west lon- gitude, or nearly so. They range parallel to the coast from the Perroquets at the west, to St. Genevieve at the east end of the chain, a distance of about forty-three nautical miles. Their northern points are no where more than three and a half miles from the mainland, and are generally close to it ; while their southern or outer points, do not extend further off the main shore than six and a half or seven miles. The most extensive island is called Large Island, being about ten miles in circumference, and Esquimaux island is not much smaller. The general character of the group is low, the highest points not exceeding perhaps 300 feet above the sea. On the north, east, and west sides, are bold and frequently steep cliffs; but on the south side the outline is low and shelving. In these and other respects, the Mingan and Esquimaux islands resemble the opposite island of Anticosti, from which, at the nearest point, they are distant about 144 miles. Both the groups are entirely calcareous, and the strata dip only a few degrees to the southward, or a little to the westward of south. The limestone varies much in different parts even of the same island, being sometimes com- pact, or earthy, or shaly, at others imperfectly crystalline, and occasionally it passes into a calcareous sandstone, in which grains of the minetals compo- sing primitive rocks and fragments of shells, are agglutinated by a calcareous cement. the Geology of the North ‘Coast of the St. Lawrence. 93 | The small columnar or prismatic structure was several times observed, precisely similar to spe- cimens, which I have seen, from the limestone of Kingston in Upper Canada. At Betchewun harbour, between Hunting island and the main, we noticed parallel, semi-cylindrical groovings in the limestone, of various dimensions, and diagonal to the direction of the strata. At first we ima- gined they had been produced by the attrition of boulders drifted by running water; but further observation induced us to think, they were due to structure. There is plenty of stone fit for the common purposes of building, but we saw none adapted fur ornamental architecture. Many of the strata are very hard, and although I do not think very large blocks could be procured, yet the stone appears of excellent quality and stands the weather well. Masses of flint were found several times on the beaches, and nodules of chert are not uncommon in the limestone, particularly at Harbour island, Mingan, where the nodules are evidently derived from organic remains. I found Orthoceratites, Encrinites, &c., completely converted into chert, but with their shapes perfectly retained. In the greater number of these nodules, however, the form of the organic body had been nearly obliterated, and in many cases it was not perceptible. No metallic minerals were found in any quantity, but traces of lead, zinc, copper, and iron were observed in all the islands. In some places there are few or no organic remains, but they are generally abundant. The most common is a species of Ammonites, next Orthocera, and both were seen occasionally of very Jarge size. Encrinites and corals were also numerous, and several kinds of bivalve shells. Un- chambered univalves were very rare, as we found only four or five specimens of two kinds. Many of the fossils are similar to those in the limestones of Anticosti, Cape Gaspé, the neighbour- hood of Quebec, Kingston in Upper Canada, and the Manatoulin islands in Lake Huron, a cir- cumstance which induces me to think, that these limestones are of the same age. From the organic remains, and all the strata being carbonaceous or bituminous*, I infer also that they are analogous to the mountain limestone of England. 7. On most of the Mingan islands the limestone cliffs have been broken by the waves into columns of various shapes, frequently resembling flower pots, or arched and perforated rocks, &c. Plate V. fig. 2. It is extremely worthy of remark, that there are limestone columns and beaches of limestone shingle, or gravel, exactly similar to those now forming, high up on the islands, from thirty to sixty feet, at the lowest estimation, above the present level of the ocean at the highest tides, and far back among the trees, in rear of the present sea beach. One of two hypotheses must, I think, be adopted to account for these appearances :—either the general level of the ocean has fallen or the land has risen, If the latter supposition be the correct one, and I think it by far more probable than the former, the raising of the land cannot have been violently accomplished, for the strata are not disturbed, nor the columns thrown out of the per- pendicular ; neither can it have been done all at once, but by a succession of gentle move- ments at different epochs, acting uniformly over a great extent of country at the same time. This reasoning is founded upon the following appearances and observations :—The land carnot have been raised by one great operation, because the columns and beaches are at different levels on the same island; and because on groups of flower-pot shaped, or other columns, there are * The limestone of the Manitoulin Islands is occasionally very bituminous. I have found Orthoceratites from which, when broken, the bitumen flowed like tar. 94 Capt. Bayriezp’s Notes on marks of the sea having remained for a considerable time at different levels; to which parallel beaches of limestone shingle correspond. I imagined, at first, that the peculiar shapes of these natural columns might be the effect of at- mospherical agents, and the unequal hardness and consequent power to resist that effect, in the dif- ferent alternating strata of limestone. Observation however soon convinced me, that these agents are incapable of producing such effects. They may and do wear away the cliffs rapidly, aided by the expansive power of freezing water, in a climate whose winter temperature is so low; and if the cliff be composed of strata of a nature to be unequally acted upon, it may be undermined, or several projecting ledges may be left, and these may be divided by natural fissures, so as to cause the face of the cliff to assume a variety of shapes; but a talus is soon formed which protects it from further destruction from this cause. The action of the atmosphere alone, therefore, cannot form groups of isolated natural columns or perforated rocks, and carry away the debris or arrange it in parallel beaches of waterworn fragments, whose levels correspond with those at which the columns remain, or to the parts of those columns which appear to have been worn slender by the long continued action of the waves. But if we attend to what is going on at present on these islands, we shall have little dif- ficulty in deciphering the memorials of the past. We see columns of limestone, evidently the ruins of former cliffs, assuming the various shapes of flower-pots, towers, arches, &c., and standing on the gently shelving limestone, laid dry only at low water, and at a short distance from the per- manently dry shore. ‘They are worn away by the waves acting upon a space which depends upon the rise of the tide, until they become very thin at the mean level of the sea. It is thus that they so frequently assume the shape which has led to their being termed flower-pots. The limestone gives way to this incessant washing, in angular fragments, which, after undergoing attrition in the surf for some time, are finally deposited in beaches of shingle, upon the shelving limestone, at an ele- vation corresponding to the highest rise of the tide. Such is the process at present, and the columns, with beaches of corresponding elevation, were observed to be forming in every favourable situation. Now the columns which occupy levels far above the reach of the sea at present, are not only ex- actly similar in appearance and shape to those which are forming, but are accompanied by beaches of limestone shingle, more or Jess waterworn, and of corresponding elevation to the worn stems or shafts of the flower-pot columns. These appearances, I think, can only be explained by allowing, as before stated, either that the land has been raised, or that the level of the ocean has fallen, In either case the changes of level have been only a few feet at a time, with long intervals between, as is indicated by the wearings of the columns, which must have required a long period of years, and by the succession of the beaches one above another*. * There is one more indication which was observed by Dr. Kelly, R.N., in the harbour of Quarry island. He there found the limestone perforated by Lithophagi at a height not reached by the sea at present, excepting perhaps in very high spring tides. The harbour is so well sheltered that there is never any surf to wash this perforated ledge of limestone when the water does not otherwise rise to it. Considering all the circumstances, it is possible that the sea may attain the height of these perforations, and remain at it for an hour or two at a time, during two or three tides in a month; but it is probable that in the summer, when there are seldom gales to cause extraordinary high tides, the ledge may not be reached by the water for two or three months in succession. Lithophagi could not possibly live in such a situation, perfectly dry and heated by the sun for weeks together. We frequently found masses of limestone on the beaches perforated by Lithophagi, the shells of which remained in the cavities, but they appeared to have been washed up by the surf, and we have every reason to believe that these animals live, either constantly submerged, or in situations which are dry only for a short time during each tide. the Geology of the North Coast of the St. Lawrence. 95 That several similar elevations of the land or depressions of the sea would be necessary to account for all the appearances on the Mingan islands, may be inferred from the following. We ascended several times cliffs at the water’s edge, and on their summits, thirty feet above high tide level, we found beaches of limestone pebbles, more or less rounded and water-worn, which were continually falling down as the cliffs gave way beneath them, by the undermining of the waves or of the elements. In rear of the first beach I counted five or six others, each higher than the preceding, and all more or less covered with vegetation, and the higher ones with trees. The highest was sixty or seventy feet above the sea. Appearances exactly similar have been observed on Lake Huron, and described in a paper published in the Transactions of the Literary and Historical Society of Quebec*. Most of the flower-pots and other columns were from fifteen to thirty feet, but some exceeded forty feet in height above the plateau of rock on which they stood. They were frequently ar- ranged in lines upon a terrace of limestone, precisely as they are forming at present, at the water’s edge, out of cliffs which are washed by the waves. In those columns which have been successively worn or scooped out by the waves at different levels, it is not unworthy of remark, that the part so worn generally corresponds, in perpendicular height, to the rise of the tides at present ; thus leading to the inference, that although the level of the land or sea must have changed to produce the appearances described, yet that that change has not been sufficient to materially modify the circumstances, upon which the height of the tidal wave, in an estuary, depends. A faithful record of the powerful effect of natural agents, in the present day, will best enable us to judge of the past. It is, on this account, that I mention an instance of the partial destruction of these rocks, during an absence of ten months from the Mingan islands. In the autumn of 1831, we noticed several remarkable flower-pot columns on the east side of Mingan island, some near the water, others considerably above its level. We were familiar with their shape and appearance, having looked at them frequently through our telescopes, and used them as stations in the trigonometrical survey. Lieutenant Collins had also examined them closely. On our return, in June, 1832, we found the heads of several of these flower-pot columns broken off by an agent, traces of which still remained. An immense bank of ice and snow was on the island, in rear of the broken columns, and was not totally dissolved on the 17th of July, when we last saw it. This had doubtlessly been forced up during heavy easterly gales, and the pressure of the ice had broken off the heads of the flower-pot columns. This change of level appears to me of so much interest, that I must add a few more remarks respecting it, before I proceed with my description of the Mingan islands. In almost every part of the estuary of the St. Lawrence, we observed other appearances which we could also account for only by supposing either that the level of the sea, in the estuary and gulf, has fallen, or that the land has been elevated. In many bays and entrances of valleys near the sea, are sandy terraces at different levels, corresponding on opposite sides, and so shaped that it was impossible to resist the idea, they had once formed the margin of the ocean. I have mentioned (2. p. 89), that the rivers have cut sections through the soft strata of clay, sand, and gravel, and that the detritus which they bring down, is principally derived from these formations. I have also alluded to the resemblance between these more ancient strata and those of undoubted alluvial origin, which have been formed and are still forming at the mouths of those rivers. * Vol. i. p. 6.—1829. 96 Capt. Bayrizip’s Notes on The following additional remarks will show that resemblance in a stronger light, and have re- ference to the phenomena which I have described upon the Mingan islands. Sand and gravel are the most abundant materials brought down by the rivers, and are arranged around and off their entrance, forming low points and sand bars, which rest upon clay, at, or a few feet beneath the low-water level. Many of the rivers bring down argillaceous matter also, and this lighter material is carried further by the streams, and deposited in the comparatively still water without their entrance. But as these sandy points have extended further into the sea, they have covered the argillaceous matter previously deposited, and hence it is, that we always find clay under the sand in these alluvial formations. The streams, of course, cannot place these ma- terials above their own level or that of the sea at high water. Sand shoals, which are dry every tide, are first formed, and the action of the winds and waves does the rest. The tendency of these sands to arrange themselves in strata, was frequently observed, where small streams had cut sections through the beaches. In walking inland from the entrances of these rivers, we pass over low flat ground, composed of sand hills and sand beaches, covered first with grasses and shrubs, and further inland with trees. The immediate banks of the river are low sand cliffs, having their bases washed by the stream. Next succeeds a sandy terrace, rising abruptly twenty or thirty feet. Directly opposite, on the other side of the river, is a similar terrace, the cliffs on each side corresponding in elevation. Another flat succeeds, and frequently a second, and sometimes a third, the last being a hundred feet or more above the sea. If we attend to the sections cut by the streams through these ter_ races, we find the cliffs horizontally stratified or nearly so, the lowest stratum visible at the water’s edge or a few feet above it, being clay ; but if we ascend the river sufficiently far, we find that this lowest stratum of clay occupies a level above the present ocean, and in situations where there are no gorges of valleys, which we can imagine so closed up, as to raise the waters within to a higher level. If, therefore, these ancient terraces and soft strata are alluvial deposits, analogous in their mode of accumulation to those forming at present, then the relative levels of the land and sea have certainly changed, let the cause be what it may. Near the Falls of the Bersimis river, Mr. Bowen found the clay, under the sand, in thin strata, semi-indurated, and having a tendency to break into rhomboidal fragments :—a circumstance, which I shall have to mention again in similar formations. Among other proofs of a change in the relative levels of the land and sea in the estuary and Gulf of St. Lawrence, is the bank of semi-indurated sand and clay at Beauport, near Quebec, full of shells, of species existing in the estuary.* This bank is far above the present level of the river. We also noticed a bank, apparently an ancient beach, containing similar shells, at the en- trance of the Riviére du Loup, on the south side of the St. Lawrence, and about sixty feet above the present high water mark. It rests on the greywacke and slate rocks. Several other instances of banks of shells at high levels, on each side of the river and estuary, have been mentioned to me, but as I have not visited the localities, I merely state the circum- stance as of frequent occurrence. I believe there is much in the valley of the St. Lawrence to reward the researches of the geological traveller, who may turn his attention to these comparatively recent deposits; and I am surprised that they have not attracted the attention of those who have visited the St. Lawrence, and written on its geology. * The St. Lawrence is perfectly fresh thirty miles below Beauport, yet the species of shells in the bank mentioned, are all, or at least by far the greater number, inhabitants of salt water. The are also frequently perforated by a marine boring worm which also lives in the estuary and gulf. the Geology of the North Coast of the St. Lawrence. 97 I shall describe one more proof of a change of level, which came under my own observation, at La Petite Riviére, near St. Paul’s Bay. Between Cap Maillard and Cap de la Baie, near Quebec, the hills of gneiss, abounding in garnets and magnetic iron ore, recede so as to form an irregular crescent, the interior of which is filled with a low alluvial formation, not more than 20 feet above the rise of the highest tides. This formation consists of clay thinly covered with sand, and contains many boulders principally derived from the adjacent mountains. The clay is in thin, horizontal strata, and semi-indurated, so that it can be raised in large pieces, which are easily broken by the hand into rhomboidal slabs, from six inches to a foot in diameter. It abounds with impressions of rushes, partly filled with and stained by, brown oxide of iron, derived, by filtration, from the neighbouring hills. It con- tains also occasionally clam shells, similar to those existing in the river. Everything indicates a quiet deposition, when the waters of the river had a higher relative level than at present. On this alluvial flat, the farms of La Petite Riviére are situated. At present the St. Lawrence is fast destroying this alluvial formation, not by a rise in its waters, but by a change apparently of the direction of the tidal currents, depending perhaps upon the formation of shoals in other adjacent parts of the river. Every high tide, accompanied by a strong north-east gale, washes away large portions of the fields, so that the inhabitants are driven to seek for fertile soil among the hills. This gradual destruction has been going on for many years, as I was in- formed by a Canadian, ninety years old, who had resided there from his youth. He pointed out to me large boulders, now lying on the shoals, dry at low water, which he ploughed around thirty or forty years before. The old church of La Petite Riviere has been washed down by the waves, and the present one is likely to share the same fate, at no very distant period. The old church of Les Eboulemens which was built upon a similar formation, has been also destroyed in the same manner. The wall next the water has fallen, having been undermined by the waves, and trees now grow within the other three, their roots assisting to preserve the ruin. Such are the indications of a change of level which have come under my own observation. I must now conclude this subject with the following remarks. I cannot affirm positively that the heights of the terraces, in valleys and bays of the main land, are exactly the same as those of the ancient sea beaches of the Mingan Islands, but there appeared a very near agreement. It is certain that terraces of the same height extend over very large areas, and it appears ex- tremely probable that the same agent may have simultaneously elevated these ancient alluvial terraces, and the ancient beaches and natural columns of the islands. It is not easy to imagine any alteration in the level of the sea, within the Gulf of St. Lawrence, without an equal change in that of the Atlantic Ocean. It is to volcanic agency, therefore, we must look for the probable cause of the appearances which I have endeavoured to describe ; and the probability of this inference is manifested by the fact, that the great agent alluded to is still felt. Shocks of earthquakes are frequent at Murray Bay, Les Eboulemens, St. Paul’s Bay, and the adjacent country, of force sufficient, at times, to split walls, throw down chimneys, &c.* The earthquake of 1663 is said to have lasted six months, and to have caused land slips and other changes in the face of the country. It is to be regretted that there are no clear and detailed * For an account of the earthquake of 1791, see Lieut. Baddeley’s Notes on the Geology of St. Paul’s Bay, Transactions of the Literary and Historical Society of Quebec, vol. ii. p. 83, et seq, 1831. VOL. V.—SECOND SERIES. 9 98 Capt. Bayrrexp’s /Votes on accounts of this event; but it is sufficient for the object which I have in view, to mention the fact of its occurrence. Frequent shocks have been felt every year since, though less violent.* I must now return to the description of the Mingan Islands, from which I have digressed so greatly in pursuing a subject, which I believe, had not been before touched upon by any author on the geology of the shores of the St. Lawrence. 8. The Mingan and Esquimaux Islands have very little soil. The lime- stone, where not bare, is covered by limestone shingle or gravel, or by de- cayed vegetable matter resembling peat. Hence the islands may be con- sidered barren in an agricultural point of view. ‘The timber also is small, and principally spruce, with a few birch and Canadian poplar or aspen trees. Blue or whortleberries, cranberries, and several other wild fruits are in abundance. The stream of the tides is not very strong among these islands, seldom ex- ceeding a mile an hour, except in narrow channels, where it sometimes attains a rate of two anda half. The rise is about seven feet in ordinary spring tides, and about three feet in neap tides. 9. The mainland is composed of low granitic hills. St. John’s Mountain, some miles in rear of the entrance of the river of the same name, and 1416 feet above the sea at high water, is the loftiest point in the neighbourhood. There is land about 1000 feet high, opposite Quarry Island, ten miles east of Min- gan, but towards the east end of the chain of islands the mainland is very low, the hills being far back in the country. The granitic rocks, a few miles to the eastward of Mingan, are composed * In July, 1831, the shocks at Murray Bay were more than usually severe. The walls of the church, it is said, were split, stone ovens and chimneys were thrown down or displaced, and a rocking motion was communicated to the houses. Many of the inhabitants were so alarmed as to seek safety on board of vessels in the bay, where the shocks were also felt. This earthquake was experienced at Beauport, nearly ninety miles to the south west: how far it extended in the op- posite direction is not known, there being no inhabitants. It was also felt on the south side of the St. Lawrence, at the Riviére Oulle, and at St. Roques: how far it might have been felt to the northward of the St. Lawrence is also unknown, the country in that direction being uninhabited. An intelligent lady, who was then at Murray Bay, informed me that the shocks were always pre- ceded by a subterranean noise, resembling distant thunder, which approached from the northward, and appeared to pass under the houses. When this noise seemed immediately beneath the house, a heavy shock was felt, as if the house had received a heavy blow; this was succeeded instantly by a rocking motion of the building and undulation of the ground, producing a sensation not unlike sea-sickness. The earthquakes have been, in general, accompanied or succeeded immediately by squally weather, sudden gusts of wind, &c. Shocks were felt very frequently during the months of March and April, 1833. the Geology of the North Coast of the St. Lawrence. 99 of red felspar, quartz, and hornblende, the felspar predominating. They are succeeded to the eastward, opposite St. Genevieve Island, by true granite, consisting of red felspar, white quartz, and black mica. The connexion of the granite and limestone is well shown at several points. On the east side of Pillage Bay and Mount St. Genevieve, 332 feet above the sea, the limestone rests immediately upon the granite in nearly horizontal strata. Opposite St. Genevieve Island is a round, isolated and precipitous hill of limestone, which rests also upon genuine granite ; and other similarly shaped hills of limestone, with mural sides, but smaller and of less elevation, occur in the same vicinity, resting likewise on granite. The country for many miles inland is composed of low granite mounds, the intervening hollows being filled with stagnant water, peat, or other vegetable matter. The great irregularity of the bottom of the sea among these islands, as indicated by the sound- ing lead, strengthens the inference from analogy, that the islands rest upon granitic hills, in the same manner as the isolated hills of limestone mentioned above. Some of the rocks and shoals, under the sea, are as precipitous as the islands above it, having thirty or forty fathoms of water close to them. It does not seem difficult to imagine, in this respect as well as in others, a resem- blance in these ancient calcareous formations, to those which are forming at the present day,, on the summit of submarine hills in tropical climates. Neither limestone nor any other transition or secondary rock, was met with to the eastward of St. Genevieve. 10. The coast thence to Cape Whittle, in the longitude of 60° west, and latitude 50° 10' north, is composed of varieties of granitic rocks, in which, contrary to what has been observed of the granites of Canada, hornblende is a rare constituent. The coast is of very moderate elevation, possesses few remarkable features, and cannot be distinguished from the deck of a vessel, at a distance exceeding four or five leagues. It is broken into bays and inlets, and lined with innumerable small islands, rocks, and reefs*. The granite of the main and islands is almost everywhere covered with peat, full of stagnant ponds of dark bog-water. ‘Trees become more and more scarce as we proceed to the eastward, till at last they are almost exclusively confined to alluvial formations of sand and clay, which are of rare occurrence, and, excepting at Natashquan, of limited extent. It is not my intention to describe mineralogically the different granitic rocks which occur on this coast. Metallic minerals, with the exception of * Few places can be imagined more barren, dreary, and desolate, than this coast, or more gloomy than the climate in which itis situated. It is girded with ice, and covered with snow, from October to June, and is wrapped in dense and cold fogs for more than two thirds of the remain- der of the year: yet it teems with life in the summer season. o 2 100 Capt. BayrieLp’s Notes on iron, appear to be rare: native copper, associated with epidote, was met with by Lieut. Collins in only one instance, about five leagues eastward of St. Genevieve, and in very small quantity: schorl and traces of iridescent or Labrador felspar were observed in the same locality: and hypersthene, or Labrador hornblende, was often noticed. I sometimes imagined, that I could perceive an imperfect stratification in these granitic rocks, but it may have been the result of structure, and upon the whole I regard them as unstratified. They are traversed occasionally by trap veins, insignificant in size, when compared with the immense dykes of the Lake Superior granites, which appear to have poured forth such extensive beds of greenstone and amygda- loid, an operation which probably took place under the ocean, from the frequent association of beds of rolled masses of porphyry, cemented by a paste of the same material as those igneous rocks. Six rivers of considerable magnitude, besides smaller streams, enter the Gulf of St. Lawrence between St. Genevieve and Cape Whittle, namely the Nabe- sippe, Aqwanus, Natashquan, Mushquarro, La Romaine, and Coacoatcho, and are respectively distant from St. Genevieve 33, 38, 50, 79, 97, and 110 miles. They are all unnavigable in consequence of shallows or rapids, com- mencing a short distance within their entrances. The Natashquan, which flows into the gulf directly opposite the east end of the Island of Anti- costi, is the largest, and is remarkable for the great quantity of sand which it discharges into the sea; and its wide hed, like that of the Moisic, is full of sand-banks. Its mouth is on the west side, and near the southern extremity of an alluvial promontory, the materials ‘of which it appears to have brought down during the course of ages. This alluvial accumulation, formed evidently by the combined action of the river, tides, winds, and waves, is the most extensive which we have seen on the north coast of the St. Lawrence below Quebec, unless that of the River Moisic be equally so. Its area is forty-eight square miles, and it has completely covered the low granitic islets and rocks. ‘Thus, it has not only interrupted the direction, but also completely changed the character of the coast for the distance of twenty miles, substituting cliffs of sand, or sandy clay, with a fine sandy beach in front, for innumerable islets, rocks, and reefs. 11. To the southward of the Mingan islands and along the coast of La- brador, as far east as we have yet examined, are extensive banks having from twenty to forty fathoms of water, and composed of gravel, sand, and immense quantities of broken shells. In sounding over many hundreds of square miles, fragments of shells, and occasionally of coral, were brought up, by almost the Geology of the North Coast of the St. Lawrence. 110 every cast of the lead. Indeed there is nothing more remarkable than the immense quantity of calcareous matter, supplied by testaceous and crustaceous animals, in the Estuary and Gulf of St. Lawrence. The beaches were occa- sionally composed almost exclusively of small fragments of shells. In depths exceeding fifty or sixty fathoms the bottom was usually mud. Another fact which forced itself upon our notice, was the frequent occur- rence of the bones of cetacea along the shores, and probably, for the most part, of animals destroyed by the whalers. ‘They were frequently observed on the low alluvial flats at the entrances of rivers, and were sometimes ac- companied by marine, freshwater, and terrestrial testacea, together with the bones of quadrupeds and birds*. In such situations these remains can scarcely escape being carried away by freshets, at the periodical melting of the winter’s snows, and being promiscuously deposited in the mud and sand on the bars of the rivers. May we not attribute to similar combinations of circum- stances, the admixture of marine with freshwater, or terrestrial remains, in more ancient formations, where no other circumstances appear to contradict such an inference ? 12. I shall close this paper with a few observations intended to complete a very rough outline of the geology of the river and estuary of the St. Lawrence below Quebec. All the islands on the south shore of the St. Lawrence above the junction of the Saquenay, and the few below it, together with the whole of the south coast as low down as Cape Rozier, are composed of alternating strata of grey- wacke and slate, dipping to the southward at angles varying from about 30° to nearly 90°. Above Cape Chat the hills which bound the valley of the St. Lawrence to the southward, are some miles from the coast, but at Cape St. Anns, a few miles below Cape Chat, they approach the sea, and give a mountainous character to the remainder of the coast as far as Cape Gaspé. We have ascertained, by actual observation, that the hills next the sea, as high as 1000 or 1500 feet, are of greywacke and slate. There is a higher, parallel chain a few miles back, which, in one part, is nearly 4000 feet above the sea, being the highest Jand in Canada or the United States, excepting the mountains of New Hampshire. This higher chain has been said to be primary and the outline or contour of the hills which compose it, lead to that infer- ence. I doubt, nevertheless, of this being the case, because I lave observed * On the sands at the entrance of the river at Mingan, I saw the whole of these remains together. 102 Capt. Bayrietp’s Notes on the St. Lawrence. that the dip of the transition rocks is not changed by their immediate vicinity, and because other hills of considerable elevation and of the same appearance, have been ascertained to be of sandstone. I am inclined to think that they will be found to be of greywacke, or of secondary rocks over- lying that formation. The south coast of the St. Lawrence follows the direction of these hills, curving to the southward as we proceed to the eastward ; and it is worthy of remark, that the direction of the strata seems to follow that of the coast. The greywacke series terminates on the coast at Cape Rozier, and is succeeded by conformable strata of limestone, dipping at an angle of about twenty-five degrees to the south-west, and forming the remarkable and precipitous head- land of Cape Gaspé. This limestone contains Encrinites, corals, Orthocera, Producta, and other shells similar to those found in the limestones of Anticosti and the Mingan and Esquimaux islands. It contains thin veins of galena and blende, but not worth working. This limestone, which I conceive to be the younger transition, is succeeded to the southward, by a series of alternating sandstones and shales, the strata of which are much disturbed, but preserve a general, conformable dip to the south-west. Both the sandstones and shales are highly bituminous, and pe- troleum springs have been found in the neighbourhood. , Still further to the southward, at Percé, near the entrance of the Bay of Chaleur, conglomerate, sandstone, shale, and limestone were observed, alter- nating in conformable strata, and preserving the same general dip as before mentioned. Among these, coal is said to have been discovered, thus indi- cating the approach towards the extensive coal formation of New Brunswick. It is probable that we shall learn more respecting the formations of this neighbourhood, when we survey the southern part of the gulf. I must now close the paper with a hope, that the desultory and imperfect nature of the information which it contains, will be excused, when it is con- sidered that the remarks, here given, were the result of those casual ob- servations, which we were enabled to make, during the prosecution of our professional duties. | : ‘| ? de Ly f \ 7 > i J ; f ‘a a | i ' wy ‘ . i ’ , : te - ad a 1 TA PPT A TOA S26 yg SUBST, “1009 Soy ’ Te z z a p__$1.- Eye ¥¢ woo ® SAP JO AyDIe snnnaansennstfoe é rune : T AANT 9 ary “Boy, rs ¢: Du, JUD: ae a uounue, hi oS ovsesstinn AIIM . = arm ; o° Ld yt C re retin en ys” Yin Br UA puoi LE ae eee punos” “hd: v7 LDH je "Ss ep AUS 7 PAD) SIISSD: Fini amdis Dy GL PSLNUOS a “* Sebioag 3° uUnapsabides 5 mara WEL ‘cord SOTALOUINP Pasn App WOLL PAYPEYS 82 PRT Mp JO RUN MYT, “AY Tos nary Aq “SPCQWYA FHL JO NVTI Bs a wp ynyy sypmupy PRL 008 LITY COT Ony 2 Su F 103 3 V.—On the Geology of the Bermudas. By RICHARD J. NELSON, Ese. Lieut. R.E. Br eProunicated by George Betias Greenovuen, Esq., P.G.S. [Read April 23, 1834.] HAVING been stationed at the Bermudas, ai different periods between the years 1827 and 1833, I made a series of notes on the peculiarities of their structure, and the following memoir is the result. Much information was de- rived from sources which are no longer accessible, such as the aspect and arrangement of the strata, presented by large excavations made during the progress of the works, conducted by the Royal Engineer Department, and are either no longer in existence, or are masked by revétements*. Though the Bermudas are barren of mineralogical interest, they have yet claims to attention in the striking lithological resemblance, which some of their rocks bear to chalk and other secondary limestones ; and I hope that my descriptions may afford a clue to the origin and nature of those formations. Conceiving also that a comparison of the Bermudas with the coral islands in the Pacific, described by Kotzebue, might be instructive, I have given refer- ences to those passages in the work of that author, which present any ana- logy or important variation. The Summer Isles, Somers’ Islands, or Bermudas, (see Plate VI.) con- sist of a group of about 150 islets, lying within a space of fifteen miles by five, and containing altogether nearly twenty-one square miles. This singular little archipelago is situated very near, and conformably to, the south-east side of an elongated ring of what are commonly called} coral reefs, and rudely approaching the shape of an ellipse, twenty-five miles long by thirteen broad. 'The direction of the group, as well as that of the major-axis of the reef, to which it is parallel, is about north-east and south-west. Although of a more regular form than any exhibited by Kotzebue, it bears a considerable * The collections formed by the author have been presented to the Museum of the Geological Society of London, the United Service Museum, the Berlin Academy, and the Cabinet of Sir John Tilden. t “Commonly called.” This qualification is explained in pages 105 and 116, where it is shown that many reefs are formed by Serpulz. 104 Lieut. Netson on the Geology of the Bermudas. resemblance to the Otdia, or Romanzoff islands. The principal islands are generally separated by channels, from ten to twenty feet deep, and many of the spaces between the smaller islands are fordable. The depth within the reef rarely exceeds twelve or fourteen fathoms*. The highest land is at Sear’s Hill, immediately above and to the westward of Harrington Sound. Its summit may be about 260 feet above the sea ; that of Gibbs’ Hill is 245 feet. These and all the other numerous small emi- nences, have much the appearance of sand hills in shape, and chalk downs in colour. The whole of the islarids are composed of calcareous rocks, derived from comminuted shells and corals; and vary in texture from loose sand to a hard compact limestone, susceptible of a good polish. The varieties are irregu- larly associated, and without any order of superposition f. From the saddle-shaped sections observable throughout the islands, the strata have evidently been accumulated round numerous and contiguous centres: the question as to the agency to which this is attributable, will be discussed in its proper place tf. The bottom of the basin consists of coral reefs (which do not appear above low water mark, except at spring tides) and calcareous sand, the last being associated with considerable tracts of chalky ground, in which the best an- chorages are found. I have met with this chalk likewise as a constituent of the rock, lying irregularly among its beds in a soft state, or lining caverns, * Kotzebue describes the coral islands of the Pacific as consisting of circles of islets, amounting in some instances to sixty, and surrounding a lagoon. The intervals between the islets are dry at ebb tide; but the centre of the lagoon generally varies in depth from thirty to thirty-five fathoms, the soundings gradually decreasing towards the margin. In those seas, where the con- stant monsoons prevail, the windward side of the island first rises above the level of the water, being composed chiefly of blocks of coral and fragments of shells thrown up by the waves. Voyage to Behring’s Straits, vol. iii. p. 333 : 1821. In Kotzebue’s chart of the Radack and Ralick chains, there are exceptions to the rule of the islands being exactly on the windward side. Bermuda is not subject to any very regular wind ; perhaps more to the south-west than any other. Currents have been likewise observed setting towards the island from the north-east, though I cannot say whether permanently or not; or whether the gulf stream possesses any influence in those parts. The harbours at Bermuda are not always so particularly ‘calm’; and it is only in certain points that they are absolutely ‘ secure’. There are several entrances to the interior practicable to vessels of about twelve feet water ; but only two for ships of any size, the south-east passage, and that of the north rock, both very intricate. + See Kotzebue’s similar account of the structure of coral islands, Ibid. vol. ii. p. 357 ; vol. ii. p. 141 ; and in particular the alternation of beds of sand and limestone, Ibid. pp. 144, 145. t See Kotzebue, vol. ili. p. 144, for similar conformations in the strata. Lieut. Nexson on the Geology of the Bermudas. 105 but seldom exceeding a few square yards in surface, anda few inches in depth”. The islands are covered with about a foot of dry, red earth, containing vegetable matter, and behaving before the blowpipe exactly like common aluminous earth. The only minerals which have been noticed, are small pieces of oxide of iron, of very questionable origin ; menaccanite, found near the ferry between St. George’s Island and Bermuda or Main Island; arragonite, and a minute quantity of manganese in the red earth. Unless immediately after a heavy shower, or when a fine cool morning acts as a refrigerator to the evaporation of the preceding, sultry day, or in the im- mediate neighbourhood of the marshes, the dew, though it does fall in all places, is scarcely perceptible, owing to the porous nature of the rock. Having thus briefly noticed the coincidences between the structure of the Bermudas and the coral islands of the Pacific, I will mention an instance which indicates a difference. Kotzebue says, “The reefs at Otdia consist principally of dark coral, which is mixed with but a little red; at low water the rocks are visible for about two feet, which was the case when we used the stream anchor; but all was soon covered by the rising tide. We had at a small distance from it forty fathoms’ depth, but which increased a little further so much that we could find no bottom.” This answers to the description of our serpuline reefs, but not of those which owe their origin to zoophytes. The observation was made by Kotze- bue, and seems to have been overlooked by Chamisso. It is proper to add, although the animal of the Serpula can live for many hours out of the water, yet that of most corals, on exposure, deliquesce in a few minutes into a slimy liquid. The tides at Bermuda average about four feet six inches ; and at low water the serpuline reefs stand about two feet above the surface. The variations in the outside soundings, are by no means as rapid as in the South Sea coral islands. * Capt. Kotzebue says, ‘‘ The greatest depth in the whole group (Capeniur) was twenty fathoms. In our anchorage place we had only six fathoms : the bottom consisted of white clay, a circumstance which we had not met with in any other group.” ‘As this clay is noticed by Captain Kotzebue, and not by either of the naturalists, it is very probable that the word ‘ clay’ was used without respect to its more specific meaning, as restricted to aluminous earth. The local name for the Bermudian chalk, is pipe-clay. + Kotzebue says (vol. ii. p. 45.) “no dew falls,” and (vol. i. p. 152. vol. 3. p. 145.) “ the in- habitants depend on rain for their supplies of fresh water ; of which, however, there is no want in the larger islands, as it rises in pits dug for the purpose.” { Vol. ii. p. 16. VOL. V.—SECOND SERIES. P 106 Lieut. Nexson on the Geology of the Bermudas. GeotocicaL Drraits oF THE PRINCIPAL IsLAnDs IN GEOGRAPHICAL ORDER *. St. George’s Island.—The strata dip southward with considerable uniformity along the southern and eastern shores, which are protected from violent attacks of the sea by St. David's, Smith’s, and Longbird islands; and by the reefs which bound the intricate passage into Murray’s Anchorage. The north side is exposed, throughout its whole length, to, the fury of a sea which has had, within the area of the north reef, a distance of seven or eight miles, sufficient space to re- accumulate its destructive energies ; and exhibits in the cliffs the saddle or dome-shaped structure, (variously exemplified in figs. 1 and 2,) the lines of lamination dipping towards every point of the compass. In one or two instances, the summits of what were once internal hills, are bared, and within a few square yards the coats of this nucleus range round it with perfect regularity. As might be expected, this north side consists, in a great measure, of abrupt cliffs, and landslips brought down by the undermining of the waves. Fig. 1. Sections at the summit of Retreat Hill. This section is at right angles to Fig. 1, the points (a) coinciding. The sandstone on the summit of some of the hills, is scarcely tenacious enough to hold together ; but from Mullet Bay to the ferry, on a level of not more than twenty feet above the sea, the rock suddenly becomes a very hard, fine-grained or compact limestone, in which scarcely a vestige of organic structure is visible. Just above high-water mark, along a considerable portion of the south side, is a stratum of calcareous sand, about six feet thick, apparently a distinct deposit from the rock above it. Vertical crevices abound, filled with a substalagmitet much harder than the rock. In some places the arrangement of these cavities resembles that of veins in old slate or limestone. Where the partitions stand comparatively unimpaired by the weather, their planes constantly intersect one another, and thus form reticulations, once filled with the soft sandstone. In all cases the veins are younger than the crevices, from whatever cause these last may have originated. St. David’s.—Like St. George’s, this island consists of a low, irregular belt of hard limestone * Map, Plate VI. + I have employed this word to designate uncrystallized calcareous incrustations and deposits; whilst I have retained the word ‘stalagmite’ to describe such as are crystallized. Lieut. Netson on the Geology of the Bermudas. 107 which commences in the centre of the north side, and continues westward, through Stock’s Point, till it appears, as above noticed, at Mullet Bay. Cooper’s Island.—Here I have remarked nothing, except the supposed cast of a tree at the south-east point. It will be referred to under the head of ‘ Organics.’ Longbird Island—Affords an excellent horizontal section along the south side of strata, depo- sited in irregular undulations, and not contorted by any subsequent disturbance. Nonsuch, Castle, and Goat Islands.—As far as interest depends on variety, these possess but little. They, however, exhibit the frusta of the saddle-shaped structure, which may often be traced from one island to another, though frequently separated by considerable intervals. Bermuda, or the Main Island.—The description given of the north side of St. George’s answers in all respects to that of the whole of those coasts which are exposed to the ocean. On the south side, the sand has made several encroachments, but only at Elbow Bay, with any great success. This sand tract will be more minutely described under ‘ encroachments ;’ but I may here remark, that wherever the rain, in effecting its escape, has scooped channels in the slope of this sand, their sides and bottom are lined with substalagmite of about one eighth of an inch thick. This is not peculiar to Elbow Bay, for, generally, wherever the sandy rock has been exposed in a hill side, it will be found coated with this incrustation. Westward of Hungry Bay, the rock assumes a somewhat uniform character. A stratum of sand, corresponding to that on the south side of St. George’s Island, begins to show itself at about the centre of the island, continuing thence for a few miles westward; but in both in- stances there seems little difference in age between these sand beds and the strata above them, as the same shell, an helix, is found in abundance at all levels. Fig. 3. PN wg Oe APR me @ GA ee SO ae Figs. 3 and 4 are general sketches of the cliffs along this south coast, especially between Elbow and Whale Bays. Fig. 3, a, b, ordinary rock, friable calcareous stone occasionally appearing, as under e, fig. 4, with faults, where the sand stratum (c) has been washed away, and thus assisted the sea in strewing these coasts with landslips and huge blocks. Fig. 3. d, Apparently a very new deposit, from the looseness of its texture, and its containing perfectly recent marine shells ; it seems to be merely a covering to the regular rock lying under c. Somerset.—One of the prettiest islands, has but little to attract the attention of the geologist. P2 108 Lieut. NEetson on the Geology of the Bermudas. Treland.—The position of this island is similar to that of St. George’s ; but owing to its narrow~ ness (in one place, Cockburn’s Cut, the breadth being hardly fifty yards) there is little room for the development of the saddle-shape ; although I conceive that a reference to figs. 5, 6, will show that however now truncated, it once existed. Fig. 5, section east end of the island, and Fig. 6, section at right angles to a, Fig. 5. Fig. 5. LE: MY UE EEE Ms Mts tt Z LIE ty Yj ido 8 WV) alll Li 7 b. a. f. i. h. medium stone, c. soft sandy bed passing into b. g. d. d. e. g. hard rock. Fig. 7. Tica Me No a ea Caverns under stratum d, fig. 5, and covered with red earth /. Although, as before stated, a species of helix occurs in all the strata, not merely imbedded, but filled with a hard stone, yet in this island there are six or seven marked divisions in the section, showing different deposits of red earth (fig. 5), similar to that on the surface, not only in compo- sition, but in being deposited in the rude troughs formed by the abraded basset edges of the strata. The rock above d is uniform in structure and texture, and thus contains the best quarries ; that below it, is generally rubbly and short-grained, varying constantly from a hard limestone to loose sand ; below this bed also, numerous caverns (b,) have been opened during the progress of the fortifications ; and, with but very few exceptions, whenever they are perfect, they contain salt- water, having their bottom below the sea level. In every instance except one (fig. 8. p. 112), the red earth lies almost immediately on the roofs of these hollows, fig. 7. l. Ireland is remarkable for having the finest quarry of building materials in the whole group. The stone of the eastern half consists of fine and coarse particles of comminuted shells or corals, hard subcrystalline limestone, and masses of corals imbedded in compact or granular limestone. The softer varieties prevail from Cockburn’s Cut, westward. ALLUVIUM. All that can be noticed under this head is the black, rich, tenacious mud of the marshy districts ; it has obviously much of a vegetable nature, and makes an excellent garden soil when mixed with the red earth. By different measurements which I have taken, the Mangrove Swamp and Lieut. Netson on the Geology of the Bermudas. 109 Salt Marsh A* is on a level with B: as far as I can judge, all the others in the islands are not above the sea level. The water is almost fresh, but in sum- mer, these ponds become stagnant and very offensive. _ ENcROACHMENTS. Land on Sea.—The harbours and inlets of Bermuda share the same fate as those of all other places, where it is easier for the sea to introduce silt and sand in its first strength, than to withdraw it when the velocity of its waters is reduced by the obstructions of the sand-banks, rocks and reefs forming the confined and labyrinthine passages among coral groups. Thus at the head of Crow-lane, Bermuda or Main Island, within the memory of the present generation, ships of some burthen used to lie at wharfs, where now scarcely a large boat can repair at all tides. The same has occurred in the narrow channel between Ordnance Island and the Market-wharf at St. George’s, but to a far greater extent. The Flatts Inlet, entrance to Harrington Sound, is perceptibly filling, notwithstanding the benefit it receives from the Sound as a backwater. - Sea on Land.—There is a limit to these encroachments ; for although the action of the sea is powerful enough to undermine the ordinary strata, yet when it reaches the hard calcareous rock it can proceed no further ; and this stone, which I shall hereafter designate as ‘ Base rock,’ will be found wanting under all the recent landslips ; hence, with these exceptions, I know but one instance of marine encroachments. In 1801 Shelly Bay scarcely existed: what is now the mouth, was at that time a row of sand hills; and the road on the north side lay close within. Some free blacks who lived there, being in want of fuel, cut down the plants which kept these sand hills in a solid state. Being no longer duly opposed, the sea quickly broke through, and now retains pos- session of the ground at least 100 yards in rear of the old road, traces of which are still visible. The Mangrove Swamp between the beach and the present road, was until then a garden. Sand Encroachments——Though there are objections to the last being termed a strictly geological fact, yet I have introduced it, and the following details of the sand flood at Elbow Bay, on account of their great utility. The proprietor of the principal part of the land of this bay, the venerable Captain Lightbourne, remembers an attempt about seventy years ago, when the inhabitants expected an attack from the French and Spaniards, to form a breastwork along the sand-hills, which then, as at Shelly Bay, skirted the coast. In doing so, they cut through the natural protections given by the sea-shrubs and creepers which usually abound in such places. From that day the sand, supported by con- stant supplies from the sea, has steadily proceeded up the hill to the very summit, a height of about 180 feet. It is, however, surprising to observe the singular state of arrest under which the * Map, Pl. VI., Fig. 2. 110 Lieut. NEtson on the Geology of the Bermudas. invader stands before the children of the soil. A few straggling cedars,widely scattered in advance of the wood which now bounds the space, have been passed by this sand flood, yet the dazzling, dry, and almost snow-white sand is checked, before the front rank of the trees, in a steep bank, varying from ten to twenty-five feet in height, and so remarkably well defined that scarcely a particle is scattered beyond a distance of twenty yards. As soon as the mass shall have over- topped the woods, I know nothing capable of opposing its progress, as there are no streams at Bermuda to act like the little brook in St. Owen’s valley at Jersey*, which has so effectually stopped the march of the Quenodis. Although this inroad commenced so long ago, yet the principal advance has been since 1807, from which date about 200 yards have been gained on the eastern side. Before I left the colony in March 1833, the sand had reached the northern corner of a cottage belonging to a man called Ned Keel (on Mr. Butterfield’s estate); and the top of the bank, eight feet high, was on a level with the eaves of the shed. During the last fourteen years it has progressed, at this point, only about forty yards, in a bed from four to eight feet deep, in consequence of the repulsive action of a thin belt of cedars just below. Very near this spot also, is a small circular group of the same trees, which the sand has passed, and imbedded to the depth of from six to eight feet ; but the space within has been so perfectly screened, that the bottom of this little oasis is the natural green- sward. There is another encroachment at Tucker’s Town, said to have taken place about sixty years ago; and has crossed the neck between Harrington’s Sound and the sea; but beyond this it does not seem inclined to move. The sand has not been stopped, at the eastern extremity of this beach, where the bluffs commence, by their very considerable declivity,—though it has been most effectually at the crest of the slope, by a natural fence of sage bush, growing partly in the soil and partly in the sand; which, as it ascended, seems to have thus rolled on with the seeds of de- struction to its progress, in its own bosom. The same operations appear to have occurred throughout the sand tracts at and near Great Turtle Bay. Whatever scheme may hereafter be executed for the further defence of the south side, it will be well to remember the fate of Captain Lightbourne’s property ; so that if a military road be formed over such ground, to make it on the turf, and on no account to cut through it. Hence also, where a stream of water cannot be commanded, plantations of trees, suitable to the soil, will for a long time maintain a very efficient opposition; and though it is to be feared, that eventually they must succumb, where turf and creepers have not established themselves, still, to have effected the preservation of a district for a generation or two, cannot be considered as the attainment of a trifling object. a In Elbow Bay the sand contains, generally on or near the surface, layers, scales, and tubes of calcareous stone, which cannot have been many years in forming, though f have not sufficient data to determine the precise number. The greatest thickness of the layers is about 1} inches ; and although found on the surface, they are not, I apprehend, produced there, but at a few feet or inches beneath. The sand on the weather side of the little saddles is constantly blowing away, and the edges of the reverse strata, or rather lamina, becoming exposed and undermined, fall down. An inspection of some of these slabs will prove how perfectly, recent specimens may be con- * See a paper of mine, published in the late Quarterly Journal of Science for October 1829, on the Geology of Jersey, and its relation to that of the Devonshire and Norman coasts. Lieut. NEtson on the Geology of the Bermudas. 111 tained in stone which has acquired great hardness. On the beach, about 300 yards west of Rose- lands, the matrix was so firmly attached to slabs of sound, compact, sonorous limestone, as to be in many instances perfectly identified with them. It cost me nearly as much labour to dislodge some of these specimens as I have bestowed on greenstones. An Astrea, like 4. Rotulosa, Z'urbo Pica, fragments of Ostrea, Spondylus, &c. &c., all contributed with the shelly sand towards the formation of this striking conglomerate. Other blocks of coral reef may be found, imbedded in the rock on the south side. There is one in particular 300 yards east of Elbow Bay, about ten yards from the water’s edge, and four or five feet above it; at some points this block is quite assimilated with the matrix, but at others, stands out in relief, in consequence of its greater durability. The calcareous tubes are very generally found throughout the islands, apparently aggregated around grass or small roots, as nuclei, which have subsequently decayed. They have almost always an earthy matter running down the axis. Beds, nay strata of these tubular deposits, may be found in various parts, as in the neighbourhood of Tobacco Bay near St. George’s, and in the bank a little to the westward of Harris’s Bay, where the cliffs commence; though nowhere to such an extent as at Ireland Island, between Bombay and the south-west point, where the stratum is about four feet thick, and corresponds to a similar formation on Skinner’s or Tate’s Island. The cliffs to the westward of Elbow Bay are curiously perforated to a great extent by similar tubular holes; but there they are detached from each other, and are generally vertical and much larger. ORGANICS. The whole of the Bermudas, and perhaps many of the older rocks, may be called “ Organic Formations,” as they present but one mass of animal re- mains, in various stages of comminution and disintegration. From the most compact rock to the very sand of the shore, the materials are universally frag- ments of shells, corals, &c. &c. Of the former the Venus Pennsylvanica is the most abundant, being found in every part of the colony, more especially among the newer aggregates on the coast; and in every state, from the perfect specimen to the smallest particle. A stratum of these, in indifferent preservation, is in the quarry whence the stone for the pier at St. George’s ferry was obtained. This bed, however, is of trifling extent compared with an apparently corresponding one in the chain of islets reaching across the mouth of Crow-lane Harbour, beginning near Phyllis’ Island, and continuing thence through every point in the line till it reaches Harris’s Island: it is about five feet thick and lies about six feet above the water. In the chain above-mentioned I have obtained excellent specimens of the Scutella Quinqueforis, having the pores of the crust filled with crystallized carbonate of lime ; like the Echinites occasionally found similarly circum- stanced in the European chalk. The Turbo Pica is very abundant, with the nacre and colours ; but like the Venus Pennsylvanica, it is chiefly met with in sand-pits, and more recent formations, though without the slightest reference to the hardness of the 112 Lieut. Netson on the Geology of the Bermudas. stone containing it. It seemed difficult at first to account for these large shells (Turbo Pica) being found on heights, where, from their weight, it was impossible to suppose they had been carried by the wind; but a solution may be found in the habits of the Soldier Crab, which, on more than one occasion, I have seen running about in these shells. The most interesting organics with which I have met, were in the rock now inclosed by the North Bastion, at Ireland Island. Whilst cutting the escarp of this work, a large block of reef was discovered in the solid rock, fifteen or twenty feet from the surface, and at about four feet above high water. This specimen contained Meandrina areolata, the common Mytilus of the coast, retaining its black colour, and a pink Millepore very common in the serpuline reefs. This spot, conceiving the truncated strata of Ireland to be restored to their proper form, must have been at the very apex of the saddle, and is perfectly distinct from the loose, soft, and newer sandstones. Above the level of this spot, lie the strata a a, fig. 8, which for some hundred yards along the north side, consist chiefly of a hard subcrystalline limestone. Although this stone is by no means as subcrystalline as the transition, or other old limestones, yet it is sufficiently so to show that the structure can be attained by very new rocks, and by other means than that of heat under pressure. Had heat been in anywise applied to such extent, it is more than probable much of the carbonaceous* matter (one of the constituents of the shelly sand) would have been altogether evolved, and would not have remained, black and mixed amongst the particles of the rock. At all events the colours of the Mytilus and Millepora could not possibly have been retained. Fig. 8. In the centre of this rock, fig. 8, was a cavern; and entangled amongst the stalagmitic lining (as well as in that of other caves and crevices), or else lying in heaps in the loose red earth within, we found abundance of a large and delicate Helix. In another instance, upwards of thirty bushels were discovered, without any earth among them : a circumstance easily accounted for by the common habit of these animals to shelter in holes, wherever they can find them. * I have paid some attention to the membranous tissues of zoophytes, and find full proof of their existence in many varieties of the Bermuda stone. A careful solution in very dilute mu- riatic acid, generally gives a minute flocculent precipitate, which the microscope shows to be the mere animal part of the subject. Lieut. Nexson on the Geology of the Bermudas. 113 I have never seen these creatures alive, nor have I ever heard of their having been seen in that state; but still they were found with a smaller Helix deep in the compact rock at e, fig. 5. This Helix, which is the common, living snail of the island, I obtained in the hardest stone, and in the loosest sand; sometimes lined with druses of carbonate of lime, sometimes filled with a solid cast, at other times slightly cemented together, and frequently retaining some colour; in which condition they are generally found, as before mentioned, in every part of the colony. Returning to the cavern at the North Bastion (fig. 8.). In the heap of red earth, which in this instance only had rather an unctuous feel, mixed with the large Helix, were found quantities of birds’ bones. From the best accounts, the caves at Ireland were frequented until lately by a sea bird, whose local name, derived from its peculiar cry, is Pim-li-co. In hazy weather, or at night, this sound was always a warning for vessels from the West Indies to put about, and avoid the perilous south-west bar and reefs; but since the establishment of the dockyard at Ireland, these birds have almost left the Bermudas. Whilst excavating a ditch near the cavern shown in fig. 5, p. 108, a small hole was discovered in a rather hard rock, composed of comminuted fragments, with the interstices not filled up; it was about twenty feet above the sea, thirty yards from it, and fifteen feet from the top of the hill, but without any apparent connection with the surface. In this hole were found an eggshell and many fragments of bones, similar to the preceding, but they were all, as well as the egg, coated with carbonate of lime*. Ireland is however by no means the exclusive mine for these fossils. Bones, apparently those of birds, have been found in the limestone on the coast of Harrington Sound by Mr. Hill, to whom I am indebted for the. information. He obtained specimens fifty feet from the water, twenty feet above it, and four feet under the surface. Three eggs were found close to the bones, and similarly imbedded. Another egg was found in a block of limestone near Hamilton. A gold knee buckle and a canister shot were dug up in a coarse limestone, whilst excavating the foundations for one part of the North Bastion, across the bottom of the cavern: they were ac- companied by Scutella Quinqueforis, containing crystallized carbonate of lime as before, and Agaricia undata. This rock, a genuine coral rag, is three or four feet thick, and is evidently in a progressive state of consolidation. As it was under water, and as we constantly find stalagmite in the caverns similarly situated, it seems that evaporation, however conducive to the com- pactness of strata, and the depositing lime once held in solution, is by no means a necessary requisite. Turtle bones were also procured from the North Bastion coral rag, and from the sands at Elbow Bay. The turtles seem, like the poor bird before mentioned, to have been buried while de- positing its eggs, as the two skeletons when first discovered were entire and undisturbed, Their dimensions were nine feet in length, and seven in breadth, as I was informed by an eye-witness. These bones, as well as those of birds from the North Bastion, Harrington Sound, and the ditch near 4, fig. 5, all adhere strongly to the tongue; hence no further reliance can be placed on this circumstance as a criterion of age. Nor can crystallization or compactness be considered unequivocal testimony, in arriving at conclusions respecting the age of a rock. In the North Bastion, in the interior crevices of the coral rock, were many fine specimens of Cypreea and Bulla, but with abraded surfaces. * It is the known habit of many sea birds, particularly the tropic bird, or ‘ Boatswain,’ so numerous at Bermuda, to make their nests in hollows of the cliffs; and it would seem as if the animal had been immured during the period of incubation, by some fresh deposit of sand which had afterwards hardened into the walls of its prison house. VOL. V.—SECOND SERIES. Q 114 Lieut. Netson on the Geology of the Bermudas. The last individual Animal Organic which I shall mention, is a Strombus which I chiselled out at Long-bird Island, and had the cavities in the substance of the shell filled with crystallized car- bonate of lime. I may terminate this list comprehensively by saying, that almost every shell now known in the surrounding sea, may be found in the rock quite perfect, except with regard to colour, especially among the newer beds on the sea coast. Chalk.—It may be considered rather a bold step to place this mineral un- der the head of ‘ Organics,’ but from all that I have seen during different examinations of decomposing zoophytes and shells, from the least calcareous to the large and massive Meandrina and Astrea, not only whilst breaking or cutting them with my own hands, but as obtained from the extensive ex- cavations made by the dockyard diving-bells for the foundations of the wharfs, and from the soil torn up by large mooring anchors, [ have no more hesitation in attributing the existence of the Bermuda chalk to such a source, than I have for asserting that the obvious material of the Bermuda stone is derived from the same origin; with, however, this difference, that in the latter instance the fragments are the result of mechanical subdivision ; while in the former, the elementary particles are due to the decay, by long submer- sion, of the membranous tissue*, which, pervading their whole structure, releases the constituent calcareous matter dispersed through the texture, when it is ruined by decomposition. ‘These animals, and the many marine plants, consisting chiefly of lime, produce this chalk, just as terrestrial animals and vegetables give carbon to soil when they decay. I no more pretend to argue that the European chalk was thus produced, than that the caverns of all the various limestones were formed by means similar to those which excavated the caves at Bermuda (see page 119) ; or that the coral rag of the oolites is related to that of the North Bastion ; but certainly the external and the chemical peculiarities are as much the same as their common character of being marine deposits. This chalk, as found in the harbour bottom, is much mixed with shell-sand, corals of many sorts, shells in a perfect state, and gigantic masses of equally perfect Astrea and Mzandrina, as well as in every stage of decay, leaving no doubt of their having lived and perished where they are found. The aspect of this chalk when fresh, is precisely that of crude mortar. A variety, which may be termed stalactitic, was found in some of the newly opened caves, and resembled curds in consistency+. In some cases it occurs in small shapeless deposits among the regular strata, or lining the crevices and insides of caverns. This variety, when dry, consists of very fine white powder, which yields to the least pressure and soils the fingers. * When a fresh specimen of any sort of coral is carefully submitted to very diluted muriatic acid, the membranous tissue may be obtained as satisfactorily as from a bone. + The same substance is to be found on the lower surface of the crust covering the bottom of Chudleigh rock caverns. Lieut.. Netson on the Geology of the Bermudas. 115 The surface of the calcareous sandstones, is, in some places, coated by compact stalagmite, and I believe a strong resemblance, if not identity, will be found between its nature and the hard chalk near the basaltic districts of Antrim, the solidifying of which has been attributed to fire. This inference may be true; but here isa clear fact, that such limestone can be otherwise pro- duced. Not that the conclusions from Sir J. Hall’s most interesting experiments are the less valid, countenanced as they are by the results of the action of Trap and Whin on the immediately contiguous strata. Such a mode of consolidation, however, is not perhaps so likely to occur on an extended scale, or to produce such regular strata, as that which has formed the Bermuda stone. It is, moreover, an additional means of arriving at certainty, to allow every known force its fair consideration. Vegetable Organics.—These are doubtful. Fig. 9 is however a sketch and section of certain rudely-shaped cylindrical blocks which are to be found on every part of the surface of Bermuda, though I never heard of their being discovered below it. They are very frequently arranged in groups of from twenty to fifty, as if they had once been the roots of as many trees. Fig. 10, c, d, are plan and section of the recent Palmetto root, which has, in common with the subject under consideration, a very marked socket, or deep cup*. When this tree dies, it generally falls out of the cup, of which excellent examples may be seen at low water in Shelly Bay, north of Harrington Sound, Bermuda. It is the general surmise that these curious cylinders (fig. 8) are the remains of the Palmetto. I think it very likely that they belong to a mem- ber of the family of Palms; though I have my doubts as to the Palmetto being the individual, as the internal surface of its root socket is entirely composed of * Sometimes only casts of these roots are left as pits in the rock; but in the compacter limestones, I have more than once met with cylindrical excavations, evidently the work of water. They vary from two to three feet in diameter, and may be about eight or twelve inches deep, These are mentioned merely from their singular resemblance to the ‘ Rock Basons,’ on the crags of Dartmoor, supposed to be Druidical. That which I have more particularly in mind is on the apex of Heytor. The flat bottom of the latter showing its broad streaks of felspar, had evidently a different origin from the equally flat ones of the Bermuda pits, which seem to be a natural deposit and mixture of sea salt and sand. Q 2 116 Lieut, Neson on the Geology of the Bermudas. the ends of the nearly straight and tubular roots, about one-fifth of an inch in diameter, which diverge into the ground as so many radii. Now in the supposed organics, in the inside of the cup, although smooth, I never could detect these ends of the radicles ; and there is too much irregularity to allow me to join in the received opinion without hesitation ; though nothing like any other description of palm relics has been yet discovered. Reers. The notices relative to these structures, which I at first intended for this paper, have so exceeded it in bulk, that they are reserved for a separate essay. I merely remark that there are two distinct kinds; those formed by Serpula, and those by Zoophytes of all descriptions, which construct calca- reous skeletons. : Figs. 11, 12, and 13, exhibit such plans, sections, and views as will suffice to illustrate their leading peculiarities, especially one that is common to both varieties, that of forming a belt round any obstacle which offers a rallying point ; whether such centre be the head ofa rock, or the base of a mountain. Fig. 11. Plan of a Coral Reef forming around a sandbank. Lieut. Netson on the Geology of the Bermudas. 117 Fig. 13. Serpuline Reef and Section, near Elbow Bay, “C1 7gy Y Pia Me) Dituviat AGENCY. External Evidences.—Fig. 2, Plate VI. illustrates the true forms of the ground taken at points in the islands without any especial selection. The lines are surveys of horizontal contours, traced by a spirit level, at given heights. An eye accustomed to such topographical considerations, will, I think, recognise a similarity to the results which in other parts of the world have been referred to the sweeping action of a huge body of water. I cannot but suppose that such singular lines of islets, as those terminating Long-bird island, those in Crow-lane Harbour, the ‘ Stags,’ near Crawl Point, &c., are most naturally accounted for by the exertion of such a force; as the strata in these little spots are nearly always horizontal, and evidently frusta of a more extensive formation. It has just been stated, that reefs generally collect close, and parallel to any shore as a nucleus. Throughout the whole extent of the south side of the group, there is exactly such a general conformity to the shore in the Serpuline reefs, which, nevertheless, vary in their distance from it, between fifty and five hundred yards. Its contour-like resemblance (Map, Plate VI.) to a former coast line is very striking, especially when the numerous coincidences are duly considered between the present positions of its fragments, and those of the more or less truncated hills along the sea side ; at the original foot of which they would generally lie, were the slopes of the ground restored. Such circumstances can however yield only probable evidence. To convert them into positive testimony we should require that points of hard persistent rock should appear through this reef at such irregular distances as would be suggested by the variable density of the Bermuda stone ; and we might likewise expect that, occasionally, the summits of these peaks should exhibit a stratified appearance. We have abundance of such witnesses in what are called ‘ Boilers,’ ‘ Breakers,’ &c., or rock heads, which have served as points of aggregation to the reefs around them. Such are the Boilers on the continuation of the line of the point, at the west end of Great Turtle Bay ; those in the centre of Common Landing Bay; the long and dangerous chain of about thirty sunken rocks, between the Bear Boiler and the South-West Breaker; the ‘Stags,’ between Ireland island and Spanish Point, &c. &e. From accounts received, I have reason to suppose that such are to be found all round the North Reef; but at one place I am certain of it, the ‘ North Rock,’ or as the old French maps used to call it, ‘ La petite Bermuda;” and it is to be observed that the 118 Lieut. Netson on the Geology of the Bermudas. highest pinnacle bears the ultimatum of the desired evidence of ‘ Diluvial Agency,’ a stratified summit, as pointed out to me by the keener eye of my late brother officer, Lieut. Browne, R.E. This monument to departed strata, stands in a Serpuline reef, which is as usual tabular, and appears above low water. The largest rock is about sixteen feet high; and like all those which have withstood the onset of the Atlantic, is composed of “ base rock.” Internal Evidence.—Ireland is the only place, as far as I am aware of, which has supplied such arguments ; the deposits of red earth in fig. 5, contain stones that would have been too heavy for the wind to have moved without utterly dispersing every grain of the soil containing them. From the number of these deposits, we are warranted to conclude, that five or six such cata- strophes have befallen these islands; though the organics establish clearly enough, that as delicate jand shells, they and the strata in which they are imbedded could never have been produced under water; and if a rock in the heart of an island, and at its lowest point, presents animal remains possessing even colour and membranous tissue, with a considerable degree of perfection ; the superincumbent masses cannot boast of any great claims to antiquity; hence the expression ‘ Diluvial Agency,’ as the heading of this section must not be restricted to the Noachian deluge, but to the repetition of several probably subsequent, local ones, and the results of distant vol- canic action, CAVERNS AND PINNACLES. The caverns are numerous, and many of them very beautiful. The largest, and, geologically speaking, the most instructive, is Basset’s, near Somerset- bridge. It is said to extend for more than a mile; but the first few hundred yards of toilsome progress usually satisfies the curiosity of the majority of its visitors. It seems to be comparatively recent, from the fresh state of its surfaces, and the smail quantity of stalactite observable; this absence of incrustation, however, renders the origin of this cavern very palpable; namely, the undermining of the substrata by the sea, the waters of which lie in pools at the bottom. Hence we may consider such caverns as hollows produced by internal landslips; from the most normal of which, to the simplest niche, there is every intermediate point of transition. The north side of the Main island is to a remarkable degree indented with these re- cesses ; and when they occur in more sheltered places, are sure to be rich fields for the naturalist. Lieut. Nzxson on the Geology of the Bermudas. 119 Fig. 8 (p. 112) exhibiting the section of the cavern which once existed under the North Bastion, and Fig. 14 a section of the ground and its caves near the Magazine Pond at Ireland, are I apprehend sufficient to explain my views respecting the origin of these phenomena, as far as Bermuda is concerned. The caves at Walsingham, near the Ferry, are well worth examination, but in point of specu- lative interest, they are inferior to the many and very singular hollows near them, on the neck of land separating Harrington Sound from Castle Harbour; respecting which, all that I can venture to surmise from their sections, their steep and occasionally overhanging sides coated with stalag- mite, is, that they are the remains of former caverns, laid bare by diluvial action. Vertical sections of caves are common enough in the cliffs, Fig. 5, c; and oblique sections (such as that so well known, close to the Ferry, between St. George’s and Hamilton) are not unfrequent on hill sides. , Tucker’s Island cavern was a perfect bijou; with one splendid exception it has hitherto stood unrivalled amongst the caves of Bermuda. This little cavern shown in fig. 5, b, had a length of eighty feet, a breadth of about fifty, a height above the little lake within of at most fifteen, and a depth below its surface scarcely exceeding fourteen. The stalactites were remarkably clear and beautiful, varying from the massive pendent of six or seven feet in length, to the slender incipient fragile tube, which crumbled at the slightest touch. It was a scene not to be readily forgotten, when we launched a little boat into the miner’s first and narrow opening, through which the sun shone strongly, and reflecting its light from the face of the water upwards and with power to the sparry fretted ceiling of the vault, illuminated it in a way which can only be appreciated by those who have been eye witnesses of such effects. This cave was shortly afterwards destroyed, as interfering with the safety of the works. The irregular density of the rock is exhibited on all scales, from minute flaws and patches to large masses of dry sand ; which more than once occurred during the progress of our excavations, in the heart of otherwise hard, sound rock. Fig.15 is a sketch of one of these hollows ; and whatever may be the scale of operation, it is just such a form as would have been left had the sea extracted its contents. 120 Lieut. Nexson on the Geology of the Bermudas. To the unequal distribution of that carbonate of lime in solution, which forms ordinary rock on the upper parts of a section ; or druses and breccias, as it filters through the strata of red earth to the lower beds or to the caverns where it crystallizes as stalagmite and stalactite, I attribute, not only the caverns and sandflaws, but the pinnacled rocks almost equally common in the islands. The most remarkable groups are at Tobacco Bay, St. George’s Island (fig. 16), and at the North rock. I cannot but consider these as merely blocks, sufficiently impregnated with the dissolved car- bonate of lime to have resisted the attacks of the waters, with the same success as the ‘Base rock.’ Fig. 16. I apprehend that such caverns as those described in the preceding pages, are rarely found in any but calcareous rocks. The Grotto of Antiparos ; the caves of Torquay, Chudleigh, Plymouth, and Kirkby, as famous for their organic remains, as those of Gaylenreuth and others, in Ger- many ; the various caverns in Derbyshire; Peter Frazer’s Bear Den, near Picton, in Nova Scotia; the different subterraneous courses of certain rivers in England, &c. &c. ; are all found in lime- stones of various formations. It is almost trite to quote such instances to the general geologist ; but I have thus reassembled them, to show how well the series is terminated by the corre- sponding examples, which have supplied the materials of this section. WATER. Fresh water may be had in nearly all parts of the islands, provided the bottom of the well is not sunk under the level of low tide. Generally speaking, it is deemed prudent to be contented with twelve or eighteen inches of water, rather than incur the risk of rendering the well brackish ; since, from the porous nature of the rock, the salt water always filtrates through. At the naval wells below Mr. Langton’s, where large quantities of water are required for shipping, it is only taken between the half flood and half ebb, to avoid the brackish quality of water drawn at improper seasons; for all the wells, on the sea coast, are affected by the tide ; and more or less so those at a distance from it. Lieut. Netson on the Geology of the Bermudas. 121 Buitpine Mareria.s. The Bermuda rock is much whiter than the ‘ Bath stone.’ Blocks of any ordinary size and strength can be obtained. ‘The softer kinds, weighing at an average about ninety-five pounds per cubic foot, with a cohesive strength equal to only a quarter that of brick, are quite strong enough for house walls, where no great skill is required from the stone-mason. The houses are in general roofed with thin slabs of this material, which admit rain unless secured by proper washes. The harder sorts, like those of which the eastern half of Ireland Island is composed, vary in specific gravity from 1600 to 2560. In raising these, powder must be employed; and the usual tools for hard stone, in their conversion into ashler. In large masses, such as escarps, wharf walls, &c., it generally answers tolerably well; but it scarcely deserves a very high reputation, from the cracks which the unequal composition of the stone occasions, when under very heavy pressure. It is too pure to afford a good lime for external purposes, as it takes a long time to harden in thick walls. Equally good lime is manufactured from all descriptions of stone found in the island, regulating the choice by such localities as determine the economy of the burning process. Tue BanAMAs. Judging by hand specimens, from such reports as I have been able to collect, from their form as given by the best maps, and their position with reference to the gulf of Mexico, I think it highly probable, that the Baha- mas were produced by the same causes as those to which the Bermudas owe their existence. I have been told on respectable authority, that the red earth is to be found on the coasts of Florida. I have also seen specimens of Menacchinite from the shores of Virginia. ConcLupiInc REMARKS. Amongst the different speculations on the origin of coral groups, none are more common than such as would effect the whole by plutonic action; but I can see no proof that the islands, though once formed beneath the surface of the sea, were suddenly and subsequently elevated. ‘The peculiar arrange- ments of the strata, both in the mass and detail, and the constant occur- rence of the Helix, appear to be conclusive against the above theory ; and if dislocations of strata do occur, in only one instance (fig. 13, p. 118) are they to be met with to an extent like those, which I have seen in the chalk near Dover, and at Alum Bay, and due to undermining of the strata. In most notices on the Sunderbunds, it is stated, that islands are rapidly formed around any nucleus, such as the trunk of a tree in the bottom of the river, &c., which, reducing the velocity of the current, affords it the op- VOL. V.—SECOND SERIES. R 122 Lieut. Netson on the Geology of the Bermudas. portunity of depositing the sand; and this procedure must necessarily be of universal occurrence under similar circumstances. Once thrown down, unless carried off by a more powerful action than the original one, every fresh layer of sand net only increases the obstacle, but likewise the tendency to arrest the passing materials, until such time as a limit is attained by the increased, and consequently destructive velocity of the current in the thus narrowed channel. Assuming then any such initiative, as the head of a rock at the bottom of a sea in which enormous districts of zoophytes, &c., abound, as between 32° or 34° on each side of the equator, and from which dead portions to a con- siderable amount are incessantly torn off, and moved on with the waters until stopped by the rock, there will then follow the continued operation of the preceding law, of which this is the commencement. Zoophytes and other marine animals, of which the germs are passing on with other matters, attach themselves, as my own observations enable me to assert, indifferently to the first base they can find; and by their growth, re- production, and death, add to the stability and bulk of the colony. In this manner, I conceive* submarine mountains are constructed, and around their summits, the coral reefs. If the tides have their usual action and alternate direction, then the necessary form assumed by such a bank, will be like that of the average of sand banks and coral groups, elongate, and more or less ovate. Such germs as are dispersed in the water, on touching the bank, will on the whole collect in greater quantities on the declivities of the edges than on the plateau of the upper surface, over which they are far more likely to float away. Most zoophytes affect a vertical growth, and in this attitude have a tendency to add to the accumulations of the exterior fence, to the prejudice of the space circumscribed. Hence, I would surmise, is their generally annular form; and as to their somewhat uniformly level upper edges, that is of course regulated by the sur- face of the tides, above which the animals cannot for any length of time exist. The Bahamas lie in the bight of the gulf-stream, and the Bermudas on its outskirts; whether this is, or is not, the immediate parent of these groups, if we admit the above premises, then once above water, the wind is sufficient to complete districts of indefinite extent; and far larger than those which have formed the subject of this Memoir. Although the stone has been described as forming rapidly at Elbow Bay, I * In some places the reefs interfered with the works; and when destroyed in consequence, I never saw sufficient reason to induce me to alter my views as above stated. Lieut. Nexson on the Geology of the Bermudas. 123 can scarcely imagine the probable depth to which such accumulations are likely to be consolidated. As a tolerably general rule, the upper strata are less compact throughout the Islands than the lower ones ; but there is a con- tradiction to this, not only in the large and deep sound cliff from which our works at Ireland are supplied, where the bottom is as soft as the top, but in the still more remarkable instances afforded by the beds of sand, mentioned at pages 106 and 107, as lying just above high water along much of the south sides of St. George’s, and of the Main island. These sand beds lie under cliffs of good rock, sometimes fifty feet high. Why has not the rain water deposited the lime which it cannot but have dissolved in its passage amongst these beds ? I had a tube, two inches square inside, and six feet long, filled with sand, suspended vertically from a shelf. For two years water was kept dripping on the upper end, with no greater interruptions than those which might have occurred from an occasional want of rain; but on opening the tube at the end of that period there was not the slightest appearance of cohesion amongst the particles of sand. Want of opportunity for the water to eva- porate through the sides might account for this ; but such heavy exceptions to an extensively applied general rule, like that regulating the consolidation of the Bermuda rock, are very embarrassing. 3 a eS OP 5% . 7 7 ane . Be va Kee POY he eee page - ee ae. ee ag on dl tebe nanel * wad Nei a any m j , Abdon £ ot, bevel Trains COnglomera, tie Section on the Line AB. Ditton TS Laughton Bast PLAN & SECTION ofthe all BROWN CLEE HILL, SALOP. (oal measures Millstone Grit Old Red Sarudbstone | Jeale 2 Inches to one Mile . PD? D? Conglomerate » Cofn stone one Series, Ve _ Jan Astone Section on the Line CD. V1.—Notes on the Geology of the Brown Clee Hill, in the County of Salop. By ROMLEY WRIGHT, Ese. Employed on the Ordnance Trigonometrical Survey of England. [Read Dec. 18, 1833.] THE old red sandstone which forms the base of the Brown Clee Hill*, gene- rally dips from 5° to 10° to the east and south-east. Its lowest beds are re- markably soft and clayey; but through a large portion of the counties of Hereford and Salop, it almost invariably contains one or two beds of lime- stone, provincially called cornstone, and much used for agricultural purposes. The old red sandstone, as it rises towards the Brown Clee Hill, instead of continuing to dip towards the south-east, gradually assumes a basin-like form; inclining on all sides towards the centre, at an angle of about seven degrees. A bed of cornstone, about twelve feet thick, ranges almost entirely around the hill; and a second bed, also much quarried, occurs above it. From the circumstance of these two beds reposing in the form of a basin ; and from their proximity to the superincumbent coal deposit, they appear to have been considered as representatives of the mountain limestone: but 150 feet of the old red sandstone lies between these cornstones and the coal mea- sures, and passes on the western side of the hill into a regular conglomerate. Immediately upon this conglomerate, the coal formation reposes ; its greatest thickness being about 150 feet; and the dip of the beds conforms to that of the subjacent strata, or towards the centre, at angles varying from 3° to 5°. The outburst of its lowest bed, locally termed the “ Bottom Rock,” is marked by a soft white clay, which freely throws out springs of water. This “ Bottom Rock”’ has but little quartz, and in grain resembles whitish oolite. ; Coal has been discovered, to the amount of six feet in thickness, distributed in three different veins, namely, The Three-quarters Vein ... 1 foot 7 inches. Phe Batty, Vetiyi3% «ja - ts: 2 feet 6 inches. And the Bottom Vein ...... 2 feet. When worked it is chiefly by means of a windlass ; but the beds are neg- * Plate VII. 126 Mr. Wrieut on the Geology of the Brown Clee Hill. lected in consequence of the superior quality of the coal which is found three or four miles distant, in the Titterstone Clee. There are three separate faults, ranging nearly parallel to each other in a north-east direction*. The first, which is but a few inches in width, throws up the coal veins about three feet on its south-eastern side; the second throws them up about five feet; and the third, which ranges near the centre of the superincumbent mass of basalt, called the Clee Burf, is about thirteen yards in horizontal thickness, and throws up the measures nearly nine yards. The “ Wall,” as this last fault, or the basalt which accompanies it, is termed by the miners, is so hard as to require to be blasted, no tools which they possess being able to work it; but the coal in immediate contact with the basalt, is represented as not being in the least charred. It may be followed on the surface for about 400 yards, and in the prolon- gation of this line, the measures are found in abrupt and unconformable contact with the old red sandstone; the lower beds of which also lose their continuity, as may be observed above Pickleton Grange. The coal field of the Brown Clee Hill, comprises nearly two square miles, and, owing to an inosculation near the middle of the hill, its outline much resembles a figure of 8 (see Plate VII). Within its area are two isolated caps of basalt, forming the highest points of the hill, namely, the Abdon Burf, exceeding 1800 feet above the level of the sea; and the Clee Burf, which is about 200 feet lower. The basalt of Abdon Burf appears to be about 140 feet thick, but it has very extensively fallen down, and now appears only in the form of large blocks of stone. To the eye the basalt precisely agrees with that of Rowley Regis, near Dudley ; and is much finer grained than the basalt at Earls Shilton in Lei- cestershire. From the large fault in the coal measures, specimens of the rock were obtained, similar to the overlying mass of basalt. After the most careful and repeated examinations, no traces of a columnar arrangement could be per- ceived in the basalt of the Brown Clee Hill. From the almost inaccessible nature of their situation, each of these two hills was formerly occupied as a for- tified post, in the same manner as the Titterstone Clee. At Bouldon, about two miles distant, there was formerly an iron furnace, and it is generally believed that the ore was obtained from the Brown Clee Hill. Immense heaps of refuse are yet seen, from which the metal has been but very partially extracted. It is certain that iron ore is associated with this coal deposit ; but its site is not sufficiently known to admit of being introduced into the accompanying plan ; for the same reason I have omitted to mark the outburst of the beds of coal. * Plate VII. Map and Section E. F. ji MM VII.— Observations on the Geological Structure of the Neighbourhood of Reading. By J. ROFE, Jun., Esq. Communicated by Rogerr Hunter, Esq., F.G.S. [Read Feb. 26, 1834.] I HAVE the honour of presenting to the Geological Society a few specimens illustrative of the geology of the immediate neighbourhood of Reading; and I may, perhaps, be permitted to accompany them with a short account of the beds in which they were found. The substratum of the neighbourhood of Reading is the upper chalk, abounding in fossils and flints, many of the latter containing sponges or other organic remains, and very many having cavities lined with crystals of quartz of various colours, or with mammillated chalcedony. The chalk on the north-west side of the town, rises abruptly a short distance from the Thames, forming a range of hills; but on the north-east more gradually, and the hills are farther from the river. The high land which, in Reading, separates the Thames and Kennet, rises suddenly from the Holy-brook (a tributary of the Kennet), but falls gradually towards the Thames from the Basingstoke Road to Caversham Warren. The highest part of this ridge is covered by gravel, under which are numerous beds of sand and clay, be- longing to the plastic clay formation. In the Thames valley the chalk is principally covered with the gravel over which that river flows. To the south of the town is also a range of high land, bounding the Thames and Kennet valleys ; and, like the ridge between the two rivers, belongs to the plastic clay ; while on the western side, in the Kennet valley, several brick- fields are now worked through all the strata of that formation to the chalk; and it was in these beds that most of the specimens were found. In the Katesgrove field, wrought for considerably more than a century, the clay for bricks and tiles is procured from the side of the hill above the general level of the field ; but the chalk, used for lime, is obtained from pits sunk be- neath it, though never to a depth exceeding fifteen or sixteen feet, as the water prevents deeper excavations. The upper part of the chalk, for about a foot, is in a very singular state. It can scarcely be called chalk-rubble, but 128 Mr. Rore’s Observations on the resembles wood which had been penetrated by the teredo, and the tubular cavities afterwards filled with sand. Covering this is the bed of oyster-shells, twenty-seven inches thick, but divided into two parts. In the lower, which is thirteen inches thick, the oysters are imbedded in a brown clay, and are much larger than in the upper, but are more difficult to procure perfect and to pre- serve, as they rapidly fall to pieces when taken from the bed. In the upper, which is fourteen inches thick, the shells are found in a bed of sand, contain- ing minute green particles, and occasionally small green nodules and flints, some of which are rolled and some angular. In both beds the shells are accompanied with a considerable quantity of fishes’ teeth. Resting on the oyster-shell bed is another of clay, nineteen inches thick, parted by small seams of crystals of selenite; and on this are five feet of quartzose sand, near the upper part of which is a bed of ochreous nodules, from two to three inches thick, which yield an excellent pigment. The strata above this, as far as I can observe, correspond with the statement in Dr. Buckland’s Memoir*, excepting that about six feet from the surface of the hill, is a thin bed of shells not noticed in that paper, nor in a passage in the Outlines of Messrs. Conybeare and W. Phillips, (p. 42.) when speaking of this place ; or at page 39, where it is said, ‘‘ There is not the smallest trace of animal or vegetable remains in any of the strata of this formation at Read- ing in Berkshire, except in the green sand +.” In this field, where the bed is so near the surface, it is considerably decomposed and may easily escape notice ; but in other places in the neighbourhood, the matrix in which the shells are imbedded is sufficiently hard to take a tolerable polish. The same beds have been worked through to the chalk, at spots on the other side of the Kennet, and nearly in a line with the Katesgrove field. They contain the sand with green particles and rolled and angular flints covering the chalk, as at Katesgrove, and occasionally oyster-shells and teeth. In making the new road into the town, on the eastern side, over the corpora- — tion property, the upper part of the chalk has been exposed and is covered with sand and rolled pebbles, but there are very few of the green particles, and neither teeth nor shells. In this spot the chalk rises very near the sur- face, and the sand with the pebble bed is very irregular in its thickness, and is covered with the vegetable earth ; but in the upper part of a field on the side of the Oakingham road, immediately under the soil, are thick beds of gravel, containing chalk flints, some of them very little rolled, and abundance * Geological Transactions, Ist Series, vol. iv. p. 278. + In the section presented in July 1837, the bed was twelve feet below the surface, and about ten inches thick. Geological Structure of the Netghbourhood of Reading. 129 of organic remains, principally Echini and Terebratule in flint. In the pit on the Oakingham road bones and teeth of the elephant have been found. To return to the thin bed of shells near the surface at Katesgrove. I can- not discover that it has been found on the north-western side of the town; and it probably crops out at Katesgrove. In Clackman’s field, about a quarter of a mile south-east from that pit, in sinking a well the bed was found in a very perfect state about four inches thick, and about thirty feet below the surface ; and the shells, though in a very brittle chalky state, were firmly concreted by sand. The best of the specimens are deposited in the Mu- seum of the Reading Philosophical Institution. In these specimens, some of the shells are lined with crystals of iron pyrites and some with crystal- lized carbonate of lime. This stratum has also been found at several places south of Reading ; and at Woodley Lodge, the residence of James Whitle, Esq., about three miles east of the town, the thickness of the bed is about an inch. It was found about forty feet deep, in sinking a well, and immedi- ately under it a supply of indifferent water was obtained. It is also recorded ‘‘that in an unsuccessful attempt to procure coal at Hose Hill’ (in the parish of Burghfield, and on the south bank of the Kennet Valley, about four miles and a half south-west of Reading) “a few years ago, a bed of cockle shells, firmly concreted with sand, was discovered about twelve feet below the surface*.”’ This, there can be little doubt, is the same bed as that found at Katesgrove and at Woodley. Before I conclude I may be allowed to notice another fact connected with Reading, which has been verified by repeated observations and is well known by the well-sinkers. All the wells in the town (excepting those supplied by soakage or land-springs, which are mostly of bad quality), whether * Since the foregoing account was written, I have been favoured with a letter from Mr. Wheble, of which the following is the substance :— The blue clay prevailed for about forty feet, when the concrete of shells and clay appeared. On breaking through this mass, water was found in a small stream. The men then continued to sink through a clay streaked blue, red, and white, to the depth of ninety-five feet from the surface. Boring was then commenced and continued about thirty-five feet deeper, always through the second sort of clay, but with more of sandy particles occasionally, without meeting with any further supply of water than the one above mentioned. In the first forty feet many oysters, &c. were found, not concreted, but disseminated in the clay. One large rounded flint with several oyster-shells firmly attached was brought up. In the course of the sinking, the air in the well was very sulphureous and disagreeable to the workmen, and for a considerable period the water was powerfully sulphureous and chalybeate. The supply of water seems to have increased of late years, but it never rises above the level which it oiginally attaind. VOL. V.—SECOND SERIES. Ss 130 Mr. Rore on the Geology of the Neighbourhood of Reading. north or south of the Kennet, even those within thirty yards of its banks, are regulated by the Thames, rising and falling with the river, and not being at all affected by the Kennet floods. This may be accounted for by the Kennet flowing through a bed of tenacious clay, whereas the Thames flows through gravel immediately over the chalk, into which all the wells (except soakage wells) are sunk from ten to twenty feet. The depth of the wells from the surface varies of course according to the situation, some being from ninety to a hundred feet deep, others not more than fifteen to twenty. The following is a list of the shells alluded to by Mr. Rofe ; and it appears that the upper bed contains the fossils of the Bognor Rock. The Upper Bed. Cytherea incrassata .......... Min. Con. Tab. 155. f. 1, 2. also Bognor. Pectunculus brevirostris ...... ———-— Tab. 472. f.1. Ibid. Modiola elegans...... wists wee —_————. Tab. 9. Ibid. Dentalium planum.....+.++-+++ —— Tab. 79. f. 1. Tbid. Ampullaria sigaretina ........ ——-——- Tab. 284. low. fig. _ Ibid. Katesgrove Oyster-bed. Ostrea Bellovacina....sesesece Min. Con. Tab. 388, f. 1, 2. pulcher ...... covecces ———— Tab. 279. ——— POHCL ici taivietelninisteimicts sic ae SS eee Tab. 252. f, 2. Geol. Trans, 2¢ Serics Vol.V_PL. VIM. Oh LED EL EA IL LOL OGL aa yhey Senn Lae ea SN as gt i ev is {wee on SS ys cm mt: 9B fo ee ee ea TT) crt “D.C. Sowerby fe 1b. Ue Lda = 0 Geol. Trans. 2¢ Serres V. 1t TDC. Sowerby, tec FLIgl J VIII.—Observations on a Well dug on the South Side of Hampstead Heath. By NATHANIEL THOMAS WETHERELL, Esg., F.G.S. [Read June 4, 1834. ] A WELL dug at Lower Heath, Hampstead, in 1833, yielded a considerable number of fossils, and in consequence of the London clay having been cut entirely through, and the plastic clay to some depth, it became an object of interest to the geologist. It is well known that a great part of the heath is covered with sand, which has been described as belonging to the upper marine formation*. At the southern part, however, the sand gradually disappears, and the clay is met with on the surface, and it is at this part that the well was made. The following is a section of the well. ondomGlay 2... Mite eee sn 285 feet. IRGGIEN Sarees tiv cre tates a od ole stele. 5 Plastic Glavine: 6.5 ais700/«'= a's vie) ois 40 330 feet. The London clay for the first thirty feet, was of a loose texture and reddish brown colour, and contained a good deal of decomposing pyrites and selenite. From 30 feet to 200 feet it varied in colour from blue to dark brown, and contained many septaria. The lower part was as usual very sandy. At 260 feet there were a few fruits and seeds, the former being of the same descrip- tion as fruits found at Sheppy, and the latter being similar to the seeds ob- tained at the Highgate Archway. I have a cylindrical piece of pyrites, radia- ting from the centre, very like that which occurs in the chalk. I mention this circumstance, because the pyrites 1 had hitherto met with in the London clay were irregular nodules, or flat masses, without any radiation internally. It was found 265 feet from the surface. Between the last-mentioned depth and 285 feet, the bottom of the formation, the clay abounded with vegetable re- mains in a compressed and decomposing state. The fossil copal, or Highgate resin, | believe was not met with. * Outlines of the Geology of England and Wales, p. 14, 1822. s2 132 Mr. WetHERELL’s Observations on a Well dug on Hampstead Heath. Between the London and plastic clays a hard rock, five feet thick, was bored through. It abounded with green, siliceous particles ; and contained numerous shells, disposed in layers, but the greater part were in a very chalky, decomposing state. A list of the organic remains obtained in the London clay, is given at the end of this paper; and on perusal it will be found to contain many fossils which have been met with in distant localities of the same formation, as Sheppy, Bog- nor, and Barton. 1 mention this as an important fact, but by no means as a new discovery, since Mr. Parkinson states in a most able paper on the Strata and Fossil Remains near London*, that at Kew and at Highgate Hill, fossils had been found of the same description as those of Sheppy and Hampshire. In the Hampstead Well were obtained some interesting remains of the class Radiaria. The portions of Asterias in my possession, consist of a considerable number of ossicule. The largest, being granulated, probably belonged to the sides of the animal; and some of the smaller, without granulations, to the middle or inner part. The ossicule were irregularly distributed on the surface, and within a piece of clay, but by immersing the mass in water, I was enabled to save the greater part. Of the genus Pentacrinites, I have remains of two species; one is evi- dently described by Miller in his Crinoidea, as having been found by the late Mr. James Sowerby, at White Conduit House, Islington, &c., and is thus spoken of : “These columns much resemble in size and shape those of Pentacrinites basaltiformis, but have the angles more rounded. From their exhibiting no marks of muscular corrugation at their ex- terior surface, and the points being of uniform thickness, I apprehend the fragments before me to have been full-grown columnar portions. I wave distinguishing it as a species, not having the means of furnishing a specific character; yet, should it prove such, I should propose for it the name Pentacrinites subbasaltiformis.” p. 140. I have a specimen of spatangus which is strongly marked, but very fragile, and was found at the depth of 250 feet. The same species was also found at the Highgate Archway ; and the late H. H. Goodhall, Esq., informed me he had in his collection one from the London clay at Barton. It is worthy of notice, that on comparing Terebratula striatula obtained from the well with specimens found in the chalk, there was no apparent difference f. * Geological Transactions, Ist series, vol. i. ¢ Though this fossil is abundant in the London clay at Sheppy, and in the excavations for the Birmingham Railway, near Chalk Farm, yet it has been rarely found in the English chalk. Aug. 1837. Mr. WerHereELt’s Observations on a Well dug on Hampstead Heath. 133 In the list appended to this notice are ten new species belonging to the class Conchifera*, and several species of Microscopic foraminiferat. In Plate VIII. fig. 2. 2.a., are represented two curious fossils. One of them is cylindrical, externally smooth, and shining, and is composed of dark brown spar; radiating internally like the Belemnite. The other is quadrangular, but with the angles rounded, and possesses internally the same structure as the first. Both effervesce strongly with muriatic acid. They are considered by Mr. J. De C. Sowerby to be remains of Pennatule. The shells procured from “the rock” between the London and Plastic clays, are as follows : Rostellaria lucida, Natica glaucinordes, a Nucula, Pano- pea intermedia, Cardium nitens, Venus incrassata, and a few casts apparently of the genus Pleurotoma. Lignite and scales of fishes also occurred. In some parts of the rock, were layers of calcareous spar, the surface of which was beautifully studded with crystals of pyrites. ‘The bed contained a great many rounded flint pebbles, some of which were in a decomposing state ; and a few of the same pebbles were imbedded in the lower part of the London clay at the depth of 230 feet. I believe it is not very usual to find a bed of sandstone between the two clays, but from its contained fossils, as the Panopwa inter- media, &c., there appears some analogy between it and the Bognor rock+. The plastic clay presented several varieties of colour, as red, grey, white, and yellow, variously intermingled. I examined it very closely without find- ing the slightest trace of organic remains. At the depth of 330 feet, the workmen arrived at a bed of sand, of a green colour, containing small flint pebbles, and at this part soft water was obtained, which gradually rose to within 200 feet of the surface. A steam engine is about to be erected on the spot, but whether an adequate supply of water will be obtained without the necessity of boring into the chalk, remains doubtful. * Plate VIII. + Plate IX. t In a paper by Mr. Richardson, (Geological Proceedings, vol. ii. p. 79,) much sand and green earth are stated to occur in the London clay near Herne Bay; and in Mr. Rofe’s paper on the plastic clay of Reading, a rock is described at the top of the plastic clay. See p. 128 et seq. of this volume. I have also a specimen from Egham. ‘uoyieg pue = *prqy *piqy *plqy "PIqL *pIq] ‘puaynog pure -piqy “L0usOg pure ‘pIq] ‘pIqy ‘piqy *plqy ‘Addayg pure ayeSysipy -aurysduepy ‘sanquoyorag *qitomspue A pur [[eyxXne A uses \ -9q pue ‘uoySur[sy ‘asNOFY JNpuUoD a71y MA ON "PIE “PII Loe PET ‘Addayg pur ayes y Spy Dihy Vowteg "10US0g ‘27g ‘AyVSYSIPY ‘pusy Nog ‘19jsuI se ‘aye Sysipy ‘Addayg ‘puouryary ‘UO Sus] ‘OsNOP] WMpUoD ast Ay Ivan ‘ayeSysipy *a19Y MAS] 134 Mr. WetHERELL’s Observations on a Well dug on Hampstead Heath. CP at eiare eae eee = * * 82 NORIO *T *[OA Ol ‘bE J oie aie ence sa Saeed EI 94 8 “F °60G *G¥ "ES “[OA eee sere eerseeeeeeee 4 ie | ‘LL J ‘HIA ‘ld ‘Aqiamog “G6L *GeI ‘SG *[OA 8 ‘F °G6L “GPI °S “[OA SF HEg ‘qei"g "JOA P 6‘ ‘J °F99 “qed “9 “JOA [TJ °LG "Qed “T “JOA “UOd ur “OLY "6 J “TILA ‘Id ‘Aquemog sere ee HT qe |] [OA "UOD “UIT, reeeeseseg IITA ‘Id ‘Aquemog oT FST “Ge "S “or "er" OTS "qed “yh ‘Joa — eeeeeee “OIG *qvy ‘P *[OA ‘uory “Ulf - - eeeteoe JO i ‘TIIA ‘Id ‘£qalaMog 61h *Qe} *G “OA GOL *Qet *T “TOA "WoD “UIT eeeeee 6 J = @ | ‘Id °G ry "HIA ‘Id "#4 Kid “*b J TITA ‘Id THA ‘Id Cort oded ‘vaprourty s,t9]]171) ‘8 J IIIA ‘Td “LS TIA ‘ld (S10quoiqg) "1s ‘J ‘suiduoudg puv saoualajoyy (-AinjQ wopuorT) % a et enon yy snjnounjoodg eOlY wuimipaeg snugA SNUIXY a}IvSy eulonyT bet IAF BlNq109 vedourg opaiay, eindasag jsadrofjog euayy hg snovisy qgoury SOWULLN8}U9 J snsuvyedg Svlloysy epnjyeuuag —_—— |umyyAydousag PRE LICRCHECANY ‘4 tlyurqiomog ity SILOS ne vULTUTU ml eyeyur ‘2 saproyepsAue e snjessnoap “4 eqyoduat “s suo} 23 suojtu “% — eyeLgsmua} *d ey esseIoUl “0 snjepnsue 2 eyeoni Ms H[eqpoot) #) suapuojds 2 eyNjoOAdt “ vIpaulsozUut # eeynvusjue “4° esseio 7) "a eyeqieq i) ) satoads ¢ “st IIqaMog SIUIOF[eseqqns 0a 4 se "s mr) *satoadg eiodaljag vIysnpy *snuey “poasdunzy “Ymaz] Lanoy yo agg V Suyuis ue hojQ uopuoy ay, we punof smpuay nunsic BIIJIYUOD saplpauuy epadiuiig — eaoejsnig BLIvIpey vjAydooz *SSPIO “Pra *OJVSYSIP] "U0}V *jauun [, uo}SuT[s] ‘kddayg pure ‘prq] Bt Is oe Moye pus Id Pi MONE PEE. PIT oat *‘syooy tousog pure ‘Addayg = ‘prqy api pCO Ne ate ‘Addayg pur ajesysipy *10us0g ‘aouRLy pue ‘uojIeg ‘ayesysIpy ‘ax ‘Addayg ‘puayynog “uo}suIqqnig *syivg opAP] pue puowmyoryy ‘Addayg pue = -piqy ‘1ousog pue ‘piqy -ayeSy sip] 029 ‘TM YAeq puowyony ‘1ousog Mr. WetuERELL’s Observations on a Well dug on Hampstead Heath. 135 v fq poysmBunstp are sayauea pue soroeds Mau oy, 08 ‘J VION * GI J ‘VMRT[AISUD ‘81 OF ST Y ‘eROY eee errtseeseseeseoee 6L ‘J ‘LILA ‘Id ‘Aqzemog eke ceiniemie eleisie Tet TOG nia Ton ereeeeereee 8°9‘F°SOT *qeI °S *[OA sila Uleleilplefere 8ST "16 "qe "| *[OA soinsy szaddn aaayy "9 *qe3 *T [oA eoveveeeesne Gp } “Gg °qey °[ "JOA e eoneeeevecece I6¢ *qe3 “} "JOA eeeeeveeeaespeord TL °qe3 oT *[OA ‘uoy “Ul, "SL J TILA ‘Td ‘Aqremog ¢ J °LL9 Ge °9 [OA — S B'S ‘LJ 96S “GeI *g "JOA UOD ‘ur (oT J ‘eurynursaeypy {pF geuMorpuory SO] pue 6 pure g yy ‘euyNONIY * 1076 TXT Id “Puesopon vlauasd ay} 0} Suojaq varayruruesiog oy, 4 "XI PUP “TITA ‘Id 843 03 aouarazar ‘uoulutos Arana 9°a $oaea AOA *u°a $UOWUIOD *a {a1 SUM [ISSOJ OY} FYI SOYIUSIS 4 y a oh) “4° wmnsnya1 7) e[NosnrAey] “b eje[NUs oY) epiony 7) eyeUlIeo 9) snqeouryiay ch) sI[rxou “sb “L winjnjed ‘4 *4a *esopun L eye[nonar ‘2 'aSISUdTIOUSOg "4 casiysduiepy ay} 0} snosojelue satoeds aay J, ee ereeee LI ‘J "ITIA ‘Id ‘fqiamog ee Re J ‘OL *qe} *T "JOA I ‘ Ore 6. "qe 4 *[OA oeeeer ts g qu3 °] “TOA eee Bey “GL -qES “T [0A eeeevee CoP °Q23 °G *[OA G “bE "JF '9SS “qeI “9 “[OA creetes Gg "Guy “GOA SS ‘LF G19 "qe4 "9 “Joa ce Caer "OL J TILA ‘Td ‘fquemog sae) oe here, <0) fi OM —. os oe ey Bg “Gey “108 reeeeets 9-83 *T ‘fou 6 °Qe} *T “[OA *UOD “UIT, “PL J ‘TINA ‘Id ‘Aquemog "ST ‘J HIIA ‘Id ‘(sekeysoq) oe ae . e ° WON "UIA eeoaeeeseeeens or} sdaour “sh suastu ‘2 unjessesoUl ‘2'a Saplouloney|s “sb sinua} “L BIvoul] oy} RNyeLys “L snou109 7) snjeordnp *t vaoeaXkded £°Q eyenoie om) eIpaut “4 stuyye “6 essoidap os) suesoja Ps) essaidui0o “100 *eyelI}s jo ajvyed ‘eiey qj903 ‘sntenbg fsnjne yy wnpnAag Bldelpaouers) RMON y BIIL][OISOW vlepisseg xoinj] enikg eLUI0}OINIT J wintiejog BLIe[eag Snjaulda A winiyeju9q eae nN eynsury eIMouy elnjzeiqaiay, u9}09q RNA euurg elOIROn y[nonyy SoOSIq HH Hil AIT vlaytyouoy ‘Gaba Description of the New Species and Varieties figured in Plates VIII. and IX. By Mr. J. De Carte Sowersy. Desmophyllum. This genus has been established by Ehrenberg, for a portion of those corals hitherto placed among the Turbinolie. The type of the genus given by Ehrenberg is the Madrepora dianthus of Esper, the Caryophyllia dianthus of De Blainville. It is distinguished from Turbinolia by having been attached at the base; and from the Cyathina of Ehrenberg (Caryophyllia cyathus), by the lamelle being fasciculated. Pl. VIII. fig.1. (a.) The termination of the plates magnified. (0.) Section of one segment. Pennatula. This fossil resembles the bony axis of P. phosphorea, (Lam.), which occurs recent on the British coast, and has the same structure, and the form of the section also varies from square to round, in the same bone. Pl. VILI. fig. 2. (a.) The natural size. (0.) Magnified. Pentacrinus subbasaltiformis, (Miller). Pl. VIII. fig. 3. (a.) The principal stem. (6.) The side arm, nearly cylindrical and extremely long. Pentacrinus Sowerbii, (Wetherell, MSS.). Joints unequal in diameter, 5-lobed, with two obscure tubercles on each lobe of the larger joints. Pl. VIII. fig. 4. Polliceps? Posterior and lateral valves. PI. VIII. fig. 5. and Pl. IX. fig. 2. Tellina splendens. Ovate, convex, highly polished; beaks central, small; posterior extremity pointed, bent to the right. Gregarious, occurring in thousands in Septaria. PI. VIII. fig. 6. Lucina Goodhalli. Subglobose, nearly smooth; anterior slope concave; lunette broad, flat, sunk; pos- terior slope convex, with one narrow and one broad groove on each side of it, meeting near the edge. The young shell is sometimes very globose, at other times rather flattened. Pl. VIII. fig. 7. Venus tenuistriata. Oval, gibbose, marked with nearly close, concentric strie; beaks prominent, nearest the anterior extremity ; lunette rather broad, pointed. PI. VIII. fig. 8. Arca nitens. Transversely oblong, convex, smooth; anterior portion small, rounded; posterior subcunei- form ; front oblique; shell thin. Some specimens have a few punctures, in which character they approach the next species. Pl. VIII. fig. 9. Arca impolita. Transversely oblong, very convex, marked with longitudinal rows of punctures; anterior portion small, rounded ; posterior rounded; front parallel to the hinge line; shell thin. It approaches A. cucullaris of Deshayes, vol. i. p. 206, pl. xxxiil. figs. 1, 2, 3; but differs slightly in form, as well as in the teeth being all transverse. PI. VIII. fig. 10. Nucula Bowerbankii. Elliptical, convex, smooth externally, striated within; anterior extremity obliquely truncated, the slope filled by a large, pointed, nearly flat lunette; edge toothed; impression of the abductor muscles shallow. PI. VIII. fig. 11. Nucula Wetherellii. Suborbicular, transverse, gibbose, smooth; extremities pointed. beaks nearly central ; margin obtuse, edge toothed. The radiating structure of this Nucula, common to other species of the genus, is very conspicuous ; but the inner surface is not striated as in N. Bowerbankii. Pl. VIII. fig. 12. Nucula striata, var. (Lam., Ann. Mus., tom. vi. p.126., tom. ix. pl. xviii. fig.4 a., b.—Deshayes, vol. i. p- 236, pl. xlii. figs. 4, 5, 6.) This variety is less equilateral than in Lamark’s and Deshayes’ figures. PE VIL. fig. 13: Nucula compressa, Ovate, compressed, smooth; anterior portion very small ; lunette wanting. Pl. VIII. fig. 14. Avicula arcuata. Transversely ovate, arched, compressed, smooth, thin; nearly twice as wide as long ; posterior ear large. PI. VIII. fig. 15. Avicula papyracea. Nearly orbicular, much compressed ; concentrically waved; ears small, unequal. An extremely thin pearly shell, sometimes assembled in considerable masses. PI. VIII. fig. 16. Dentalium anceps. Slightly arched, longitudinally ribbed towards the apex; one rib on each side of the arch prominent and sharp ; smooth towards the aperture, which is round. Pl. VIII. fig. 17. Scalaria undosa, var. (Min. Con. tab. plxxvii. fig. 4). This differs from the variety figured in Min. Con. only in having the coste less waved. PI. VIII. fig. 18. Ovulum retusum. Egg-shaped, short, transversely striated. This differs from Ovulum ovum, the young state of which it very nearly resembles, in being shorter. We have not seen it with an inflected or thickened edge to the lip. Pl. VIII. fig. 19. Cytherina barbata. Transversely ovate, gibbose, smooth, with several spine-like processes at the extremi- ties. Pl. EX fiesy di. [ .137- J IX.—Observations on the Strata penetrated in sinking a Well at Diss, im Norfolk. By JOHN TAYLOR, Esga., Treas. G.S. [Read June 4, 1834.] SOME interest has been excited by an attempt to bore for water at Diss in Norfolk, as no similar experiment had been made, and as the town had hitherto been ill supplied with water of good quality. This attempt was un- dertaken by my relative Mr. Thomas Lombe Taylor, for a brewery in which he is concerned ; and as it has proved to be a successful experiment after con- siderable perseverance, and has ascertained the thickness of the chalk in that district, where it was hitherto unknown, it may be useful to record the particulars. | A well had been previously sunk to the depth of fifty feet, all of which was through clay, but sand was met with at the bottom, which yielded an imper- fect supply of impure water ; and as it was found extremely difficult to sink in this sand, cast-iron pipes were driven through it, which reached the chalk at the depth of 100 feet from the surface. At this point the boring commenced, and proceeded through 100 feet of soft chalk without any stone, then 100 feet of chalk with flints at the distance of about a yard from each other. The next 100 feet were less flinty, but the flints which were found, were of a larger size than those above them. Having attained a depth of 400 feet, and some apprehension being then entertained as to the probability of succeeding in penetrating the chalk, and of obtaining the object of the undertaking, I was asked to advise as to the prudence of going on with it. No opinion could be given as to the probable thickness of the chalk in a part of the country where it never had been proved ; but it was, at the same time, certain that if it was passed through and the sand beneath it could be reached, a plentiful supply of good water would be obtained, and would probably rise to within a moderate distance from the surface. I, therefore, encouraged my relative to persevere, and the boring was continued to the depth of 615 feet, where the tools sunk rapidly for about five feet, as if there had been a cavity ; but this was probably owing to the sand being put into motion by the sudden rise of the water through the VOL. V.—SECOND SERIES. T 138 Mr. J. Taytor on a Well at Diss. orifice which the tools had made. The water rose rapidly to within forty- seven feet of the surface, where it stood when I received the account. The stratification determined by the boring appears to be as follows :— SLAG ites cis = sos 2 0 von © 0 bial tleje pai sian cieteay eB nte Ssevccssee 50 fect, Sand ..... 5555, WOE oo ns ks Re soee 50 Chalk withont flints, soft and marly........000.s.s:-mess “nee done 100 Chalk with flints in layers of single stones, distant about a yard from BEEINTEED ys 6.0 ooo oo 00 10 0 ule y nite aMent ie meiaintelais atthe ene E 330 Grey chalk, with now and then a layer of white chalk, free from flints.. 60 Light bright blue chalk, rather approaching to clay, with white chalk EETIGS Fevs ickc.ic\ so o\0 0 6 ese eve eel nip teyptbin te are latatedeiateteliaterate lelsietetatsteretarstetetete 20 SHTIEL ESATA crera-s cei s bo vid ct\pieteeietetektan oes eld deb betes sists oibiele aes 5 615 feet. It could not be ascertained whether there was any organized matter in the chalk, as the tools ground everything to powder. 138 Mr. J. Taytor on a Well at Diss. orifice which the tools had made. The water rose rapidly to within forty- seven feet of the surface, where it stood when I received the account. The stratification determined by the boring appears to be as follows :— OA So 5 555055 (SAN OSC Sano aan rae ier aioe cocceseee 5O feet. Sand ...... See MET Cis ie cieivioie's «ss 0 0.0)s aimin a pias aisle ales die's/ecas 50 Chalk without flints, soft and marly.........seeeeeeceeees ee 100 Chalk with flints in layers of single stones, distant about a yard from Pete SC EEMME DS SU iris eis se © a)~ vc 4 ac oo oe u's» aiivivinia Binis wloieaeaiainia 330 Grey chalk, with now and then a layer of white chalk, free from flints.. 60 Light bright blue chalk, rather approaching to clay, with white chalk BEONES | aielelslais''s{ocls\2\s 6 's)c Sie teiotite yin oJolle/o:0.0 seers \e ov cl eiele teins henenanere es AL SATE SOM ear ePeN eT etd cle pis loi eye Siece o/c. 5 ole hoh bie 0.0 olalathhs oiehihare hie ite 5 615 feet. It could not be ascertained whether there was any organized matter in the chalk, as the tools ground everything to powder. 1) A IN EMT SS a Blackpots Banth Me PL round a s (Blackpots to Bart? BR t A N Seale one Dpalre i in t and Gea MM BE Bap h OMA Clareh *} = 3 § DBO iy & jehvutince Map Inch to a Mile Ce Liane OL P. Bart? SiS ieTe ton of Camric Bay Pp. tO. 15 N; ; : Tinton Viva fiudt Vitrified towe 260 4% OM Kal =, Sendetone 6 Dark clay similar te thet at MDulf & Blackpote in which Wins tossile have been tiund Jeetons Map (orizontal Seale 4 inches VWertical Seale 4) Diluviumn ordrin | Te more numerous the dots Red Conglonerate | OM Red. Sandstone ees Sdhistoce Rocks De 2 St = 1 Mile 800 fet. 4 Mile No S. new Alors near 5 Atfforsk part of aden Mill ee Gamrteé From N p. 145 Straa tr with Tepy Gamrie Via 3 \Z Fouto file. Tap ee | the thicker the deposit Anticlinal Lines ee = Dip —s Strike f 139 4 X.—On the Structure of the Neighbourhood of Gamrie, Banffshire, particularly on the Deposit containing Ichthyolites. By JOSEPH PRESTWICH, Jun., Esq., F.G.S. [Read April 8, 1835.] Inrropucrory REMARKS. THE Ichthyolites of Gamrie were first brought before the public by Mr. Murchison, but, having been prevented from inspecting the precise locali- ties, he contented himself with pointing out their existence ; and obtained from Mr. Pentland, an account of their zoological characters*. M. Agassiz, during his recent visit to England, was much struck with the peculiar forms of these Ichthyolites, and expressed his opinion, that they belong to a deposit more recent than that in which the fossil fishes of Caithness are found, and has been shown by Messrs. Sedgwick and Murchison to pass down into strata of the age of the old red sandstone. Impressed with the importance of deter- mining precisely the age of the strata containing the Gamrie fossils, and unable in consequence of other geological researches to do so himself, Mr. Murchi- son, on finding that I was about to visit Scotland, suggested the inquiry which led to this memoir. The result is, that the age of the fish-deposit, as de- termined by the position of the strata, coincides precisely with that suggested by M. Agassiz, from the zoological characters of the Ichthyolitesf. These fishes were first discovered in the summer of the year 1826, by Mr. Christie of Banff, and Mr. Dockar of Findon, who, while exploring the bed of a small brook, which flows through a narrow ravine and empties itself into the Bay of Gamrie, observed numerous, flattened, calcareous nodules frequently containing remains of fishes. ‘Tracing these specimens up the brook, they arrived at a thin bed of bluish clay, which inclosed the Ichthyo- lites. In my inquiries to ascertain the geological relations of this stratum, I have to acknowledge the attention and civility of the above gentlemen. * Geol. Trans., 2nd Series, vol. ii. p. 363. + See postea, p. 146. T 2 140 Mr. Prestwicn on the Structure of EXTENT AND SurFACE*. The Bay of Gamrie is about nine miles east of Banff. The country is hilly, bleak, almost destitute of trees, and unenclosed. The extensive slaty districts, where not overlaid by drift, generally form moors covered with heather and furze ; but where partially cultivated, they yield scanty crops of herbage ; while the red sandstone, conglomerate, and drift constitute the arable lands. High and picturesque cliffs of slate rocks skirt the shore, forming numerous small headlands; between two of which, namely, Gamrie and Trouphead, is the small fishing hamlet of Gamrie or Garmstone (Pl. X. Map and Sec. No. 2.). The breadth of the bay is about one mile and a half, and its depth half a mile. The promontories by which it is formed, consist of high and craggy cliffs of micaceous and argillaceous schists, dipping rapidly south and south-west, whilst the centre of the bay displays a rough and broken range of red sandstone and conglomerates + ; the bright vermilion colour of the former giving to the cliffs a singular and beautiful appearance. The slates and red conglomerates attain an altitude t of about 400 feet and the red sandstone of about 200 feet. The slates of Gamrie Head stretch inland and form a continuous range, intersected by a few ravines and small valleys ; and are separated from the old red sand- stone by a wild ravine, which ranges nearly due south. Along part of the east- ern side of the ravine the red sandstone appears; whilst on the western side is an escarpment of slate rocks, and at the further end of it, are the bold and pre- cipitous crags of the red conglomerate. The red sandstones form an abruptly undulating tract, much less elevated than those composed of the slates or the red conglomerates, the last attaining, at Findon, an altitude nearly equal to that of the encircling slate ranges, or about 600 feet above the level of the sea. Here and there are small outliers of superficial or drift clay and sand, the former containing lias fossils. To the south-west of Gamrie, is a small conical hill of this dark blue clay, resting upon the red sandstone ; and another small similar tract, rests upon the slate rocks above Crovie. The streams take their rise either in the upper marls of the conglomerates, or in the overlying clay, and run through numerous ravines into the sea. ScuistosE Rocks. ' Describing the strata in the ascending order, I shall briefly allude to these * Map and Sections, Plate X. + The section being nearly at right angles to the dip, the strata appear to a spectator facing the cliff to be nearly horizontal. { Not having had the instruments necessary to ascertain correctly the height of the hills, I can offer merely a rough approximation, founded upon a level taken from the coast up the bed of the rivulet to Findon. the Neighbourhood of Gamrie, Banffshire. 141 ancient rocks, as forming the base on which the younger deposits were accu- mulated, and as exhibiting a type of the general character of the slate series of the district. Upon a bed of light-coloured, fine-grained gneiss, exhibited occasionally in some of the anti- clinal lines, reposes a beautiful variety of mica slate, consisting of slightly waved beds, alternately of a silver grey and light red colours, and oécasionally studded with imperfectly crystallized gar- nets. These strata pass up into siliceous beds, consisting of a colourless quartz with a small quan- tity of hornblende ; and are succeeded by argillaceous schists alternating with coarse roofing slate ; which in turn are overlaid by strata of dark micaceous schist with waved surfaces, the uppermost beds being light grey and dark red, sandy and argillaceous. The minerals found in this formation consist, as usual, of crystalline white quartz in the veins of the rocks; of a few small crystals of hornblende disseminated in some of the schists; and of small, imperfect garnets in the mica slate. Chromate of iron is also found, in the state of fine powder, in the sands at the base of the cliffs at Macduff, but the vein whence it was derived has not been discovered. An excellent section of the slates is exhibited along the coast from Black- pots to Gamrie ; the lowest and the middle parts being displayed between Blackpots and Banff*, and the middle and upper parts between Banff and Gamrie. The strata are greatly contorted, and present, especially near Macduff and between Blackpots and Banff, numerous anticlinal and syn- clinal dips. Oxp Rep SanpsTone. In the cliffs behind Gamrie, and in the brook at Crovie, the upper beds of the schistose rocks pass apparently into the old red sandstone; strata of a dark purplish sandstone at first alternating with slates, sandstones and marls, and finally graduating into a bright red sandstone. This deposit is of great thickness, and is well characterized by its lithological structure. Its lower beds form beautiful cliffs to the west of Gamrie, but the upper can be studied only on the banks of the streams below Findon; where, the friable sandstones and fine conglomerates of the higher part of this formation crop out. These upper strata dip slightly south-west, and are ex- posed in a succession of soft, red and yellow, slightly micaceous sandstones and marls, alternating with thin, subordinate beds, containing a few pebbles of quartz and slates. In the descending series, the beds become thicker, more compact, and of a brighter red streaked with yellow, and the subordinate conglomerates gradually disappear. That part of the formation which crops out on the coast, is peculiar (as I have before mentioned) for its fine bright red colour. In the lowest beds, the yellow streaks are replaced by round, light yellow spots, about the size of a shilling, and as regularly shaped. These beds are tolerably hard, and are used as a building-stone. I could discover no fossils in any part of this red sandstone. Rep CoNGLOMERATE AND Ctuays wiTH IcHTHYOLITEs. A good, and indeed almost the only section of the Ichthyolite-bed, is exhi- bited in a cliff, overhanging a small rivulet about 200 yards north of Mr. #)P]. X: SecioNo. 1: 142 _ Mr. Prestwicn on the Structure of Dockar’s farm at Findon. The following sectional list shews the position of this bed. 1. Fragments of schistose rocks imbedded in a coarse, fer- ruginous, slightly micaceous sand .......+++++++++ 35 feet. 2 RCO A ie ir vinis i fin.nine © ojsis,2 =.*.= * oi = agnip nivale mp ee 8. Grey clay, with Ichthyolites ..........eeeeeeeeeeee 4 — 4. Grey shale, slightly micaceous, with a few scales of fishes and traces of vegetables ...... eeeeeeeeeesess cree 1B — 5. Red conglomerate ......+-+eee-- ce eeeeeerecs as ee go — 6. Coarse, red, micaceous sandstone, with remains of fishes... 3 — 7. Loose breccia, very similar to No. 1. The outcrop of the underlying strata may be traced in descending the channel of the brook. They consist of thick beds of coarse, red conglomerate, separated by thin layers of micaceous, coarse, red and grey sandstone, forming a total thickness of about eighty feet. The old red sandstone is here brought up by a fault, which prevents the outcrop of the lower part of the red conglomerates ; but a better section of the latter, appears in the deep ravine, about a quarter of a mile west of Mr. Dockar’s. (See wood-cut). Clay and shale with Ichthyolites (Nos. 3 and 4 of the preceding Section) ..ee.seeeceecsceeccceccees Conglomerates, and sandstones, with remains of fishes Coarse and thick-bedded, red conglomerates, with no YoStiis Seer cee es oe eR RTE Ee oe us The gradual passage of the clays, shales and sandstone into the thick, underlying conglomerates, may be seen there to greatadvantage. The conglomerates become coarser, and are generally harder as they descend; and at the same time the inclosed rolled fragments, present a greater mineralogical variety. Thus, the uppermost bed, which overlies the clay with Ichthyolites, consists almost solely of angular fragments of schistose rocks, varying in size from one to four inches, and imbedded in * The red clay is of a variable thickness. Its colour appears to be owing to the percolation of water through the overlying ferruginous breccia, the Neighbourhood of Gamrie, Banffshire. 143 a coarse, reddish-brown ferruginous and slightly micaceous sand. ‘The sandstone underlying the clay is coarse, micaceous, and of a deep red colour, as is likewise the matrix of the underlying conglomerates. The rolled pebbles imbedded in them are commonly not larger than a marble, and consist principally of quartz and clay slate. The bed No. 7. of the first section, is, however, less compact, and more resembles No.1. Below No. 7. (see section with wood-cut) the conglo- merates gradually become coarser and harder, and inclose, with the pebbles of the schistose rocks, a few rolled masses of gneiss. Only a small portion, however, of the lower beds can be seen in either of the above-mentioned places, as the old red sandstone comes to the surface at a short distance from the outcrop of the Ichthyolite beds (Pl. X. Map, and Section No. 3.). The sand- stone, at first sight, seems to rise from beneath the conglomerates, but is in reality brought into juxtaposition by a fault. Owing to the soft and friable nature of its upper beds, its presence is at once indicated, by the grassy slope of the sides of the ravines, instead of the bold and rugged escarpment presented by the conglomerates. ‘The latter may be seen in fuller development in the cliffs between Gamrie and Crovie, which rise to the height of about 400 feet. Near Crovie they rest unconformably upon the lower beds of the old red sandstone (Pl. X. No. 2.), and dip at an angle of about 40° to the S.S.E., or from the face of the cliff as exhibited in the section; but upon approaching the fault, the strata rise rapidly westward or towards it. The beds are here of great thickness; and differ considerably from the upper beds in mineralogical composition, as well as in the size of the inclosed, rolled pebbles. The matrix is generally siliceous and extremely hard, occasionally of dark grey, and at other times of a white or red colour. In some of the lower strata it occasionally consists of a white, crystallized carbonate of lime. White quartz pebbles predominate in some beds, whilst the rounded fragments of granite, gneiss, micaceous and argillaceous schists and hornblende rock, are mostly of the size of a cannon-ball, but sometimes much larger; a few which I measured being from three to four feet in circumference. Rolled masses of a fine-grained, red and variegated sandstone, are also occasionally found in the lower part of the series. This phenomenon, together with the character of the cement of the lower beds, would indicate that the matrix of this part of the red conglomerates, had been principally derived from the destruction of the red sandstone upon which it reposes. Such are the general lithological characters of the deposit. ‘There can be no doubt, I should imagine, that the clay and shales inclosing the Ichthyo- lites* belong to the upper part of this series, passing, as has been shown, ra- pidly into the subjacent sandstones and conglomerates, in which occur remains of fishes, similar to those in the beds above. The Ichthyolites are disposed in the clay in nodular layers six or eight inches apart ; and most of the nodules appear to have been formed upon a nucleus of a portion, or of an entire fish, whose remains are, however, generally in a very imperfect state. Scales of the * The nodules are of a grey colour, flattish, and when they contain any portion of a fish, split by a smart blow of the hammer in the plane of the major axis, and are broken with difficulty in any other direction. The interior of most of the nodules is quite compact, and surrounded with a crust of fibrous carbonate of lime, occasionally speckled by green carbonate of copper. The species already figured in M. Agassiz’s Poissons Fossiles, are as follows :— Cheirolepis uragus, vol. ii. tab. 1°. fig. 1, 2, and 3. Cheiracanthus Murchisonit, vol. ii. tab. 1°- figs. 3 and 4. and Osteolepis arenatus, vol. ii. tab. 24. 144 Mr. Prestwicu on the Structure of same fishes with imperfect vegetable impressions, occur occasionally in the underlying bed of micaceous shale. In the subjacent, red, micaceous sandstones, alternating with beds of con- glomerate, fragments of the same fishes are also found; and it is only where these sandstones are entirely replaced by the conglomerates, that the fish exuvie disappear. This absence might be expected, from the fragmentary nature of the deposit, which must have been accumulated by a body of water possessing great velocity and transporting power ; and the friction of such numberless masses of rolled rocks, must have destroyed any animal or vege- table remains thrown amongst them. As we ascend in the series we have indications of alternating periods of comparative calm, during which the finer sandstones were deposited. As these periods increased in duration, the more favourable became the condition of the water for the existence of animals, until at last, during the slow and gradual deposition of the grey clay stratum, the entombed reliquiz indicate an epoch, when the waters probably possessed but little velocity. This temporary calm was followed by another paroxysm, by which the shales and clay were covered to a great thickness with a friable, brecciated mass. This breccia forms the highest bed of the deposit in the district, and caps the hill upon which the small hamlet of Findon is built. Trap Rocks. A dyke of trap appears on the coast, near the junction of the red sandstone ‘und the slate rocks not far from Gamrie church (see Pl. X. Sect. 2.), and ranges inland in a southerly direction. It is composed of a sienitic green- stone, and is from twenty to thirty feet across, At Castle Hill, Gamrie, and at several other places in the same neighbour- hood, and also on the schistose cliffs between Banff and Blackpots (see Pl. X. No. 4.), a dark-coloured tenacious clay, containing a few, subordinate beds of a light yellow sand, reposes almost horizontally upon the other rocks. I have been informed that lias fossils are found in this deposit*. * In the paper originally read before the Society, this deposit was described as lias upon the authority of geologists in that country.—See Proceedings, vol. ii. No. 40. page 187, March, 1837. See for a correction of this statement the Appendix to the paper, p. 146. the Neighbourhood of Gamrie, Banffshire. 145 Fautts. Two great and important dislocations affect the continuity of the forma- tions. By one of them, the Gamrie Fault, which ranges inland in a south- easterly direction (Pl. X. Map and sections 2 & 3), the highly inclined strata of the slate rocks, are brought successively on a level with the nearly hori- zontal beds of the red sandstone and red conglomerate, and at the point of contact, the edges of the sandstone and conglomerate are slightly turned up. The second, or Findon Fault, is well exhibited in the high cliffs immediately east of Gamrie (see Map and sect. 2 & 3.), where the micaceous schist, over- laid by the red sandstone, occurs also upon a level with the red conglomerate, and subsequently brings the red sandstone and conglomerates into contact. The schist, where it rises from beneath the red sandstone, dips at an angle of about 20°, but near the line of fault the strata are horizontal, and the beds of conglomerate against which they abut, are tilted at a considerable angle. This fault ranges in a south-westerly direction, crossing the ravine at the back of Gamrie. It may be seen at several other points near Findon. A few less dislocations are visible in the cliffs and ravines, but they cannot be traced to any distance. That the upheaving, which produced these faults, was attended by a considerable lateral pressure, is denoted by the great tilting of the edges of the disjointed strata of the red conglomerates. 1 cannot speak positively as to the amount of disturbance, exhibited by these faults. That it was very considerable there can be no doubt; for in the Gamrie fault at the Old Church, we see the disjointed edges of the slates in contact with those of the centre of the old red sandstone series; whilst the Findon fault, has almost entirely thrown out the whole formation of red sandstone, indicating thereby a difference of level, amounting at least to several hundred feet. (See Pl. X. sect. 2 & 3.) ConcLusion. Mr. Murchison directed my attention to the Gamrie Ichthyolites for the purpose of determining, as far as I was able, the age of the deposit in which they occur. From the observations detailed in the preceding pages, I con- sider that the strata belong to the upper series of a red conglomerate, more recent than the great mass of the old red sandstone described by Professor Sedgwick and Mr. Murchison*. The same observers have suggested, that the Caithness schists pass down into the old red sandstone; but as the con- glomerates containing the Gamrie Ichthyolites lie unconformably upon a sandstone (considered to be the equivalent of the old red sandstone of * Geological Transactions, 2nd series, vol. ii. p. 125, et seq. VOL. V.—SECOND SERIES. U 146 Mr. Prestwicu on the Structure of England), I conceive, that it belongs to the carboniferous series, and most probably, to be the representative of the millstone grit or mountain limestone ; and, therefore, to be younger than the Caithness schists*. APPENDIX. [Read May 3, 1837.] In the preceding memoir, as read before the Society in April 1835, I stated, that lias fossils had been found in outliers of dark blue clay and sand, which in several places overlaid the older rocks, and upon that evidence, I suggested the beds might be of the age of the English lias. I had not then carefully inspected those deposits, and in the cursory examination which I made, I met with no fossils. Subsequent researches, however, having led me to doubt the correctness of my former surmise, and having again visited the district last summer, I now beg to retract that opinion, and to state briefly the conclusions at which I have arrived. It is true, that lias fossils are occasionally found in the cliffs of Blackpots, and in the beds of clay in other places around Banff ; but they always occur in separate, rounded nodules and fragments of shale and limestone, associated with pebbles of the schistose rocks, and are disseminated in layers and patches in a dark, tough, or slightly micaceous clay. This ar- gillaceous deposit, forms at Blackpots, cliffs eighty feet high, and rests upon sand which is rarely exposed ; a bed of gravel usually intervening between the clay and sand. The stratification of this accumulation is nearly horizontal, but irregular. Above McDuff it caps the hill to a considerable thickness, its lowest bed being grey loam, twenty feet thick, full of angu- lar fragments of slate rocks. Patches of it range eastward by Melrose to Gamrie, and thence by Crovie to the back of Troup ; but it is at Castle Hill, Gamrie, that the deposit is best developed. (Plate X. No. 4.) This hill is about 250 feet high, of a roughly conical form, and is exposed on one side by the cliff, and on two other sides by deep ravines. The base of the hill, to the height of about 80 or 100 feet, consists of old red sandstone, upon which reposes a series of sands and clays, and on the summit are the remains of a small vitrified fort. A few fragments of shells scattered on the grass about half way up the hill, induced me to make an excavation, by which I succeeded in ob- taining several well-preserved specimens ; and though the shells were rather numerous, they were * Mr. G. Anderson of Inverness has recently informed me that Ichthyolites, the same as those of Gamrie, have been found by Mr. Miller near Cromarty, in a bed of clay, overlying the great system of conglomerates and sandstones the Neighbourhood of Gamrie, Banffshire. y 147 so extremely friable, at their first exposure, that it was very difficult to procure perfect ones. The following section exhibits their situation. 1. Soil and grey clay. 2. Yellow loam ...... Soa Bail poe bie ate sid olevele «+++- 6 inches. 65 Gravel in Oehredussclay oo). gd sa eie cle oedesalee ne 8 —— 4, Dark grey clay, very tough....... Seals d ctainogih 6 —— 5. Dark brown do. do. SCAG OO ECOG coccoe 4 —— 6. Fine sand, with irregular patches of bleached shells, and occasionally gravel. About fifty yards distant, the following somewhat similar section is displayed. 1. Loam, striped grey and yellow ...........+005: 2 feet. 2. Gravel in ochreous clay (same as 3 of last section) 24 Sop Datile cla ins wash & «sets he hapten viet) «obra bince 2 ia SANG MN ae a: ahebaTaiet cin .etaisla\s @ixlaiacaic Asels «id peie,« Pe!) . The shells, which are all recent, may be traced at intervals, and upon the same level around the hill. They consist of Astarte Scotica, Tellina tenuis, T. Donax, Buccinum undatum, Natica glau- cina? Fusus turricola, Dentalium Dentalis. The sands and clays vary considerably in thickness, and are accompanied by thin, subordinate beds of gravel, the lowermost of which reposes immediately upon the old red sandstone, and con- sists almost entirely of slightly rolled angular fragments of argillaceous slates with a few quartz pebbles. A second bed lies above the shells, and the pebbles are more rounded, and have been derived from a greater variety of the older deposits. A third, which occurs in the uppermost stratum of sand, is similar to the second. There are, besides these, a few small irregular layers in the upper sands. The most persistent of these beds is the lowest, which varies in thickness from four to thirty feet, and almost invariably accompanies the deposit; whereas the others are frequently wanting. Flints (apparently chalk) are common on tiie beach, and it is probable that they were derived from some of the upper beds of gravel of this drift; for Mr. Christie of Banff informed me, that he had found them in the gravel on the top of McDuff Hill, and they have been met with also in the interior of the country. From the above details it appears, that the series of sand and clays, was partly derived from the destruction and transport of the lias and lias marl. It is also evident that the disturbing power was of long continuance and of varying intensity. The rolled fragments, which generally underlie the trans- ported, lias clay, indicate periods of paroxysms, when the waters, breaking and tearing up the lias and older rocks, bore them from their original to their present position ; rolling and rounding, in their course, the harder frag- ments, and holding in suspension the finer clay, which, upon the cessation of the more violent action, subsided according to gravity, and thus formed a layer of fine clay resting upon a bed of gravel. The sands indicate a vu 2 148 Mr. Prestwicu on the Structure of Gamrie, Banffshire. period of calm; for in such a state only could the delicate remains imbedded in them, have been preserved. This deposit appears to have been uplifted from the bottom of the sea in which it was formed, by a power not acting uniformly ; for a gradual rise is perceptible in it, from the level of the shore at Blackpots, to Gamrie, where its base attains a height of 100 feet; indicating a disturbing power, whose energies increased as it tended eastward. These and other phenomena, on the shores of the Moray Firth, prove that the level of the land has been altered several times, during recent geological periods. Some of these phenomena, indicative of an elevation more recent than the one just described, and well exhibited along the coast three miles to the west, and twelve miles to the east of Banff, I here purpose to notice briefly. At various points along this line, the effects of the last uplifting of the land are unequivocal, and prove a rise of the coast to an extent varying from six to twelve feet. 'To the west of Banff, at White Hills and Black- pots, may be seen, at the foot of the cliffs, and at about six feet above high- water level, a bed of shingle, which, in some places, contains large quantities of Patella vulgata, P. levis, Trochus ziziphinus, T. cinerarius, Littorina littorea, and Turbo retusus, all of which inhabit the adjacent sea. This change of level is also well exhibited in the cliffs of old red sandstone in the Bay of Gamrie, where remnants of a raised beach, four feet thick and ten feet above the level of high tide, remain in the indentations and hollows of the rock. This beach consists of flattened pebbles of the adjoining schists, precisely similar to those forming the present beach ; but it contains no shells. To this elevation may be ascribed the drainage of the former low lands of the country. Around White Hills* there exist, at a height of about twenty-five feet above high-water level, patches of a drained peat moss. It is composed of thin layers of peat, alternating with two seams of a fine gravel of white quartz grits, containing land and freshwater shells. The thickness of the whole does not usually exceed four feet. The peat is much decayed, and the shells, which are excessively friable, consist almost entirely of the Succinea amphibia and a species of Helix. * See Map, Pl, X. The full extent of this deposit is not marked on the map. ies A se. ‘odie: atcaaiaeteee A ayy : , Rath BA wen i 5 aa Mek , aN fou 7 ta 4 ad Saar rahe. es. uN iiew r ty vd ne Fie paar Ma ih ER Ot + ry : } a: AOE ND Sic! A itr ' ¥/ Ww ¥ a] is - 4 \ y ‘ a! 7 Lr, D » ‘ 148 Mr. Prestwicu on the Structure of Gamrie, Banffshire. period of calm; for in such a state only could the delicate remains imbedded in them, have been preserved. This deposit appears to have been uplifted from the bottom of the sea in which it was formed, by a power not acting uniformly ; for a gradual rise is perceptible in it, from the level of the shore at Blackpots, to Gamrie, where its base attains a height of 100 feet; indicating a disturbing power, whose energies increased as it tended eastward. These and other phenomena, on the shores of the Moray Firth, prove that the level of the land has been altered several times, during recent geological periods. Some of these phenomena, indicative of an elevation more recent than the one just described, and well exhibited along the coast three miles to the west, and twelve miles to the east of Banff, I here purpose to notice briefly. At various points along this line, the effects of the last uplifting of the land are unequivocal, and prove a rise of the coast to an extent varying from six to twelve feet. 'To the west of Banff, at White Hills and Black- pots, may be seen, at the foot of the cliffs, and at about six feet above high- water level, a bed of shingle, which, in some places, contains large quantities of Patella vulgata, P. levis, Trochus ziziphinus, T. cinerarius, Littorina littorea, and Turbo retusus, all of which inhabit the adjacent sea. This change of level is also well exhibited in the cliffs of old red sandstone in the Bay of Gamrie, where remnants of a raised beach, four feet thick and ten feet above the level of high tide, remain in the indentations and hollows of the rock. This beach consists of flattened pebbles of the adjoining: schists, precisely similar to those forming the present beach ; but it contains no shells. To this elevation may be ascribed the drainage of the former low lands of the country. Around White Hills* there exist, at a height of about twenty-five feet above high-water level, patches of a drained peat moss. It is composed of thin layers of peat, alternating with two seams of a fine gravel of white quartz grits, containing land and freshwater shells. The thickness of the whole does not usually exceed four feet. The peat is much decayed, and the shells, which are excessively friable, consist almost entirely of the Succinea amphibia and a species of Helix. * See Map, P]. X. The full extent of this deposit is not marked on the map. elentig ‘at Soe 7 poets - fllatia NOOR TUE RN iC OAS Tf. OF AS Y-10:.. AND) +S Lin G: 0 bv Arctudeacon Verschoyle. Lriste Mile Rulon > 7 ee are Cartwataren Carton, C.2 a et Cooking ee] Drirwtive oo Top Dries Hoemiderahr Vhite r ae | Geol Trans. 2™ Series VOL NORT EE RN VCWAS OF MAY Oe snp- Sadie: tock by Archdeacon Verschovle. English Miles i 2 i a. ee ee 6 Zz é 2 IO _ Pi zz PA af Z 2 3 = o 7 7 ry 9 72 74 Trish Miles —————_ i Peat Bog and Moor Trachyte Trap and Basalt Carbenitrous Limestone Colitic Ditto Shale & Grit i - (i | Lae Direction of Trap Dvkas “Dvhes actually Quart: Rock Geiss Miew Slate Fiornblende Slate Granite SVE. pata Knock Bough WV. = Tnock na Sy Downpatrick He Downbrivta Kock: Sligo Harbour [ 149 ] _X1.—Notices on the Geology of the North Coast of the Counties of Mayo and Sligo in Ireland. By ARCHDEACON VERSCHOYLE, M.A. Communicated by Roperick Impey Murcuison, Esq., P.G.S. {Read November 7 & 21, 1832.] THE country I propose to describe, comprises the northern districts of Mayo and Sligo. In constructing the map*, I have used for the former county, the excellent map of Mr. Bald, some fishery charts by Nimmo, and some local surveys; and for Sligo, a corrected copy of Larkin’s Map. In connecting the two counties, J have used triangles resulting from the operations of the Ordnance Survey, most liberally communicated by Captain Portlock, with the permission of Colonel Colby; and where doubts and deficiencies in the details occurred, observations were made with a three-inch sextant, or Kater’s Compass. The drawings (pp. 158. 162. 165. 167.) are from sketches taken on the spot, with every determination to sacrifice picturesque effect to accuracy. The only notice which has been published respecting this part of Con- naught, is a short but very able and accurate sketch in Mr. Griffith’s paper on its Bogs, attached to the 4th Report of the Commissioners. The Ox mountain ridge extends through the district from south-west to north-east. It is chiefly formed of mica slate, hornblende slate, gneiss, and quartz rock, the strata dipping rapidly to the south. At the base occurs a conglomerate, alternating with sandstone and slate clay ; and overlaid by the carboniferous limestone, which extends westward from Sligo to the Nefin group. This group is the commencement of the primary tract, reaching northward and westward to the ocean. The section from Lough Talt to Downpatrick Head, displays the succession of stratat. The Ox Mountains have a mean height of 1300 feet. On the north-west, the summits present abrupt rocky peaks; but the ravines are not of great * Plate XI. + Plate XI. fig. 3. 150 ArcupEacon Verscuoy.e on the Geology of the North Coast of depth, and rarely reach to the base of the chain, being gradually lost in the slope of the sides. On the south-east, the ascent is more gradual, less rocky, and streams are more numerous. The principal passes through the range, are from Colloony to Ballisadere; from Coolany to Baltra by Carrick-na-Shouock ; from the barony of Liney to Skreen by Knock-a-Chree; from the same barony to Easky by Lough Eask ; from Tubbercorry to Ballina by Lough Talt ; and the Pontoon near Foxford. The first, at Colloony, is very picturesque from the magnificent falls of the river over the limestone at Colloony and Ballisadere, and the much shattered and broken mountain of mica schist, called the Union Rock, which rises through the Union Wood; as ifa course had been opened for the river by some violent convulsion, the further effect of which has evidently excavated the Bay of Ballisadere, assisted by the subsidence or removal of the limestone. The rocks surrounding Glen Lough at the foot of Benbulben, indicate a similar subsidence. On the south side also of the Ox range, the soil and even the strata of limestone, have been removed, and have probably formed materials for those immense ridges of water-worn gravel, called eskers, which are found in every part of the country. Near Tubbercorry, the surface for a considerable extent, is an almost naked limestone rock, like the shore of the barony of Tyreragh, presenting the same rounded cavities in the surface, as well as the same water-worn aspect, wanting only the sea-weed and the recent shells, to complete the identity. The drainage of this district is through the pass at Colloony, by the Owenmore, which, rising from the west side of Cash Corran, receives at the Union Wood the River Arrow, and be- fore it reaches Colloony that from Coolany, whose source is near Knock-a-Chree. The steep and rocky escarpments of the passes through which these streams flow, with the debris scattered over the surface, mark the effects of a powerful torrent. At the falls of the river, at Colloony, the limestone ceases, and thence to Ballisadere mica slate is laid bare, to a depth of fifty-five or sixty feet, lower than the limestone above the falls. The bank of the river at Coolany, about five Irish miles from the sea, is 298 feet above high-water mark, and the average descent is, therefore, 59°6 feet in the mile. The grey peak above the Union Wood and the precipices of mica slate which skirt the river below, are memorials of the ruin which has taken place; while the frag- ments of the same rock so abundantly strewed in large boulders on the opposite side of the estu- ary of Ballisadere, exhibit both the effect and the direction of the torrent, which evidently flowed from the south-west into Galway Bay, spreading thence to the north-east towards Foxford and Sligo, as indicated by the perpendicular faces and broken strata of the limestone mountains, pre- sented to the south-west and west; by the caves in Cash Corran, perfectly resembling those into which the waters of the Atlantic rush along the coast of Erris; and especially by the direction of the ridges of limestone gravel throughout the baronies of Liney and Corran, and the southern part of Mayo. The second pass, Carrick-na-Shouock, derives its name from a bold and precipitous rock, which serves as a landmark to the harbour of Sligo, rising perpendicularly on three sides, and on the fourth with a very steep and difficult ascent. The road through the pass, winds over successive strata of quartz rock, gneiss, and mica slate, dipping to the south-east, and presenting to the north-west the broken edges of the beds. Proceeding westward, we next reach the pass of Carrow-na-Skea, which crosses the ridge below Knock-a-Chree, the highest summit of this chain (1714 feet), and on the north side descends the Counties of Mayo and Sligo in Ireland. 51 into Tyreragh, behind Skreen hill. On both sides, the foot of the mountain is covered by a stratified quartzose conglomerate, which extends as far as the pass of Lough Talt. The next communication between the baronies of Liney and Tyreragh, is through the mountain valley in which lies Lough Eask, the source of the river Eask. A small patch of granite borders the road which passes along the east shore of the Lough. The river Moy having received, before it reaches Foxford, an accession of water from the Guishaden, as well as the lakes Conn and Cullen (about forty feet above high-water mark), passes, below the town, through the mountain chain between Carrick o’Hara and Shraheen Hill. The course of this river from its source to the Atlantic below Ballina, is about thirty Irish miles; and the descent being 300 feet from its head to high-water mark, it has a fall of ten feet in the mile, or one-sixth of that of the Colloony river; and probably from this cause, the effects of the stream are less striking, the pass through the mountain chain being also less abrupt: the soil likewise has not been so entirely removed as at Colloony. Foxford stands on gneiss, from below which mica slate rises, at the hills of Shraheen and Bur- ran on the Moy. Lough Cullen communicates with this river near the town, having received the drainage of Lough Conn, by the rocky strait at the Pontoon, where the waters have forced a passage through the beds of gneiss, leaving immense boulders scattered on the surface, even to the summit of the hills over the pass. It is remarkable, that throughout this district clay slate is never found either in situ or boulders. In the cliffs along the sea coast (see Pl. XI.) the succession of strata is satisfactorily exposed. Commencing at the promontory of Tarmon in Erris, a district where primary rocks only occur, granite is quarried near Blacksod Point, and lies in beds which may indeed be called strata. The felspar is brick red, the quartz smoke grey and translucent, and the mica black: no imbedded minerals have been observed. In a small inlet on the shore, at the west end of the hill, below the Signal Tower, mica slate appears, dipping 15° to the east, and abuting against the face of the granite beds, which incline to the west 45°; and in a narrow cove, south of this inlet, the dip of the mica slate increases to 70°, its direction becoming south. Numerous veins of granite penetrate the slate, and in some instances contain fragments of it. Proceeding to the north-east, the coast presents only a succession of sand- hills and beaches, except where a few reefs of gneiss or mica slate project into the sea. The first range of cliffs is at Annagh, the south headland of French- port, and consists of mica slate traversed by a trap dyke; but the north head- land of this inlet is formed of gneiss, composed of red felspar and black mica. On approaching Scotchport, garnets appear, the mica increases, and the felspar gradually diminishes, till the gneiss becomes mica slate, which graduates into quartz rock, in the direction of Erris Head*. This formation constitutes the lofty and broken cliffs to Broad Haven, with the exception of a few places, * For additional observations on this part of the coast see p, 160. 152. Arcupneacon VERscHoy_e on the Geology of the North Coast of where mica slate occurs. From Knocknalina the shore is low, consisting chiefly of peat, and the subsoil is a ferruginous clay, resting on fragments of mica slate. Near Belmullet, on the isthmus separating Broad Haven and Blacksod Bay, are vertical beds of mica slate, pierced and disturbed by the continuation of the trap dyke at Annagh. This mica slate, with many varia- tions and transitions into gneiss, continues till it disappears beneath the clay banks of Blacksod Bay. The eastern side of Broad Haven and the moun- tains of Kilcommon, are also mica slate, which at Donkeehan, on the north side of the haven, presents nearly vertical strata, inclining to the north, and striking east and west. Its texture is close and fine-grained, and colour greyish yellow. The small peninsula which stretches to the south from Kil- galigan, and terminates at Rinroe Point, is formed of this rock, traversed by a trap dyke. Continuing along the coast northward, the mica slate is soon succeeded by quartz rock, a prolongation, probably, of the Erris Head strata. It underlies the mica slate, becoming nearly vertical, and continues to Porta- cloy, but varies much in its dip. At the first headland, to the east of Kid Island, a trap dyke rises from the sea, and will be hereafter described. Pursuing the examination of the coast to the eastward, the quartz rock continues up the narrow harbour of Portacloy, the western cliff of which is a truncated cone, connected with a narrow isthmus terminating about twenty feet below the summit, and accessible only by steps hewn in the rock. At the west side of this headland, called Doonminulla, is a magnificent cavern, into which the sea flows through an arch about thirty feet wide and twenty- five high, the roof within, rising in a dome of above forty feet, and the length and breadth of the hall or chamber,averaging about sixty-five or seventy feet. This opening was probably produced by the disintegration of a mass of trap and the action of the waves ; as arches and passages, in other parts of this coast, clearly exhibit such decomposition in progress. Between Portacloy and the next landing-place, Porturlin, a small and very narrow inlet, mica slate prevails ; but across the mouth of the inlet a vein of trap passes, and is again seen in the headlands next to Benmore. From the latter point the coast continues precipitous, and is composed of mica slate or quartz rock graduating insensibly into each other. In the perpendicular face of Benwore headland, the beds diverge from a point beneath the surface of the water, like the rays of an expanded fan, probably influenced by the same dyke, which separated Horse Island from the mainland. At the east side of Balderig inlet, a bed of very compact trap is found below high-water mark, and seems to have been protruded between the strata of quartz rock, and to have pro- ceeded from the Horse Island vein. ‘Thence to Conoghrea there is nothing the Counties of Mayo and Sligo in Ireland. 153 very interesting ; but we there arrive at the termination of the inferior and the commencement of the intermediate order of rocks, including the carboniferous limestone ; and these beds extend without interruption to Ballyshannon in Donegal. From Fohurlin to Kilcummin, west of Killalla Bay, the cliffs present strata of sandstone, occasionally containing vegetable remains, and alternating with shale and argillaceous limestone; the whole dipping regularly to the south- east, when undisturbed by the intrusion of trap veins. Very fantastic scenery, resembling arches, and towers, as well as caves of unusual forms, abound along this part of the coast. In some places, the sea, having penetrated the lower strata of the cliff to a considerable distance, has excavated spacious caverns, at the extremity of which a portion of the roof having fallen and been also washed away, an opening to the surface has been formed, by means of which the waves are seen to rush with vio- lence against the end of the cavern. One of these excavations extends across the headland of Downpatrick, a distance of about 500 yards, and in the centre, a large chasm, or, as it is locally called, a pigeon-hole, has been formed, and is 120 feet deep to the water below. Downbrista rock, which resembles an enor- mous, insulated, and inaccessible tower, 130 feet high, has been probably separated from the main land; as the continuation of a wall, whose remains are plainly traceable to the very edge of the cliff, stands on the summit of the rock. The powerful surge of the Atlantic breaking on the north-west face of the headland, also 130 feet high, rises with such force and momentum as to tear up the rocks at the summit edge of the cliff, and in many instances to raise on their edges, fragments from among the debris, weighing at least halfa ton. In the north-westerly gales, the spray ascends in a magnificent column, to twice the height of the precipice against which the swell breaks, and is carried to a great distance inland. On the west side of Downpatrick Head, between Downbrista Rock and Buntraher Bay, the Horse Island Dyke (No. 2.) is again seen ; and on doubling the head, passing eastward, another dyke, a continuation of No. 1, lies against the cliff, like an immense wall. On the sandy beach of 'Tracal Bay is a creek, called Poolagranny, which deserves careful examination. Proceeding around the promontory of Kilcummin, a range of elevated and perpendicular preci- pices, bounds the coast as far as Poolaclogher ; whence the shore is chiefly composed of gravel in waved beds, apparently much disturbed. Crossing the estuary of Palmerstown River, and following for some distance the sandy beach of Ross, the porphyry or trachyte formation, described in the 2nd sec- tion, occurs. Thence to Enniscrone, the Bay of Killalla, is bounded by the VOL. V.—SECOND SERIES. x 154 Arcupeacon VerRscHoyLe on the Geology of the North Coast of sand-banks of Bartra Island and Scurmore, to the north of which, on the Sligo shore, is a continuation of the trachyte, first seen in Ross. From this point to Ballisadere Bay, the coast is composed of mountain limestone and the asso- ciated beds of sandstone. These strata are strikingly displayed in the preci- pitous sides of Knock-na-ree, to the east of Ballisadere Bay, and are streaked horizontally with beds of light grey rock, tinged with various shades of purple and yellow ; and are skirted by a talus of fragments from the cliff above. 1 have thought it convenient thus to separate the general sketch of the district, from those geological details, which are the more immediate object of this communication. Sreconp SEcTION. In considering the subject of this section, I adopt the arrangement of the Rey. William Conybeare, in his Outlines of the Geology of England. Com- mencing,, therefore, with the highest formation in the district, the following series will be described : A. Carboniferous’ limestone. B. Ditto colitic. Intermediate order...eseesseee C. Calcareous and argillaceous shale and grit underlying the limestone. . Old red sandstone and conglomerate. . Quartz rock. . Gneiss. D E The inferior or primary rocks .. 3 5 G. Mica slate and hornblende slate. H ii, K. . Granite. Trap rocks, porphyry, and basalt. Trachyte. INTERMEDIATE ORDER. A. Carboniferous Limestone. This formation prevails on the north and south of the Ox Mountains. Ben- bulben' (1697 feet) and Knock na Ree (1057) on the north of the chain; and Knock na Shee (480) on the south, are entirely formed of it. The lower beds contain nodules of black chert, and invest the organic remains which abound in limestone throughout Ireland. It varies in texture from compact to highly crystalline, and in colour from grey to light brown; its specific gravity ranging from 2°670 to 2°685. Arragonite, fluor, brown spar, pyrites, and quartz crystals are often imbedded in it, or line rifts and fissures. A vein of sulphuret of lead accompanied by blende and iron pyrites, has been worked at Ballisadere, but is now abandoned. It is said to have been very rich in the Counties of Mayo and Sligo in Ireland. 155 silver. About eighty years since, another lead mine was wrought at Lug- gawarry, on the north face of the Ox Mountains, near the pass of Carrick na Shouock. ‘The level and some shafts are still open, and the ore was found near the junction of the limestone with the subjacent rocks. Organic re- mains abound in the formation, some occurring in it exclusively, as far as I have examined the midland parts of Ireland. Among these, polyparia are prominent, especially a gigantic species of Cyathophyllum ; and among the shells I have seen two specimens of a very large Kuomphalus, armed with formidable spines*, also many species of Productus, Spirifer, and Tere- bratula. In the Hill of Skreen, among the lower beds of this rock, near the junction with the subjacent conglomerates, are some thin strata containing numerous quartz pebbles cemented by limestone; and beneath these are layers containing shells, but no quartz pebbles. In the neighbourhood of Killalla is the following peculiar formation, which I have not observed else- where. It is interposed between the limestone and the older sandstones. B. Oolite of the Carboniferous Limestone. This deposit, which lies below the limestone from Moyne to Rathrea, varies in colour from iron grey to dark smoke grey ; and is composed of gra- nular concretions not larger than mustard-seeds, but, under the microscope, appear to consist of concentric lamine. Its durability as a building material, is proved by the ruined abbey at Moyne, the arches, pillars, and smallest mouldings of which, retain the most delicate touches of the chisel. Marine exuviz occur in this rock, but so comminuted that the genera are scarcely determinable. It contains also, though rarely, carbonized and pyritous, vegetable remains, resembling reeds and the leaves of the Iris; also nodules of black shale containing particles of pitch coal. Sometimes cavities occur, lined with arragonite, in fibrous radiated concretions. The beds are fre- quently separated by layers of brownish slate clay, varying in thickness, and interspersed with fragments of black slate clay, not at all water-worn. This oolite, as already stated, is very limited in extent, being found only from Moyne by Killalla to Rathrea. In some parts of the county of Sligo, the lower beds of the carboniferous limestone are highly crystalline, and much resemble this rock; but a magnifier immediately detects the absence of the spherical concretions. At the outcrop of this deposit along the shore, between Killalla and the Abbey of Moyne, is a breccia composed of angular fragments of oolite, im- * A species somewhat analogous is figured in the 2nd part of Prof. Phillips’s Geology of York- shire, Pl. XIII. fig. 5. we 156 Arcupeacon VerscHoy_e on the Geology of the North Coast of bedded in an argillaceous cement. It occupies the spaces between large masses of the same rock, thrown confusedly together. The edges of the beds are elevated and much fractured, while their recurrence to the north, to which point they rise, indicates a subsidence or fault ranging east and west. The beds of peat and bog-timber, found below high-water mark in Killalla Harbour, may be connected with the fault. Near this place the sandstone emerges from beneath the oolite in rude columnar masses, much disturbed, and forms the commencement of the grit and shale beds described under the next head. C. Calcareous and Argillaceous Shale and Grit. The mountain limestone rests on alternating layers of sandstone, slate clay, and argillaceous limestone, except where the oolitic strata intervene ; and the lower beds of grit, graduate, in some places, so insensibly into the subjacent quartz rock, that the limits of the two formations are very difficult to determine. At the western boundary the transition is gradual, and were it not that the strata of quartz rock at Glen Lassera, are unconformable to the beds of sandstone, the demarkation could scarcely be ascertained. The conglomerate of the old red sandstone is also absent there; but along the foot of the Ox Mountains, it is interposed between the grit and shale beds and the older strata. To detail the succession of layers is impossible, but two examples, taken from Ross and Moyne, may be instructive; and Mr. Griffith’s Memoir on Mayo, in the Re- ports of the Bog Commissioners, made in 1814, furnishes the details at Bal- horig in Erris*. Section at Ross, near Killalla. Ft. In. Ft. In Sandstone, highest bed .......+ 12 0 Brought forward 24 6 Claystone: %).'s.sjianiae ee aeeiar 5 0 Schistose Sandstone .......... 2 0 Clay parting. sic/witecsnmiaete tae 0 5 CIA YECOT SSisioic nw ohe wine Bin aul vols 6 0 Wiacke. . s't. i's amet be eho eee 0 8 Schistose Claystone .......+.. thie Wellow Clay’ <..0...00 cena 0 5 Wachee roc ll, Aint apne ee 5 0 WAI cfe.we ie sls swe vibid vc ela 0 9 Sandstone, with clay nodules im- BEANIE cas’. sco codw ac eee 0 2 ellded. 1 Ser oo ies ve 1. Green, Sandy Clay ....0+.0e80s 0 7 Yellow Clay. 5s Sites merce eevee 0 9 BSIGWHEGNE! 6s < vic vie Siv'ec Ses tiles 2. 0 Wacke and Sandstone, with wood ‘ SRIMLETY Aelwia's, «xe p'e'uie se oo. ates tate 0 9 in a bituminized state...... RHAUVMOIAY oo Saice ss ecccloe viet 0 6 Black Shale... ve csteu ews s'e's « iG WUC sete bole we oelcicield Wile adlete 0 3 Claystone (lowest bed exposed).. 10 0 PME AAS lof joe non pie’. wisiele ois Ly 40 be 9 24 6 the Counties of Mayo and Sligo in Ireland. 157 Section at Moyne, north-west of the Abbey. Ft. In. Ft. In. Oliver. cterierrents siavelate f° 4,06 Hee GAO Brought forward 47 4 Black Limestone, email A Alternate beds of Shale Dib pane Cirri, clayey and friable .... MGTMEStONE) 1 cle oars c oie cle ees Sandstone in beds ...... aveie sew TO Calcareous Sandstone........ ied bal l(C. WintephaleA Laue. i... ra 0 OMAN Pelateains ld eid sd Vs Pele va yy a WAMGSLOHEY osié fein ollelbin ci» dlakholele . 1 4 Argillaceous Limestone ..... - Sees Sandstone and Shale, in eal ae Shale ak cigisparidig ale eee, aes Las BON aio siWin i Sg Sate De ie Ochrey Sandstone ............ 0 47 4 57 10 There is a striking resemblance between these grit and shale beds, and those which accompany coal; but they lie decidedly below the great limestone, over which all the Connaught coal district is placed. Their total thickness may be estimated at 1700 or 1800 feet. The most instructive sections are exposed along the coast from Ross, near Killalla, to Port Conoghrea, where the quariz rock is first seen. In many quarries, the surface of the grit beds exactly resembles a sandy beach deserted by the tide, presenting the same waved, ripple marks. Beneath the varied succession of strata, which underlie the carboniferous limestone, is gene- rally found the D. The Old Red Sandstone and Conglomerate. This rock occurs uniformly along the base of the Ox Mountains, both on the north and south declivity ; but, at the shore on the confines of Erris, where the intermediate and primary strata join, it has perhaps either never existed, from the absence of the causes which influenced its deposition else- where, or it has become identified with the lower portion of the grit, by a change in the grain and texture. In general, the strata are very distinct, though composed of large pebbles of quartz, jasper, and primary schists im- bedded in a tenacious cemeut. ‘The argillaceous soil formed by the decom- position of the matrix of the conglomerate, is stiff, cold, and sterile. I have not observed any organic remains. The conglomerate graduates, in many places, insensibly into the subjacent quartz rock, especially on the south de- clivity of the Ox Chain, where the two formations lie conformably on the inferior strata; but on the northern slope, the conglomerate rests on the edges, or outcrop of the older beds. This position may be very distinctly seen at the foot of Knock-a-Chree, above Drimnagoole, where the mica slate dips to the south, to which point the beds of old red sandstone rise, lying un- conformably on the edges of the schist, and followed by the grit, shale and carboniferous limestone, in regular and parallel succession. In Glen Co, on the banks of the Owenmore River, in Erris, this rock emerges from under the series described by Mr. Griffith, and lies on the quartz rock, which pre- 158 Arcupracon Verscuoy.e on the Geology of the North Coast of vails to Bangor. The hill of Addergool on Lough Conn, and Glen Nefin, on the flanks of the Barnagee Mountains (a prolongation to the south-west of the Ox Chain), are old red sandstone, in regular beds, though remarkably coarse, being formed of rolled pebbles of unusual dimensions. The thick beds of peat which generally cover the declivity of the mountains, preventing an exact knowledge of the boundaries of the rocks, the demarkations can be ascertained only in the ravines, where the streams have removed the bog, soil, and decomposed strata. Tue Inrerior oR Primary Rocks. E. Quartz Rock. This formation overlies the gneiss in many places along the south declivity of the Ox Mountains. It is generally composed of very fine, white, quartz grains, firmly compacted, and free from extraneous mixture ; and it is laminar or schistose in structure. This may be considered the purest variety, and of such Nefin in Tyrawly, 2639 feet high, consists ; also the vertical beds in the headlands, east and west of Broad Haven. In other places it is mingled with white, compact felspar, the laminz being thicker and less regular ; and mica also enters into the compound, which then graduates into gneiss. Rising from below the old red sandstone, on the banks of the Owenmore, in Erris, it prevails around Bangor and the south shore of Carromore Lake; but on the east bank mica slate appears. The northern part of the Mullet is also quartz rock ; and in a perpendicular cliff, at a place called Mycreeny, between Blind Harbour and Erris Head, are several very interesting and perplexing, shifted quartz veins. (See the following sketch, No. 1.) No. 1. the Counties of Mayo and Sligo in Ireland. 159 The derangements represented in the sketch might have resulted from repeated slips of the strata in varying directions ; suppose (see diagram No. 2.) the aggregate of beds marked A 1, 2, 3, 4, to have slid together in the direction E E, the interruption at C would be the result; after which a series of successive slips of the individual beds A 1, 2, 3, 4, in the altered direction F F, parallel to the vein C C but oblique to D D, would displace the latter in each bed, as represented in the plan; while G G, in consequence of its position, so much inclined to the planes of those strata, would be differently affected, and the breaks in its continuity might be scarcely perceptible*. No. 2. A great part of the coast from Broad Haven to Glen Lassera consists of quartz rock, varying considerably in dip and direction. Kast of Broad Haven, from Kilgaligan to Kid Island, the beds are nearly vertical, and of pure white, granular quartz, in which I saw no vestige of imbedded minerals. At Sheea- nemore, between Porturlin and Balderig, is a remarkable slip, the western portion of the cliff being depressed about 300 feet. At Glen Lassera this for- mation disappears beneath the intermediate rocks, and recurs no more along the coast to the eastward. F. Gneiss. This rock is well characterized at the Pontoon Bridge between Lough Conn and Lough Cullen ; also at many places in the peninsula of Erris, and in the mountains at Mulli na Shee above Coolany ; but sometimes it graduates into mica slate. At the Pontoon the mica is black, and the foliated structure is strikingly displayed; while the occurrence of imbedded crystals of red fel- spar, gives a porphyritic character to the rock. The beds dip from 10° to 45°, and 60°, to the south-west, the prevalent direction throughout the Ox Chain. * The explanation offered in the text accords with that proposed by the late M. Schmidt, to account for the phenomena of veins having been apparently shifted in opposite directions, with- out any intermediate break (1 C. D 1, Exposed Section, and wood-cut No. 1.); and depends upon the strike of the veins not being parallel (C C and D D of Plan). In the above case, at My- creeny, the movements are supposed to have been in the direction of the arrows, or towards the front of the cliff (No. 1. wood-cut) ; and the upper or shifted portions to have been removed. 160 ArcupEacon VeERScHOYLE on the Geology of the North Coast of In Erris, behind the vicarage at Tarmoncarra, the rock is well exposed in the cliffs. The strata range north-west and south-east, and though when considered generally, the gneiss appears to lie above the mica slate, and below the quartz rock, yet when examined in detail, frequent alternations and transitions are ob- servable, even in the space of a few perches; so that it is only from an inspec- tion of the whole deposit, its nature and character can be determined. For instance, at Annagh, the south headland of Port-na-Frankagh (French Port), mica predominates, and the gneiss approaches in aspect to mica slate, while the north point presents gneiss, distinctly marked, abounding in red felspar, with black mica; and more northward, near Scotch Port, it is studded with garnets, and the mica coalesces into small feathery crystals, while the felspar has dimi- nished into fine grains, detectable only by a magnifier. Proceeding along the shore, hornblende gradually becomes a component, and even occasionally the predominant ingredient, and sometimes the mica slate contains crystals of sahlite. Between Scotch Port and Donamoe is, however, a sudden change. A narrow fault or fissure, scarcely a foot wide, filled with a clayey breccia, apparently derived from the detritus of hornblende and gneiss, and ranging in an easterly direction, cuts through all these beds, having on the south the horn- blende schist, and on the north, mica slate, perfectly distinct, and containing those peculiar plumose concretions of mica, alluded to above. From this sud- den variation, we may conclude, that an elevation has taken place at the north side of the fault, produced, probably, hy the same operation which erupted the dykes parallel to it ; and that the mica slate and gneiss of Port-na-Frankagh, or French Port, are here forced up to the surface ; the coast rising once more into mica slate cliffs, in which the mica again diminishing and the felspar reappear- ing, the rock passes into gneiss. Oxydulous iron in lamine is met with here, accompanied by druses of felspar crystallized in oblique rhomboidal prisms. From this point mica again predominates, and Donamoe consists of mica slate. Proceeding to the northward, the mica and the felspar decrease gradually, and the beds pass into quartz rock, which, towards Erris Head, as already detailed, exclusively constitutes the sea cliffs. In the eastern part of the district, at Mulli-na-Shee, below which the road from Coolany to Tyreragh passes, the same transition from quartz rock to mica slate is seen, the latter containing an unusual ingredient, in small crystals of asbestos disseminated through the mass, and accompanied by minute prisms of felspar ; schorl and calcareous spar also sometimes occur. The beds under these abound with garnets. The entire series, from the conglomerate to the mica slate, dips about 15° or 20° to the south-east, which is the general inclination of the strata in the Ox Mountains. the Counties of Mayo and Sligo in Ireland. 161 G. Mica Slate and Hornblende Slate. H. Granite. Mica slate and its subordinate strata constitute the prevailing rocks in the Ox Chain and Erris Mountains. At the sea shore below the western declivity of the hill of Tarmon, which forms the southern point of Mullet, the slate is penetrated by granite veins. An instructive example of this interference appears in a small cove, about four yards wide, near a point called Toneadoon. At a bifurcation of the vein, a small detached fragment of mica schist, is en- tangled in the granite, the lamine being in a direction different from those of the surrounding schist. The vein is seen at both sides of the inlet, and it has rendered the schist looser in its texture, as well as somewhat friable; the laminated structure also is partially obliterated, and the mica is replaced by a mineral resembling hornblende. This change takes place gradually in the neighbourhood of the vein, which is highly crystalline, the felspar being in large rhomboidal crystals of a flesh red. The granite is laminated, the mica is greenish white, and the quartz nearly translucent ; and the layers are parallel to the sides of the fissure, but coarser and larger in the middle. It is evident, the rock has been disturbed subsequently to the formation of these veins, as a vertical slip has almost broken their continuity near the ex- tremity next to Tarmon Hill. The mica slate there dips 70° to the south, and appears to have been shifted about half the breadth of the vein. It contains also veins of quartz, sometimes four feet wide. The junction of this rock with the granite, can also be examined at an inlet north of the signal tower, the mica slate dipping 15° to the east, and the edges of the beds abutting unconformably against the mass of granite. At Doonaniron, north of Broadhaven, the quartz rock dips 60° to the south, and upon it the mica schist lies conform- ably, but distinctly separated; the quartz beds being unusually pure and unmixed with extraneous matter, and the schist abounding remarkably in mica. Mica slate prevails through the district south of Kilcommon, as far as the banks of the Owenmore ; and continuing thence to the river Munneen, the boundary probably ranges by the foot of Corslieve, Nefin, Knock-na-Ree, and Shraheen Mountains, to the Ox Range, where, in the gap of Lough Talt, beds of the schist approach in composition hornblende rock. But this is merely a local variety. Above Lough Eask garnets abound, and pinite some- times occurs; and to the eastward asbestos is found. On the north coast, mica slate forms the eastern cliff at the entrance of Portacloy, where the beds are most capriciously contorted by the influence of the first dyke; and it extends to Porturlin, but is there succeeded by quartz rock, which prevails to Benmore. At this point mica slate reappears, rifted and disturbed by the intrusion of trap, which rises perpendicularly from the sea two thirds of the height of the cliffs, and then turns off for a short distance VOL, V.—SECOND SERIES. Y 162 Arcupeacon VerscHoyLe on the Geology of the North Coast of in conformable stratification. At Balderig Inlet the mica slate disappears, re- curring no more on the coast. ty F The inferior rocks, granite, gneiss, mica slate, and quartz, just described, frequently graduate so insensibly into each other, that the observer is inclined to allow them a common origin, modified only by variations in the proportions of the ingredients of which they consist; for instance the Erris granite in most instances passes into gneiss, the gneiss into mica slate, and this into quartz rock. Below the signal tower of Tarmon, veins of that granite, how- ever, pierce the mica slate, producing decided and obvious proofs of protrusion and derangement, and at the exposed junction of these rocks the mica slate is unconformable in stratification, the edges of its layers abutting against the inclined face of the granite. I. The Trap Rocks, Porphyry, and Basalt. These are the most interesting and remarkable rocks of the district. They form dykes, unexampled, I believe, for length, directness, and parallelism, and for their varied effects on the adjacent strata*. Their strike is nearly east and west, differing only 4° or 5° to the north of west. I commence their de- scription with the most northerly, which may be distinguished as No. 1.; and proceed with my details in a direction from west to east. No.3. Strata of mica slate bent over projecting masses of trap at Attatovick Point. * See Map, Plate XI*. The points at which the dykes were actually seen are marked by a line ; and the supposed connexion or continuation by dots. the Counties of Mayo and Sligo in Ireland. 163 No. 1. This dyke emerges from the sea at Benwee Head, in Erris, where it has occasioned a slip in the cliff; and the lamine of the quartz rock are much curved and disturbed. A cavern passing through a point of the headland, and practicable by boats in calm weather only, has been formed by the decay of a portion of the dyke. Opposite the rock called Calliagh, a branch of the dyke appears as a mass of trap, enveloped in curved laminz of the including rock. Further eastward, at Doonminulla, its disintegration has produced two caves, near which the strata are highly inclined, and the trap is conformably interleaved. Crossing thence the inlet of Portacloy, it rises vertically through the point of Attatovick, the strata of which are heaved up and bent over projecting portions of trap, like doubled folds of cloth, in the manner represented in the cut No. 3, From this point it passes under the sea to Pig Island, which it penetrates, presenting in the lower part, a pervious cavern, formed by its decay, and in the upper the appearance of a wall regularly built from shore to shore. This dyke does not intersect the coast again till it passes through Downpatrick Head, where it resembles a massive facing of polygonal prisms, raised against the cliff on each side of the point. I have not traced it further. No. 2. The next dyke, to the southward, first appears in an inlet called Preeson, near Kid Island, traversing the quartz rock vertically for one fourth of its height, and then turning off horizontally in waved and irregular veins to the north and south, seems to have lifted the strata and penetrated between them. At Porturlin inlet, it forms a regular wall, piercing the precipice on the west side from the water’s edge to the summit, and so closely resembles a fence of masonry, that a careless observer might be deceived. Crossing the entrance of the creek, and traversing the eastern point, it passes beneath the sea to Benmore Head, where it rises in the face of the cliff to half its height, and then ranges horizontally for some distance, terminating at last in a wedge. It appears also in the channel which separates Horse Island from the mainland, and can be most satisfactorily examined at low water, leaning against the quartz rock at the east end of the strait. A cave is there pervious to some distance, the roof presenting a very acutely pointed arch, and the passage between the Island and the main resulted probably, from the disintegration of the strata, altered by the trap. A vertical cross vein of wacké intersects it at an angle of 70°, having at the west side a thick wall of white quartz, in many places tinged green with oxide of copper, and a few yards from this cross vein, are two small parallel dykes of trap, containing zeolite. The stratification of the island is very much disturbed, and the derangement extends to the mainland, where the strata, in the next point in Balderig inlet, are elevated at an angle increasing from 70° next the sea, to 90°, On the eastern side, this dyke inclines to the south, underlying the strata of quartz rock, with which it would appear to be interstratified, and a prolongation has been thrown out in the form of a dyke, but it cannot be traced far. The very extraordinary channel separating Illaan Maister from the extremity of Benmore Head, has been produced also by the removal of a branch of this dyke ; its disintegration having left a chasm barely sufficient for a boat to row between its perpendicular and perfectly plane walls, 700 feet high. This pass is nearly dark in the middle, but of great grandeur and singularity, and accessible only in the calmest weather. In the cliffs to the west of Horse Island are many fantastic and inexplicable appearances. ‘The dyke, rising through the beds of rock, cuts them obliquely, and sends out, at one side, a regular stratum lying conformably between the layers of quartz rock. Near this, a mass of trap, in- cumbent on the edges -of the quartz strata, which are perpendicular, penetrates between them like a series of wedges ;—the vertical layers of rock, at one side of an upright vein of trap, are perfectly regular and parallel, while at the other side they are much waved and contorted ;—masses Wane 164 Arcupeacon Verscuoyie on the Geology of the North Coast of of the whin also occur, imbedded in undisturbed and regularly stratified rock, without an appear- ance of fracture, though of the most extraordinary shapes. At Port Conoghrea the intermediate rocks commence, but their inclination and position are much disturbed by the vein, which passes thence to the south of Downpatrick Head; where it is seen to great advantage, forming an immense wall which lines the cliff from the water’s edge, and is constituted of polygonal prisms closely fitted, transversly across the dyke, their ends forming the face of the wall. On the west (east?) side of the headland it is cut through by a cross vein of coarser trap, ranging north-west; but apparently no changes have been produced by this inter- ference, On the east shore of Killalla Bay, the dyke is again found near the point of Kenisharrock, and afterwards in the cliff at Killeenduff, rising vertically from the water’s edge. Further east it appears at both sides of Aghris Head, and proceeds to the sandbanks of Strandhill, which pro- bably cover it. I have not sought it further. The course thus detailed is forty-five English miles; and to view the dyke satisfactorily, at least half this distance must be passed in a boat, as closely as possible beneath the cliffs. No. 3. Parallel to No. 2, and about two miles to the south, the third dyke emerges from the sea, near the south end of Rinroe Point, in Broad Haven, and extends by the foot of Knock-na-Ree, north of Ballisadere Bay, to Dromahair, in the county Leitrim (and probably further), a distance of about sixty-five English miles, while its breadth seldom exceeds forty feet. At Rinroe, the adjacent mica slate is considerably altered, all schistose structure having been obliterated, and the rock rendered loose and easily broken into irregularly angular fragments. It rises like a mole or pier from the water’s edge, and this resemblance is rendered more striking, by the contiguous schist having yielded to the surge for some feet at each side, leaving a narrow and deep channel, up which the sea rushes. At forty yards distance is a parallel vein, but much smaller. Both veins cross the harbour, and appear on the east side at the water’s edge. These dykes have been traced across Ballinglan, and at Poolagranny, near Kilcummin Head, they are beautifully displayed, the northern being ten feet wide, and the southern about twenty. Passing through the alternating strata of sandstone, slate clay, and coarse limestone, they have given the shale a conchoidal fracture, prismatic structure, and black colour, in short converted it into flinty slate; the sandstone has been altered also, being partially translucent, much rifted, and in prismatic masses at the point of junction. These changes having rendered the strata ex- ceedingly destructible, the surge has broken them up in the neighbourhood of the trap, and the dykes remain like ramparts of cyclopean masonry. At the east side of the creek, the beds of shale or slate clay mouldering away, have formed a cave or recess of some depth, bounded on one side by the trap vein, and on the other by the less decayed strata; the roof and sides of the cavity being covered by calcareous tufa, which frequently accompanies, and indeed often indicates the presence of trap. Over the entrance, a constant dropping of water has formed a sort of curtain or screen, The trap is here of a very coarse grain, and blackish green colour, the basis seems to be hornblende, with a sparing mixture of felspar, and is thickly studded with zeolite, in spherical concretions, and sometimes contains small nodules of green earth. The passage of these trap dykes through both inferior and intermediate rocks, proves, that the fissures which they fill, could not have resulted from the contraction of the strata in drying or con- solidating ; the same cause having divided the quartz rock and mica slate, which, according to this theory, must have been firm and solid before the deposition of the shale, sandstone, and calcareous beds. Jn the banks which rise over the creek of Poolagranny, the upper beds of sandstone are much curved, with joints open above, in the convex part of the curve, and below where it is concave, while the Counties of Mayo and Sligo in Ireland. 165 the beds beneath remain horizontal. This derangement, therefore, can have resulted only from a lateral pressure forcing the layers of stone horizontally, but acting superficially. Such is the ap- pearance exhibited in the hill north of Poolaclogher, on the east of Kilcummin headland, especially at a point near the landing place, represented in the accompanying wood-cut, No. 4. Contorted strata of shale and grit north of Poolaclogher. At Poolaheny, on the east side of Killalla Bay, the course of this dyke is often obscured by the drifting of a shingle-beach, but it is found to the east of the mouth of the Dromore River, on the coast of Tyreragh, preserving the same characters, and influencing the adjacent rock in the same manner. Thence, holding its direct course to the south-west of Aghris Head, and rising from the water through the beds of rock covered at high tide, it is seen for about 200 yards, but on reaching the shore, the sand banks and soil prevent further observation; and the dyke is concealed to the picturesque chasm, called the Glen, produced by it in the side of Knock-na-Ree. The soil and the fallen rocks which have been thrown together and levelled to form a walk through “ the Glen,” obscure the trap except at a few points, where it may be examined satisfac- torily. To judge from the present appearance of the rift, it was never filled to the brink with trap; as the sides would close together with scarcely any void, the projections of one face coinciding ac- curately with the recesses of the other. I have next observed this dyke below the village of 166 Arcupeacon Verscnoy.e on the Geology of the North Coast of Dromahair, in the county Leitrim, running parallel to the river, which falls into the east end of Lough Gill; and here an unusual change occurs, the material of the vein consisting of vertical layers of serpentine. The mica slate, when in contact with the vein, presents a bright red colour, and crumbles between the fingers, as if it had been intensely heated; and veins of asbestos occur abundantly in the dyke between the coarse laminze which compose it. The schist rises towards the vein at each side, as if it had been elevated by a force from below, and the serpentine forms a narrow line of hill along the river, where its stream turns to the eastward, opposite Friarstown, about half a mile from the town. I have not traced it further, but there is no appearance of a termination. No. 4. This dyke is found in the west side of Erris Head, where a pigeon hole (as those caverns in the cliffs, with an opening in the roof are called) has resulted from its disintegration. It appears again at the opposite side, rising from the water’s edge to the summit of the precipice ; and it crosses Broad Haven, but the drifting sands at the mouth of the Glanamoy River conceal its course, as do the bog and moor to the valley of Ballinglan. At the last locality, the shale and grit beds are much deranged by its influence, the shale being indurated and converted into a black quartzy chert, rifted most irregularly, and the crevices are filled with quartz, highly crystalline, and shooting into hexagonal pyramids; and the layers of grit are disturbed and fis- sured. It is prolonged thence to Kilcummin, appearing in the road on the west side; and traver- sing the head it is seen among the rocks on the sea shore, near Castlemagee. It is there por- phyritic, being chiefly composed of large tabular concretions of felspar, and contains augit and green earth. On the east shore of Killalla Bay, it passes through the limestone, and may be ob- served further east, at Conquil Bridge, and is well displayed at Dromore West, having there raised up the limestone at each side, altered the colour, and rendered the structure more granular. It constitutes the fall in the river close to the bridge; beyond which the stream runs in a deep ravine, caused by the decomposition of the limestone, but the dyke lines one side of the bank some distance below. It has been observed by Mr. J. Wynne, of Hazlewood, at Dromiskeybole, near the west end of Lough Gill; and in the pass through Slish Mountain, close to the Ballintogher road, it either sends a branch to the north-west, or is crossed by another dyke. I have, as yet, been unable to determine this point, but a ridge of serpentine is found there, near and parallel to the road, for the repair of which it furnishes the material. There is almost an identity between specimens from this site and those from the Dromahair dyke ; they are both laminated, both con- tain asbestos, and agree in colour and hardness. My examination terminated here. No. 5. This dyke first appears as a singular and picturesque narrow stair-case of prisms, ascend- ing from the sea between two high walls of indurated mica slate, almost porcelainised by its contact, and the schistose structure is obliterated. The steps consist of short columns, lying horizontally across the vein, from side to side. Penetrating the peninsula of Erris, and crossing, eastward of Broad Haven, the district of Kilcommon, the peat and soil conceal its course, till it appears in Ballinglan, where it can be traced up a ravine through which a stream flows from the moory summit of Knock Aghleeg ; and on the east side of that hill, it crosses the stream of Carrickanass, traversing the beds of sandstone without any apparent effect. It continues thence by Rafron and Ross to the Bay of Killalla, passing for some distance through the bed of trachyte, where it assumes the appearance of basalt, black, fine-grained and prismatic, in one place regularly columnar, and the pillars are as neatly defined as those of the Giants’ Causeway, but their axes are nearly horizontal, being at right angles to the walls of the vein, In Palmerstown River it appears like three walls of polygonal prisms, built in contact with each other; and the surrounding rock having been de- composed and washed away, its construction is laid open. The prisms where weathered, peel off the Counties of Mayo and Sligo in Ireiand. 167 easily in concentric layers, but they increase in hardness as the interior is approached, where they are extremely tough and refractory. ; The appearance of this fifth dyke, on the east shore of Killalla Bay, is attended with peculiar and instructive circumstances (see the accompanying wood-cut, No. 5.). Rising through the carboniferous limestone, it destroys the colour as usual, but about four feet from the surface the limestone strata above the dyke are much shaken and disturbed, and the trap has turned off late- rally beneath this disturbed mass, and divided into small nodules, cemented together by calcareous spar, thus forming a conglomerate. A careful examination has convinced me that the trap, on reaching the point where its ascent ceased, became mingled with fused limestone, the carbonic acid of which was separating abundantly from the diminution of pressure. The conglomerate could not have been produced by infiltration, because the cement occupies more space than the nodules enveloped by it, which are not in contact. The further course of this dyke has not been ob- served, Trap dyke in carboniferous limestone east side of Killalla Bay. No. 6, the next dyke in succession, commences at the sea, near the vicarage of Tarmoncarra, in Erris, and has caused one of those caverns, called Pigeon-holes. From its direction, this dyke may probably be identified with that which appears opposite to the mill of Tully, above the bridge, on the Palmerstown river, penetrating the sandstone strata, a few yards from their junction with the overlying limestone; and is seen again at the coast guard boat harbour at Enniscrone, on the east side of Killalla Bay. It is there twenty feet wide, and has rendered the limestone white and compact for several yards at each side, but the calcareous strata gradually resume their usual dark grey colour. I have not searched for the continuation of this vein. No. 7. dyke begins in mica slate at Annagh in Erris, and crosses to Bel Mullet, where it is found on the shore a little north of the town. It reappears in the new road to Ballinglan, south-west of Killalla Bay, and afterwards in the inlet below Moyne Abbey, where are five parallel branches 168 Arcupeacon VerscuHorLe on the Geology of the North Coast of which have produced much derangement in the rock, and apparently contributed to the sub- sidence in the neighbourhood of Killalla, from the mouth of the river Moy to the bridge at Pal- merstown. The abrupt facade of oolitic limestone, from near Moyne by Kilroe to Castlerea, appears to be a portion of the undisturbed stratum, while the broken and sunken beds of rock which skirt the shore, and the depression which is covered by the tide within the Island of Bartra, seem the result of a subsidence. One of the veins of trap below Moyne differs in composition, containing calcareous spar and olivin, and breaking with a compact fracture, while the others are externally decomposed, very friable, and abound with small concretions of zeolite. No. 8. The point where this dyke might probably first be seen in Erris, is covered by drift sand, but on the south shore of Broad Haven, below the road near Derracorib, it has tilted the strata into a vertical position. It is well seen near the Glebe House at Mullafarry, south of Killalla Bay, where it consists of concentrically foliated spheroids, weathering in successive coats, and surround- ing a very tough, crystalline nucleus. The limestone, as usual, is white, friable, and earthy near the dyke. This vein was exposed near Annaghmore, during an alteration in the road at Ardcree Bridge. Its possible range further east will be alluded to hereafter. No. 9. dyke is seen near Ballybroony, south of Killalla Bay, and crossing the Moy, traverses the glebe land of Killanly. The limestone is converted by the dyke into a calcareous breccia of angu- lar fragments cemented by calcareous spar, as if heat had rifted and cracked the rock, among the fragments of which, fused limestone had been then injected. No 10. crosses the valley of Glencastle in Erris, near the eastern end of the bridge, the parapet of which abuts on the vein. It penetrates the mica slate, and the beds are much waved and con- torted as the dyke is approached; but at the meeting of the trap and schist, the latter is decom- posed to a ferruginous clay: the dip also is altered from about 45° north-west to 80° north. It contains quartz veins abundantly. It is seen again along the side of the road near Netley Park, and crosses the river Moy near Bunree, the marl or calcareous tuff indicating its presence ; it is also visible in the mail-coach road to Dromore. No. 11. This dyke traverses the peninsula of Erris, appearing on both the west and east shores, and produces considerable alteration in the hornblende rock at Leam, which is rendered so nearly identical with the trap, that it is difficult to distinguish the exact boundary. A dyke is seen on the right bank of the Moy, about a mile from Ballina, on the road to Dromore, and probably is the continuation of this. I have not sought for dykes to the southward of Ballina, but I think it very likely that many may be found; I have heard that one is visible near Castlebar. K. The Trachyte Formation. 1 have not seen any notice of the occurrence of this rock in the British Islands; but the use of the term has been sanctioned by the authority of Mr. Poulett Scrope, as applied to the formation in question ; and I take this opportunity of acknowledging the kind aid of his opinion. It is found in Ross, north of Killalla. On tracing the coast southward from the mouth of Palmerstown River, a bold sandstone rock rises suddenly from the beach in irregular but Jevel strata, which, however, soon dip to the south in a confused and fractured state, and are followed by a mass of trachyte composed of glassy felspar in irregularly quadrapgular tables, mingled with black augit in laminar concre- the Counties of Mayo and Sligo in Ireland. 169 tions, the plates of which are generally parallel, reflecting the light at the same angle over the surface of the specimen. Quartz in hexagonal pyramids also occurs, as well as green earth, lepidolite, and different zeolites. Near the middle of the mass, which is about 1100 yards wide, the felspar becomes opaque, yellowish grey, and regularly crystallized in rectangular prisms, the augite diminishing in quantity, and the zeolites and quartz increasing ; but on approaching the southern boundary the augite predominates, and the felspar resumes its transparency and greyish colour. Near the limits of the mass, changes gradually take place, the grain becoming closer, and the crystals di- minishing in size, till the trachyte can scarcely be distinguished from the sandstone. The latter rock also becomes more compact and harder at the junction, while the shale passes into Lydian stone, and the stratification is much deranged, the dip being towards the trachyte on both the north and south limits. A small dyke or vein is seen at the southern part of this bed, having nearly an east direction. A few yards from the point where it emerges from the bank, it is broken across and discontinued, but about three feet to the south, occurs ‘again in the same direction. This lateral shift or removal, is twice repeated before it reaches low-water mark, and suggests the idea of successive horizontal slips having taken place, from the north, after the consoli- dation of this vein and the including rock. The trachyte is continued across the lands of Ross to the Palmerstown River, where it forms the bank for some distance, and its junction with the sandstone is well displayed under the old church of Templemary on the opposite shore. Having been protruded late- rally, it lies above, and at the plane of contact a substance is interposed resembling fine clay slate, except in the lamellar structure. Could this inter- vening layer have proceeded from fusion of the sandstone alone, or from its component parts mingling with those of the liquid trachyte in the proportions which form clay slate? Analysis might determine the question. Augite here predominates, and the rock graduates into a coarse basalt in jointed columns. Ascending to the cross-roads at Mullinacrush, the bed approaches more to porphyry, being almost entirely composed of glassy felspar in thin tabular crystals laterally compacted together, and in detached portions presenting a schistose aspect, but in the mass rising in blocks like granite, without any approach to stratification. It contains very sparingly, zeolite, chalcedony, iron pyrites, and augite. It occupies the summit of the hill, not, however, ex- tending far to the westward. On the opposite shore of Killalla Bay, I found the trachyte on the lands of Cahirvove, bounded by limestone, upon which it appears to lie; but no seam divides the two rocks, which are mingled irregularly at their junction, the limestone containing both felspar and VOL. V.—SECOND SERIES, Z 170 ArcupEacon VERscHOYLE on the North Coast of Mayo and Sligo . augite. At this side the character of the bed differs slightly from that of Ross, being more varied in structure, and might be applied to ornamental pur- poses, if not too hard to be wrought satisfactorily. The felspar, which occurs abundantly at Ross, presents unusual varieties in the crystallization. The crystals appear to be rectangular prisms, having the terminal angles replaced by triangular planes; but on close inspection they are found to consist of two or four prisms attached laterally. Striz may be seen with a magnifier on the planes parallel to the edges of that replacing the angle of the prism ; and as these strie diverge from the line of junction, the crystal has a feathered appearance, as represented in the wood-cuts. The conditions under which the complicated arrangement of the ultimate particles, and of the simple and com- pound crystals were effected, apparently indicate per- fect tranquillity, complete fusion, and very slow cool- ing of the mass. This conjecture is supported by the fact, that the most perfect crystals are found about the centre of the bed, the part which would longest retain its heat and fluidity. The occurrence of trachyte (a formation hitherto unobserved in the British Islands) at the shores of the bay of Killalla, is an interesting discovery. Of the period when the rock was formed, it can only be said with certainty, that it is newer than the mountain limestone, and older than the system of trap dykes, as it lies on the former, and is penetrated by No. 5, one of the latter. OS eee ee — oe ee *y > > > wen “se ~~ ‘g Ss i Fite _ XII.—Description of some Fossil Crustacea and Radiata, found at Lyme Regis, in Dorsetshire. By W. J. BRODERIP, Esq., F.G.S., F.R.S., &c., V.P.Z.S. [Read June 10, 1835.] LorbD COLE and Sir Philip Egerton having placed in my hands some fossils, which they have lately found at Lyme Regis, I proceed to describe those which appear to me to be new. (See Plate XII.) 1. CrusTACEA. The first of this class to which J shall call attention is a crustacean, which must have been of considerable size, and which, from its form, appears to me to be very interesting. Though the post-abdomen, or tail, as it is vernacu- larly called, is entirely wanting, enough remains of the anterior parts to in- dicate in a satisfactory manner the organization of the animal, and its place among its congeners. The lamelle of the external antenne would show that it was a macrourous decapod, of the Shrimp family (Salicoques of the French), and the chele have some characters approaching to those of Pale- mon ; but the absence of the serrated rostrum and the presence of other cha- racters forbid us to arrange it under that genus. The middle notch of the carapace, and indeed the general form of that part are very like Palinurus. If the habits of this animal may be considered to have approached those of the Shrimps (and the very thin armour of the carapace would lead a good way to this conclusion), its remains are those of a comparative giant of that race, fit to grapple with the decomposing flesh of the Enaliosaurians. Upon the whole evidence the place of this animal appears to me to be between Palinu- _rus and the Shrimps, and its organization leads me to consider it as a crusta- cean sui generis*. I have named it in honour of Lord Cole, whose zeal in * M. Milne Edwards, in his Histoire Naturelle des Crustacés (tom. ii. p. 337.), gives the cha- racters from my description in the “ Proceedings,” and says, “ Le Genre Coxera, établi réecemment par M. Broderip, d’aprés un Crustacé fossile du Lias, n’est aussi qu’ imparfaitement connu, mais nous parait devoir étre intermédiaire entre les Astaciens et les Salicoques ;” and he, accordingly, places it between Nephrops and Crangon. When M. Milne Edwards wrote, the smaller but more perfect specimen with the post-abdominal segments was not known to me, nor were Zz 2 172 Mr. Broperir on some Fossil Crustacea and Radiata collecting is only equalled by the liberality with which he applies the riches of his museum to the advancement of science. Since the above was written, Mr. Lonsdale forwarded to me another spe- cimen from Lyme, which upon examination turned out to be a young indivi- | dual of the same species, having the post-abdomen or tail zm situ, and the other parts comparatively perfect. This specimen, which is in the Museum of the Geological Society, so entirely corroborates the view which I had formed from the examination of Lord Cole’s large specimen, that I have only found it necessary to add the description of the post-abdominal segments*. Co.LeEliaA. Generic Character. Antenne. Base of Mesial antenne (antennz interne) not extending beyond the anterior spine of the thorax ; each antenna terminated by two annular setz, the external sete being the longest. External antenne provided with a large and wide scale; the terminal sete large, but the length undetermined. Eyes, pedunculated, directed outwards, approaching in their situation and form to those of Palinurus. Thoraz (carapace), thin, divided transversely by furrows indicating the different regions, tuber- culated, spinous at the sides, and with three deep emarginations anteriorly, the middle one the largest, each of the four anterior angles produced into a strong spine. Feet, First pair long, slender, the cubit (cubitus) with small spines or serrations on the in- ternal margin, and terminated externally by three strong spines. Hand (manus) elongated, slender ; digits slightly incurved, filiform, unarmed, pointed. Post-abdominal segments, tuberculated and strongly marked by transyerse ridges. Caudal lamella approaching in their form to those of the salicoques or shrimps. Species. Coxi1a ANTIQUA. Mus. Cole. PI. XII. fig. 1, 2. Found in the lias at Lyme Regis by Miss Anning. I have next to notice a fragment of the post-abdomen of another macrou- rous decapod, approaching in its sculpture nearest to Palinurus. This crus- either of the figures which now illustrate this part of the paper published. M. Milne Edwards in giving the description seems to think that the carpus, not the cubitus, was intended by the author, when he describes the joint as having small spines or serratures on the internal margin, and as being terminated by three strong spines; for M. Edwards writes, “le cubitus (Carpe ?) garni de petites épines,” etc. It is the cubitus that is so armed. (Sept., 1837.) * This interesting specimen was the property of Alfred Cloyne Austen, Esq., F.G.S., who left it with Mr. Lonsdale to be described. When Mr. Lonsdale informed him that it was introduced into the plate illustrating this little memoir, he most liberally presented it to the Geological Society. found at Lyme Regis, in Dorsetshire. 173 tacean must have been of large size, as large as that of the common Palinurus (sea crawfish of the shops)*. From the lias. A series of specimens next claims our attention; but the state in which they are renders it difficult to lay down any generic character. The remains are those of another macrourous decapod of a rather small size. The chele and legs are washed away, and the carapace is very obscure. Two of the specimens however present a curious phenomenon. In these the accurate observer will see the breathing organs of this delicate crustacean, after an inhumation of thousands of years, presented to him in a petrified state. The tips of the four larger branchiz, and of the four smaller ones below, may be observed pointing towards the situation of the heart, and these branchiz show that the crustacean before us did not belong to the Amphipoda, but to the highest division of the Macroura. The spines are like those of Crangon salebrosus ; and the general organization, so far as it is presented to our view, reminds us of the arctic forms of the Macroura. Iam aware that the information afforded by these specimens, though it is of a highly interesting nature, is only scanty ; but there is enough to satisfy me, and indeed to convince my friend Mr. Owen, whose attention to this branch of natural history makes his opinion of great value, that these crustaceans evidently belonged to the salicoques of Latreille. I am inclined to think that two of the specimens are specifically different from the others, and in one a monodactylous leg is preserved. ‘T'wo of those which afford the best information on the subject of the petrified branchia are figured Pl. XII. fig. 3, 4. These crustaceans were found immediately below the town of Lyme, on Broad-ledge, which consists of a bed of finely laminated lias shale. They were associated with Pholidophori, viz. Bechet, latiusculus and medius; and also with several species of Tetragonolepis and Dapedium, and with remains of Ichthyosaurus and Plesiosaurus. 2. Rapiata. Genus Ophiura. The specimens of this Ophiura, which I believe to be undescribed, were found about half a mile west of Bridport Harbour, in masses of micaceous sandstone which had fallen from the cliff to the beach. (See Mr. de la Beche’s section, Trans. Geol. Soc. vol. ii. pl. III. 2d series.) Mr. Lonsdale considers * The figure of the imperfect remains of a crustaceous animal, from the cabinet of Miss Phil- pot of Lyme (Trans. Geol. Soc. vol. iv. Pl. II. 2d series), does not afford sufficient information for accurate comparison. ~ LWA Mr. Broperip on some Fossil Crustacea and Radiata. the bed to be a member of the lias, between the alum shale of Yorkshire, and the lias of the west of England. He considers the lower part of the sand, repre- sented in Mr. de la Beche’s section, to be the marlstone of William Smith ; and the bed of grey marl to be the representative of the alum shale of Yorkshire. OpuiurA EGERTONI. Oph. radiis tereti-subulatis, articulis superné subtrilobatis, disco sub-plano, subpentagono, rotundato*. Mus. Cole.—Egerton. Pl. XII. fig. 5, 6, 6*. This species approaches very near to Ophiura texturata, nor is it at all improbable that the living Ophiura may sometimes rest on the remains of its ancient fossil congener ; for Lord Cole and Sir Philip Egerton dredged up the recent animal from the trawling ground at Lyme. Some of the specimens have been weathered to a nicety, and these display in a beautiful manner the articulation and structure of the animal. Others are surrounded and clogged with the matrix, and this is only noticed that the different appearances may not lead to a supposition that there is among them more than one species, viz., that which I have named after the indefatigable Sir Philip Egerton, who worked the specimens out with his own hand. Since the above was written Lord Cole has found some very small individuals. Ophiura Egerton: differs from Ophiura Milleri of Professor J. Phillips, inasmuch as, among other differences, the disk of the latter is lobated, according to the figure given in the ‘ Geology of the Yorkshire coast,” Plate XIII. fig. 20. There is no description; but there is authority for con- sidering the figure to be correct, though it is stated to have been drawn from separate parts f. Genus Cidaris. Several specimens of this genus are among the collection submitted to my observation. ‘They appear to me to be the same species in different stages of growth, and may be identical with that figured as an Echinus by Mr. de la Beche, in the Trans. Geol. Soc. vol. ii. Pl. 1V., 2d series. I have not seen the specimen, but the proportion of the mamilla, or ball of the spine joint, as given in the figure, is larger than that of the same part in those before me. Ciparis BrecHet. Cid. testa subglobosa, mamillis parvulis, spinis elongatis, aculeatis. Mus. Cole.—Egerton. I have named this cidaris after my friend Mr. de la Beche, whose geological works are too extensively known and valued, to require more than an allusion to them on my part. * The reader must remember that the external surface is abraded, in the specimen from which the description and principal figure are taken; and that in its natural state, the disk had probably a more rounded form. + I have not been able to procure a sight of the fossil Ophiura, in the museum of Mr. Matthew Wright of Bristol, from the lias on the banks of the Severn in Gloucestershire, and the cast does not convey sufficient information for comparison. Professor Sedgwick has been good enough to forward to me three specimens of Ophiura, which he had procured from Miss Anning. They appear to me to be all Ophiwre Egertoni, — — a ae ——— Pig 1 a & b Tarsometatonsal bone of wfofsu bird: p 777 35 and Fofsl brds bones p 177 7 ie as LI ery ih ry. efyn fy nt Thaa Fa Lov est | ; Te ett _ Prenton’ by CHa lig 2. La somieaarsad of the Llvevon ( Ardew concrow/ 4 Dustad eatrvemity of the Lars 0 -Mennevs: once Re [ 1% ] XIII.—On the Bones of Birds discovered in the Strata of Tilgate Forest, in Sussex. By GIDEON MANTELL, Esg., L.L.D., F.R.S., &c. [Read June 10, 1835.] TuE remains of birds are so seldom found in a fossil state, that a notice of unquestionable relics of this class of animals, however imperfect, cannot fail to be interesting to the geologist and comparative anatomist. Mr. Lyell has well remarked in his Principles of Geology*, that it might readily have been anticipated, that the fossil bones of birds would be of rare occurrence, since the power of flight possessed by these animals, preserves them from many casualties by which quadrupeds are destroyed and imbedded ; and that even when birds are drowned, or chance to die on the water, the tubular structure of their bones, and their feathery coverings, would generally occasion them to float on the surface, until their carcases were devoured. We find, ac- cordingly, but very few authenticated examples of fossil birds, certainly none (with the exception of those which it is my present purpose to describe) that can be referred to strata of an earlier period than the gypsum beds of the Paris basin}. It is true that the thin fragile bones which occur in the slate of Stonesfield were formerly assigned to birds{, but all these are now known to belong to Pterodactyles. Soon after my attention was first directed to the fossils of the Wealden of the south-east of England, I discovered in the strata of Tilgate Forest, several bones of such extreme tenuity as could have been required only by animals intended for flight, and some of these, from their close resemblance to the tarso-metatarsal bones of certain Gralle or waders, I was induced to refer to birds§. But when the correctness of the opinion of the late Mr. Miller, that the Stonesfield bones belonged to Pterodactyles, was established, it was naturally conjectured, that the fossils from Tilgate Forest might also have been derived from flying reptiles; and Dr. Buckland expressed a doubt * Principles of Geology, 5th edition, vol. iii. p. 230. + Oss. Foss., 5me edit. tom. iii. p. 303. { Geology of England and Wales, p. 208. § Geology of Sussex, 1822. Fossils of Tilgate Forest, 1827. 176 Dr. Mantett on the Bones of Birds, “‘ whether there were any certain evidence of the existence of fossil birds in strata more ancient than the tertiary*.” Having subsequently discovered a few specimens with more decided characters, I was led to resume my former opinion, the accuracy of which was confirmed by M. Cuvier, during his last visit to England, who pronounced, without the least hesitation, that the spe- cimens were the bones of some wader, probably a species of Ardea, or heron. Yet, notwithstanding this high authority, the imperfect state of the specimens induced some eminent naturalists to regard the question as still undeter- mined ; their scepticism however will, I trust, be now removed, by the recent discovery of a bone, which, as will hereafter be shown, can be no other than the tarso-metatarsal of a bird. A short time since, my friend Mr. Lyell and myself, being engaged in some investigations relating to the fossil bones of turtles, the supposed birds’ bones of the Wealden again came under our notice ; and as the subject was of deep interest, the presumed existence of birds during the period of the secondary formations, resting solely on the evidence afforded by the specimens in my collection, we determined to submit the most characteristic bones to the ex- amination of Mr. Richard Owen, of the Royal College of Surgeons, a gentle- man whose profound knowledge of comparative anatomy, is only equalled by the liberality with which he imparts his valuable information to others. Mr. Owen’s attention was first requested to the metatarsal bone above mentioned, and particularly directed to the oval cicatrix (9, fig. 1. 6, pl. XIII.) and the longitudinal ridge (x, fig. 1. 6) observable in that specimen, both of which are very peculiar characters. The following observations are the result of Mr. Owen’s examination : “ This fragment (fig. 1. b) is undoubtedly the distal extremity of a left tarso-metatarsal bone of a bird. The oval spot (0,) denotes the articular surface or place of attachment of the posterior or opposable toe, and is a mark of more than ordinary importance, since much may be deduced of the habits of the bird by observing its relative situation to the articular surfaces of the other toes. Thus, in an insessorial, or climbing bird, it is placed nearly on a level with the others, that the back toe may be effectually opposed to the fore toes ; and the same obtains in the raptorial birds for seizing their prey. I infer that your specimen belonged to a wader, and that the back toe was a long one, the better adapted for supporting the body on a marshy soil. The thin longitudinal ridges of bone in the fossil, also agree with what may be observed in the metatarsals of birds; they afford attachment to the aponeurotic thecze, which tie down the tendons as they glide along the metatarsus to the toes. As the soft articular extremity of the bone has been destroyed, it is probable the bird was young, and the epiphysis not anchylosed. Another of the specimens is very like the head of a humerus ofa bird, but differs from any in the museum * Geol. Trans., 2nd series, vol. iii. p. 220. { ; jrom the Strata of Tilgate Forest. 177 of the College, in the sudden expansion of the head. Fig. 3 appears to be the proximal end of a tibia. In others of the long bones from the Tilgate strata, there are longitudinal grooves which accord with what is observable in the metatarsal bones of birds, but similar grooves appear also to characterise most of the long bones of Pterodactyles. However, the metatarsal bone (fig. 1, a, b,) settles the question in my mind as to the existence of the remains of birds in the strata of Tilgate Forest.” The confirmation of my opinion, first by the immortal Cuvier, and now after a rigorous examination of other specimens, by Mr. Owen, must I con- ceive remove all doubts on the subject, and the occurrence of the remains of birds in strata antecedent to the chalk, be henceforth considered as unques- tionably established as that of mammalia in the Stonesfield slate. I proceed to describe the specimens of birds’ bones in my possession ; they are but few in number, and unfortunately all of them are more or less imper- fect, the extreme thinness of the bones, and the compactness of the rock in which they are imbedded, rendering it impossible to extricate them without injury. Tarso-metatarsal bone of a Wader, P\, XIII. figs. 1, a, bs\—This is the most important spe- cimen hitherto found; it consists of the two extremities only, the shaft of the bone having been crushed, and a considerable portion of it, perhaps four or more inches, lost. Its circumference is three times that of the corresponding bone of a heron. The annexed sketches illustrate its most essential characters; the distal extremity, fig. 1, 6. is represented on its posterior aspect: o, shows the oval depression for the articulation of the hind-toe, or thumb: x, a ridge for the attachment of the aponeurosis of the tendinous sheath which embraces the tendons passing down to the foot : fig. 1, a, anterior view of the same specimen. * Tibia ? or metatarsal.” Cuvier. Pl. XIII. fig. 6—A slender bone, six inches and a half in length, the head of which is partially exposed ; the distal extremity is wanting. Fragments of similar bones are represented, Pl. VIII. figs. 1.18. Fossils of Tilgate Forest. Tibia? Pl. XIII. fig. 3.—The head of a tibia(?): this specimen is figured PI. VIII. fig. 11. Fossils of Tilgate Forest. Ulna.—I have two fragments of cylindrical bones, apparently portions of the ulna, each having a small tubercle, like that observable in birds for the attachment of the quills of the secondary feathers ; but these specimens are too imperfect to warrant any positive inferences. Such are the scanty materials from which I venture to infer the existence of birds during the Iguanodon epoch; and if my deductions be correct, another beautiful instance is afforded of the light shed by anatomical science on the obscure records of the early history of the earth. ins! > VOL. V.—SECOND SERIES. * a 7 ° ; a incall) ‘ ) ea € t *F ; % a a 4 a P a.) ¥ a%-5 a is 5 pinned i ¢ e. fesinde ; al pevaaal bel) WW bid &Y. ‘ ' Pee ™ Re Ley ; ee i wi pin suit ett ot Hninneyes, } te i ey ; . ue wine Oe 5 [1799] XIV.—On the Syenite Veins which traverse Mica Slate and Chalk at Goodland Chiff and Torr Eskert, to the south of Fair Head, in the County of Antrim. By RICHARD GRIFFITH, Esg.,F.G.S., M.R.I.A., P.G.S. of Dublin, &c. [Read January 6, 1836.] THE geology of the northern portion of the county of Antrim, has been often treated of; but there are several interesting facts, which have appa- rently escaped the attention of preceding observers. One of the most import- ant was described by me in the Geological Section at the late meeting of the British Association in Dublin; and I have since revisited the place, accom- panied by my friends Professor Sedgwick and Mr. Murchison, at whose re- quest I have prepared the following memoir for the Geological Society*. The part of Antrim to which this paper refers, is situated between Fair Head, on the north, and Cushleake Mountain, on the south. The geological structure of the country is exhibited in the accompanying section, No. 1. It will be seen, that mica slate forms the substratum or base No. 1. FAIR HEAD LOUGH FADDEN 612 Fee a e b a, Mica slate; b, coal shale; b with dots, coal sandstone ; c, new red sandstone; d, chalk ; e, trap, or syenite. of the country; that secondary rocks, belonging to the coal formation, the new red sandstone, and chalk rest upon it unconformably ; and that these secondary rocks are surmounted by an overlying mass of rudely columnar * These veins, together with that at Torr Eskert, were originally observed by Mr. Nicholson, one of the first class of valuators employed on the general valuation of Ireland. 9a? 180 = Mr. Grirritu on the Syenite Veins which traverse Mica Slate trap, which at its northern extremity, forms the magnificent promontory, called Fair Head. P The mica slate is distinctly bedded, and passes from a fine-grained, shining, slaty rock, into a coarsely granular gneiss. Its subordinate strata are hornblende slate and schistose limestone ; the latter occurring in several places, particularly on the sea shore, close to the south side of Torr Point, and on the shore at West Torr. At Goodland Cliff, near the northern extremity, the dip is north-west, at an angle of 15° from the horizon, and the subordinate beds of schistose limestone and hornblende slate dip conformably with the mica schist, and are consequently con- temporaneous portions of it. Other rocks containing hornblende are, however, frequently associated with the mica slate, and though apparently imbedded with that rock, are veins which have been intruded, subsequently to its formation. This is particularly the case at Torr Point and other localities, one of the most remarkable of which is on the sea shore, half a mile to the south of the commencement of the mica slate in Murlough Bay, where are two decidedly intruded veins of syenite, which pass into syenitic greenstone. (See the following cut, No. 2.) No. 2. Syenite veins (¢) passing through mica slate (a), in Goodland Cliff, south of Murlough Bay. These veins pass obliquely through the mica slate, in the face of the stu- pendous cliff of Goodland, which is upwards of 500 feet high, and for the greater part nearly perpendicular. They are clearly visible along the face of the cliff for more than half a mile. At the sea shore, the veins appear to range so regularly and conformably with the strata of mica slate, both in strike and dip, that if not closely examined they might be considered subordinate beds; but on minute inspection, it will be found that the edges —_— —— and Chalk at Goodland Cliff and Torr Eskert. 18 are frequently rough and saw-like ; and that the projections are filled by sy- enite, continuous with the mass; and the indentations in the veins with mica slate, having a tortuous structure. On tracing these veins as they gradually ascend the cliff to the south-east, their true nature is at once discernible. There, they may be seen pursuing undulating courses, neither parallel to each other nor to the laminz of the mica slate; in some places approaching to within four feet, but in others, being more than twenty feet apart. (See cut, No. 2.) About 150 yards to the south of the point, where the veins meet the sur- face of the ocean, and where the lowest has reached the height of about 120 feet, the cliff is fractured by a great fault, or downthrow of the strata to the north ; and by means of which the cliff is accessible. To the south of the fault, the veins are at about 100 feet higher Jevel than to the north, and it is remarkable that to the south of this point three veins are observable, instead of two, by the introduction of a small vein, which, when first observed, is in contact with the upper surface of the lower vein, but gradually diverging from it, approaches the upper vein, and afterwards descends a second time towards the lower vein. The accompanying sectional view, No. 3, was taken a short distance to the south of the fault. At this place the upper vein is about five feet thick ; the middle is fourteen inches, and the lower about seven feet ; and the distance between the upper and lower veins is fourteen feet, including the middle vein. SVU sah -— —— ATi J A ‘ S} = Sj ‘gy y SS f 4 ‘ = Wifi Q es | ntl t i AMT ‘Vasil d) Syenite veins (e) traversing mica slate (a) in Goodland Cliff, south of Murlough Bay. SS 182 Mr. Grirrits on the Syenite Veins which traverse Mica Slate The mass of the upper and lower veins is composed of dark green, crystallized hornblende, brownish red felspar, and occasionally quartz. The rock may be said to be finely grained. The hornblende is crystallized in long six-sided prisms ; and the felspar exhibits its usual rhomboidal structure, but no distinct crystals. It is to be observed, that the hornblende is more abundant near the upper and lower parts of the vein than in the centre, and a regular transition between syenite and greenstone, is observable in the mass of the vein. This variation is most remarkable in the thin centre vein, which contains much black hornblende, and some black quartz. This vein is also peculiar from its presenting oval-shaped masses, from two to ten inches in diameter, and about one third as thick, composed of crystalline greenstone, enveloped in a congeries of plates of pinchbeck brown mica. In one or two places, I observed a tendency to similar structure in the upper vein. When seen at a distance, the upper and lower veins present a rudely colum- nar structure, the prisms being at right angles to the inclination of the veins. Syenite, similar in every respect to the upper and lower veins, occurs near to the summit of Torr Eskert Hill, about half a mile to the south of Goodland Cliff. (See wood-cut, No. 1. p. 179.) Owing to the covering of diluvial matter, the surface soil, and herbage, it is impossible to trace the syenite veins of the coast to this point; but in lay- ing down the line of the veins of Goodland Cliff on the Ordnance Map, and making due allowance for their average inclination, and the elevation of the hill, I entertain no doubt that the syenite of Torr Eskert, is a prolongation of one of the veins of the cliff. Torr Eskert Hill is about 970 feet above the level of the sea. Ata distance, it presents a bold escarpment to the north, and in this respect exhibits a cha- racter quite distinct from the comparatively tame outline and green acclivities of the neighbouring chalk hills. Its summit is composed of strata of compact chalk, dipping east, at an angle of 5° from the horizon; and is divided into three perpendicular escarpments, having sloping terraces between them. The vertical portion of the two upper escarpments, may each be about ten feet in height ; and that of the lowest is also ten feet, but its upper half is composed of indurated chalk, and the lower of syenite, a part of which is rudely co- lumnar. This syenite cannot, either in external aspect, or in internal structure, be distinguished from that of the cliff, and the same transition into syenitic greenstone is observable. Having made an excavation and cleared away part of the surface soil and grass, both above and beneath the syenite, I ob- tained the following section. Commencing from the top; compact chalk, five feet* ; syenite, five feet; an irregular bed of chalk, from nine inches to one * The grain of this chalk is closer and more compact than that of the chalk forming the summit of Torr Eskert. and Chalk at Goodland Cliff and Torr Eskert. 183 foot; containing quartz pebbles, green sand, and numerous, red, siliceous grains, some of which resemble garnets, and others carnelians. This stratum rests on soft, leafy, mica slate, regularly stratified, and dipping north-west at an angle of 10° from the horizon. The syenite is divided into large masses, which in several places are sepa- rated by intervening chalk, containing quartz pebbles and green sand, also numerous fragments of the fossils, usually met with in the green sand of the north of Ireland. The views, Nos. 4 and 5, represent the connexion of the chalk and syenite at Torr Eskert. It is to be observed that in the vertical masses of chalk (see wood-cut, No. 4.) the numerous fragments of belemnites, shells, and other fossils, are also nearly vertical ; and consequently are not in the position in which they were deposited. In examining closely the line of contact between the syenite and the chalk, it will be seen that the elevations and depressions of the out- line, are accurately filled with the syenite. It is also to be observed that the chalk, in immediate contact with the syenite, is unusually compact, and that the colour is changed from yellowish white to reddish white. P GV, Ghee YN Wid Nis f Niae Merap a ih nA ai ion . SS sta " Wy Connexion of chalk and syenite at Torr Eskert. a, mica slate; d, chalk ; e, syenite. One of the specimens (No. 10.) presented to the Society’s Museum * contains a wedge of chalk, included in the syenite, and the lower part is so compact as to assume the appearance of marble, * The specimens alluded to in the Memoir are in the Museum of the Geological Society. 184 Mr. Grirriti on the Syenite Veins which traverse Mica Slate agreeing in this respect with the character which chalk usually presents, when found in contact with common whin dikes. It is remarkable, that a small reniform mass of syenite, is included in the centre of this wedge of chalk; but is much finer in grain than the usual mass of the syenite. It is evident from its external appearance, that this small mass has not been rounded by attrition. In another specimen (No. 11.) the chalk is nearly enveloped by syenite; and the minute pro- jections at the point of contact are well developed. The specimen marked No. 12. exhibits a small portion of the syenite passing through the chalk in the form of a vein; and that numbered 13. contains five small portions of chalk insulated in the syenite, and it is remarkable that the union at the contact is so perfect, that the chalk appears to form an integral part of a compound rock. Connexion of the chalk and syenite at Torr Eskert. a, mica slate ; d, chalk; e, syenite. There are several other peculiarities which render this contact of syenite and chalk very interesting, and which may probably give rise to much dis- cussion. The most remarkable, is the occurrence of reniform or flattened spheroids of the syenite included in the chalk. The positions of several of these masses, are shown to the right of the sectional view No. 4, which was drawn with great care, and accurately represents the facts when the last excavation was made: any fresh excavation will of course cause a change in the detail, but I have no doubt that the principal char acters will be continued. Included in the collection is a specimen (No. 14.) which exhibits two, detached, flattened masses of syenite, resting on chalk. It might be argued from the smooth edges of this specimen, that the and Chalk at Goodland Cliff and Torr Eskert. 185 fragments had been rounded by attrition, and consequently that the chalk which surrounds them is newer than the syenite. But it may be observed, that the syenite itself includes pebbles of quartz, similar to those contained in the green sand and chalk. This fact, when coupled with the peculiarly rounded and indented form of the upper surface of the syenite, and the smooth flattened one of the lower, leads to the conclusion, that it was injected in a fused state into the chalk, when the latter was soft or plastic; and that it may be considered similar to the small reniform fragment of syenite included in the chalk, as seen in specimen No, 10. If the chalk were not first formed, how can we account for fragments of that substance being included in the syenite, as exhibited in the drawing No. 4, and in specimens Nos. 10, 11, 12, 13; and above all, how can we account for the irregular stratum of chalk, with green sand, &c., which occurs below the syenite, and interposed between that rock and the mica slate, as exhibited in cuts Nos. 4 and 5? It may also be mentioned, that it is not unusual to find chalk intermixed with trap, and trap entangled in chalk on the Antrim coast. Examples of both occur at Kenbane Head, west of Bally- castle; and in the section No. 1, appended to this paper, the southern extremity of the greenstone of Fair Head, is shown penetrating the chalk, while the chalk itself includes masses of trap. It is perhaps unnecessary to dwell on this subject, as it is hoped that the drawings, together with the specimens, will sufficiently illustrate the relations of the mica slate, chalk, and syenite: and if it appears, that the views now put forward, have been substantiated, a new and important fact will have been added to those, already described by other observers, which may ulti- mately lead us to attribute a comparatively recent origin, not only to syenite veins and to greenstones formerly called primary, but also to many other crystalline rocks. I have long doubted the existence of true beds of the large grained cry- stalline greenstone or granite, in schistose sedimentary rocks, being of opi- nion that if carefully examined, they would, like the syenite now described, prove to be intrusive veins, and not beds subordinate to those rocks; but I forbear entering further upon this subject at present. October, 1835. VOL. V.—SECOND SERIES. 2B ') , + ea ae a ®, “ae ya, Peet < i aero. 7 : 1 At iw 5 < he aa y » Pay | 1 Py . a } ee 4 4 b ey \ ees xh ») alae i \, “Oe Tt : ras: Lean i Mee An: eh, ae Se the Ware 4S ce Sa af ee : nes Pai Phi : a ns =e iat on ? +in Fe mdi Ni? Cats bag ae tk tie en 2a ar GAY Aa neptty it ile onetien were or (el eee ee ak 7 SN Ne ee eee C Scharf ael et lithoy h Trinted by ue lervica Verlbobroo of LBhpyosgaris pron Bo Las of Lyme hones and, vor | [ 187 J XV.—On certain peculiarities in the Cervical Vertebre of the Ichthyosaurus, hitherto unnoticed. By Sir PHILIP GREY EGERTON, Barr., V.P.G.S. [Read June 8, 1836. | SOME of the facts contained in the present Memoir, were announced to the Geological Society in a short notice, read May the 13th, 1835*. Since that period I have followed up the inquiry by the examination of a great variety of Saurian relics ; and I am now enabled to enter more fully into the details of those facts, the bare occurrence of which was all I could safely offer in the former communication. By the aid of the illustrations given in Pl. XIV, the anatomical details will, it is hoped, be rendered sufficiently intelligible, to enable the reader to judge of the accuracy of the conclusions, which I have founded upon a consideration of them. ATLAS AND Axis. In the spring of 1835, I procured from Miss Anning (whose zeal and in- telligence are well appreciated in the Geological community) a specimen from the lias of the neighbourhood of Lyme Regis, showing the atlas of a small Ichthyosaurus, apparently anchylosed to the second vertebra of the column. Having directed her attention to this circumstance, she informed me that though she had frequently found similar bones, yet it had never happened to her to see them disunited, even when a dislocation of every other bone of the animal to which they belonged, had taken place. In less than a week I re- ceived from her an atlas, seven inches and a half in diameter, corroborative in a remarkable degree of her former observations. The axis was firmly united to it, and she assured me that this was the only instance, in which any two bones had been found in contact, after she had collected a large portion of the ske- leton to which it belonged. I have subsequently had opportunities of examining nearly thirty specimens of all sizes, and probably of several species, in various * See Proceedings, vol. ii., No. 41, p. 192. 2B2 188 Sir P. G. Ecerton on certain peculiarities in the stages of growth, some in their natural position in the skeleton, others de- tached and rounded by attrition on the beach, all of which exhibited the same peculiar features. T'wo views of a very perfect specimen, from the collection of Lord Cole, which I have selected to illustrate the following details, are given at plate XIV., figs, 1 and 2. Upon referring to fig. 2 it will be seen that the outlines of the two vertebre are very clearly defined; I have found, however, by the examination of polished sections, that in the internal structure the bony texture generally extends without interruption from one to the other*. Once only have I succeeded, after the sacrifice of several specimens, in obtaining a forcible se- paration of the two vertebrz, and in this case I found that no intervertebral cavity existed, the bones articulating together by surfaces perfectly flat and even. (Fig. 3. A. B.) It is probable then, that in individuals of tender years the atlas and axis existed as distinct bones, but the extreme rarity of specimens in this condition, leads me to imagine, that the union between the two, took place at a very early period of the animal’s life. The atlas differs very materially from the other bones of the spinal column. It is furnished anteriorly with a semicircular cup (Plate XIV. fig. 1. a.) for the reception of the articulating tubercle of the basilar occipital, widely different from the conical cavities of the other vertebre; for whereas in these the margin of each intervertebral cup is produced into a thin edge for arti- culation with its neighbour, in the atlas it is rounded into the form of a thick and solid lip, bounded on either side by a broad and rugged surface occupying the position of the costal articulation, which probably served for the insertion of the ligaments connected with the head. (Fig. 2. a.) The axis, as I have already remarked, is flat anteriorly for articulation with the atlas. (Plate XIV. fig. 3. B.) It resembles the dorsal vertebre in the form of the posterior cavity, as also in being furnished with bases for the attachment of ribs. (Figs. 2. d. and 3. c.) SuBVERTEBRAL WeEpGE Bongs. I now arrive at a very remarkable feature, at once distinguishing the first and second from the other bones of the spinal column, viz. the configuration of the inferior part of the vertebral body. On the under surface of each bone there exists an unusual enlargement in the form of a solid wedge-shaped process placed transversely to the smaller diameter of the vertebra. By this arrangement four triangular planes are produced, disposed in the following order. The first and largest (Plate XIV. figs. 1 and 2. 6.), is based upon the lower anterior margin of the atlantal socket, having its apex directed down- wards and backwards until it meets the apex of a similarly shaped, though * See a polished slab in the British Museum from the collection of the late Mr. Bullock. Cervical Vertebre of the Ichthyosaurus. 189 smaller plane (fig. 2. c.) proceeding downwards and forwards from the pos- terior margin of the atlas. The third of like shape and size with the second, (fig. 2. f.), extends from the anterior margin of the axis, and joins the apex of the fourth (fig. 2. g.) which inclines forwards from the posterior portion of the same bone. This fourth plane is considerably smaller than the others, and corresponds in size with a fifth (fig. 11. a.), placed on the anterior border of the third cervical vertebra. When, therefore, the three anterior vertebre are in their natural position, the arrangement of the five planes is as follows. The first and largest occupies the lower front of the atlas; the second and third, by the union of their bases, produce a triangular socket on the under surface of the atlas and axis ; and a second smaller socket is formed between the axis and the third vertebra, by a similar disposition of the fourth and fifth planes. Having endeavoured to render intelligible the arrangement of these parts, I shall proceed to describe three peculiar bones which articu- late with the above-mentioned planes, and which I propose, from their form and position, to designate subvertebral wedge bones. The fortunate acquisition of an Ichthyosaurus having the first subvertebral bone zn situ, enables me to omit a series of arguments by which I was pre- pared to show, that a bone did exist supplementary to the atlantal socket, and that the specimen represented at Plate XIV. figs. 4, 5, 6. was to be ascribed to this position in the skeleton*. The second bone of the series is frequently found with the atlas and axis, and is not uncommonly fixed in its position by anchylosis. The third bone is of rare occurrence, in consequence of its diminutive size, and is probably in some species altogether wanting. Fig. 7. is an accurate representation of the cervical apparatus of the skeleton I have above mentioned, and shows the three subvertebral bones so far displaced as to allow their respective sockets to be seen. Fig. 8. a. b. c. is an enlarged view of the same bones seen from below. First Subvertebral Wedge Bone. This bone is of great strength and solidity. Its form triangular. The under surface is thick- ened into a central projecting boss, Plate XIV. figs. 5 & 6. a., from which it spreads out anteriorly into two alz, representing two angles of the triangle. (Figs. 4, 5, 6. b.) The base between these points is occupied by a smooth semilunar socket (fig. 4. c.) which receives the lower hemisphere of the articulating tubercle of the occiput. A rapid contraction of the bone posteriorly forms the apex of the triangle which is slightly truncated, (figs. 5, 6. d.) The upper portion of this * I have just seen in the magnificent collection of Mr. Hawkins an Ichthyosaurus from the lias of Somersetshire, having the first and second bones in their natural position, 190 Sir P. G. Ecrrton, Bart. on certain peculiarities in the bone forms a rugose articulating surface, (fig. 4. a.) extending backwards from the semilunar socket until it meets at a considerable angle a smaller facet (fig. 4. d.), formed by the truncation of the distal extremity of the bone. The former corresponds in size with the plane on the front of the atlas, and articulates with it; the latter abuts against the anterior extremity of the second subvertebral bone. In order that the arrangement of this part of the skeleton may be fully un- derstood it will be necessary to consider the nature of the connexion between the head and trunk of the animal. In the several species of Ichthyosaurus, the proportion of the head to the total length of the body varies considerably, but is in all very large. The articulation with the trunk is effected by a ball and socket joint, between the basilar* portion of the occipital bone and the atlas. How far the mechanism of this joint would have been complete without the aid of a supple- mentary bone will be immediately perceived by fitting the atlas to its corresponding occipital bone. By the application of this test I have invariably found the cup of the atlas incapable of receiving more than two thirds of the occipital condyle. In well-preserved specimens this portion of the articulating process is defined by a slight depression on its surface+ (fig. 7. m.). This seeming deficiency in the socket of the atlas is more than compensated for by the supplementary bone I have above described; for the angle at which it unites with the atlas (fig. 6.) is so contrived that the semilunar socket on its proximal extremity does not coincide with the plane of the atlantal socket, but projects forwards in such a manner as to embrace the whole lower circumference of the occipital condyle. An universal joint is thus effected at the same time that the subvertebral bone affords by its form, solidity, and position, a most powerful fulcrum to restrain the downward pressure of the animal’s head. Second Subvertebral Wedge Bone. This bone (Plate XIV. fig. 7. h.), like the one already described, is strengthened below by a boss of solid bone. It is generally lozenge-shaped, but variations occur both in its form and proportions, probably consequent upon the species and age of the animal to which it belonged. Above, it is divided by a transverse elevation (fig. 3. b.) into two facets articulating with those between the margins of the atlas and axis, and, in front, it impinges upon the extremity of the first subvertebral bone, affording it a strong basis of attachment, and greatly enhancing its power. Third Subvertebral Wedge Bone. This bone (Plate XIV. fig. 7. i.) resembles the second in form, but is considerably smaller. It is lodged in a depression between the axis and the third cervical vertebra, and imparts much firmness to these bones, at the same time that it does not materially affect the amount of motion between them. I have before stated that the third subvertebral bone occurs rarely, and is probably in some species altogether wanting. ‘This may reasonably be inferred, if there be any truth in the argument, by which I shall endeavour hereafter to show the office, which I believe these bones were destined to perform. CERVICAL VERTEBRZ&. The third cervical vertebra of those species of Ichthyosaurus which are * This appears to have remained distinct from the other elements of the occipital bone in in- dividuals of every age and species. Mr. Owen remarks that evidence is thus afforded of a languid circulation in this family of Saurians. + See a gigantic vertebral column in the British Museum. Cervical Vertebree of the Ichthyosaurus. 191 furnished with three subvertebral bones, is characterized by an articulating facet on its anterior margin. (Plate XIV. fig. 11.a.) Certain modifications appear also to have obtained in the form of the intervertebral cavities in this re- gion of the spine, producing a diminution of capacity to a greater or less extent as compared with those more distant from the head. A remarkable instance of the contraction of the cavity, combined with other striking peculiarities is shown at figs. 9 & 10. The vertebra there represented is seven inches in diameter, and was probably the fourth. It belonged to the same animal as the large atlas already mentioned. The anterior cavity is here reduced to a small cylindrical depression, not larger than a shilling in circumference. (fig. 9. a.) The remaining surface is nearly flat for articulation with the antecedent vertebra. The fifth vertebra resembles the fourth, but is somewhat smaller. Both are furnished behind with conical cavities of no great depth, for the reception of intervertebral matter. These bones exhibit a remarkable contrivance, by which the security of their articulation was much increased, although at the expense of a small amount of flexibility. {n front of each, near the lower margin, a depression is so situated as to receive a corresponding eminence projecting from the contiguous vertebra (figs. 9, 10. b.), whilst on the upper margins similar depressions and projec- tions are placed in the inverted order, affording twofold checks against the danger of dislocation. (Figs. 9, 10. c.) The combined result of this construction, and of the reduction of the in- tervertebral cavities, must have been a considerable increase of power in this part of the spinal column. I shall only further remark that, proceeding from the lumbar vertebrae towards the head, the column attains its minimum dia- meter about the fifth cervical vertebra, from which point to the occiput it in- creases in size very rapidly. Having concluded the anatomical details, I now proceed briefly to examine how far the structure I have endeavoured to describe agrees with the design of the other parts of the animal fabric, in adapting the Ichthyosaurus to the peculiar conditions under which it was destined to exist. Whether we consider the osteological characters which I have detailed indi- vidually, or collectively, in their most contracted, or in their most extended state of development, we see in them provisions well calculated to increase, to a greater or less amount the power of the cervical region. We also see that this increase of power, is combined withonly a slight decrease of the flexibility, so ad- mirably provided for inthe other parts of the spinal column. Letusnow inquire, how far this combination of motion and strength in the neck of the Ichthyo- 192 Sir P. G. Eeerton, Bart. on certain peculiarities in the saurus, is compatible with the ideas we may have formed of the exigencies of the animal, from our previous knowledge of its structure and habits. It has been established, upon evidence the most conclusive, that the Ichthyosaurus was a carnivorous reptile, inhabiting the sea, and breathing air, and the more we study its organization the more we see the beautiful adaptation of all its parts to such a mode of life. The lengthened snout, capacious jaws, and prehensile teeth, enabled it to seize and retain its slippery prey; while the broad expanse of tail, and the fish-shaped vertebre, afforded a powerful appa- ratus for progression through the fluid that it is supposed to have inhabited, in pursuit of the finny tribes, which, principally, constituted its food. This com- bination of organs of pursuit and prehension for the capture of its prey, would have been of little avail, without the power of control and direction ; conse- quently we find in the thoracic region, a powerful apparatus connected with the anterior extremities, to regulate and govern the movements of the body. Mr. Conybeare, speaking of this structure, says*, “ The form of the sternal arch, and the broad surfaces of the clavicles is such as to impart great strength to the chest, enabling the animal to breast the most disturbed waters, and affording an extensive surface for the attachment of powerful muscles to assist in moving the anterior extremities.” It was further necessary that the head, constituting one-fourth of the entire length of the animal, should be furnished with adequate powers to enable it, not only to cleave the waves with steadiness and ease, but to obey each impulse, in directing the pursuit, with quickness and precision. If we examine living structures, we find in the whale, a fulcrum for the support of the ponderous head in the anchylosis of the cervical vertebra. In fishes we find provisions for rapid progression in the con- struction of the spinal column. The Ichthyosaurus required a combination of the two powers ; and as former observers} have demonstrated most clearly the beautiful adaptation of the animal’s organization for progression through the waters, so I trust I may no less clearly have established, by the foregoing details, the existence of contrivances in the cervical vertebra, fully sufficient to have afforded that enlarged amount of power, which the habits of the animal, and the proportions and arrangement of its parts would seem to suggest to have been almost necessary to its existence. Doctor Buckland, when speaking of the ‘““Ossemens Fossiles,’’ and of the author of that work, in his Bridgewater Treatise, sayst “‘ Nothing can exceed the accuracy of the ~ * Geol. Trans. 1st Series, vol. v. p. 578. + Geol. Trans. 1st Series, vol. v. p. 559 et seq. 2nd Series, vol. i. p. 103 et seq, t Vol. i. p. 140. Cervical Vertebre of the Ichthyosaurus. 193 severe and logical demonstrations, that fill these volumes with proofs of wise design in the constant relation of the parts of animals to one another, and to the general functions of the whole body. Nothing can surpass the perfection of his reasoning in pointing out the beautiful contrivances, which are provided in almost endless variety, to fit every living creature to its own peculiar state and mode of life.’ If I have succeeded in adding one instance to those amassed by the illustrious Cuvier of ‘‘ conformity of design,” I trust the im- perfections of the foregoing memoir may be pardoned. Since this paper was written, I have received from Mr. Hawkins (whose splendid collection of Lias Saurians far exceeds any I believe in the world) the atlas and axis of an Ichthyosaurus tenuirostris found near Street. (Plate XIV. fig. 12.) The bones are firmly anchylosed together. The articulating facet on the front of the atlas is large. ‘The second subvertebral bone is im situ, and is much smaller in proportion to the first than those I have before seen. ‘The third subvertebral bone is entirely wanting. This interesting specimen confirms the statement I have before ventured, that modifications in the forms and proportions of the cervical apparatus, would probably be found in animals of different species and age. VOL. V.—SECOND SERIES. 2 th 7 ‘ : ’ vy avs » 2 ip r _ we i Le a eee tint: &: _ pete gir ol ; ue nae eee ae aks.) atid “ rye >. i see pian: wa —_ 7. fe feel oe dot le "ae ae .. cata a Aid os cs ee 7 ae aed seen oi Ape aH “aoe, | wnat viheeen er. oT. | a Se * jan. i i _ = ae a , <28 » 7 — et J sn ra & - _ —s os 7X COAL FIELD, FOREST OF DEAN Hi \ ya io vw ie fe = } ary Maclaychlan Evg! Pes, Penal Common 4 Tretheebs Beacon Hithe XVI.—Notes to accompany a Geological Map of the Forest of Deri Coal-field. By HENRY MACLAUCHLAN, Esgq., F.G:S. Employed on the Ordnance Trigonometrical Survey. [Read February 6, 1833. ] THE following notes were collected during the progress of the Ordnance Survey in 1830, but some additions were made at a subsequent visit to the Forest of Dean. It is desirable that I should acknowledge the several au- thorities from whom information has been obtained. From occasional intercourse with the Rev. W. D. Conybeare, I derived the little knowledge which gave rise to these notes. The memoir by Professor Buckland and the Rev. W. D. Conybeare, on the south-western coal district of England; as well as that by T. Weaver, Ksq., on part of Gloucestershire ; and the section of the Forest of Dean by D. Mushet, Esq.*, have served as foundations to the map+ and the notes. Charles Bathurst, Esq., of Lydney Park, supplied the minute observations respecting that neighbourhood, particularly those relating to the fault between Lydney and Denbigh Lodge. _ D. Mushet, Esq. and Mr. Henry James, of the Forest of Dean and Lydney, greatly assisted me, not only in marking the outcrop of the beds of coal, but in pointing out where the best information could be obtained. Mr. Moses Teague, of Parkend, supplied the outcrop of the two upper beds of coal from actual observation; and the accuracy of the northern curve of the same beds was confirmed by Mr. James Bennett, of Drybrook, who has extensive works on the spot. From information supplied by Aaron Hale, of Coleford Meend, have been laid down the fault from Worcester Lodge to Bury Hill, and the probable range of the Coleford high delf coal, between Bic Slade and Carter’s- piece Meendf. The author’s colleagues on the Ordnance Survey, have from time to time * Geological Transactions, vol. 1. of the Second Series, pp. 280, 288, 352, also Plate 32, 38, and 39. + Plate XV. t It is suggested that this range should be received with caution, notwithstanding it has been partly confirmed by Mr. Mushet; as it is difficult for a beginner to comprehend perfectly the remarks of a practical miner. 2c2 196 Mr. Mactavucutan’s Notes to accompany a Geological Map supplied much information and many extensive boundaries ; but, as these obser- vations as well as his own, were made in the course of duty, it isnot presumed that they are so precise, as if undivided attention had been given to the subject. The greater portion of the outline from Mitcheldean to Penhow, was traced by Mr. John R. Wright and Mr. R. Wright. Old Red Sandstone. The old red sandstone, which constitutes so large a portion of Hereford- shire, and passes under the coal-field of the Forest of Dean, may be divided into three portions. The lowest *, containing beds of cornstone, occupies the flat district between Hereford and Kenderchurch, stretching on the north-west from Wormbridge to the east of the Black Mountain, and by Hay and Talgarth to Brecon: on the north-east it extends from Wormbridge by Dewsall and Aconbury, and crosses the Wye, near Fownhope, towards Sellershope, where the strata are thrown up by the outcrop of the transition series. Along the course of the Wye, to the south of Hereford, these beds are overlaid by diluvium; and to the south-west as far as Thruxton. The sandstone, however, may be observed at intervals ; and the occurrence of a bed at Brandon Hill, near Bullingham, dipping to the north, renders it probable, that a line of elevated strata ranges from Kender-church, in an irregular direction, to Shucknell Hill, to meet the anticlinal line which extends from May Hill to the apex of the Bristol coal- field. The same line of elevation is supposed to pass from Kenderchurch, southward by Clytha (where the transition beds are thrown up) to Usk. The next bed, which from its position may be called the middle, is a con- glomerate, and may be easily distinguished by its elevated position, forming the northern escarpment of the hills, from the Graig at Grosmont, where it attains the height of 1380 feet, by Garway Hill and Aconbury, at which point its dimensions are much diminished, to Capler Camp on the Wye. This conglomerate, it is presumed, may be an outlier of that which occurs at the Doward Hill on the Wye, near Monmouth (Map, PI. XV.); and the pre- sumption is strengthened by a want of connexion between the beds at a lower elevation, as far as has been observed ; and by a coincidence of opinion with Mr. Mushet of Coleford. It is supposed that this bed of conglomerate, occupies the elevated summit of Trelloch Beacon ; and that it passes by Wye Wood Common, and Chep- * The district occupied by this division, and the greater part of that, by the second or middle, are not included in the map. of the Forest of Dean Coal-field. 197 stow Park to Wentwood on the Usk ; and that it is overlaid si the new red sandstone near Newport on the same river. This conglomerate or hard grit, it may be scarcely necessary to observe, is some way below the top of the old red; and it sometimes forms two distinct beds * The hardness, as well as the number of the pebbles, varies; but there is scarcely a place along the outcrop of the old red, where fragments at least, of the conglomerate, are not seen (except north-east of Lydney, where the con- glomerate is cut off by the fault) ; and it usually presents a steep ridge, suc- ceeded by the soft ground of the upper beds and of the limestone clay. These argillaceous strata often throw out springs, accumulated in the limestone rocks above ft. The upper bed of the old red sandstone, is given in Mr. Mushet’s sec- tion as twenty fathoms in thickness ; and it rests immediately on the conglo- merate. The Penyard and Chase Hills, near Ross, (Map, Pl. XV.), are outliers of this upper bed and the subjacent conglomerate, the latter constituting, all around the hills, projecting masses which dip about 12°, soas to take the ground again, and form the rugged and picturesque scenery from Hope Mansel, and the bold promontory of the forest coal-field south of Lea, as well as the escarp- ment by Warm Hill, Goodrich, and Huntsham to the Doward and “ Buck- stone,” where a highly inclined mass of it, forms an object of interest to the antiquary as well as to the geologist. The similarity between the conglomerate bed of the old red sandstone and the millstone grit, has led some miners to sink for coal in the former, about a mile to the north-west of Penhow. Had they extended their observations, on the surface, a little more to the south-east, they would have seen the carboniferous limestone, which must have been familiar to them, dipping conformably to, and resting upon, the strata they were piercing ; and they would have saved much expense and waste of time. At Bircham Hill, near Newland (334 miles south-east of Monmouth), the old red sandstone appears to have been forced up through the carboniferous limestone ; a supposition which is strengthened by the strata dipping in every direction ; but it must be observed, that the valley from Newland to Red- * At Chapel Hill, near Lydney, there seems to be a second upper layer of it very distant from the first, but this appearance may be due to a fault. Near Monmouth, at the Kimin Hill, and Buckstone, there are similar indications, and the conformation of the ground, and a general view of the hills from Trelleck to Penhow, would lead to a similar conclusion. + A very micaceous stone sometimes occurs in the upper part, near the conglomerate. Quartz pebbles are sparingly dispersed in beds above the hard conglomerate, and for some way below it. 198 Mr. Mactaucuian’s Notes to accompany a Geological Map brook, is cut out of the sandstone for the greater part, and is connected with Bircham Wood. On the other hand, the occurrence of the conglomerate at Bircham, when taken in connexion with the diversity of dip, supports the sup- position, of an upthrow in this particular spot. The surrounding limestone dips regularly into the coal-field, and is ap- parently undisturbed. It may be worthy of notice, that this conglomerate, at Bircham, forms, with that at Buckstone on the north and Ailberton Common on the south, a line of conglomerate nearly parallel to the general conformation of the coal-field on the south-west. Near Ailberton Common, the dip of the old red is not always great, but varies through every degree of inclination, and over a large part of the surface, is less than 30°. The strata are often nearly or quite horizontal, and when that is the case, a slight undulation makes the dip vary to quite a different point of the com- pass, as is indicated by the arrows in the map. This nearly level position of the old red sandstone greatly increases the difficulty, where it occurs, of distinguishing that formation from the new red sandstone; but in general, the upper beds of the old red are more highly inclined than the lower ; though in the Tidenham Chase Hills, south of Hew- elsfield, where such is the case, the mountain limestone conforms to the gentle dip of the lower beds. Sometimes, the angle not even of the upper beds, is great, particularly along the whole of the Ailberton Common district. In this country, the distinction mentioned in the Geological Transactions (2nd series, vol. i. p. 284,) between the middle and lower divisions of the old red, seems hardly maintainable. Corn- stone nodules occur in the very lowest beds in the Severn Cliffs about Gatcombe, opposite the transition limestone ; also in the cliffs on the left bank, between the outcrop of that limestone and Sharpness Point; and they are found at Blakeney. On the other hand, the flagstones are by no means confined to the lower beds; but are more common in those of the Mill Rough and the hills west of Blakeney, in a higher part of the series than that in which any cornstone nodules occur. For a few miles east of Lydney, the country, for the most part, consists of clay, except perhaps the upper beds along the Mill Rough and Horage Wood; but even in these localities, the sandstone by no means exclusively prevails. The position of the small stone beds of the old red, sometimes varies sin- gularly near the surface, lying thus,— SS ere owing appa- i rently to unequal depositions. Such sections occur in the turnpike-road east of Alvington, and some way east of Lydney. of the Forest of Dean Coal-field. 199 Along what may be called the Blakeney range of the old red, from Newn- ham to Ailberton, the dip is from the river, or towards the Forest. A second dip, always gentle, but quite different, viz. towards the north-east, is met with in the Ailberton Common ridge, also from Ailberton Chapel to Bream Lodge, and in the lower strata belonging to the old red, which extend nearly to Woolaston. This ridge of conglomerate is intersected, in one place, by a cross fault, raising the part furthest from the Severn, and affecting the outline of the limestone, but the dislocation cannot be traced into the body of that formation, or far into the lower part of the old red. The line of hills, which may be called the Chase Hills, from near Bream Lodge, by the east of Hewelsfield, to Tidenham, have a third dip nearly parallel to the first. Each of these, where it joins the next, seems generally to do so by a sudden line, not graduating round ; but this is difficult to prove with certainty. The upper strata near Bream Lodge are an exception, as they seem clearly to bend evenly round, including the conglomerate at Prior’s Meend. Carboniferous Limestone. The carboniferous limestone surrounds the Forest of Dean coal-field, with the exception of the line of fault between Lydney Park and Denbigh Lodge, a distance of four miles. According to Mr. Mushet, a bed of iron ore divides the lower and more crystalline, from the upper and more argillaceous and sandy strata. A section of these beds is well exposed on the side of the tram road, about a mile below Cinderford Bridge, on the east side of the Forest, and at Lidbrook on the north. There is a small outlier of the coal measures, including the lowest bed of coal at Howl Hill; it does not appear, however, to rest on the same bed of limestone as that in the large field at Ruerdean, but on a more argillaceous and thinner stratum, which is not supported by the bed of iron ore or lower crystalline limestone. ‘To the east both the limestone and the coal thin out, or are cut off, the coal measures resting on the old red sandstone. The valley of the Wye is cut through the limestone only, for on the summit of Copped Wood Hill, the same argillaceous beds occur again, and all attempts to trace a continuation of the outlier of coal, have been unsuccessful. On the Doward Hill the iron ore bed reappears, and the ancient workings on the summit of the Little Doward, may have been mistaken for an entrench- ment, on that commanding and military position. The dip of the beds at Howl Hill is very slight, but it increases westwards towards Doward Hill, where it is considerable. 200 Mr. Macraucutan’s Notes to.accompany a Geological Map At a place called “‘ the Dunder Hole” (Thunder ?) on Bishop’s-wood, a stream sinks through the strata with a considerable noise, and emerges again in the valley to the south, a little above Bishop’s- wood House, where it is perhaps thrown out by the bed which underlies the great stratum of lime- stone at Ruerdean. A similar occurrence takes place in the limestone about a mile to the south of English Bicknor. Near the “Dunder Hole” is a bed of gravel in the position of the millstone grit, but it is very different in appearance from the grit in the Forest. It has much the character of diluvium ; and if there were an aperture through which the Wye at any elevation could have deposited it, the similarity in appearance would lead to such a conclusion. There isa small outlier of the carboniferous limestone at Penallt Common, about three miles south of Monmouth ; it dips conformably with the sandstone on which it rests, and is so valuable for manure in that clay and sandy coun- try, that it is nearly worked out, though it must have covered two acres in the first instance. ‘There is no appearance of the coal strata. Coal Measures. In tracing the outline of the coal measures, Mr. Mushet’s Section, pub- lished in the 1st volume of the Geological Transactions, 2nd Series (PI. 32. No. 5.), has been particularly useful, as it crosses the field in almost the only direction, which includes all the strata. The beds of coal may be conveniently divided into two series ; Ist, the rock beds, or those separated by a coarse sandstone, including all the seams from the lowest or “ Trencher,” to the “ Brazilly,” and, 2ndly, the argzllaceous beds, or those above the Brazilly, and characterized by shale. Of the lower series, the outcrops of only the “ Trencher” and the “ Cole- ford High Delf” have been traced almost continuously around the field ; but these beds differ in their relative distances and qualities; and it is said that one increases in value where the other decreases. At Lydney Park the “Coleford High Delf” and “Trencher” are not well defined at the angle, the outcrops being there very obscure. From this point they increase in dip, with the rising ground, to Bream’s Eaves, and afterwards decrease again, but at Gorse Hill and Coleford Meend, they become hori- zontal, and crop out to the westward, more from the declivity in the ground than from their ascending position in that direction. This observation will apply to their outcrops on the north also, from a little south of Symmonds’ Gate to Joyford and Carter’s-piece Meend. At this place the line of division*, ranging from Bic Slade to Carter’s-piece * This line is nearly parallel to what is assumed to be the line of greatest depression, or central line of the field or floor, which rises to the north at about 10°. of the Forest of Dean Coal-field. 201 Meend, between the inclined or eastern and the horizontal or western part of the bed, emerges to the surface, and the coal crops out in opposite direc- tions, for some distance, from the Whimberry Slade to Carter’s-piece Meend ; but beyond the latter point the two beds crop conformably with those above them, into the valley of Lidbrook. Mr. Mushet observes, that this line of division causes the western side to dip gently to the west, and afterwards to rise again, forming on Coleford Meend a slightly inclined basin rather than a horizontal bed. At Oakwood Mill the “Coleford High Delf” is not worth working, pro- bably from the effects of a fault. The divergence observable in the outcrop of the beds to the northward, arises from the decrease in their angle of position. The Trencher Delf begins tobe workable coal about north of Bream ; but its range has been traced from the clay observable in its line of outcrop; and though of little consequence to the miner, it should not be altogether disre- garded by the geologist. At Lidbrook Valley, on the north of the coal-field, there is a contortion on each side, which throws down the High Delf coal, in one instance, seventy yards, and in two others, thirty yards each (see the accompanying diagram which is parallel with the strike or at right angles to the dip of the beds), Lidbrook Valley. Joy’s Green. Horse Lea. Plud’s Enclosure S.E. N.W. - Leas : b. Carboniferous limestone. c¢. Millstone Grit. d. Coal measures. The ten yards of clod ceases as a covering to the coal before we reach Carter’s-piece Meend, and its absence is probably connected with the effects of the fault; for on showing this section to Mr. Mushet, he confirmed the details, as received from a practical miner, but reversed the order, making the double contortion on the western side of the valley, and the seventy yards depression at one step, on the eastern, where this section is represented to be. In the double step, the descending portions are useless coal, and represented to be dust and dirt. The local name for this contortion is “* Horse,” whence ‘‘ Horse Lea.” V'rom Worcester Lodge near Coleford, to Bury Hill, is a line of disturbance, the course of which is marked, on the surface, by a series of ponds, called Howler’s Well, Leech Pool, Crabtree Pool, Hooper’s Pool, and Hall’s Pool. It is possible the water may be kept up by the clay in the fault, which is said to be 200 yards thick, extremely hard, full of silicified wood ; and when acted on by powder, it separates without disturbing the surrounding mass, yet causes much trouble to the miner. One branch of the fault ranges to Elmore Mill; and others are said to diverge along its course, but they have not been defined. VOL. V.—SECOND SERIES. 2D 202 Mr. Mactaucutan’s Notes to accompany a Geological Map These are the only interruptions to working the coal of any consequence which have been ascer- tained; those found occasionally in other pits occur here, but they are of temporary inconve- nience. Above the “ Trencher” isa bed called “the Spider,” which is wrought at Gorse Hill, about a mile south of Coleford, and in no other place as far as could be ascertained. Above the “ Coleford High Delf” is the “ Whittingtons Delf,” known also as the “ Yard Coal.” It is worked principally in Bream district, but is found at Dark Hill, and its clay is said to have been cut through in a shaft sunk to the west of Birch Hill Lodge, though no trace of coal was observed. From its position in the series, it is presumed to be the same bed, with that which crops out again on Carter’s-piece Meend, at Nail Bridge ; and it thins out on the west side of the field in the Haywood Enclosure, with several others, in- cluding the strata of sandstone in which the coal beds occur. This fact was proved by a level driven by Mr. Moses Teague at Cinderford Bridge from the “Churchway,” one of the clay beds, to the “ Coleford High Delf,” without meeting with any other coal seam. At Staple-edge Enclosure the “ Whit- tingtons”’ is brought in again with the strata of sandstone, and is traceable thence to the Bream district. The “ Nag’s-head,” or ‘‘ Yorkley” seam, is nearly parallel to the “ Braz- zilly’’ above it, and the “ Whittingtons”’ below, except in Ruerdean-hill En- closure, where the true position has not been well ascertained. The outcrop of the sandstone beds, may be easily traced by the step made in the wearing away of the clay and coal, leaving a projecting hard ledge of rock. In the clay beds there is no such guide; and the information collected from the miners, and occasional traces of coal, have been relied on. As ithe outcrops of the clay-bed seams are faintly indicated, no attempt has been made to trace them on the surface above the ‘‘ Parkend High Delf”. This bed is occasionally called the ‘‘ Lowery”, and is well known around the field by these names. Those above it are not so generally worked, and the outcrop has not been so well ascertained. The uppermost seam, called the “Woor Green,” is known only near Cinderford Bridge, or a little east of Yewtree-brake Lodge, where it has been wrought. An outcrop near Crab-tree Lodge is supposed to belong to the same bed ; and one cut through in digging the well at the “Speech House,” may be a continuation of it; and this sup- position is in some measure confirmed by the structure of the ground. The dotted line in the map defines the probable course of the outcrop. The beds between this and the “ Parkend High Delf”, are enumerated in Mr. Mushet’s List and Section (Geol. Trans., 2nd Series, vol. i. p. 288), but all endeavours to trace them around the field have been unsuccessful. of the Forest of Dean Coal-field. 203 An attempt has been made in the map to mark the outcrop of the principal beds of coal. Those belonging to the Rock or Lower Series, being further from each other and thicker, are best known. Where the information was obtained by personal observation, or from good authority, the outcrop is marked by a continuous line; but where the data were doubtful or conjectural, bya broken line. The “ Churchway” or “ Oakenhill,” and the “Parkend High Delf” or “ Lowery” (Lower-high?) being most worked or best known, have been selected to define the range of the upper or argillaceous beds, and the five others (according to Mr. Mushet’s List), which occur between them have been omitted, from the crop being confined to the intervening narrow space. Those above the “ Parkend High Delf’ have not been ascertained satis- factorily enough to be inserted, and the “ Woor Green Delf’’ has been dotted in, from conjecture, but after an attentive observation of the construction of the ground, with the exception of its known outcrop near Cinderford. Iron Ore. The stratum of argillaceous iron ore, worked near Cinderford Bridge, occurs immediately below the Trencher coal, and probably accompanies it round the field, though the workings have not been sufficiently extensive to prove it. In the neighbourhood of Ailberton and towards Bream, the very upper- most, and nearly the lowest beds of the limestone, seem to be those which produce iron, but principally the uppermost. ‘The position is marked by a line of rocky ground, some parts of which, called “scowls”, are the effects of ancient excavations, and are nearly continuous from the Old Park Wood to beyond Clearwell. The limestone which occurs in the millstone grit at Clearwell Meend is oolitic, and partly shelly ; but it is not thick, though probably continuous to Oakwood Mill. Newent Coal-field. The Newent coal-field, though not included in the map, deserves a brief notice. The boundary of the field is not easily defined; but its northern and western range may be sufficiently understood by drawing a line from Oxen- hall Church westward along the brook, to the road from Newent to Ross, a little to the west of Kilcot Green; thence it may be traced on the west of Kilcot Wood, where the coal measures are well marked, and along the road to Aston Ingham as far as the end of the wood; and afterwards by the western edge of Clifford’s Mine, or Meend, to where the common Jand joins the Newent Woods, and even for a short distance within the woods. At this place the coal 2p2 204 Mr. Mactaucutan’s Notes to accompany a Geological Map measures appear to rest upon the transition series, but at Kilcot Green, or rather to the west of it, on the old red sandstone. The eastern side is overlaid irregularly by a conglomerate of the new red system, formed principally of siliceous pebbles ; and it occasionally assumes the appearance of a bed of gravel ; but in no case does it resemble the mag- nesian limestone. Over this bed are other similar conglomerates which alter- nate with strata of sandstone, dipping at a low angle (5°) to the eastward. The western side of the field is composed of a fine-grained sandstone, with small quartzose par- ticles occasionally disseminated through it; the stone is generally iron shot, and sometimes thinly laminated, and contains specks of coally matter. At Hill House, previous to working the coal, a boring was made to the depth of fifty yards, and the following beds were passed through, according to information received from one of the work- men employed in the undertaking. Redelay sss asst 30 yards (new red sandstone). Sand. rock. (15. 2s sie 4 feet. Clod or clay..% asin 8 feet Catt ons secs ee 7 feet Cod Ssipiewm seer ate 4 feet CoGl. ess sae ee es 2 feet 6 inches. Clade SoVeEA see 15 feet. Coal 2de shit decks his 4. feet. The rest of the boring was through clod or clay. The seven-feet coal was the bed principally worked; but it was much disturbed, and dipped rapidly, or two feet in a yard, to the north-east or east. In 300 yards, four faults of considerable magnitude were encountered, and the coal contained a large quantity of sulphur. These circumstances, with the canal bringing the Staffordshire coal so close to the field, may have caused the relinquishing of the work. Several other attempts have been made at Bowlsdon Farm, about a mile to the south-west of Newent; where the coal is apparently near the surface ; and, as it is said to be seven feet thick, it is probably the same bed as that which was worked at Hill House. The fuel, however, is better, and less charged with sulphur than at that point. No engine was used, but numerous pits were dug, from which it may be inferred, that unskilful means were empluyed to extract the coal. No attempt has been made for several years. It is possible that the nearness of this coal-field to the anticlinal line, ranging from the valley of Woolhope by May Hill to the Severn, may be the cause of the disturbances found in the strata; for the measures are so far advanced to the westward, at Clifford’s Mine, as to rest upon the trans- ition beds, The Fault between Lydney Park and Denbigh Lodge, Forest of Dean*. It has been correctly stated{ that along a certain portion of the edge of the Forest coal-field, the limestone is cut off by a fault. This fault extends * See Map, Pl. XV. + Geol Trans. 2d Series, vol. i. p. 256. of the Forest of Dean Coal-field. 205 somewhat further, though not in a completely straight line ; for near the west end of Ailberton, where the strata dipping with those at Ailberton Common, join the beds which dip conformably to the Blakeney range, a fault begins, separating these two dips from one another. The strata which this fault divides, in proceeding northwards, and in which three different dips appear, are, first, old red on both sides ; then, after pass- ing the Chapel, old red on the right, and limestone on the left; in Lydney Park there is limestone on both sides; then at the back of the Red Hill, the fault divides the millstone grit on the left from limestone on the right. It afterwards makes a little turn to the right, apparently just beyond the junction with the lower coal, and cuts across the end of the limestone first, and then of the upper beds of the old red, and of the conglomerate, and some of the beds under it. At the same time the strata to the left of the fault, which are here the coal measures, change their direction, and dip thenceforward nearly as those on the right. From that point, therefore, the fault is marked by the omission of the limestone, on the surface, and not by any great difference of dip. For some distance, the strata on each side, are nearly parallel to one another and to the fault (see the accompanying diagram) ; but after entering the forest, it is conjectured, for it is difficult to determine from the thickness of the new plantations, that there is a sort of converse in some respects from that which occurs near Lydney ; for while the coal measures (d) continue to range parallel to the fault, the upper beds of the old red (a), which had been cut off near Lydney, gradually and obliquely come in again, as inferred from the dip ; and then at Denbigh Lodge the fault turns for a short distance at about 45° to the left, and cuts across the end of the conglomerate (d), the beds above it (a), and the limestone (0), which are thus restored to the surface, at the valley of Blackpool Brook. It is presumed that at this spot, the fault returns to its former direction, and does not terminate, for the millstone grit is not restored at this point, though the limestone (0) is, but gradually appears further on (c). Left. Fault. Right. a. Old red sandstone. 4. Old red conglomerate. b. Carboniferous limestone. ce. Millstone grit. d. Coal measures. Though in one sense, the fault which exists near Ailberton may thus be 206 Mr. Macraucutan’s Notes to accompany a Geological Map, &c. considered as continued into this great fault from the Leech Pool to beyond Denbigh Lodge, another description of continuation of it, is in the line or axis which runs into the coal-field through the successive points of acute flexure made by the different beds or “ delves” of coal. This flexure or irregular basin shape seems here moulded by the two un- conformable dips of the old red, which the fault at Ailberton divides; but they seem to bend from one position to the other less abruptly, and with less dislocation of the strata, than near Ailberton. It is suspected, however, that at the bend of the upper coal beds at White- croft, there is some little dislocation ; and very possibly near Lydney, the Cole- ford High Delf does not bend so completely without dislocation, as it is repre- sented to do in the map. In that part of the line, where the fault runs nearly parallel to the strata on both sides, it has not been found possible to distinguish clearly one formation from the other, or consequently the exact line of dislocation. The characters of the millstone grit and old red are likewise not well defined. A remarkably hard, fine-grained, purplish rock occurs, in white clay, at Old Croft, also at a spot further on in the Forest, and a similar rock appears near Bream. It sometimes contains quartz pebbles, and is possibly a variety of millstone grit. It has a slight mixture sometimes of calcareous matter; and limestone itself is here occasionally subordinate to the grit*. Its position, however, partakes somewhat of the obscurity, already mentioned, respect- ing this line of fault, from the Leech Pool near Lydney, to Old Croft in the Forest. * At Clearwell Meend, near Coleford, the limestone is worked in two places in the millstone grit; and small pieces have been dug out at Old Croft bearing the red sandy appearance of that at Clearwell Meend. Geol. Trans. 27 Ser, ZA Wt . am os CLM Witt, 2 ° pitti VO Mites. ie fda. < IAS XN cS ® Kg DN NEN ™ L& SS S SO WV ® Ny ye Wl Pl eee Thy c Gy 16 YS. fe 207 te’ flex é Vi Wt! Ce SY aie aw 5 \\ SN Ny oY § SAGES aN RS NY NS rs SS xe iI NASA I} Wo Sle Lys bod fearlea — V/ LE e Up: Zvi ( “itl. Wood from ‘ A nlipua; ft.208. ie A Mey ine IT ASLZ AL - Ting, P ¢ WIR pillippil ttl tl Ma VPLS [ 207 ] XVII.—Notice respecting a Piece of Recent Wood partly petrified by Carbonate of Lime, with some Remarks on Fossil Woods. By CHARLES STOKES, Esgq., F.G.S. [Read June 8, 1836.] THROUGH the kindness of Mr. Heuland I have lately received a collection of fossil woods from Germany, that gentleman having very obligingly engaged one of his correspondents to attend to the particular inquiries I wished to make, and to collect for me the objects described. To this collection was added a specimen of recent wood in which some portions have become petrified by carbonate of lime ; and although this is not the first known instance of the occurrence of wood partly petrified by calca- reous spar, yet it has, from its peculiarity, Jed to comparisons with some other fossil woods of remarkable appearance, both calcareous and siliceous, and for which it appears to have afforded some explanation. I am induced to submit to the Geological Society the following observations respecting it, in the hope, that by exciting attention and remark from other observers, we may obtain some knowledge on the very difficult question of the process of petri- fication. This piece of wood is of the common heech (Fagus sylvatica), and was found by M. Cotta of Tharand in an ancient Roman aqueduct at Kilsen in the principality of Lippe Buckeberg, but I understand that he has not pub- lished any account of it. The size of the portion in my possession, is about 33 inches by 43, and the thickness is nearly one inch. For the better understanding of the description, the accompanying drawing has been made of the specimen (Plate XVI. fig. 1). The wood is, for the most part, in the state of very old dry wood, but there are several insulated portions, in which the place of the wood has been taken by carbonate of lime. These portions, as seen on the surface of the horizontal section, are irregularly circular, varying in size, but are generally a little less or more than + of an inch in diameter, and they run through the whole thickness of the specimen in separate, perpendicular columns. The vessels of the wood are distinctly visible in the carbonate of lime, and 208 Mr. Sroxes’s Notice respecting a Piece of recent are more perfect in their form and size, in those parts of the specimen, than in that which remains unchanged ; as if the petrification of those portions had taken place, while the wood was yet in sound condition, and the remaining part had since contracted around them, as it gradually decayed. This is shown by the bending of the medullary rays, adjoining the limits of the calcareous portions. Dr. Turner has examined one of these portions, and finds it to contain 9 per cent. of ligneous fibre, the rest being carbonate of lime. I have not obtained an account of the situation of the wood in the aqueduct, or of any circumstance to explain how it had become exposed to the action of water containing carbonate of lime in solution, but I am unwilling to delay the communication to the Geological Society, of the remarks it has suggested to me. Mr. Robert Brown, to whom I had the pleasure of showing this specimen on the day I received it, immediately reminded me, of one of silicified wood from Antigua in my own collection, which we had formerly examined together, and in which the polished horizontal section exhibits a similar appearance of insu- lated portions, that have the structure preserved in a more perfect state than the rest of the specimen, as is represented in the accompanying drawing. (Pl. XVII). The whole specimen is completely silicified, and takes an excellent polish. The portions best preserved are irregularly circular in form, about + of an inch or rather more in diameter, and in them the vessels and medullary rays are distinctly seen in good condition, while in all the other parts (although the general form of the stem is preserved) the vessels are compressed (particularly round the more perfect portions) and the medullary rays are bent and compara- tively indistinct. From the different condition in which the different parts of the wood have been preserved, it ap- pears, that the process of petrification had first taken place simultaneously at a number of separate points, and then had stopped, and that the unchanged part had subsequently in some degree decayed. If at this period a transverse section of the wood had been made, its condition must have been similar to that of the wood from the Roman aqueduct, having some parts petrified while the greater portion was still in the state of wood, though not in a sound state. After this, the progress of petri- faction was again renewed, and the partially decayed remainder of the wood has been silicified. Another instance (which is of calcareous petrification) appears also to have an analogy to the above-mentioned. ‘This is the specimen from Allen Bank in Berwickshire, described and figured by Mr. Witham (On the Structure of Fos- sil Vegetables, Pl. VIII. fig. 7), under the name of Anabathra pulcherrima. The texture of this plant, whatever it may have been, was much more lax than that of the woods before spoken of. The horizontal section shows some instances, in which the structure is preserved from the centre to the circum- Wood partly petrified by Carbonate of Lime. 209 ference, but more frequently only insulated portions of about one tenth of an inch in diameter, in which also the structure is well preserved. The direction of the rays, which pass through these portions, shows that they are, with scarcely any exception, in the same position as when the stem was entire, although they are now surrounded by mineral matter (carbonate of lime), in price scarcely a trace of the structure of the plant remains. From this condition of the fossil, it appears, that as in the former instances, the progress of petri- faction commenced at a number of separate points and was afterwards interrupted, but in the present case, the whole of the remaining portion of the wood appears to have been entirely destroyed by decay, which occurred after the interruption, and no renewal of the process took place, while any of the other parts of the wood existed. The fossil wood from Linnel Braes, described and figured by the same author (Pi. 3.),is also a case where parts only of the wood have been petrified and the remainder entirely decomposed by subsequent decay, but the petrified parts are in their places, and the intervening space is filled up by crystallized carbonate of lime. Such are the appearances shown by sections made in a transverse direction, or at right angles to the axis of the growth of the wood. In the examination by means of longitudinal sections, we shall find the following differences be- tween them. In the recent wood from the Roman aqueduct, the carbonate of lime runs, as I have stated, through the whole thickness of the specimen, the petrified portions appearing to be in long columns. In the Antigua specimen, the well preserved portions are not, in any of the instances I have seen, more than three eighths of an inch in the longitudinal section, and their form is irregular. In the Allen Bank fossil, the insulated petrified portions are of the same size in the longitudinal as in the transverse sections, showing that they are of spherical form. In the last named instances it appears to me, that we must conclude, that the whole of the wood was penetrated by a saturated solution of the mineral matter, and that the solution was in the state at which crystallization was about to commence. In solutions in such a state, we know that cry- stallization frequently begins simultaneously at a number of separate points, round which the cry- stalline matter continues to aggregate. In the Allen Bank fossil, at the external part of the section, this has evidently taken place, as an examination with a magnifying glass shows, that although the structure of the wood is preserved undisturbed, yet that the petrifaction is there made up by the contact of a number of small spheres. The progress of petrifaction, however, appears to have stopped before it had mineralized the whole of these specimens, and this may have been caused by an accession of water diluting the solution, below the point at which crystallization would go on. The variation in the quantity of rain falling at different periods, or in different seasons, might occasion such a result. After this, as I have before remarked, the unchanged portion of the wood was subject to decay. In the case of the Antigua specimen, before the process of petrifaction VOL. Y.—SECOND SERIES. 2E 210 Mr, Stoxss’s Notice respecting a piece of Recent was renewed, the wood had in some degree decayed and contracted ; but in the Allen Bank fossil it had entirely deeomposed and disappeared, leaving scarcely a trace of structure in the remaining parts. These are filled up with calcareous spar, which has crystallized from a number of separate points, and continued till the whole mass was united. I must here advert to what I have mentioned, respecting the position of the insulated petrified portions of the Allen Bank fossil, in which the structure shows, that they are scarcely at all removed from the position in which they grew. As these seem to have remained in their places, after the other por- tions of the wood had decayed and disappeared, and before the intermediate parts had been filled up by solid mineral matter, it appears to follow that they must have been suspended in the fluid solution which has since crystallized around them,—a condition which it is certainly difficult to comprehend. In regard to the piece of wood from the aqueduct, the petrified portions are also separate and insulated, but as they are in long continuous columns, it is probable that the whole of the wood was not equally penetrated with the calcareous solution. The other cases I have met with, of a partial petrifaction by carbonate of lime, are those of the hazel nuts at Belfast Lough, mentioned by Dr. Mac- donnel, in 1810*, and of partly petrified wood and nuts, described by Mr. Phillips, from the vale of the Aire, near Ferry Bridge, in Yorkshiret. In this latter case, it appears that the wood and nuts are in a deposit of alluvium. Many pieces of the wood, and the kernels of some of the nuts, found at a depth of 12 feet, are partially petrified. A specimen of the wood here mentioned, which was given by Mr. Phillips to Dr, Buckland, who has allowed me to examine it, is a portion of a stem or branch, split longitudinally, about four inches in length, and about two and a half in diameter. In this, a part near the centre, is now completely petrified by carbonate of lime. This portion is about half an inch in diameter at one end, and extends longitudinally through the wood to the length of about three inches, and terminates ina point. It is in its natural position, and the medul- lary rays are continuous through the calcareous part and the unchanged por- tion, as shown in the accompanying wood-cut. The line of separation between the calcareous part and the unchanged wood, is perfectly well defined, and although we may suppose that the vessels of the wood, have acted as conductors to the solution, and given it a direction longitudinally through the stem, yet it is difficult to understand why the petri- faction has been confined to a single spot or column. * Geological Transactions, First Series, vol. iy. p. 448. + Philosophical Magazine and Annals of Philosophy, New Series, vol. iv., 1828. > Wood partly petrified by Carbonate of Lime. — 21] Partially petrified wood from the Vale of the Aire, near Ferrybridge, Yorkshire. It is indeed evident that the vessels of the wood have thus acted as conductors to the solution, from the sinuosities in the outline of the petrified portion which follow the irregular direction of the fibres, where they have by knots or other interruptions been forced from a straight line. The calcareous material was probably derived from the neighbouring limestone beds, and might be supposed to diffuse itself through the alluvium; but in the case of the aqueduct, we cannot imagine that there was so large or so generally diffused a supply of mineral matter. I should mention also, that the examination of thin slices with a microscope shows, that the structure is rather better preserved in the wood at Ferrybridge, than in that from the aqueduct. Mr. Brown has also shown me specimens, in his possession, of petrified wood, in which the greater portion is silicified, but there are some parts still in a soft state, and not at all penetrated by the silex. Some of these are from Lough Neagh, and others from Bonn. Although the amount of information obtained by the preceding observa- tions is but small, yet, in establishing the facts, that petrifaction sometimes commences at a number of separate points, and that it is liable to be inter- rupted and again renewed after an interval of time, we have an explanation of the circumstances which have been difficult to understand, in regard to many specimens of fossil wood, in which parts of the ligneous structure are preserved in good condition, while other parts appear to be more or less decayed. The same facts appear to occur both in siliceous and calcareous petrifac- tions ; but nothing that I have met with, is calculated to throw any light upon the question, of the means by which the solution of siliceous matter has been accomplished, A short description of the different conditions in which fossil wood appears in different specimens may be worthy of attention. Sometimes the most minute parts of the structure have been preserved, as is shown under the microscope in the markings of the vessels of Palms, and the well known instances of the circular discs peculiar to the vessels of coni- 252 212 Mr. Stoxes’s Notice respecting a piece of Recent ferous wood, which are as distinct in the fossil as in the recent wood. From this high state of perfection, we have every degree of condition, down to the very last stages of decay ; hence it appears, that there is not anything in the state or condition of the wood, which has influence upon the process. Sometimes we find petrifactions of the most close grained, and probably the hardest kinds of wood, in good condition ; at other times, we meet with stems of a soft and succulent character, and there are also instances of the complete silicification of the young leaves of a palm tree, when just about to shoot forth, and in that state which, in the West Indies, is called the cabbage of the palm. The different states in which the stems of palm trees have been preserved, are also deserving of notice. These consist of a cellular tissue, among which are separate fascicles of ligneous vessels, which rise through the stem. In some few cases, the cellular tissue is well preserved, while scarcely any of the vessels or woody fibres remain, and the spaces they occupied, are now hollow passages through the specimen. In other cases, the cellular tissue has dis- appeared, and the bundles of vessels alone are well preserved. Other cases occur, in which both the cellular tissue and the vessels, are preserved in good condition. On these facts, 1 would remark, first, that where the cellular tissue has been petrified, and the vessels have disappeared, the process must have taken place, soon after the wood had been exposed to the action of moisture, because the cellular part would soon decay; and that it was then suspended, as in the cases described in the beginning of this paper. Se- condly, where the woody vessels alone have been preserved, 1 conclude, that a time elapsed before the process of petrifaction commenced, during which the cellular tissue had decayed. Thirdly, that where both structures are preserved, the process had commenced at an early period, and continued without interruption till it was completed throughout. There are also some cases, in which hollow dicotyledonous trees have been petrified, and in these cases the middle part is filled up with chalcedony and agates, sometimes leaving cavities which are coated with crystals of quartz. I have also seen cases, in which the cellular tissue only of the stems of palms has been preserved, and the structure of woody vessels lad disappeared, but the places where they had been, have been filled up (doubtless subse- quently) with agates. In conclusion, I have only to state my regret, that the information I have to offer is so scanty, and to express the hope that this subject may be taken up by others, who have better opportunities, and more knowledge and talent for conducting the inquiry. Wood partly petrified by Carbonate of Lime. 213 Further Notice on the partially petrified piece of Wood from an Ancient Roman Aqueduct in the Principality of Lippe Buckeberg. [Read December 14, 1836.] SINCE I communicated to the Geological Society, the preceding notice on the partly petrified wood from the ancient Roman aqueduct at Hilsen, in the principality of Lippe Buckeberg, Mr. Robert Brown has shown to mea speci- men from the same piece of wood, which was presented to him at Tharand, in the month of October last, by M. Cotta of that place, who discovered the wood in the aqueduct, and remarked its peculiar condition. Mr. Brown has pointed out to me in the longitudinal section, that the petrified portions, in his specimen, are about two inches in length, and in the middle part, nearly a quarter of an inch in diameter, and terminate in a point at each end. The petrified portions are, in these instances, completely inclosed within and sur- rounded by the unchanged wood. See Pl. 16, fig. 3. Mr. Brown has observed another remarkable circumstance in the condition of these petrified portions. The change of the longitudinal fibres appears to be complete, but the medullary rays, of which the ends are seen in this section, are still in their ligneous state, as shown in the magnified engraving, Pl. 16, fig. 4. From this it appears, that the petrifying process had not been so fully com- pleted, asin the portion of the same wood, which first came into my possession ; but on referring to that specimen, I have found some instances, in which a part of the medullary ray, that passes through the petrified portion, has not been so completely changed as the surrounding longitudinal fibres, or the part of the same ray, which is more in the centre of the petrified portion. Of the rest of this specimen, some part is much decayed and worm-eaten, while another part is hard and in good condition; and the line of separation between them, is, in some places, remarkably well defined. Although the latter does not to the eye, present any appearance but that of sound wood, I was induced to examine it, and had the pleasure of finding, that, what may perhaps be considered as the first stage of petrifaction, has taken place in it. I cut in a transverse direction as thin a piece as I could detach with a sharp knife, and placed it in water under the microscope, then adding with the point of a quill a drop of muriatic acid, I immediately perceived the disen- gagement of gas, which seemed to proceed chiefly from the inside of the larger vessels, as if an extremely thin coating of carbonate of lime had been deposited within them. In the more decayed part, there is also a slight action produced by the acid, but not so strong as in the sounder part. 214 Mr. Sroxes’s Notice respecting a piece of Fossil Wood. From Dr. Buckland, I have received some specimens of fossil wood from Allesley, near Coventry, respecting which he has sent a communication to the Society*, and at his request, the Rev. W. Bree has also sent to me specimens from the same locality. Among these, which as far as I have been able to ascertain, are all coniferous woods, are several in which some portions are in a much better state of preservation than the rest of the specimens, although the whole is now silicified. These cases are analogous to that from Antigua, described in my former notice on this subject ; but in that mstance, the longi- tudinal section showed, that these better preserved portions were not more than three-eighths of an inch in length, and these were the longest I had then ob- served. In some of the Allesley specimens, these portions are fullan inch in length, and terminate in a fine point at each end, in the same remarkable manner as I have above described to be the case, in the portion of the piece of wood from the Roman aqueduct belonging to Mr. Brown. In others, the best preserved portions are long narrow columns, going through the whole length of specimens, three inches long. I have not much to offer in the way of remark, in addition to the simple description of facts above stated. The instances in which some parts of specimens of petrified wood, have the structure better preserved than the rest, are not uncommon ; but in the detection of the commencement of a mineral deposition in the vessels of the wood, and in Mr. Brown’s remark of the me- dullary rays remaining unchanged, while surrounded by the petrified longi- tudinal fibres, we have, I believe, the first ocular demonstration of progressive steps in the process of petrifaction. Since the above was written, Mr. Arthur Aikin has obligingly communicated to me the following particulars of a piece of wood containing small particles of metallic copper. ** About twenty years or more ago, it was discovered that a bog near Dolgellau in Merioneth- shire, contained small lumps of greenish blue carbonate of copper. It appeared to some speculators in Liverpool, that a profit might be derived from cutting out the peat, burning it, and then smelting the ashes, in which, of course, the copper would be contained. In prosecuting this undertaking (which I believe was soon abandoned) small branches of oak and birch were met with, impregnated more or less with metallic copper. Of these two or three small specimens came into my possession. ** The copper probably came into the bog in the state of sulphate from the decomposition of copper pyrites in the face of some adjacent rock, and was carried thence into the bog by the rain. It must of necessity have entered the pores of the wood while in solution, and then have separated itself from its oxygen and acid, but by what agency is not very clear tome. Both tan and Gallic acid are very efficacious in reducing certain metallic oxids, and these two substances had probably some share in producing the appearances in question.” * Proceedings of Geological Society, No. 48, vol. ii. p. 439. [ 215 ] XVIII.—Remarks on a Section of the Upper Lias and Marlstone of Yorkshire, showing the limited vertical range of the Species of Ammonites, and other Testacea, with their value as Geological Tests. By LOUIS HUNTON, Esa. Communicated by J. F. Royie, Esq., F.G.S. {Read May 25, 1836. ] ON presenting a stratigraphical arrangement of the fossils in the lias forma- tion on the coast of Yorkshire, I wish to offer the following remarks re- lative to their geological distribution. The section (p. 221.) refers to that part of the coast between Whitby and Redcar, in which the Loftus and Boulby Alum Works are situated, and was named by General Mudge “ Easington Heights.” Its greatest elevation is 681 feet. It includes the inferior with a part of the great oolite series ; and the lias is better developed in this place than in any other part of the coast, the upper shale having a thickness of 200 feet, and the marlstone of 160; and there are about 150 of the lower shale also exposed. With regard to the correctness and universality of the order given to the fossils, the position of no one species was fixed till after several had been ex- tracted from the situation indicated in the section, as well as in various differ- ent localities from the Alum Hills, fronting the vale of Thirsk, to the peak near Whitby; and in the majority of instances, from thousands of specimens afforded by the quarrying of the lias shale in the manufacture of alum. Though it would have been easy to have added many more species, the geo- logical situation of which is determined, yet wherever the limits of distribution have not been clearly defined, they have been omitted. Upper Lias Shale-—Commencing at the surface of this deposit, the first fossil present in any quantity, is the Nucula ovum (see section, p. 221.); which, after descending a few feet and entering what is technically called the “ hard or cement stone seam,” occurs in great abundance; but below that bed it 216 Mr. Hunton’s Remarks on a Section of becomes gradually scarcer and smaller, so that after a descent of 60 feet, it is rarely met with, and I believe has never been found so low as the jet rock. The Orbicula reflexa, and the small, but delicate and beautiful Plagiostoma pectenoideum are associated with the Nucula, and similarly distributed. It may be worthy of observation, that the Nucula ovum is singularly character- istic of that portion of the upper shale used in the manufacture of alum, and that wherever the shale occurs without this shell, it has been found unfit for the remunerative production of the salt*. This is owing to the nature of the shale, the upper part, where calcined, being richest in sulphate of alumina ; not, as might be supposed, from containing originally more sulphur, but a less proportion, the lower strata having such an excess of pyrites and bitumen, that the contents of a kiln made from such schistus, invariably overroasts. A large Pallustra, or Amphidesma, (the Amphidesma donaciforme of Phillips) is also plentiful in the upper part; but it is occasionally found in the lower, and a similar shell occurs in the Marlstone. But of all organic remains, the Ammonites afford the most beautiful illus- tration of the subdivision of strata, for they appear to have been the least able, of all the Lias genera, to conform to a change of external circumstances. Of the species, most plentiful in the upper part, scarcely any are found in the lower ; except a few doubtful individuals of A. communis (the prevailing spe- cies in the “ hard seam’’) which are now and then seen so low as the jet rock ; and though A. fimbriatus and A. heterophyllus are found in that stratum, they are always dwarfish, seldom attaining three inches in diameter, whereas in the upper beds, they are met with twenty inches in diameter. The portion of the series mentioned before as the “Jet Rock,” is a very compact and highly bituminous bed, from 20 to 30 feet thick and 150 feet below the surface of the formation. It contains many flattened, pyritous nodules, which generally inclose organic remains. The rock itself is also so very sulphureous, that when a small heap of it was calcined at the Loftus works some time ago, the melted bitumen and sulphur flowed in flaming streams. The whole of the jet used in the manufacture of ornaments, is ex- tracted from this stratum ; for when occasionally met with higher up, it is like coal in its fracture, and too brittle to work well ; and in the inferior strata, as the marlstone, it forms merely a thin coat, enveloping a lump of fossil wood. * The Alum Works, of which lias shale is characterized by the Nucula ovum, are the Peak, on the extreme east, and Stow Brow, Godeland Banks, Sandsend, Kettleness, Boulby, Loftus, Selby Hogg, and Osmotherly, on the extreme west. Failures have occurred to different works in attempting the calcination of the lower portions of the Upper Lias, or those strata undistinguished by the N. ovum. the Upper Lias and Marlstone of Yorkshire. 217 The seams are sometimes 20 feet long by 6 feet broad, but they are often smaller, and their greatest thickness is 3 inches. The Jet Rock is also peculiar for containing the remains of the T'eleosau- rus ; for though Ichthyosauri and Plesiosauri appear pretty equally distributed through the upper shale, this (fluviatile ?) reptile is rarely found but in, or im- mediately above, the Jet Rock. Its bones are generally scattered in separate nodules, the upper jaw being scarcely ever united to the lower. With the exception of the specimen in the Whitby Museum, I am not aware of any instance of this animal having been found entire, whereas the other saurians seldom want more than the head or paddles. On inspection of the section, it will be perceived, that the Jet Rock has its peculiar suite of Ammonites, and here, as was before observed, A. heterophyl- lus and A. fimbriatus make their first appearance, being about the size of a half-crown, while in the “ hard seam” they attain the enormous magnitude of 1 and 2 feet in diameter. ‘The Ammonites Crassulus, (n.s.) common to the whole upper lias, on the other hand, has its greatest development in the Jet Rock, gradually diminishing from 13 inches to 3 an inch in the overlying beds. An interesting, though perhaps it may appear trifling, circumstance attending this fossil is, that as it decreases in size it becomes more numerous, many hundreds being then found together. The lowest bed of the upper shale is hard, compact and sandy, and is sin- gular for its great barrenness of fossils, occurring as it does immediately beneath one so prolific as the Jet Rock. This scarcity, combined with the arenaceous nature of the stratum, may perhaps afford some hints for elucida- ting, hereafter, the anomaly of fluviatile reptiles being mixed up with pelagian shells and fishes. It is a plausible speculation, that during the formation of the upper lias, the bottom of the sea in which it was deposited, was gradually settling. This conjecture is supported, by the greater prevalence of vegetable matter and fluviatile (?) reptiles in the lower part, and the increase in num- ber of the larger species of Ammonites, Nautili, and Belemnites in the upper. This conjecture is further supported by the mineralogical nature of the schistus, silex being more abundant in the inferior parts, and alumina in the superior, an arrangement which would naturally take place, if the coast during that epoch gradually sunk, and the land, the detritus of which afforded the material for the lias, as gradually receded ; the finer argillaceous sedi- ment being consequently carried into the deeper and more and more distant parts. Marlstone.—On entering this series, we at once perceive a striking contrast to the upper lias, for independently of the decided mineralogical difference, VOL. V.—SECOND SERIES. 2F 218 Mr. Hunton’s Remarks on a Section of not only the species and genera, but the order of Testacea have undergone a total revolution. Instead of a preponderance of Cephalopods and a scarcity of bivalves, we now have an overwhelming majority of the latter, some of the beds being almost constituted of Cardia and Gryphytes, which have also an extensive vertical distribution. Avicula Cygnipes, A. inequivalvis and Pul- lastra antiqua are equally abundant in the whole series ; but other shells, as Cardium truncatum, occur more plentifully in the inferior strata, whilst Terebratula triplicata and T. trilineata crowd the superior. The species of Ammonites, though few in number, are, however, highly characteristic ; thus we find A. vittatus about the centre of the series, con- fined to a very small range, associated in nodules with the Cardium multicos- tatum, Turbo undulatus, and Pecten planus ; but the two latter occur in other parts of the formation. The A. maculatus, is constantly found at the junction of the marlstone with the lower lias, which here pass so gradually into each other, that it is impossible to determine where the sandstones end and the blue shale begins. I have long sought for A. maculatus in the upper and central portions of the marlstone, but have never found it many feet above the junction beds ; and though this and other Ammonites from unequal geo- graphical distribution, may be more abundant in one place than in another (A. maculatus is in greatest number at Staithes, 4. Hawskerensis at Haws- kerbottoms), yet they constantly maintain an invariable relative position. A. Hawskerensis 1 believe to be also a junction Ammonite, but from its rarity in other situations, than that mentioned, it is not entered in the table. The above description may not, in some instances, exactly accord with pre- vious statements, but one great source of error has hitherto been, the collect- ing of specimens from the debris of the whole formation, accumulated at the foot of cliffs or other similar situations, where they have long laid, and the inferring of their position from the nature of the matrix. A strong tempta- tion to this method arises from the facility it affords of obtaining finer fossils than can possibly be procured from newly quarried nodules, the hard nature of which renders it very difficult to extract the fossil entire, without long exposure to air and moisture. Annexed is a systematic list of the fossils found in the upper lias and marl- stone, and noticed in the section. the Upper Lias and Marlstone of Yorkshire. 219 List of Fossils found in the Upper Lias and Marlstone*. Genus. Species. Reference. Formation. Ophiura Milleri...... eee ce le is Rts fies BOP. cuss Seelelelele ele wes Marlstone. Pholadomya obliquata ........-.....|Phill. T. xiii. fig. 15.... 0. eee esee ee eees sand —————— ambigua (Lutraria Y.&B.)|Sowerby {, Y. & B. T. viii. fig. 4§ ........ Amphidesma? donaciforme..........|Phill. T. xii. fig. 5...... meehees Ras Seleieelatale Upper lias. ae TOCMUAUEN see eee | Oe Pe Rit, fig. 62636353835 Fopionickoed eee Pullagtrd amitiqua ...sessesceee ses ci Mike Le Kil. fig. 16s ,ccssvcccces Pate cs Marlstone. @ardium'! trancatum).s.¢0ce. 08 os os Sowerby, Phill. T. xiii. fig. EAS he cre ees cla MiMnCOstatGners tite ane |e ue re Ste Hes Ob cake es is Ss.) Se Nucula ovum ......eeee- Svs sacs eowerbyy POUR Ts sit. fie) 4s 3 5.s 6 bd. Merseens Upper lias. Modiola‘scalprum ....sc0scnsccess Sowerby,/Phill Ts xiv; fig.:2 ‘scasc dds. .-| Marlstone. Inoceramus: GUDTUS Ih clei olelcites sc Sowerby, Dhileee Mite hig a LAr 3s ONS ee Upper lias. Avicula cygnipes....-eseceses .oe-..(Enhill. T. xiv. fig. 3. Pecten Y.& B. Pl.ix. fig. 3} Marlstone. Inzequivalvis ..ssevecccccors Sowerby, Phill. T. xiv. HAY a Fie ek tele etties oO Plagiostoma pectenoideum .......... Sowerby, Phill.’F. xin fig. 1305060) ees. Upper lias. = PPCRMANMM © ees scle e 2 « TR MOMUZ o's ore vice weed Honcolouaucuepic otererete Marlstone. PeGtem Sequival vid. .0.-00 cen ose e(SOWErDY, L. CXXKVES 66666668 Siva olsyensheh esters -- sublevis.....0.... eatstae seta Ve Oc-b. El. tev og. 93 Phils T xiv. fig. 5 Gryplied depressd iia cescscseses «[P Mil. L. RIV. fg. Loses JES SEC Werebratula acuta... vaescece ses sf Sowerby, Eni, T. sate fig, 25 00.6... Sas [3 CS sige ace cri ats ac aie Pails Dr sie We Shire ce cies tee east as vas — Compress! ys sess lass Deters OR Wii eae BA 80g 6 ae ote i ielt eres GEERT A) sess cic cla ats vine’ COWL DY, Le IKERIL) fig. Aric. cieeesedens see PrUNGatd ceils aie de stel VolGe Ds 0. Wills MPs d cueidcls wes els wel 0 Se PEUDN CAGE oo are aft onsicie aja on POM eile MO aa es a dialed wesc o's Sete) Orbicula reflexa....... Males efeiete: «slates Sowerby, T. pvi. fig. 1 ..cccecvssees »«+++| Upper lias. Dentalium giganteum........2.20020> Phi Vj S1V5 HE. Siccacc ec cede ccuass .--| Marlstone. Pueho undilatus oe scisess ssa dees Phil T. xt. fig. US ccs ccc ee en sees eyatersiers al Belemnites compressus ...... sees s0/ De Dlamville||, Phill. T. xit. fig. 21 ........ Upper lias. =) ClOMM AGUS 4 <\sngleina) ois div, e cic eis 0's ee VOR cic aicicis cc etacecsascees a oo Nautilus astacoides ...... meg RE ore epee eae Ui SANs P12: 6/05 40s wes eeie.e 3.0@e] Upperlias. Ammonites angulatus:.............. NSOWEEDY, Lo. CVIle. oes cinicwns oe wieiajaie efee.n.¢ ers AMMUAAENG! ery a/e'eles se «ces oie Sowerby, T. ccxxii.....eessens see veeeees — Boulbiensis .........00.- ¥o@ Bip. 267. 00000003 cv eceeseeccece aD ———— communis......... emeaee Sowerby, T. evii. fig. 2. Y. & B. Pl. xii. fig. 3 CONCAVE, sa arate! hays a) chs) sia) ele Sowerby, T. xciv. low. fig. ....+-.06. wceleimte — * In the table, those species only are enumerated of which figures have been published. Where two references are given, the first is to the author who named the fossil ; the second to the work in which a Yorkshire specimen is figured. t+ Phillips, Illust. Geol. Yorkshire, part i. 1829. { Sowerby, Mineral Conchology, 1812—1829. § Young and Bird, Geol. Survey of Yorkshire Coast, 2nd edition, 1828. || Mémoires sur les Belemnites, 1827. [ Observations on Belemnites, Geol. Tr. 2d Ser. vol.1i. ** Observations sur les Belemnites, 1830. A 2 220 Mr. Hunton on a Section of Upper Lias. Genus. Species. Reference. Formation. Ammonites crassus .....+++++++++e+|Phill. T. xii. fig. 15, tuberculated var.......| Upper lias. Cieauitahdd 2 ee Y& sy p- 267 (? elegans Phillips, but we Minti Cetin). jo n:in\nitimet bein ine 0 ine ape ielded EXAaTAatUS..+eeeeeeeeeeees| VY. & B, Phill. T. xiii. fig. 7 ...+eeeeeeeeee fibulatus...........-++++|Sowerby, T. cccevii. fig. 2 ..eeseeeeceees fimbriatus. ..........+++-+|Sowerby, (cornucopia) Y. & B. T. xii. fig. 8.. heterophyllus..........++|Sowerby, T. cclxvi oc eeecccceccccsseees Lythensis. ......+.++++++|Y. & B. p. 267. Phill. T. xiii. fig. 6 ........ MiMIgtAVAMS fis so 00a wes] Ved B. TT; sipefig. By cetews ce mmmatined tnx — OVALS «0 sien ce ndence cen Y,& B. xiii. fig. 4. Phill. T. xiii. fig. 10.... — Sigmifer ....ccdecessecss Phill. T. xiii, figs 4.00 cccccsccscccenes ee Subarmatus ....sceeeee .| Sowerby, T. cccevii. fig. 1....... aS Sere BUDCATIMATOS s wi. 2). se ose Y¥.& B. Phith Bi xi, fg. 3... c csc, a. Woaleotii ../:. of oles ss .poowerby, Levin ¥.& Boxib fig. by is 72.5 5: ear <4 ——_— Clevelandicusis-indons acess of \ 4 (Os Dine ae fig. Noe sicie ets one wecsccune Marlstone. maculatus ........ vaeeee| X- & B, xiviee@. Phill. T. xt. fig. 21 on. « — VittatUS eo reaccocecccoes Y.& B. T. xiv. fig. 11. Ph. T. xiii. fig, 1 variety Lepidotus gigas. syivedasclss(owie's «>» A gassin® 65.6 odes ves prance atacs ie bistro le tie, Sa Upper lias. Ichthyosaurus communis..........+- Conybearet and De la Beche ............ ee is, platyodon.........+.: Conybeare and De la Beche ............-- Plesiosaurus .....20. mpaiaatetas) «[e,.076 0 © Conybeare}......... Stetalte, ahniere alert Ae Teleosaurus Chapmanni ...........- Y.& By PR aeiftige 4d coarse steams « ® Recherches sur les Poissons Fossiles. + Geol. Trans. Ist Ser. vol. v- 2nd Ser. vol. i. t Geol. Trans. 1st Ser. vol. v. 2nd Ser. vol. i. ntl ete tlie Os 5 3 . Section of the Upper Lias and Marlstone at Rockliff, near Whithy (Easington Heights, Mudge’s Survey), showing the limited Distribution of certain Species of Testacea, and the Order Cephalopoda in particular, Local Dip S.W. One Foot in Ten Feet. Sandstone beds, containing Plant seaMS ..s...seseeeseeeee Inferior oolite se eenoeeesereeeees Shale, 10 feet seaeenseeeveceeses Harp or CEMENT-STONE SEAM. Numerous calcareous nodules, exclusively manufactured in- to Roman cement, 25 feet... Nodules in these and succeed- ing beds highly ferrugi- nous, occasionally been smelted at Newcastle Lowest level worked for alum, 90 feet from the surface... 150 feet Jet Rock. Many pyritous nodules, very much flattened, 20 feet...... Hard compact shale, very sandy ; a few small nodules. Very barren in fossils, 30 ft. Main Ironstone Banps, Connected blocks of hard iron- stone, a foot and upwards in thickness, with thin seams of shale intervening, 25 feet... Sandy shale, 5 feet ..... opdooce Tron dogger ....cscossosceseere es Sandy shale, 10 feet............ Tron dogger ..... Aapreceere es aoes Sandy shale, 15 feet..........0. Iron dogger ..... sdecees Scouchane Sandy shale, 18 feet......... ace Iron dogger Shaley sandstone, 10 feet...... seoee Alternations of calcareous sandstone and sandy shale, generally one sandstone bed alternating with another si- milar bed; the seams covered with fossils, 40 feet eeeeeeeee Shaley marlstone ...... Acoeescer Shaley sandstone, gradually partaking of the nature of the lower lias shale, 20 feet LOWER LIAS SHALE, 150 feet above the level of the ANAT AXONS TM I i CT TAR UM OHTVUVIUUASTVTNNLIQTTUORTUTIUTTTCTITOAIBSUUUUNTUULICLNTINATITONATUTCQN ITU ra TT MLE OC ETE pT Tuc a TATHFUCAAQAETLAYSAPERETCTUNN TT TERHUUH EUCLA AYQUUEUULLESSS nage HUY A are eR TID UIUIINOV IU NLUACCILICACCATS ATT Nucula ovum Ammon. communis, Walcottii, subcarinatus. Belem. elongatus. trifidus, with many undescribed species. very abun- angulatus, crassus, fibulatus. dant ; beds subarmatus, Lythensis, Boulbiensis. most pro- annulatus, heterophyllus, fimbriatus. ductive of alum. Naut. Astacoides. Nucula ovum, Plagiostoma pectenoideum, Orbi- cula reflexa. N.B. The only portion of the shale used in manufacturing alum is that in which Nucula ovum occurs. Nodules containing Ammon. sigmifer, elegantulus, exaratus, Mulgravius, concavus, ovatus; occasion- ally Am. fimbriatus and Heterophyllus, though always dwarfish. Lepidotus Gigas (Agas.); rarely met with elsewhere. Teleosaurus Chapmanni, with remains of Ichthyosau- rus and Plesiosaurus, generally in pyritous nodules. Dun HNC a fi ut TTT TMA MUU) At Terebrat. trilineata, very abundant. STOLINUTUCLLAN TT ALAT CTT T OANA CCTM NTO TUNA TTTMOOMUOTONTOL TUN UMNO TTT re ——_—————e—————SSSSSSS5SSSSSs S=—=——SS—_—SS_[==sa_aS=Z==SS=_q5 Am. Clevelandicus. AUK Am. vittatus in nodules, with Card. mulii- costatum. Pecten. planus rarely occurs but in this position. Ferruginous shell seams, with dm. maculatus. Cardium proximum (new species). ' = Tnoceramus dubius and an unde- scribed Belem. , Turbo turritus, Pholadomya Modiola scalprum, Belemnite, n.s., Plagiostoma Hermanni, Pullastra crassa, Pholadomya (ambigua Y. & B.). siterminus Ophiura Milleri, Belem. angulatus, cras- obliquata, iforme and A. rotundatum (Phillips), all in ber in the upper part, gradually diminishing Am. heterophyllus and fimbriatus, Belem. com- nhidesma donac pressus, with Amp reatest perfection and num various genera and species. in quantity downwards. Ammon. crassulus, Ichthyosaurus platyodon, I. communis, with Saurian bones of g Pecten sublevis and equivalvis, Sy Gryphea depressa, (Dentalium hiefly in lower part), Terebratula Pullastra antiqua, Turbo undulatu giganteum, Cardium truncatum ¢ compressa, triplicata, and bidens, Belem., n.s., Terebra- Avicula cygnipes and inequivalvis, tetredra, tula acuta. H y a ‘i ; ‘We “ = y aay i y : ; oo) * ao | z ae “sti ung | | bane pee . . ATI en $ he oe rem a ’ fi hd a J 1 Ae ole kn, re » SG caw’ Os hareygetein Pie (iat bel cure Lee OF oT 4 fay [ 223 ] X1X.—On the Distribution of Fossil Remains on the Yorkshire Coast, from the Lower Lias to the Bath Oolite inclusive.* By W. C. WILLIAMSON, Ese., (CURATOR OF THE MANCHESTER SOCIETY OF NATURAL HISTORY.) [Read May 7, 1834, and November 2, 1836.] THE formations noticed in the following pages are the lias, the inferior oolite, the lower carboniferous series of Smith, and the Bath or great oolite. Lias. The lias series on the north-east coast of Yorkshire, occupies a range of lofty cliffs, varying from 100 to 600 feet in height, and extending with little inter- ruption from the Peak Hill, near Robin Hood’s Bay, to the village of Saltburn, near Redcar. It is separable into three great divisions, Ist. the lower lias, 2nd. the marl- stone, and 3rd. the upper lias or alum shale. 1. Lower Lias.—On no part of the coast is the whole of this division exhi- bited, or has its depth been ascertained. At the base of Rockcliff, near Staithes, it has a considerable thickness, and at Peak Hill, a section of about 300 feet is exposed. It is probable, however, that its vertical dimensions are much greater, as blue clay is brought up by ships’ anchors at a considerable distance from the shore; and as Trochus Anglicus with some other fossils, is found only among the shingle, generally much water-worn, and apparently washed up from submarine strata. At present, nothing is known of the fossils contained in those inferior beds. In the exposed portion, the marl, in the lower strata, is compact, arenaceous, and generally of a dull blue colour, whilst in the upper it is more shaly. The fossils are thinly scattered, and few in species. On the scar at Robin Hood’s Bay, near the lowest known part, occurs Gryphea incurva, and alittle higher Gryphea Machullochi, both in great abundance ; and associated with the latter, is sometimes found Gryphea depressa. A little above this bed is a seam which also contains organic remains, the most common, being Hippopodium ponderosum, Pholadomya ambigua, Pholadomya * Inthis memoir two papers are embodied, one, on the distribution of Lias Fossils, on the York- shire coast, read May 7th, 1834: the other, on the distribution of Oolitic Fossils, read Nov. 2, 1836. 994 Mr. Wiiu1amson on the Distribution of Murchisoni, and Pinna folium. They are found at Robin Hood’s Bay, and near low water mark, under the heights of Rockcliff. At the former locality the Hippopodium preponderates, and at the latter the two species of Pholado- mya. The Pinna, which occurs at both places, is sometimes obtained of a very large size, and one which I measured at Rockcliff was two feet in length ; but, as is usually the case with this fossil, it was so crushed that it could not be preserved. Towards the lower part and about the middle of this division of the lias, are found Ammonites planicosta, with fragments of Pentacrinus Briareus and P. vulgaris, (P. caput Meduse, Miller ), principally broken columns, which are very numerous, particularly at Robin Hood’s Bay. Still higher in the series, and towards the top of the sandy strata, I have procured Ammonites cornu- copia, A. Turneri, and A. geometricus, especially opposite the Boulby Alum Works; but I am rather undecided respecting these fossils, as they are rare. Thestrata next in succession are softer, and separated by seams of irony nodules, having below them at Robin Hood’s Bay and Skinningrave, a bed which contains the little Plcatula spinosa. 'Towards the top of the lower lias rock, Belemnites compressus occurs, though not very plentifully. I found it princi- pally at Boulby, where the highest beds are well exposed, 2. Marlstone—The next series of beds belongs to the division called the Marlstone ; and has an average thickness of about 130 feet. The first hun- dred feet are composed of alternating sandy and shaly seams, and the next or upper thirty of sandy shales, divided by bands of argillaceous, irony nodules, which are sometimes united in solid strata, 6 inches thick. Towards the lower part of the division Cardtum truncatum is very plentiful, especially near Staithes. An interesting fact is connected with this shell. The specimens which have both valves united, are found distinct from those with the valves separated ; in the former the casts of the ligaments are preserved, but in the latter they are wanting. In the sandstone seams towards the middle and lower part of the series, are found the following fossils in great numbers and confusion. Ophiura Milleri, O. loricata, Asterias Murchisoni, nob. in Mag. Nat. Hist., Cidaris, with smooth spines, Dentalium gigantewm, Belemnites elongatus, Pla- giostoma leviusculum, Modiola scalprum, M. Hillana, Avicula inequivalvis, Gryphea Bullata? Ostrea. Of these, Ophiura Milleri, O. loricata, Asterias Murchisoni, Plagiostoma leviusculum, Modiola scalprum, and the Cidaris are the most rare; the others, especially the Ostrea and Avicula, form immense masses, almost entirely composed of compressed and broken shells. This portion of the stratum is best examined on the shore between Staithes Fossil Remains on the Yorkshire Coast. 995 and Saltburn, where large blocks of the sandstone have fallen from the cliffs. Above these sandstones is a layer of detached, irony and calcareous nodules, very rich in fossils ; the principal being, Ammonites Clevelandicus, A. Stokesit, Turbo undulatus, Isocardia lineata, Cardium multicostatum, Corbula cardi- oides, Amphidesma recurvum, Mya V. Scripta, M. literata, Terebratula bidens, ‘T. subrotunda, T. tetraedra, T. triplicata. Of these, Ammonites Clevelandicus, Cardium multicostatum, Isocardia lineata, and Terebratula tetraedra, appear to be the most abundant. Hight or ten feet higher, is a series of beds from twelve to fourteen feet thick, consisting of arenaceous, blue shales, divided by bands of ironstone. The shales are filled with a profusion of fossils in a fine state of preservation, but difficult to extract, owing to the fragile nature of the shell, which is easily separated from the cast. The following isa list of the species : Pecten equi- valvis, P. sublevis, Avicula cygnipes, A. inequivalvis, and Plicatula spinosa ; also two species of Belemnites. The principal locality for these fossils, is under the signal cliff at Staithes, where the shales are near the beach and better exposed than elsewhere. In the uppermost bed of ironstone, dividing the marlstone from the upper alum shale, the Ammonites Hawskerensis is found, at the south point of Runs- wick Bay, and associated with it, at Skinningrave, is a small fossil, apparently a Trochus. 3. Upper Laas or Alum Shale.—This division consists of three very distinct deposits, which are extremely persistent. a. Lowest part, soft shale .........006+ oe sepa videdsccdvietepe 15 to 20 feet. b. Hard shale, ditfering from the preceding in being much more tenacious, and in the lamine breaking into larger fragments, about .........+ 30 c. Shale resembling the lowest part, being soft and rubbly, and breaking into very small fragments, average thickness about.........+seeeeees 130 Though well distinguished by lithological structure, these deposits are much better characterized by their fossils. (a.) Near the junction of this deposit with the marlstone, Belemnites com- pressus occurs in considerable numbers, in a thin layer, especially at Runs- wick Bay ; and at the top, almost immediately below the hard seam (d), is a layer of argillaceous nodules, which is first seen about a mile north of the village of Staithes, and again under the cliffs at Lyth. At these places the shale, on the Scar, is completely studded, for forty or fifty yards, with round con- cretions, each containing either one or two Ammonites annulatus, or the alveo- VOL. V.—SECOND SERIES. 26 226 Mr. Wittiamson on the Distribution of lus of a Belemnites compressus, the solid portion projecting from the nodule, and resting in the shale. The number of these fossils forms a remarkable feature. (b.) About the upper part of this deposit occurs Belemnites tubularis, which is almost universally depressed at the smaller extremity, indicating apparently, that it was thin and delicate. It forms a regular but thin layer, a few inches above or below which it has not been noticed. I have seen it only on the Scar, a little to the south of Whitby, where Belemnites compressus is also found. The top of this deposit is occupied by numbers of Ammonites ele- gans, and Inoceramus dubius, the former being almost always depressed and as thin as paper; and both it and the Inoceramus are beautifully coated with iron pyrites. Throughout the greater part of these shale beds, the fine hard jet, so valu- able for manufacturing ornaments, is found in lenticular seams, from half an inch to three inches thick. It is obtained in quantity only in this deposit, which is called by the workmen the “ Jet Seam.” Towards the middle and upper parts of the seam, large fragments of bi- tuminized, coniferous wood occur, some of them weighing nearly a hundred pounds. (c.) This division is by far the most interesting of the three, in its fossil contents. Near the lowest part are immense numbers of spherical nodules, all strongly charged with sulphuret of iron. They vary in size from a small nut to six or eight feet in circumference, and often contain Ammonites exaratus, and A. elegans. These nodules are well exposed between Staithes and Runswick. A little higher is a bed in which numbers of Nucula ovum occur. This fossil is generally diffused through the upper part of the series, but more par- ticularly in this portion. Associated with it, and sometimes even attached to it, is found Orbicula reflexa. A very small variety of Avicula inequivalvis is met with in the same stratum. In all the lower portions of this division, (the one from which alum is pro- cured) the remains of Saurians have been found:; and some of the specimens cbtained from it ornament the museums of Scarborough, Whitby, and Mr. Witham, of Lartington. As yet, I believe only one species of the Teleosaurus and one of Ple- stosaurus have heen discovered, but two, and probably more, of Ichthyosau- rus. One of them corresponds with J. tenwirostris, and the other must have been an immense species, as I have seen a lower jaw which is seven feet in length, and has many of the teeth preserved, some nearly three inches long. The Plesiosaurus varies in size, but from a comparison of detached bones 7— Fossil Remains on the Yorkshire Coast. 99% with those of more complete specimens, the animal appears to have averaged from fifteen to twenty feet in length. The large specimen in the Scarborough museum would measure, if complete, at least eighteen feet. Its general characters resemble those of the Plesiosaurus common in the lias of Dorset. The Teleosaurus Chapmanni is sometimes found with the remains of the bony plates or scales attached, as in the splendid Whitby specimen, and some fragments in the Scarborough museum. It is rarely obtained with a perfect snout, the dilated extremity* being generally broken off. Above the beds containing these remains, the large and beautiful Nautilus astacoides and Ammonites Heterophyllus occur in argillaceous nodules. When slit, they present beautifully the internal generic distinction, the chambers being generally filled with calcareous spar, and the siphuncle with only lias shale. The surrounding nodules, in some rare instances, are composed of sulphuret of iron. In this portion of the series, large fragments of bitumi- nized, coniferous wood are very common, having occasionally a thin coating of jet. From thirty to sixty feet above these strata, Ammonites Walcotti and A. ovatus occur, both in the shale and argillaceous nodules. At the Peak Hill, near the top of the upper alum shale, T'rigonia literata and Ammonites crassus are found in a thin layer. The latter is remarkable for the thickness of its whorls, and the frequent decomposition of those which constituted the centre of the shell. A little above these strata, Ammonites communis, and A. fibulatus are invariably found in small nodules, especially at the Peak to the south, and at Hawsker, to the north of Robin Hood’s Bay. At both places the upper portion of the stratum is seen to great advantage as it descends to the Scar. At the Peak, imperfect remains of an Astacus occur in the same layer of nodules, but generally so crushed that its character is indeterminable. The top of this shale at the Peak Hill, appears to contain Ammonites striatu- lus, enclosed in indurated calcareous masses ; and I am not aware of its having been met with at any other locality. It occurs so near the top that doubts are entertained whether it belongs to the alum shale, or to the overlying in- ferior oolite. InFERIOR OOLITE. The subdivisions of this formation next come under our notice. They are best seen at Blue Wick, which presents the following ascending section : a. Thick beds of dark grey, finely grained sandstone ......eeeeeeeees 20 feet. 6. Irregular beds of yellow sandstone .........ccecerccsconvesccees 20 * See Buckland’s Bridgewater Treatise, Pl. 5. 262 ea Mr. Wixtiamson on the Distribution of c. Hard ironshot sandstone .occescscseccrcnscesevess vecnceesene 1) feet. d. Irregular beds of yellow sandstone, in some parts ironshot.......... 30 €. Hard ironstone sococseccescccssccsccsen ge Uae sip is 6S ow ein Stwlermies 4 Ff. Hard ironstone ...cccsecvcvcccccccncccncrcesecoerenseoevess 8 (a.) At the bottom of this bed, we find a number of argillo-calcareous nodules, resembling those in the upper alum shale, and containing 4mmonites striatulus, Ammonites, (a new species), Orbicula reflexa, Lingula Beani, Terebratula bidens, and Avicula echinata? 'These fossils are chiefly obtained at Blue Wick. No other organic remains occur until within ten feet from the top of this divi- sion of the formation, where a layer of small nodules is met with, enclosing Astacus rostratus, and a new and larger species which has also been found in the clay of the cornbrash. A beautiful specimen of an antenna is in the Scarborough Museum. A little higher in the series is a thin but extremely characteristic seam of Vermetus compressus, also obtained in the coralline or Oxford oolite. (b.) Proceeding upwards, we arrive at the series of irregular layers of soft yellow sandstone, throughout the whole of which small fragments of dicotyledonous? wood, and a species of Belemnites are rather numerous. Towards the top I have found, though rarely, Mya literata, and still higher, two species of Ammonites, one of which resembles A, concavus, which also exists in the upper lias. The other is a new species, which I have named A. inornatus. | (c.) The next bed, a hard ironstone, contains numerous, small, grey peb- bles, also the same Belemnites as in the seam below, and is characterized by a great abundance of Terebratula trilineata. (d.) The beds of yellow sandstone, occasionally charged with oxide of iron, enclose, within a few feet from the bottom, two seams about four inches each, of small pebbles, and at the top is found the same Belemnites as in the beds } and c though sparingly scattered ; the shell resembling Avicula echinata is mingled irregularly with the pebbles. (e.) From the hard ironstone bed, though only four feet thick, are ob- tained the greater portion of the fossils characteristic of the inferior oolite on the Yorkshire coast. The following is a list of the principal species, which chiefly occupy the middle and lower parts : Trochus granulatus. Auricula Sedgvici. — ‘bisertus. Nerita costata. pyramidalis. Turbo levigatus. Solarium calix. funiculatus. Actzon humeralis. Rostellaria composita. ‘Fossil Remains on the Yorkshire Coast. 299 Natica adducta. tumidula, Ostrea Marshii. solitaria. Astarte elegans, Trigonia angulata. costata. striata. gibbosa. Avicula Braamburiensis. Nucula axiniformis. minima. Modiola pulchra. Isocardia concentrica. cuneata, Cardium incertum. Mytilus subleevis. Pholadomya ovalis. Cardita similis. Unio abductus. Pecten virguliferus, Gastrocheena tortuosa. abjectus. Towards the upper part, are found, Turritella muricata. Terebratula obsoleta. quadrivittata. Caryophyllia convexa. humifusa. whilst the top of the seam is characterized by Turritella cingenda, Melania Heddingtonensis, and Terebratula obsoleta. (f.) The highest beds of the inferior oolite consist of seven or eight feet of hard ferruginous sandstone, and are apparently destitute of fossils. The Ammonites striatulus, Lingulus Beant, Orbicula reflexa, Terebratula bidens, and the Avicula echinata sometimes occur in one mass in the lowest bed (a.). The Lingula and Orbicula are always found together, but the Ammonites are more frequently in masses by themselves. The Avicula and Terebratula bidens are very rare. The characteristic fossils of this stratum are given by Professor Phillips in his Geology of Yorkshire, and the list continues correct. Lower CARBONIFEROUS SERIES OF SMITH. With the exception of the upper sandstone and shale, the divisions of this series are the most irregular of any on the Yorkshire coast. I have, however, taken sections at nearly every point where the series occurs, and I have been guided in my details by those which appeared the most striking and uniform. The best defined and least irregular are at the elevated cliffs between Clough- ton Wyke and Blue Wick, where the whole of the series is well exposed ; and where the upper and middle beds, containing the greater portion of the fossil vegetables, are alone visible. The following section is in ascending order : (a.) Immediately above the inferior oolite, is a black carbonaceous shale, con- taining no vegetable impressions ; about ........-0+- Sdine donsen bod 10 feet. 230 Mr. Wixuiamson on the Distribution of (b.) Ironstone, containing a large species of Calamites, fronds of Zamia gigas, and remains of a remarkable fossil, apparently connected with the fruc- tification ofa wiges mamcinace BMics bo.auis os -)+ | ose aGisiieibitins vvl>piniaih wae 20 feet. (c.) Hard, pale, gritty isandstone < oo. so. ve ccc nc snus ce cons oo@uswiswisinnn 20 Ud) Shales watethsieteteetebe siete Oe «e's o's occa a oa bsiiwin wipeammels immune wy pee ALO (e.) Gritty sandstone resembling the bed c ...........- is pale ie ii nite Sie «+ 20 (f-) Soft yellow sandstone, containing stems of Bauisaiaes Piuaies in a ver- tical position, with their roots downwards ........eesseeeeesseenee 8 [The opinions respecting these stems being deposited perpendicularly, are various ; but that given by Professor Phillips, and urged by Mr. De la Beche in his Geological Manual, appears to me the most probable ; viz.—that the plants were transported to their present positions, and deposited with their roots downwards, in consequence of the greater specific gravity generally possessed by the roots of this class of plants. The upper extremities being all broken off, afford rather a strong proof of their having been exposed to the action of disturbed water. We should expect to find the same effect produced upon the delicate vascular Equisetz of the present day. The place whence they have been transported, cannot however have been far distant, or they would have been still more disjointed and compressed; on the contrary, they often retain all their original roundness. | (7) Bleek Abale Deis o's ope ms © a)m on ae ayaa ee sales lavas aiesa(e Minions tet hibia cjsrarers es’ iki 5°) vei (h.) Sandstones and shales of varying thicknesses. The sandstones are hard, fissile, and used as flags ; total thickness about ........-...+++ Eee) tO (i.) Resting upon this series is another group of sandstones and shales ; divided as follows :— The lowest part, dark shaly sandstone ........ auuvinsie's ata se || VO ROCs Harder, gray sandstone .....ccessccccccccccecscssevcccs § 6 Laminated sandstone, which contains numerous remains of beau- tiful ferns and cycadean plants ........ 22404: eer Sess wcoe «66 20 The following is a list of plants obtained from the group: Equisetum laterale. Pterophyllum pectinoides. Lycopodites Williamsonis. ——___—— minus. falcatus. Zamia lanceolata. Thuytes expansus. Otopteris acuminata. _ Sphenopteris ? longifolia. Cyclopteris digitata. hymenophylloides. Teniopteris vittata. Neuropteris ligata. Solenites Murrayana. Pecopteris curtata. Tympanophora racemosa. — Whitbiensis. simplex. ——-— Williamsonis. Seeds of a Cycadites*. The superior strata of inferior oolite composed of about 170 feet of sandstone and shale, con- * Towards the lower part, it also contains thin seams of jet, of a quality inferior to that procured from the lias. Fossil Remains on the Yorkshire Coast. 231 tain no remains cf well defined plants; but near the centre of the series is a seam of inferior coal, about a foot in thickness, which is worked at Cloughton, but only for burning in limekilns. The plants of this lower series of carboniferous shale, except when found in ironstone, ave far from being so beautiful and well preserved as those in the upper shales; from which they also differ in the greater abundance of Pterophyllum minus, Otopteris acuminata, Sphenopteris hymeno- phylloides, and the deeply lobed variety of Cyclopteris digitata, and are apparently characterised by Pterophyllum pectinoides, Equisetum laterale, Zamia lanceolata, and the Tympanophora of Lindley and Hutton. The thick beds of sandstone may be readily traced along the shore, but the other portions are very variable. The sandstones are generally micaceous and hard, but split readily, and are exten- sively used as flags. As building stones they are much inferior to many of the beds above the great oolite. We will now proceed to describe Tue Great or Batu Oouirte. The lithological characters or fossils of this formation vary very little to the north of the White Nab, near Scarborough, but to the south, a striking change occurs, which will be described in its proper place. We will first examine the sections at Cloughton Wyke, and the White Nab, where the great oolite presents the following general arrangement. a. The lowest bed, a hard blue limestone ...... 14 to 20 feet. b. Hard, blue, fine-grained oolite, sometimes ironshot .. 6 c. Hard, blue clay, often much tinged with iron ...... 2 dy. (Nodular ironstone; Six Inehes\ tO) Vejasilcle esi sinus lee © © 1 foot. Biba Clavie te laiatnipret Saba ooreial ern 2 0Ne afiala\Giaiwiciowetere e'm's ses © 1 f. ayers of nodular ironstone and argillaceous oolite .. 3 feet. (a.) No fossils have yet been discovered in the lower and middle portions of this division, but towards the upper, Ut have found a species of Ostrea, Amphidesma decurtatum, Mya calceiformis, and an undescribed Ammonite ; and the top of this bed contains Belemnites compressus, B. Aalensis, Me- lania Heddingtonensis, Amphidesma decurtatum, Serpule ; and in a layer between this bed (a) and the hard blue, fine grained oolite (6), are found large tuberculated spines of a Cidaris. Of the Belemnites, the species which I consider to be the B. compressus of Sowerby, not Voltz, is occasionally twenty inches in length, and about two in diameter ; and the diameter of the other, B. Aalensis, is three inches, but the length is not more than seven. The spines of the Cidaris are sometimes five inches long, and about the diameter of an ordinary goose quill. Though they are not rare, I have found no traces of the Cidaris itself. 232 Mr. Wittiamson on the Distribution of (6.) This bed is apparently destitute of organic remains. (c.) The following fossils have been found in this stratum, chiefly at Cloughton : Rostellaria composita. Gervillia acuta. Acton glaber. Cucullea cancellata. Terebra vetusta. Astarte minima. Phasianella cincta. Cardita similis. Trochus. Pholadomya acuticostata. Avicula Braamburiensis. Plesiosaurus. Of the Plesiosaurus, we have remains of only one animal, which was found by my father near Scarborough, in 1825. To judge from the size of the humerus and femur, the creature was twelve or fourteen feet long. ‘The bones which have been obtained, consisting of the humerus, femur, vertebre, and phalanges, differ but little from those of the Plestosaurus Dolichodeirus of Whitby and Dorsetshire. The humerus, however, at its flattened extremity, expands equally on each side like the femur of P. Dolichodeirus. ‘Two detached teeth have been found, which, if they really belonged to this animal, will prove a strong character in distinguishing the species. They are about an inch in length, nearly smooth, and very much resemble those of the crocodile. (d.) The nodules of ironstone sometimes contain specimens of Ammonites Blagdent. In this seam a mass of extraordinary bones was found, at the White Nab, near Scarborough. T'wo of the bones agree in form with those represented in fig. 4 and 5, of Mr. Mantell’s ‘ Illustrations of Tilgate Forest,” and supposed by him to be the metatarsal bones of the lguanadon. The lon- gitudinal circumference of the Scarborough specimens is 11+ inches, and the transverse 10+ inches. ‘The same mass contains also three bones, which re- semble the humerus of an unknown Saurian, given in Pl. 14, fig. 3 and 6, of the same work. Their length is 14 inches ; the circumference about the middle of the shaft, 81 inches ; and around the condyle, 16 inches. There are two other bones which are supposed to be tibias. They are ten inches long ; and their circumference at the superior extremity is 151 inches. The circumference at the vertebral extremity of the fragment of a rib is 5+ inches, and about the middle of the bone 6 inches. The same mass encloses also a singular bone, something resembling in form the humerus of an Ichthyosaurus: the length of the supposed, cubital, articulating extremity is 8+ inches, and the diameter 7 ; while the diameter of the cylindric part, at four inches from the above extremity, is 31 inches. The Fossil Remains on the Yorkshire Coast. 23a entire length of the bone when perfect is uncertain, but it appears to have been of gigantic size. The only portion of a vertebra is a fragment 43 inches long by 2+ inches in diameter. It is very possible that these remains may belong to the Megalosaurus ; and if this should prove to be the case, we shall have in the superior beds of the great oolite of Yorkshire, some of the interesting fossils of the Stones- field slate (e.) The seam of clay, above the ironstone, contains Amphidesma decur- tatum with fragments of Avicula Braamburiensis, and of a Gervilia. (f:) The next bed, consists of nodular ironstones, separated by alternating seams of argillaceous oolite, each layer being generally about eight inches thick. In the lower argillaceous seams at Cloughton Wyke, Perna quadrata occurs rather abundantly, and in the upper are the following fossils : Melania Heddingtonensis. Gervillia acuta. Terebratula spinosa. Trigonia costata. Gryphea nani. clavellata. Ostrea Marshii. Astarte minima. Pecten Jens. Corbula depressa. Plagiostoma interstinctum. Pinna cuneata. Avicula Braamburiensis. Pentacrinus vulgaris. echinata ? Cidaris vagans. The most abundant of these are Avicula Braamburiensis, with the species resembling A. echinata, Plagiostoma interstinctum, Gervillia acuta, and Astarte minima. Of Trigonia clavellata, I have found a single specimen, at the junction of one of the lower argillaceous seams, with a layer of ironstone. It agrees with the fossil found in the Cornbrash. The Cidaris vagans is rare, and not being larger than a shilling, can have no connexion with the long tubercular spines before men- tioned ; but the smaller spines which I shall have occasion to mention, may belong to it. In the hard beds of ironstone, Ammonites Blagdeni sometimes occurs, but more rarely than in the bed d. I will now describe the upper part of the Bath oolite, at two other locali- ties on the same range, and not more than three miles from White Nab. These points are at the northern and southern extremities of Cayton Bay, and at low water, on the south side of Carnelian Bay. At the south point of Cayton Bay we find the following descending section. a. Soft beds of argillaceous oolite, containing Amphidesma decurtatum, Belemnites compressus, Avicula Braamburiensis, and large tuberculated spines of a Cidaris resembling those in the layer (a.)p. 231 ...... aisvetatiehev esas Sec od header b. Alternations of sandstones and carbonaceous shales .....-eseeeceeeeeees VOL. V.—SECOND SERIES. 2H 234 Mr. Witutamson on the Distribution of e.* c. Sandstone, sometimes containing Pecopteris Williamsonis and Otopteris obtusa 1 foot. d. Tenacious blue shale; the lower part carbonaceous: in this seam all the beautiful Gristhorpe plants occur .. 1.1... cree eee ce sree cers cece cov» 4 feet. e. Impure coal 6... seeeee cece cece eect cence eee eeeeeeesecseretecnns 3 inches. f. Alternating sandstones, ironstones, and shales i+ © wisleisie Mibate vei ciete cinirete mene 25 feet. g. Irony nodules sess ceceeeseeece cece ce ceeetset crac renseseecess cece 1 foot. h. Hard granular bed, very much ironshot, especially at the fissures.......... 8 feet. From the occurrence of the large tubercular spines of a Cidaris, of Avicula Braamburiensis, and Belemnites compressus in the thin calcareous seam, (a) it appears clear to me that the upper beds of the Bath oolite, which at Cloughton Wyke and White Nab are at least thirteen or fourteen feet thick (p. 231 from the top of a to f ), are here diminished to three. If this opinion be correct, all the mass of sandstones at this point, considered by Professor Phillips as belonging to his Upper sandstone and shale, must necessarily be removed from that series, and be considered as merely a local and subordinate division of the portion of the oolites of Bath and Brandsby, to which the name of Great or Bath oolite is more particularly applied; and the beds (g) and (h) will form the lower portions of the series thus removed. I should arrive at this conclu- sion for several reasons. Ist. The occurrence of the three fossils above al- luded to, which are not met with in the cornbrash of the Yorkshire coast, the only other formation to which the calcareous bed (a) can be referred, are found together in the upper beds of the Bath oolite; 2ndly, the existence of beds of sandstone filled with carbonaceous fragments, evidently belonging to the upper sandstone and shale, resting upon the calcareous deposit, whilst in the immediate neighbourhood, we find the cornbrash, surmounted by the Kelloways Rock ; and lastly from the absence of the blue clay, upon which the cornbrash of the vicinity reposes. These inclosed sandstones do not appear to extend more than two miles along the coast ; and I suppose they thin out beneath the low water mark in some part of Carnelian Bay, as at its northern extremity, or White Nab, we find the supe- rior oolitic beds in their true position; whilst at its southern point, or Ewe Nab, the ferruginous beds occur as atGristhorpe. So small a portion of the super- incumbent sandstones are here exposed, owing to the low cliffs being partially covered with diluvial clay, and the beach with sand and gravel, that we can- not compare them with the section at the opposite side of the bay. On the south side of this point is a small dislocation, but from the limited space between this ferruginous bed, and the spot where the cornbrash first appears to the south, 1 should say that even here the sandstones are far less extensive than at Gristhorpe. In the middle of Gristhorpe Bay a singular depression of the superior rocks, sinks these measures far beneath the line of low water, eee Fossil Remains on the Yorkshire Coast. 235 but they rise into the cliff at the southern point, where we find most of the plants figured by Prof. Phillips in his Geology of Yorkshire, and by Lindley and Hutton in their Fossil Flora of Great Britain, as from the “‘ Upper Sandstone and Shale.” How far the series continues under the sea to the southward, I have no means of ascertaining. This interesting deposit bears every appear- ance of a Jocal accumulation, resulting from some eddy or current produced by the flow of a river into an estuary. The hard granular bed (h) is literally one mass of fragments of Millepora stra- minea, large papilla of a Cidaris, resembling C. florigemma, an innumerable quantity of small smooth spines of another species, which I before alluded to as probably connected with C. vagans, a small muricated spine belonging to the same genus, and small columnar joints of Pentacrinus vulgaris. All these are deposited in extremely regular and even layers, which are so close to each other as completely to fill the rock ; the Millepora being found only at the top. This bed, from the quantity of iron contained in it, is extremely hard, and altogether different from any other part of the series. If the view I have taken of the sandstones, &c. be correct, it will leave but a very small number of fossils to the true upper sandstone and shale. The planis found in the seam (a) are nearly all new to geologists: the following is a list of such as have already been figured by M. Brongniart, Professor Phillips, and Messrs. Lindley and Hutton. Pecopteris lobifolia. Cyclopteris digitata. insignis. Glossopteris Phillipsii. undans. Teeniopteris vittata. polypodioides. major. propinqua. Solenites Murrayana. Williamsonis. Lycopodites Williamsonis. acutifolia. Sphereda paradoxa. ——_—— obtusifolia. Pterophyllum comptum. —————. dentata. ——_—_—_—— pecten. ——_—— exilis. —___— minus. ceespitosa. Otopteris cuneata. Neuropteris recentior. —— Beanii. ligata. Ctenis falcata. arguta, Cycadites tenuicaulis. Sphenopteris stipata. Dictyophyllum rugosum. Williamsonis. Equisetum laterale. Cyclopteris Beanii. Winged seed. I have also in my collection several new species, especially of Sphenopteris, (two species,) Glossopteris and Cyclopteris. 2H 2 236 Mr. Wixttamson on the Fossil Remains in Yorkshire. With but few exceptions, these plants are all characteristic of the shales in which they are found. The following species also occur in the lower sand- stone and shale. : Pecopteris Williamsonis. Teeniopteris vittata. Neuropteris ligata. Solenites Murrayana. Sphenopteris stipata. Lycopodites Williamsonis. In the same seam I have found Cypris concentrica, Unio distortus, (Bean) and another undescribed species of Unio. This fact, combined with the ab- sence of marine remains, would seem to indicate that the origin of these sandstones and shales is lacustrine, a fact of which I have little doubt. If this be correct, it would appear that a considerable time must have elapsed between the deposition of the marine fossiliferous divisions forming the top of the Bath oolite and the hard ironshot seam of Crinoidez, upon which the sandstones and shales rest. The fossils characteristic of the oolitic seams of the great oolite are few, as they bear a general resemblance to those of the cornbrash and inferior oolite. The long tuberculated spines of a Cidaris have not been met with in this neighbourhood in any other rock. Professor Phillips has pointed out Phola- domya acuticostata and Rostellaria composita as characteristic of the stratum, and on the coast, at least, | am not aware of the following fossils having been found in any other. Ammonites Blagdeni. Terebratula spinosa. Belemnites Aalensis. Large spines of a Cidaris. Phasianella cincta. To these may be added the mass of gigantic saurian bones from the layer of ironstone. The Bath oolite on the Yorkshire coast is not extensively used as a build- ing-stone, but the lower part of it, and the hard crinoidal bed at Gristhorpe Bay and Ewe Nab, have been very successfully employed in erecting the piers at Scarborough. These beds are remarkably durable, and are conse- quently well calculated for strong water-works, where no particular smooth- ness is requisite. The attempt has been made to procure lime from some of the beds, but with so little success as to check further trials, especially in a country where a superior material is abundant. a ae [ 237 ] General Stratigraphical Table of the Formations described in the preceding pages, but in descending order. GREAT OR BATH OOLITE. Cloughton Wyke and White Nab, 30 feet. Layers of nodular ironstone and argilla- ceous oolite......... akeLei sisi shel aiehe ts 3 feet Clay xcaviotea ats 346s -Hiabee SWE ae 1 Nodular ironstone, 6 inches to ...... 1 Hard, blue clay, often much tinged with GOT elereistere Mhevenstel cial shart elevate ar etaliers 2 Hard, blue, fine-grained oolite, some- times ironshot...... aia stohave sisteteiens 6 A hard, blue limestone ........ 14 to 20 Cayton, Bay, South Point, 51 feet. Soft beds of argillaceous oolite ...... Sandstone and carbonaceous shales .. 9 Sandstone Tenacious blue shale ; lower part car- bonaceous: Gristhorpe plants .... 4 3inch. Alternating sandsts., ironsts., & shales 25 feet. Impure coal...... wf siieiatst a iateiat cts ia/elane TOGMIEMG AMIE <..,c14,0+0gacane:s:alerale jn)»: clotesein ciel oie! Bieleraners aXoNerene srstetelstes eve e tts ehaseteelerotctele 100 Lower Lias, Peakhill. In the upper beds the marl is shaly, in the lower, compact, arenaceous, and generally of 300 a dull blue colour, visible thickness ......secccsccvecrccccrcsserrcvssevcvees 238 Mr. Wiuttamson on the Distribution of Systematic List of Fossils noticed in Mr. Witu1aAmson’s Memoir*. GENUS AND SPECIES. Thuytes expansus .... Cycadites tenuicaulis Zamia lanceolata Pterophyllum minus .......+- Equisetum laterale.......- ate Sphenopteris? hymenophylloides ? longifolia ...... —— stipata .. — Williamsonis .... Cyclopteris digitata .......-- IRGANIT cislcic:etelale oie Glossopteris Phillipsii_ . Teeniopteris vittata.......++- Pecopteris curtata ......++.- acutifolia .. -_—_—— INSIQMIS .e.eeeeees Ho bitolia’ss:.'.is.s.etelsie =TODEUSILOLIA o/c. e.cte oh polypodioides propinqua .... ———=— = UNGANS- ceccveseds Williamsonis Lycopodites falcatus ........ Williamsonis .... Neuropteris ligata ..... recentior ——— pectinoides .... comptum ..... pecten ......-. ceespitosa .....eee dentata ....--see- arguta eee REFERENCE, FORMATION. Sternbergt, Phill. 10, fig. 11.4, | Lind. and Hut. 167§ ........ ai Low. sands, and coal. Paulo Piit, te. 19... . so. scree Lindley and Hutton, 194 ........ Ad. Brongn.||, Lind. & Hut., 67, fig. 1 Ad. Brongn: | 0's s'sic ee his > Phall yi, Ge AT bes tetra aw (a ie PLR, Bs gitic win wie eetooiie'¢ Ad. Brongn., Lind. and Hut., 131 .. Ad. Brongn., Lindley and Hutton, 64 Lindley and Hutton, 44 .......... Ad. Brongn., Lindley and Hutton, 63 Ad. Brongn., Lind. and Hut., 62,176, B Lindley and Hutton, 92 .......... a IRE AR et ET aa Als cpt Murray, Lindley and Hutton, 157 .. Phil. 5, fg. 105.5. -- Me leteictetek = ters Williamson, Lindley and Hutton, 169 Great oolite. Low. sands. and coal. L.S.&C. Greatoolite, Low. sands. and coal. Great oolite. L.S. & C. Great oolite. Low. sands. and coal. L.S. & C. Great oolite. Great oolite. L.S. &C. Great oolite. Great oolite. L. S. & C. Great oolite. Great oolite. Low. sands. and coal. Great oolite. — Phill. 8, fig. 16..... we ccceesccees | —<——— Lindley and Hutton, 106.......... Lindley and Hutton, 179........ “15 Murray, Lindley and Hutton, 158 .. Ad. Brongn., Lindley and Hutton, 160 Lindley and Hutton, 119.......... Lindley and Hutton, 120.......... Ad. Brongn., Lindley & Hutton, 134 Ad. Brongn., Lindley & Hutton, 126 Young and Bird§], Lind. and Hut., 61 Ad. Brongn., Lindley and Hutton, 93 Lindley and Hutton, 69 ...... cees Lindley and Hutton, 105.......... Lindley and Hutton, 68 .......... ——$___ —$ L. S. & C. Great oolite. Great oolite. L.S. & C. Great oolite. Low. sands. and coal. L.S. & C. Great oolite. Low. sands. and coal. L.S. & C. Great oolite. Great oolite. * Where more than one reference is given, the first applies to the author who named the fossil. + Flora der Vorwelt, 1820-1826. + Geology of Yorkshire, Part I., 1829. § Fossil Flora of Great Britain, 1831-1837. || Prodrome d’une Hist. des Végét. Foss., 1828; and Hist. des Végét. Foss. ¥ Geological Survey, Yorkshire Coast, 1828. Fossil Remains on the Yorkshire Coast. GENUS AND SPECIES. Otopteris acuminata ......++ Beaninitee:... oo | Phill. 5, fig. 26 ..ccesvwsrscccens - Mytilus sublevis ........4. Sow. 439, fig. 3 occ cscccesvvnee Pinoa‘folium sacrces «tesco 2's Y. & B. 16, fig. 7. Phill. 14, fig. 17 | Lower lias. ~/CUMERID Aue onc nes 25 020 LG; MARCI Pia nie oe m0 nd Great oolite. Perna quadrata ...... Bini sie BOW AOS ce nn awiec es sk PEN RAT DE ¢ compte: ts Gervillia AEUEA | 9 s2.5\2 moms a'eie Sow.010, fig. 5 ..cecsnses eneves Inoceramus dubius........4. BOW O4, MT, Sols bun bare ass bs, Alum shale. Avicula cygnipes .......... Y. & B. 9, fig. 3. Phill. 14, fig. 3 .. | Marlstone. ineequivalvis ........ Bow. 264, figs, 2:8 sect... ees Marlst. Alum shale. BOMMAEET) Fs. w/o sr 8 Sow. mas, fig olive xs puers Inferior oolite. ——— Braamburiensis...... Sow.p@bill..6, fig. GB) aisie sp as a's ve Inf. and Great ovlite. Plagiostoma leviusculum ....°| Sow.2382 “.nncecstscscedsesnee Marlstone. unterstmetum .. 22°) Phulll 7; He. 1b. Se esos 0 ois bes vs Great oolite. Pecten equivalvis .......... Sow.ihao, iam BM, pcs ve vs baw bese Marlstone. BMICSWES DS cio k ee soso Phill Day “Ge Se sists ve ee wack clare ——- abjectus ........ fie et SINS Oy Gee Sete het ole te eerie ie Inferior oolite. ——- virguliferus ........ Phill, 11, figs 200. .5.2s. 6... akon ——— lens....... Rie tete eae isles Sow.-205, figs, 298+ ven veos nak Great oolite. Plicatula spinosa...... Babee bat SOW SLO ss 0 cle als biea hive mas .... | Lower lias. Marlstone. Grypheedteeiieta saiencies cn ell, 14) fic, 7 6... anos « oases Lower lias. Fossil Remains on the Yorkshire Coast. 241 GENUS AND SPECIES. REFERENCE. FORMATION, Gryphza‘incurva .......+.. | Sow. Y. & B. 8, fig. 13.......... | Lower lias, _=-Wientochias «bees s*t SOW. O47, figs? ISO FT. 6 o'e's'e'e'e” | eee = Hullata ects bets PP SOWs COS" % cee cteccs's ce cee eee'e's se’ | Marlstone. toa Wana vec. crea dott i Sow. 383, fig. 3 ..... Mire avec ae Great oolite. Ostrea, species not determined. | ++ -seeceeeseeeeceeeeeeevencs Marlstone. Marshit occ e's« o'e's'ee’ Sow. 48 CR toe xa -» | Inf. and Great oolite. SOLGATIANs se c's acre toie lots Sow.468; fig) 2 200.2055 afecerenetels - | Inferior oolite. Orbicula reflexa........ +» | Sow. 506, fig. 1-........ miera utente - | Alum shale. Inf. oolite. Terebratula bidens.....%% es» | Phill: 13; fig. 2480... oc cee e’ Marlstone. Inf. oolite. — tetrahedra ..... wt *¥s Ge By 8, fig Wor vs vee ant acre Marlstone. - triplicata ........ Phill. 13, fig. 22 s.cecessccccces : Obsoleta™.. ..%es% Sow: S8sfigs 7 US. eee... sees” | Inferior oolite, trilineata ........ | Youngand Bird ......... Peace = "spinosa". ....+%. Swnith; PHM) 9, fig 18% s0.06.% 50% -| Great oolite. Lingula, Beant fe ae sass % "et Phill, 11,-fig. 24 ¢..5. eveeeceeeee | Inferior oolite. Mollusca. Auricula Sedgvici .......... Eee) El edhe Oo eelste oie eieiahe eeeeeeee | Inferior oolite. Melania Heddingtonensis .... | Sow. 39. Y. & Be VN, fer 8K. cs. - | Inf. and Great oolite, Nerita costata....ss.eee.- wee | Sow. 463, figs. 5,6 ...+eeeeeeee | Inferior oolite. Natica adducta ...... spire naier PEIN, LL Bs BO exe a ww o0)p ola. AR aa I Minia oeieds vivierere |) PEs, Dly shige 25! nia. 6 oie. wa. oboe | as Acteeon humeralis ........ oo | Ebill, 11, figs B4 ci cece ecensees | ————, glaber ....0«. Pies) | Hol. 9; fig. ot vecesecces | ———— Wermetusscompressus is co.cc | Elite, fs, 17 ac’ ctele « eters Phill, 95) fig: 27, ss .iicoe ee HOO. Belemnites compressus . Voltz (not De Blainville) ........ L. lias. Marls. Al. shale - elongatus........ Geol. Tr. 2nd ser., ii. 7, fig. 6 .... | Marlstone. =atlibUlanismmctrererercicls Y. & B. 15, fig. 6. Phill. 12, fig. 20 | Alum shale, — Ss SPECIES NOE NAMIEU «: ||| s/a/s'ele sv clnis.sle w'e'< 0ecees Teleosaurus Chapmanni...... REFERENCE. VOltz siiectee nie sin o's vaeevensees De Blainville, Sow. 590 ...cceveee Y. & B. 13, fig. 2. Phill. 12, fig. 16 Y. & B. 12, fig. 8... A. yaa Sow. 164: 5... nja/einin wenn areeree Sow. 73, caesenccda o ¢isiecececces Y. & B. 13, fig. 7. Phill. 14, fig. 6.. Sow. 19] {ge eels sips uyicies ee dese Y. & B. 14, fig. 6. Phill. 13, fig. 8.. Sow. 229 te. ae Ahaha ie fe reese Sow. 107, fig. 2. Y. & B. 12, fig. 3. Young and Bird, p. 253.....0..00: Sow. 94, uppendig. . vepeceecceses Y. & B. p. 266. Phill. 13, fig. 7.... Sow. 407, fig. 2icore cdesbeccccns DSOWe/ OO) cckis ans his w's's's 0 cishauraeiee Y. & B. 13, fig. 4. Phill. 13, fig. 10 OW LOD, ie spiceany g nivies ied alse 'n,% ‘ Sow. 94, lower fig, . 2+ oncceeeves Nobis suis. i + aicisplststateinis\die'ais: ' i ; "pil ae hoe i et! aE Nd sa a a LE : A ' Be Wh Val Vai es vy pate > x hs F pa oy a i ‘pata, vi , i a) ea) es: «tanh i sd bd oe itt ea Foard al \ vin cut ‘ i pow bea e fuc25929 XXI.—Noitices and Extracts from the Minute-Book of the Geological Society. 1.—Observations on the Cliffs in the neighbourhood of Harwich, made in De- cember 1832. By James Mitchell, LL.D., F.G.S. [Read May 15th, 1833.] HARWICH is situated upon a peninsula, which is defended from the ac- tion of the sea by a promontory on the north-east ; and on the east and south- east it is partially protected by walls and lines of posts or groins. About 300 yards to the south of the light-house begins a cliff consisting of London clay. Where it first appears it is low, but as it projects towards the sea it rises in the course of 300 yards to 35 feet ; but for the next 300 yards it re- cedes from the sea, and declines to the height of 15 or 20 feet. From that spot it again rises to 30 feet, and extends for nearly three quarters of a mile, when it sinks to a level with the shore. At the point where the cliff is highest, is a small remnant of a battery, which, about twenty years ago, was 30 yards from the edge of the cliff. A whole farm on this part of the coast is said to have been swept away ; and within the last twenty-five years a piece of land, called the Vicar’s Field, has been totally removed. At the highest part the cliff presents the following section : Vegetable soil. Chalk flints, rolled pebbles, and clay ; the two first predominating 1 ft. Red clay, in beds, from six inches to four feet thick, and separated by seams of whitish or greenish clay, not calcareous ; about . 20 Blue “ cement marl,” or indurated clay, two beds separated ee) a bed of clay ; about : : 2 Cement stone, consisting of flattened spheroids Staal dives ae in diameter. : . 10in. Blue clay, divided into re Beds bya whitien trea: alioule : by go 2 These measurements were taken by the eye, but the height being small, it is presumed that they are tolerably correct. The lines of stratification are parallel; but, at the point where the section was taken, they are not horizontal, having a gentle anticlinal dip. A second bed of cement stone is visible on the shore at low water, and about 2L2 260 Notices and Extracts from the Minutes of the Geological Society. 20 feet in perpendicular descent beneath the first bed*. It appears to be of greater magnitude, as some of the masses are so large that nota crack appears over a surface of 30 feet. On the top of the cliffs, about 20 years ago, was a patch of crag, which has been entirely destroyed. In the southern prolongation of the cliff, in that part which extends about three quarters of a mile, the clay is divided by only four whitish streaks, and is nearly the same from top to bottom. The thickness of the formation in Harwich is inconsiderable, the chalk having been found at the depth of only 60 feet from the surface ; and though there is a great accumulation of alluvial matter on the peninsula on which the town stands. Iron pyrites occur abundantly, and lignite is found, but not in considerable quantities. Fossils are principally procured from the cement-stone, the most common being a Venus. Nautili are sometimes found, and Mytili with the nacre ; also a species of Patella. The cement-stone, when it first falls from the cliff, is rather soft, but after exposure for some time it becomes very hard. Being of a black colour it is usually mixed with cement made from the Whitstable stone, and is less valu- able than the Sheppey. The greater darkness of the colour is attributed to the greater quantity of manganese. The cliff at Felixstowe, about three miles north of Languard Fort, consists of blue London clay, similar to that at the foot of the Harwich cliff ; and on the top is a stratum of crag from 10 to 15 feet thick, the London clay being about 35 feet. No cement stone is seen in the cliff, but at low water, two beds may be found at the same perpendicular distance from each other as at Har- wich. 2.—Notices of the Red Marl and Lias of Worcestershire ; of a Fault by which they are affected; and of fossil freshwater Shells at Shotover Hill. By Hugh Edwin Strickland, Esq., F.G.S. [Read December 4th, 1833.] TueEsE notices were accompanied by a manuscript map, on which are laid down, with greater accuracy than had before been attempted, the boun- daries of the red marl and lias in the districts adjacent to Pershore, Evesham, * This measurement was ascertained during the sinking of a well in the fort, on the hill at the south side of the town. i ae i ee ee Notices and Extracts from the Minutes of the Geological Society. 261 Bitford, Alcester, Droitwich, and Worcester. Mr. Strickland points out, also for the first time, a line of fault ranging from a little north of Bredon Hill, in Gloucestershire, to Inkberrow, north of the road from Alcester to Worcester. By this fault the relative position of the red marl and the lias has been affected, the former constituting a valley of elevation, bounded on each side by the latter. Mention is also made of bones and teeth of the hippopotamus, anid of a deer having been found in the gravel near Cropthorne, between Evesham and Pershore. Mr. Strickland likewise alludes to the occurrence, on Shotover Hill, near Oxford, of fossils which he believes to belong to the freshwater genus Paludina; but the specimens which he procured are imperfect casts. These shells, he adds, were first discovered by the Rev. H. Jelly of Bath, in a sand-pit on the brow of the hill, much higher than the pit in which the Portland strata occur. 3.—Notice of the Analysis of a Mineral Water from the Island of St. Paul, in lat. 38° 45' S., and long. 77° 53' EK. By John Bostock, M.D., F.G.S. [Read January 7th, 1835. ] Tue Island of St. Paul is stated, on the authority of Capt. Ford, who pro- cured the mineral water, to be of volcanic origin, very rugged in its outline, the highest part being about 700 feet above the level of the sea, and to have the form of abowl 10 or 12 miles in circumference, into which thesea flows through a narrow opening capable of admitting a boat. The surface of the island is, in many places, covered with pumice ; and at night flames issued from various crevices in the rocks. With the exception of the island of Amsterdam, about 40 miles to the north, St. Paul’s is at a great distance from any land. In the hole from which the water was taken the thermometer stood at 212°; and there were numerous other springs, all of which were by the edge of the sea. Dr. Bostock then explains the manner in which he conducted the analysis; and afterwards compares the results with those obtained by Dr. Marcet from water procured in the middle of the South Atlantic; and infers from the great difference in the mineral contents, that the water of the Island of St. Paul is not merely the water of the neighbouring ocean in a state of dilution or aliered simply by mechanical filtration. 262 Notices and Extracts from the Minutes of the Geological Society. Comparative analysis of the water from the middle of the South Atlantic and of that from the Island of St. Paul, lat. 38° 45' S., long. 77° 53' K. Residuum obtained from 100 grains of the Residuum from 100 grains of the water of St. water from the South Atlantic. Paul. Muriate of soda .........-- 2°666 grs. Muriate'@f sGflassstesicws.cs cscs 2°303 grs: Sulphate of soda.......... "466 Sulphate of soda ...........- 053 Muriate of lime........... 195 Muriateof lime. .).3/.0 5. 05. 340 Muriate of magnesia....... 991 Muriate of magnesia.......... 059 L088... OR ise cideeenatan hae 038 4°118 2°790 4.—Notice of Fossils found in the Bognor Rocks. By Woodbine Parish, jun., Esq., Sec.G.S. [Read January 7th, 1835.] Tue author, Woodbine Parish, Esq.,inaletter addressed toG. B.Greenough, Ksq., President of the Society, states that in consequence of the destruction for the purposes of building, of such parts of the Bognor rocks, as are accessible, specimens of Nautilus, formerly abundant, are becoming rare. Toge- ther with his communication he forwards a collection and a list of the Bognor fossils. The author also notices that about a mile to the east of Bognor, and in front of the village of Felpham, chalk is exposed for a considerable distance cropping out of the sands between high and low water mark ; and at low water it may be traced for upwards of a mile in the direction of Middleton. It abounds, he states, in its characteristic fossils, of some of which he gives a list. Where the chalk first appears, it is almost as hard as stone, and is thickly interspersed with flints; further on it becomes soft, and the flints are not so numerous. Chalk marl has long been dug out of the beach near Middleton, at low tides, for manuring the neighbouring beds. List of Bognor Fossils in the possession of the Geological Society, including those presented by Mr. Parish. Teredina personata. Modiola elegans. Solen affinis. Pinna affinis. Pholadomya. Exogyra. Panopza intermedia. Ostrea Bellovacina. Venericardia Brongniartii (?). Lingula tenuis. Astarte rugata (?) Anomia lineata. Cytherea incrassata. (?). Dentalium planum. Pectunculus brevirostris. Vermetus Bognoriensis. — decussatus. Ampullaria (?) sigaretina. Notices and Extracts : Jrom the Minutes of the Geological Society. 263 Solarium. Cassidaria striata. Pyrula Smithii. —— carinata. Fusus rugosus. (?) Voluta luctator. Rostellaria Sowerbii. Nautilus Imperialis. es 5.—Extract from a Letter addressed by Dr. Daubeny to the Curator, on a Saline Spring near Oxford. [Read June 10, 1835.] “Dr. Bucktanp having announced to the Society (April 29, 1837,) the existence of the salt spring lately discovered near Oxford, an analysis of the water may perhaps interest the Society, as it contained, when I made my ex- periments, more sulphuric salts than any other spring in this country, and like- wise a certain proportion of iodine. The saline contents in a pint were as follows :— Chloride of sodium. ; 3 5 : ig -FORSS calcium. : ‘ : : i725 magnesium ] , ; ‘ ig 4240 Sulphate of soda ; zen 2°40 132°87 Also a proportion of hydriodic acid, yielding of iodine, in the pint, about zi; of agrain. The date of this examination was March 26th (1837), at which time the borings had reached to 280 feet below tie surface. Some days later the water was not so strongly charged with sulphuric salts, though _ the quantity was considerable.” 6.—Notice of a Letter addressed to Capt. Belcher, R.N., F.G.S., by H. Cuming, Esq., dated March 5th, 1835, on the Earthquake in Chili, November 19th, 1822. [Read December 2nd, 1835.] Tue writer arrived at Valparaiso in January 1822, and resided there con- stantly until 1827, and from the latter period, with occasional absences, till May 1831. At the time of the earthquake, he lived in the Plaza Mayor, near the landing place at the arsenal, and his house was destroyed by the first shocks. He did not go to the beach during the night, but was informed that the sea had retired a considerable distance, and had immediately returned with great force. On the morning of the 20th he noticed the effects, but found nothing more than a high tide. At the time of the convulsion it was dead low water. He never heard of the rocks having been heaved up, or of the permanent retirement of the sea, until the publication of Mrs. Graham’s work 264 Notices and Extracts from the Minutes of the Geological Society. on Chili, to the statements contained in which, neither he nor his friends could subscribe. Mr. Cuming’s pursuit of conchology and natural history generally, caused him to visit frequently the rocks and inlets with which the northern and southern parts of the bay abound; but though the rocks were covered with Fuci, Patelle, Chitons, Balani, &c., yet he never perceived the least difference in their appearance from the date of his arrival to his finally quitting Valpa- raiso. He mentions particularly, as points which he often examined, the Caleta, the Quebrada de Dios, and the Cruz de Reyes. He also never found the least trace of the above productions, except in situations covered by the tide. After the earthquake, Mr. Cuming resided in a house in the Arsenal, where the spring tides came un to the same mark as they did previously to that event. He refers especially to the tides of 1822 and 1823. Another circumstance which convinced Mr. Cuming that no change of level had taken place, was the existence of asmall detached rock opposite the Estanco, half-way between the Custom-house and the Market-place, and about fifty yards from the walls at half tide. From this rock he had often taken Concholepas Peruviana, previously to the earthquake, and subsequently it retained the same position. The vessels occupied the same anchorage as they did before November 1822; and nautical men affirmed that there was not the least difference in the depth of the water in any part of the bay. The opinion that a change had taken place in the relative level of land and sea, Mr. Cuming conceives, originated in the accumulation of detritus at points where the tide flowed anterior to the earthquake, and on which houses and even small streets have been since erected. ‘Though these accumulations ap- pear to have been forming between 50 and 80 years, yet they were small previously to the violent rains in June 1827, which brought down into the bay the loose granitic soil of the hills and the ravines. ‘This detritus has since been thrown up by the tides, and formed into a firm open space exceeding 250 feet in breadth, on which the buildings have been erected. In front of the Custom-house, however, the accumulations were trifling, and the landing place remained in the same state as in 1822. The quantity of matter thus carried into the bay has not affected the an- chorage, and Mr. Cuming, when dredging within two hundred yards of low- water mark, never founda grain of decomposed granite, or any kind of recent soil, but fine sandy mud, well stocked with several species of shells of mature growth. Notices and Extracts from the Minutes of the Geological Society. 265 Both to the northward and southward of Valparaiso, where the coast is open, namely, at Lagunilla, Vina del Mar, Con-Con, and Quintero, the sea has thrown up high banks of sand, many feet above the level of the land be- hind them, and reaching inland from 1000 to 2000 feet, and at Quintero to a much greater extent. At this place the sand contains beds of shells “ina semi-fossil state,” which are burnt by the natives for lime. Mr. Cuming visited these localities previously to the earthquake, and often subsequently, but never saw a shell beyond the range of high water, except those in the state above mentioned, and the owners of the land declared that no change had taken place. Mr. Cuming also states, that about 70 years since, he believes at the same time that Conception was visited by an earthquake, Valparaiso was also visited. The sea retired to a very great distance, and returned with so great violence that it destroyed all the houses, carrying the boats and canoes to the church of San Francisco, which is about a quarter of a mile, on a gradual ascent from where the tide usually flows. VOL. V.—SECOND SERIES. Qn rest sdus fo W090. ge, EXPLANATION OF THE PLATES AND WOOD-CUTS. PLATES I. & II. lilustrate Mr. Weaver’s paper on the Geological Relations of the South of Ireland : p. 1 to 68. Pratt I. Contains—(a.) View of the mountains on the south of the Blackwater river, extending (6.) No. No. from the Neagles mountains on the east to MacGillicuddy’s Reeks on the west. Taken from Drumskeha, about four miles south-west from Kanturk, and three miles north of the Blackwater. View of mountain and hilly ranges, from the Mullaghaneesh on the east to the Cahirconrée on the west. Taken from the southern brow of the coal country, about three miles north of the town of Castle Island. N.B. These two views (a. and b.) combined, extend through the principal mountain chain in the south of Ireland. Sections through the South of Ireland. . 1. Section from the sea at Loop Head, on the south-west, through the county of Clare to Lough Derg, on the east. . 2. Section from the sea at Castle Haven, through the counties of Cork and Kerry to the sea at Kerry Head, from south-east to north-west. . 3. Section from the river Maine (Section No. 2.), through the counties of Kerry and Limerick into Tipperary, from south-west to north-east. 4. Section from the sea at Courtmacsherry Bay, through the county of Cork to Broadford in the county of Limerick (Section No. 3.), from south-east to north. west, and from north-west to north. 5. Section from the sea at the entrance of Cork Harbour, through parts of Cork and Waterford to the county of Tipperary, from south-west to north-east. . 6. Section through the Dromagh Coal Field, from south to north. N.B. In the Sections Nos. | to 5, objects are, in some cases, projected on the line of section, though they do not stand immediately in the line. EXPLANATION OF THE PLATES AND WOOD.CUTS. Pratt II. Contains a Geological Map of the South of Ireland ; Also a Geological Map of all Ireland. WOOD-CUTS ILLUSTRATIVE OF MR. WEAVER’S PAPER. Plan and Section of Muckruss Copper Mine : p. 29. Plan and Section of Ross Island Copper Mine, with the embankment against the Lake of Killarney : p. 30. Diagram illustrative of the relative position of the properties in the coal district south, west of Kanturk : p. 51. Plan and Sections of the Annagh Lead Mine, near Castlemaine : p. 64. N.B. I take this opportunity of noticing, that in the 5th Vol., First Series, of the Geological Transactions, and Plate VII., View No. 4, of my Me- moir on the East of Ireland, the words “ Keeper mountain” are engraved in a wrong position. They should have been placed over the round topped mountain, which is situated immediately west of the western *¢ Bilboa mountains.” PLATE III. Map illustrative of Mr. Bryce’s Memoir on the north-eastern part of the county of Antrim: p. 69 to 81. PLATE IV. Lithographic Drawing of the Squaloraia, described in Dr. Riley’s Memoir: p- 83 to 88. Figs. 1. 2. 3. Magnified representations of a scale. (This plate has been copied, by permission of M. Agassiz, from Table 42, Recherches sur les Poissons Fossiles.) PLATE V. Illustrates Capt. Bayfield’s paper on the Geology of the North Coast of the St. Law- rence: p. 89 to 102. Fig. 1. Sketch of the River and Gulf of St. Lawrence : p. 89. Fig. 2. Natural columns of limestone on the east side of Niapisca Island, one of the Mingan Islands: p. 93. This drawing was made by Mr. Bowen, R.N., not with reference to geo- logical phenomena, but on account of the picturesque beauty of the columns. EXPLANATION OF THE PLATES AND WOOD.-CUTS. PLATE VI. Map and contours of ground illustrative of Lieut. Nelson’s Memoir on the Geology of the Bermudas: p. 103 to 123. Fig. 1. General Map of the group, the outline of the reef having been sketched from the usual authorities. Fig. 2. illustrates contours of ground taken at points without any special selection : the difference of level is indicated by different intensity of tints: pp. 109 & 117. WOOD-CUTS ILLUSTRATIVE OF LIEUT. NELSON’S PAPER. Fig. 1.& 2. Sections at the summit of Retreat Hill, St. George’s Island. The waved lines mark the disposition of the layers of sand: p. 106. Fig. 3. & 4. General sketches of the cliffs along the south side of Bermuda, or the Main Island : p. 107. Fig. 5. Section across the east end of Ireland Island : p. 108. Fig. 6. Section at right angles toa. Fig. 5. The difference in the direction of the dip indicating the former existence of mantle or saddle-shaped strata: p. 108. Fig. 7. Caverns covered by red earth: p. 108. Fig. 8. Cave once under the North Bastion, Ireland Island : p. 112. Fig. 9. Sections through a supposed fossil palmetto grove. The parts marked a are filled with hard compact stalagmite: p. 115. Fig. 10, c and d. Plan and section of the recent palmetto root : p. 115. Fig. 11, Plan ofa coral reef forming around a sand-bank: p. 116. Fig. 12. Section of a small isolated coral reef: p. 116. Fig. 13. Plan and section of a serpuline reef near Elbow Bay, south side of Bermuda : pe E17. Fig. 14. Section near the Magazine Pond, Ireland Island, illustrative of one of the first steps in the formation of caverns: p. 118, Fig. 15. Sand caves: p. 119. Fig. 16. Pinnacles near Tobacco Bay, St. George’s Island: p. 120. PLATE VII. Map and Sections illustrative of Mr. Romley Wright’s paper on the Brown Clee Hill : p. 125 and 126. PLATES VIII. & IX. Fossils from the well sunk at Hampstead, and described in Mr. Wetherell’s paper : p. 131 to 136. EXPLANATION OF THE PLATES AND WOOD.CUTS. Priate VIII. p. 136. Fig. 1. Desmophyllum. Fig. 11. Nucula Bowerbankii. Fig. 2. Pennatula. Fig. 12. Wetherellii. Fig. 5. Pentacrinus subbasaltiformis. Fig. 13. striata, var. Fig. 4. — Sowerbii. Fig. 1A. compressa. Fig. 5. Pollicipes (?). Fig. 15. Avicula arcuata. Fig. 6, Tellina splendens. Fig. 16. papyracea. Fig. 7. Lucina Goodhalli. Fig. 17. Dentalium anceps. Fig. 8. Venus tenuistriata. Fig. 18. Scalaria undosa, var. Fig. 9. Arca nitens. Fig. 19. Oyulum retusum. Fig. 10. —- impolita. Priate IX. p. 136. Fig. 1. Cytherina barbata. Fig. 12. Marginulina. Fig. 2. Pollicipes (?). Figs. 13. 14. 15. 16. 17. 18. Rotalia. Figs. 3.4. 5. 6.7. Nodosaria. Fig. 19. Cristellaria. Figs. 8. 9. Articulina. Fig. 20. Miliola. Fig. 10. Articulina ? Fig. 21. Cellepora. Fig. 11. Frondicularia ? Fig. 22. Flustra ? PLATE X. Map and Sections illustrative of Mr. Prestwich’s paper on the neighbourhood of Gamrie: p. 139. The Map extends along the coast from White Hills to Trouphead. The dotted portion represents gravel and other superficial detritus. Sections—No. 1. Is the coast section from Blackpots to Banff. The horizontal scale of this and the other sections is four times that of the Map. No. 2. Cliff of Gamrie Bay: pp. 140. 145. No. 3. From Gamrie to near Afforsk : p. 145. No. 4. Section of the superficial detritus at Castle Hill, near Gamrie: p. 146. WOOD-CUT. Section of the strata containing Ichthyolites at the ravine near Mr. Dockar’s house, Finden: p. 142. PLATE XI. Map and Sections explanatory of Archdeacon Verschoyle’s paper on the north coast of Mayo and Sligo: p. 149 to 170. EXPLANATION OF THE PLATES AND WOOD.-CUTS. WOOD-CUTS ILLUSTRATIVE OF THE PAPER. No. 1. Shifted quartz veins in a perpendicular cliff at Mycreeny, between Blind Harbour and Erris Head: p. 158. No. 2. Diagram explanatory of No.1. The portion folded back is intended to re- present the surface, at the top of the cliff; and the other part of the diagram the . . cliffas represented in No. 1. In using the diagram, the portion folded back should be held at right angles to the other: p. 159. No. 3. Strata of mica slate bent over projecting masses of trap at Attatovick Point : p. 162. No. 4. Contorted strata of shale and grit, north of Poolaclogher : p. 165. No. 5. Trap dyke in carboniferous limestone east of Killala Bay : p. 167. PLATE XII. Illustrates Mr. Broderip’s memoir on some fossil Crustacea and Radiata found at Lyme Regis: p. 171 to 174. ' Figs. 1. 2. Coleia antiqua: p. 172. Fig. 1. represents a young individual in the col- lection of the Geological Society. Fig. 2. a. Peduncle of mesial antenne. b. Internal sete. c. External sete. d. Lamelliform appendage of the peduncle of the external antenne. e. Base of the terminal sete of the external antenne. Fig.1. f. f: Eyes. Fig.1.2. g.g. Thorax. Feet. First pair or chelw, which have been displaced in both specimens, and pushed for- ward in the smaller one. Fig. 2. h. Humerus. z, Cubitus. k. Carpus. 7. Manus. m. Digitus. n. Pollex. Fig. 1. 0.0. Indications of the other feet, shown by the partial removal of the thorax. p. Post abdominal segments. q-q- Caudal natatory lamelle. Figs. 3.4. Remains of a macrourous Decapod, allied to the Salicoques of Latreille : p- 173. a.a. Point to the impressions of the branchia, exposed by the removal of the lateral portions of the thorax. b.b. Terminal spines of the post abdominal segments. Fig. 5. Ophiura Egertoni from the collection of Mrs. Murchison. The figure repre- EXPLANATION OF THE PLATES AND WOOD.CUTS. sents the inferior or ventral aspect of the animal; in consequence of weathering, the external surface is gone, leaving an internal view of the disk and arms: p. 174. Fig. 6. Represents the external surface of the dorsal aspect of an arm of the same species, found by Lord Cole, and in his possession. lig. 6*. Three magnified segments of the same. N.B. The arms in the specimen, figure 5, are truncated, but there is no doubt that in this, as well as in the other species, the arms were continued to a great length, till they terminated in a very fine point. PLATE XIII. Description of the Plate accompanying Mr. Mantell’s memoir on the Fossil Bones of Birds, discovered in the Strata of Tilgate Forest : p. 175. Fig. 1. a. The anterior; and fig. 1. b. the posterior aspect of the lower extremity of a left tarso-metatarsal bone of a bird. At o is seen the elliptical rough sur- face denoting the place of attachment for the posterior or opposable toe ; and it is situated at such a distance above the other toes as to prove that the bone belonged to a wader, and not to an insessorial or a raptorial species. The dotted outline represents a restoration of the inferior extremity of the bone, which is wanting in the fossil; probably, as Mr. Owen has suggested, from the bird having been young, and the epiphysis not anchylosed. x Fig. 1. 5. Marks the longitudinal ridges for the attachment of the aponeurotic thecz, which tie down the tendons as they glide along the metatarsus to the toes. Tig. 2. Posterior view of the left tarso-metatarsal bone of a heron (Ardea cinerea) for comparison with the fossil : o marks the place of attachment of the opposable toe. Fig. 8. The proximal extremity of a bone which was found with fig. 1. in the same block of sandstone, and is so similar to the latter, both in colour, surface, and sub- stance as to appear like the other extremity of the same bone. Mr. Owen con- siders it to be the proximal end of a tibia of a bird. Fig.4. The distal extremity of a tarso-metatarsal bone, and the bones of the toes of a heron, to illustrate the nature of the fossil specimens. Fig. 5. a. A fragment of a bird’s bone imbedded in sandstone, showing a longitudinal groove. Fig. 5. b. represents a section of one extremity. Fig. 6. The tarso-metatarsal bone of a bird imbedded in Tilgate grit. This specimen was carefully examined by Baron Cuvier, who confirmed the opinion of the author of its belonging to some species of Gralla. WOOD-CUTS Explanatory of Mr. Griffith’s memoir on Syenite Veins in Mica Slate and Chalk, at Goodland Cliff and Torr Eskert, county of Antrim: p. 179 to 185. No. 1. Section exhibiting the geological structure of the country from Fair Head to East Torr: p. 179. Nos. 2.3. Syenite veins passing through mica slate in Goodland cliff, south of Murlough ; | EXPLANATION OF THE PLATES AND WOOD.CUTS. Bay. In No. 3. a third vein is represented, interposed between the two principal veins: p. 180. Nos. 4. 5. Connexion of chalk and syenite at Torr Eskert: pp. 183, 184. PLATE XIV. Illustrates Sir Philip Grey Egerton’s memoir on certain peculiarities in the cervical vertebra of the Ichthyosaurus: p. 187 to 193. [All the figures are of the natural size except 9 and 10, which are reduced to one half.) Fig. 1. Atlas of an Ichthyosaurus. a. Occipital socket. b. Articulating surface for the first subvertebral bone. Fig. 2. Side view of fig. 1. A. The atlas. B. The axis. a. Surface for the insertion of ligaments. b.c. f:g. Planes for the articulation of the subvertebral bones. d, Articulation of the first rib. Fig. 3. Atlas and axis disunited. a. Articulating surface for the first subvertebral bone. b. Second subvertebral bone in situ. c. Articulation for the first rib. Fig. 4. Upper view of the first subvertebral bone. a. Surface articulating with the atlas. b, b. Anterior ale. c. Socket embracing the lower circumference of the occipital tubercle. d. Plane abutting against the second subvertebral bone. Fig. 5. Under view of fig. 4. a. Central boss of bone. Fig. 6. Lateral view of fig. 5. Fig. 7. View of the cervical portion of an Ichthyosaurus. a. Basilar element of the occipital bone. b.c.d.e. f. Cervical vertebra. g.h.i. Three subvertebral bones. k,l. Sockets for the first and second subvertebral bones. Fig. 8. Three subvertebral bones seen from below. Figs. 9.10. Cervical vertebra of a large Ichthyosaurus, reduced half. a.a. Intervertebral cavity. b.b.,c.c., Alternate elevations and depressions of the articulating surfaces of the bones fitting into each other. Fig. 11. Third cervical vertebra of a small Ichthyosaurus. a. Articulation for the third subvertebral bone. Fig. 12. Atlas and axis of Ichthyosaurus tenuirostris from Street, in Somersetshire. a. Articulation for the first subvertebral bone. b. Second subvertebral bone in sztu. c. Sharp edge of the axis, showing the non-existence of the third subyertebral bone in this species. EXPLANATION OF THE PLATES AND WOOD.-CUTS. PLATE XV. Map and Sections illustrative of Mr. Maclauchlan’s memoir on the Forest of Deane. The scale is the same as that of the Ordnance Map: pp. 195 to 206. WOOD-CUTS. Diagram to explain the contortion in the Coal Measures near Lidbrook Valley : p. 201. Diagram of part of the great fault between Lydney and Denbigh Lodge : p. 205. PLATES XVI. & XVII. Illustrate Mr. Stokes’ memoir on a piece of Wood, partly petrified by carbonate of lime ; with some remarks on Fossil Woods: p. 207 to 214. In Pl. XVI. Fig. 3. and Pl. XVII. Fig. 1. the dotted lines indicate the portions pre- sented in the magnified figures, Pl. XVI. Fig. 4. and Pl. XXII. Fig. 2. WOOD-CUT. Partially petrified Wood from the Vale of the Aire, near Ferrybridge, Yorkshire : p- 211. WOOD-CUT. To illustrate Mr. Hunton’s remarks on the distribution of Fossil Testacea in the Up- per Lias and Marlstone of Yorkshire: pp. 215, 221. PLATE XVIII. Fossils of the Faxoe Chalk : noticed in Mr. Lyell’s Memoir on Seeland and Méen: p- 243 to 257. Fig. 1. 2. 3. Cyprea bullaria (Cyprecites bullaria Schlotheim) from a drawing supplied by Dr. Beck: p. 250, note. Figs.4.5.6.& 7. Nautilus Danicus, (Schlotheim.) Figs. 4. & 5. From drawings supplied by Dr. Beck. Figs. 6. & 7. From a specimen in the Geological Society’s Museum : p- 250, note. WOOD-CUTS. Fig. 1. Valve of a Venericardia resembling V. senilis of the Crag: p. 245. Fig. 2. Section in the Cliffnear the church of Hoierup, Stevensklint: p. 247. Fig. 3. Cliff between Hoierup and the lighthouse, Stevensklint : p. 248. Fig. 4. Caryophyllia Faxoensis (Beck) : p. 249. Fig. 5. Coral allied to Isis, from the limestone of Faxoe : p. 249. Fig. 6. Section from Stevensklint to Faxoe: p. 251. Fig.'7. Section of a chalk cliff near a rock called Taleren, Moen : p. 254. Fig. 8. View from the sea beach of the ravine at Sommerspiret : p. 254. Fig. 9. Side view of part of the northern precipice in the same ravine, exhibiting a great mass of sand let into the chalk, and a huge fragment of chalk again included in the sand: p. 255. Fig. 10. Section of a promontory between Taleren and Sommerspiret, in which a mass of blue clay intersects the chalk: p. 255. Fig. 11. View of the Cliff called Dronningestolen, Island of Méen: p. 256. P q > TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. SECOND SERTES. VOLUME V. PART THE SECOND. Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque iis uti, sed ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. Novum Organum, Prefatio. LONDON: PRINTED BY R. AND J. E. TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1840. OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY OF LONDON. 1839. PRESIDENT. Rev. WILILAM BUCKLAND, D.D., Professor of Geology and Mineralogy in the University of Oxford. VICE-PRESIDENTS. GEORGE BELLAS GREENOUGH, Esq. F.R.S. F.L.S. LEONARD HORNER, Esq. F.R.S. L. & E. CHARLES LYELL, Jun., Esq. M.A. F.R.S. & F.L.S. Rev. ADAM SEDGWICK, M.A., F.R.S. F.L.S., Woodwardian Professor in the University of Cambridge. SECRETARIES. CHARLES DARWIN, Esq. B.A. F.R.S. WILLIAM JOHN HAMILTON, Esq. FOREIGN SECRETARY. HENRY THOMAS DE LA BECHE, Esq. F.R.S. F.L.S. TREASURER. JOHN TAYLOR, Esq. F.R.S. COUNCIL. CHARLES GILES BRIDLE DAUBENY, M.D. F.R.S. & F.L.S., Regius Professor of Botany, and Aldrich’s Professor of Chemistry in the University of Oxford. Sir PHILIP DE MALPAS GREY EGERTON, Bart. M.P. F.R.S. WILLIAM HENRY FITTON, M.D. F.R.S. & F.LS. ‘ ROBERT EDMUND GRANT, M.D. F.R.S. L. & E. & F.L.S., Professor of Comparative Ana- tomy and Zoology, University College, London. WILLIAM HOPKINS, Esq. M.A. F.R.S. ROBERT HUTTON, Esq. M.P. M.R.I.A. Sir CHARLES LEMON, Bart., M.P. F.R.S. WILLIAM HALLOWS MILLER, Esq. M.A. F.R.S., Professor of Chemistry in the University of Cambridge. RODERICK IMPEY F.R.S. & F.L.S. RICHARD OWEN, Esq. F.R.S. & F.L.S., Hun- terian Professor of Anatomy in the College of Surgeons. Sir WOODBINE PARISH, K.C.H. F.R.S. and F.S.A. GEORGE RENNIE, Esq. F.R.S. Rey. WILLIAM WHEWELL, B.D., F.R.S., Professor of Casuistry in the University of Cam- MURCHISON, Esq. bridge. CURATOR ann LIBRARIAN. WILLIAM LONSDALE, Esq. ADVERTISEMENT. THE Editors of the Transactions of the Geological Society are directed to make it known to the Public, that the Authors alone are respon- sible for the facts and opinions, contained in their respective papers. It is requested that all letters and communications to the Secretaries, and presents to the Society, may be addressed to the Apartments of the Geoiogical Society, Somerset House, London. XXII. XXII. XXIV. XXV. XXVI. CONTENTS. PART II. On the Structure of the Sevalik Hills, and the Organic Remains found in them. By Proby T. Cautley, Esg., Capt. Bengal Ar- tillery, F.G.S. : - : : . ; . : 2 ape Description of a Raised Beach in Barnstaple or Bideford Bay, on the North-west Coast of Devonshire. By the Rev. Prof. Sedg- wick, V.P.R.S., F.G.S., §c., and Roderick Impey Murchison, Tigre S ERG St icwe rete 8 2) ie ey Oi) ay, Extract from a Letter, by the Rev. David Williams, F.G.S., on the Raised Beaches in Barnstaple or Bideford Bay. . 3 op: Memoir to illustrate a Geological Map of Cutch. By C. W. Grant, Esq., Capt. Bombay Engineers. . . . 5 5 ps On the Upper Formations of the New Red Sandstone System in Gloucestershire, Worcestershire, and Warwickshire; showing that the Red or Saliferous Marls, including a peculiar Zone of Sandstone, represent the ‘“‘ Keuper” or “ Marnes Irisées ;” with some account of the underlying Sandstone of Ombersley, Broms- grove, and Warwick, proving that it is the “ Bunter Sandstein” or “ Grés Bigarré” of Foreign Geologists. By R.1. Murchison, cus) lon) ~t 289 Esq., V.P.G.S., F.R.S., and H. E. Strickland, Esq., F.G.S.. p. 331 XXVII. A Description of various Fossil Remains of three distinct Saurian Animals, recently discovered in the Magnesian Conglomerate near Bristol. By Henry Riley, M.D., and Mr. Samuel Stutch- bury, 4.L.S8. Communicated by Charles Lyell, Esg., Pres. GS. p. 349 CONTENTS. XXVIII. Extracts from a Memoir on the Geological Structure and Pheno- mena of the County of Suffolk, and its Physical Relations with Norfolk and Essex. By the Rev. William Branwhite Clarke, M.A., F.G.S. . - p- soo XXIX. On the Geology of the Thracian Bosphorus. By Hugh Edwin Strickland, Esq., F.G.S. ; : : : : : - p. 385 XXX. On the Geology of the Neighbourhood of Smyrna. By Hugh Edwin Strickland, Esq., F.G.S. ; ‘ . : 4 : . p. 393 XXXI. On the Geology of the Island of Zante. By Hugh Edwin Strick- land, Esq., F.G.S. : : : : : . F . p. 403 XXXII. Letter from Mr. James de Carle Sowerby to the Secretary, on the Genus Crioceratites and on Scaphites Gigas. - : . =p. 409 The Third and concluding Part of the Volume being nearly ready, will be published in February, and will contain the following Memoirs :— Prestwicu on Coalbrook Dale ; Fox on Mineral Veins ; Caurney and Fatconer on the Astragalus of a Fossil Monkey ; Darwin on the Formation of Mould ; Owen on the Tail of the Ichthyosaurus, and on the Plesiosaurus Macrocephalus ; Matcotmson on India; Bett on Mazunderan ; Haminron on Asia Minor; Srrickianp on Sandstone Dykes ; Darwin on Earthquakes ; Sepewick and Murcuison on Devonshire; Stokes on Orthocerata; and Syxes on Cutch Fossils. List of Donations and Index. CORRIGENDA. Page 302, line 7, for Turbinella read Turbinellus. Page 348, line 4, for destructive read distinctive. ee cre” for Plate XXIV. read Plate XXIX. Page 354, line 7, XXII.—On the Structure of the Sevalik Hills, and the Organic Remains found in them. By PROBY T. CAUTLEY, Esgq., Capt. Bengal Artillery, F.G.S. [Read March 9, 1836.] THE mountains, a part of which I am about to describe, range (with the exception of the debouchures of rivers) almost uninterruptedly from the Sutluj, which separates the territory of the British Government from that of the Sikh chieftain, Runjeet Sing, to the Burhampootur river, and the district of Cooch Behar. Their general bearing, in the portion near the Sutluj*, is N.W. and S.K.; but in that approaching the Burhampootur, it is many points nearer direct east and west. They lie at the foot of the great Himalayan chain, with which they are in some parts connected by a succession of low mountains ; but in others, as in the districts under review, they are separated by valleys from three to ten miles in width, and called by the natives Deyra Dhoon, Kearda Dhoon, &c., or the Valley of Deyra, the Valley of Kearda, &c. The highest peaks do not far exceed 3000 feet, and the generality of the sum- mits vary from 2000 to 2500 above the level of the sea. It is necessary, however, to premise, that my observations have not extended further eastward than the Ganges; and that whatever I may record, in this paper, beyond that river, is given on the authority of others. Between the Ganges and Jumna rivers, this line of mountains is separated from the great chain of the Himalayas by the Dhoon, or valley of Deyra, the average width of which may be under ten miles. At the Ganges, or south- eastern extremity, a road passes between the chain and the river; and no dif- ficulty whatever is offered to the approach to the valley. At the opposite or Jumna extremity, on the contrary, the mountains are in many places scarped into the river; and the footpath used by the boat and raft people, is an irre- gular track, over ridge and through hollow, and impinges upon the river at # Plate XIX. Map. VOL. V.—SECOND SERIES. Qn 268 Capt. Cauttey on the Sevadlik Hills. those points only where the stream, in its meandering course, strikes the oppo- site side of the channel. The intermediate roads, or ghats, follow the rivers or hill-streams ; for in such an utter confusion of mountains, any other pas- sage is impossible. A few of these roads are passable for wheeled carriages, but the generality are bad footpaths. Between the Jumna and the Sutluj are two other valleys, the Kearda and the Pinjore, separated from each other by one of those complex masses of mountains which connect the lower with the upper Himalaya range. The hills are generally less precipitous in this neighbourhood ; and the higher points and ridges are separated by valleys, af- fording a drainage to the country, and displaying on each side high and beau- tiful sections of the stratification. ‘These valleys, or plateaux—for, with reference to the rivers running below them, they may be considered as such— vary in width, but extend along the whole course of the mountain-streams. As much confusion may be avoided, in the absence of a native name for the whole range of these mountains between the Sutluj and the Burhampootur, by establishing one, which may be considered legitimate, I wish to propose that of Sevalik*, formerly applied to the portion between the Ganges and the Jumna; a name which appears to me better than that of the “ Lower Hills” or the “ Sub-Himalayan,” terms, equally applicable to the subordinate ranges northwards of the Himalayas. These preliminary observations, with the appended sketch of the countryt, will make the reader acquainted with the field of our fossil discoveries ; and I proceed to the description of the geological features of the tract. The for- * In Smith’s Exotic Botany, vol. i. p. 9., is the description of the Rhododendron arboreum: he refers it “ to the mountainous tract called the Sewalic chain, which separates the plains of Hin- dostan, between 75° and 85° E, long. from the Himalaya mountains. I make the quotation for the value of the name, though the statement is evidently wrong; the rhododendron in question growing in the Himalayas themselves at a high elevation, and in company with oaks. The chain separating the plains of Hindostan from the Himalayas, which is the one now under review, is subject to a mean temperature perfectly inimical to oaks and the Rhododendron arboreum. The name is quoted also in Dow’s History, and in some traditional writings in the possession of the high priest or Mahant residing at Deyra. The derivation supplied by the high priest is as follows :— “ SEWALIK, a corruption of Shibwalla, a name given to the tract of mountains between the Jumna and the Ganges, from having been the residence of Ayshoor Shib, a name of Mahadeo and his son Gun, who, under the form of an elephant, had charge of the westerly portion, from the village of Doodhli to the Jumna; which portion is also called Gungujur (gwjur, elephant): the portion eastward from Doodhli, or between that village and Hurdwar, is called Deodhar, from its being the especial residence of Deota, or Ayshoor Shib. The whole tract, however, between the Jumna and the Ganges, is called Shibwalla, or the habitation of Shib.” + Plate XIX. Map. Capt. Cautxey on the Sevalik Hills. 269 mations composing the hills, consist of beds of boulders or shingle, either loosely mixed or agglutinated by clay and carbonate of lime; of sands of various degrees of consistency ; of marl or clay conglomerate* ; and of an in- finite variety of clays; the two latter being most extensively developed to the westward of the Jumna. The strata dip from 15 to 35 degrees, generally towards the north; and the breadth of the inclined beds is from six to eight miles. The succession of the strata is irregular, with the exception of the shingle in the more northern tracts, where it appears to overlay as well as to alternate with the sandstones ; whereas, although the debris is in considerable abun- dance in the water-courses, and on the flanks of the hills, I have never met with these shingle-beds south of the most northern half of the hills. A similar remark applies to the marl, but in a contrary direction, as it occurs only to the south. The want of the marl in the northern sections may be accounted for, by supposing it to have been either a local deposition or a general one, which is not exposed throughout its entire range. Although I consider the whole of this tract of mountain as composed of one formation, it may be of use to divide the portion between the Jumna and Ganges, from that westward of the former river, as it appears to me, that there is a marked difference (as before stated) in the shingle strata, as well as in the position and number of the clay beds ; although perhaps nothing further than would be exhibited on any extended line of country, formed of debris from different tracts of mountains. The causes which upheaved this district, apparently acted more energetically in the contracted surface eastward of the Jumna, than in that to the westward ; though, in the latter, the surface up- heaved is much more extended. I shall therefore divide these notes into two sections; the first consisting of the tract between the Jumna and Ganges; the second, that westward of the Jumna. To commence, therefore, with the range between the two rivers. HILLs BETWEEN THE JUMNA AND GANGES. Shingle and Sandstone.—The beds of shingle are of enormous thickness, and alternate with the sandstone. The former precisely resemble the shingle in the beds of the existing great rivers of the country, and consist of boulders * T call this stratum clay-conglomerate, the beds being composed of fragments of an indurated clay, cemented together by clay, sand, and carbonate of lime; the clay itself effervescing strongly with acids. The rock is, in general, exceedingly hard and tough, as is shown in those parts where it is in contact with the stream of the rivers, which appear to have had little power upon it. 2n2 270 Capt. Cautiey on the Sevalik Hills. of granite, gneiss, mica slate, quartz, hornblende schist, and traps ; and every other rock, through which these rivers hold their course. If the beds of the Jumna and Ganges were to be upheaved, in the same way as those of former rivers, the appearance of the strata would be exactly similar. The sandstone consists either of grains of pure quartz, with different proportions of mica, or of an admixture of the other ingredients so common in all river sands. The pre- sence of oxyd of iron causes a great variety in colour, from red to gray, whilst the induration of the rock appears to depend on the proportion of carbonate of lime. In the more easterly limit opposite Hurdwar,as well as other places, the stone is quarried for building; and in many localities where it is crystalline, it is highly valuable in architecture. On the Jumna are the remains of an ancient hunting palace, built by the emperor Shah Juhan at the end of the 17th century; and although now in utter ruin, amongst its fragments are capitals of columns, and scolloped arch work, &c. cut in this sandstone, which prove it to be well adapted for architectural purposes. It is easily worked, and the mixture of mica gives two splitting surfaces. On exposure to weather, however, it exfoliates and crumbles, as is conspicuously shown in some lintels, still in position at Badshahmuhul. The colours of the clays are endless ; and a light blue variety, which is found under the marl, as well as higher up in the series, where it contains fresh-water shells, is exceedingly pure. The strata of this blue clay are thin, but those of the other varieties are of all dimen- sions. Lignite—Carbonaceous matter occurs throughout the sandstones, either in detached fragments exhibiting vegetable origin, or in strata or seams com- posed of sandstone and lignite in equal proportions. Lignite is also found in the marl, but generally in the form of black dust ; leaving, on its removal, an indistinct, vegetable impression. In one instance, I also met with it in the shingle strata. It has never been found in sufficient abundance to excite an inquiry as to its adaptation for ceconomical purposes ; though it is common to the whole of this tract of mountains. Eastward of the Ganges it has been found, to the north of the Moradabad district ; and it agrees in every respect with that found elsewhere. It has also been met with at points still more easterly ; but the examination of that tract has been very slight. The most interesting point at which I have found lignite, is at the mouth of the Ka- lowala Pass, one of the entrances into the Deyra Dhoon, from the plains. A stratum or bed of yellow and red sand, about 18 inches thick, is there com- pletely charged with lignite, either in long flattened masses, or in trans- verse sections of trunks of trees, which show, by their elliptical form, effects Capt. Cautiey on the Sevalik Hills. 271 of vertical pressure. The lignite, in these cases, constitutes merely the outer covering ; the interior of the trunk being composed of the sandstone matrix. The bed is enveloped in strata of the marl, abounding in the remains of ani- mals; and both the lignite bed and the marl, appear at this point most dis- tinctly to have been deposited ina hollow ; the beds, at their lateral extremi- ties gradually attenuating, until they meet the sandstone rock ; and the lower surface being concave. Although the marl is evidently limited at this spot, it seems to exist so generally in extended strata, that, supposing it to have formed tracts of marsh land, those tracts must have been very extensive. I have be- fore remarked, that I have seen the marl only on the southern limits of these hills, between the Jumna and Ganges. In crossing the former river, how- ever, the same stratum, with the same organic remains, is met with on the north of the mountain ridge, on which the town of Nahun stands. Here the upheavement has been more violent than elsewhere ; and the point of junction of this tract with the higher Himalayas is consequently much dislocated. It is necessary to state, that there are appearances of trap* in the neighbourhood of these disturbances; a fact which may lead hereafter to an interesting geological disquisition on the point of junction. Fossil wood, apparently dico- tyledonous, abounds in the sandstone. The woody fibre is generally perfect, but impregnated with the sandstone, and frequently mixed with carbonaceous matter ; in which case the fossil is black, and on fracture has the appearance of an intimate mixture of coal and sand, or of an imperfect coal. The only remains of animals yet found are fragments of tortoises. Marl, with Organic Remains.—As the marl is in greatest abundance in this section, I will now give an account of its organic remains; confining myself to classes and genera. These fossils are in appearance perfect, and the deep black colour which they have derived from hydrate of iron, renders them ornamental. The medullary cavities are, in many cases, filled with pyrites, and in others with pure white crystallized carbonate of lime. The greater part of the fossils, already procured, is from the deposit in the Kalowala Pass ; and as my collection is not only large, but abundant in different genera, the number already found in such a limited space, indicates the great variety of animal remains, which a diligent and extensive search may produce. Teeth, and the more solid part of the bones, are found in the greatest quan- tity. Most of the former are perfect, and as sharp in their outline as when the animals existed ; and even in the fragments, the sharpness of the fracture * Dr. Falconer has made the same observation. Journ. Asiatic Soc. Bengal, vol. iv. p. 50; date of communication, 3rd Jan. 1835. 272 Capt. Cautiey on the Sevalik Hills. proves, that they were quietly deposited in the sediment in which they are found. The following is a list of the fossils already discovered in the marl :— MamMaLliA. Pachydermata - ~ Teeth, and the remains of a species of Anthracotherium. Carnivora - - - Genera doubtful; but some of the teeth correspond with the third incisor of the bear. Rodentia - - - Rat, and a small variety of castor. Ruminantia - - - Deer, several varieties, and one molar of a very small species. Solipeda - - - Horse, one incisor, and one molar from the right side of the upper jaw: they exhibit a peculiarity in the form of the enamel flexures. Reprizia. Crocodilia - - - Gharial. (Gavial of naturalists.) Teeth and bones in abundance. Crocodile. Teeth, in great abundance, fragments of the osseous plates, vertebrz, and other bones. Chelonia - - - - Emys. Fragments of the plates of the back very perfect; also ribs, with the attached osseous part of the buckler. Tryoniz. Ditto, ditto. Some marked differences in the form and position of the rugous surface of the fragments of the buckler, may hereafter point out a variety of species. Pisces. Vertebre and Scales—The latter doubtful. TESTACEA. Bwalve - - - - Imperfect, but resembling Unio. Univalve: a cast resembling that of the Paludina of the present fresh-water*. Besides these more easily determinable remains, there have been found a number of incisor teeth, which I cannot assign to any genus ; also quantities of bones, in fragments, and portions of ribs, one of which must have belonged to a large animal; also vertebra, metatarsal or carpal bones, &c. With the exception of the teeth, the remains are generally in fragments, and separated ; nor does it appear probable that we shall meet with anything approaching to a complete skeleton. In the tract then between the Jumna and Ganges, the fossil remains as yet discovered are thus disposed :— * The only univalve which has been yet found in the marl is the cast above-mentioned, from the rock north of Nahun. I have entered it here, considering, as I do, that the deposits are identical. Capt. Cauttry on the Sevdiik Hills. 273 Shingle, or Gravel Beds—Lignite, scarce. Sandstone - - - - Trunks of dicotyledonous trees in great abundance; lignite, and remains of reptiles. Marl - - - ~- - Remains of mammafers, reptiles, fishes, shells, and lignite. The mineral products are, carbonate of lime, the general cement of the whole formation, also in stalactites and stalagmites ; selenite, in small tabular crystals; and pyrites, but apparently in the neighbourhood of organic re- mains only. Soda abounds throughout the mountains, efflorescing on the shingle and sandstone rocks; and the presence of this alkali may explain the partial disintegration of the boulders of which the shingle is composed: for, I believe, I am right in asserting, that every variety of boulder, from granite to quartz and sandstones, has been acted on: and when it happens that the boulders can be removed entire from the bed, they fall to pieces, either after exposure to the air for a time, or by pressure of the hand imme- diately. With regard to fractures in some of the boulders, and their consoli- dation on different planes, as in a slip of stratification, no remark whatever appears requisite, as these are the necessary consequences of that movement, which raised the beds from their horizontal position. There does not appear to be any further remark necessary on this tract, more than can be reserved for the general summary ; I shall therefore proceed to describe the hills westward of the Jumna. Hitts WEstT oF THE JUMNA. These, as I before stated, consist of the same series of shingle, sand, clays, and marls; but they differ, in the beds of shingle being less abundant, al- though equally inclined, and in containing a different description of boulder. The rolled fragments eastward of the Jumna are all of primary or lower rocks, whilst those to the westward are confined to varieties of clay slate, and quartz. The marl, which, between the Jumna and Ganges shows itself in the southern limits, is here exposed at a point north of Nahun, cropping out on the northern slope of the mountain ; and the fossil remains resemble those found in the marl eastward of the Jumna, consisting of mammafers, crocodiles, tortoises, fishes, and shells. From Nahun to the plains there is a succession of sandstones and clays, without any abundance of shingle. The sandstone, which, in the vicinity of Nahun, is much indurated, and used for building, be- comes softer on approaching the plains; long before reaching which, the whole formation consists of an interminable succession of sandstones and clays, the latter being in the greatest abundance, of every variety of colour, and 274 Capt. Cauttey on the Sevalik Hills. dipping, on an average, 20° to the north. The topographical outline of these mountains, shows a considerable southing of upheavement, in the hills west- ward of the Jumna, as will be observed in the map*: and the circumstance of the fossil remains abounding in the sandstones and clays in this tract, and not in that between the Jumna and the Ganges, may probably be due to the non- upheavement of the line on its prolongation eastward of the Jumna. The drawings which accompany this paper} show that the action, in all proba- bility, was exerted irregularly ; and although in the large scale we may lay down the dip and direction with accuracy, the former as varying from 15° to 35°, and the latter from N.E. to S.W., local details give very different results. The sandstone rock, from which the fossil remains sent to the Society’s Museum were extracted, reposes at the above angle, over numberless beds of clays, more or less rich in testaceous remains. ‘The fossil bones lie in great abundance on the surface of the slopes in the neighbourhood of the sand- stone, amongst the ruins of fallen cliffs, in the beds of water-courses, &c. The bones which we have had the good fortune to dig out of the rock are perfectly sharp, and in all their original perfection. I may here advert to a circum- stance to which the preservation of the water-worn specimens is chiefly due. The sandstone is generally soft, but in the proximity of the fossils it becomes ferruginous, concretionary, and so hard as to turn the edge of the chisel ; and thus protects the fossil from destruction in its progress, as a boul- der along the torrent’s bed. These concretions are occasionally globular, and become singularly conspicuous, by the weathering of some of the ridges, when the mass of rock takes the appearance of huge spherical concretions piled confusedly on each other. The organic remains of this sandstone yet brought to light, belong to the following classes and genera: most of the species are new ; and the appearance of totally undescribed forms will add very considerably to our fossil genera. The new genera themselves will be the subject of separate accounts in their proper piace. MamMALIA. Pachydermata - Mastodon—elephant—rhinoceros—hippopotamus—hog. Carniwora - - Canine and feline. Ruminantia - - Elk—ox—deer in great varieties. Solipeda - - - Horse. * Plate XIX. t Ibid., fig. 1 to 4. Capt. Cautiey on the Sevdlik Hills. 275 Reprti.ia. Crocodilia - - Gharidl—crocodile; both very closely corresponding with the existing species now in the rivers. Lacertine remains indeterminable. Chelonia - ~ Emysand tryonix; some of the fragments are of the most gigantic pro- portions. Of the smaller varieties, nearly entire specimens have been found ; upper buckler and carapax complete. My cabinet also contains three heads, wanting only the occipital portion of the cranium. Pisces. Genera not established. Many other fragments have been found, but so imperfect as to render a classification impossible. I may remark, that there appears to be no end to the variety as well as quantity of these remains; and we may expect to do much, even in this remote region, in advancing the inquiries respect- ing fossil zoology. Of each genus above mentioned, with the exception of the horse and the carnivora, I have already almost perfect skulls. The bones of the body, how- ever, appear to have been much broken and mutilated; but it is a singular fact, that from many places where the fossils have been found as mere debris of fallen cliffs, fragments of bone have been obtained, which have admitted of being joined, although the fractured ends were coated with carbonate of lime, as if they had been fossilized separately. A beautiful example of this, is ex- hibited in an almost perfect rib of an elephant or mastodon, which is forwarded to the Society’s Museum, and which consisted of no less than eight pieces. A perfect humerus of a ruminant has been secured in this state; and the bones of two hind legs, namely, the upper part of the metatarsal connected to the lower portion of the tibia by the intermediate tarsal bones, with, also, the os calcis entire, and all the smaller bones of the tarsus equally so. These remains have belonged to an enormous animal, and, I believe, to the same genus as that of a skull in my possession, and now under description by my friend Dr. Hugh Falconer, of the Bengal medical service, and myself. Although I refrain from zoological details, I must mention, that we have an animal evidently forming a connecting link between the Pachydermata and Ru- minantia, or between the Tapir or Paleotherium, and the latter order of mammalia. The hippopotamus of this sandstone appears to be a new species, having six incisive teeth, besides other peculiarities, particularly in the pro- portion of the bones of the head: the tusks also differ from those described by Cuvier in his Ossemens Fossiles. The great depth at which the marl lies beneath the upper strata, with the discovery in it of remains of the horse, is an interesting fact. In the sandstone strata the remains of the horse are VOL. V.—SECOND SERIES. 20 276 Capt. Cauttey on the Sevalik Hills. by no means scarce. There appears, however, to be a local disposition in the deposits of these remains. In some places the hippopotamus, elephant, mas- todon, crocodile, tortoise, &c., are found in abundance, with the remains of ruminants; in others the hippopotamus and the water reptiles are almost totally absent, and only the remains of ruminants and carnivora occur ; all tending to prove that these animals were destroyed on the site of their habi- tats; and that this former world was not more mysterious than the present ; that there were vast tracts of marsh and river, with their attendant hippopo- tami and crocodiles in the waters, and elephants and mastodons in the neighbourhood ; and that there were other tracts free from water and marsh, and frequented by their natural inhabitants, ruminants, carnivora, &c. Dr. Falconer, ina note read at a meeting of the Asiatic Society of Calcutta*, suggested the identity of this deposit with that near Prome, some of the fos- sils from which have been so beautifully lithographed in the Society’s Trans- actions}. The mastodons in the Sevalik strata are in great abundance ; and as we have perfect skulls, we are enabled to form some opinion of the denti- tion and the change of teeth. Three of these skulls, now in my cabinet, have the front tooth worn, and the rear one coming into use; the whole line of teeth stretching on a surface of 19 inches, and forming an arc of 90°. The front tooth I cannot distinguish from that of the M. Latidens figured in the Geologicai Transactions ; and the rear one, in the same animal, bears such perfect resemblance to the M. Elephantoides, that I cannot help risking the conjecture that the M. Latidens and the M. Elephantoides are one and the same animal ; the specimens, from which the specific characters were taken, having been detached teeth. Bringing this forward in the way of suggestion may be of use, in ultimately leading to truth. The question, however, must be determined by a strict ex- amination of specimens; and having advanced the above supposition, I will take care that the means shall be provided f. * Journal Asiatic Society, vol. iv. p. 58; date of communication, 3rd January 1835. + Geological Transactions, 2nd Series, vol. iii. p. 377 et seq.; pl. 36 to 43. { The rear or newly-formed teeth of every species of mastodon resemble those of the elephant, so far as relates to the integrity of the apices or summits of their transverse ridges; and they might therefore be mistaken for those of the M. Elephantoides; but the observations which led to the conclusion, that the Ava specimens of mastodon belonged to two distinct species, were not made on detached teeth. A repeated examination of the jaws and teeth described by Mr. Clift, and the knowledge that his opinion was formed from considering the size and number of the transverse ridges in relation to the length and breadth of the teeth, have tended to confirm my belief in the establishment of two species, which I must retain until further and more definite evidence to the contrary is adduced.—REFEREE. Capt. Cautiey on the Sevalik Hills. Q77 The minerals in this tract, west of the Jumna, correspond with those to the eastward, with the exception of the presence of the gold, which occurs in the beds of the rivers in these mountains, both eastward of the Ganges, and westward of the Jumna; but I am not aware of its existence in the intermediate tract. Under Nahun, gold-washers are constantly employed during the dry months ; their daily return varying from two annas to two rupees, or from 3d. to 4s. The process is ex- tremely rude. A piece of board, a long wooden trough, a ladle made out of a gourd, a sieve of the large grass which grows so abundantly in this part of the country, and a piece of hollow bamboo with a little quicksilver, constitute the portable apparatus of these most primitive washers for the precious metal*. A great deal of the gold-dust must necessarily be lost'by this method of proceeding; and all the mercury, as it is evaporated in open air. The grains of gold are not larger than the small scales of mica, so common in river sand; and I have not heard that the metal has been found in large masses. This gold, too, has its localities, some streams being much richer than others. Where is the fountain head? In some stratum of this alluvium, per- haps, yet to be discovered, as the streams have no connexion with the higher mountains. A description of the washers, and the method practised by them eastward of the Ganges, have been given in the Journal of the Asiatic Society; and as there is little difference in the apparatus used at both places, it is not necessary to refer to it further. Some of the fossils obtained by Mr. Colebrooke in the hills near Cooch Behar, and described by Mr. Pentland+, are identical with some of those obtained by the present discovery; and as the former were found in the most eastern extremity of this line, it is possible that a careful examination would prove the existence of animal remains throughout the whole of the intermediate mountains; all the tract being probably tertiary. An inquiry into the difference between the hills bounded by the Ganges and Jumna, and those westward of the latter; and into the confused and interminable dislocations, without any flats in the former, and the more scattered ridges with the intermediate plateaux of the latter, would only lead to a disqui- sition on the general formation of the dhoons or valleys lying between the Sevalik hills and the great chain, which the limits of this communication will not admit, and must be left for future inquiry. It will be sufficient to state, that the general form of the mountains approaches more or less to a right angle, the long slope being covered with vegetation, and the crest terminating in a perpendicular and generally mural cliff, which descends into the beds of the torrents. ‘The scenery from these cliffs is most picturesque, and many of the passes or ghats up the torrents are bounded by gigantic walls of sandstone, varying both in height and character, and subject to all the tortuosities depend- ent on a river’s course, forcing its channel through a complication of moun- tains. 'This effect is considerably heightened by the pointed and jagged style * See further particulars of the gold-washings in the Gimté river, by Capt. Cautley, Journal Asiatic Society of Bengal, vol. iv. p. 279; Plate VII.; April, 1835. + Geological Transactions, Second Series, vol. iii. p. 393; Pl. XLV. 202 278 Capt. Cautiey on the Sevalik Hills. of the outline, depending on that abundance of clay and carbonate of lime throughout the whole formation, which permits even the shingle-beds to hold up their pointed summits in the wildest manner imaginable. At places, a per- fectly inaccessible needle of shingle raises its head far above the others, and is crowned by one solitary fir tree, Pinus longifolia. This conical form, pro- duced in the clays by weathering, is sometimes magnificently displayed, by the whole face of a cliff, consisting of light pink, yellow, and blue clays, being externally decorated with small conical spires of the clay from top to bottom, a height of 1000 feet from the bed of the river. The origin of this structure is due simply to a little coping stone, of some harder material than the matrix of the strata, and upon which the weather does not act so rapidly as upon the clay. Under a bright sun, the beauty of these cliffs, with their illumined pin- nacles, is exquisite ; particularly westward of the Jumna. I have before adverted to the presence of great abundance of lime, forming stalactites, and the cement of the sandstone and conglomerate. There is another striking method of deposition on the surface‘of the large stones which lie in the beds of the rivers, and which, during the greater part of the year, are in contact with the water. The substance is very similar in appearance to the coarse brown paper made in this country; and is produced by the water, while washing the stone, depositing its lime, and entangling the finer particles of vegetable matter, sand and mica, until the stone acquires a superficial coating, of a brownish yellow colour, which on removal resembles the substance before mentioned. Manukmow, near Suharunpoor, June 30, 1835. Nore By THE Epiror. For detailed descriptions, by Capt. Cautley, Dr. Falconer, Lieut. Baker, and others, of the most important animals found in the Sevalic Hills, see Asiatic Researches; Calcutta, 1836 ; vol. xix. Part. I.; and Journal of the Asiatic Society of Bengal, No. 35. vol. iii. p. 527; Nos. 45, 46, and 48. vol. iv. pp. 495, 565, 706.; Nos. 49, 53, 55, 57, 58, 59, 60. vol. v. pp. 38, 291, 294, 486, 579, 661, 739, 768. [ 279 |] a. Local debris. 6. Raised beach. c. Blown sand-hills. d. Silurian rocks. XXII.—Descripiion of a Raised Beach in Barnstaple or Bideford Bay, on the North-West Coast of Devonshire. By tue Rev. Proressorn SEDGWICK, V.P.R.S., F.G.S., ann RODERICK IMPEY MURCHISON, Esg., F.R.S., F.G.S. [Read December 14, 1836. ] DURING a recent examination of the county of Devon, undertaken in the hopes of ascertaining the geological succession of the more ancient rocks of which it is composed, we were unexpectedly gratified by the sight of the finest raised beach which has come within our observation. It extends, at intervals, along the shore and cliffs, for a distance of about three miles from the northern side of the mouth of the Taw, or Barnstaple river, to the bold headland called Baggy Point. After toiling through the hillocks of blown sand which encum- ber the mouth of this estuary, we were turning the rocky headland of Saunton Down, when, to our great surprise, a succession of yellow-coloured, low cliffs broke upon our view, running close along the shore, and rising to a height of about 50 feet, as an undercliff, upon the sides of the ancient rocks which form this part of the coast. It was evident (even at the considerable distance from which we first saw it) that this undercliff was composed of horizontal layers ; 280 Prof. Sepewickx and Mr. Murcuison and as, in colour and aspect, it differed entirely from any rocks by which we were surrounded, we first imagined it to be an outlying mass of oolite or green sand; nor were we undeceived, until we actually descended to the shore, so precisely did it resemble the sea-worn cliffs of many of our younger secondary formations. We then found that the top of this undercliff was occupied, to a depth of eight or ten feet, by a mixed detritus of angular frag- ments of the adjacent rocks, contained in a matrix of sandy loam. Beneath this drift, the yellow cliffs, which had attracted our attention, consisted, at their upper part, of finely laminated sand, with here and there an imbedded sea-shell, such as a common cardium or oyster, but generally in too fragile a condition to bear extraction. These beds of sand are about 25 feet thick ; and, as they pass downwards, they become harder, and are occasionally inter- rupted by a course of small water-worn pebbles, perfectly identical with com- mon beach shingles. Though usually arranged in horizontal lamine, these sands presented, at intervals, those appearances of false bedding so common in our tertiary and secondary strata (see vignette), putting on the form of wedges, the laminz of which run diagonally across the principal layers of the deposit. In descending to the shore, we found the lower part of the cliff passing into solid sandstone, and, finally, into a hard bed of shingle, or con- slomerate, resting upon the highly inclined and broken edges of rocks, which we refer to the “‘ Silurian System.” This portion of the cliff, consisting of hard sandstone and associated shingle beds, contains several marine shells, of existing species, among which are Cardium edule, Patella vulgaris, Mytilus edulis, Solen, Donax trunculus?.* On examining this portion (the lowest part being generally about three feet above high-water mark, at spring tides), we were forcibly struck with the analogy which the strata presented to many rocks formed before the pre- sent era. The grains of sands are agglutinated into a compact mass, which, on fracture, exhibits a shining, chatoyant lustre, common to calcareous grits of the secondary rocks, with an occasional tendency to run into concretionary forms ; and these regularly bedded, stony masses, pass into grit and shingle on the one hand, and into soft, incoherent sand, on the other. The maximum thickness of these lower consolidated strata, at the point where we first met with them, is about 11 feet, of which the upper seven feet are sandstone, and * We believe that all the shells in this raised beach belong to existing species. We should not, however, have been surprised had it contained some organic spoils resembling those of a warmer climate: for seed vessels of Mimosz, inhabitants of the Mexican Gulf and the West Indies, are annually washed on these shores, by currents probably connected with the great Gulf stream. We met with several examples of this kind. on the Raised Beach in Barnstaple or Bideford Bay. 281 the remaining four coarse and hard shingle. Occasionally, however, a small band of fine shingle, or a pebble of considerable size, may be met with in the upper portion. There is no exaggeration in stating, that much of this modern deposit is quite as difficult to break as the ancient Silurian rock on which it rests. By its texture, it will resist the ordinary action of weather ; but the surge, in vio- lent storms, beating against the lower portions of it, has worn them into caverns (see vignette), exposing, in their interior, the edges of the shelly beds; whilst over them is seen the successive beds of sandstone and sand, above noticed, At the point where these appearances are presented in greatest perfection, the total thickness of the beach amounted to about 36 feet ; which, with the overlying drift, and the inferior ledge of Silurian rocks, gave a height of 40 or 50 feet. By reference to the vignette, it will be perceived that the bottom of the beach accommodates itself to all the irregularities of the subja- cent rock, just as sand and gravel are arranged upon the broken edges of the chalk in the south-eastern parts of England. The deposit we have been describing, is continuous from Saunton Burrows, where it disappears under the blown sand, to the south end of Croyde Bay, on approaching which the cliff gradually subsides. ‘Throughout the area of that sandy bay, the rocky and high ground recedes from the shore, and there are no traces of the beach for nearly a mile; but on the northern side of the bay it is again met with near some lime kilns, where the lower shingle beds are perhaps fuller of shells than in any other part of their course. Here the coarse shingles, in parts expanded to the thickness of 19 feet, rise rapidly to the north, from a point three or four feet above the sea-level, to a height of 60 or 70 feet above high-water mark, resting on the rugged and abrupt face of Baggy Point—one of the boldest and loftiest headlands on this coast. It is worthy of remark, that it is near the point of greatest elevation, that the materials composing the beach are most coarse and brecciated, and in the greatest quantity. Such is a brief sketch of the nature and arrangement of this deposit, the position of which naturally leads us to offer a few remarks on the causes by which it has been produced. To this end, we shall endeavour to show, Ist, that the configuration of the neighbouring coast harmonizes with the supposition that this beach has been raised (within the modern era) from beneath the sea to the height at which we now find it; 2dly, that similar phenomena, on the coasts of Devonshire and Cornwall, and in other parts of England, agree with and confirm this hypothesis. 282 Prof. Sepewick and Mr. Murcuison 1. Phenomena on the Coast and in the Neighbourhood. We have stated that the southern end of the raised beach is lost under the blown sand of Saunton. This blown sand occupies a wide area of undulating hillocks (partially covered with bent-grass), which choak the northern side of the bay; the united rivers, Taw and Torridge, finding their course through them to the sea over bars of sand, which render the access to the ports of Bideford and Barnstaple very difficult. On the southern side of the bay these sand-hills disappear ; but, between the town of Appledore and the sea-shore, is a very remarkable and elevated straight ledge of rounded bowlders, called the “ Popple,” or pebble bank ; which, although quite analogous to the well- known “ Chisel Bank,” has not been noticed in the map of the Ordnance Survey. Itrises to a height of about five feet above the high-water mark of spring tides, is about one mile and a quarter long, and about 15 to 20 paces wide upon its summit, with shelving slopes on each side, giving it a broad and firm base. Itrises from 10 to 12 feet above the sands. The large rolled and rounded blocks, mixed with smaller gravel and pebbles, consist exclusively of a hard, grey and slightly mottled sandstone, of which there is a vast abundance on the reefs and headlands between this spot and Clovelly, and which, with the other strata around Bideford, we consider to belong to rocks of the age of the coal measures. This pebble bank, stretching from Rocks Nose northward towards the mouth of the estuary, shelters the marsh land behind it from the elements ; and hence it is, that a broad and low alluvial flat, interposed between it and the town of Appledore, is covered with grass, and exempted from the de- structive sweep of the blown sand, which has overspread the opposite side of the bay. Although it at first seemed difficult to account for the origin of this remarkable ridge of gravel, it appeared to be explained by the raised beach on the northern side of the bay: for we could not avoid inferring, that this pebble bank was one of the indications of a considerable rise of the land. In a former condition of things, when the neighbouring cvast was at a lower level, the materials of the present shingle bank might have existed as a natural marine accumulation, in the form of a reef; or they may have gradually assumed their present form, while the sea and land were changing their rela- tive level. Such a change would inevitably bring successive parts of the coast within the destructive operations of the surf, and naturally produce accumulations of water-worn materials. At all events, the “ Popple Bank’ appears to us not accounted for by the actual configuration of the coast and the ordinary action of the sea. on the Raised Beach in Barnstaple or Bideford Bay. 283 Jn addition to what has been said, we may remark, that the interior of the country near Barnstaple, has the configuration which we might expect on our hypothesis: for we may follow, both on the north and south side of the low tract near the mouth of the Taw, ridges of hills extending far into the inte- rior, and having the exact form of an ancient coast-line. 2, Similar Phenomena on the Coasts of Devonshire and Cornwail. Were the appearances above stated without any parallel on the English coast, they would be comparatively of small interest. In fact, however, they form but one of a long series of phenomena, all tending to the same con- clusion, viz. the changes of sea level during the modern period. We have no reason to look for frequent examples of raised beaches on the eastern shore of England: for, supposing them to have once existed, most of them would have been long since swept away by the encroachments of the sea line. But on the iron-bound coasts of Devonshire and Cornwall, this line is nearly stationary ; and, where the forms of the land have favoured the manifestations of changes of sea-level, raised beaches may be traced in so many places, as to form an almost connected series of phenomena. ‘The raised beach of Hope’s Nose has already been described by Mr. Austen; and after an exami- nation of the spot, we think his description exact, and his conclusions true*. We there find shingles and shell beds alternating in thin layers, utterly unlike any thing drifted by wind, or placed in their present position by the hand of man, and admitting of no rational explanation, except that which we have given of the similar beach in Barnstaple Bay. The Rev. Mr. Hennah long since pointed out to one of us, a shingle beach at Plymouth. Similar phenomena were observed by us, in 1828, on both sides of the western extremity of Cornwall: and in the elaborate work of Dr. Boaset, not only are numerous examples cited, of horizontal deposits of shingle and shelly marine sands at various levels above high-water, but the true cause is assigned for some of them—a change of sea level. Unfortunately, however, his descriptions are obscured by language derived from the then prevalent diluvian theory; and on that account do not produce their deserved im- pression. The accurate survey of Cornwall, by Mr. de la Beche, cannot fail to give us all the information we want on this interesting subject ; and we may expect from him a detailed account of all the phenomena of elevation and depres- sion (for there are proofs of both) exhibited on that coast. We may, how- * Proc. Geolog. Soc., vol. ii. p. 102. + Trans. Roy. Geol. Soc. of Cornwall, vol. iv. pp. 259, 270, 273, 320, 466. VOL. V.—SECOND SERIES. 2p 284 Prof. Sepewick and Mr. Murcuison ever, state generally, that the Cornish raised beaches, are not all at one level, nor of one character; and though they are all of the modern era, they do not belong to one epoch of elevation. They may be divided into Ist. High shingle beaches, resembling the large rounded blocks so con- stantly seen at the highest water level on all rocky shores. 2dly. Mid-water beaches, composed of rounded pebbles, broken shells, &c. exactly resembling materials washed up between high, and low water mark. These accumulations are seldom regularly bedded, but have more or less of a confused aspect. 3dly. Low-water beaches. 'These have originally extended from a few feet above low water, to an indefinite depth ; and, consequently, such masses are regularly stratified, being made up of small gravel, alternating with sand, single shells, and beds of shells, all similar to living species of the present coast. Such appears to us a natural division of these beach deposits ; and the Cor- nish coast offers fine examples of each class. The phenomena, described by Mr. Carne, near the Land’s End* (viz. large rounded blocks, 30 or 40 feet high, in the successive bays and headlands, and nearly all at the same level), were observed by one of the authors in 1828 ; but, misled by the diluvian theory, he then misinterpreted their meaning. But we can now perfectly understand how these high-water shingles should appear by themselves, the other parts of the beach having been washed away. The shingle beach at Plymouth may be mentioned as an example of the second class. But the third class is incomparably the most interesting; be- cause it conducts us to the old water-worn rocks, once washed by the sea, and forming the actual ledge on which these low-water beaches rest; and also because, having been partially deposited under the sea, it is charged with abundance of marine spoils, and sometimes with regular beds of sea-shells. Of course, the shells, as in beaches of the present day, were for the most part dead, when entangled in the layers of sand; but in some cases, we have a proof, that the animals were not dead at the time they were first entangled in the deposit where we find them; though now raised many feet above the highest tidal level. Such examples may be seen north of St. Ives Bay, and south of New Quay, and at several other parts of the north coast of Cornwall+. Now in most cases of raised beaches, we may infer, @ priorz, that the coast was shelving and shal- Jow before their elevation ; for such beaches could adhere but imperfectly to an abrupt shore ; and if adherent for a short time, would soon be washed away. Hence it is, that where we find raised beaches, we may look for extensive * Trans. Roy. Geol. Soc. of Cornwall, vol. iii. p. 229, et seq. + Ibid., vol. iv. p. 259. on the Raised Beach in Barnstaple or Bideford Bay. 285 low-water sands. ‘The two sets of phenomena generally occur together, so that one becomes an indication of the other. On the coast of Cornwall, wherever we meet with low-water sands of any extent, they are drifted by the fierce western gales over all the neighbouring cliffs, and, in course of time, have, in some places, converted whole parishes into deserts. After what has been said, we need not be surprised that these drifted sands should chiefly occur along those parts of the coast, where raised beaches most prevail: in short, the two things are generally found together. This fact misled some of the early writers in the Transactions of the Royal Geological Society of Cornwall*, who attributed the raised beaches themselves to the blown sand, under which they, as well as the older rocks, were partially buried—a very great mistake, though quite natural at the time when it was made. Dr. Boase, we believe, had the merit of first pointing out this error +. The conclusions from these facts are obvious, and in perfect harmony with our observations on the beach and shingle of Barnstaple Bay ; both as respects their structure and their occurrence in the mouth and seaward flanks of an estuary, so much covered by blown sands. The elevation of the northern side of Barnstaple Bay, makes it almost cer- tain that the south side must also have been affected by a similar movement ; and in our reasoning respecting the “ Popple-Bank,” and the configuration of the neighbouring country, we have assumed that both sides have been raised above a former level, by a similar movement. But, at the time of our rapid passage along the cliffs south of Rocks Nose, we were not aware of the existence of any phenomena on the northern shore of the bay, or, indeed, on any portion of the east coast of Devon, such as we have now described ; and hence we omitted to look out for any direct proofs of elevation. Again; the great elevation of the coast line, extending to Baggy Point, could hardly have taken place without simultaneously affecting the portions of North Devon and West Somerset, which form the southern shore of the Bristol Channel. There, however, we found no traces of any raised beaches, though our atten- tion had been previously drawn to them. Their absence is, however, easily accounted for, by the very abrupt form of these bold cliffs, and the deep seas by which they are washed ; which are so adverse to the formation, and permanent elevation, of extensive shelly and sandy deposits, like those above described. The raised beaches to which we have alluded, in South Devon and Corn. wall, have been stated to indicate an elevation of the land, varying from 10 to 40 feet; but our case, in Barnstaple Bay, gives a maximum rise of 60 or 70 feet, indicating a greater intensity of elevatory movement as we proceed to the north. If we ascend the estuary of the Severn, and follow that river up * Trans. Roy. Geol. Society of Cornwall, vol. i. p. 4. + Ibid., vol. iv. p. 260. 2P2 286 Prof. Sepewick and Mr. Murcuison on the Raised Beach, &c. to the highest navigable points in Shropshire, we find (as has been shown by one of the authors*) that gravel and sand, with sea-shells of existing species, occur in many places, at elevations of from 300 to 600 feet above the sea: and still further to the north, the elevation of similar deposits is maintained through Lancashire, till they approach the mountains constituting the southern fringe of the Cumbrian chain. Hence we have no hesitation in admitting, that in a portion of our island which ranges from Cornwall and Devon to the southern limits of the Cumbrian chain, there have been great movements of elevation subsequent to the creation of existing mollusca; these movements apparently increasing in intensity as we proceed from south to north, or rather from south-west to north-east. No doubt there are many portions of the coast of our island, where we not merely have no proofs of any change in the relative level of land and sea, produced by elevation during the modern period, but where we appear to have direct evidence of a partial depression of the land. It is not, however, our in- tention to enter any further on these subjects. We have described a local phe- nomenon of some interest, and endeavoured to show its connexion with similar phenomena on a more extended scale. But any consideration of the effects produced by such movements as we have described, on the general configura- tion of our island, or on the drifted materials which are accumulated on its sur- face, would lead us into details quite beyond the purpose of this short memoir. * Proceedings Geol. Soc., vol. ii. p. 333. [ 287 ] XX1IV.—Eztract from a Letter, by the Rev. Davin WiuiaMs, F.G.S., on the raised Beaches in Barnstaple or Bideford Bay. [Read March 8th, 1837. ] THE first beach extends from Braunton, or Saunton, Burrows, (where its eastern limit is concealed by ancient drift sand) to Downend Point, round which it winds, and flanks the southern promontory of Croyd Bay. On the north coast of this little bay are vestiges of another beach, extending in patches from near the lime-kiln, to the bold and bluff headland called Baggy Point. In consequence of its prolongation into deeper water, and its having been consequently exposed to a more constant and heavy action of the sea, it is, in places, nearly all removed ; but enough remains to show, that it once extended a long way between Croyd Sands and Baggy Point. In both instances the beaches contain abundance of recent marine shells, and afford a sufficiently compact and tough sandstone to be used in the construction of boundary walls. They frequently present the diagonal lines mentioned in the paper of Professor Sedgwick and Mr. Murchison, and so common in the new red sandstone. That these beaches have been raised from five to ten feet, or that the level of the Atlantic has been depressed to that amount, | have no doubt; for on a careful examination of the slate rocks, at their immediate contact with the present base of the ancient beach, I found, in many places, countless Balani on the surface of the slates, yet so entangled and cemented in the sandstone, that, on detaching a mass of the latter, the Balani were torn off the slate. It is probable, that they may be also found at higher levels under the sandstone, as at points where I noticed them, the beach had been denudated horizontally at least twenty-five feet. It is certain, however, that they may be seen from five to ten feet above the level, where the living Balanz exist on the same slate rocks; and there is a considerable interval between the living and the dead, where none occur. Another fact in corroboration of the relative changes of level, as regards the sea*and the sand-cliff, is a magnificent granite block at the base of the sandstone, and resting directly on the slate rock, but above high-water mark. It is so perfectly smooth and close-grained, and so rounded at its edges and 288 Mr. Wits on the raised Beaches in Barnstaple Bay. angles, that I had great difficulty in detaching a small fragment. Its exposed surface is six feet long and three feet deep; but I could not ascertain its real dimensions, as its further extremity is concealed by the incumbent sandstone of the beach, and its base by shingle. It is flesh-coloured, like much of the Grampian granite, and is traversed by two veins of red-coloured, compact felspar, intersecting each other. In my opinion it is neither Lundy, Dart- moor, nor Cornish granite. As the beaches show few or no evidences of disturbance, resting in hori- zontal unconformity, on highly inclined slate rocks, I inferred that the move- ment which effected their elevation was gentle, or that a great area had been simultaneously raised en masse. With this impression, I examined the di- strict for phenomena, which might corroborate the hypothesis, that the pre- sent position of the beach was due to gradual elevation, and not to a depres- sion of the level of the ocean. When we examine the submerged forest ex- tending from the mouth of the Parret to Minehead, can we deny that there must have been a subsidence of this line of coast at a recent geological period? If we continue our researches in the marshes, about seven or eight miles to the eastward, we observe at Benthill and in King’s Sedgmoor, sand-banks and ancient sea-beaches, containing an abundance of recent marine shells. Looking at these sand-banks on the one hand, and the submerged forest, con- taining stags’ horns, hazel-nuts and leaves on the other, I apprehend that the phenomena can only be explained by partial elevations and depressions of the land, and not by lowering of the ocean’s level. The distance may be fifty miles between the submerged forest and the beaches of Barnstaple and Bideford Bay; but when we consider the great scale on which Nature conducts and has conducted her operations, I trust, I am not straining probability too far, when I assume that the oscillations and vibrations which could elevate the old bank or beach at Santon Downend, and a great adja- cent area of land, would extend along the whole coast. Bleaden, near Cross, December 31st, 1836. [ 289 ] XXV.—Memorr to illustrate a Geological Map of Cutch. By C. W. GRANT, Esq., Capt. Bombay Engineers. [Read February 22, 1837. ] CONTENTS. GrocrapuicaL Position.—Physical Aspect of the Country. Formations :—p. 290. 1. Syenite and quartz rock, p. 291. 2. Sandstone and clay, with beds of coal—tron ore and manufacture of—Coal—Borings for coal—Vegetable impressions—Extent of coal field—Alum works near Mhurr, p. 292—296. 3. Red sandstone, p. 296. 4. Upper secondary formation—Description—Relative position with respect to the other strata—Apparent position with respect to the English series—Fossils-— General shape of the hills—Manner in which the hills have been formed, p. 296—299. 5. Nummulitic limestone and marl—Characteristic fossils, p. 300—302. Tertiary strata—Fossils—Extent of the formation, p. 302—304. 7. Alluvial, or recent deposits—Land gaining on the sea—Marine forests—Effects of floods, p. 304—306. 8. Volcanic and Trappean rocks—Evidences of disturbing agents—Distinct periods of volcanic eruptions—Alternations of basalt with strata of the upper secondary formation—with calcareous grit—with travertin—Dykes of basalt—Extinct volcano—Igneous outbursts, p. 306—318. Tue Granp Runn.—Natural walls—Successive depositions of marine and fresh-water strata, p. 318—325. Concxusion, p. 325. Apprenpix, Description of Fossils, p. 326, et seq. GEOGRAPHICAL Position, AND Puysica ASPECT. THE province of Cutch, in the East Indies, is situated between the 22° and 24° of north latitude, and 68° and 70° of east longitude*. It is bounded to the north by the Grand Runn, beyond which is the Thur or Little Desert; to the S.W. and S. by the Gulf of Cutch and the Indian Ocean ; to the E. and S.E. by the district of Guzerat ; and to the N.W. by the eastern branch of * See Map, Plate XX. 290 Capt. Grant on the Geology of Cutch. the Indus and the territory of Sinde. Its extreme length from E. to W. is about 180 English miles, and its extreme breadth is 50 miles; but in one place it is not more than 15 miles across. It contains about 6500 square miles, independently of the Grand Runn, which ought, however, to be con- sidered as a part of the province, and which, including the islands with the portion bounded by the Guzerat coast, occupies an area of at least 9000 square miles. Physical Aspect of the Country.—The province is hilly and rocky, with the exception of the part forming the southern coast, which is a dead flat covered with a fine rich soil. Three distinct ranges of hills, having an easterly and westerly direction, may be traced (see Map, Pl. XX.). The most northern forms an irregular chain bordering the Runn, and, for the greater part, pre- sents to the north a perpendicular cliff surmounting a sloping talus, and to the south an inclined plane. It is composed chiefly of rocks, containing marine re- mains. The next, called the Charwar range, passes transversely through the centre of the province, and is connected with the former, at its north-western extremity, by a cluster of hills. It consists partly of sandstone containing beds of coal, and partly of a series of strata of slate clay, limestone slate, and slaty sandstone. The third, or southern range, and composed entirely of volcanic materials, has the same direction as the other two; but it is of smaller extent, and a branch of it, striking nearly north and south, passes through the centre of the Charwar range. | Rubbly Basalt. Ex ——-| Crystalline Travertin. & ” Friable calcareous stone, so Travertin. 5° Ss ure Friable Iron.clay. soe | } Solid Basalt. a VS pF tN ISSN gegeice t ee Friable Basalt. The friable basalt forms the base of the fall. Above the columns the bed of the small stream consists of a loose, calcareous calc-tuff. This section presents several interesting facts; as, from the alternation of basalt with the lime- stone or travertin, it is evident, that a considerable time must have elapsed between the igneous eruptions. The variety in the texture of the limestone or travertin may be accounted for by supposing, that the waters under which it was deposited were sometimes perturbed, or rendered muddy by a flood; but at other seasons clear, when a pure calcareous precipitate would take place. The basalt forming the columns is very hard, compact, of a dark blue colour, and smooth surface ; and it may: be traced to some small hills northward of the spot. Near this place the surface has been affected in a manner worthy of ob- servation. Every here and there, a small spot, varying in size from 3 to 20 a Capt. Grant on the Geology of Cutch. 315 yards in diameter, has been raised into a convex form; the pavement, that covers it, consisting of tabular plates of slaty sandstone, broken into small masses ; and the fractured lines generally radiating, though in an irregular manner, from a centre. In some places the tops of these little globular eleva- tions have been removed, leaving a regular circle of stones, whose bounding lines are disposed like the stones of an arch. In other instances they assume a more conical shape, resembling small hillocks, from the upper part of which the outer coating or tabular masses have generally fallen away. When they are of a larger character, the whole presents a heap of broken masses of rock. Denodur Hill, an extinct Volcano.—Of the detached hills, the elevation of which I conceive to be due to volcanic influence, the principal is that called Denodur, and is situated near the shores of the Runn. It is the largest and highest hill in the country, and is evidently the remains of an extinct volcano, an irregular crater being still visible. In the north side is a large gap, reach- ing nearly to the foot of the hill, but partially blocked up by a lower ridge, or a kind of traverse. Its western flanks are composed ofa series of ridges of lami- nated clay and loam, interspersed with flat, angular fragments of slaty sand- stone and slate-clay. The surface of some of these ridges is smooth, consisting either of thin slabs of slate-clay, or of thicker slabs of a very compact, crystal- line, and slightly calcareous stone, the same as that which overlies the laminated series, and forms the walls on the Runn, &c. Near the base of the hill and for more than two-thirds up its side the construction alters, being composed partly of a loose sandstone, and partly of the calcareous grit, containing imbedded, angular fragments of basalt; the uppermost part is a perpendicular wall of basalt, which, apparently, continues all round the top. A stream of very compact basalt runs past its north-western flank, and in other places. Nu- merous small conical hills, composed of horizontal Jayers of limestone grit, or of basalt, are scattered over its sides, and its base is covered with a thick mould, formed of decayed vegetables, with earthy matter. Nowhere did I find any traces of recent disturbance, although the people of the neighbour- hood, particularly the Jogees, or religious devotees, who inhabit a temple on its northern flank, asserted that fire issued from it during the earthquake of 1819. If it did, there would, of course, be some signs of it remaining ; but I was unable to penetrate into the interior of the hill, owing to the dense Bauble Jungle, or crooked thorn tree with which it is covered. Not far from this place, and adjoining the village of Nuckutrana, is a hill of some size, called Ungia-soorud, the elevation of which has also been effected by volcanic agency. The flanks and base are composed of a very loose, friable, calcareous sandstone and grit, apparently stratified, but inclined VOL. V.—SECOND SERIES. cue 316. Capt. Grant on the Geology of Cutch. at all angles ; and the remainder consists of very compact basalt. The hill is divided into two parts by a narrow, tortuous cleft, the sides of which are nearly perpendicular, and composed of irregularly triangular prisms of basalt. The cleft is not more than four feet wide at the bottom, though it is somewhat broader at the top; and as it passes completely through the hill, we must suppose the whole to be similarly composed. All the other numerous isolated hills scattered over this part of the province, including that called the Nunnaw, next to Denodur, appear to be similarly constructed. The hill called Lecka, deserves particular notice. It forms one of a group of hills on the borders of the Runn, at the north-western extremity of the pro- vince, and is composed of two portions ; one consisting of stratified beds of sandstone ; and the other wholly of basalt, in irregular, triangular columns, The beds of sandstone are horizontally disposed, and of various colours and textures; the lowest stratum being a coarse, brown, quartzose grit. The igneous rocks crop out in various places near this spot, forming a cluster of small hills between it and the Jooria range; the intervening spaces being broken in the most confused manner. Recent Outbursts.—Having given as many examples of the elevatory ef- fects of volcanic action as my space will admit, I shall conclude my account of their phenomena with a description of some igneous outbursts of, apparently, avery recent epoch. ‘The principal one occurs at the village of Wagé-ké- Pudda. ‘The spot which has been acted on is a rather high table-land, com- posed of the nummulitic marl, and is flanked by low, irregular hills of iron- stone and gravel, called by the natives Kara Rurraw. The first view of it, is very striking. Conceive a space of about two square miles, blown out into a flat basin, the sides being broken into fissures, with craters, ravines, and hol- lows ; and the interior, or bed of the basin, interspersed with hillocks and cones of every variety of colour, black, red, yellow, and white, and with patches of cinders, similar to the refuse of a furnace ; the whole looking as fresh as if the igneous agents were still in operation. The surface of the table-land immediately surrounding the blown-out space, is covered with a burnt ironstone, divided into irregular cells, similar to Sep- taria ; below which are steep banks, 40 to 50 feet high, consisting of commi- nuted particles of clay, sand, gravel, scoriz, and small angular pieces of basalt; the whole being loose, and having a dry and brittle feel. Within the centre are several small craters, or circular spaces, surrounded by walls of basalt. None of them are perfect circles, being broken through by watercourses ; but one has about two thirds of its circumference com- — Capt. Grant on the Geology of Cutch. 317 plete, the sides of which, about forty feet high, are in the upper part quite perpendicular, and consist of very compact basalt, of a columnar structure ; while the lower ten feet present a talus, composed of volcanic sand, and scorie in very thin lamine. — Below the columnar basalt is a bed of a friable variety, three feet in thickness. In some parts the columns are capped with a thin band of ironstone. The interior of this crater is about 80 yards in diameter, and consists of volcanic sand, with imbedded angular fragments of basalt. The most perfect of these craters, or circular spaces, are generally hid from view, being approachable only by the narrow ravine forming the outlet of the watercourse which cuts through them. The basalt varies greatly in texture and general appearance : in some places it is columnar, exceedingly hard and com- pact, in others it contains imbedded crystals of felspar, and it occasionally presents the structure and texture of an amygdaloidal clay. Some varieties also consist of concentric layers of a kind of brittle, clayey substance, inclo- sing a nucleus of hard rock; the whole being imbedded in a mass of clay, which looks as if a number of small roots were entwined about it. All the varieties are frequently found in the same bank or hillock. Several other small basins have been blown out in the surrounding’ table- land, forming inverted cones, about 15 or 20 feet in depth; and are composed of the same materials as those just described. Many of them consist entirely of small, brittle particles, of a pale yellow colour, evidently sulphuric. The clay has, in various places, been burnt into a perfect brick ; and the marls, or sandy clays, are frequently of a beautiful bright purpie. Quantities of talc, or mica, lie scattered about, twisted and contorted into a variety of shapes; and some of the iron ore which covers the surface, appears to have been partially fused, consisting of a spongy, vesicular mass. The whole has the appearance of having been for some time subjected to considerable heat, and then suddenly blown up. The cones and banks of loose volcanic scoria must be yearly washing away ; and it is difficult to conceive, that the walls of solid basalt forming the sides of the craters, can belong to a similar period, having all the appearance and texture of very old basalt ; but it is possible that a recent erup- tion may have taken place in the site of one of a more ancient date, thus pre- senting a mixture of old and recent volcanic products. If it is true, that basalt owes its columnar structure to its cooling slowly under a great pressure, it is impossible that these masses of columnar basalt and the loose cones of scoriz can be contemporaneous. In the nummulitic marl forming the banks of a river which flows past this patch of blown-up ground, is a stratum of earth containing small nodules or 272 318 Capt. Grant on the Geology of Cutch. rounded masses, of a pale yellow colour, translucent and brittle, and which burn with a bright flame, giving out a strong aromatic odour. It is contained in a dry, olive-brown earth, so light as to float in water. Numerous Echinodermata, and other fossils, are found on the table-land, and some of the fields are thickly strewed with casts of a'Turbinella of a very Jarge size, the external shell being always wanting. On breaking them, small fragments of igneous matter are found in their interior. In the table-land just south of the outburst, is a large fissure, about a quarter of a mile in length, 40 yards broad, and 40 or 50 feet deep. One extremity communicates with the river, and the other is rounded, or formed into a basin shape. The sides are perfectly perpendicular ; and it is clearly an opening in the ground, there not being the slightest indication of any- thing of the kind, until directly at its brink. 1 was informed by a native of the village, (the only present inhabitant,) that smoke issued from the outburst about twenty-two years since; but little dependence can be placed on the statements of these people. Another similar, but smaller, outburst occurs about three miles south of Mhurr, near the spot in which, in my account of the tertiary deposits, I men- tioned that a large basaltic dyke crosses the river. ‘The space here blown out, does not exceed 100 yards in diameter, and 15 feet deep, consisting of similar cones of volcanic scoria, and comminuted particles, as above described ; but there is no trace of any basalt nearer than the dyke in the river. From what I have now detailed, it appears, that igneous action has affected all the formations of which the province is composed ; and it will also appear, by the following details, that the Grand Runn, the most remarkable feature of the country, owes its peculiar characters to volcanic action. Tre Granp Runn. With a short account of this large and singular tract, I shall conclude the paper. It has been described by Captain Burnes, in a memoir in the library of the Royal Asiatic Society ; and referred to, at considerable length, by Mr. Lyell, in his “ Principles of Geology *.” This tract, contaming an area of upwards of 7000 square miles, exclusive of the space occupied by the Bunnee, and the islands of Puchum, Khureer, &c., is, perhaps, unparalleled in any known part of the globe, as it may be said to be placed on a level between land and water. Itis dry during the greater part * Sth Edit., vol. ii. p. 183 et seq. Capt. Grant on the Geology of Cutch. 319 of the year, when its surface consists of a sandy flat, totally devoid of vegeta- tion; but, perhaps, on account of its saline nature, always sufficiently moist to prevent its particles being drifted. During the prevalence of the south-west winds, however, so much water is blown up its eastern inlet by the Gulf of Cutch, and, at its western extremity, by the eastern branch of the Indus, as to cover its whole surface ; augmented by the freshes, which, at the same time, come down the Loonee and Bunass rivers, and the numerous small streams which intersect the northern coast of Cutch. At those seasons, the Runn has all the appearance of a sea, and is passable only on camels, and, in some seasons, with difficulty. It has been described as the dried-up bed of a sea; but it is not easy to account for its drying up, unless we suppose a gene- ral depression of the ocean, We must, therefore, look to other causes. In several parts of the world, particularly in the Baltic, there are undeniable proofs of a gradual rising of the land; and, in time, parts of that sea might be converted into a tract similar to that of the Runn*. It does not become me to inquire whether this gradual elevation is due to a series of so minute ele- vatory movements as to be unnoticeable, except from the effects which subse- quent measurement proves them to have produced, or from a gradual expan- sion by volcanic heat. But in Cutch we have evidence of movements within a very late date, and every reason to believe that similar ones have occurred at various periods. The earthquake of 1819 is known to have produced a remarkable change on the western extremity of the Runn, by throwing up a mound 50 miles in length, 16 in breadth, and 18 feet high; and by depressing an adjoining tract, so as to convert it, from a cultivated district, into a large salt lagoon. As the changes in level, thus effected, have, however, been de- tailed in other papers, I shall merely observe, that when I was at Luckput in January, 1834, very little if any change had occurred since Captain Burnes’ visit, in 1828; except that the Sindians had repaired all the bunds across the river, and thus, by preventing further supplies of fresh water, the lagoon had assumed much the same appearance as previous to the freshes of 1828. I was also informed by a boatman, who constantly plied up and down from Ullah-Bund to the sea, that between Sindoo and Sindree (see Map), there isa bank, six miles broad, covered by only one foot of water; and as there is no channel through it, the boatmen are obliged to get out and haul the boats across the bank, after which they follow the windings of the channel to Ullah- * See Mr. Lyell’s Memoir, on the proofs of gradual rising of the land in Sweden, Phil, Trans. 1835, p. 1 e¢ seq. 320 Capt. Grant on the Geology of Cutch. Bund. It would therefore appear that this portion could not have been so much sunk as that around Sindree, and between it and Luckput. I was also assured that pieces of iron and ship-nails have been thrown up from fissures in the Runn; and Capt. McMurdo* mentions a boat which had been buried under 15 feet of alluvium, having become exposed in a mud- bank, near the village of Wuwania, on the Kattywar side of the Runn, or where it joins the Gulf of Cutch. The number of places still pointed out as Bunders, or quays, together with the large stones formerly used as anchors, one of which still lies on a small elevation on the Runn, not far from the Puchum Island, and the confident assertion of all the inhabitants on its coast, tend to confirm the opinion that the district must once have been covered by a navigable body of water. Some parts of the shores have precisely the appearance of having been re- cently deserted by the sea. ‘This is particularly the case near the village of Charee, which is separated from the Runn by a low range of hills. To the northward of this range is an inlet, about one mile and a half in breadth, and it looks precisely like a small creek or bay from which the tide has just ebbed. Its surface is composed of smooth, whitish clay, with numerous scattered gravel banks, the ends of which have been worn round, and the sides present perpen- dicular or overhanging banks. Several masses of crystalline sandstone also rise suddenly out of the bed; and some of them consist of immense fragments, which look as if they had been piled one on the other, and have a strange effect from a short distance. Beyond the inlet is another range of hills of the same description, but it is more broken and confused than any other in the country. In some places, the upper stratum of hard rock has been thrown into a position like the roof of a house; in others, it precisely resembles a ruined fort with towers on a hill; but the greater part of the stratum is a confused assemblage of huge fragments of rock. Northward of this range, and sepa- rated from it by a narrow belt of the Runn, is a steep conical hill, called Keera, 600 or 700 feet in height, consisting partly of the same materials as the others, and partly of basalt ; and it appears to have been formed in a similar manner to the hill called Ungur-soorud, before described, and others of that class. It is also more than probable, that the peculiar, fractured appearance of all the ranges is due to the same cause acting at the same period. Supposing the bed of the Runn to have been raised by a series of violent movements, such as must have upheaved the Keera, and its surface to have * Extract from Captain McMurdo’s MS. memoir on Kattywar, in Captain Burnes’ Travels in Bokhara, vol. iii. p. 329, note. Capt. Grant on the Geology of Cutch. 321 been broken, and covered with fragments of rock, its present level outline may be ascribed to subsequent operations. ‘The Runn is bounded to the north, as already stated, by the Thur or Little Desert, a district composed entirely of sand. The Loonee and Bunass rivers also flow through a sandy soil, as do many other streams which enter from the Cutch side. Now, during the peri- odical floods, vast quantities of sandy alluvium must have been brought down by these rivers, deposited at their mouths, and washed thence and spread over the surface of the Runn by the sea-water annually blown up at its eastern and western extremities. This operation, repeated yearly, would fill up all inequa- lities, and produce in time a level surface. It is probable, however, that the present state of the district may also be, in some measure, owing to a gradual rising of its bed, as it is only to such operations that some of its shores, as those of the inlet above mentioned, can be ascribed. There are also many facts to prove, that this tract has been elevated at very different periods. The high hills bordering its southern shore are, as before stated, composed principally of the laminated series, and their surfaces are co- vered with Ammonites, Nautilites, Belemnites, and other fossils of that geo- logical period ; whereas along its immediate line of shore, there are generally low ridges, composed of rocks full of marine‘remains of a totally different cha- racter, many of them belonging to existing species. Numerous small rocky islets, consisting of shells agglutinated into a solid mass, occur in various parts of the Runn, and are barely raised above its present level. They are pro- bably merely the higher portions of large tracts, the lower parts of which are covered by sediment. Natural Walls on the Runn how formed.—Still more striking instances of the effects of upheavement, since the Runn assumed its present characters, are exhibited in the detached, elevated masses of rock which I have called the Natural Walls on the Runn. They consist (see woodcuts) of disconnected portions of rock rising abruptly from the surface of the Runn, and presenting a smooth, vertical wall, occa- sionally upwards of thirty feet in height, and in one instance upwards of two End view of a wall, about 15 feet high, and two miles long. miles inlength. Some of them resemble domed or vaulted buildings, the 322 Capt. Grant on the Geology of Cutch. Dome-shaped wall. reversed side consisting of a talus of broken fragments of rock and soil. 3 CB 2 === ee vided into masses, but not broken. \ z, S : Side view of the same, showing the stones on end. Capt. Grant on the Geology of Cutch. 323 oh YES ==) f= MTSE Z ‘ 2 SN ahh 00. yds E : Sa eS ae 70 yas Two walls on the Runn, forming a semicircle, but sloping outwards. In one place these walls form a semicircle about 500 yards in diameter, both walls slopmg outwards. That the walls have been uplifted into their present form is quite evident, first, from the stones being all on end, that is, with the grain in the direction of their present position, and peeling off in scales down the face of the wall; and secondly, from my having met with the same phenomena ona smaller scale, in other parts of the country, where the slabs of rock are at all angles, and even, as those before mentioned, turned over. It should be noticed, also, that the borders of the Runn, near these walls, are composed of friable beds of the laminated series, covered with thick tabular masses of hard sandstone, precisely similar to those forming the walls. Had they been uplifted during the permanent prevalence of the waters, the sloping talus of earth and fragments of rock, with which they are all backed, must have been washed away. It should be stated, that these examples are situated on ground now almost recovered from a state of Runn ; some parts having been sufficiently augmented by means of the sandy alluvium, washed down from the neighbouring hills to support vegetation ; whereas the iso- lated rocks, several of which rise out of that part of the Runn, and are still subjected to inundation, have no detritus or talus, but present smooth walls of perpendicular rocks. I could never perceive any water-marks on them, nor any remains of marine testacea, which might occur, had the sea ever washed the present level of their foot. It is probable that their origina base lines have become obliterated by the sediment which must have accumu- lated round them in course of time, and which forms the existing surface. A very good example of a similar wall occurs in the centre of the province, near the village of Rampoora; itis a ridge of coarse sandstone about 300 yards in length, and from 10 to 15 feet in height, the stones being evidently placed edgeways, and in so regular a manner as to resemble precisely an ar- tificial wall. It rises from a base of the same sandstone, and on one side it VOL. V.—SECOND SERIES, 2u 324 Capt. Grant on the Geology of Cutch. Wall of sandstone near Rampoora. is nearly flat, but broken into masses, while on the other side are heaps of stone, broken and confused, and the interstices are filled with sand and small trees. At the extremity of the wall the stones slope up like the end of a roof. In the immediate vicinity of this wall is a small range of basaltic hills, striking however at right angles to the direction of the sandstone ridge. Some of the rivers which flow towards the Runn from the Cutch side are lost in the sand at their mouths ; though at a short distance up the bed of the river, the stream runs freely. It would thus appear, that at these spots, the bed of the Runn has been increased, by the sediment, probably, brought down by the stream ; but so loose is the soil, that the water soaks into it and even flows under it, instead of wearing channels. ‘This phenomenon is observable in the sandy beds of many of the rivers in the province. The stream may be noticed running with some rapidity and of a sudden to cease, the bottom of the river presenting a smooth sandy surface ; but a mile lower down the water again issues and continues its course ; the intervening parts being sometimes quite hard and dry ; in others forming very dangerous quicksands. The natives have various traditions that the drying up of this sea was sud- den, and that boats were tossed on the land and wrecked ; they pretend also to assign a date to this event, but their accounts differ so materially and are so vague, that not the slightest reliance can be placed upon them, except to the general fact. It is evident that the Runn could not have been drained by the bursting of its boundaries, at least since it was deep enough to be navigable ; because its present surface, notwithstanding the sediment which yearly accumulates on it, is even now so little raised above the sea’s level as to be flooded by the mere effects of the wind; but the most probable supposition is, not that it was ever a detached inland sea or lake, but that it communicated with the ocean by its present outlets, and that its bed has been raised, partly per- haps by a gradual movement, and partly by violent upheavements during AE ES A I ay re EE” NR 6 CA a aaa AOR oy, Capt. Grant on the Geology of Cutch. 325 earthquakes. Even such marked changes of level as the raising of Ullah Bund, and the sinking of the ground near the large town of Luckput, would have passed unrecorded but for the accidental circumstance of the district having been visited by a British officer. Other portions of this vast area, the greater part of which is never traversed by man, may have been similarly affected at that time, and yet the changes remain unknown. Successive Marine and Freshwater Beds.—The submerged tract near Luckput, or Lake of Sindree, may, I think, illustrate the manner in which suc- cessive marine and freshwater deposits may be produced. This tract was at one period a richly cultivated district, periodically flooded by a branch of a great river, and produced large quantities of rice. In this state numerous land testacea no doubt occupied it, and were mixed with the remains of fluviatile species brought down by the floods. ‘The bones of animals used in agriculture, and those of various domestic species, also the remains of broken pottery, perhaps coins, and other proofs of civilized life, might likewise have been imbedded. Suddenly, owing to the damming up of the river by the Sindians, the supply of fresh water ceased, and the tract was no longer cultivated or inhabited. Some time afler this an earthquake occurred, up- lifting one part and depressing below the level of the ocean another, which was immediately converted into a salt lake. A perfectly new description of deposit and organic remains must then have been accumulated, consisting wholly of marine animals, principally such as inhabit shallows and tide-ways. Again, owing to the sudden melting of the snow on far distant mountains (the Hima- layahs) the waters of the river came down with such force as to burst all the bunds built across it, as well as that thrown up by the earthquake, and covered the tract with fresh water, or perhaps with fresh at its upper or northern ex- tremity, and brackish at its southern near the sea. Supposing this state of things to have remained for some time, the river continuing to pour its water into this lagoon, another change would take place in the description of the sedimentary deposit. Once more the bunds were erected across the river, the supply of fresh water ceased, and as that on the lagoon evaporated, the sea again flowed in and converted it into a salt lake, which is its present state. All the above changes are known to have occurred ; and it is easy to suppose that if the shallow part at Sindoo were slightly raised above its present level, thus shutting out the sea, the part around the Fort of Sindree would be con- verted once more into dry land. If, therefore, at any future period, the river should again cut a channel, the banks might present various, regular heds alternately enclosing marine and freshwater exuviz, the latter being also as- sociated with land productions. 2u2 326 Capt. Grant on the Geology of Cutch. The ruins of one of the towers of the Fort of Sindree remained, when I visited Luckput in 1834, and in all probability now stand as a monument of the changes, which are daily taking place on the earth’s surface. Conclusion.—In concluding this paper, I have only to observe, that I have throughout endeavoured to describe facts as they appeared to me at the time I examined them, without regard to any particular theory ; and if I have failed in making my descriptions intelligible, I have only to plead the diffi- culty of having had a great deal to describe in a limited space. As the country to which this memoir relates is, however, unfortunately from its geographical position, beyond the reach of general observers, I am induced to hope, that this sketch, however imperfect, may be found to possess some interest. For the arranged list of fossil shells, given in the Appendix, as well as for all my information on that subject, | am entirely indebted to Mr. James De Carl Sowerby, who had my specimens (now in the cabinets of the Geological Society) for some time in his possession for examination. The woodcuts are copied from drawings taken by myself on the spot, for the express purpose of geological illustration, and are unexaggerated views of what they are intended to represent. December 31st, 1836. [ 327 ] _APPENDIX. SYSTEMATIC LIST OF ORGANIC REMAINS, THE PLANTS DETERMINED BY MR. JOHN MORRIS, AND THE REMAINDER BY MR. JAMES DE CARL SOWERBY, A.L.S. The fossils considered as belonging to previously described species, are distinguished by a reference to the work in which they were first noticed ; the new species are described in the explanation of the plates at the end of the part. Class, Genus, and Species. Plate. Formation. Locality. Remarks by Capt. Grant. Plante. Ptilophyllum acutifolium ....] XXI. 1 a—3. |) — Cutchense......| XXI. 4. | Lycopodites affinis ....+.+++ coal eas Os Sandstone, Clay Sonile of the Fucoides (Codites?) dichoto- MUS sroaccacenssors sqoceapeatce 2), DG Te Stems of LEquisetites or a Monocotyledonous Plant .| XX.1b, 6. |J ° with Coal. Charwar range. Poryraria. See a Lycophris Ephippium...... wae -15, |Nummulitic group. : a" (p. 300 Orbitolites.)| 15 a,b. ten rae Very abundant. AisPANsUS s+.e.000 XX a Os ilenaseeeue Wbidi is ede32 8 P : Rapraria. 16 a, b. ; c Crinoidal stems cecececscescves X XIII.14-16.| Upper Secondary |....... Charee....... moe on hills ears Chareesnen Echinus dubius ...-.esecceees «| XXIV. 18. | Nummulitic group] Baboa Hill, Wagé- mmonites and other fossils. ké-pudda. Galerites pulvinatus .....+00 XXIV. 19. |...... od LS ho soemcaca| Sead Baboa Hill Clypeaster affinis ? ......00000+ XXIV.20,20al......... Ubidiecesesss Ibid. and near Goldfuss, XLII. 6. Joongrea. ee UTILS asnovseieers NEXT Vi2 1 Qaleeecccas MbId Feces Ibid. and Wagé-ké- pudda. Found in great numbers, and simi- AePessus ...0.c0ee XXIV.26, 26al...... Tertiary ....0.|-..«esSOOMTOW:...+0- { lar in colour and form, to recent OLLONGUS...+2s2e000s 2-00 Ve Pp “|enodencne Dbidversosence Between Joongrea specimens, but flatter. Lamk. 25 a. and Kotra. Spatangus obliquatus .....++.. XXIV. 22, | Nummulitic group |..... Baboa Hill.....| Very numerous. S. Buckl.? Goldf., XLVdI.6.} 22 a,b. acuminatus? ....... DOIG PBI I bacanosea bide osc. pesleseesacer Ibid. Goldf., XLIV. 2.) 23 a—c. CLONGALUS ..e.s.000s 2.0.0 e725 | ceoceanoc L1G bHssoaenod Besoraode Ibid. ANNULATA. WerpuUla ? VECLA ...0rceareeees ers MOXOS Ura ss| see ee) LCLUALW seceselnaiss Near Kotra..... Bodies of similar form occur in vast Siliquaria Grantit. ..s...ceceefere DO. ia eer oorioon Tertiary ...... BordersoftheRunn.| quantities on isolated banks in Cirrirepa. the river near Kotra. Balanus subl@vis...ccccccseesee{ees PROXG Vii Gateec|aesiecnesell WlGuascesesos| atcred s,Soomrow. ConcHIFERA. Pholadomya ? inornata ..,...|... XXI. 8. ...|.. Upper Secondary..).... near Charee....} ] Found on some hills bordering the GTANOSA « v2.00.) eee OT 9. aol sas evciane MDidieeehcees| sensectee WoC b-soeseqse f Runn, which have been much ————_angulata......]... PROXGT TO Fes | rectsnie bid Geecmctecee see-as- Uy C be SRdoncon disturbed by volcanic action. Amphidesma? ovale « ....+.+++|e+ OR n Withee cell bedooaods Ubidssscesccsslececereus Ibid. TGS. cedpoooced aon D.C nana A bedoanana Ubideacceesees|eoes eelipide Corbula lyrata .....s.sececcseeefoes 2.0.4) 5 1B becd pecedaces USSG hccogasocn bosndscod Ibid. trigonalis ....++++++0+.). 5 oO. 4 dboncen AMEE goatee Borders oftheRunn. BUD OR Cp welaeisacantc as siess|: 5 2. Wo Ba6 dloccoon cell Ghcoccaketidloconcencs Ibid. HCHIRG CLONAL ssecesessscesse\ess OKAY Ge ocd joadaoncbo Mbideeescsdesclecse Soomrow. Astarte unilateralis ..........)e0 XXI. 14....|.. Upper Secondary..|...... Charee. DASULONMIS) 2c2sesesens| ++ XOX allo seas| sarees WG Loecoaqoddl boondeas Ibid. VENUS GANS sa... .c0seroecess[oss OOo hg cbq\oogan Tertiary ..... alpeewes Soomrow. CONCEAL ce ee veceess\ous BO, OAC aee loceoodoad II)9) G Beqacomond Beaood Ibid., Kotra. - MONSCEUDUG sctiacesssecesc|se 6 ON {35 ed lonn0ns06 bideeerercces|tecess Soomrow. Pullastra? virgata ......0000..\.0. OREO Gadi ee cancoos los ocaspancine| ecndcadae Ibid. Cardita intermedia? ......... oie OW 10h 6 |lane000500 8006 ngcconnod aocooocdn Ibid. Brocchi, XII. 15. 328 Class, Genus, and Species. Plate. Formation. Locality. Trigonia costatd, Var......+4\.+ XXI. 16....|.. Upper Secondary..|........Charee....... M.C., LAXXV. ——— — PUllUs sececeevecerees|oas XXI. 17....|. Upper + yaa Bae dose Charee. ...... Cardium intermedium ........|-- XXIV. 1....| Nummulitic group |..... Baboa Hill. - AMDIG“UUM ooseeeeeele 52.0.6 Wap 29 |raseeeaa Eid set ssi. tah tee Ibid - EUfOV ME. ac oecosceeee|-s 20.05 Se a JNeehai7 saneed nocd Soomrow. Cuculle@a virgata .s...ccecsees MED, Qe. "Upper Secondary..|.... Hubbye Hills... Arca hybrid ....ecseceeeecsee|ere XXIV. 3...,Nummulitic group.|..... Baboa Hill. FOOLED rc eseecoresss2se00]s 5 OO, US Absccans Mentianyo.scres|-eeces Soomrow. tortuosa? Linn.....+.+++|- 5 OR TGs dl Bo peccrceal lot RE cme Renae Ibid. Pectunculus pecten ......1.+++|-+ XXIV. 4...|Nummulitic group.|..... Baboa Hill. Nucula tenuistrata. .....0000/00 XXII. 3...|. Upper eG Wael A “-Hubbye Hills... ? cuneiformis...... ano.) li earl ee Abidsencaccene .. -Charee........ Baboensis ...sse+00++ "[...X XIV. 5...| Nummulitic group. =a0h0 Baboa Hill. Pecten partitus........+000+0-- XXII. 5, 5 a.|. Upper Secondary .|...Hubbye Hills. Le vicostatus ....++.+0+\++ XXIV. 6...| Nummulitic group. SOoMrowensis....++0+4|++- PRON As cnloaesess ertiarysccnsss|-ccee Soomrow. OP LICULALUS. .00ce+e00s\0 OKO eel Obst nae osne's DIG, os atse on Banks of the Runn. Plicatula pectinoides .........|... XXII. 6...|. Upper crim aad | - near Charee. IMCs | CCCGEK |. XOX. 9.4 ..|.0...000. bid: -esece ..Katrore Hill. be ae COMMCMiepensetesesenn less PROROIU i oca|senesosa Ibid. ....00...|scosnsene Ibid 5 iGig 2 C- QE OXON Cais globosa? Keodagsnoosad HAE ROKGVis Ge. 3|Seccc00l Cktiatysncssan wobsseseo MOOR. M. C., CCCXCLI. Ostrea Marshii...... dessteepee|sae XXII. 9...|. Upper Secondary . M.C., XLVIII. war range. COVINGED ® Jestonsacen.|eos XXII. 8...] Nummulitic group,]....... Charee. M. €., CCCLXV. —— callifera? .......0000.|e0 KORN SWE, ale vaesees bide <.ceens Wagé-ké-pudda. ... | Lamk. ——— or bicularisecc......0++|+++ XXIV. 8...|-.00e0ss Ibid. i. -oonseu{esnnes Luckput...... AN GUIAA wr eeeeeerssees|ere PRON VnaLZ aes|s yee ses Wenharyccescy:|steantes Kotra. ——— Flabellulum ......00)00 VES. 5 lose meee TCE Goapgace) osso ccc Cheeosir....... M. C., CCLIII. ——— tubiferd.......s.e0e00e Pee Ov cala ois wage Thid. J... ccex0 TINGUG ..reccveececcreee pee V5 20) salenans «sos UDIG. dear eean) ect near Joonagrea and Kotra. Terebratula intermedia, var.|.. XXI1 Upper Secondary .|...... Charee. M..C., XV. 8. — biplicata, var..|.. XXII. 11..}......... UDG. doce ves .. Jooria Hill. M.C.,XC.&CCCCXXXVII. sella, VAT.....006 PRON el Die clves neces Ibid..........| Pass of the Hubbye M. C., CCCCXXXVII. 1. Hills. concinna?.. Oe. @-4 E38 Receereeee Ibid..... ...Jooria Hill. M. C., LXXXIIL. 6. Bo ele PROS LAr afore vicinus Upid....<.<... . near Charee. . dimidiata?....s.++00+s 2.811 Sail) 54] bape Mbid: eeeeaeee M. C., CCLXXVIL. 5. major Peapogs oso -apeee ro MATT, 16. .|.oceeees. Did saeccscesslpaends Charee Motuusca, Bulla lignaria, Linn..........|-.-X XVI. 1...]-.-+0. MEL iAry:. .< Dertiary ......|s-eoes Soomrow. sometimes very large. Mitra scrobiculata? Brocchi.|..X XVI. 23..}......... Wpiditecesstanlesease nce Ibid. PUSsifOr MIs ....ccerceeeee 5 O15 07; Bancroceal lla ecesnocet Booooence Ibid Volta JUG OSA. ..+.essseecereees 5 OO Bind bpcconoe lll ci Lesgericaer|sasadcene pidvcces. 4.) neh ee eee 16 Total. .20 No. 94.—Wellat the entrance to the town. Feet. 1., Diluvial loamy sails os%.--<).- -.--- 1-00 @.. Crag'sand’: iad eae wei Tee Total. .50 and Phenomena of the County of Suffolk. 383 No. 95.—Well at Post-office, Woodbridge, (particulars burnt in the fire at Rendlesham House). Feet. Peeluwauni— (land Spring) 3.0... 56000 00s eee vs nee ce we PMR CANARIO SARE. eae yee) + By als eels «2s Giois wees a alee swe 40 aa \ be CO DOD CHO COE Eahoe oy CeO Ore Pip 210 4. Plastic clay SMO Nica Be Pa rcld Pe iar cl ory a1) vs en al as, of. #6 sheiew ea 6] ansve Flyers 150 Total. .660 Water stands at 29 feet from the surface ; it is very chalky and bad. There are 40 feet of copper pipe in the chalk. No. 96.—Well at Hemley, 4+ miles S. by E. from Woodbridge. Feet. PPO aS totet a ahire le oe. [oka aie cena wie fold @ ote chaele = a6 ava 8 deal ss 6 See MMM a se orig nc alchie safe Bae xtn. GIS, elaeh are’? eu ee pe senate 44 Total. .50 No. 97.—Well in Havergate Island, 8 miles S.E. from Woodbridge, (height of surface, 4 feet above low water mark of sea). Bt in: 1. London clay—blue clay, with usual rocky concretions... 80 0 CASE OG) od aha BCs Pre Hen de eeree bce © FO elc Sn oer earner 0 2 BPE EROLC] Cla ——— SSM, orale citi neil © wie yatcyalin(os\ + a. <'e ee'el 20 0 | Total..100 2 N.B. The slope of the plastic clay, from Harwich to Havergate, gives about 5 feet in a mile; which agrees with the computed slopes of the chalk (see Nos. 16 and 18) the average of which is 5 feet; proving the original conformability of the beds. The distances and bearings are calculated from the Ordnance maps. P.S. Since the above memoranda were committed to the press, I have been informed that cement stones have been found in great abundance at Assington, near Sudbury ; but whether they belong to the beds of the Lon- don clay, or are drift septaria from the diluvial clay, I do not know. If the former, Layham (p. 362) is not the most westerly point of that formation, The statement requires authentication. WBC: Stanley Green, near Poole, 20th October, 1838. | 4 his hi i Nid eqriys Teg Wh hi ide eae and ae “a anh i Chi TD ata i mn / Be aA bent, fri They: ahs ant Bi ' [ 385 ] X XIX.—On the Geology of the Thracian Bosphorus. By HUGH EDWIN STRICKLAND, Ksg., F.G.S. {Read November 30, 1836. ] DURING a short residence at Constantinople, in March 1836, I made some researches into the geology of its vicinity. A very cursory examination suf- ficed to show, that the district was unexplored, and that the brief geological remarks, which exist in the works of other travellers, are very unsatisfactory. I therefore communicate my observations to the Society, m the hope that, though slight, they may serve as a guide to those geologists who may here- after be induced to explore this interesting district*. The formations in the neighbourhood of the Bosphorus may be classed as follows :— 1. Silurian schist and limestone. 2. Igneous rocks. 3. Tertiary limestone. 4, Ancient alluvium. 1. Stlurian Schist and Limestone. This formation occupies both sides of the Bosphorus for about three quar- ters of its length, and extends thence towards the W.N.W. and E.S.E., to an unascertained distance in Europe and Asia. It may probably form a great part of the Balcan range, of which the hills above the Bosphorus are a con- tinuation. Section west coast of the Bosphorus from the Sea of Marmora to the Euxine, 2 a a 2 ) a wo iS aS 4 5 5 3 5 S 2 s &9 3 P 42 Z > : S a = a a. a a os ry a f=} & ro = = 2 = a =| ° o Lt o Gy 3 > iS) Ay < [=<] Q FQ an Se pt , : Suge ee Tertiary Silurian Schists and a Lime- @ stones. gs Trachyte and Tufaceous conglomerate. Limestone. mal = S uo) uo) - =) o 2 & E a a & (>) oO 5 a a * These observations were made in company with Mr. Hamilton; but that gentleman being still on his travels, I have been deprived of his direct assistance in drawing up this paper. 386 H. E. Stricxxanp, Esq., on the Geology The formation may be described as a mass of argillaceous schist, compact brown sandstone, and compact dark blue limestone, passing into each other by insensible gradations. The argillaceous schist predominates greatly over the other two rocks, and frequently exhibits an oblique or slaty cleavage. The whole formation bears a close analogy to the lower Silurian and upper Cambrian series, exhibited in Wales and Devonshire. From its resemblance to the type of northern Europe, Andreossy* and an American traveller+ re- ferred it to the transition series on mineralogical grounds alone; and this opinion is now confirmed by the discovery of organic remains, analogous to those of the Silurian rocks of Britain. This fact is interesting, from the ex- treme rarity of fossils in deposits of this early age in the southern parts of Europe. The stratification of these rocks is in general much disturbed and con- torted ; and in other cases it is very obscure and difficult to detect. Hence it would require a closer examination than I was able to give, to establish the prevailing strike of the formation. Organic remains appear to be extremely local, and were noticed in only two localities. The first of these is in the ravine above Arnaout-keui, a vil- lage about four miles from Pera, on the European side. The rock is an argillo- calcareous schist, splitting at an angle, oblique to the stratification. Impres- sions of various Brachiopoda and joints of Crinoidee occur in it, lying in the planes of stratification. The substance of the shells has perished, leaving a brown dust; and the casts are in general much distorted by the compression and consolidation of the strata. These remains were first noticed by M. Fontanier{, who mistook the shells for Pectines, and thence inferred that this was a secondary formation. Had he examined them with more care, he would probably have agreed with M. Andreossy, who, without the assistance of organic remains, referred these rocks, as already stated, to the transition era. The only other locality, where organic remains were seen, is on the hill called the Giant’s Mountain, on the Asiatic side of the Bosphorus, about fifteen miles from Constantinople. It is singular that of three authors (Andreossy, Fontanier, and the author of “ Sketches of Turkey’’), who have noticed with more or less exactness the geology of this hill, not one has remarked the nu- merous and interesting fossils which occur there. The lower part of the hill consists of compact limestone, thickly bedded, of * Memoire sur le Bosphore. 8vo. Paris. + Sketches of Turkey, by an American. New York. 8vo. 1833. * Voyage en Asie Mineure. Paris. 8vo. of the Thracian Bosphorus. 387 a dark grey colour, and slightly crystalline. It is exposed in extensive quar- ries, where it is traversed by some remarkable trap-dikes, to be mentioned hereafter. Organic remains are rare in the limestone; but I detected a few impressions of Terebratulz and crinoidal stems, exhibiting the same crystal- line fracture, which distinguishes them in the carboniferous and other lime- stones of England. Above the limestone is an argillaceous schist, with an oblique cleavage, and it extends to the summit of the hill. Impressions of shells, similar to those of Arnaout-keui, occur in it in many places, and in tolerable abundance. I have found only one specimen, which can be referred to the family of Trilo- bites. Itis a small fragment, but it so accurately exhibits the structure of the eye of an Asaphus, that I have no hesitation in referring it to that genus. The following is a list of the fossils of this formation, as far as the imper- fection of the specimens admits of identification. I am indebted to Mr. Murchison and Mr. James De Carl Sowerby for assistance in determining these fossils. Brachiopoda. . Spirifer.—Allied to Spirifer speciosus, Bronn. Leth. Geog. II. 15. . Spirifer——An undetermined species. . Producta (Leptoena) sericea? . Producta (Lepteena) euglypha? Dalm. . Producta (Leptcena).—New species. . Terebratula affinis, Min. Con.—In the Upper Silurian series of Great Britain. . Terebratula unguis ?—In the Caradoc sandstone of Great Britain. . Atrypa.—-An undetermined species. moanrta a - ow wo & . Orthis.—New species. — oO . Orthis.—New species. Crustacea. 11. Asaphus.—Eye like that in Buckland’s Bridgewater Treatise, pl. XLV. fig. 10’. Crinoidea. 12. Detached joints of undetermined genera. Polyparia. 13, Cyathophyllum, Goldf. 14. Favosites, Lam.—Similar to one in the Cambrian rocks. Should any geologist ever devote that share of time and attention to this country, which it well deserves, he would probably find several other localities VOL. V.—SECOND SERIES. 3 E PCa eee ie St Re en ere ee ee ee Ste 388 H. E. Srrickxxanp, Esq., on the Geology for these Silurian fossils, and perhaps be rewarded by the discovery of many Trilobites and other organic remains, which I did not meet with. The compact limestone of this formation is quarried in several places near the Bosphorus, especially at Baltalimani, where it dips to the westward. In the lower part the strata are thick, but they become thinner upwards, and, after assuming a concretionary structure, pass into argillaceous schist. The limestone exhibits some very obscure traces of organic remains. The sandstones are best exhibited in the cliff between Scutari and Monda- bornou. They are brown, commonly compact, sometimes schistose, and the stratification is distinct, being much broken and distorted. The evidence of the organic remains justifies me in referring the forma- tion to the Silurian system of Britain. The occurrence in this remote locality of rocks, which approach so closely to the type of north-western Europe, is somewhat remarkable ; and the more so, as nothing of the kind occurs, as far as I know, in the more southern parts of Asia Minor, or in any portion of the Mediterranean basin. Many geologists are of opinion, that the transition and secondary rocks of northern Europe belong to a different type from those of the Mediterranean basin; and that the characters, both mineral and zoo- logical, of these two parallel series present scarcely any common points of comparison. A line, nearly coinciding with the Pyrenees and Alps, appears to divide these two great basins, if we may so term them. Further investiga- tions may perhaps show, that this line admits of being continued from the Alps through European Turkey to the range of the Mysian and Bithynian Olym- pus; and this may explain the appearance at Constantinople of rocks be- longing to the type of northern Europe, which are wanting further south in Asia Minor. The transition formations, which we have been considering, unite on the north to a mass of igneous rocks, and on the south-west to tertiary deposits. At present, | have no clue to the relative age of the two latter, but as the ig- neous rocks are in more immediate relation with the Silurian group, I will notice them next. 2. Igneous Rocks. The igneous rocks of the Bosphorus may be described, in the aggregate, as consisting of trachyte and trachytic conglomerate. On the Asiatic side they commence, en masse, at Kavak under the old Genoese castle, and extend thence to Yoom-bornou on the Black Sea, or perhaps further. They consist chiefly of angular trachytic fragments, imbedded in a tufaceous paste. The conglomerates, viewed on the large scale, are distinctly stratified ; and of the Thracian Bosphorus. 389 from Kavak to Anadoli-fanar they have a regular inclination towards the north. They rest upon, or alternate with, trachytic rocks, more or less compact, and occasionally passing into phonolite and basalt. In some places, especially near Anadoli-fanar, dikes of the latter substance intersect the conglomerate beds. The basalt occasionally assumes a columnar form, which is seen in the greatest perfection at Yoom-bornou. The prevailing colour of these rocks is greenish, owing to the presence of copper, a circumstance which gave the name of Cyanez to the weather-beaten rocks of the Symplegades. Near Filbornou the conglomerate contains bowlders of a brownish trachyte, softer than the greenish trachytic paste which envelopes them; hence they decompose with the weather, and give a honey-combed appearance to the rock. The contrary, however, is more often the case, when the imbedded fragments, being harder than their matrix, project above the general surface of the rocks. These igneous formations contain many veins of red and white cornelian, and varieties of chalcedony. In one place near Filbornou the veins are perpen- dicular and straight, intersecting the conglomerate, and cutting indiscrimi- nately through the tufaceous paste and the imbedded fragments——See the accompanying wood-cut. a,a, Angular trachytic fragments imbedded in a tufaceous paste. 6, 6, Veins of chalcedony traversing both the fragments and the paste. The deposition of these conglomerates appears to have been effected with the assistance, if not solely by, water. The fragments imbedded in them, though commonly angular, are sometimes rounded, and are contained in finely laminated strata of volcanic sand. An instance of this, on the north side of Anadoli-fanar, is represented in the following wood-cut. 3E2 390 H. E. Srrickianp, Esq., on the Geology Section north side of Anadoli-fanar. Lighthouse. Trachyte. a, a, Caves. On the European side of the Bosphorus, the igneous rocks commence on the north of Buyukderé. Here a species of trachyte of a yellow colour forms some considerable hills. It is much decomposed, and resembles loose sand, when viewed at a distance. Further north is a series of conglomerate beds, similar to those of the Asiatic side, and extending to the Black Sea. These are the general features of the mass of igneous rocks, which abuts against the northern flank of the Silurian schists above described. The works of MM. Andreossy and Fontanier contain some information on their mineral contents. A variety of trachytic and trap dikes occur in the Silurian schists, and are doubtless connected with the general mass of igneous formations. At Balta- limani and on the hills above Bebek, a ferruginous decomposing trachyte ap- pears in the midst of the schistose rocks. At Kiretch-bornou is a dike of fine- grained greenish trap, about 15 feet in thickness, cutting through strata of calcareous and argillaceous schist. A similar dyke occurs in the limestone quarries at the base of the Giant’s Mountain. It is perpendicular, 4 or 5 feet thick, and from the removal of the limestone on each side, it resembles a wall running across the quarry. Some fragments of limestone occur in the midst of the trap, but neither they nor the rock on each side of the dike, show any signs of alteration. Lower down in the quarry, near the level of the Bosphorus, are some masses of greenish and white quartz rock, which have more the appearance of an altered sandstone than of an igneous injected rock. 3. Tertiary Formation. This formation commences immediately on the west of Constantinople, and extends along the north coast of the sea of Marmora for many miles, its western limit being at present undetermined. On the west side of Constanti- nople the formation ranges inland for about three miles, till it meets the trans- ition series, but the nature of the junction is not exposed by any section, which I could meet with. The beds are best exhibited in the quarries at Baloukli and Makri-keui ; where they consist of soft white shelly limestones and marls, resting on sand of the Thracian Bosphorus. 391 without fossils. The stratification is in general horizontal, a character com- mon to nearly all the tertiary formations, which I saw in Turkey. That portion of this deposit which occurs near Constantinople appears to have been accumulated in an estuary. The most abundant shell isan oval, sub- triangular bivalve, apparently a Mactra, which composes almost the entire substance of some of the beds; there is also a ribbed bivalve resembling a Cardium. ‘These are apparently the only fossils which belonged to marine genera, all the rest having been natives either of the land or of fresh water. Potamides, 1 species. Bulinus, resembling B. montanus. Neritina, 1 species, the delicate black stripes , similar to B. acutus. remaining. Clausilia, 1 species. Cyclostoma, 1 species. Pupa, | species. Helix, a species like H. pomatia. Planorbis, like P. alba. —, a species resembling H. rufescens. Cypris, 1 species. The terrestrial shells are remarkable for their near approach to existing forms. They are less generally diffused than the marine and fresh-water species, but are abundant in the quarries at Makri-keui. A single specimen of a bone occurred in this formation, but it is too im-_ perfect for me to decide, whether it belongs to a mammifer or to a reptile. I found no traces of a tertiary deposit along the banks of the Bosphorus, whence it may be inferred that this channel has been opened at a compara- tively late period. ‘Tertiary beds are said to exist along the shores of the Euxine; and lignite has been worked for fuel at Domouz-deri, a few miles west of the Bosphorus. A. Ancient Alluvium. A few miles north of Constantinople are some extensive deposits of clay, sand, and gravel, reposing on the Silurian schist. The latter formation is barren and devoid of trees, but the alluvial clay favours the growth of the oak and causes the forest of Belgrade. These deposits are of great thick- ness and consist chiefly of ferruginous clay, with pebbles and bowlders of quartzose and sandstone rocks interspersed. The general want of stratifi- cation and the rounded form of the bowlders, denote an aqueous action of considerable violence. ‘These accumulations of detritus appear to skirt the southern side of the Lesser Balcan range towards the N.W. Taken as a whole, the deposits bear a close analogy to those which in Eng- land have been called diluvium ; and they appear to have resulted from causes acting on a greater scale than any of those, which produced the local alluvia, noticed by me in Asia Minor. November, 1836. ees ag XXX.—On the Geology of the Neighbourhood of Smyrna. By HUGH EDWIN STRICKLAND, Ese., F.G.S. [Read April 5th, 1837. ] THE vicinity of Smyrna presents geological phenomena of considerable in- terest, and of a more complicated kind than is usual in Asia Minor. A resi- dence there during the winter of 1835-36 enabled Mr. Hamilton and myself to investigate this district with greater attention, than we could bestow upon the other parts of Asia Minor, which we visited ; and its geology may, there- fore, deserve to be laid before the Society in a separate communication. The details of the paper can be understood only by reference to the accom- panying map, Pl. XX XII., and by a general description of the geographical features of the district. The Bay of Smyrna and the alluvial plain at its upper end lie between two parallel ridges of high land, ranging from east to west. That on the north commences with the lofty hill of Sipylus, rising abruptly from the plain of Sardis; and this ridge, which separates the waters of the Hermus from the Bay of Smyrna, terminates at Menimen near the estuary of that river, the western part being known by the name of Cordileon. Its total length is about thirty-two miles. The ridge on the south side of Smyrna Bay, begins with Mount Tartali, the ancient Mastusia, which is the western termination of the T'molus range. Descending towards the west it passes into the table-land which overhangs Smyrna on the south. Further west the country again rises and forms the group of conical mountains, anciently called Corax, which terminates at the Isthmus of Vourla. The distance from Mount Tartali to Vourla is about twenty-four miles. These two lofty ranges are united at the Pass of Cavakluderé by a trans- verse ridge, which separates the Vale of Nimphi from that of Smyrna, and completely isolates the latter. The rocks in the vicinity of Smyrna belong to the following formations :— 1, Micaceous schist and marble. 2. Hippurite limestone and greenish schist. 3. Tertiary lacustrine limestone and marl. 4. Trachytic rocks. 394 H. E. Strickianp, Esq., on the Geology The general features of these and the other formations of Asia Minor were explained in a paper laid before the Society on November 2, 1836 *. In the Smyrna district, the mountains of the hippurite limestone formation apparently once contributed to form the boundary of a great lake, in which calcareous matter was deposited to the depth of many hundred feet. Two vast eruptions of igneous matter have since taken place, one on the north, the other on the south of the present Bay of Smyrna. These convulsions pro- duced great changes in the form of the surface, and in the arrangement of pre-existing rocks, and the study of this district is thus rendered both interest- ing and difficult. As the phenomena exhibited on the north of the Bay of Smyrna are not visibly connected with those on the south side, it will be best to consider each portion of the district separately. I will begin with the southern side, and take the formations in the order of age. 1. The micaceous schist and saccharine marble, which compose the ridge of Mount Tmolus, terminate near the village of Trianda, and form part of the eastern boundary of the lacustrine formation. The micaceous schists of Asia Minor being fully described in the memoir before alluded to, it is needless to repeat their characters in this paper. 2. The compact gray limestone with Hippurites is, in this district, asso- ciated with an abundance of compact sandstone and schist, of black, greenish, or cream-coloured hues. The whole formation has been so greatly disturbed, that it is difficult to determine, whether the sandstone and schists were depo- sited above or beneath the limestone ; but their union with it is too intimate to admit of their being regarded as a distinct formation. They seem analo- gous to the greenish sandstones of the Morea and the macignos of Tuscany and ‘Trieste, all of which have been referred to the cretaceous system. The western boundary of the hippurite limestone of Mount Tartali is at the village of Cucklujah, whence it extends eastward for perhaps fifteen or twenty miles, along the northern declivity of Mount Tmolus. Further details re- specting it at this locality will be found in the memoir alluded to. The range of Mount Corax consists almost entirely of sandstones and shales, but at one point, about 34 miles west of Smyrna, a small mass of gray lime- stone is exposed, and serves to identify these rocks with those of Mount Tartali. Around the village of Baltchikeui the shales are of a pale cream colour, soft and friable, and contain a considerable admixture of sand, which is sometimes so coarse as to become a conglomerate of fragments of quartz, a quarter of an inch in diameter. * See Proceedings of the Ge o logical Society, vol. ii. p. 423. a | of the Neighbourhood of Smyrna. 395 About 13 mile beyond Baltchikeui is a thermal spring, on the site of a temple to Apollo mentioned by Strabo. In the ravine immediately above it, the beds of shale are dark-coloured and compact, dipping thirty or forty degrees to the northward*. 3. Tertiary lacustrine limestone. This deposit forms an extensive table-land, ranging southward from Smyrna for about fifteen miles. On the east it abuts unconformably against the hippu- rite limestone of Tartali and the micaceous schist of Tmolus, and on the west it is bordered by the range of Mount Corax. The southern boundary is near Trianda, where the formation rises above the alluvial plain of Tourbali; but the original barriers of the lake on that side are not now apparent. This area is occupied principally by white or yellowish limestone, varying in texture from lithographic stone to soft chalk. The more compact beds closely resemble the secondary limestones of the Ionian Islands, and like them contain nodules and layers of black flint and quartz resinite. From this resemblance we were at first inclined to refer the compact limestone near Smyrna to the secondary series, but after a close search Mr. Hamilton and myself succeeded in finding Jacustrine shells (see p. 402) which indicate a tertiary epoch. The flints and quartz resinite exhibit an analogy to those in the lacustrine deposits of Au- vergne and of the Cantal, as described by Mr. Lyell and Mr. Murchison f. White and greenish marls are often interstratified with the limestone, and are most abundant in the central parts of the area between Boudjah and Sedikeui. About twe miles north-east of the latter place the marls contain traces of vegetable remains, and are accompanied by extensive beds of gravel, which both alternate with and overlie them. ‘These gravel beds much re- semble the ancient drift or alluvium of England, but are merely a local portion of the lacustrine deposit. They contain rolled pebbles of nummulitic limestone and schist, derived from the surrounding mountains, also fragments of red trachyte similar to that which occurs, en masse, near Smyrna. As is usual with the lacustrine basins of Asia Minor, the beds of limestone and marl pass into conglomerate as they approach the foot of the surrounding mountains. The southern boundary of this formation near Trianda consists almost wholly of gravel imbedded in yellow clay. The pebbles of trachyte, in the central parts of the formation, appear to prove that, at this point, the lacustrine deposits were continued after the erup- tion of trachyte, which overlies them near Smyrna. The bed of the lake being probably lowest in the centre, water might lodge there, after the main body * The author of “Sketches of Turkey ” calls them limestone rocks, but on the application of acid not the slightest effervescence takes place. + Annales des Sciences Naturelles, 1828. VOL. V.—SECOND SERIES. 3F ee aeneneaad SSS SSS Se 396 H. E. Srricxianp, Esq., on the Geology of the lake had been drained by the igneous eruption ; and streams flowing from all sides would carry to this point the pebbles which, during the quiescent state of the lake, formed a shingle beach around its margin. In course of time the denudation of the outlet would complete the work of desiccation, and the whole drainage, of what is now the Plain of Sedikeui, would reach the sea by the ravine at present traversed by the Meles. That all these operations have taken place, will, I think, be evident to any one, who will make a careful survey of the locality. The stratification of the lacustrine series is, in general, nearly horizontal ; some local exceptions, however, exist in the vicinity of the igneous rocks. 4, Trachytic rocks. The greater part of the lacustrine series had been deposited, when the basin of Smyrna became the seat of volcanic action ; and an enormous mass of tra- chytic matter was poured forth, and spread over the bed of the lake. The eruption appears to have ceased as suddenly as it began, for there are no al- ternations of trachytic and lacustrine rocks,—no injection of dykes, or other phenomena, which indicate a long continuance of igneous action. These rocks occupy a surface of about five miles by two, and a reddish- brown, porphyritic variety prevails throughout nearly the whole area. A remarkable feature in the trachyte is the close approach, which it occasionally makes to a stratified structure. It splits into slabs from a foot to an inch in thickness, and their cross section exhibits stripes of various colours, parallel to the planes of cleavage. These strata (if they may be so called) are in some places accumulated to the thickness of one hundred feet, and are traceable laterally for as many yards. This is especially the case on the hills about two miles west of Smyrna. The crystalline texture of this stratified trachyte de- cidedly indicates igneous fusion, and the explanation of this peculiar structure is, therefore, by no means easy. It may, however, be conjectured, that when the fluid trachyte expanded horizontally from the point of eruption, any vari- ations of substance or texture would be drawn out and extended in planes parallel to the horizon, and when cooled would cause coloured stripes and fissures in the rock, in the direction of those planes. It must, however, be observed that the apparent strata are now far removed from the horizontal position, supposing them to have once occupied it. These trachytic rocks are, in general, homogeneous, but in some places, they contain numerous angular blocks and fragments of black porphyritic trachyte, much harder than the reddish paste in which they are imbedded. This species of conglomerate is well developed, about 2 miles west of Smyrna, in a ravine near the sea. On the north side the trachytic rocks descend to the shore, but along their a of the Neighbourhood of Smyrna. 397 southern border, they overlie the lacustrine limestone and marl of the Plain of Sedikeui. The boundary of the two formations is well defined, the trachyte terminating abruptly, with a steep slope, like the margin of a modern lava coulée. A stratum of pumiceous tufa is commonly interposed, between the trachyte and the lacustrine strata. ‘The uppermost bed of the latter is a con- glomerate of rounded pebbles of quartz, hippurite limestone, and schist, but not the least trace of any igneous rock is discoverable in it. Beneath this bed are calcareous marls, containing Planorbes and other fresh-water eae and passing downwards into white limestone. The absence of igneous products in the conglomerate proves the sudden eruption of the trachyte which reposes on it ; yet it is possible that this bed of transported pebbles may be connected with that event. Earthquakes pre- ceding the eruption may have caused currents in the lake, which would wash these rolled pebbles from its gravelly margin into its central parts, and termi- nate that long period of repose, during which the subjacent marls and lime- stones were deposited. The highest point attained by the trachyte is about 3 miles S.W. from Smyrna, near the valley which separates these rocks from the Corax range. The view from this eminence proves how much the picturesque and botanical features of a country depend on its geology. On the south is the vast, undu- lating plain of lacustrine limestone and marl, the greater part of which is cultivated and interspersed with villages. On the west, the decomposing sand- stone and shale of Corax form a cluster of conical mountains thickly covered by evergreen shrubs. Jn the east, the view is terminated by Mount Tartali, where the compact gray hippurite limestone forms crags and precipices, with fir and other trees sparingly scattered among them. Lastly, the trachytic rocks in the foreground produce neither trees nor shrubs, but present innu- merable masses of naked rock, jutting through a fine green turf, adapted only for pasturage. Having now given a general sketch of the sedimentary and volcanic rocks which occur near Smyrna, I will introduce a more detailed account of Mount Pagus, where several of them are brought to view within a very small space. (Plate XX XII., Sec. Nos. i and 2.) The hill anciently called Pagus rises immediately to the south of the mo- dern town of Smyrna. It forms the north-eastern extremity of the mass of trachytic rocks above described; and a deep ravine separates it on the east and south from the plateau of lacustrine deposits, whose drainage produces the classic river Meles, which escapes into the sea through this ravine. The height of Mount Pagus may be estimated at about 500 feet. It is principally composed of trachyte and trachytic conglomerate, which on the 3F2 398 H. E. Srricxxanp, Esq., on the Geology east and south extend from the summit to the bed of the Meles ; but along the northern declivity they terminate about half-way down, and repose on strata of the lacustrine series. The uppermost of these freshwater beds is here, as elsewhere, a conglomerate of gray limestone, schist, and quartz, in rolled fragments. It passes downwards into beds of sand which may be traced by means of ravines and sandpits for a depth of more than 100 feet, till the houses of Smyrna preclude further search. At the lowest visible point, the sand con- tains abundant impressions of leaves; also, though more rarely, imperfect shells of Helix and Unio, which identify it with the lacustrine formation. It is remarkable that these beds of sand and conglomerate dip about 20° éo- wards the trachyte of Mount Pagus, which, having been erupted subsequently to their deposition, might be expected to have heaved them in an opposite di- rection. They are clearly not overturned, because the conglomerate of lime- stone pebbles is here in its regular position, on the top of the other lacustrine strata. At the north-eastern side of the hill, the sand is replaced by beds of marl and white limestone containing Planorbes; and above them is the never-failing conglomerate, extending under the trachyte. (See Pl. XX-XII., Sec. No. 1.) A few yards lower down, at the foot of the hill near the Caravan bridge, we come unexpectedly upon a rugged mass of rocks belonging to the hippu- rite limestone formation. Its whole area does not much exceed an acre, and we must suppose that it has been brought up by some convulsion, connected with the outbursts of trachyte in the vicinity. It consists of friable, marly, cream-coloured shale, similar to that at Baltchikeui, and it contains veins of crystalline carbonate of lime, and some masses of a hard, yellowish, calcareo-siliceous stone. The stratification is very obscure, but as far as it could be determined, it dips towards Mount Pagus, conformably with the lacustrine marls, a few yards higher up. These friable schists are extensively quarried, and when broken small are used in Smyrna for garden walks and terraced roofs. On the east side of the schist are some irregular masses of compact, gray limestone, similar to that which, in Mount Tartali, contains Hippurites ; and they identify the whole of these dislocated rocks with that formation. About half a mile N.E. of this point, ts a small, isolated hillock of trachyte, the elevation of which may have caused the otherwise anomalous dip of the lacustrine strata, on the N. and N.E. sides of Mount Pagus. (See Section 3.) The right bank of the Meles, opposite Mount Pagus, presents an escarp- ment of the lacustrine formation. (See Section 2.) The trachytic rocks on this side are of small extent, but rise, in one place, about half-way up the south side of the ravine, and appear to abut against the edges of the lacus- of the Neighbourhood of Smyrna. 399 trine strata, which form the upper portion of the hill. The highest stratum exposed, is a compact white limestone, containing, though rarely, a small species of Paludina. A singular substance is also found here, being an aggre- gate of coarse crystals of carbonate of lime, but too loosely united to constitute saccharine marble*. Below the limestone containing Paludinz, strata of marl with calcareous nodules are exposed, till they are obscured by the trachyte below. The only alteration apparent in the lacustrine strata, from their contact with the igneous rock, consists in a greenish colour imparted to the marl, limestone, and ac- companying flint or resinite, and not observable at a distance from it. In descending from this point to the ford through the Meles, a singular mass of conglomerate is found in the midst of the trachyte. It consists of rolled quartz pebbles, imbedded partly in a red and partly in a bright green paste. This mass, which is but a few feet in extent, seems to have been derived from the subjacent lacustrine beds, and caught up by the trachyte. Near this point, the latter rock contains some veins of white chalcedony. We now proceed to the geology of the north side of Smyrna Bay, where phenomena are exhibited similar to those, which are described above. The gray limestone of Mount Sipylus seems to have formed part of the northern margin of that ancient lake, which was bounded on the east by Mount Tartali, and on the west by Corax ; as lacustrine strata still flank the south side of Mount Sipylus ; and they probably once extended across the alluvial plain from Bournabat to Cucklujah. Whether that extensive vale has been formed by denudation or by subsidence is uncertain, but its origin is probably con- nected with the igneous action, which has convulsed the district. A vast eruption of trachytic matter, apparently contemporary with that near Smyrna, has on this side also broken up and overlaid the lacustrine deposits. It forms the western half of the Sipylus range, called Cordileon, a mountain whose height may be estimated at about 2000 feet above the sea. §. 1. The eastern part of Sipylus consists of compact gray limestone, rising precipitously from the plain of the Hermus. Further westward, the limestone is accompanied by black and greenish shales, resembling those of Tartali, be- fore mentioned. ‘The boundary between this formation and the trachytic rocks coincides in general with the ravine, which descends from the lake of Kizghioul to Bournabat, but considerable intermixture of these two rocks occurs along the line of junction. * Strata of the same substance are seen in ascending by the easternmost road from Smyrna to Boudjah. 400 H. E. Srricktann, Esq., on the Geology §. 2. The lacustrine beds repose against the southern slope of Mount Si- pylus, from Djaki-keui, in the Vale of Nimphi, to Bournabat, where they are covered up by the trachytic rocks. The most interesting sections of them are on the west side of the ravine, about half a mile north of Bournabat ; and the right bank of the torrent here exhibits the phenomena shown in section4. A small outburst of red trachyte has heaved up strata of white and greenish mar], containing concretionary masses of brown, hard, crystalline limestone. Some of these masses are thickly perforated with sinuous tubes, and resemble tra- vertin formed around reeds ; yet it is doubtful whether the tubes originated in any organic body. Above these strata is a succession of whitish calcareous marls, extending about 200 yards to the northward, and dipping 35° N. In one place, a thin bed of brown clay is interposed, and contains fragments of shells and vegetables. The upper part of these marly beds affords a rich mine to the student in fossil botany ; some of the strata being crowded with leaves and other portions of plants, perfectly preserved. The substance of the leaves commonly remains ofa ferruginous colour, and contrasts beautifully with the pale cream-coloured matrix. The leaves belong to about twelve species of trees ; and some of them appear referable to the genera Laurus, Neriwm, Olea, Salix, Quercus, and Tamarix, all which still flourish in Asia Minor ; but it is yet undetermined, whether any of them are identical with existing species. These fossil vegetable remains are accompanied by shells of the genera Cyclas, Paludina, Planorbis, and Cypris. Lacustrine marls occupy the west side of the ravine, to the height of per- haps 150 feet above the spot, where the fossil plants occur. Their junction with the overlying igneous rocks affords the following interesting series of beds. (See also Plate X XXII., Section No. 1 and 3.) 1. Brown porphyritic trachyte capping the hill, and continuous with that which forms the mountain of Cordileon. we Alternating beds of tufaceous conglomerate and sand, regularly stratified, and resembling the conglomerate of Mount Perier, near Issoire, in France, except that the trachytic fragments are less rolled—30 or 40 feet. 3. Tufa, with numerous fragments of decomposed pumice, 8 or 10 feet. 4. Beds of rolled pebbles, from the size of an egg downwards, of gray limestone, quartz, and schist, but no igneous substances ; and similar to the conglomerate which underlies the trachyte on the south side of Smyrna Bay—20 to 30 feet. or White and yellow marls, containing, towards the upper part, Planorbis, Lymnea, Paludina, and Cyclas. ‘They extend downwards to the bed of the torrent. All the strata, from No. 2 to 5 inclusive, are conformable, and dip about 20°'S. W. of the Neighbourhood of Smyrna. 401 §. 3. Trachytic Rocks——These extend westward from the torrent of Bournabat to the mouth of the Hermus, and compose, as before stated, the whole mountain of Cordileon. The prevailing rock is a reddish brown tra chyte, identical with that of Smyrna, and, like it, is occasionally divided into lamin resembling strata. The junction of these rocks with the lacustrine beds near Bournabat, is al- ready described. In following up the ravine to the lakes of Kizghioul and Karaghioul, several varieties of trachyte and tufaceous rocks occur along the junction of the hippurite limestone and schist. At the lake of Kizghioul, a branch from the igneous rocks extends to the eastward for some distance. The Section, No. 5., Plate XX XII., is here exposed. About four miles further west, immediately opposite Smyrna, (see Map) a long, narrow ridge descends the side of Cordileon, and divides the waters of two torrents. ‘The composition of this ridge differs greatly from that of the brown trachyte of the surrounding hills. It consists of decomposing felspar, principally of a white or yellow colour, yet it presents also various shades of red and brown. Jt has a soapy feel, and would perhaps be a valuable material for pottery. At the upper end of the ridge, near a village, is a steep, broken escarpment, where some dikes of bluish and reddish trachyte penetrate the light-coloured substance, above described. The soft, decomposing state of this rock has given that smooth, rounded form to the ridge which so strongly contrasts it with the rugged neighbour- ing hills. Its surface is covered with rounded, erratic bowlders of brown tra- chyte, probably brought down by the torrents, which now flow on each side of the ridge, at a time when they occupied a higher level. From an inspection of hand specimens, it would not be easy to decide, whe- ther this white earthy trachyte has been altered since its ejection, or whether it was originally poured forth in a different state from the ordinary brown tra- chyte. The latter opinion, however, is the most probable, if we consider first, the complete dissimilarity between this rock and those which imme- diately surround it; and secondly, the manner in which this long ridge de- scends, like a coulée, from the higher parts of Cordileon. These are the principal phenomena which I noticed on the north side of the Bay of Smyrna; and it will be seen that they present a great analogy to those on the south. The geological events to be inferred from the facts described in this paper, may be summed up as foliows :— 1. An elevation of several mountains, composed of rocks of the cretaceous age. 402 H. E. Srricktanp, Esq., on the Geology of Smyrna. 2. A long and tranquil deposition of lacustrine matter, with shells and vege- tables, in a depression between these mountains. 3. A sudden eruption, at two principal points, of igneous matter, which broke up and overlaid the deposits of the lake, and drained the greater part of its waters. It seems to have been preceded by a commotion in the lake, spreading non-volcanic pebbles over the bottom. 4. A more or less sudden cessation of the igneous action, proved positively by the homogeneous character of the erupted rocks, and negatively by the general absence of injected dikes, or of alternate coulées of trachyte, tufa, &c., such as are seen in Mont D’Or. 5. A continuance of aqueous deposition in the central and lowest point of the lake after the igneous eruption, proved by beds of marl, alternating with gravel, containing trachytic pebbles. 6. The drainage of this remnant of the lake by the denudation of its outlet, now traversed by the Meles. List of Fossil Shells noticed in the Lacustrine Basin of Smyrna. SPECIES. Locatities. 1. Helix, similar to H. carthusiana, Drap. ..North side of Mount Pagus. i b B bat. 2. Planorbis, similar to P. alba. .......- es nie ani a if : A point about 4 miles S.W. of Smyrna. . Lymnea, resembling the recent L. pe- (N.E. side of Mount Pagus. WEPIM Episivs vives cescre sccncsensne Ravine above Bournabat. is) i ‘sacred ies, li 4, Paludina, a small turrited species, like Wie wide of Mond Baoan, South side of the Meles, towards Boudjah. Ravine above Bournabat, in company with {xin above Bournabat. RREMKECENMCEs: CRED ..0s 0.0 0s. ole ose wie 1 on hee C. Amelia |: 5. Cyclas, a small species, like C. pusilla 4 vGieble Saaeeeian 6. Uniden Ovate Species... ,......eccce008 N. side of Mount Pagus. 7. Cypris cvecvcsccccccsecscesecsevcces Ravine above Bournabat. The specimens of those fossils, which were obtained, are not sufficiently perfect to warrant a greater degree of precision in their determination, In- deed, fossil fresh-water shells rarely possess characters sufficiently marked to form the basis of accurate specific distinctions. [ 403 ] XXXI.—On the Geology of the Island of Zante. By HUGH EDWIN STRICKLAND, Esg., F.G.S. [Read November Ist, 1837.] THE observations detailed in this paper are the result of a few days’ resi- dence in the Island of Zante, during which I was enabled to take a general view of its geological features ; but a complete survey of this and the other Ionian islands is still to be desired. Such an investigation would be a work of labour, for though there is little variety in the rocks, there is much com- plexity in their arrangement. ‘The structure of Zante, more simple than that of the other islands, presents an epitome of their component rocks in an almost unbroken succession ; and it may, therefore, be selected as a type to which the phenomena of the other islands may be referred. The geological phenomena of Zante may be arranged under the three heads of, 1. Apennine Limestone; 2. Tertiary Deposits ; and 3. Mineral Springs. (See Map, Plate XX XIII.). 1. Apennine Limestone.—This is perhaps the most convenient appellation for that deposit of compact white or grayish limestone, which is so largely de- veloped in the south of Europe, and especially on the shores of the Adriatic. It has an uniform character throughout many thousand feet of vertical thick- ness, and many hundred miles of horizontal extent. The few fossils it contains agree with those of the cretaceous, and in part also of the oolitic series of northern Europe. It constitutes, in Zante, an anticlinal ridge, extending in a N.N.W. and S.S.E. direction along the south-western coast, from Point Skinari to Point Cheri, and this ridge is continued through the island of Cephalonia. Along the eastern side the prevailing dip of the strata is from 30° to 45° to the E.N.E. ; west of Point Skinari an opposite dip commences, and continues, with few exceptions, to near Point Cheri, where the strata again dip to the eastward. The tertiary beds occur only on the east of this ridge. On the west we find a series of cliffs, upwards of 600 feet high and almost perpendicular, the sea-worn caves and fir-clothed crags of which present highly picturesque scenery. ‘This steepness is continued to a great depth beneath the surface of the sea, as is proved by the deep sounding’s along this coast. VOL. V.—SECOND SERIES. 3G AOA H. E. Srricxianp, Esq., on the Geology The Apennine limestone, of which these cliffs are composed, is nearly white, and Jess compact than usual, often resembling the hard chalk of the north of England. No beds of flint were noticed here, though in Corfu they are not unfrequent. Organic remains are by no means abundant, yet Nummulites, fragments of Hippurites, and indistinct traces of other fossils, may frequently be detected by searching. From its compact, inflexible, and brittle texture, the Apennine limestone generally abounds with faults and fractures, which give rise to numerous ca- verns, (catavothra), subterranean rivers, and thermal and mineral springs. In these respects, no less than in its mineral structure, it presents a close analogy to the Carboniferous Limestone of northern Europe, for which it has often been mistaken by observers, who paid no attention to its fossils. The frequency and violence of earthquakes in many parts of the south of Europe, may perhaps be accounted for by the unyielding texture of this rock, the vibrations being propagated to much greater distances, than in countries composed of more loosely aggregated or more elastic materials. In Zante the Apennine limestone presents numerous faults, one or two of which will be alluded to in a subsequent page. 2. Tertiary Beds —These occupy the greater part of the island of Zante. Reposing on the eastern flank of the Apennine limestone, they extend to the coast : they rise also in several detached hills through the alluvial plain which forms the centre of the island. They have evidently yielded to the same disturbing force as the limestone range; and they dip from this rock to the eastward. ‘The upper portion is the counterpart of the beds, described by Mr. Hamilton and myself, as occurring near Lixouri in Cephalonia*. In Zante, they are best displayed in the Castle Hill above the town, and in the cliff which extends thence to the eastern coast. (See Plate X X XIII., Sect. 1.) The upper strata near the Lighthouse consist of a porous, calcareo-arenaceous stone, ofa pale yellow colour, and easily worked. Fossils are rare in it, except on the east coast, where one or two of the strata contain numerous casts of Cerithia and other mollusca. These strata are succeeded by a’ thick deposit of blue clay and marl, form- ing the height on which stands the citadel of Zante. The shells found in it are principally Pectunculus auritus, Broch., Buccinum semistriatum, Broch., and Natica glaucmma, Lam. All these species occur also in the middle portion of the Lixouri section, but more abundantly, and associated with many others. The gypseous beds, which at Lixouri succeed the argillaceous strata, are not visible in this part of Zante, but on the south coast they form the com- * See Geological Proceedings, No. 51, and postea. of the Island of Zante. 405 mencement of a section which carries us much further down in the series than the lowermost beds examined at Lixouri. (PI. XX XIII., Section 2.) The gypsum also occurs in white and conspicuous patches on the hill at the S.E. extremity of the island. The rest of this hill consists of sand and clay be- longing to the upper part of the series; but the beds are much disturbed, and not easily reducible to the regular arrangement seen in Sections 1 and 2. The uppermost beds in Section 2 consist of gypseous marls and gypsum, sometimes fine-grained and saccharine, but sometimes only a coarse agere- gate of selenitic crystals like that at Lixouri. The stratification is occasion- ally preserved, though in others it appears to have been obliterated by the action of crystallization. Angular fragments of a black marlstone, imbedded in the gypsum, seem to have been derived from strata of stone, broken up by the force of the crystallizing process. The strata of yellow limestone above the gypsum, exhibited in Section I, and at Lixouri, clearly belong to the Pliocene epoch, many of their fossils being identical with those of the Subapennine hills. The strata which underlie the gypsum in Section 2, consist of a series of brown sandy clays and marls, but whether they also belong to the Pliocene or to a prior epoch, it is not easy to determine. They extend for about two miles along the coast, and dip about 25° to E.N.E., with a few local interruptions. Fossils are very rare in these beds, and in general they are too much crushed to allow the species to be determined. They were noticed only near the middle of the argillaceous series and near its base. At the former spot are crushed fragments of echini and obscure bi- valves ; and at the latter, is a bed of indurated bluish marl containing an abun- dance of the shells of Hyalea and Creseis, but they are larger than those of the species now living in the Mediterranean (Hyalea cornea and Creseis spi- nifera), and are therefore probably distinct species. The argillaceous beds are succeeded by yellowish calcareous sandstone and loosely aggregated limestone. A great subsidence appears to have taken place between that point and the range of secondary limestone, about a mile distant. This tract forms the marshy plain of Port Cheri, towards which the tertiary strata dip on bothsides. There is consequently no traceable sequence between the argillaceous beds above described and the calcareous strata, which we are now considering. ‘The latter dip about 18° S.W., and extend along the east side of the marsh, forming some hillocks at its upper end. They consist in ge- neral of calcareous particles, interspersed occasionally with pebbles of secondary limestone; but some of the beds approach the texture of Portland stone. Minute Foraminifera are abundant in it, and the only other fossils noticed were two species of small Pectens. 3 G4 2 EEE ee SSS eee ees SS Pa eT 406 H. E. Stricxrianp, Esq., on the Geology These calcareous rocks seem referable to a distinct epoch, and may perhaps eventually prove to be of the Meiocene or even of the Eocene age. The fine-grained limestone, extensively quarried near Lixouri in Cephalonia, be- longs probably to this part of the tertiary series. On the west side of Port Cheri is a low cliff of blue marl and clay, the beds of which abut against the secondary or Apennine limestone, and dip about 18° north-east. The only fossils noticed in it, were a few scales and vertebre of fish, and a species of Vermiculum, Mont. (Quinqueloculina, D’Orb.) This small, argillaceous mass has been probably derived from a higher part of the tertiary series, and brought down to its present position by the sub- sidence, which seems to have formed the valley and bay of Port Cheri. Of this depression, there is further proof in a remarkable fault, which occurs in the Apennine limestone, and is marked by a smooth surface of the rock descending to the sea. It may be traced inland in a direction W.N.W. for half a mile or more, rising like a wall above the downcast portion on the north-east side. At the point where it joins the sea the surface is nearly a plane, inclined about 55°. It is scored with numerous stria, inclined at an angle of 65° to the horizon, the dip of the strata being about 25° N.E. The enormous friction and pressure of the descending mass have imparted to the surface of rock, a remarkable degree of hardness, and a darker colour than usual. This change of character penetrates to the depth of about two or three inches from the surface; the rock below being softer and white, and resembling the compact chalk of Yorkshire. The tertiary beds range from Port Cheri northwards along the foot of the limestone, and reappear on the north shore about two miles beyond the village of Catastari; they are shown in Section 3, which is in some respects a counterpart of Section 2, but presents differences which it is not easy to ex- plain. The porous yellow limestone, which at Port Cheri intervenes between the argillaceous beds and the secondary rocks, is here wholly absent, and the tertiary clay appears to pass gradually into the secondary limestone. The highest beds in the section, consisting of blue marl with shells of Creseis and Hyalea, are the precise equivalents of that which contains these fossils near Port Cheri ; and we are thus furnished with a common point of departure in our comparison of Sections 2 and 3. They are succeeded (Section 3) by numerous beds of blue clay and marl, apparently destitute of fossils, becoming more calcareous in the lower part, and ultimately passing into a white lime- stone resembling hard chalk. A stratum of conglomerate, used for millstones, occurs here, and consists of rolled pebbles of compact Apennine limestone ; beneath this are other strata of compact limestone, undistinguishable from that of the Island of ante. 407 of the secondary mountain range. The beds above described are conformable throughout, and seem to pass downwards into the secondary limestone ; whether this is really the case, cannot, however, be determined from the section before us, for the sequence is again interrupted by an extensive fault, (seen at the left hand of Section 3). It is therefore possible, that the lime- stone beds below the conglomerate may be considerably above the true base of the tertiary series, and that an Azatus may exist between them and the real secondary limestone, which they so much resemble. A careful survey of the line of junction between the secondary and tertiary formations throughout the island, would perhaps solve the difficulties, presented by this section. § 3. Mineral Springs.—The springs of bitumen, for which Zante has been celebrated from the time of Herodotus, rise in the marsh at Port Cheri, (see Pl. XX XIII., Section 2.). The principal one is a well about five feet deep ; the bitumen oozing up from the bottom; and above it the well is filled by clear, cool, and tasteless water, which is probably only an accidental accom- paniment of the bitumen. Some travellers (Walsh, Chandler, &c.,) state that bubbles of gas are given out by the bitumen, but in two visits which I made to the spot, nothing of the kind was observed. The produce has been stated at forty barrels annually*. Bitumen also rises in the Bay of Cheri, some hundred yards from the shore. (See Map.) ‘This circumstance proves, that the bitumen is not derived from the peaty soil of the marshy plain, and there is nothing in the composition of the rocks around, to induce us to refer its origin to them ; we must therefore suppose, that this substance is derived from that region of volcanic action, which may be almost demon- strated to underlie the Ionian Islands. ‘This supposition derives farther pro- bability from the fact before noticed, that the spot, where the bitumen rises, has been the site of a vast dislocation. On the northern coast is another remarkable mineral spring, which seems to have escaped the notice of previous observers. It occurs about half a mile to the north of the junction of the tertiary and secondary rocks shown at the left hand of Section 3, Pl. XX XIII. The Apennine limestone here forms a low cliff descending abruptly to the sea. A spring of turbid water, resembling diluted milk, gushes out at the foot of the cliff beneath the sea level, and rising to the surface, from its less specific gravity, flows away above the sea-water in a stratum a few inches thick ; flakes of a slimy white substance (probably Glairine) abound in this water, and are seen in the surrounding sea for a considerable distance ; a strong smell of sulphuretted hydrogen is diffused * For further details relative to the “ tar-springs,” see Hawkins in Walpole’s Travels in the East, Chandler's Travels, vol. ii. ch. 79, &c. 408 H. E. Strickranp, Esq., on the Geology of . ‘ - Part of the County between the SUTLUJ and the RAMGUNGA Te illustrate Gap! Gautlevs memoir on the organic remains found in the Sevalik Hills. Moradabad ° gh < © Suharunpoor § Canal Seale of English Miles to wo 3 we jo Latiude of Hardwax 29! 67 Nov Longitude = 78. 2 East Lruns bal Suc 24 Screws Vol VIG ; { —— SSS —_ PLATEAU near the Village of Jabree, MURKUNDA RIVER Hed and Brick Coloured hays: Shingle or Leds of ‘Lialders. While Sundefuie PLATEAU upon which the Village of DEONI is situated, MURKUNDA RIVER. 7 Zs Groot Trans 2° Series Vat VLAD & i r r ce / m (pen De 3 A Parkur : a. § e x ba | i i te : a|: E © Nuggur ) » | s : Sie t * } (a é | a, i Ullah , %, hn ipep,| ~—<, : ahs sigs : ; ai] § § Goutila Tate s : * ~ = . Ss ~ 6 . | = a 2 = 7 s :@- ME = \ mee as, Cop Mideenda x H & eg ah = | Bara heer Cine ee if oes = q = Ee Gangla L ral 6 f rh . z 2 | | = af fH Hauterness bos] 5 = i i - 1 i Ey E Se ee R U. N N 2 a i | y i); } 4 , & i@: = 5 < + ~*~ = = j os < 3 = = & i a = e DIVISIONS. 24 North. — *0 70 East. ee ee ee nt ee | es nao ¥ EEASY . - - . & t » - : ee ANNs Ae BAe nahh NERVE nom anme ne Geol. Trans.9¢ Series Vol VEL XXT. SECONDARY FOSSILS, CUTCH. = Pf cr p ie iy ‘ , ae ¢ i K 2 ; “alt 5 R A oy «i? t } ¥ ‘ a i Geol. Trans. 2% Series Vol VEL. XXU. SECONDARY FOSSILS. . COTCH. ww \\ Bee abl vif 1a a eee ee 1% 4 Ly if : Cp) a t Bo . es a MN tae § es ‘ tay), ; aA = ; ‘ Geol. Trans. 20 Serves Vol VILA, “=e SECONDARY LOS SLES, CUT CH. : Geel, Trans. 2% Series Vol VFL AXLV” NOMMUTATIC L SHE STONE FOSSILS, COLTCH. Cae Cee ee So c om vm XP. “ LL rares. 2% Serias Val. VLE X 7OO. C LOSSIDS, TERTIARY CUTCH. Geol Trans. 20 Serres Vol V L7 AXAXVT, TERTIARY FOSSILS, CUT CH. Geol Trans 24 Series VV LLARVI. SER. Fig. 1.7.29 in Fig. 2. 7-29 ; Fig. 3, p-s39. Corgewood pig 9 e aw 5.E. Bing. a Paphilt ales W. eMilphauee if E Quarrien. Inkberrow. ie — a Pat Mark —a ee - Lower Red Marl — Red Mart. z ¢ Fig 4 : : Shrewley ig yp rs B17 49.548 a a a ee Se von a = SS = = Le denver Red Marl cupped by a “Orpe Red Sanat ° v Wart ower Red Mart cuppad by Keuper Sandatone. Tre Bade ot Hel Sandstone aa rape fal er UPPER FORMATIONS ogi Fig.5. W. of Droitwich pp.sse.se oe of Male Bridge ompersiey. Mad st Trough of Saliferous. Marts. ; the E == ms = = —— Sa. _ NEW RED SANDSTONE SYSTEM, Lower, beds of Loner bale ot Ved ower Red Mart, — VhP fale oe New Ret power Bods of N.Redt Sandet. in GLOUCESTERSHIRE — WORCESTERSHIRE TANLE OF COLOURS {General Section) ; (Sallie Marg Red S@ndsatone New : | Bunter Sandstein or Grés — bigarré| ( Keuper or Marnes riser) AXD WARWICKSHIRE . to illustrate the Memowr by M" Murchison & M' Strickland P3831 Scale of Milis tor Mp & Horizontal distancee of Sections. , eo hte New Cae « : > Engraved by J Gardeor Regen Str*Zandiow et a yee wr i. > va! hey 5 oe ia oe A " "4 on", ‘da ‘le ; MEMMDOY A BZOTaU7E CAN May ie , WAALS VAN A, attie rs 20 ¥ EI ee. eS a a Geol Trans 2" Serres Vol V Ll 28 ——— ss a ee ‘ heyy 6 natare Ore Kal SORE nak Nae piles of the Bade NIH Pog } Fipils S the Aeupr anion p aan Sandton with ryple marks and inpresionr yf fiotlips Fig 2 The pootstaps Lig 3 Lethyodoralite gy, Hybadus kepor Hig 5 Fortun of the lower paw ofa Fish Lig 67 Weeth of MegadosaurasLig Fu. A lioth prom Leanangton Lg & lieth ofc pane ? é tof the ribbed suyfice Fig 56 Lorton of interur Fig: 5° Tieth of an Lybodis Fig 4 Losrdonomya mini la lig & A tweth found atleamingtin Fig 10 Virtebra ofa Saurcan Fg M Ma. Lohinestachys vblongus p. 910. j ; i . *y, v 4 : : — A ; . - - lo ‘ “| *) © 3 és > ~~". Py “ — ® . ’ a v * . ° . Fine tri’! ee en eat * > ieee Scharf lthog. ' . “0 . pee a Ome O- N.S, on The CGA 5k. of em meio = ONL I and EOS S E XY to accompany the Rev? W.B. Clarkes, Memoir. Pp. 359. Tig 1. p.362._ Coast Section trom Walton (Suttolk) to Bawdsey Haven, Mouth of the Deben., Horizontal Scale 8 Inches to a Mile, Vertical Scale to Horizontal 3 to 1. Boal vs Col UF (SE. of Walton) tela Tower artificial Mound | c Tower in Ruins Martello Tower All the Shore trom the East Point, a Clay bottom with fossils and. Sand. Fig. 2. p.362._Wast Section trom Bawdsey Haven to the ancient embouchure of the Alde N.of Aldeburgh. Gast Guard House aus Aldborough High Lightho. or Taw Lightho. Slaughden Quay. Aldeburgh 2 Marshes and River Alde. Beacon Bawdsey y Martello Tower Martello Tower : ‘ anda HoMleseley ot Gyda Church Dayton th. Butley Lig. 3. p.362 — Section trom the Mouth of the Stour to Landguard Fort. (Scale 4 Inches = 1 Mile | Kayborugh Cui? & Ridge. Walton Ridge- Landguark Fort Boat Walton Gar AY River Orwell Mouth oF the Stour a Shingle Beach Fig. 4. p.362_ Front View of the Naze Citts, Walton Essex. Fiji. 50: Gag 8 i = Stratiord S! Mary, Suffolk, ae W° 5. p.a62—Protile of Wallon Naxe & Ridge atthe 60 ®mile-stone from London. Signal Station & Tower End ee ee OE ES = s Hig 7. p.302.-Essex Coast trom Walton Naze to Harwich Harbour. XN. : ( Seale 1'2 Inches-1 Mile / Walton Name (sce Dover Gurt. Sith Clifte Barnuck cli. Entrance to Landeemore Coment Tanks a Cay a -. & Sand ce | Vegetable Soil Beach | Trans Ciol Soe. 224, Serres. Vol BLA GE SAUItAW Lemons from the Magqnescan Conglomerate p 349 tig 1 lo 6 reduced to one half the Natural Str Oh Ds Si I ot Vem Fh ya ermal ee 4 _ * vey ih se 4 oe it mi i) D HAN Nh Oh ANY iN ly, fs Gand \\\ ha ON f Beatie My sos? Geol. Trans. 2% Series. Vol.V. Pl XFXL. 1s ae A Sedikewi. Nel. General Section across the Sandy beds with l SS Si hell. NV? 4. West Side of Stream '2 Mile N. of Bournabat p.4oo. re | Micaceous schist and Marble Hy ite Limest. nn Lacustrine Linest a 77 & nonigneous gravel Plain of Bowrnat.a tt. Saal oo radwtic Rocks TM i Hq of the to aecompany p. 393. district of Smyrna. pp-397.398.599.400. SS = z 2 = ——S = Trachyte Tufaceous rg ral = Conglom.ot Grey Limst. Quartz & Schict. White BT lon dirt chal. rae Grey Limest.& Schist. N? 5, About § Miles N.of Bournabat. p. 401. Ww E Trachy te and & erpicmy emule: Pumiceous and =Tore, Sandy tata, i a, e Trai of 2 a) 2G a 2. Trachylic @nglom. o,f 99 Go, 2a. Lacustrine gravel with tradwtc pebbles Merr Iv Sb CTT ONS ENVIRONS of. SMYRNA MH. E. Strickland s, Memotr. LL Lledo alluvium Loe & >) i WhO wave Pree | wh ', j Fessaecn ism * 4 on ~~ Ladweente eM Uli | a . Geol. Trans.24 Series Vol.V. Pl. XXXMI. Sketch of the LSLAND OF ZANTE. p. 403 Plan of the Coast near the Mineral Spring. p. 408. SS f Twn of Zante Downeast Side Upeast Side Section ll, North Stade of the Bay of Zante. p.rtosss Lighthouse Yellow Limestone Section 2, North Side of the Bay of Cheri 7.405407 ¢ NE. we louse of the Square Tower Port Chet 4. Porous Limestone te 3, a a on 2 es eS *e es te Section 3, near Catastari pss ESE. z = am Apennine Limestone = Compact Limestone Calcareous Marl Blue Mart andyClay = Pee ee | ce Valery . < @ pn: DO vrernine sinest. Faas Olde Tey =| Newer Tertiary ees Wategr $ Bitumen Geol Trans. 2 Sertes Val 4. Fl. G4, fig 74 hig La figia Milf he Nat.’ Sthe Aithey from nature by 6 Sehoaf CGroceratles Bowerbanhu PY Srnted ty C Ealimanded ’ Scaphites Cigas ees ee ee ee SS es r bal q - : Ae e - . 7 . a . i> i ial } i ¥ . PA Yi ; 7 ‘y A = , ; b é Postscript to the Paper on the Geology of Zante, by H. E. Strickland, Esq. Since the printing of the paper on the Geology of Zante, I have been favoured by Dr. Daubeny with the following analysis of the mineral spring described at p. 407: Specific gravity, 1-020. Solid contents in one pint, 174 grains. Ferrocyanite of potash produced no effect, proving the absence of iron. Barytic salts produced a cloud, proving the presence of sulphuric acid. Nitrate of silver produced a dense cloud, proving much common salt. Oxalate of ammonia produced a cloud, proving presence of lime. Phosphoric test caused evident indications of magnesia. From the above analysis it appears that the water of this spring differs but little from ordinary sea-water. Indeed, from the manner in which it rises in the sea, a large quantity of sea-water must unavoidably become mixed with it. At the same time, its inferior specific gravity, its milky colour, the floc- culi of Glairine, and the streng smell of sulphuretted bydrogen, all serve to characterize it as a mineral spring analogous to those of volcanic regions. 7 H. E. Srrickianp. TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. SECOND SERTIES. VOLUME V. Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque lis uti, sed ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. Novum Organum, Prefatio. LONDON: PRINTED BY R. AND J. E. TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1840. Pry Aces tas ee ies i ted Che i TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. SECOND SERIES. VOLUME V. PART ‘TLHE THIRD: Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque iis uti, sed ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. Novum Organum, Prefatio. LONDON: PRINTED BY R. AND J. E. TAYLOR, RED LION COURT, FLEET STREET. SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1840. or ae . os us he sl a Ee Reh il tech: 1 Beinn ba mew ie tiely's 4 ¢ OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY OF LONDON. 1840. PRESIDENT. Rev. WILLIAM BUCKLAND, D.D., F.R.S. & F.L.S., Instit. Reg. Soc. Paris. Corresp., Professor of Geology and Mineralogy in the University of Oxford. VICE-PRESIDENTS. GEORGE BELLAS GREENOUGH, Esq. F.R.S. Rev. WILLIAM WHEWELL, B.D., F.R.S., & F.L.S. Professor of Casuistry in the University of Cam- LEONARD HORNER, Esq. F.R.S. L. & E. bridge. Sir WOODBINE PARISH, K.C.H. F.R.S. = SECRETARIES. CHARLES DARWIN, Esq. B.A. F.R.S. | WILLIAM JOHN HAMILTON, Esq. FOREIGN SECRETARY. HENRY THOMAS DE LA BECHE, Esq. F.R.S. & F.L.S. TREASURER. JOHN TAYLOR, Esq. F.R.S. COUNCIL. ARTHUR AIKIN, Esq. F.L.S. RODERICK IMPEY MURCHISON, Esq. FRANCIS BAILY, Esq. V.P.R.S. F.L.S., Instit. F.R.S. & F.L.S., Hon. M.R.I. A. Reg. Soc. Paris. Corresp. EDW. WILLIAM WYNNE PENDARVES, VISCOUNT COLE, M.P. F.R.S. Esq. M.P. F.R.S. WILLIAM HENRY FITTON, M.D. F.R.S. PHILIP PUSEY, Esq. M.P. F.R.S. & F.L.S. GEORGE RENNIE, Esq. F.R.S. WILLIAM HOPKINS, Esq. M.A. F.R.S. DANIEL SHARPE, Esq. F.L.S. ROBERT HUTTON, Esq. M.P. M.R.I.A. Rev. ADAM SEDGWICK, F.R.S. & F.L.S., CHARLES LYELL, Jun., Esq. F.R.S. & F.L.S. Woodwardian Professor in the University of WILLIAM HALLOWS MILLER, Esq. M.A. Cambridge. F.R.S., Professor of Mineralogy in the University of Cambridge. CURATOR anv LIBRARIAN. WILLIAM LONSDALE, Esq. ADVERTISEMENT. THE Editors of the Transactions of the Geological Society are directed to make it known to the Public, that the Authors alone are respon- sible for the facts and opinions contained in their respective papers. It ts requested that all letters and communications to the Secretaries, and presents to the Society, may be addressed to the Apartments of the Geviogical Society, Somerset House, London. CONTENTS. PAR TT. I. On the Geological Relations of the South of Ireland. By Thomas Weaver, Esq., F.R.S., F.G.S., M.R.LA. . - , Sit II. On the Geological Structure of the North-eastern Part of the County of Antrim. By James Bryce, Jun., M.A., F.G.S. (Member of the Geological Society of Dublin, and of the Natural i Society of Belfast.) : : 2 : p: III. On the Squaloraia. By H. Teg M.D. (Communi by Charles Stokes, Esq., F.G.S.) : : : . De IV. Notes on the Geology of the North Coast 8s, the St. Lawrence. By Capt. Bayfield, R.N., F.R.A.S. (Communicated by George Bellas Greenough, Esq., P.G.S.) . ° : - ; E ape V. On the Geology of the Bermudas. By Richard J. Nelson, Esq., Lieut. R.E. (Communicated by George Bellas Greenough, Esg., P.G.S.) p. VI. Notes on the Geology of the Brown Clee Hill, in the County of Salop. By Romley Wright, Esq., Employed on the Ordnance joie metrical Survey of England. : : : : ° Dl eps VII. Observations on the Geological Structure of the ate) Wap of Reading. By J. Rofe, Jun., Esq. ae 4 Robert Hunter, Esq., F.G.S.) . ‘ 5 5 ite VIII. Observations on a Well dug on the South side of Hampstead Heath. By Nathaniel Thomas Wetherell, Esq., F.G.S. : : Shop IX. Observations on the Strata penetrated in sinking a Well at Diss, in Norfolk. By John Taylor, Esq., Treas. G.S. é ; “us Pe X. On the Structure of the Neighbourhood of Gamrie, Banffshire, par- ticularly on the Deposit containing a ia eae Prestwich, Jun., Esq., F.G.S. . A : p- XI. Notices on the Geology of the North Coast of the Counties of Mayo and Sligo in Ireland. By Archdeacon Verschoyle, M.A. (Com- municated by Roderick Impey Murchison, Esq., P.G.S.) . vps XII. Description of some Fossil Crustacea and Radiata, found at Lyme Regis, in Dorsetshire. By William John Broderip, Esq., F.G.S., E.R. §e. V.P.Z.S. : : : : : 4 ; a 69 83 89 103 159 149 171 CONTENTS. XIII. On the Bones of Birds discovered in the Strata of Tilgate Forest, in Sussex. By Gideon Mantell, Esq., LL.D., F.RS. . é 2 ope XIV. On the Syenite Veins which traverse Mica Slate and Chalk at Good- land Cliff and Torr Eskert, to the south of Fair Head, in the County of Antrim. By Richard Griflith, as » F.G.S., IR.1LA., P.GS. of Dublin . : ° : . . a XV. On certain Peculiarities in the Cervical Vertebre of the Ichthyo- saurus, hitherto unnoticed. te Sir ae Grey Egerton, Bart., SEP) V P.G-.S. : ; : . : cea XVI. Notes to accompany a Geological Map of the Forest of Dean Coal- field. By Henry Maclauchlan, Esq., F.G.S., at on the Ord- nance Trigonometrical Survey . ° : : : - p. XVII. Notice respecting a Piece of recent Wood, partly seinen by Carbon- ate of Lime, with some Remarks on Fossil Woods. a Charles Stokes, Esq., F.G.S. : : ° : Pp: XVIII. Remarks on a Section fe the Upper Lias and Marlstone ” Yorkshire, showing the limited Vertical Range of the Species of Ammonites and other Testacea ; with their Value as Geological Tests. By Louis Hunton, Esq. (Communicated by J. F. Royle, Esq., F.G.S.) «ip. XIX. On the Distribution of Fossil Remains on the Yorkshire Coast, from the Lower Lias to the Bath Oolite inclusive. By W.C. Williamson, Esq., Curator of the Manchester Society of Natural History . p. XX. On the Cretaceous and Tertiary Strata of the Danish Islands of See- land and Moén. By Charles Lyell, Esq., P.G.S., F.R.S., Ge. . ps XXI. Notices and Extracts from the Minute-Book of the Geological Society : . = i L. Dbedvibatiiteass on the Cliffs an the Nespibolw hood of Beach: made in December, 1832. By James Mitchell, LL.D., F.G.S. [Read May 15, 1833.] : : p: . Notices of the Red Marl and Lias of peta stia: of a Fault by which they are affected; and of Fossil Freshwater Shells at Shotover Hill. By Hugh Edwin Strickland, Esq., F.G.S. [Read December 4, 1833.] : p: . Notice of the Analysis of a Mineral Water from the Has. of St. Paul, in lat. 38° 45! S., and long. 77° 53° E. By John Bostock, M.D., F.G.S. [Read January 7, 1835.] :

00 Plard sandstone; .7.'2's c'e)s ace « sleraiele'so'ale'sie¢ 007-6 20. Beadstone ...... Very impure clayey limestone ........ siarcieh A PEEP TIG PEP ENACKS 5 0 «si cinie 3 o's Bituminous Shales veyaeicislcletctee crerslerctsieveelelels OTF RanG 22, Hard white rock..Hard sandstone, a few feet below which the basaltic) rocks appears... 00602500 Grill Bh (0) MW) = AUS se) * The fossils in this rock agree with those of the adjacent limestone of Steeraways, which Mr. Murchison has shown, by its organic remains, to belong to the carboniferous series. + Iam rather inclined to think that a deposit of trap of variable thickness underlies the car- boniferous limestone from its first appearance near Little Wenlock to Steeraways. 426 J. Prestwicn, Esq., on the In the road leading from the Hatch to the Wrekin, and in some other places, the superposition of this limestone on beds of trap, with their rise against the igneous axis of the Steeraways, is well exhibited. From Steeraways to Lilles- hall the limestone is not exposed ; but at the latter place, it forms a narrow band about 14 mile in length, overlying the trap and Silurian rocks, and rising from beneath the coal-measures. It abuts against new red sandstone on the west. The dip varies from N.E. to E.and is at different angles. The north end of this wedge of limestone exhibits an apparently anticlinal line in the prolengation of the major axis of Lilleshall Hill, whence it might be supposed, that the limestone wraps all round that hill, but there is nothing further to support this hypothesis. The anticlinal dip takes place within a few yards of the Lilleshall fault, ranging parallel to it, and might therefore have been produced by the lateral pressure of the new red sandstone. The limestone at its outcrop near Lilleshall, is capped by a few yards of fissile sandstone, belonging to the coal-measures, which from the northward dip of the strata, rapidly acquire a greater importance, though not sufficiently to bring in the productive measures. This zone of limestone gradually decreases in width by the convergence of the Lilleshall and great east faults, and near Church Ashton it disappears in consequence of these faults meeting*. (See Map and Sections.) Between Lilleshall and the pool at the bottom of the Hadley inclined plane, no sinkings have been made, which could point out exactly its course below the coal-measures : in digging “ the pool,’’ however, the limestone is said to have been met with, striking parallel to the fault. It was reached also in a pit sunk by Mr. Hombersley about half a mile south of Watling Street, at a depth of 80 yards, and in a nearly horizontal position. At Steeraways the limestone has been traced only a few yards below the coal measures ; but its range under them has been lately confirmed, by its having been noticed rising to the surface at the Horsehays, in the centre of the coal-field. Owing to its rapid dip to the N.E. and small development, it has not been worked, and its further prolongation therefore is not positively known. Nevertheless there is no doubt that the carboniferous limestone immediately underlies the coal-measures from Little Wenlock to Lilleshall. (See Pl. XX XVI., Sections 5 to 7, 13 and 14.) At Little Wenlock and Steeraways the upper beds of the limestone are very thin, argillaceous, and of a bluish gray colour. As the strata descend they become purer, but still conta much alumina and silica, which cause the lime, made from this rock, to set well under water. It is quarried for several iron furnaces. At the above places and at Lilleshall, the lime rock is subor- * Its depth at this point is 150 yards. Geology of Coalbrook Dale. 427 dinate to beds of sandstone. At Lilleshall the deposit is much thicker than at Steeraways, being 60 yards, and it is also purer and generally of a lighter colour. The upper beds are dark gray and the lower nearly white; but they are all subcrystalline and hard. The partings between them are frequently composed of a red ochrey clay, which generally colours both the broken limestone and the workmen’s dress. The following is a rough list of the strata at Lilleshall given me by Mr. Bolls: Thickness. Local Names. Yds. Ft. In. ¥, White grit..... ne alae Thinly laminated, light-coloured and mottled, coal-measure SANGSHONES siec'e se sis'ee oes bn obcocooGdata07 cK variable. 2. Gold lumber ........ Mellow Clay aie: ere icisi alors ore ase ais ohelctehatcateias Seb eiot tin cveters Os) Te GNGTUNM . 6 ccciceun ...-.».Nodular layers of crystalline limestone, with thin seams of clay ; they become more compact in descending.. 5 0 0 di, Shien 6 Go dnoaoues is > oAVEO GENTEGUS Clay aa/t clei se vulwlclenslareishe carole ae Mavolalckenete Wk 6 MPRORTUM. <5 ces cee oc ciel ee Sante aseNOSS) are-caicrate ceeraia esaceistuie sie tissue meade, cin in beve ¢ 0 2.56 6. Splother ..........6. Gray imipire litestOnel..a7 syes%e.0 1s solve sic cine es ce ct nis © « AO. 0 fio RIM 6 GogenoobucdacD BLOC: Claires a racteterets bo doOob an ooC Loudno ooauoDOoOgGs oO @ 8. Riding quarry........ Gap MestOes. aie aveieroia'ete oteun ccengieettdl ele utccal esses eae eG 9. Red limestone........ Tight red limestone? pets) - Wi Ago a“ A en LiPg mg gs p—- yyy 7 Ligapapuly ey Uy Ly iif UY If MY FELLLL YIP YL ELI LLU pEIP ates Ls, \ fey Yyupy My Mp W“Ug yy YG 2 2 Z Meh VM l 1 “ny, ye Se GG LMU Generally, however, the strata on the sides of the small slips are not much contorted. The above instances (2, 3, and 4,) are more commonly appli- cable to the larger faults, as in 5. The following section of the “best coal” along a level at the Meadow pits, Madeley, shows the prevailing character of the small disturbances. Sometimes, owing apparently to the greater hardness of certain strata, the line of fracture assumes a step-like form, as in the annexed i: diagram 7, taken in the lower coal level at Priorslee. Where two slips have met, singular effects have been occasionally produced, as in diagrams 8 and 9 taken in the Hill's Lane pits, Madeley. No. 8 is situated in the best and clod coals, and No. 9 in the little flint coal, and is on a larger scale than the other diagrams. These disturbances are difficult to account for: a, a’ appear to be masses subsided or fallen into a wedge-shaped fissure, enlarged probably at the mo- ment of disturbance by the increased separation of b and c, so that a’ would fall into the cavity and crush down the seam of coal as in No. 9. The intersection of two faults occasionally presents the phenomena in dia- gram (10). A small fault or slip usually commences by a simple fracture, accompanied by a slight difference of level between the two dislocated sides; but the difference rapidly increases, until the smaller fault joins a larger fault (see Map, PI. XX XV., also a, Diagram 11, page 455). Thus the Arleston fault, which commences between New Hadley and Ketley as a simple fracture, at- Geology of Coalbrook Dale. 455 tains, in the course of its range towards Arleston, and at the distance of about a mile from its first appearance, a vertical change of level of about 100 feet. Numerous other instances might be adduced ; sometimes, however, a fault will thin off at each extremity ina simple fracture, as in fault 19, PI]. XX XV., which ranges about half a mile, and produces a difference of level amounting to 30 feet in the centre of its course, In the Old Park, (Map, Plate XX XV. fault 33.) is a series of four of such faults, in parallel and consecutive planes, one fault commencing at a point in one plane corresponding to that where another fault ended in the adjoining plane. The maximum effect of one of these faults is about 24 feet, and the range of the whole amounts to nearly three quarters of a mile (see Map). At Wrockadine Wood, two faults cross at an angle of 55°, and the disturbance of both amounts, at a few hundred feet from this spot, to 25 feet; but at the point of intersection the faults diminish to mere fractures, which do not affect the level of the strata. Some of the small slips extend but a mM few yards and produce only 1, 2, or 3 feet of vertical disturbance. These minor dis- locations are so numerous that it would be almost impossible to lay them down. In the map, therefore, I have represented only those which have not less than 20 feet of vertical change of level. The annexed plan of a small district between the Boundary and the Ketley faults exhibits, however, the ramifications of the whole system of fractures. It isa solitary instance ofa plan of all the minor faults carefully and minutely laid down by a ground-bailiff, Mr. Jones, of New Hadley. The numbers refer to yards, de- noting the amount of disturbance, and are placed on the side of the highest level. Thus 1.0 or 0.2 denote that the fault at its point of junction with a larger one produces a difference of level of one or two yards, gradually decreasing as it recedes from that point to zero. All the large and main faults also vary greatly in the course of short distances. Near Woombridge church the A56 J. Prestwicu, Esq., en the Ketley fault produces a change of level between 500 and 600 feet; but at New Dawley, distant two miles, of only 40 or 50 feet. The Lightmoor fault at Snedshill produces a change of level of 300 feet; at the Dark Lane and Malinslee, of nearly 700 feet; at New Dawley, of 350 feet; at Dawley Green, of 400 or 450 feet ; and at Great Dawley, of 500 feet; but at Light- moor it diminishes to 300 feet. This variation arises partly from the junction of other faults, but is principally owing to a slight difference in the angle of dip of the disjointed portions of the coal-field. I have mentioned that the edges of the disjointed strata are generally much bent; the bend being fre- quently flanked by a series of small faults. Thus, in the following diagram of the dislocations, on approaching the Ketley fault, near Donnington Wood fur- naces, a series of minor faults is represented flanking the principal or Ketley fault. Seale, 150 feet = 1 in. Ketley Fault. yards. The same effects are exhibited in several parts of the Lightmoor fault, and likewise precede the Madeley fault near the Hay House. They were noticed also on approaching the line of the Great East fault at Southall. The ra- pidity of the dip stopped the miners before reaching the main fault. The phenomenon of a principal fault flanked by numerous smaller ones, is termed by the colliers ‘ the splitting of a fault.” Thus the Ketley fault is said to split upon approaching the boundary fault near Donnington Wood furnaces. (See Map). Whether in this and other cases the side or branch faults result from a temporary and local division of the larger fault, whether they pro- ceed in gradually diminishing magnitude from the large faults, or whether they form a series of small parallel and independent faults, I have no positive data to prove. J am however inclined to adopt the two latter hypotheses. It is rather remarkable, that although the district is so much disturbed, and bosses of trap protrude in many places through the sedimentary strata, yet there is only one instance of an apparently continuous trap dyke. This occurs in the case of the Boundary fault, along which are indications of the proximity of trap, a mass having been met with near Woombridge, and the coal along great part of the line from Ketley to Donnington being converted into smut. This change of coal into a sooty substance has been noticed also Geology of Coalbrook Dale. 457 at Madeley, near the Hay House. For an account of the effect of the trap rocks, see ante, p. 449, et seq. The faults cannot be traced by any modification of the surface; as they pursue their course indefinitely over bill and through dale; and those towering irregularities, due immediately to the convulsions, powerful effects of which are still attested by the fractured and shattered strata, have been leveled and swept away, leaving scarcely a trace of their presence. It must, however, be observed, that, although the masses of strata do not re- tain their original superficial inequalities, as effected by the dislocations, yet these disturbances have materially aided in modifying the outline of the coun- try, by bringing to the surface, rocks of different degrees of hardness, which having yielded very variously to powerful denudations, great diversity of hill and dale has been produced. The “ Symon fault” not being the result of fracture, is treated of under the head of lithological characters. (See p. 432.) Having taken considerable pains to trace the faults of this district, I am able to describe them in some detail*. To avoid minutia, however, I have arranged them, as far as possible, in a tabular form; and all dislocations of less than 20 feet of difference of level are, with few exceptions, omitted, as well as in the sections and plans. (See Appendix D.) The two principal faults, called the Lilleshall and the Great East, diverge at an angle of about 20°, a little south of Newport, and bring up a wedge of the Silurian and carboniferous rocks into horizontal juxtaposition with the fractured edge of the new red sandstone. After ranging south- ward nearly four miles, a central axis of disturbance intersects longitudinally the included coal- measures, and divides them into three distinct systems, each bounded by prolonged and nearly parallel lines of fissure, ranging between the limits of N.E. and S.W. and N.N.E. and S.S.W., and called the Boundary, Ketley, Lightmoor, and Great East faults. The two exterior systems constitute at first deep troughs. This trisection of the coal-field forms a very marked feature in the Woombridge and Ketley districts; but as we proceed southward the depth of the eastern system of beds, compared to that of the central, considerably increases, and in the same district the western becomes nearly as shallow as the central. ‘Thus the coal-measures in the western and * The following observations are much more ample than those contained in the memoir read February 1834, which presented a short sketch of the principal faults. I have now added further de- tails respecting their range, connection and effects. In detecting these disturbances I received great and valuable information from the miners; but, owing to their experience being confined to small areas, they are, with few exceptions, unable to trace the range of any fault. Although, therefore, I have taken every care in dovetailing these several fragments, slight inaccuracies in the exact course and termination of some of the minor faults may exist. Where considerable doubts have been entertained, I have omitted the information altogether. The courses and magnitudes of all the larger and more important disturbances are, I trust, laid down correctly. 458 J. Prestwicu, Esq., on the central divisions gradually thin off, until, in the parallel of Little Wenlock, they entirely crop out, after a range of 9 miles. Within the same range the eastern division increases in breadth and im- portance, but its continuity is for a short distance completely broken by the limestone fault, which crosses it diagonally from S.W. to N.E., and tilts up this division of the coal-measures to the westward. (See Map, and Section 8.) After crossing the Severn the same eastern division widens considerably, but it is much broken and elevated by aseries of transverse fissures, some of which are parallel to the limestone fault, but others are at right angles to it. In consequence of these dislocations the coal-measures gradually and irregularly crop out, and the Silurian rocks are brought to the surface. The above systems of longitudinal disturbances are affected by numerous small transverse faults, which, proceeding from one of the principal dislocations, sometimes extend across to another, but more often gradually diminish in their range, and disappear. These transverse fractures diverge from the main longitudinal ones at all angles; but the larger commonly at 90°. In the deeply seated strata of the northern portions of the coal-field, their number is comparatively small ; but in the parallel of the igneous axis of the Wrekin they are extremely numerous. At Langley, Lightmoor, and Madeley, they are of rare occurrence; and again, as we proceed south over the Severn to the edge of the coal-field, they become very numerous. Returning to the western system we find it gradually rising towards, and ultimately, obliquely intercepted and thrown out by, the mineral axes of the Wrekin and Steeraways, which we will now consider. The Wrekin is a long knife-edged mountain, ranging from S.W. to N.E., and rising to a height of 1320 feet above the level of the sea. It is formed by a central ridge of igneous rocks, flanked by the lower Silurian deposits. Its Jength, including the Ercal and Primrose hills, is three miles, and its breadth is about two-fifths of a mile. Towering high above the disturbed district, of which it forms the main axis, and still higher above the surrounding and extensive tract of new red sandstone, it constitutes a fine isolated and conspicuous object. Parallel to the major axis, and on the north-west flank of the Wrekin, are evidences of a very large fault, by which the disjointed edges of the new red sandstone are brought into contact with those of the lower Silurian rocks. The latter are seen to dip rapidly to the foot of the Wrekin and Ercal hills; and although we meet with no section exhibiting their juxtaposition with the new red sandstone, still, from the circumstance of having found this deposit in a well on the farm close to the foot of the Wrekin, dipping but slightly towards the north, and again to the north-east, near Eaton Constantine; and, from the specimens dug out at the foot of the Wrekin, indicating that the beds there do not belong to the lowest members of the new red sandstone, and likewise from the formation ranging in a nearly straight line parallel to the Wrekin, and not extending into the transverse slopes and glens, I think we may fairly infer the existence of a very considerable dislocation west of the Wrekin, and into which the Boundary fault merges somewhere at the northern extremity of that igneous axis. Again, as we know the coal-field to be fractured, and its level, with regard to the new red sandstone, greatly altered, both on its eastern side and on its north-western, from Lilleshall to Steeraways, at which point commence the igneous axes of the Steeraways and Wrekin; it follows, that as the coal strata are disturbed relatively to the new red sandstone in the parallel of Woombridge, so, in the parallel of the Horsehays, to the east of the Wrekin, where we trace the prolongation of the same disturb- ance in the coal-measures, the relation of the carboniferous series to the New Red Sandstone must continue the same; and that, though separated by the Steeraways and Wrekin hills, the terminating planes of both those formations must be fractures. Nearly parallel to this axis of eruption, and ¢ the distance of 32 miles to the S.E., ranges ~~ a a tata aye less tas ta — Geology of Coalbrook Dale. Ab9 another important but minor line of disturbance. In its course through the coal-measures, where its nature can be advantageously studied in the extensive works at Lightmoor and Madeley, it is known as the “ Limestone fault,” from the circumstance of its axis being composed of Wenlock limestone and shale. This disturbance forms an anticlinal line; and from the phenomena exhibited in its passage through the coal-measures, it appears that a narrow, central ridge of the subjacent deposits is protruded between the fractured edges of the carboniferous strafa, throwing them off, in nearly vertical dips, but in opposite directions, and producing a change of level, higher, on the N.W. side, by 200 or 300 feet. This disturbance, however, merely affects the position of the strata in its im- mediate proximity; for, at the distance of less than a quarter of a mile on each side, the usual slight dip to the eastward, is unaltered by it, even at the depth of 700 feet. (See Plate XXXVL, sections 15 and 16.) The inclination of the included Silurian strata cannot be well ascertained, as they are much broken. The outcropping edges of the Wenlock limestone, which flank the southern side of this disturbance constituting Lincoln Hill, and Benthall and Wenlock Edges, dip rapidly towards the S.E., and have escaped the denudation which has removed the underlying shale from the centre and N.W. flank of the axis; wherefore the opposite dips, although very visible in the coal-measures, are not well marked, where the axis traverses the Wenlock shale. At Benthall Edge, the centre and the north-western flank of the anticlinal ridge have, by the denudation of the Wenlock shale, been worn into a-deep valley. At Tickwood Hill the strata are much broken, and have a quaquaversal dip. The southern prolongation of this anticlinal fault probabiy produced the well-marked ridge of Wenlock Edge. Northward, the Limestone fault is not traced beyond Windmill Hill, but it continues its north- easterly range towards Shiffnall. Parallel to, and south-east of this second axis, are several smaller disturbances, producing slight anticlinal lines, which present a central and broken nucleus, a few yards broad, bounded by two parallel fissures, from which the flanking and disjointed strata rapidly dip, and exhibit, as in the preceding instances, proofs of considerable lateral pressure. ‘The first of these small anticlinal lines is about 2} miles to the S.E. of the Limestone fault, and ranges, by the Upper Ridding, across the Broseley and Bridgenorth road, at the Dean, to Willey and Shirlot. Another anticlinal line exists one mile S.E. of the last, traversing the Ludlow rocks and the lower coal- measures, and is exposed in the brook below Caughley, and near Linley Hall. In the preceding cases the disturbing power appears to have acted in a direction nearly S.W. and N.E.; but at the northern apex of the coal-field is a short, eruptive axis of trap, partially flanked by Silurian and carboniferous strata, ranging nearly N. by E., and S. by W., and consti- tuting Lilleshall Hill, which rises to the height of 433 feet above the level of the sea. It is bounded on the N.W. side by a large fault, which brings the new red sandstone against the trap and the Silurian rocks and carboniferous limestone. In its prolongation towards the southwest, it joins the Boundary fault, whilst towards the north-east it apparently intercepts, at an acute angle, the Great East fault at Church Aston; and is most probably continued with it into the new red sandstone. The abrupt termination of this axis on the south is remarkable. It should intersect the Don- nington field, but we there find the strata in the plane of the axis, and distant from Lilleshall only 14 mile, entirely unaffected by it, and nearly horizontal, with only a few transverse faults; while as we proceed southward, it again shows itself in the elevation of the central division of the coal- measures of which we have already spoken. Its subsidence northward is equally rapid. VOL. V.—SECOND SERIES. 30 460 J. Prestwicn, Esq., on the Notwithstanding all the dislocations, disturbances, and changes of level, which we have enume- rated above, the coal-measures and the other formations are not much contorted; neither is the angle of dip materially affected. Were it not for the actual exposure of a fault by means of sec- tions, or more generally in the pits, its existence could rarely be inferred from the relative dips of the disjointed strata. I now allude to a case where a repetition of similar lithological characters renders a positive recognition of the majority of the strata impossible. For example: from the dip at Bullock’s Leasows and Randley, an observer might easily suppose a perfect continuity of strata between those two places—the planes having a similar inclination, and in no wise indicating the important intervening fractures. (See Section 6.) From the dip of the strata at Amies and Caughley, they might be supposed to range likewise uninterruptedly between those two places ; whereas a disjointed section of New Red Sandstone separates them. We might also imagine, from the dip of the carboniferous series at Steeraways, that a consider- able fault ranged between that highly-inclined outcrop and the nearly horizontal strata half a mile to the east, but only small slips have been noticed. (See Section 5.) So on both sides of all the large faults, the disjointed strata preserve a near parallelism of dip. Thus, notwithstanding all the dislocations, the deposits maintain a general dip eastward, de- pendent upon the main line of disturbance or the protrusion of the igneous axis of the Wrekin. (See Sections 3, 4, 5, 6, 7, &c.*). Dituvium, or Drirt. The district bears evidence of a powerful aqueous action on its surface, a large portion of it being covered with thick accumulations of gravel and sand. ‘These deposits are frequently separable into two divisions: the lower consisting of a fine red sand, associated with beds of angular and rounded peb- bles, derived from the adjacent rocks ; and the other of gravel, composed also of rolled pebbles of the neighbouring formations, with a few small boulders and pebbles of granite and older rocks, imbedded in a coarse, reddish sand, frequently much mixed with clay. Where the sand is wanting, the separation of the two gravels is almost impracticable. The sand occurs in only limited patches, though of considerable thickness, both in the valleys and on moderate elevations, but more especially on the sides of hills. Thin, distant seams of marl and clay show the irregular and cur- * From the phenomena detailed in the preceding pages, it appears, that the coal-field is but a fractured portion of a Jarger deposit ; the remainder of which must, therefore, exist below the surrounding new red sandstone. From the large faults which we know to traverse the coal strata, and many of which are doubtlessly prolonged through the new red sandstone, the former may, in some places, be brought within a moderate depth from the surface. Still, from the proved irregular persistence of the coal and ironstone strata, it would require great caution in inferring the existence of those beds below any given portion of the new red sandstone, except in the places adjacent to the line of fault, where the coal-measures are well-developed and pro- ductive at their abutment. —— gg IT A nt gt Siang pn a IE ot — aes Geology of Coalbrook Dale. 461 vilinear deposition of the mass. In the sand are frequently found angular frag- ments of coal varying in size from a marble to blocks 5 or 6 feet in diameter ; and extensive accumulations of local gravel, of very variable thickness, are generally exhibited in its lower part. I discovered no organic remains in this deposit. On the hilly district south of the Severn the sand is not abundant, though traces of it occur in Benthall and Posenal parishes ; but it has accumulated in beds of considerable thickness in the valley of the Severn from Coalbrook Dale, through Buildwas and Cressage, and thence westward, covering almost everywhere the Wenlock shale and Caradoc rocks. In some places, it forms small hillocks, as near Buildwas Abbey; at others, as at Strethill and Shineton, it flanks, to the depth of several yards, the sides of the hills bordering the val- ley. On the platform of the coal-measures it is again less abundant, and only in patches, as at Lightmoor, where it is dug for the use of the iron furnaces. It may be thence traced occasionally on the flanks of the hills and in the valleys through Dawley and the Horsehays, increasing in importance as it ranges northward, and extending over great part of New Lawley, New Dale, and Ketley. In the latter place it much resembles the sands of the new red sandstone, and is extensively excavated, for the moulds at the iron furnaces, by the side of the high road immediately west of the Ketley works. It also covers the surface rocks around Wellington, Hadley, and Woombridge ; like- wise the low ground of Donnington, and the north of the coal-field. West- ward of the Wrekin it appears very generally in the valley ranging parallel to that mountain. The overlying deposit of gravel is of more general occurrence. It consists of rolled pebbles of the adjoining Silurian and trap rocks, limestone, red sand- stone, the shales, sandstone, &c. of the coal-measures ; also of a few small boulders of granite, and schistose rocks. Fossils from the Wenlock shale and limestone are extremely abundant in it at Madeley and on the scuth of the Severn. In some parts of the valley on the eastern flank of the Wrekin, this drift is imbedded in a tough, brownish clay derived apparently from the de- gradation of the trap and other igneous rocks of the neighbourhood. Mr. Thursfield of Broseley discovered in the Willey gravel-pits a very singular fossil. It was much water-worn, but displayed a chambered tube inclosed in a sheath, to which it was attached by connecting septa. From its mineralogical character, it had been probably derived from the Wenlock lime- stone or shale. It possesses considerable similarity to the Orthoceratites from the shores of Lake Huron, figured in one of the plates which accompanies Dr. Bigsby’s paper, in the Geological Transactions, 2nd Series, Vol. I. 302 462 J. Prestwicn, Esq., on the Beds of coarse gravel and sand, formed apparently by the junction of the two foregoing divisions, abound in the valleys and on many of the hills from Bridgenorth to Lilleshall, accumulating in great thickness in some valleys, as in Willey Park, in Lightmoor Old Park, New Lawley, and Woombridge. Al- though it ranges over several hills, attaining, as does the sand, a height of 700 feet above the level of the sea, still the summit of many of the hills and the surface of a few valleys are free from it. The thickest deposits are in the valleys running from the lowlands westward of the coal-field, as Muxton, Oaken Gates, Ketley, New Dale, New Lawley, and Buildwas. Eastward of the coal-field, it abounds over the new red sandstone, especially through the parishes of Sutton and Brockton. The rapid variation in the thickness of this deposit is everywhere remarkable. At Hills Lane, where the ground, although high, is level, the thickness in one place is more than 90 feet, whilst 100 yards distant it is only 7 feet. It is frequently found to be 50 to 60 feet thick, as at Willey, Lightmoor Park, in places near New Lawley furnace, Ketley, Woombridge, New Hadley, and Donnington. A good instance occurs in the valley extending from New Hadley to the Oaken Gates. Near Woom- bridge church the Ketley fault throws up, to the eastward, the lower series of the coal-measures, the strata cropping out successively on the sides of the hills, leaving the lower coal-beds in the valley; but owing to the deep and extensive denudation in this valley, the coals are frequently removed, and at other places are immediately overlied by the gravel, and cannot in consequence be worked. The denuding action of the water has here worn a deep and precipitous channel, on the north side of which the truncated coal-measures being cut off almost vertically, the gravel filling the channel acquires, in a few yards, a thickness of above 100 feet. It thus appears that the drift has accumulated principally in valleys, hollows, and narrow channels, but that it spreads occasionally, in decreased thickness, over the high grounds*, materially modifying or leveling the more consider- able irregularities of surface. Marine shells of recent species are occasionally found in the upper gravel. Amongst them are specimens of an Ostrea and of a spiral univalve much broken, but apparently of the genus Turritella f. * The frequent occurrence of this drift interferes greatly with the examination of the surface rocks, preventing, in the more level districts, any natural sections from being exhibited. + In Mr. Murchison’s account of this drift in its extension over Salop, Cheshire, Worcester- shire, &c., the Buccinum reticulatum, Dentalium entalis, Littorina littorea, Tellina solidula, Car- dium tuberculatum, Cyprina Islandica, Turritella ungulina, with fragments of Venus, Astarte, and Donax, are stated to have been found in this gravel; and amongst the localities quoted is one near Wellington. See Silurian System, p. 533. Geology of Coalbrook Dale. 463 CoNncLusION. In the foregoing pages I have confined my observations solely to the geo- logical description of the coal-field and the accompanying formations, with- out reference to any hypothesis deducible from the details. I now propose briefly to restate those facts, and afterwards to draw such conclusions as they may appear to warrant, I intend, in the first place, to investigate the mode of deposition, and to endeavour to ascertain the age of the coal formation ; secondly, to review the nature and effects of those disturbances which have so powerfully affected the several formations ; and, thirdly, to examine the nature of the agents, which have since acted upon and modified the surface. “The first point involves the disputed question, whether the coal was formed from vegetables which grew upon the spot now occupied by it, or from vege- tables transported from a distance. It has been shown that each stratum of ironstone and several of the beds of shale and sandstone are characterised by peculiar organic remains ; and in some cases of a most decided nature. Thus the “ white flats” are distin- guished by several new and peculiar species of Trilobites, and the Penney- stone measures by Orthocera, Spirifers, and Nautili. From observations upon those beds which admit of ready and extensive examination, it has been ascertained, that the northern division of the coal-measures can be divided into deposits alternately characterised by marine with some fluviatile and ter- restrial remains, or by solely freshwater and land exuvie ; and it is not impro- bable that a further inspection of the less exposed strata will enable future observers to establish a greater number. At present I know of five decided alternations, and of two which are doubtful, as only fishes have been found in them. Terrestrial detritus .... Such at present appears to be the character of the thick and unproductive strata lying above the Chance Penneystone. 1. Marine and Fluviatile. Chance Penneystone. Terrestrial and Fluviatile. Downwards from the Chance Penneystone to the fungus coal inclusive. 2. Marineand Fluviatile. Bas above the blackstone coal. Thomesivall o64o00 6000 Blackstone coal. 3. Marine, Terrestrials | Blackstone, ironstone. and Fluviatile...... ILeMmeiAll Go oadooose To the ballstone inclusive. 4, Marine? or Fluviatile. Bas over top coal. Terrestrial, Fluviatile .. To the blue flats inclusive. 464 J. Prestwicu, Esq., on the 5. Marine, Terrestrial, : ae White flat stone. Fluviatile ........ Terrestrial............ To flint coal bas. 6. Marine? or Fluviatile. Flint-coal bas. Terrestrial .......... Flint-coal and underlying sandstone. 7. Marineand Fluviatile ? Penneystone ironstone. Terrestrial and Fluviatile. Strata below the Penneystone to the base of the coal-measures*. These alternations necessarily lead to the inquiry—whether they were pro- duced by oscillations of the land, whereby it was at one time submerged and covered with a stratum of silt containing marine exuvie, and at another raised and converted into a marshy tract, overspread with a thick, luxuriant vege- tation, and harbouring in its shallow waters numerous freshwater shells, to be again submerged and overlaid by another marine deposit,—or whether the phenomena cannot be accounted for by supposing, that the coal-measures were accumulated in an estuary, into which flowed a large river, subject to occa- sional freshes charged with the testacea peculiar to its waters and the vege- tation of the adjacent districts. In examining the various strata, we obtain in their lithological changes some clue to the transporting power of the water by which the beds were accumulated. As there is a remarkable difference in the range of organic remains, attended also by corresponding but minor changes of lithological structure between the northern and southern portions of the coal-field, it will be necessary, in describing the mode of deposit of the measures, to refer as nearly as possible to the central districts, where the principal phenomena of north and south are co-existent. _The reader must bear in mind, that in the north of the coal-field at Donnington and Woombridge, the animal reliquiz exhibit their greatest variety ; that in proceeding south, they gradually de- crease, the change commencing with those highest in the series; and that they eventually disappear with the Penneystone stratum at Broseley (see Plate XXXVII.): certain general lithological characters, subject, however, to considerable local variations, are co-extensive with these changes. When reference is made to local phenomena, it is always mentioned. Immediately succeeding the marine deposit of carboniferous limestone are thick irregular beds of coarse sandstone, frequently passing into conglomerates, and containing a few impressions and casts of imperfect fragments of vegetables. They graduate upwards into fine sandstones and sometimes into shale. The crawstone, which occurs in one of these sandstones, contains numerous beautiful casts of the Stigmaria ficoides, of which the internal structure is sometimes preserved, * The diagram of the coal-field, Pl. XXXVII., exhibits proofs of these alternations. Geology of Coalbrook Dale. 465 also several species of Unio—the first trace of animal life we meet with in the coal-measure. The same Stigmaria is also very common in the little flint-coal and sandstone above the crawstone. The characters of this series, therefore, apparently indicate a period of considerable turbulence, or a sudden and violent change in the condition of the land succeeding a long period of repose, during which the carboniferous limestone had been formed. In the lower strata the thick sandstones and conglomerates, the great and rapid changes in se- veral beds at very short distances, and the local occurrence of one bed and the absence of others at greater distances, all indicate a period of much disturbance and sudden changes ; but these signs of varying velocities gradually diminish as we ascend the series. Such effects we are natu- rally led to expect, if we consider the great difference between the characters of the coal-measures and those of the carboniferous limestone. In the latter, we have every indication of a formation gradually accumulated in the ocean during a lengthened period, whereas the structure of the for- mer denotes the proximity of dry land, and bears evidence of violent operations by which one portion of the bed of the ocean became dry land, while another was partially raised and converted into an extensive estuary, receiving the detritus borne down by the rivers intersecting the newly- exposed land. The abrasion of the recently elevated tracts, then but barely covered with soil, may account for the prevalence of thick, unproductive, coarse sandstones in this lower division, while the presence of a few coal seams, and of the crawstone with its well-preserved specimens of de- licate Stigmaria, higher in the series, may have arisen from a more abundant growth of plants during a period of calm, succeeding the first effect of the change of level. The recent origin of the estuary and the violent action attendant upon the transport of the conglomerate, would account for the absence, in the lowermost beds, of marine Testacea. The next series of strata, extending from the clod-coal to the Penneystone, consists, in the lower portion, chiefly of thick beds of shale, containing large quantities of finely-preserved vegetable remains, and alternating near the bottom very frequently with seams of coal. In the south of the coal-field some of the shales pass into sandstones, which always inclose an increased number of plants in passing from a fine to a coarser grain. This point appears to me to be important, and to prove either a greater supply of vegetable remains from a body of water more widely extended and of greater transporting power, or a more complete decay in the plants from the slower accumulation of the fine-grained sandstone. The coal-beds are far more persistent in this than in other portions of the coal-measures. Each bed is generally underlaid by a thin seam of indurated clay, containing few or no fossils ; whereas the overlying stratum suc- ceeding the few inches of fine bituminous shale, immediately incumbent on the coal, is coarser and thicker and abounds in vegetable casts and impressions, which decrease rapidly in number as the distance from the coal increases. From these facts, I would infer, that the lower clay and shale were gently washed down during short periods of calm, and of rapid vegetation, and that the overlying coarser silt and sand were accumulated by increased volume and violence in the current, consequent upon the floods which originated the coal seams. It nevertheless appears probable, that no lengthened period elapsed between the uprooting of the plants and their entombment, for the casts and impressions in some of the roofs of the coal-bed, exhibit perfectly the delicate external organization of several genera of ferns and Lycopodicez, and sometimes retain a portion of their vegetable tissue. The period, therefore, during which this series was deposited, seems to have been one of repeated but not violent changes. Thus far, in the portion of the lowest measures which we have reviewed, the unsettled state of the land and water appears to have checked the increase of animal life. We now, however, ar- 466 J. Prestwicu, Esq., on the rive at a deposit, the Penneystone, indicating a long period of repose. This ironstone measure, in its interesting fossils, unfolds to us the existence of numerous marine animals—the great Megalichthys, the Gyracanthus, the Cyathocrinites quinquangularis, together with a considerable number of Testacea*; but associated with them are a few large Unios, and remnants of vegetables. The slow accumulation, it is probable, totally prevented the preservation of the more delicate parts of plants, and permitted only small and worn portions of stems or branches, which resisted the lengthened exposure, to be preserved from destruction. So tardy was the accumulation of silt, as proved by the fine and homogeneous texture of the stratum, by the existence of shells in all stages of growth, and by their general and uniform dispersion, by the absence of the finer and more delicate parts of plants, and by the presence of parasitical animals attached to the re- mains of fishes and shells, that unless the body were encased in an ironstone nodule its decay appears to have been almost inevitable ; for, as before mentioned, the fossils are, with rare excep= tions, consisting chiefly of the scales and teeth of the Megalichthys, found solely in the ironstone nodules, and not in the shale. The numerous Coprolites attest the existence of many fishes. Yet where are their remains? Here and there only are a few preserved from that destruction to which long exposure most probably consigned the greater bulk of them. A considerable interval seems to have elapsed between the accumulation of the Penneystone shale and the deposition of the overlying coarseish sandstone called the flint-coal flint; for in the north of the coal-field, thick tablets and large blocks of ironstone, containing a peculiarly crystal- line compound of carbonate of iron and carbonate of lime called curlstone, lie on the top of the Penneystone shale; and in the same situation in the southern districts of Madeley and Broseley occur extensive tabular masses of conglomerate ironstone, varying in thickness from 1 to 12 inches, and consisting sometimes entirely of small white quartz angular pebbles, varying in size from a pin’s head to a small marble, mixed with grains of white decomposed felspar, and imbed- ded in a matrix of ironstone, with which it occasionally forms thin alternating layers. This con- glomerate also contains small rolled pebbles of ironstone, characterised by the fossils of the Pen- neystone measures. We thus have proofs of a transition from a long period of calm and repose to one of some vio- lence, which apparently was continued in a modified form during the deposition of the overlying stratum of sandstone; for upon leaving the Penneystone, we suddenly lose all traces of animal * Mr. T. Bell has recently called my attention to a singular fact connected with recent fresh- water Testacea; viz. that in old shells the umbones of bivalves and the apices of univalves bear traces of erosion more or less according to the age of the animal. This circumstance appears to hold good in all cases except with light and fragile shells such as the Lymnea. Now it appears to me that this fact may be of considerable value as applied to the discrimination of marine and freshwater shells in a fossil state, and as a test whether several fossil shells supposed to be of freshwater origin, yet found in situations difficult to reconcile with that supposition, are to be considered indicative of the presence of freshwater—such as the extensive series classed as Unios. I have examined a considerable suite of shells, apparently belonging to this genus; but as they are all casts in ironstone, I have not been able to come to any very decided opinion ; neverthe- less, the greater number of specimens exhibited no trace of erosion, but a few, and amongst them several from the Penneystone, decidedly did. Geology of Coalbrook Dale. 467 life—the increased transporting power of the water accumulating thick beds of sandstone, and entombing large quantities of gigantic Sigillaria, Calamites, and Stigmaria. The vertical position of a few of the larger specimens, with their roots attached, does not mar the supposition of their having been transported, for the greater number of these fossils lie horizontally, or nearly so, and at all levels. The gigantic character of this Flora, so different from that of the other strata, appears to be a natural consequence of the long period of quiet during the accumulation of the Penneystone measure—a period during which the vegetation of the country flourished vi- gorously and uninterruptedly. May not part of the flint-coal which reposes upon this sandstone have beenderived from the woody matter of the large vegetable casts entombed in the rock ? The flint-coal lies upon this sandstone, and is, in the central and northern districts, covered by a thin stratum of a very fine, dark, bituminous shale, containing a few scales and teeth of fishes, and generally, in its upper part, a band full of crushed Unios, resulting probably from a suddenly increased fluviatile action succeeding a period of calm. This is further confirmed by the inter- polation between the shale and the white flat measure of a stratum of coarseish freestone or sand- stone, occasionally conglomeratic, which commences at Ketley, and rapidly attains a thickness of several yards, affording almost the first indication of a strong local action from the north-west- ward, and forming a thick and irregular sedimentary deposit betwixt the regular and quiet accumu- lation of the flint-coal bass and the white flat measure, which stratum thins out northward of Ketley; but to the southward of Ketley is in immediate superposition with the flint-coal bass. It is in this portion of the coal-measures, that the important variations, both in the organic remains and in the lithological structure of the northern and southern districts, begin to show themselves distinctly. The white flat measure, which then succeeds, again brings us to a period, when conditions prevailed somewhat similar to those under which the Penneystone measure was deposited. Though the epoch was probably of shorter duration, yet we here find several new species of the Trilobite family, and a large proportion of Unios and of plants, the more delicate parts of which are well preserved, indicating, probably, a greater rapidity of accumulation than in the Penney- stone ; whence the abundance of fluviatile, and the scarcity of marine Testacea, The system overlying this stratum consists of numerous alternations of rather thick coal-seams, shale, and ironstone, and subordinate, fine-grained sandstones. The numerous remains of Sigil- laria, Lepidodendra and other plants, generally associated with Unios, which occur sometimes, as in the blue flats, in great quantities,—the frequency of the repetition of the different strata, and their extensive and uniform persistence as far south as Lightmoor, appear to indicate many changes and extensive but not powerful floods. Incumbent on the top coal, the highest in this last series, is a thin bed of fine bituminous shale, which again proves the existence of the Megalichthys and other fishes, probably marine, whose de- tached and scattered remains are preserved almost uninjured. Next follows a deposit, apparently of rapid but tranquil accumulation, forming the ballstone mea- sure, astratum characterised by the delicacy and beauty of its Flora, and by the absence of animal reliquiz. The impressions of the leaves of the Cyclopteris, Neuropteris, &c., are so perfect, that itis impossible to imagine the fronds could have been transported by violent currents, or that they could have been long exposed to the action of the atmosphere and the water. The slightly rumpled appearance of the delicate and unbroken tissue of the Cyclopteris orbicularis, the sharp- ness and distinctness of every fibre of the Newropteris gigantea, and other plants, could only have resulted from an immediate and tranquil entombment. VOL. V.— SECOND SERIES. 3P A468 J. Prestwicu, Esq., on the The ballstone is overlaid by a series of thick beds of sandstone, with subordinate shales, and a few limited seams of coal. The lithological characters mark a period of some duration, disturb- ance, and change, with a few intervals of quiet, as during the deposition of the brick measure and the blackstone. In the latter deposit we again find a few marine and fluviatile Testacea associated with land plants. At Donnington, the thin bed of fine bass above the blackstone coal contains numerous well- preserved Lingule, with other marine testacea and remains of fishes, indicating a nearly complete cessation of that fluviatile action, which in other parts of this series.accumulated such quantities of Unios. The strong and intermitting fluviatile action was prolonged upwards to the Chance Penney- stone, where another considerable interval of calm occurred, during which marine Testacea again lived and multiplied, as is proved by the abundance of the Leptena scabricula, associated with a few other marine Testacea and fishes. The characters, above described, of the strata between the top coal and the Chance Penneystone are limited to the north of the coal-field, to which the accompanying coals and ironstones are almost entirely confined. Above the Chance Penneystone,—the thick preponderating beds of sandstone,—the change in the mineralogical characters of several beds,—the scarcity of vegetable and animal remains, yet evidently with a continuation of a powerful aqueous action, probably resulted from a considerable mutation in the condition of the adjacent land, to which we shall recur shortly. It will be now necessary to point out the principal changes of lithological characters and animal reliquiz of the coal-measures in their horizontal range: lst. The lower series of coals, up to the Penneystone, are tolerably persistent throughout, from Donnington to Broseley ; but above that stratum, the coals and ironstones, with their asso- ciated marine reliquiz, have a gradually diminishing horizontal range southward, so that the upper beds are limited to a small district in the north of the coal-field. (See Diagram, Plate XXXVIII.) 2ndly. The absence of organic remains in the Penneystone at Donnington, and the gradual and rather abundant appearance of marine reliquiz, accompanied by a decreasing thickness of the stratum as it trends southward until it disappears at Broseley, deserve special notice. A narrow band of limestone, apparently of fresh-water origin, makes its appearance in that district higher in the vertical range of the measures. 3dly. Other changes, claiming particular mention, are the presence of numerous beds of red and variegated clays and marls, and calcareous sandstones, in the south-east of the coal-field, and the expansion of many of the shales and sandstones to the northward, with the abrupt thinning out of all the coals and ironstones above the Penneystone between Donnington and Lilleshall, accompanied by an increased importance in the upper series of soft conglomerates and sandstones. 4thly. It is necessary to mention the great variations of lithological character, and irregularity of range of almost all the arenaceous strata. The conclusion, therefore, which I think may safely be drawn is, that the deposition of the coal-measures commenced immediately subsequent to some great convulsion altering the relative level of land and water ; and—judging Le = Geology of Coalbrook Dale. 469 from the peculiar lithological character, and the preponderance of large and aged corals in the carboniferous limestone, conjointly with its gradual thinning off in its range southward, indicating its accumulation in a tranquil and rather shallow sea, undisturbed by the immediate influx of any large river, yet evi- dently receiving, as the sea became deeper to the northward, a large supply of fine silt, perhaps from the northward—it is probable that the change con- sisted of a subsidence along the south-west shores of the sea in which the lower carboniferous limestone was accumulating; for had the movement been elevatory, a portion of the bed of the ocean, and consequently of the carboniferous limestone, must have been exposed, and outliers of that forma- tion would most probably have existed at a distance from the coal-measures, which now, on the contrary, overlap its edges. Again, we could not expect to find in the detritus derived from land recently elevated from the bottom of the sea, remains of land plants ;"whereas these remains are extremely common, and we even find a thin and irregular bed of coal at the very base of the mea- sures. We may consequently infer, that an extensive area experienced a con- siderable subsidence, depressing one portion beneath the sea, and materially modifying the physical geography of the remaining dry land, giving rise both to a new line of coast and to a new system of drainage, enlarging some rivers and forming others. No sooner, indeed, do we pass into the coal-measures, than we find, throughout their entire vertical range, evidences of strong river action in the presence of transported vegetables, of which the majority are, according to A. Brongniart, such as might be expected to have flourished on low and marshy lands ; and fluviatile shells, intermingled with the marine Tes- tacea of the sea into which they were drifted. From these great mutations would probably result—at first, barren conglomerates and coarse sandstones, succeeded by strata produced by a more fixed and settled order, as the effects of the preceding paroxysms were gradually softened down and effaced. Vege- tation, it may be inferred, flourished on the land, and Testacea and fishes mul- tiplied in the sea, during those intervals of disturbance arising from inunda- tions and freshes of the river, which flowed probably from the south-westward, carrying its detritus into a sea, where the dispersion of it was apparently limited by a current from the northward. While on this subject, a few remarks may be made on the debris forming he coal-measures, and on the origin of the ironstone. The fine-grained quartzose sandstones—the constantly recurring pebbles of white quartz— the general diffusion of mica, and occasionally of felspar and slate rocks, evidently denote an origin in the older stratified formations ; whilst the red 3P2 470 J. Prestwicn, Esq., on the clays and marls, with the subordinate calcareous seams of the southern dis- tricts, may have been derived from the old red sandstone and upper Silurian rocks. We find the peroxide of iron distributed in a greater or less degree throughout the whole of the coal-measures ; but it is in those beds of shale only which appear to have been formed gradually and slowly, that we find it in any great plenty. This proves the abundance of iron in the rocks from which the silt was derived. Now we know that all trap rocks contain more or less iron. Dr. Withering found in those of Staffordshire, 20 per cent.* ; Klaproth, in those of Hazenberg, 20 per cent.t; and out of numerous specimens of basalt which he analysed, Bergman found, upon an average, as much as 25 per cent.t. As the ironstone itself contains only about 33 per cent. of iron, it would require no very extensive degradation of trap rocks to produce a bulk of ironstone equal to the entire volume of that existing in the coal-measures ; whilst the residual silica and alumina, in the proportion of about 73 of the former to 27 of the latter, give nearly the composition of the ironstone shales. As a further support of this hypothesis, I have found, in several of the con- glomerates of the coal-measures, traces of the debris of igneous rocks. It has also been shown, that the carboniferous series frequently reposes upon beds of trap and basalt. Irom the soft and friable texture and rapid disin- tegration of many of these rocks, when exposed to the action of the atmo- sphere, they would admit of great abrasion, and afford ample materials for extensive beds of ironstone. The presence of titanium in the iron ore (see table of minerals, Appendix B.) tends to corroborate its derivation from these igneous rocks, as that metal is of very common occurrence in them. According to Mohs, sphene is found “in beds of syenite, and other trap rocks§.’” Dela Beche states that ‘‘ Basalt is supposed to be essentially com- posed of felspar, augite, and titaniferous iron || ;” whilst Berthier says, “ mais c’est surtout dans les roches volcaniques, que le titane abonde ; il y est tou- jours combiné avec le fer et le manganése{.” It will readily be seen that the Coalbrook Dale coal-field differs greatly, both in its lithological character and its organic remains, from most of the English coal-fields. The latter are in general nearly destitute of animal reliquiz, and exhibit but few conglomerate strata, whereas the former abounds in both. * Conybeare’s Outlines of Geology, p. 139. t Ure’s Chemical Dictionary, 3rd edition. + Ibid. § Mohs’ Mineralogy, translated by Haidinger, vol. ii. p. 376. || Geological Manual, Ist edition, p. 122. q Essaies par la Voie Séche. Paris, 1834. Vol. ii. p. 112. . ee Geology of Coalbrook Dale. 471 In the Coalbrook Dale field the mountain limestone has but a trifling com- parative thickness ; the millstone grit also is entirely wanting below the coal- measures ; and as the organic remains present a far closer analogy to those of the carboniferous limestone of Yorkshire and Northumberland than to the coal-fields of those counties, it appears very probable, that this coal-field is of older date than most of those in the north and south of England. The coal-fields to which it bears the closest resemblance are those of North Northumberland, Durham, parts of Yorkshire and Scotland. Many of the Conchifera and Crinoidee, the Conularia, the Megalichthys and Gyracanthus, which characterise the Coalbrook field, are abundant in the subordinate beds of limestone and ironstone in the Scotch coal-fields. Mr. Phillips, in his excellent Illustrations of the Geology of Yorkshire, di- vides the carboniferous formation into three groups, viz. the Millstone grit, the Yoredale series, and the Great Scar limestone, each characterised by peculiar but variable lithological composition, and, during the prevalence of like conditions, by organic remains of a generally similar character. Upon comparing the sections of Wensley Dale, Whernside, Penyghent, and Coverdale* with that of Lilleshall (pp. 425, 427), the general similarity in litho- logical structure is very striking ; there are the same alternations of arenaceous strata with subordinate limestones, characterised by the presence of numerous Polyparia, some Brachiopoda and Cephalopoda, but with very few Crinoidea. Again, the resemblance between the black limestone group of Yorkshire and that of Steeraways, both characterised by the presence of Lithodendra and large Leptene (Producta), induce me to consider the limestone strata of Lilleshall and Steeraways as the equivalents of the Yoredale series, which Mr. Phillips has shown to attenuate and become finer grained as it ranges southward. Supposing, therefore, that these limestones represent the Yoredale series, ora portion thereof, it is probable, that the measures of Coalbrook Dale, which immediately succeed, are coeval or synchronous with the lower millstone grit, and that the variable fine conglomerates and concretionary shales, form- ing the upper portion of the coal-measures, and eventually throwing out the coals and ironstones in the north of the field, may be the representatives of the Upper Millstone or Brimham grit. The greater abundance than is usual in the millstone grit, of many marine remains of the limestone groups, might arise from the augmented vertical range, in this district, of those con- ditions suited to the existence of Testacea, and which prevailed during the * See Phillips’s Illustrations of the Geology of Yorkshire, Part II. pp. 37—57. 472 J. Prestwicu, Esq., on the deposition of the lower series in the north of England ; still, from the littoral and fluviatile character of the deposit, it is possible, that its interpolations of freshwater and land detritus with that of the oceanic currents, may have been prolonged during the whole remaining carboniferous era, and even have continued to that of the new red sandstone, for it has been shown that in parts of this district, the coal-measures appear to graduate upwards into the lower new red sandstone ; and Mr. Murchison has proved that in most of the adjoin- ing fields, there is a conformable transition between these two formations. Upon the second point, which refers to the nature and effects of the disturb- ances, but little need be said. It has been shown in the observations upon the faults, that the whole of the Coalbrook Dale district has been protruded * through the new red sandstone, and that this angular promontory of up- lifted rocks forms merely the extremity of the principal zone of the Silurian system described by Mr. Murchison. This form of the detached area is due apparently to the intersection of two lines of disturbance. The more im- portant one constitutes the axis of the Wrekin, with its parallel longitudinal dislocations and anticlinal axes, ranging nearly S.W. and N.E.; the other trends rather N. of N.N.E.; and the intersection of these two converging lines gives rise to numerous diagonal, connecting dislocations. We have no direct evidence of the precise period at which the dislocations were effected. It can only be stated, that they took place subsequent to the deposition of the Lower Red Sandstone system. From the details in pages 447 and 457, and from the description of adjacent coal-fields by Mr. Murchison, it is evident, that the coal-measures of Coal- brook Dale are but a part of an extensive deposit from which they have been disjointed and separated by great subterranean movements. Hence, we may infer, that a portion of that deposit still remains intact below the overlying formations of new red sandstone of Shropshire, Cheshire, and Staffordshire ; and it is not improbable that, by other lines of disturbances traversing these counties, the coal-measures, although covered by the new red sandstone, may * I use this word to signify merely the change, by subterranean agency, of the relative level of these two sedimentary deposits, as 1 consider that this effect being due to the contraction of the interior nucleus of the earth, the collapse of the strata resulting therefrom would produce a gene- ral and tolerably regular subsidence of large central areas, accompanied by the elevation, fracture, and tilting of narrow longitudinal segments ; whence the strong lateral pressure evinced in the anticlinal axes and along the lines of fault, and the absence in this disrupted district of open fissures, such as would have resulted from the tension attendant upon an independent expansion of a portion of the interior nucleus. + See Mr. Murchison’s Silurian System, p. 79, et seq. Geology of Coalbrook Dale. AT3 be, in some places, at no great depth from the surface. But lines of disloca- tion are traced with difficulty through that formation, the different strata of which are rarely characterised by fossil remains, or by any great dissimilarity of lithological structure. Underlying the new red sandstone, these coal-measures would probably have remained yet for ages unknown, had not portions of them been broken off and uplifted, and this too in an order beautifully commensurate to the wants of man. A few seams of coal and ironstone cropping out to day, originally led to the discovery of a valuable deposit ; and though the means of working them were then limited, yet was the supply easily attainable. In time, as the demand in- creased, so did the means multiply, and thus were successively brought into use, the gradual descending downcasts of the coal-measures, from the outcrop at the Steeraways, then over the Ketley fault to the Lightmoor fault, which delayed further progress for some time, but was at last passed ; and now when that stage of the coal is exhausted, there appears every prospect, though at still greater depths, of a further supply, and probably equal to any with which we are yet acquainted*. The third and last point claiming consideration, is the nature of the agents which haye modified the surface of the country. It having been shown in p. 452 et seq., that the disturbances which affected this district not only de- stroyed the continuity of the sedimentary deposits, but placed their fractured portions on widely different levels,—it follows, that if the surface had not been denuded, it would now present great irregularities, and even mountainous ridges, exceeding, in some instances, 2500 feet in height. The existing surface is, however, comparatively flat; and it is therefore evident, that, in the ele- vated central, western and southern districts, where only the lower divisions of the coal-measures remain—all the upper strata, amounting to not less than 800 feet, with at least the whole of the lower new red sandstone, which was pro- bably more than 1200 feet thick, have been removed; and that in the valley of the Severn, as well as in that between Barrow and Shirlot Hills, not only have the new red sandstone and coal-measures been completely denuded, but also 500 feet of Wenlock rocks in the former instance, and 600 feet of old red sandstone in the latter. Notwithstanding, however, the extent of these effects, still the diversity of * The reader must not however infer, that coal and ironstone strata necessarily exist everywhere beneath the new red sandstone of the surrounding districts, because it has been shown, that although the coal formation, as a whole, may be extensively persistent, still from its littoral cha- racter all the terms of the series are liable to rapid variations. The coal and ironstone will be limited to an area, proportionate to the strength of the fluviatile currents. ATA J. Prestwicu, Esq., on the hill and dale must be ascribed, as before stated, to the disturbances which have traversed every part of the district. Whether the change of relative level and the subsequent denudation were effected slowly or violently, are questions too complex for me to investigate in this paper; but I am tempted to infer, from the superficial obliteration of the faults, that the change in the levels took place under water, and that the surface was long exposed to its action. I would also infer, from the debris of Silurian rocks distributed through the drift, that during its accumulation, cur- rents flowed over the coal-field from the west and north-west. Although the remains of Testacea in the gravel are scarce and much broken, still they suffice to prove the identity of the shells with those of exist- ing species, and therefore to establish the recent withdrawal of the waters. Geology of Coalbrook Dale. APPENDIX. A475 SECTIONS OF COAL PITS. (A.) LIGHTMOOR WIMSEY PIT, 1788. Ne hee bt ale Yds. Ft. In. ; : : 31. Pale OOirevisnlesievisieveesivcesenaesivasis o rom Plymley’s Agricultural Survey of Shen ne) 32. Coal (the ak COGN) icessscseecerees meets 2 0 : : : See en |oo-clunchyofia;danks blue) sescacessteeconses 1 6 1A peed, and mixed soil (gravel 6 0 0 34. Coal ie re coal, aS by a few , Sa eek BE eT PRE inches of grey earth)...........scss008 1G Dee bale ole) clunc hy ececcccssalesseeesacteass - 16 0 0} 35 crunch iA a Blue, with coal ia dhe - Say Ee RaR Me ge roa Sy Pf vite middle17 in. thick, (the coal is called Bt hiree sulphur coals, divided by pale ete ao Sake ccece i oeeeeeseece ecceres 1 10 blue earth, 2 in. between each...... 1 ae Tea 37. Lin, Ge bOe: Wha 8 see Em iui 2 0 6. Strong clod, mingled pale blueandred 16 0 0 : Rica a ( saved vipa ft PAL ; 7. Brown rock (the sulphur coal rock)... 7 1 0 38. A ble ag aia O naaences mae es Te 1 2 8 Three sulphur coals, divided by pale eas C rae a © sscee coe oe ceeecesene- 0 6 blue.earth,.4or 5 in. betweeneach. 3 0 0 ; ; Coal (the best coal)’ ....:.....00008 Sieaisieis 1-36 GO), TYRES GEE Gooccosnecocoancdocoonoconeccbe 482 08 lee Black basa or slatess...-2-..0.0-- eg ae UG), JE alleyrqscl alyi@ posonocooserepsoodonroncoos a O 0 oo ee Pee si nee Pine is hac Fe 2 11. Rough rock (full of dark brown hard 43. Coal aoe arent CeoergeeasecceWexser 6 pebbles and ironstone).............00. 7( ee Cled ¢ rig Je hie ) sesnesssnene ee 1 10 12. Bind (pale blue clod).....s...:scesseeeeee Te Oss On bial aay emt ea TT coe cuties ; 8 13. Stone clod (ditto) in which lies a bed 7s Cittl ue pay 2 ee ee ae = of ironstone called ballstone ......... i Y - Little Hint (a rock of a dark grey min- ide, LET eels QIN GononcogoanocubccodpanoosedocoooD it gled with pebbles and ironstone)... 16 0 0 15. Coal (top coal, exceeding good fuel)... 1 1 0 16. Top eoal toush (a dark blue earth and 47. Di f lof 2h SL ER aD 1 - Die earth, a pale blue hard clunch 17 Ape ihe ie car ) i i 1 ‘A (Wenlock shale) said to be ...... .. 100 0 0 18. Slums* (blackslaty earth and a heaving TING ASTIN) iets eltelsalatsletoieldaleelsislelsfelsisicrsste INGUSOE! (cacrsoerdscqcscccr-esccosescenaltseut.W.SiueWaascaskeheastteeks Recess 28. White clunch ...........+6 ..Blackish grey dry clay sageeathneoh dateanes oo aceonbacnscemnsetas Aes Gon 29. Grey rock........scescsreseses Llight| grey, Tine SAndsLonel...C..ouis..0sesnsosnatocansevoesteocdens pareeence 30. Brick measure .......+...+0+ Alternating strata of grey ironstone and dry clay ........s..seeeeeeeee Billet SINGMDASS pasha coca. aioe ncsens slack dry Clay s.c-sacscutsenctirce senccrnescoanpanebaternets atdenteraeausteees SUA NMGlecscescscaccssccseces concn Brownish grey, very fine, argillaceous SADAStONA paxensecsenre eetheet edaqusessence Specenosnaco: - Beocenclcle uae 45. Yard coal poundstone ....-. Black dry clay resembling acs ...bed.n uth dorduunt acetone wee 46. Quoice neck............ece00e Greyish black dry clay with very shining surfaces ..........s:00ec0008 47. Blue flat .....weccrecereeeeeee Strata of brownish grey ironstone in dry clay, in the upper part MLOUUI ABATE A odo dba cotac Wocusccarensaseuccsscouce's cat eee eta 48. Pitcher basses ...s.scccssseee Black bass or indurated schistose clay (schiefer Thon.) ike; No. 36. 49. White flat......... Sepeeece suet Beds of ironstone in a black grey shivery dry¥:claynss. fwh ced. 50. Flint coal rock...........000. Fine whitish sandstone, with some mica ...... Secbeubbce see tebicceeeeare 51. Flint coal roof ..........0s00s Blackishipreyidry clay ........:0sesnsmmsnaassaseuleestacascesaeders eee cae 52. Flint coal ...corewcessseoees ...Good burning coal; at Madeley Wood it is charged with salt water BS. ARNG: sraceacctenteeceslemmer cies Fine grained @hitish sandstone, used for building ..........s0-seeeee0s 54. Penney measure ......+0+04- Blackish grey dry clay, containing iron nodules; in the upper part of this stratum, close under the flint, the coal is found .......... BS, Sulphur coal. .......c.csccers Coal, containing a great quantity of pyrites, which are used for vi- erigls being cheap it is chiefly consumed in burning brick, line, BECHER Mesrivcrccsiedeeentacleescccs'ss Basducddadoaadadsobacocusanssdans 56. Sulphur coal bass............ Greyish black dry clay ..........2++++ sade sc cceccntosessecectecnentennennce 57. Upper clunch coal .......... Good coal, but being thin is not got except when the coal above is worked OM Gneteremsnepoaends ans sarge acdssaa,sscceecscseesteccccere nee: BG -eUppericlinch).......-cecssse- Light grey shivery clay, much shed for fire bricks...... PPPS 5 fait Wb 5OeClumehvedaly..ccsvescoaseesses INeversrotieectersnaecearcrtseoccsoriesecacsodcocscdsvescxscccscecsceemeaetere: 60. Lower clunch .......... .....Grey dry clay used for fire bricks ...........ceccsscsssevenes Sopoasonnoso coo (=) oN SRK NOS coco RPOoONFRNOCOCSO OR SK eS NOK eS SH OCH N = Br nweccron = mb onzao ceooococoocoocecooocs GQoeooeoodescso cosoo aoccoccoocroo coococse So 10 Geology of Coalbrook Dale. ATT - No. Yds. Ft. In. G1. Wwo-fo0t Coal covcce+seeaeoses SOMEUMMES FOL. osescoscersseecascececscassesoscoccctors FeincernobG scoopncocona «WP (0) 62. Linseed earth ............00 Black grey dry clay, used for fire bricks ............sscescosossoseescave a0) 0 63. Best coal .....0.sceceesseesers This is the best coal; in the northern part it is 9 inches; but ay Quo sO the southern ae a pannbesncdae AaGaed Scpaderdcadada S0dad08 prootncas HIF 0 ivanGlercod We ercsaseseeacoss ss Tsithesbest suposs COAllssnctur-miseececcerecrns acocimoqgducedoonoEcnecde pend Se Beanock reaccodaooooee Beeneee Brownish grey very slippery dry clay, good for fire pricks'vesceesen: OB) GG= WloducOdlscccaccaccesccrcceecs Used for smelting in all the Shropshire iron cticooder BEACHoOBES Sracesoosy tly Nn G) 67. Paleiblue clodis..ccccs.ccasee Bluish grey clay with vegetable impressions v stestegeceeeees Seeceeeeeune Ih th a 68. Sandstone.........esscesereeee Fine argillaceous sandstone, containing vegetable impressions ...... 3 0 0 69. Little flint coal...........+0.. Good) burning coal... ..sccscscss-cs coteansadéodnaqboSaHocn eisciesiecisenios ca WO Be @ COMMUMIPIOTUIN Er. .csscss22sceceene ery tineswiiter sandstone. o.s-asacccontcsescesceesececececttcarcesster Stoceay Shi tldy Dy (0) ait LITTLE WENLOCK. No. Yds. Ft. In. No. Wdsz)Ht-n.)} 19> (Penneystone ......0.c.0-co soscsreceeee 9 O O BROAN iassenensescacenscaeoe Seswisiqcieen'en tts eat 48101210) 20:-Sulphur coal) ........-.-- Base aceseeeties os 24 WO DMNVGUOWSEONE CALE sireanicniesacerouciisuwislesied Tid OVHOW h 2H, MBI. sae aeciecarcareete Praneocae Faseeetnee: coo 2). 63 RP PMMESIEL CU oot nics sclne es wiinicivs'olsw'cleiedidceceeee wie on) 10) } 22: Upper iclunches<:..23.0.2.05. CODER S0BI0a08 HO) 4. Ballstone ........... cisehaw steeples seca Ae iOnnOgh 2e— Mower clunchesicscc.cc.ceerceccceeaceence Te) 16 Sy, TNoye @@plansgpeacndnosassospedus aa eissseason 2-0 (0 } 24. Sill coal ..... peceenanteae Gcduascocneo Beer (De 9G) PPO) Olu x oo ce ciassSeisiopeeiowis Sweet ceewace cee O» 1.0 | 25. Two-foot coal rock:.2.0225253662. Setecaces E26 MPMELOOICOAL saj-aenaceaciepsatarensonaseceteent Ongel-. LOs|) 26.) liwo-toot coalic..ctcessccvocecesanet te cees il M83 NeMISASSCSs concsnecacreccecsesccccncesnascaccsore OM 2 AOL Die Rocka cacdess: soccescasnsencetecct cee iG) 9. Dhree-quarters coal .:...0.ce-esccscosess Ole 2 iO) 2S Best COdlecscaacstcce. ceatccec cote econ Oh il ie MONMEV OCG sciewisnincce ses sseiciauescnaesinccianesorte 0° 1. 0 | 29. Randle coal: v.01... ..ccecccceenee Scboceon il lo) Il. Double.coal........... oanacouccs Metered: Dee NNO) oO me loducodl rocks. eeecceccasecamcecest neers 8) (0) 0G) APA ARCTNOVN Ci COAN aisajcinessiowssisielejsiceinasinaioeeee ORNZ AtOul) ol -wbannockencsmcrececcs-costutee er cete res OQ ioe Reem AN COAL sas cnciectuia swans anmasaaesiaisewaunts 1, 0 0 | 32. Smithies and hard coal --/222.2.......... O09) HAMMISASSED: tree catenonesterescrcsseSccexsan oat SO BKON| 39 a ClOGICOSI rt rcccscctccrscaranasteacecoreess Sl) 9 AG MaeMULING COAL TOUS mccccccesexsssionces tease i ae) ) ee MOMMALINECOAll each seseawanceacersuossouse heats 2 4 , 66 011 WIE LITLE LOCK: (ives odesceesceseseissawnses corsets Basset Pit. | Deep Pit. 18. Penneystone measure ........-2...0000 8 0 0| LODGE PIT, MADELEY. yds. ft. in. | yds. he. in. 1), Swale Cell Aooeagoncosoanodnoocdadceccods Zar or ON eS ofleyee cee Se Seb odes Sondecen oat Ope a6. | Omnia A) Upper clunchesi...cc.s-ossesersnerceeaccss Ze OO) ROD. Can aeeicdacnt shee sanssvesietenes W Oe Zeyh a. Zt PAG Sill coal eee rec vcc cee eeeseccccsesescccceseee OY PG 835.(Gronrel sail EUoRbaeecneeen cons 5.0) 6 5 1 0 2A mLower ClINCHES ccsss-asoeeswens seek eeiseictes 2 0 Q)| 4. Brick CF ial a ee Wor pee saya (y AasmMOWwer Si COALy .cencscesscueccsoctoeess Oi whO) ob). Miley Glaynss secceece ssencereees 1 ON Tie eT ee PA MLCOCK: news aina sins sivas conisweortehioswineclssPectons OMT NG 6. Upper part of the rough rock.3. 10) (Su|*3i10)..0 2B TNG@ WOnGOE less soscecsteacceascaenonsea0ns 0 2 0} 7, Peldon pebbly ......... nee OY DG il wo“ 26. Randle coal rock . Ceecccccecsccccecsscosoe bak: 460 8. Lower part of the rough rock10 0 4/1/10 1 0 Piembvan dle) Coal sjscsswaccwscseistbiesisielee coos tk (YM) | Gg), Heaving: arth) .\....0.0scssecss NO) Gy 28) DE pLOUCHIClOGIN .nhecsadsandeidecsqacedertes 4,0 :0:| 10. (Big flint ~ INET, NEAR BROSELEY. No. Yds. Ft. In. 1. Rock and clunch ............ aeaoceees eo ASO K0 PROD es. sas, secssecsce Beane anaacascececcsna5 Oe Ey) SoaClunchy-e.ccescccoresesecs'es She ceseromenens On) 4. Two foot coal...... Sec seacaSeremn eancaeens O22" 0 5s Clonchescsssecssse0s Lwenseceondedcemartens pce ONO, G2) \GaneycOal,.5....0..+ccssccnsercsseusas oes Oy 280 TMP CLAY ne sean sane gehsssassce sano stots cp 1 © Seliopjecallscsssconerensssce codenctocsane-oe 02 0 OM Gloditedesevsscccascsracvaverte misttealole cieteiainis ete 0) 0: 46 HOPNbesticodl-ccesaesscoeescanereee See to dweases 0 2 8 MileyBirerclay.cnsr<.+ssesse0 Sppgscbencon sane eneeey AO LEO PEO lod\coalsawccssenccnteeceseccecesscssecoess Ome2are WB SOROCK Ne sscencccesseseseseeseseses ADORE EROOE 5.42580 Lan biiaticOal tesccaccerstcccssicsscsvescseceass DORRo 41 O11 AMIES FIELD, NEAR BROSELEY, 1. Clays .....scoseeeee Petetccsas eres arsenare ae 620 <0 GLO MRE eca saat oe cesses caacacetiecmpesis Opal 40 BUUIDOCKESOLG ve sasccessscccssesne scone) ackes OMA 36; 4 Olod! wescceeoss Seren eicsee saeteseesoutesete Oe 0 EMO K isccesese perindaedneeec cccnenscanaenvmenar 0, 0° 6 BG mOlotiicvecss ance Subsecee's ogeedeetnmandeeres On 2 PomOCKecceswnesscassccsse mecsveccscadeneepedes 3.4 16 MEOlOtmescscscatciccse tresceccovecceseasanmareen 0" 0 9. Dingle rock ..........scssresseecscnccesoes Oo 98 10. Clod, with four small sulphur eT 07 1 6 MENEAME aecncte va sccncsen eh ecidesemanss TT TRAE sagas acaneee ECOAC Dee Soatesassasss 1) on Nw luie clodecesssecaces ccuncalcs Cesencweesatonan 6° 2500 AB SOLE LOCK 2. beeen: one tcsannckGapenbeaeseees OMG 14, Strong rock......cccscseccevsevevcvveceerers Oe 15. Lime rock (Freshwater limestone: he es 0 TGs sblne ClOdy evccacccss sev sess SesatAnadeee 110) FO UZ Pedi clodlcsccsccssccctsvsecteecstoeeeenescese 10" 30 18. ‘Sulphur coal rock’ .........-.csssescerens- Gy 0 0 19: Sulphur coal'roof <....0.c...-cssescesones 2 0 0 ZO SUPOUL COM tesc.sssnosceileolencacssnpecmns 02 6 21. Sulphur coal Poundstone .............+. eaih 15 PopepriCkiand UilCiClAYS sceesaecsenteuescenns Caeilests 23. Ganey coal rock...............s.scscoocees 7 40 20 AMMO LON Mccain ccccctocneccoccwocceneucrcnectoueene a 0) 0 Wamebest COAL TOCK . i. sccchscenacececeeocenees Dia) eo OMMISESLCOAle.., esaceccssensserestcecsacssctte ste 1 a0" PEMA COAL *.05ccesccscocvsctescevscccces tO) a0) BR MEROLOU ICOM] Cosececsscdcconccceccsscsccuececonee oT 8 ee MICK ID SUeeeconasseecececssonescrosasease ces ONL 0 30. Clod coal Penneystone ......... sescsacer Leg Oe 31. Black clod ...... acto bucsstes st etecnececae 0) ea SPIEL ECUREOUE ls caccncccececccecccscccccocescoos Onn O OPMUEIDIACOAaceea cect secesecoseccsecscecs ant 10 70 Depth in naan * Wantothe SNEDS-HILL. Bye) BID SOUS COMMeeectatanee =e eicnaee sacle LO) 20 5S: Stone Coal tasctaeemdeaenecaeterecssesvese 1010 93) » Brick: measure: Pucaivesedecessncosee cer 10) 10 HOLS seBallstone: scscncaducecwereenesnescsen came 0.60 LOSS bopicoal<.......ceq ecnsunmeanane rosacea eG 100%-Double coals .-..-scsssommdecsteacee tess 2:10 0 TUG Wellowstone «..csseccossteacsreseess pecan! O' 0 TdienVard coal. ....cccccccosedencnee coeuater 1 20))0 120F blue Mat ......ccsescteceetecomeeeeeeteeee 2 tt) =) TOMMMAbite flat ...05060.avecscoaseoeeeeeee 20 0 VOGIPEINGICOAL is cscisscsencccsssedsccesensens Teed 6 133. Penney measure.........0.sssscesescere of RW) J. Prestwicn, Esq., on the No. i Ft. In. 140. ‘Sulphuricoallis..-csecsrerec. aac apnabeeee 190 144. (Clunchiccall psccesssscccaecess Pane oe : 0 0 150. Two-foot coal.......... eaeaveneacaus sac0 10) 2a 1514. Wandletcoal:, scccscssccescceescoseens ones OMO 154.0 loducoal cccccssasascescecse cere hy) 2) 160:. diittle flint coal) ...ccscoasccoreaseecseee Ono 1 8 LANGLEY 1. SOll ss. sccocaceseeees Mae asacuiseslsete sais nee O29 2. Wed Clave weetecceecseeestoots LAB AR SAS int TO nee 3. Brown Shivery,TOCk) cacecmscss-sssseracrs 3.14 4." Blue clod. c.cccvasasnseac orton: tenes sesea ns 0. 2erG 5. Brown rock: cssecorsenee aeatesetwecbarcs =< Ly 2aas 6. Blue clod and stone ......... sceaieeaxes oe 20 ao 7. Red fire clay ..... Sans: sesvevenccsurens (O02) 47, Oi AUATCVINOCK esssesecnarsceccene wee atauacseees 0 0 6 9. Blue clod and stone ............005 osescog LENOMEG 103 Nellow.wock.; 5.scvssstesesssurcs teres ss ALS BME SClod |, sxscvesccesesenasasesces Sacssones 0 1 4 12. Black wock-<.ccscccsces sce Sauianteneactoneel 3050) i 18; Brome COCKY .2.ce0 eres cesecestoeee Aeesssacs 40a ND 14s (Blue clod. ..c.0.ccsecssece Rasaccassecceenss 2 1 3 15. Peldon with joints............s0008 «. -- 2 0 6 UG sy Blineiclod: cececcenes canccaseeaccecnccecteee ie 17. Calaminker, red and white ....... coors eOee. 10 18. Blue clod ...... vscsin seanbivavasensnoreeeee LO, TO. RMedtclod cos; s.ccsanoses~ esc cencoasescces eee 180) 40) BO) Blue PIMs cosscacecheccs coccnecstasseresean 9.80, 9 O1;.Calaminker 0.2... .09ss-sacesusceanteneoees 5 010 2D SNe) DING casaers chee cetae Blacksccases- +s S biaidiaie nsisieacielve atsetaaisd cae wie OL Fs 61. White flats ......... Rahat seas teeddiasesen BAD Te G2it Blip t Conliecccccsetuceccsccesssecet ote Peessls 1OsGS G3 PE int se teerces cow ecess cise sbcacsancdueedecs Or eO 64. Penney MEASULE......--.-s0cccessesscesees Ga R0 Go SUIPHAEICOA st ernssecccase.sasseeess i Seems HO’ 4: GGOMOCERICIUINCNES. se sc0ccccecscsaseseccsecce as, dO OO G7emSilltcoalitc..cstkiccsece Shae wee saatdeces 0 010 68. Lower clunches...... Sessiaawssmaneeaeee fan (or aO' a0 GOR WO-t00b COAll..sss..ccccacseesccceceocecss One2 FO MOMMUITISCECICATE]. .ccccccececscnsoecsacas Set. olh F160 Mees COdlss.ccesccececs osecdensessaccdeeecses Ow sr. ES ESAS tes ces ocsccssscccevecs dedaes sees saaseees OFF0) 36 Gomnandle'Coal. .:...s0a ecasccsde aWcdateetenc® 150-50 ML SMISASS acecsscceeeess wecccacecdseueconerecaceaeed OO) ks MOMROLOG COAL acesceceacaacaccoeascsaccs Seeeedis Orn? 83 HOME OUNAStONCseieostes sewers Leadaw lanes ones By (0) Giemkotch ..... Ses conl ces sonausecusecscacnsesess 1 @ @ MOemILULE HINtisecccsasscestencesicesecceessanac 42 0 Mom leittle tin tieoal chase. ccccecesscsescenens O20 SOM Cra wstonesocks-a+c.csscheacesseessecoeese a 2 0 Si Grawstone rock coal.scascsesscoses:cssece O09 200 nO) ee LODGEWOOD, NORTH OF DONNINGTON. lem UNy Carthy. ssccasececsacessccccacesaccevane 66meZe0 PAB REMMeYStONe ROCK venssscdeveseedesstenss leet 3. Chance penneystone .......0...seeeesees 2 Oy Amomall sulphuricoal .s.scseescesse Ltnys@nss Gal lecacenandoconascoocos-ateenwee L028 1]. Coal poundstone and ragged robins... 2 1 7 MO Rooticoalsacyecnseeeeckese sees seeessequet sn Oh SUB lack Stone!ceaees cease cae ssoacceceeaviken cay UPS OF oe) T4lo. SOLES) ocongaanatoanoocapsotogncoadsendcans lO @ H5masconelcoall bassieedccccersacees cooseceenste LO GSES LONGNCOAl te cecsceconceesccccescsenctentes tk @ 8 Mi7amMca tals: wacteccvecasiencssssesace successes sss TS a ee Se Gurcoalenssccesa.. issoapusemsapectacoeeeees O24 IQ, CHER. enasedqeascesnbasator Spndoodasn6a0e0000 Yo oA a Oem brie ksmeasurelacescecasecssesescserice es 22 es een dubassirncanceecnccene Sasldevncsenceneeee 8) Tl DFEMBING TOCK eraceceacvecrsecteccceessccuceceis 301274 SREB Al SON) + saciasce nw vetleeetesasaaocescieestts 410 DAMMDUNCATUD cost catcesceascscessesscssoesice D3 eee lO Pi COAL PASS aeteccem se secsescersecscee see © i @ Gr LOplcod leemshiocanodeeioecseaneciinsiies 500000 ie 87 Dil, pile eral swoon CoENG Gaoganecocneecsecodac OQ 2B u@ 28, Top of double coal rock .............00. Oo eG 29. Three quarter’s coal ...........sseseseee 020 30, Lower part of double coal rock......... @ th @ Bil, IDioulls) Wireerligaaesesqecoocsse saososocdadseed iL BO $2. Double poundstone ..........ses..seeeees 0 4 S Sem YellOwsLONCrjcascccneusecmscteosscdscesenscce 208 SAemeViard(COalls ecicsccsccsesccscccesacctesccocese 0) Dili OEE LOUNAStONCslsccuesccecreesenes steerer @ i PS GHBQUOICENECK en ssateeenc escent ees teeccesenes OT 10 Sie blue tat TOCKseess stesenbestocscoerececeeee Onele0) Ore Db lueiHatibasstcicwesesetseseoeeteeceotnee. 0 010 SO mmBlucstatercnwtcerecctaeselos ceccwesccdeecoes IO AM Pitcher bassess.ts-scer-cecensees eee COGB6COS 1 10n 73 AN. Coal. seccssiee Riewioe nace abasGakcene sessions ONO S Sq eehilinticoalerocKksracescecucssecoseoesree cases 6 100 479 Yds. Ft. In. 43. Meatals. .......... ceadedacobonce aneaoson god: ASOD BASMD ASS) veaaesavetocitesy ofan eeniooee cee ene Onan s4: 45. Flint coal.... .. sadeaaceceiandesosenceseted LG lo AG. WWleatalls:. sccvecccwonesss scence unaess faiios Gan Pt PP (8) 47. Penneystone rock, and Glassonstone. 6 1 7 48, Penneystone rock, under Glassonstone 1 0 0 AGP GHEY SEONG” exec nmeeeleccnaseakvstleess ac IQ il Ore SUIP MUM COAl seecscassessunriaessecectsccndere 2 AO Od sn Claimchesswevsecnweesecs feateceene odors pone, Bie 5 2s Clunchicoalsscconsrecectooncecseneseecttos 10 4 53. Lower clunches...... Reaisiaslesieciecticeicee et lo @) 2 JA lwo=t00ticOalls,.c.ccsseesscocnss sencneeeee Oe 2) a4: JOmmMVGAtalsacccccsss teecocecscece coterie 0) 78 56. Best coal..,...... Saseduearesiecectoecsee pas Ola 1G Oi epLANSeedrealthicsscsscescscsconcsoeecenese Dea AS Wi andlevcoalls).e-asccoreccascnedocetecces il @) al FOP DANN OCK es cacdectisnceoiteccence nes acaeoktee Teron G0! (Clodicoall ccseccstteccs. tess coodeaw ae 02 4 HSSn 0 7 TRIAL PIT, NEAR LILLESHALL OLD HALL. 1. Wild red PAROEING 6 conagnoccncbodaeanecosdc 27 0 O Qralved!slumbocces «cacctsvascesscseceveses sence Oy Supelardabluemockwecccsssee eee eaenecnenenes lowell AG A SROCK is archon atceaicedasdasteaesneceoreretse 40 0 DopbINdLrOCKycesecsnrdccnvencerekce rates ceenes 100 6. Brown clod and ole WOCKriscacedsacsanas IQ Or (eed slum rathersonithyscrssascesssaseaces BO @ SAIC Od A catabecesod ase teens con cont artens Opel. a6 9-)\Coalimush and sclod) os.. iwiesieicusebiitecie ore stte One2 do 135 1 10 NEW HADLEY. ubranthrandiclayerespsre cre tetclsniete eters 2 2 O MAO) 2. Wild red ground ..... holo Gata OSL 23) 02),00 Se DIDICY LOCK siscyalaaie cite sme tctee eto 0 2.10 482 No. 4. Strong red ground......sssesseceserereers 5. Four-feet rock .......-.seeere Saeeaseease A 6. Rock binds...... dSaudacdewntoadddse einneticten 0 7. Strong clunch ......+6 seaseeee aloe e inn 8. Penneystone rock ......seeceesesereereees 0 9, Chance penneystone ...0++ scseceeeereres 1 HOF sChineh binds: s: «cs. .+10-veasmescos weneewece 0 il=*Goal-and bass. .<.00--sencecnereesneenacsome 0 12. Fungous coal rock....... aeadgesaaseweleam= 9 13. Fumgous Coal ...ceessseeeeeseenereeeceesees 1 14. Poundstone and ragged robins........- 0 SE OOL COAL, sacpancenpeetenerenedscewceses sade 0 HGS ACIOME .o ccc casetssserestepeerencaes Se) 17. Blackstone measure .....sssseeessceeeres 1 18. Clod and stone Measure.s.....--seeeeereee 1 19. Soft five clay .....0000 cosssccseesese sovece 0 20. Clod and gur Coal .......ssesseseereeeeees 0 21. Grey rock ...scccescesceeccnceneceserencees 7 22. Brick-measure stone ........sceeeeeeeeees 1 QO MCIINCH \cancaassarsccsseccensenvarccosacosns ] 2 AML Beech een aancenancavees Sona cvodccaane 0 OD AMISABS usec ccccses acess “AEB ABest Se sole 26.g Bind. TOCK ....ccecesees Cea aeCerceReeene Saccn. ae DTA BALISTONE, «,ccccaccaccercescecssasescsasoune 2 DEM UMCATEN. cep ecrssenceesaes0ccvssvescacenp 2 29. Top coal....scsecsearesecesereceseeeeeneaes 1 30. Slums and three-quarter coal ....--++- 0 81. Double coal rock ...... asteceudonseneeee 3 32. Double coal. ..........+06 aicnaue vwasseebene 1 83. Double coal bottoms .........sssccscseees 0 DAAPEOUNRUSLONCecscnceecpeccssgcce caucte-nesaen | 40 UP VIGILOWASLOME, »owoncesseseacntucetoscuesniine 0 BGAMOHSS | chcrsenssiceeesoiacseetocsnes saawene er (0) 87. Yard coal and eens Po ngncbiweddaiauee extn J BOsClOdietrsensrccscsss PE MR ese ccc 0 BOWIE RET NARS oe senses poo srssocsnenetcnceas 1 40. Hight-yard rock.......cssseesesesenseee oe 8 41. Strong rock binds .......-.sssessesesesees 4 ADEN GOA). cassnsesceaneedeanecspacesessteen 1 43.1 Flint coal: rock ....:.ccsncssecasnicvnaes ace, #0) 44, Bottom penneystone ...-..ssesseceeeseees 7 45. Sulphur coal .........sseesceseeeeeseseeers 2 46. Gritty fire clay ......cssssecscessesessoess 2 AveeGoal ‘bass and Coals’. ...0.s doscctoncensens 1 MBSMCLUNCH ...2.c0scsnesevess batenedensdcenes se 2 Pe WOMEELCOAL. cccacccavccncsewess beepb cusses 0 POMOMINICD Sav vs wa ss ac secrweteee cd oh AEE AUR | ES OBIGHTIG DASE sincvsaccsccccsecccuseccesseecs (0) POPMGITINE DUDIIGS ihc: vcccevcscceescosecvesseoes 2 DO MOIBEICOR Dh cctet ec ccccessecccvcceccccessnsins 1 54. White and blue clunch .............+s00e 7 Ode MUTTERED COB I wrincaseesccccsccccesrennas 0 OG! WMUCTERU Keer Pe iccanescesssceseccncussas 3 57. Crawstone fee (orm MEASULE,) 22.02.2000. 0 142 HOLYWELL PITS, MALINSLEE. 1.(Clay ..0... ft. meceaususnueuuasanauyyss.ss: 1 2. Minglea measure, blue and red......... 10 By Bluciclod....th cs Sadesdesnwans taneenamecestcc 15 A ML OPILOGK. ..ti-< «koa seeesaschnanaeauuaaea 25 Dy UBlUS ClOd.. fv. diadepavesenacceanemmeraesiee 28 Ga unst sulphur roe kKic...,..sessneeensseansae 11 WRMCODI ie deh ws uae dacteiene ors nan ns cenesenenest 0 Sy LNG GEN Goo-bactbadasicasnaannasondanacanat 0 DMC oad aciaccihc ss doodsccscacccasceuseseaascler 0 MOP MO opbeccpiy sc Reowdhecesscccsevencaseavoenaoase 1 11. Second sulphur rock ..........s0ceeeeeee 17 Me Ft. In. bo eee a no dosnt BS Ora SUIS ee 6c oe NoOorNOrCOCrKNh » woHAeSaneanroadooooOOOnooCoOKnoCaOOnNoCoCOoOOKTOooaGaooa Soo oo eS iE COHSHSCHRCSCOCS 50. 51. . Coal . Dark clod . Coal . Tator butt . Brickman’s measure - Rough rock - White and yellow binds - Strong binds dark ......... acess . Three quarters coal - Double coal rock - Yellow stone fay (or measure) . Wand coal) cess ecc es eee = $Ditto Poundstone siccsacasetetetecetete: sQuGree meek (evcseskdcasanae eendeseteuate » MBLC Hat fay. soncdevagbescckcuaceneeanete . Pitcher basses . Blacks . White flat clod . Flint coal and bass . Flint » (Penrneystone. clod j...4.ssr05 seas. seseate - Sulphur-coal. ...........00+ Soea nace deaeee - Upper clunches - Sill coal and bass between - Lower clunches ........ccceesees ieee 7. Two-foot coal . Linseed earth . Best coal J. Prestwicn, Esq., on the Fae eee e eee en ee en eeseeneeseecess ORO e meee e eee eee ene eeeneeeeeneeseees TARR One e eee eee ene ee ee eneneee SO eee eee ewe eew ee reee - Red and blue clod............... ane eseds . White binds - Mingled red and white clod ............ . White bindy clod Sete eee neeeaseeeee > trong dark clod.....secc<.<2ssacesteeee = Ditto binds 2 east eee Benepe - Brown tarred rock Pee eee eee Cee Cree rer ry Fee meee eee eeeeereneee 0 0 0 2 0 2 7 1 1 1 1 3 1 6 4 1 0 1 - GUDIE Rod cc. «creas aserense ni agemnscc eee 2 = Sibi Poundstone j2ccchecocaneenceceneces #~0 1 it 0 0 1 1 0 2 1 5 6 il 6 0 0 0 0 0 1 0 TORR Reem eee weet eee tenes errr e eee eee eee eee eee Seem weet neste senssseee PPP eee ee eee ee eee AOR R eee eee eee eee ee eeneee oe eee ee eee eee eee Cee eee ee eee eee Randles and bass Clod coal eee eee eee eee eee eee) 188 we] POR ED ENOKHFONN NN EMR ORHPONENONCOHROCPNENNEHONSS col RR OARAAMDOROARSCSCOAMMSOSAWSOSSASASGSSASSSOASOVO Os STURCHLEY COMMENCEMENT OF MEA- _ —_ _ — ee MOU WL Oo bo . Gravel and soil MNO DITOCK Rethececncccssssccescessccscstesatee 3 Mibluevclodiepeccccccssses cose Geunesvecere oes 3 . Strong Measure ......ssseeeeeee soccssccese I DOW PITS. . Sand and gravel............... pace sheceee 7 . Light-coloured clod + A OPSFOCKIDIOWM. oso sentavenasto dds cesar 3 . Light-coloured clod ...............0. bee SP SUIPOUL TOCKiccsnccsccscscecossecesoenenens 12 » Bassand Coal caccciepcesteswagcplesctotueee 0 pp WILEY CIA Ven ntenme-tecciesnescansthe-saseceed: 0 . Coal PUINEAUGIOMs tsncacpcespebercceasensesseseecene 1 . Light blue clod, strong ..............00+ 1 . Red clod 5 Goal isd sed aw cain cacactes setencccisansncmeeeered 0 DAWLEY PIT. Sasenenepee sence nels see's coset cS Wl eR BOON KR RR eH HO, Ne omr oO ZSIHBHODSCSAARSSOBMOOSCOASH CaaS Geology of Coalbrook Dale. 483 Thickness. Thickness. No. yds, ft. in. | No. yds. ft. in. 5. Jointy rock ecccssesserececccecseceecees pene Ome OMmOn NoOse GINSCEQCOTIN: 52: EVD TPY eblowy ShanlGstss0sz.tacaas dccaccanssoneeeteds 1 hapa FXG) 27. Yellow stone earth ......sseesseererseess 6), OF OF 18. Yard coal ..sescs3.s0enee cease aaa ome Opa 28. White cutting rock ...... seerreeeceseerenee 7 0 07} 14, Quoiceneck ......00 Sdabonance Rb aa setacears 0-1 0 BOW Stone clod..ccseocseecwes eveNivouciieradiccscen 20) Os) Ws: Bite fats foto eee oe = Oe AUEMEOD COdlt sc. cucsdeacev crv ccdnorcawseeeteens otlegtla LO jokes Buse eee ee eee EtG slutns and double eocl..ccccssccso.c00 3 Lontanl Goat tate eh eee eee Hae 32. Heathen earth ......... steeenseeessereeeense 357 OF Oh) Tee acm ite be tse ue ESTER pe sions OL 16 33. Dun Bass ...ssssesesesscessseeeseersceees og (ON 2! 34) Toy Flintieoali..6 cceigctasenescacccssaedearane vend len BE. Yard coal ...cssceesssersesscesseesesseesees BOG. | GOR Biante eerie, ster ce eeaie eaeanee 5 0 0 Oe QUOICEMNECKi acces cestescnsesserecseateccdees 0 2 3] 9, Penneystone......esscsesseeesceeessoes ay Oe 10 36. Basses and two coal..........+. apeascacone 3 0 0 | 92. Sulphur coal ........ ctecccoen seoseeneanest ee he 3h @) eile Clod ns abisaloe eee cavetvacrsteccarecceesen ans «- 2 0 0} 93, Clunch ....22:. Panna ed ie Nie sie ao 38. Flint coal... LCE CACRUEL COSECCEEE BE BSE COCHECOOC 1 0 2] 94, Linseed earth °)....:. COREE el oA ely OnleG 39. Upper flint’ ...... pe eeeeeeeessccceescnsoenees 6 0 0} 95. Two foot coal c..sssesececees sescacecneceree On 2550 40. Penney measure ironstone ..,.....+... ve 9 0 0} 96, Clunch -.1.....00+. selsdchiotesi'a Wadse desievanerts On 1, 70 41. Sulphur coal ..........ssssesesereeeecerees 1 0 0} 97. Randle coal ......... Sereoeceien dea cesseceue 1) Ae Cloditccciee. ee asattosiatuitiecis cee bnce Reamoelace 0 1 0} 98: Hard epire Sesh sd acces yon eh RL 00 6 43. Lower coal ....... teeeceecencecccneccscecces 0,0 64 “Soloed eonl tts be cscs. dese epeciaces ecces OU 2 a4: 44. Upper clunches ..........ssssseeeeeeseeees 5 1 6 | 30, Clod coal poundstone ......+.++++ debi Ce Var AD TROULNCOAL? )-sassacatitceeont ees cdbecest sone ecens Of) E Ge Sa e Renin ee fd oe a Ae Pet O. TO 46. Lower clunches .....ss+...sesseeees srseee 5 0 2} 39. Little flint......ccscceeee Rife 01 8 Afar SOLG CLOG cr vest eae nenecksenestes sere eat OF 6 48. Lower sill coal...... Deaedetseecten aver eedoes 0 1 61] Little flint rock, unknown, said to be 789 5 49. Two foot rock and coal ...........se0008 io very hard and black. TUB ENGINE PIT, BY THE FIRE-ENGINE IN DONNINGTON WOOD. Thickness|Thickness be- of the tween the Names of the Coals and Ironstones. Quality. Strata. Strata. yds. ft. in.| yds. Donnington Wood coal ............... Very good coal...... .... $390000000000000000008008000000 10) 4°27 Black stone...... SesbcatlcsGecticeptseeees Weny; CoodtstOR en ease eeereruneresseaasen-tiaereonestens il @ @ 4 MLONENCOAli: scoertseccescecsscseecedce ...| Indifferent coal........ Sedua cco deuitetoascidededbceseuiess it) Oy) 2 Garicoal’y....c.seece aectiiert sede veceraeen Indifferenticoall st escecchenetoethies oleseeiecoescaascs Q % Si © White ball-stone ..... paidoccccoCcAancedc Very good stone ............0 QEQCOnSBONCOnOGOOSOSOH005 1) 283 MOpYCOalcgccccotene cen saecesceseenaues Very OOGlCOAl mctmesnsenseceranacecsseyeienascreske: Nok |) O Woubletcoale: dcwcshedaceesscdecclecenen GoodCoalccceesnecbet neces cebesataeeseavcsuncuned ues YO) Ol Mellowastomeu «.cseccdssen soto eee Good stone ...... doncdeeiavane tustladee deer ecaeckcewess Gy gl 3 NITCICOAN. .saesiocscssadedossededeoenssres Orstingiay Goel doqaodaosienocon0ndeacebacuonacedsondconHod OOO Blwestlatistone!cccsscctenecsceresee ences Goodtstone. A tudes ccetvcrecessstaeocseesessccneseess coli EO G) © Bipwlinticosli corse ssncaecncesnsoccee: Goodtcoally. os. biciscncancoates sce aeaseseib'es obecectaecsess LG Penneystone: ...0226.:ces.e. soawhivesesss INOfiverivaCOOd isecaeseccccchscecenrsesseeasteees Beog60000 i 0) OQ) Sulphinicoal cc suesssesvccsten torceotene Badkcoalmestscescecscuscesusces Boece wow sederneccsevases LOMO ESS Siilcoalapenete Wh i ay aot ae Good coallstrcdesdercaut codecs cosnsnasescteteues wean ceee Oi ll -& ilwiosteetycoallecss sss. aemaa ental Goodkcoalteaasatdscwascecasenedestasscdeteaoeateavescees OO 73 Ol 8 Randleycodleseentes ete ieee Goodlismiths*coal.cta coc s Poe somenunes semendenns tevassesene 0 63. Sulphur coal (main). ..........+++ Foliated, pyritous coal ssccsccccssseeeceseceecsees vesecsses O 64. Light bind...........csccccseceeeees Marlo caes na SeeR a, enbdostooothncs nhgosckier one e “Rodsbace wee 65. Blue and brown clod........... «Mottled shale, very siliceous.....2...sss2+0s eee Poesia: | 66. Brickman’s clay (red)......... ...Indurated red clay......... Peascedevs cues Bicsedstnscnensces 0 67. Rough rock ...0c...csesscseeoseees Coarseish quartzose conglomerate, with a calcareous CEMENE. ...sececesccccccccccscccccccecsccscnsssssssseesss 68. Red clay........-. Astacdactnchee Indurated, red) clayecseccnsc-ssectesctse) corcoocoocooononwnoounoonocre ee ee RKOOCONNONKFORMPNORF COR FRENDS = al ob) o mb eo Oo oco¢S SCNOFONONWNMCCONKFONNK OFF — fen ASC SH SCONIAFNROUCOCWNSOOCNAOCSOO KFPODKRSCOOS — i \ — a — ee —~ ee a — | i=) PORN ORADWOAROHACMAROOAOSCS a ‘Geology of Coalbrook Dale. 487 Deep Pit.| Basset Pit. No. Local Names. Description of the Beds. yds. ft.in.| yds. ft. in. 99. Little flint coal.......ssvsceeeessS1ate-COAl......s0eeeeee AU Rabvdatdganuvereoednr- Os Omi4ieO, 0} 4 100. Rock in the coal ........ ore Fine hard white sandstone, slightly micaceous......... Mw2 a3 oll 22 oO 101. Lower little flint-coal .........Slate-coal......ssssseees saws cet ece da tahauvowaide eesatesenses On 26\aa0) 263 102. Little flint............ Seledeeatelee's Hard, fine, white: sandstone .65.3-0e tc iccsessscrceeevanens 262i 15.0 103. Crawstone measure ..........+. ‘Hard, fine sandstone, light brown, slightly 1 mica- ceous and bituminous........... waeikatetes sareeswee sooo LO ROI2. OF6 104. Coal under ditto ...... ras aN abeeee aecervewep pected Uiee case dia Teidedvdeddadadte On P00! OHO 105. Crawstone crust .......+. ..Whitish, fine, rather friable sandstone........... seats Le Whe 22.3 106. Lancashire ladies’ coal ...... Fibrous ‘coal WALT Sa dedeas es ttecews tes mene ousdssmenacr ds ODO Or 0) 70) «9 107. Rock, very hard ............... White, compact sandstone, containing numerous quartzy pebbles ............ Uiiisccasneeesreed evvese’ OB OKO De 0 108. Ditto......cosecovececosvecoesoaes -Compact, white, argillaceous on slightly oolitic...... ddedeesccktutes sedeat Wenddcladsneduseicvessseaual= OF MOMs IC G 231 0 1/230 1] The last stratum immediately overlies the Wenlock Limestone at Lincoln Hill. MINERALS OF THE COAL MEASURES. (B.) ARRAGONITE ecccecsssceeseeee =o00ceS Occurs with barytes, but rarely. Barytes, crystallised............+++ Beautiful crystals occur in the large nodules of ironstone from the bituminous shale overlying the little flint coal in Broseley and Caughley parishes. CuancoaL, mineral .........s0e.00. Common in the fungous and some of the upper coals, forming thin laminz alternating with others of the crystalline coal :—also in the sulphur coal of Kingslow, where it is frequently iridescent from its admixture with iron pyrites.—A few fragments of very pure mineral charcoal have been found in some of the Penneystone nedules. Tron, carbonate, crystallised .....In the nodules of ironstone—principally the white flatstone and Penneystone. argillaceOus.......ssseeseeee Forms the nodules of the ironstone measure. earthy red ochre.....,...... Occasionally forms nodules in some of the sandstones. PELOXIAE 2.0... 00creerevrveere Dispersed in small quantities throughout most of the strata. —Compact hema- litic masses occur in the large ironstone nodules of the little flint coal shale. phosphate .......seeeeee »+»---Rare.—In the Penneystone nodules. es eee } Very abundant in some of the coal beds—called sulphur coals. arsenical ,,.......Cryslets in ironstone nodules, and coal beds,—rather rare. . Sometimes the arsenic volatilizes, and can be collected from the blast furnaces. hexahedral ...... In ironstone nodules.—In detached masses in the interior of the Penney- stone nodules. octohedral ....... Ditto. ditto. rhombohedral ... Ditto. ditto. radiated . ......... Ditto. ditto. Leap, sulphuret, Galena ......... Rare.—In the Penneystone nodules. Lime, carbonate, crystalline ...... In veins in the coal and in ironstone nodules. crystallised ...... Beautiful tetrahedral crystals occur with the fragments of brown wood in the Penneystone nodules at Madeley, also rhomboidal and tetrahedral cry- stals in the curlstone at Woombridge. PRTROLEUM, ViSCIC ........00eee0s0 Occasionally in cavities in Penneystone nodules ; the white flats, crawstone, &c.—It is also commonly diffused throughout the central coal series, and in the flint coal and roof at Caughley. PHoLeERITE, of Guillemin. .......... Of frequent occurrence in crevices of the ironstone nodules, especially the Penneystone, in the casts of plants in ironstone, &c. ALUTAINTUM co say devs satacien Wares 8/ciiele-t Is not of rare occurrence in the hearthstone of the iron blast furnaces, where it is found both massive and in brilliant cubic crystals ; it exists naturally apparently as titanic acid combined with iron and zine. Zinc, sulphuret, Blende............ Common in almost all the ironstones,—frequently forms the casts of plants. —Beautiful dodecahedral crystals occur in detached masses in the interior of the Penneystone nodules, and in the casts of shells. CAdINifELOUS...s0sseeeeerv eens Occurs in the Penneystone nodules and the white flats, but rarely. 488 J. Prestwicu, Esq., on the SYSTEMATIC LIST OF FOSSILS (C).7_ PLANTA. ~ FORMATION. Genus, Species and Reference. COAL AND PARTICULAR BEDS. CaLAMITEs. canneformis, Schlotheim, t. 20. t. 15. f.1. .......+-+..|The first two species are common in all the lower arenaceus Jeger, see Ad. Brong., i. p. 138. t. 25.f.1.} strata, especially in the flint-coal sandstone over- t, /20-)ls O—On teceentaspteseractecaseccces cece csecrcastesees lying the Penneystone at Ketley, and occur approximatus, (Sternb.) Ad. Brong. oats ?. "133+. 24.. chiefly in the white and blue flat measures. nodosus, Schlotheim, t: 20. f. 3. ...cecesscececececeeeers CycLopreris. obliqua, Ad. Brong., i. p. 221. t. 61. f. 3. ....++se+++-|Ballstone. Rare. oblata, L. and H., iii. t. 217...... monocot: Acre fodil rele orbicularis, Ad. Brong., i. p. 220. t. 61. f. 1, 2. ......| Ibid. semiflabelliformis, n.s., Pl. XX XVIII.t fig. 7........| Ibid. NEvROPTERIS. ingens, L. and H,, ii. t.91 A. sesssersserserseeersersens .|Ballstone, and almost all the lower shales. Common. gigantea, (Sternb.) Ad. Brong., i. t. PONE ---| Ibid. Loshii, Ad. Brong., i. p. 242. t. 72. f. 1. Beecesee’ Ibid, Sorettii, Ad. Brong., i. p. 244. £70. f, Rotawe es .| Ibid. OponTorTerts. obtusa, Ad. Brong., i. p. 255. t. 78. f. 3, 4. ...++004e.+.|/Ballstone. Rare. PECOPTERIS. adiantoides, L. and H., i. t. 37.......40. seseeeaeseeeeeeeee|Ballstone, white flat, and most of the lower shales. Common. abbreviata, Ad. Brong., i. p. 337. t. 115. f. 1-4... Ibid. heterophylla, L. and H., t. 538. abled s Wola Uae Baa elon ce chiawed Ibid. lonchitica, Ad. Brong., i. p. 275. t. 84. f. 1-7. t.128| Ibid. oreopteridius, Ad. Brong., i. p. 317. t. 104. f. 1, 2....| Ibid. muricata, Ad. Brong., p. 352. t. 95. f. 3, 4. t. 97. p> ibid: nervosa, Ad. Brong., i. p. 297. t. 94. sseccsceseeeeeeeee] Ibid. SPHENOPTERIs. Conwayi, L. and Hy, ii. t. 146....ssessscecsseeees +++e+e++{Ballstone, and the best clod coal rocks. Common. dilatata, Dvand i, 1, (te 4:f. e wool BODIE Go ooo A cco ides dk wna Sas dl gach ceaie ee eae Cystiphyllum cylindricum, Silur. Syst........++++ a WGwkrs. Ie Ne (FOS | TS Lc ey Cyaphophyllum dianthus, Goldf. ........:0:::s00eeees Gis Guile win Joes | nde f re] Soe Poke 1 Ne eae turbinatum, Goldf......ssosesesseses 1G£8. bob P| os Pall kee ceil ee © scene eee eeeeeeesccessees eee eee eee * wee eee eee eee eee eee eee Acervularia Baltica, Schweig. Beobach, VI. Silur.S. 16. f. 8. we]. cao ft ane | ees,;|| ad Hees Nhtcoal eee aaa : Astrea ananas, Silur. Syst. .......+.:00++ enacts 16. f. 6. a PN (ean ee EE Pt tc) machi Monticularia conferta, Silur. Syst. ......+-+ Recneewed 16. £..5. ae abana) eon linet i bea I eee «2 ba Porites pyriformis, Ehrenberg, Silur. Syst. ....-.... 16. f. 2. wie | cass fone: lead cree Pose head eee tubulata, Silur. Syst. ......... sone sangoknenss 16. f. 3. veo | cps, fysem Ly sdecd stm, ] cco Ged ee Catenipora escharoides, Lamark. Anim. sans Vert. fom. 11. Silur. Syst. ..c.cccccssscovscscovecssesses 15 bis, f. 14. e math Lin 54-3," Syringopora ramulosa, Goldf. .....e1.ssseseeeeeeeee 25. £7. saga th phonitewe | ate [hoes Meta tll eeeca aces . La Lithodendron sex-decimale, Phillips, Geol, York. .| 2. f. 11-13, ate A RS UE Al ico e eesoeaea Face talc ——— sociale, Phillips, Ibid......+.+eseeeeeee 2). f; 9; 10. wees eee dll eel) Oe Ih tewee tf wipe" temierelll rected tees lle el Lithostrotion floriforme, Fleming, Martin Derb. ... 43, 44. ads gllwitee Hibete hae willie san ithliicse Bd ohne dl kein ben eee a ' Favosites Gothlandica, Goldf. ......sssecesesereeeeess 26. f. 3, 4 svn, [eset ses {uses | see, | casei] ice eos tie etc oete alveolaris, (De Blainv.) Goldfuss......+++ 26. tJ hades | bi a ba i2 * ‘= spongites, Goldf. ....s.ssecseesees Sauaec 28. f.1 ae us * ta — ? septosus, Fleming Brit. Anim., p. 529. eee 3 PY bel ek soe, | ces ORM Stromatopora concentrica, Goldf.......ssceseseeeeees 8: f153 ts * ‘ _ Millepora repens, Hisinger Leth. Suecica. ....-..-. 20:85. oo * . a Eschara? scapellum, Silur. Syst. .....cscseceeseeeees 15. f. 25. eh * |... | Discopora squamata? Silur. Syst....... eae pnevacepee 1528 22- Beet iesae |b ere * |... (ee Fenestella prisca, Silur. Syst. .....+++ssseeee wetestese 15; £18, a ANSE an hase ell Mean geen Rese s Meee * ES Glauconome disticha, Goldf.........scssesseeeeecereees 64. f. 15. Poatifnesetltenm || coset cast itinwrentness * an Aulopora tubzeformis, Goldf......s..ssssseeeeeeeesenees 20) f.2 eeiaitl ors yal see Aiea all eeisend | acloo tt cots Fl ee ———————————— ——i(Cé LC OCP CO SRORALECS COCR eeweeeseee eee eee eee eee eee eee eee eer . - one CRINOIDEA. Actinocrinites moniliformis: Miller, Nat. Hist. CrinOld pypemU Descceeeeecascanancsscc.ssesccsse-ovan feut|) vee} ide] (oe t ses oa] ees difecs| * ||) one —-? expansus, Phillips, Silur. Syst. ... UZ 6 £.:9e sy eee Srtemecte Sac DUB a dike * 99 (yi * ( XXXIX. f. 1 * XXXIX. f. 2 * : Bis Liew a : Bate 4 alae * XXXIX. f 3. 2 all S50 tonic BOOT al face ae XXXIX. f. 4. 57 [borate icici hgciciceed |e cCGee! etcic ae XXXIX. f. 5 bad wae XXXIX. f. 6 * >O, ODS ais * XXXIX. f. 8. Led bers itd Hectiow \iaiSctil herrea | 0c XXXIX. f. 9. He || Pea Ser hese a incite is OCOD STBTOES MI Gace hisco SONUNCTEXE Te EO | eset m EXOROXO NGS Gee |e eles * XXXIX. £13. | * - * XXXIX.f.14. | * ce * De Ney fff * 3} a D3 teelese * 2 ze XXXIX.f. 151. XEXONTNG fe Ghee eee rele LOOM TNs) coot le = XOXO Laie lees * DD, DG D.6iy 8 LC allie Ul aa Veil hassel le ocr isos 2, OOM BPO || Se Wade Ni cdo |) Goa.) 900. |] Gen 354. * sad ete A HOOs tals Erba oreo Venccal ieoeaedtameoe.|) Ago It Go Sete lO Detemt sul teecicn |ecocien (trecten|ittesam!|leteete * * WO si ie 459. f. 3. — hemispherica, Min. Con. ......... eeensiiees — gigantea, Min. Con. ..... So0quaosonone0n000K 561. EAE farce ico, | te! 0) cco 320. ao |s etsletallinreaiony | axa | res 1 Found in the Crawstone. VOL. V.—SECOND SERIES. 2 Found also in the Blackstone and Chance Penneystone. 3s Wenlock Limestone. Re: Wenlock Shale | eee * A9] Caradoc Sandstone. 492. Genus, SPECIES, AND REFERENCE. Plate and Figure. The numerals refer to the Plates which illustrate the memoir. Lepteena scabricula, Min. Con. ......... chteasoo sna: 64. f. 1 CONCINMAWVLIN GON. cfsccoscascelscesreecesc 318. f. 1 Atrypa affinis, Min. Con. ...........+. saseoonaags mesces|(l OD einaae —— galeata, (Dalm.) Silur. Syst.............065 ses| (Gods LO, Laois aspera, (Dalm.) Silur. Syst...... i ie eee 12. £15; tenuistriata, Silur. Syst. ........s.-.cescosees LON ES) Spirifera radiata, M. C. Silur. Syst.............cecee 12. f. 6. PISUMH SOUT ON GIeMEscness scx ocs-cssseseese 13. f. 9. CMSA PEDSUE SV SE Mier acsnccsscecsccsnns ss 12. £8. — sinuata, (Linn. Trans.) Silur. Syst. ...... 13. f. 10: bisulcata, Min. Con. 494. .........c0000 seoe] MOMs ide, De semicircularis, Phillips, Geol. York OnthisMnnatay slurs SO VSti.ccccse--s-cvececcensesaeceee Sof. 0a. bo. i ibe orbicularis, Silur. Syst. ......cs.eseeeeee “Ate 5. f.16. ——— hybrida, Silur. Syst. ......s.csescseesssesveses iS a aa It Ne ——-— rustica, Silur. Syst.........0.ssessscesssseeeeeees 12. f. 9 ——— testudinaria, Silur. Syst.........s.sscerssscocees 20. f. 9, 10 — alternata, Silur. Syst.........sssesssseseee Ss. 19>. /6: Terebratula lacunosa, Silur. Syst..........ssssseesees 5.f.19. 12.f.10. —— pulchra, Silur. Syst. ........:.....s000008 5. £. 21. ——— cuneata, (Dalm.) Silur. Syst. ......... 12.2. 13; bidentata, (Hising.) Silur. Syst. ...... 13. fy dewe BpHenica, SMUT. SSE. ...0sccevovesmnoe ten Me Galli ———— _ sacculus, M. C. .....sccccssccccesccccccees 446. f. 1. em «= Wilgoni, M,C. i. .ccsccccconccccccvecccess LIUSi£; 3: —-—— pleurodon, Phillips, Geol. York. ...... 2) ae 16. radialis, Phillips, Geol. York, ......... 12. f. 40, 41. EE OEAINETUS levis; WiC. 5. ccnccaetescuceveoteaserene 28. Einpula cornea, Silur. Syst: ...oiscsscensscoessssscene Sof. 3, Me WISH, POLUNSMStserescae=+enseseaenes ko kaee late): MINIMA, UT SY Steena-e-asescaresensaeseerers 5. f. 23. parallela? Phillips, Geol. York............+- LD. £. iy, 9. MOLLUSCA. (GIO WIGSIVERUSEUS ceevcsccccssovennesecsscetscecsdenszeses SOCK fe 22. Teitterinar ODSCUMB. sc.c.cesscecseseses Peed ate aaasntt XXXIX. f. 23. Euomphalus sculptus, Silur. Syst. .......e.seseeeeee 12. te Le RATHI VELA. COON. ics scecsecsscccsseeess 450. f. 1, 2. -—— MUSOSHS WII KOON, iecsccsesaceecessccess 52. hege —- discors, Min. Con. .........eeeeeeeeeees 52.1. Ibnoe Trochus? Usocona. ...... Berenice hiscse st ssces seeds pl Dep ee ls Munritella ? clavate wpseserersereseracscccccescssacossr- sce KXKIK.f 24: P Minima) Wessseenete Rae eireecanecs secssinees SHES: O4ID.s HOR Polyphemus ? (Montfort) fusiformis Conularia quadrisulcata, Min. Con. CCLX.3—6. Orthoceras annulatum, Min. Con. giganteum, Min. Conc..cccres snsnseee SS SIE RAIBN, Gannon codsasocoensco3cs pect Peco ewe sens eeeeee Nautilus clitellarius concayus subsulcatus, var. armatus falGAtiiswecsbiccassciss ceeseiseas sive ctaacevelecspann Bellerophon hiulcus, var. Fleming........csscsseeeeees —— navicula See eee treme eee terres eneeegteeens CO Peete ene eee seeeeneeeseeee Seem eee eee eeee see seeee eters esstes eee reer eee eee eee ere ey SS LOL Oe XXXIX. f. 26. > ER BO ? Found likewise in the Chance Penneystone. J. Prestwicn, Esq. on the — | |_| | | | | ——— Coal Measures Pe TRS = < eo | & 3 a8 Se o@2 Fad =) Pa elm *1 fe of * . of eso iseettwese eee e eee eee . eee . * * * * = ee eee * e * eee eee eee * eee *2 *1 * + * * * * * * *1 * * * * * * * * “ Carbonif. Limestone. ForMATIONS. 5 5 o ue Py 3 Pe 2S) o0/28 me) eas] oe su| e&e| ss se/PS | Be Os A) os a | eee eee eee ee ese | cee * vec | ce or sea cass a2 ° eee - . eee eee ese ‘ as eee of ee eee see * eee * o Woes a" yes of | as ener e * F eo ee * * . Sauillas eos | ee eee | aC oe * c oe eve || ese * ose * * sree hist mel cae | | | | eee | eee coe | wee Pin 'h ee | COW ean | oo Sci | | | ! | | | =|- 2 Found also in the Top coal bass. Wenlock Limestone. * * OK KE Caradoc Sandstone, Geology of Coalbrook Dale. 493 FORMATIONS. Plate and Figure. | Coal Measures. =. Fe ; . | z a 5 ue a -| Pe ; o . GENUS, SPECIES, AND REFERENCE. to| & | & | 28] Bel ee/ 88] 2/88] Bel ee The numerals refer| 22) 9 | & | Se\me| Bo) e¢e|/ 9/23) 25/ 38 tothe Plates which | SS | = o BY go | oc | ht) Bo) §s) ga) se » fillustrate the memoir, & a|/ = = Ss os = SI < 5 4 4 Bs Be S8 2 fq n = 4 oF ' Cornulites serpularius (Schloth.) Silur. Syst. ......) 26. f. 5-9. Peel acon ecete ll ecors tl leictocia | Macsees a Weiceoel |ctSecar| ict al (aaeaeteain (arte | Tentaculites ornatus, Silur. Syst. ........ssssseeeeeeee) 12. f. 25. Se (loco. |) Bose iodo Hl coal. dee dhcas: 1h. ccaky beau eae eer — annulatus (Schloth.) Silur. Syst. ...... 19. f. 16. aiid nsistoai le teak resem ines -talimeccn |Prscet email tes sclh coat ace PISCES. Gyracanthus formosus,’ dgass. vol.iii. p. 17. ....0.06 5. f. 2-6. oe cbt Imada | uae). ea6r | sade Haan Cochliodus?, Agass. vol. iti. p. 113. ......eccecceseeee| XLT. f. 14. he cee || oes Hybodus*? Agass. vol. ili. p. 41....... saastececnerase| elle ts Loe Nao sacgllecoarenlateeay ikem egalire acd lle ake ccs wlttonts Megalichthys Hibbertii,* Agass. vol. ii. p. 87.......] XLI. f. 10, 11.} * s0eeil sos oc Holoptychius Hibbertii,® Agass. MS. ..........0...., XLI. f. 15. 5S eee Poo) {lec race |e MmOMOLOS, 19089. VOl. iil. P. GG. senggsacnesenvolecaeccevscedasreqteral * | sos [ade Pives | ens | ane | cow fens ll) coe 1 Bones of the head and scales. 2 A tooth, see Plate XLI. fig. 14. 3 A spine and tooth, represented in Plate XLI. fig. 12, 13, are assigned to this genus provisionally, as they may possibly belong to the Coal Measure, genus Diplodus, the characters of which have not yet been published by M. Agassiz. 4 Bones of head, see ante, p. 443, and Pl. XLI. fig. 10, 11. 5 The spine given in Pl. XLI. fig. 15, is placed with doubts in this genus, its state of preservation not being good. The spine is round but compressed, and is armed with two opposite rows of teeth or tubercles inclined downwards. There are no traces of the curve men- tioned by M. Agassiz as one of the distinguishing characters of the genus. Remains of Gyracanthus, Hybodus ? and Megalichthys are found also in the Chance Penneystone, Top coal bass, and Flint coal bass. 382 A94 fault extends indefinitely. hk. NAME, Lilleshall-+ ..... Great East+... eee ween eee ee ene eee eee eee rr Nee eee e eee we eee Boundary ...... iKetley........0. ‘Lightmoor. siciiew Rock ... Average Amount of Disturbance. feet. 3000? 1000? 36 15—50 2200? 30—600 300—600 16—30 16—100 0—60 0—40 0—100 N. J. Prestwicu, Esq., on the (D.) In the first column are given the numbers of the Faults as indicated in the Map, or the first letters of those which z designated by names. In the second column the names without an asterisk are those applied to some of the lar Faults by the people in the country; those with an asterisk have been proposed by the author. The headings exple the nature of the 8rd, 4th, 5th, and 6th columns. In the 7th the connexion of the different Faults is given. Th opposite Fault 5,—4, V. 8, signify that the Fault, Number 5, is connected at one extremity with Fault 4, and at the other with Fault 8. In the same way ranging with Fault 2 is, Trap II. 3, or Fault 2, abuts against Trap at one end and joins Fault 3 at the other. Again, opposite Randley Fault, 0, Ra, g, express that the Randley Fault, Ra, at one extremity gradually thins out 0, and at the other is connected with the great east Fault g. In the next instance the case is more complex. Opposite the Lilleshall Fault is the expression, b, k, > 1, —J, g, > «x, which means that th Boundary Fault 6 and Ketley Fault & unite or merge > into the Lilleshall Fault 2; and that the Lilleshall Fault (2) a the other extremity, and the great east Fault (g) unite and extend to an unknown distance zx. each of the Roman numerals the Fault thins out at each extremity as 0, XII. o. A Where o occurs o1 Lastly x, LXIII. 2, mean that the Direction, 4 = = Zz AN Ca . 58° W. 53° W. hoo? B. 2 222 88° E. 10° W. 40° E. 2s ee 88° E. 72° W. 67° W. 50° E. Az a = 50° E. » 45° W. 70° E. 25° E, 3° E. . 63° E. ia iat 42 25° to 45° E.|é IN. doo, B. N. 50° W. Ascer- tained Extent ofrange. m. fur. a) 2 8 0 110 pe) 220 1D bie! 6 0 6, 3 0 5 i ovat ei 1 0 ters 1 4 0 5 0 6 Orns 0 { 0 > Loe 0 3 0 4 Ons. 0 4 3 4 0 5 16 Side of Highest Level. Rise, Connection, and Termination. S.E. by E. \4,4,> 4—l, 9, > 2. { \ W.N.W. W.N.W. W.N.W. N. by E. S.W. by S. S.E. by S. S.E. N.W. by W. W. by S. S.W. by S. S.W. by S. W.N.W. 5. W. by S. S.E. by E. | S S.S.W. N.E. by N.| NSW S. 45° W. N.N.W. | W.N.W. | S.S.E. S.E. a ». B.S.E.&S.E, N.W. by W. N.E. by N. | { 1, G. lim. Trap, I. 3. Trap, II. 3. Eves # 1, IV. 0. Trap, 6, k>1. EK 2: | re | i) a b, VIL. di. 5, VIIL. di. g, Li. bro. 8, IX. &. | 6, X. de. 10, XI. 13. o, XIL. o. k, XIU. 10. k, W.r. w, R. 37. o, XIV. 16. k, XV. 16. k, XVI. 15. OORVILe: || Fp ANITA oh a 0, A. 2. | o, XIX. 0. | k, XX. a. | { { | | | | { | { | REMARKS. Brings the Silurian and igneous rocks of Lilleshall into contact with the New Red Sandstone. Bounds the coal field to the eastward, bringing the measure on a level with the New Red Sandstone. It has not been posi. tively proved underground, except at Pitchcroft. It is deflected in its course. Visible in the lime quarry at Lilleshall. _ Ranges parallel to 1 at the distance of a few yards, and is visibl in the lime quarry. At the Pitchcroft pits the fall is 36 feet, but itincreases appa. rently as it trends southward. Increases as it approaches the Lilleshall but vanishes just befo it reaches the Lightmoor fault. 7 Bounds the coal measures tothe N. W., abutting them againstt! New Red Sandstone. It is joined at Donnington by the Ketley fault, and the union of the two forms the Lilleshall fault. In place basalt appears along this fault. One of the earliest known large faults in the coal field. It is frequently perpendicular and the sides of it often gape. At it junction with the Boundary, it splits into numerous fan-shaped branches. It decreases rapidly as it trends southward, Its course through the Wenlock shale and limestone cannot be ascertained with the same exactitude as through the coal fie! Its length is no doubt much greater than that which is here given. It will be perceived, that it does not range in a perfectly straight line. This is one of the best known and most important faults ii the coal field. Its effects vary greatly owing to its frequent june. tion with other faults. Increases but subdivides as it approaches the Boundary fault, It crosses 5, by which it is slightly deflected. | It presents the same phenomena as No. 6. : Decreases as it proceeds from the Lightmoor fault, of which isa branch; the chief fracture of the Lightmoor fault bending @} few degrees eastward at the point of divergence. * At its intersection with 8, no alteration of level is produced; the faults neutralising each other, but shortly resume their previous} condition. See fault 12. Increases and subdivides towards 4, Perpendicular, and from 20 to 30 yards broad. wards 10. Apparently a continuation of 9; but the continuity being par-| tially destroyed by 8, itis considered as a distinct fault : verses 10 without either fault being affected. It ramifies to- | Increases towards the Rock fault. af This fault is very irregular; on meeting 10 it is deflected seve-| . ral degrees eastward, and it terminates abruptly against 37, ~ The great dislocation ranging parallel to the igneous axis of the) Wrekin, is apparently deflected slightly more to the northward) by its junction with the Steeraways line of dislocation. The diagonal of the two passing through Kinley Wick, where we find a pro- truded boss of basalt, Increases rapidly in vertical importance towards k. Ditto ditto, Thins off quickly asit recedes from 5. The dip on the side of lowest level is more than double that on the rise. The phenomena are the same as in No. 17. Commencing between the villages of New Hadley and Ketley, it bends at Ketley and again at Steeraways. At a mile from its rise its effects are 100 feet. Past Steeraways it again decreases slightly, afterwards the strata which are nearly level on the rise of this fault, dip rapidly towards it, in the swamp. Runs parallel to k. From the rise side of this fault, the strata dip uninterruptedly 1 to New Hadley. 43. NAME, se eee eeeerccenserses semen eee eeerewesesee seer er eeeeeeereseras Ae eee mer weeeeerenees eee w eee este eneeeses Se ey Randley......... CORN e es ene w oes eeee Oe nw eeeee ewes sensee eee erry sent eee eeenerrseeees Tere were sere sereneee Limestone ...... Madeley......... Hee ee ereereeeeeoees Longwood- ... ee eee tee ee ee eeeeeens Average Amount of Disturbance. feet. 60—300 20 80 20 90 24 24 27 25 30 30 30 24 150 2000 ? 220 390 300? 100—2000 100 69? 500? 60? Geology of Coalbrook Dale. A95 Ascer- tained Direction. Extent ofrange. m, fur. Nei os per | aie N.65°W. (0 13 N. 65° W. |1 0 N. 40° RE. |0 6 N. 15° W. |0 2 N. 60° W. 0: 2 N.60°W. |0 2 N.77°E. |0 33 N.53°W. |0 3 N.62°wW. (0 13 N.55°W. |0 2 N.65°W. |0 2 N.80°E. (0 4 N. 0 6 N. 27° E. 10 2 N.48°E. |0 5 N.50°W. (0 03 N.W. (i 3) IN. 34°W. jl 1? N. 5° E. 0 3 N. 28° E. ~|2 0 N.50°W. (0 6 N.80°E. |0 2 nee Rie Mt INE GND, Nh al INeroow ee ze INGE ice een ONG N.77° ER. |0 2% N.77°E. (0 2% N.10°E. 10 6 N. 53° W 0 6 N. 55° W. 0 15 Ie HP 1D 2956 N: 23° EB. 2 4 NeDo Wee 12010 IN. 23; We 10) 5 Np GH 1, IO) 7 N. 45° W. O75 N. 42°R. OS ERIE WIG 2 2 N. 12° E. 1 4 N. 37° W. ? N. 68° E. 3° 092 N. 10° E. HES | Near e Il Oo N. 38° BE: abconciec!| N. 85° R. I - 4 NeAOZB (Altec IN tele Ie) MN INIA a ad Ree ee N.E. ? N.E. ? N.W. by W. Rise, Connection, and Termination. 20, XXL. wv. 21, XXII. &. Trap, XXIII. &. 20, XXIV. 2. 21, XXV. &. Trap, XXVI. a. Trap, XXVII. a. Trap, XXVIII. a. Trap, XXIX. a. r, XXX. hi. r, XXXI. hi. r, XXXL* hi, r, XXXIL. &. vr, XXXII. di. 7, XXXIV. o. r, XXXV. 37. r, XXXVI. 35. r, XXXVIL. 35. hk, XXXVIIL. Hi? 37, XXXVIII.38.* k, XXXIX. x. Vi XL. fi. 40, XLI. 42. li, XLII. 48. g, XLII. 48. 0, Ra. g. li, XLIV. o. 44, XLV. 48. 44, XLVI. 48. 48, XLVIL. ra. ra, XLVILII. li. 47, XLIX. ra. Pee e eter rere eeaeeeeeres s, M. x. bro, L. m. 50, LI. 54 or 52. 50, LIT. 54. m, LIIT. 52. bro, LIV. 52. s. Bro. li. bro, LV. 56. Gy UN wh 2,8. 8. 2, LVII. s? s, LVIIT. 60. $s, LIX. x. 59, LX. z. oe WUD NG 2 @, LX. 2: aw, LXIUL. x. 2, LXIV. z. @, LXV. 2x. ————. SSS principal measures which are thrown out all around. Wy 7 REMARKS. At Little Wenlock this fault brings the edges of the coal mea- sures against trap rocks, but there is no mineralogical change : the strata dip rapidly towards this fault: the trap at Saplin Farm is probably on the prolongation of it, Brings inthe Penneystone measure. Crosses 20 and a without producing any apparent change in either, and it is visible in the lime quarries as well as at the New Works. | Forms with 20, k and 22, a small deep trough, inclosing all the Runs at right angles to the igneous axis of Steeraways. Ditto. ditto. Runs diagonally to ditto. At right angles to ditto. Forms with 7 and di a detached triangular trough. The strata between these two faults are elevated 30 feet. This is almost an unique example of a series of four small frac- tures ranging in planes parallel to and at short distances from each other. One fault commencing at a little distance from the termi- nation of another, Forms with part of rock 37, a singular deep trough in the midst of a shallow portion of the field. i Not well known. Runs fromthe Ketley fault at Lawley, past the foot of Small Hill towards Coalmoor Farm south, where it | is lost. | The course of this fault is not very accurately known. The tri- angular district included between it and the Lightmoor and the! Great East faults, contains the deepest-seated portion of the coal measures. In 1838 there was but one pit in this district, | | | Commences at Sturchley, increases rapidly at Randley, where the fall is 120 feet, a quarter of a mile beyond it is 180 feet, and in the | same proportion to Priorslee. | Thins out at Langley. | Forms with 44 and 48 a small triangular area elevated 75 feet | on all sides. Forms with 45 a small narrow trough 75 feet deeper than the | measures on either side, whilst those included in the trough are much pressed up on the sides. Very variable in size and vertical importance in consequence of} its junction with so many faults. | | An anticlinal line, but known in the country as the limestone | fault. (See page 458, bottom line.) | Ranges in an irregular sine, the coal measures rise in steps to- | wards it ; at Blisses, the coal is scoty, the ironstone is red as if cal-! cined, and the shales are hardened, indicating the probable prox. | imity of igneous rocks, which however neither reach the surtace, | nor have been seen under ground. It resembles in these respects, | therefore, fault 4, and is probably a disjointed continuation of g. | Follows the course of the Severn. | temarkable for destroying the parallelism of the disjointed | strata, and its consequent change of relative level at each extre-| mity, being at one end E.N.E. and W.S.W. | | | | Increases rapidly towards bro. | Breaks the connection of the limestone escarpment between! Benthall Edge and Lincoln Hill. Too well known at Broseley by | its causing a speedy and final outcrop of the greater portion of| the coal measures. | Very uniform in vertical importance. | Brings up the Ludlow rocks at Barrow. Probably intersects} Zi, at Tickwood. Animportant disturbance bringing up the Silurian rocks and throwing out all but the lowest strata of the coal measures. It is | L well exhibited at Swinney and at the Dean Corner. | The strata dip rapidly to this fault on the swamp side. | The strata rise at an angle of 45° towards this fault in Turner’s, yard pit. Is probably a continuation of the Madeley, after crossing the Swinney. It ranges parallel to a small anticlinal line. | The strata dip rapidly eastward from this fault, which ranges: parallici to a small anticlinal line. Is exposed near the Wren’s Nest and also at the HebVins. Seen in the brook below the Hook. It may only be connected with the fault which runs along Apley Coppiceand near Sutton} Maddock. | Parallel with the axis of the Wrekin. Ditto. ditto. These two faults form a narrow, deep | trough in the small coal field of Longwood. j a, ay ih a .' * , ba ae peerior ti on Fede Ti . Tr isp my wu 7, Sr Wr hs if yy fy, as [ 497 ] XXXIII*.— Notice of a Letter from Ropert Were Fox, Esyq., to Sir Cuarues Lemon, Bart., F.G.S., relative to the Origin of Mineral Vewns*. {Read April 5, 1838. ] IT can scarcely be doubted, I think, that not only the mechanical deposits in mineral veins, but part, also, of those which are not mechanical, have been derived from the contiguous rocks or strata. It appears to me, however, that there has been another source from whence the latter may have been accumu- lated in almost indefinite quantities. I refer to the deeper parts of the ori- ginal fissures in which the water, at a very high temperature and pressure, must have acted with great energy as a solvent, and become more or less charged with earthy and metallic salts ; and ascending, under these circum- stances, through the upper and cooler portions of the same fluid in the fis- sures, it naturally there produced deposits, in consequence of evaporation, re- duction of temperature, and electrical agency. The circulation of upward and downward currents of water in the fissures must thus have continued until checked or superseded by too great an accumulation of different substances in the latter. The silicious deposits observed in the Geyser, and many other thermal springs, may be cited as examples of this kind of action. The circulation of the water must, moreover, have had some influence in wearing away portions of the sides or walls of the fissures, and may have con- tributed to produce the smoothness for which they are sometimes so remark- able. The hanging walls, it may be presumed, were most exposed to the action of the ascending currents, and the foot walls to that of the descending ones ; but I am not prepared to say whether or not such indications or distinc- tions are discoverable in mineral veins. The water-worn stones, which are occasionally met with in veins, may probably be referred to this cause. I think it is evident that the arrangement of the ores, &c. in different rocks cannot be attributed to simple chemical affinity only, because the accu- mulation of the metallic masses is not found to depend merely on the nature of the containing rock; the ore of a given metal being sometimes found in * Mr. Fox’s first communication on this subject, which was read before the Society, was dated 19th March, 1836. See Geological Proceedings, vol. ii. p. 406. 498 Mr. Fox on Mineral Veins. granite, or in “ elvan,” and not in “ killas,” and sometimes in the latter, and not in either of the former. The remarkable concentration of the ores in some rocks in preference to others, seems rather to have resulted from their relative positions, or other circumstances of a local nature ; and when I con- sidered these very striking phenomena, which everywhere occur, and the actual proofs I had obtained of electrical action in many of our metallic veins, I felt compelled to adopt the conclusion, that some definite agency, such as electricity, must have produced or controlled those relations. My views on this part of the subject, I have more fully stated in my former communication, and I imagine I see more and more reason to believe that the eastward and westward tendency of metallic veins may be ascribed to the electro-magnetic influence of the earth. In some parts of the world there may be found consi- derable deviations from this bearing, owing, perhaps, to local circumstances ; but the coincidence in their direction, generally speaking, is so decided, as clearly to indicate the operation of a generallaw. The greatest deviation in this county from the prevailing strike of our metalliferous veins has been supposed to exist in the tin veins of St. Just. I find, however, that their course, with respect to the true meridian, is, on the average, about N.W. and S.E., and that of the guides, or cross-courses, nearly north and south. It is worthy of remark, that many of the large veins of oxide of iron found in Cornwall, Devon, and other districts, have a north and south bearing, or, rather, are nearly coincident with the magnetic meridian. Much of the quartz in the cross courses may have been brought up in hot water from a great depth, and been gradually deposited as the successive portions of water became reduced in temperature. But the fibrous or crystal- line texture of this quartz, with the axis of the crystals at right angles to the walls of the cross courses, is often so marked and decided, as to indicate the operation of some general cause or force having a definite direction *. * T have obtained, by means of voltaic action, many veins of sulphate of zinc in clay, having a fibrous texture, perpendicular to the veins, like the quartz in cross courses, or like satin spar. Falmouth, January 28, 1837. [ 499 j XXXIV.—Notice on the Remains of a Fossil Monkey from the Ter- tary Strata of the Sewalik Hills in the North of Hindoostan. By Carr. P. T. CAUTLEY, F.G.S., Bengal Artillery ; and H. FALCONER, Ese., M.D., Bengal Medical Service. [Read June 14, 1837.] THE most highly organized mammifers hitherto described in a fossil state, so far as our information extends, belonged to the Cheiroptera; and the instances of these on record are very few*. ‘That quadrumanous remains should be wanting is by no means surprising, without the necessity of supposing that they did not exist. ‘The countries of which the ancient races have been most completely investigated, had a climate unsuited to be the habitat of the tribe, as we now know it, when the more recent or superficial deposits were in pro- gress of formation. If we refer to the remote epochs when the climate was suitable, and when genera now associated with the Monkeys were abundant, it is easy to conceive that the latter might have existed in numbers, without their remains being entombed. It requires in all instances many unconnected circumstances for the preservation of organic bodies, and their subsequent dis- closure. Amongst the most important of these are the habits and organization of the animals themselves. As in the case of birds, it might be predicated, that this lucky concurrence of circumstances would be rare with quadrumanous re- mains. ‘The very perfection in the organization of the Monkey entails, as a consequence, that his solid frame should seldom continue to indicate the pre- vious existence of the individual. His admirable agility and social habits pro- tect him against most aggressions. A flood might suffocate in their dens, over alarge tract of country, the burrowing tribes; and might sweep from under the feet of the monkey hundreds of its herbivorous and predaceous fellow-tenants of the forest, and bury them in the near shingle or far-distant estuary, or drown and deposit them in the stagnant swamp—while he would remain secure. The tree on which he was perched might totter, and yield to the undermining cur- * Brewster’s Edinburgh Journal of Science. VOL. V.—SECOND SERIES. 3 T Pe Oe ee 500 Capt. Cautiey and Dr. Fatconer rent, and he still escape and feed on his wonted fruits, undisturbed by the de- struction around. When the debt of nature comes to be paid, his carcase falls to the ground, and immediately becomes the prey of the numerous predaceous scavengers of torrid regions, the Hyena, the Chacal, and the Wolf. So speedily does this occur, that in India, where Monkeys occupy, in large socie- ties, mango groves around villages, unmolested and cherished by man, the traces of casualties among them are so rarely seen, that the simple Hindoo believes that they bury their dead by night. When the ancient races of India began to open upon us in the new forms and the exuberant variety which the fossils of the Sewalik Hills exhibit, we were early led to anticipate that some trace of quadrumanous animals would soon be met with to perfect a series, which would be incomplete without them. Several months ago we became possessed of a solitary specimen, which put the matter, in our own minds, beyond all doubt. We deferred making it public, however, in the hope of soon finding specimens of the cranium and teeth ; being unwilling to rest the announcement on any thing less character- istic. That chance has since fallen to our fellow-labourers in the pursuit, Messrs. Baker and Durand, of the Bengal Engineers, who have lately disco- vered a specimen, consisting of a considerable portion of the face, and the whole series of molars of one side, of a quadrumanous animal belonging toa much larger species than the bone we found. Our fossil is the specimen which accompanies this communication. It is the astragalus of a right hind leg. It is completely mineralized, having a specific gravity of about 2°8, and it appears to be impregnated with hydrate ofiron. Although but a solitary bone of the foot, the relations of structure are so fixed that the identity of the fossil is as certain as if the entire skeleton were before us. ‘The very shallow excavation of the superior surface (a) [see wood-cut] for the pulley-like articulation with the tibia ; the form and extent of the lateral articulating surfaces (8, c) for the external and internal malleoli ; the considerable elongation of the apophysis for the head and neck of the bone (c,m); the slight obliquity with which it is sent off from the body ; and the diagonal direction and form of the principal articulating surface (p) with the calcaneum, are characters which, taken in conjunction, incontestably prove that the fossil is a quadrumanous astragalus. It would be needless, therefore, to dwell on the points of difference between it and the astragali of those orders of Mammalia which have an allied form. It is only requisite to ascertain how it agrees with the corresponding bone in existing species of Quadrumana. It closely resembles, in size and general form, the astragalus of the Semnopi- thecus Entellus, which we send along with the fossil for comparison. a. nn a ee a a ee eS ee eee ee on Fossil Quadrumana. 501 The principal dimensions are as follow :— Dimensions. Sewalik Fossil Monkey. Semnopithecus Entellus. Extreme length of astragalus................ a |) area i SAD AR A 135 inch. Extreme width of body of astragalus.......... Is —...... Pattee « Bhs 1-03 Denptivef bodys 3 iii. OL 4 Bora : Greatest diameter of navicular head .......... Thickness of ditto ........ eee re ARC ie Fossil (1). Recent (2). The chief peculiarities of the fossil astragalus, compared with that of the Entellus, are these :—The upper articulating surface for the tibia (a) is more convex than in the Entellus, and less square in the outline, the lateral margins (a, b) approximating as they run backwards; the outer one being also more elevated. The peroneal articulation (8) is precisely of the same form and extent as in the Kntellus ; and the rough fossa between it and the large cal- canean surface (p) also corresponds. The articular surface (c) for the inner malleolus somewhat differs: in the fossil it is long, shallow, and rather pyriform in outline, while in the Entellus it is cup-shaped, deeper, and more extensive. Theother pits and inequalities of the inner side correspond ; but the entire surface slopes off more obliquely in the fossil. ‘The great calca- nean surface (p) has the same diagonal direction, with reference to the upper surface, as in the Entellus: it has also the same form, but it is more vaulted, and has less stretch and width. Its inner margin is bounded by the shallow, pulley-shaped fossa (£) for the tendon of the flexor pollicis longus muscle, en- tirely as in the Entellus ; and the rough pit between it and the anterior cal- canean surface (F) is alike in both. The head-and-neck apophysis is sent off @ in the Entellus. The upper surface of the neck (@) is narrower and less sloped. The scaphoid surface of the head (n) is altogether less extensive. The head itself is not so thick and massive, and its long direction slopes more obliquely upwards than in the Entellus ; its inferior articular surface is less, and there is a wide, rectagonal, rough gutter or fossa (x) running half way across, so as to make two surfaces. In the Entellus the fossa is obsolete, and 372 ee ee ee Sn Ta et ee prise Se ebeeg oee 502 Capt. Cautiey and Dr, Fatconer only indicated by a minute foramen, so that these articular surfaces run into one. This is the greatest difference observable in the fossil. The rough fossa at the outer side of the neck is alike in both. With these inconsiderable peculiarities, the fossil agrees so closely in size and general form with the astragalus of the Entellus, that it probably belonged to the same sub-genus : still the points of difference are sufficient to leave no doubt, that the fossil must be assigned to a distinct species. In equalling the Entellus, it would belong to the larger Quadrumana. This is all the inform- ation the specimen conveys, regarding the animal from which it came; but we may hope to meet with remains, which will develope its entire osteology, more especially that of the cranium and face. The fossil was found by a party of Hindoo collectors employed by us on the fossil tract of the Sewalik Hills ; and was brought to us mixed up with a promiscuous collection of the remains of the Hippopotamus, Mastodon, Ruminants, &c., like the specimens which have been sent to the Society. We have not therefore the means of knowing the exact locality where, and the circumstances under which, it was found. The discovery is interesting in itself as supplying a deficient link in the series of the former tenants of the globe; but greatly more so in connexion with the races with which the fossil was associated. We have excavated from, or found in the debris of, different beds of the same formation which yielded the fossil astragalus, the remains of a species of Anoplotherium *, the Crocodilus biporcatus and C. (Leptorhynchus) Gangeticus {, respectively the Magar and Gavial, two species which at the present day inhabit the quiet waters of the Ganges. Here then are two most instructive facts : Quadrumana co-existed with a member of the oldest ascertained pachydermatous genus of Europe ; and two reptiles now the contemporaries of man in the East, lived, and may have laved, in the same waters along with a species of one of the mammiferous genera which characterise the Eocene period of the West ;— affording another illustration of constancy in the order of nature, of an iden- tity of condition in the earth of the olden time with what it exhibits now, and of the invariableness of organized forms. ‘The two decurrent ridges on the face which specifically distinguish the C, beporcatus of the present day, * Anoplotherium Swalense, (No. 6.) a new species, of a size somewhat larger than the J. commune of the Paris basin. The species is known to us by two upper jaws in our possession with the series of molars complete. We therefore quote it unhesitatingly. + Known to us by specimens comprising the whole of the cranium and muzzle. They do not differ more from the existing individuals than these do from one another in varieties dependent on age and sex. Asiatic Researches, Vol. xix. Part II., Art. II. I Se a ul A Se Sa Ase on Fossil Quadrumana. 503 are as marked and distinct on the individuals which existed perhaps centuries of centuries ago; and an ankle bone of the Sewalik fossil Monkey so closely resembles that of a living species, that it is difficult to explain the dif- ference. The Sewalik fossils abound in monuments of this sort. There is a mixture of the new and of the old, of the past and of the present, of familiar with surprising forms, together with a numerical richness, such as no other ex- plored region has exhibited within so comparatively limited a space. The Camel*, the Antelope, and Anoplotherium, have been found, intermixed with each other in the same bed. ‘There are remains of the Elephant, Ma- stodon, Hippopotamust, Anthracotherium, Rhinocerost, Hog, and Horse ; the Tapir alone of the large existing Pachydermata being without a repre- sentative. In the Sivatherium§ is seen a huge Ruminant exceeding in size the largest Rhinoceros ; it is also armed with four enormous sheathed horns, divided and foliated like the Dicranocerine Antelopes, and able to contend for mastery with the Mastodon. Contrasted with him in the same family is the puny Musk Deer, scarcely larger than a Hare. There are the Cat|| and the Dog tribe, the Hyena, Bear{, and Ratel**, and other Carnivora. In the feathered races, there are Gralla, greatly surpassing in size the Gigantic Crane of Bengal (Cicona Argala). Among the Reptilia, besides the Magar and Gavial, there were other Crecodilest+ of enormous bulk, approaching the largest Saurians ; and the Testudinata, which have hitherto held but a humble rank beside their Saurian co-ordinals, here show their giant representatives. In addition to numerous species of Emys and Trionyx not bigger than the * Camelus Sivalensis (Nob.), Asiatic Researches, Vol. xix. Part II., Art. X., a species of the size of the existing Camel. + Asiat. Res., Art. III. Hippopotamus Sivalensis (Nob. & H. dissimilis, Nob.). t Journal of the Asiatic Society, Vol. iv. p. 706, and vol. v. p. 486. § Asiat. Research. ut supra, Art. 1, Sivatherium Giganteum (Nob.). Since the memoir was printed, Col. Colvin, Bengal Engineers, has got a specimen of the cranium with the bases of the four horns attached, and we have in our possession an almost entire rear horn, which has given the characters noted above. || Zbid. Art. XI. Felis cristata (Nob.). Smaller than the Tiger. q Jbid. Art. XII. Ursus Sivalensis (Nob.). Size of the U. Speleus. ** Messrs. Baker and Durand, Journ. Asiatic Society, Vol. v. p. 581. ++ C. Leptorhynchus crassidens (Nob.), an immense species far exceeding existing ones, and forming a passage from the Gavials into the true Crocodiles. It has the cylindrical muzzle and synostorized lower jaw of the former with the blunt thick teeth of the latter. 504 Capt. Cautiey and Dr. Fatconer on Fossil Quadrumana. small Terrapins of the sluggish brooks of Hindoostan, we possess humeri and femora of this tribe (with corresponding fragments of the bucklers) as large as the equivalent bones of the Indian Rhinoceros. As the Pterodactyle more than realized the most extravagant idea of the Winged Dragon, so does this huge Tortoise come up to the lofty conceptions of Hindoo mythology: and could we but recall the monsters to life, it were not difficult to imagine an Elephant supported on its back. Suharun Poor, Nov. 24th, 1836. [ 5605 XXXV.—On the Formation of Mould. By CHARLES DARWIN, Esq., F.R.S., Sec. G.S. [Read November 1, 1837. | THE formation of the superficial layer of earth, commonly called vegetable mould, offers some difficulties in being fully understood, which apparently have been overlooked. In old pasture lands, the mould, to the depth of a few inches, differs but slightly, although resting upon various kinds of sub-soil. The uniform fineness of its particles is one of its chief distinguishing characters ; and this may be well observed ina gravelly country, where arecently ploughed field immediately adjoins another, which has long remained undisturbed for grazing. In the latter, not a pebble will be seen, either on the surface or im- mediately below it; although in the ploughed field, a large proportion of the soil may be composed of small stones. From the prevailing use of the ex- pression “‘ vegetable mould,” it would appear that its origin is generally at- tributed to some effect of vegetation ; yet it is scarcely conceivable that the turf, in the case of the two adjoining fields, can have produced so remarkable a difference as that alluded to. My attention was called to this subject by Mr. Wedgwood, who showed me, whilst I was staying at Maer Hall, in Staffordshire, several fields, some of which a few years previously had been covered with lime, and others with burnt marl and cinders. These substances, in every case, were buried some inches beneath the turf. In several parts of three grazing fields, I dug square holes, and obtained the following results :—Ist. In some good pasture land which had been limed, without having been ploughed, about ten years before, the turf, or the layer in which the roots of the grasses are closely woven together, was about half an inch thick. At two inches and a half be- neath this, or about three from the surface, a layer of lime, or a row of small aggregated lumps of it, formed a well-marked white line around the holes. The soil beneath this layer of lime was gravelly, or of a coarse sandy nature, and differed considerably from the mould nearer the surface. About three years ago cinders also had been spread on this field; but when I examined it, they were buried at the depth of one inch. They were not sufficiently nu- merous to form a layer, though a line of black spots could clearly be traced 506 C. Darwin, Esq., on the parallel to and above the white one of lime. Some other cinders, which had been scattered in another part of this same field, only about half a year be- fore, lay either on the surface or were entangled in the roots of the grass. The second field, I mention only from the fact of the cinders being buried in such quantities, about three inches deep, as to form a stratum nearly one inch in thickness. The layer in some parts was so continuous, that the upper soil was united to the lower only by the longer roots of the grasses. The sub-soil was a red clay, and it occurred a little below the cinders. The third case which I shall describe, is that of a field which, Mr. Wedg- wood informed me, was waste land fifteen years ago. It was at that time drained, ploughed, harrowed, and well covered with burnt marl and cinders. It has not been disturbed since, and now supports a tolerably good but rather ——— — SS = = —=$——> ——— —SSSSSSaeasasasas5sSSS555 A, Cinders. B. Burnt Marl. C. Quartz Pebbles. coarse pasture. The section in this field, as represented in the wood-cut, was, turf half an inch ; vegetable mould two inches and a half; a layer, one anda half inch thick, of fragments of burnt marl, (conspicuous from their bright red colour), of cinders, and a few quartz pebbles, mingled with earth. One of the angular fragments of burnt marl lying near the bottom, measured one inch in length by half an inch in breadth, and a quarter in thickness. Lastly, about four inches and a half below the surface, was the original black peaty soil. We thus find, beneath a layer, nearly four inches thick, composed of Formation of Mould. 507 fine particles of earth mixed with decayed vegetable matter, those substances which had been spread on the surface fifteen years before. The appearance in all the above cases was, as if (in the language of the farmers, who are acquainted with these facts) the fragments had worked themselves down. It is, however, scarcely possible that cinders or pebbles, and still less powdered quick-lime, could sink through compact earth and a layer of matted roots of vegetables, to a depth of some inches ; nor is it at all probable that the decay of the grass, although adding to the surface some of the consti- tuent parts of the mould, should separate in so short a time the fine from the coarse earth, and accumulate the former on those objects, which so lately had been on the surface. I may add, that I have repeatedly observed fragments of pottery and bones buried beneath the turf, in fields near towns, (on which such substances are often thrown with manure); and as these fields did not appear to have been ploughed, the circumstance often surprised me. On the contrary, J have noticed in gardens lately dug, that the rain, by washing away the finer particles, leaves stones and other hard bodies accumulated on the surface. The explanation of these facts, which occurred to Mr. Wedgwood, although it may appear trivial at first, I have not the least doubt is the correct one, namely, that the whole operation is due to the digestive process of the com- mon earth-worm. On carefully examining between the blades of grass in the fields above described, I found scarcely a space of two inches square without a little heap of the cylindrical castings of worms. It is well known, that worms, in their excavations, swallow earthy matter, and that, having separated the portion which serves for their nutriment, they eject at the mouth of their burrows the remainder in little, intestine-shaped heaps. These partly retain their form until the rain and thaws of winter, as I have observed, spread the matter uniformly over the surface. The worm is unable to swallow coarse particles, and as it would naturally avoid pure or caustic lime, the finer earth lying beneath the cinders, burnt marl, or lime, would be removed, by a slow process, to the surface. This supposition is not imaginary ; for in the field in which cinders had been spread out only half a year before, I actually saw the castings of the worms heaped on the smaller fragments. Nor, I repeat, is the agency so trivial as at first it might be thought: the great number of earth-worms, as every one must be aware who has ever dug in a grass field, making up for the insignificant quantity of the work which each performs. On the idea of the superficial mould having been thus prepared, the advan- tage of old pasture land, which it is well known farmers in England are par- ticularly averse to break up, is explained ; for the length of time required VOL, V.—SECOND SERIES. 3uU 508 C. Darwin, Esq., on the to form a thick stratum must be considerable. In the peaty field, in the course of fifteen years, about three inches and a half had been well prepared; but it is probable that the process is continued, though at a very slow rate, toa much greater depth. Every time a worm is driven, by dry weather or any other cause, to descend deep, it must bring to the surface, when it empties the contents of its body, a few particles of fresh earth*. Thus, the manures added by man, as well as the original constituent parts of the soil, become thoroughly mingled, and a nearly homogeneous character is given to the whole. Although the conclusion may appear at first startling, it will be difficult to deny the probability, that every particle of earth forming the bed from which the turf in old pasture land springs, has passed through the intestines of worms ; and hence the term “ animal mould” would in some respects be more appro- priate than that of “ vegetable mould.” I may conclude by remarking, that the agriculturist in ploughing the ground follows a method strictly natural; he only imitates in a rude manner, without being able either to bury the pebbles or to sift the fine from the coarse earth, the work which nature is daily performing by the agency of the earth- worm. Note.—Since my communication on the “ formation of mould,” read on the 1st of November, I have received from Staffordshire an account which corroborates the statements then made, on the apparent sinking of objects placed on the surface of turf land. The first case I mention only because the substance is different from those previously described. In the spring of 1835 a boggy field, which had long remained as grass land, was so thickly covered with sand that the whole surface appeared of a red colour. At the present time, namely about two years and a half afterwards, the sand forms * Mr. W. Lindsay Carnagie of Kimblethment, writing from Scotland to Mr. Lyell on the subject of this paper, as it is given in the Proceedings, states, that in clearing away a stiff clayey soil above a stone quarry, he has seen worms in small chambered passages between seven and eight feet below the surface. The black mould on the clay was there two feet thick. Mr. Car- nagie observes, also, in his letter, that the Scotch farmers, from a belief that the lime itself has some tendency to sink, are afraid of putting it on ploughed land until just before it is laid down for pasture. He then adds, “‘ Some years since, in autumn, I laid lime on an oat-stubble and ploughed it down; thus bringing it into immediate contact with the dead vegetable matter, and securing its thorough mixture through the means of all subsequent operations of fallow ; I was considered, in consequence of the above prejudice, to have committed a great fault, but the result was eminently successful, and the practice partially followed. By means of Mr. Darwin’s ob- servations, I think the prejudice will be entirely removed.”—June 1838. Formation of Mould. 509 a layer three-fourths of an inch below the surface, that thickness consisting of peaty soil. The second case is more interesting. It has been ascertained that a field, which has since been ploughed, was covered about eighty years ago with marl; an imperfect layer of it, but sufficiently distinct to be traced, is now found at a depth, very carefully measured from the surface, of twelve inches in some parts and fourteen in others: the difference corresponding to the top and hollow of the ridges produced by ploughing. It is certain, the marl must have sunk or been buried before the field was ploughed, for otherwise the fragments would have been scattered in the soil: this conclusion, moreover, explains the circumstance of the layer being horizontal, whilst the surface is ‘undulating. At the present time no plough could possibly touch the marl, as the land in this country is never turned up to a greater depth than eight inches. Jn the preceding communication, I have shown, that in a field lately reclaimed from being waste land, three inches of mould had been prepared by the worms in the course of fifteen years. We now find, that within a period of less than eighty years, (but how much less cannot be told, unless the date when the field was first ploughed were known) the earth-worms have covered the marl, which was originally strewed on the surface, with a bed of earth of an average thickness of no less than twelve or thirteen inches. November 14, 1837. : | pew ex “ ee ‘ hb ri cu MtiR pit Te ea : Dem 7 hale hae ay li pe Beat [Perk] XXXVI.—Note on the Dislocation of the Tail at a certain point ob- servable in the Skeleton of many Ichthyosauri. By RICHARD OWEN, Esg., F.R.S., F.G.S., Hunterian Professor to the Royal College of Surgeons, London. Pirate XLII. [Read March 2lst, 1838.] IF the Cetacea, like the Enaliosauria, were known only by their fossilized skeletons, itcan hardly be doubted but that their conjecturally-restored figures as when entire and alive, would have resembled, so far at least as regards the form of the tail, those which have been published ofthe Ichthyosaurus. It may, I think, be safely affirmed, that the depressed or flattened shape of the small vertebral centres which terminate the gradually tapering tail in the skeleton of the Dolphins and Whales, would never of themselves have suggested the ex- istence, in the recent and entire animal, of so large and important an instrument of locomotion, due entirely to unossified and readily decomposable material, which the actual presence of these fish-like Mammalia in the existing state of things, places beyond the necessity of speculation and conjecture. The relation, however, which the slight modification of the terminal caudal vertebra above alluded to bears to the presence of a large, horizontal, liga- mentous fin, induced me some time ago to examine such specimens of skele- tons of Ichthyosauri and Plesiosauri, having the tail complete, as were access- ible in London, with the view to obtain evidence of the possible existence or trace of a similar structure in these species; but I was then unable to obtain from the imbedded vertebre satisfactory proof of their exchanging a com- pressed for a depressed form at this part, or deviating in any way (save in size, number of articular surfaces, and, in the Plesiosaurz, in the greater ex- cavation of their anterior and posterior surfaces of articulation) from the rest of the vertebree of the tail. I concluded, therefore, that these air-breathing inhabitants of the ancient deep, partly from being cold-blooded, as the condi- tion of the ossification of their skeleton proves, and therefore slow breathers, and more especially on account of the superaddition of posterior paddles, were devoid of any locomotive organ analogous to the tail-fin of the Cetacea; and i eae a ee ee a ee 512 R. Owen, Esq., on the that the hinder paddles principally served the purpose, in the absence of such a horizontal terminal fin, in bringing the head to the surface for the purpose of breathing. Having recently examined many saurian skeletons now in London, the greater part of which have been disencumbered of their earthy shroud by the chisel of Mr. Hawkins, a condition of the tail which, on a former occasion, in a single instance had arrested my attention, but without calling up any theory to account for it, now more forcibly engaged my thoughts, from observing that it was repeated, with scarcely any variation, in five instances. The con- dition to which I allude is an abrupt bend or dislocation of the tail at about one-third of its whole length distant from the end; generally about the thir- tieth caudal vertebra in the Ichthyosaurus communis; the terminal por- tion continuing, after the bend, almost as straight as the portion of the tail preceding it. In short, the appearance presented is precisely that of a stick which has been broken, and with the broken end still left attached, and de- pending at an open angle. Now there is no modification of the vertebra, where this bend takes place in the tail of the Ichthyosaurz indicative of the tail having possessed, during the lifetime of the animal, greater mobility at this particular point than at any other ; and it is scarcely possible to conceive how any force operating on the dead carcase at the bottom of the sea, or when it was imbedded in sediment- ary deposits, could produce a fracture or dislocation of the tail at the precise point at which we find it in so many specimens, otherwise very dissimilar in regard to their general position and degree of perfection. I incline to believe, therefore, that the appearance is due to the operation of some force acting upon a ligamentous fin attached to that part of the extremity of the tail which is thus bent down; and that this force operated while the dead animal was floating and buoyed up by the gases generated by putrefaction, and when the ligaments and other connexions of the caudal vertebra had been so far loosened as to allow the force which previously would have bent down the tail in a general curve like the top of a fishing-rod, to overcome the diminished resistance of the decomposing joints immediately proximal of its point of action, and dislocate the vertebre at that part. The two portions of the tail, like the rest of the skeleton, would then continue to be held together by the common integument, until the rupture of the parietes of the abdomen would allow the pent-up gas to escape, and the body to sink to the bottom. In thus descending through a sufficiently tranquil medium, the back being weighted with the heavy vertebral column, would be most likely the first part to touch the bottom ; and if this consisted of soft clay or mud, a heavy trunk, Dislocation of the Tail of the Ichthyosauri. 513 like that of the Ichthyosaurus, would immediately subside therein back down- wards, while the broken tail, supported by its flat surface, would afterwards be dragged down at an angle with the trunk, and with its extremity directed towards the ventral—now, as when the body floated, the uppermost side of the body: this is, in fact, the position in which the broken part of the tail is ge- nerally placed in the fossil skeletons. The prevailing amount of dislocation which most of the skeletons of the Ich- thyosauri present, is exactly such as might be conceived to take place in a dead animal body buoyed up sufficiently long to allow of a partial separation of the connecting ligaments and cartilages ; the probable toughness of the integu- ments of the Enaliosaurians would tend to retain the gases generated by pu- trefaction sufficiently long to enable this extent of decomposition to take place while the animal floated, at least in regard to the ribs and bones of the pectoral and pelvic arches. The bones of the paddles on the contrary, and those of the tail, being connected together by denser ligaments and surrounded by a less proportion of soft animal matter, would be more likely to sink comparatively undisturbed, with the rest of the trunk, when the buoyant gases were ulti- mately set free. The dead carcasses of the Ichthyosauri would of course be subject to such dislocations and separations as the attacks of predatory animals on a floating dead body would produce ; but the appearance in the tail of the Ichthyosaurus here alluded to, is too uniform and common to be due entirely to an accidental and extrinsic cause. I am therefore disposed to attribute it to an influence connected with some structure of the recent animal ; and most probably to the presence of a terminal tegumentary and ligamentous caudal fin, which, either by its weight, or by the force of the waves beating upon its extended surface, or by the action of predatory animals of strength sufficient to tug at without tearing it off, might, under the circumstances already mentioned, give rise to a dislocation of the caudal vertebree immediately proximal of its at- tachment. We have evidence, however, in the form of the vertebre that the supposed fin was not a horizontal one, and I have already observed that the superaddition of posterior paddles in these air-breathing marine animals is the compensation for the absence of such an organ ; and, therefore, a tegument- ary fin, if developed at the extremity of the tail, would probably be placed in the position best adapted to produce with rapidity those lateral movements of the head most needed in a short-necked predatory aquatic animal. Since the preceding notes were written and read to the Society, I have had the opportunity of detaching some of the terminal caudal vertebra of an Ichthyosaurus communis from the substance in which they were imbedded ; = a, + oie —— = a z EN a — — 514 R. Owen, Esq., on the Dislocation of the Tail of the Ichthyosauri. and have received, through the kindness of Sir Philip Grey Egerton, a sepa- rate terminal caudal vertebra of an Ichthyosaurus from Lyme Regis, all of which exhibit a compressed form nearly as well marked, in comparison to the vertebre of the rest of the spine, as is the depressed form in the terminal ver- tebrz of the Cetacea. ‘This structure offers additional and very satisfactory proof of the existence of a caudal tegumentary fin expanded in the vertical direction. Such a fin would be especially useful in the short- and stiff-necked Ichthyosaur ; while in the Plesiosaur, where the length and structure of the neck are so favourable for rapid lateral inflections of the head, an instrument like that which produces the corresponding movements in fishes would be un- necessary. Now, it is an interesting fact, that in all those skeletons of Ple- siosaurs in which the tail is perfect, it is straight ; and there is no indication of the partial fracture or bend in them, which is so common in the tails of the Ichthyosaurs. March 18th, 1838. Se ee ee ee [ 515 XXXVII. —A Description of a Specimen of the PLEstosaurus Macro- cEPHALUS, Conybeare, in the Collection of Viscount Corr, M.P., D.C.L., F.G.S., &c. By RICHARD OWEN, Esq., F.R.S., F.G.S., Hunterian Professor to the Royal College of Surgeons, London. Piates XLIII., XLIV., XLV. [Read April 4th, 1838.] LorD COLE having done me the honour to transmit to me for description, his unique specimen of the Plesiosaurus macrocephalus, 1 have endeavoured to devote to it an examination equivalent in care and detail to the admirable completeness of many of its parts, and have reason to hope that it will throw additional light on the Plesiosaurian modifications of the vertebrate skeleton, as well as on some interesting points in general osteology. The study of the spinal column has induced me to reconsider the views generally adopted as to the composition of a vertebra; and I have found it convenient, if not abso- lutely requisite, to give new names, applicable both in the abstract and con- crete senses, to some of the component vertebral elements. The chief specific characters are also premised of another Plesiosaur, which, from the complete- ness of its skeletons in our national and other collections, it seemed most advan- tageous to adopt as a term of comparison with the present specimen. The species to which I refer, is that which is described and figured in Mr. Hawkins’s memoir on Ichthyosaurt and Plesiosauri*, under the name of Tria- tarsostinus ; but as this designation relates to an imperfect state of the tarsus in the right foot, (for a fourth bone is present in the left tarsus of the same specimen, and a second specimen of the same species in Mr. Hawkins’s col- lection exhibits five tarsal bones on each side,) I prepose to refer to it under the name of Hawkins’s Plesiosaur (Plestosaurus Hawkinsi), as a well- deserved tribute to the indefatigable labour and remarkable skill to which we are indebted for our knowledge of this interesting species. 'To subse- quent figures, as well as to the casts of this beautiful fossil, has been applied the name of Pl. Dolichodeirus, which was originally given by Mr. Cony- beare to the Plesiosaur in the collection of His Grace the Duke of Buck- * Plate XXIV. VOL. Y.—SECOND SERIES. 3x 516 Ricuarp Owen, Esq., on the ingham : but after a comparison of Hawkins’s Plesiosaur with the cast of the Plesiosaurus Dolichodeirus in the collection of the Geological Society, and with the original remains of a second specimen of the same species in the British Museum, figured in Dr. Buckland’s comprehensive and instructive Bridgewater Treatise, I find the following differences :— The neck, in Hawkins’s species, is hardly more than three times the length of the head; while, in the Pl. Dolichodeirus it is four times that length. Mr. Conybeare states that the neck in the Duke of Buckingham’s specimen is fully equal in length to the body and tail; but in Haw- kins’s Plesiosaur, the length of the neck only, slightly exceeds that of the body or trunk; and this difference depends both on a difference in the number as well as in the form of the cervical vertebra. The cervical vertebra in the PJ. Dolichodeirus, reckoning as such those which supported hatchet- shaped, and not rib-like, lateral appendages, are, according to Mr. Conybeare, thirty-five in num- ber; while the corresponding vertebre in Hawkins’s Plesiosaur are twenty-nine in number. The cervical vertebre in the latter are also shorter in proportion to their breadth than are those of the Pl. Dolichodeirus. The head in Hawkins’s Plesiosaur is relatively longer than in the Pl. Do- lichodeirus, equalling a tenth part of the total length of the skeleton; while in the Pl. Dolicho- deirus it forms, Mr. Conybeare says, less than a thirteenth part of the same. A more readily appreciable difference is presented in the forms and relative sizes of the ulna and tibia in these nearly allied species. In the Pl. Dolichodeirus, the ulna, or posterior of the two bones which succeed the humerus, is as long as the radius; and its margin next the radius is but slightly concave. In Hawkins’s Plesiosaur the ulna is shorter than the radius, broader in propor- tion to its length, and with a deeper concavity on its inner margin. In Hawkins’s Plesiosaur, the fibula, in regard to its relative length and breadth, and its bent or reniform figure, and particularly with respect to the curvature of its outer margin, deviates in a greater degree than the ulna from the corresponding bone in the P/. Dolichodeirus. The differential characters afforded by the bones of the fore-arm and leg are the more satis- factory, because, as we shall presently see, the Plestosaurus Macrocephalus again presents different and characteristic forms of the same bones. There are other and slighter differences in the shape of the hatchet-bones, or cervical ribs, of the humerus, and of the femur; but as the aim of the present paper is restricted to the characters of the skeleton of the Plesiosaurus Macrocephalus, my object will be gained if it be admitted that sufficient proof has been adduced of the specific difference between the Plesiosaurus Dolichodeirus and the species with which I wish more imme- diately to compare the Plesiosaurus Macrocephalus. The skeleton of the Plesiosaurus Macrocephalus (P|. XLIII.) now under consideration rests upon its under or ventral surface, with the neck and head bent to the left side, so as to describe, with the rest of the vertebral column, almost a semicircle, indicating the extent to which the living animal must have enjoyed the power of lateral inflections of the neck. The exposed part of the skeleton gives a view of the upper surface and right side of the head, which is, however, somewhat crushed and mutilated. A similar view is obtained of the cervical vertebra ; but these are in general perfect, and so turned as gradually to expose more of the dorsal surface at eee ss CGE ee ae Structure of the Plesiosaurus Macrocephalus. 517 the root of the neck: and the seventh, eighth, and ninth cervical vertebra are displaced, and their component parts dislocated, so as to bring into view the upper surface of the bodies. The dorsal vertebre are also inclined to the left side, presenting principally their sides to the observer. Dislocation of the component parts of all these vertebra has taken place to a greater or less degree, but principally in the lumbar and sacral regions. A great proportion of the caudal vertebra is lost; and of those that re- main, all the apophyses are separated from the bodies. The fore and hind paddles of the left side are in a beautiful state of pre- servation. The greater part of the right fore-paddle is also present; but there is no trace of the hind paddle of the corresponding side, excepting the dislocated portions of the pelvic arch to which it was attached. Owing to the position of the skeleton, the structure of both the pectoral and pelvic arches is more or less obscured. Of the Trunk. The number of vertebre, from the atlas to the first caudal inclusive, is fifty-two. They are generally characterised by having a less antero-posterior extent of body, and a greater antero-posterior extent of the spinous process, than in the Plestosaurus Hawkins. Those vertebre, as the seventh, eighth, and ninth cervical, in which I have been able to examine the under-surface of the body, have presented a broad and slightly-produced longitudinal ridge along the middle line ; a character, however, which may be observed in a slighter degree in the cervical vertebra of the Pl. Hawkinsi. In the generic characters afforded by these parts of the skeleton, the ver- tebre of the Plesiosaurus Macrocephalus correspond with those which Mr. Conybeare has described in the original and admirable memoir* devoted to the determination of this most interesting genus of Enaliosaurs. Before, however, proceeding to compare the vertebre of the several regions of the spine in the Plestosaurus Macrocephalus and Plesiosaurus Hawkinsii, I would offer a few observations on the composition of a vertebra in the abstract. At the commencement of my examination of the fossil remains of the Enalio- saurians, I endeavoured to apply to the parts of the vertebra, (which in these animals are frequently complicated, and with the elements more or less dislo- cated) the views and nomenclature of M. Geoffroy St. Hilaire, whose analysis * Geol. Trans., Lond., vol. v., part 2. Sexe iat at = a 2 = ~ = P ee 518 Ricuarp Owen, Esq., on the of a vertebra in the abstract, has been generally adopted in this country. I was compelled, however, to relinquish the advantage which the vertebral theory of that philosophical anatomist seemed to promise, finding that it did not agree with my observations either on the cartilaginous or osseous centres as they ap- pear in the development of a vertebra in the embryo ; or on the fully-developed elements as they are exhibited in different classes of the vertebrate series ; more especially in certain parts of the vertebral column of the Plestosaurus. I need hardly observe that a vertebra may be traced through its various de- grees of complication, either in the progressive stages of growth of a complete example, or by taking permanently-formed vertebre in different animals ; or, in many instances, by comparing them in different parts of the spine in the same animal. The terminal vertebrz of the tail in most species exhibit the simplest con- dition of these bones. The most complicated vertebre which I have yet met with are those at the lower part of the neck of a pelican (PI. XLIV., fig. 3.) and some other birds, or the beginning of the tail of a python (PI. XLIV., fig. 2.), or other large serpent. The parts or processes of such a vertebra may be divided into autogenous, or those which are independently developed in separate cartilages, and exo- genous, or those which shoot out as continuations from these independent constituents: the latter are indicated by dotted lines in the diagram, fig. 1., Pl. XLIV. The autogenous, or true elements, are, Ist. The centrum or body of the vertebra, which, in Mammalia, as Cuvier has observed, is complicated by two epiphyses. 2nd. 'T'wo superior lamine developed to protect the great nervous chord which rests on the upper surface of the centrum, and which I have therefore proposed to call newrapophyses*. In some Chondropterygians each centrum supports four superior lamine. 3rd. Two inferior lamine developed, generally to protect the great blood- vessels on the under surface of the centrum, and which I have proposed to call hemapophyses +. * They are the pertaux, or perivertebral elements of Geoffroy St. Hilaire. + These are the chevron bones of Mr. Conybeare, the paraaux, or paravertebral elements of Geoffroy St. Hilaire ;—terms which he also applies to the costal processes,—regarding these as the expanded halves of the chevron bones. If I had adopted Geoffroy’s term, “ paraal,” or its English equivalent, “* paravertebral element,” I must have diverted it from its original sense, in which it is applicable to two distinct elements, viz. the ribs and chevron bones, which will be seen to co-exist in certain vertebre of the Enaliosauri, and some existing animals; and I have preferred, therefore, to invent and define a new term, which has the advantage of expressing a physiological relation ; and I am happy in being able to cite the authority of Cuvier for the propriety of this step. His Structure of the Plesiosaurus Macrocephalus. 519 4th. The superior spinous process*, which is connected, and generally an- chylosed with the distal extremities of the neuwrapophyses, and forms, in con- junction with those processes, the superior arch of the vertebra. 5th. An inferior spinous process+, which is connected and commonly an- chylosed with the distal extremities of the hemapophyses, forming, in con- junction with these, a chevron or v-shaped bone. To the category of autogenous vertebral pieces belong the ribs, which ge- nerally are anchylosed to the other vertebral elements in-the cervical, sacral, and caudal vertebrz of the warm-blooded vertebrate classes. The propriety of regarding the ribs as vertebral elements is well illus- trated in the Plesiosaurus, in the cervical, sacral, and caudal vertebre of which they assume the form of, and have been generally described as, trans- verse processes, although they are separate bones. These elements bear the same relation to the centrum and its true transverse processes which the spinous processes do to the neur- and hem-apophyses, but they are more rarely anchylosed at their central or proximal extremities. The length which the ribs attain need form no objection to their being re- garded as parts of a vertebra, when it is remembered that the spinous pro- cesses, both above and below, are in some fishes longer than the longest ribs in the same skeleton. In the system of M. Geoffroy St. Hilaire the nine elements of a vertebra are completed by reckoning the spines of the dermal skeleton which, in fishes, are intercalated or articulated with the neural and hemal spines of the true endo-skeleton as essential elements of a vertebra; and the paraaux, or hema- pophyses, are described as being developed in length and changed in direc- tion in order to form the vertebral ribs of the thoracic and abdominal regions. The vertebre of the Bird and Ophidian, already alluded to, prove that ver- tebral ribs and inferior lamin or heemapophyses may co-exist, and the com- position of the spine of the Plesiosaurus, especially in the caudal region, well illustrates this fact ; for the costal appendages, which are generally an- chylosed to the other vertebral elements in the cervical, sacral, and caudal regions of the spine of the warm-blooded vertebrate classes, retain their ori- words are, in reference to an analogous case, “ Donner a un mot connu un sens nouveau est toujours un procédé dangereux, et, sil’on avoit besoin d’exprimer une idée nouvelle, il vaudroit encore mieux inventer un nouveau terme, que d’en détourner ainsi un ancien.”—Mem. du Mus., tome ix. p. 123. * This is regarded by Geoffroy to consist essentially of two lateral moieties, termed épiaua, or epivertebral elements. + The hypothesis of Geoffroy necessitates the consideration of this part as being essentially double, forming the cataauz, or catavertebral elements. oe Py eee = ne ay = ~~» Ze 520 Ricuarp Owen, Esq., on the ginal separate condition throughout the vertebral column in the Plesiosaur, and pass by such imperceptible gradations from one condition of physiolo- gical subserviency to another, that their nature cannot be mistaken when the entire series is viewed in a complete skeleton ; although, when viewed in detached vertebre of the neck or tail, they present the appearance and have been generally described as hatchet-bones or transverse processes. True transverse processes are, however, always exogenous, or mere pro- jections from the centrum or neurapophyses, and are of secondary importance. They are of two kinds, superior and inferior; both are present in the cervical vertebre in most classes ; the inferior transverse processes alone are deve- loped in fishes. The oblique, or articulating processes, are also exogenous, and may be developed either from the neurapophyses or the base of the superior spines of the vertebre. As in other complicated bones resulting from an association of several osseous pieces, certain elements of a vertebra may be modified in position and proportions so as to perform the ordinary functions of others, which may be atrophied or absent: thus in fishes, the inferior transverse processes are gradually bent downwards, until, in the caudal region, their extremities meet and perform the functions of the hamapophyses. The costal processes or ribs are considered by Geoffroy St. Hilaire* to un- dergo in the Cetacea, a similar change of direction, and also a dislocation from their usual attachments ; and to have their distal extremities bent downwards, and anchylosed to a rudimental spine, so as to assume the form and perform the offices of chevron-bones or hemapophyses; but as the horizontal pro- cesses of the caudal vertebre in the Cetacea (as exemplified in the skeleton of a young Balena Antarctica, fourteen feet in length, which I have lately had the opportunity of examining,) are originally developed from distinct centres, and in distinct cartilages, they appear to me to represent, with the corresponding permanently separate vertebral elements in the Plestosaurs, the true costal appendages of the tail ; and the hemapophyses must, therefore, be regarded as other and different elements of the vertebra. This view is supported by the fact, that the long transverse processes supporting the ribs in the thoracic region of the spine in the same young Whale, have no osseous nuclei developed in them, but are continuous cartilages from the still unossi- fied parts of the centrum. I may observe also, that the hamapophyses in the young Cetaceans examined by me, exhibit what appears to be their permanent condition in the Enaliosaurians, viz. a want of bony union at their distal extre- * Mem. du Muséum, ix. p. 118. Structure of the Plesiosaurus Macrocephalus. 521 mities ; at least I have never yet observed a true chevron-shaped bone, suchas results from the anchylosis alluded to, in any skeleton of an Enaliosaurian. Of the vertebral elements albove enumerated, the centrum is the most con- stant in its existence; but the neurapophyses and their spines are the most constant in regard to ossification : there is an obvious reason (in the import- ance of the nervous chord which they are destined to protect), why these parts should be firm when circumstances might forbid the consolidation of the other vertebral elements. ‘Thus, the neurapophyses are cartilaginous in the Lampreys or Petromyzontide, while the centrum is gelatinous, and they are the firmest cartilaginous parts of the vertebra in the higher Chondropterygians. The neurapophyses and their spines are completely ossified in the Lepido- siren, while the bodies of the vertebre are represented by a fibro-gelatinous chord. A similar condition appears to have obtained in the fossil Microdons and some other osseous fishes, in which the ossified neurapophyses and he- mapophyses have been preserved, while the bodies of the vertebre are lost. I now proceed to apply the preceding views of the elementary parts of a vertebra to the exposition of the general characters of the vertebral column in the Plesiosaurt. Vertebral Column. The cervical vertebrae of the Plesiosaurt generally present the following parts in a separate or unanchylosed state,—the centre, the neurapophyses, and ribs ; and it is interesting to observe, that although, in general, no trans- verse processes are developed in this region, an analogy with the structure characteristic of this part of the spine in the Crocodile, is maintained in the ‘division of the articular surface for the cervical rib into an upper and lower portion by a horizontal fissure ; which structure is well described and figured by Mr. Conybeare in the Plesiosaurus Dolichodeirus. In Mammalia the interspace of the two cervical transverse processes is oc- cupied by the vertebral artery : in birds by the vertebral artery and sympa- thetic nerve : in the Plesiosaurus it is too inconsiderable to lead us to imagine it to have been subservient to the protection of any important vessel or nerve ; but its existence, besides being referable to the law of adherence to type, may also have had relation to the presence of an interarticular ligament for the purpose of firmly connecting the head of the cervical rib to the body. As the cervical vertebre in the genus Plestosaurus approach the dorsal, the inferior part of the costal articulation becomes smaller, and a correspond- ing increase of surface is afforded by the superior facet, which also gradually rises from the centrum to the neurapophyses, and in the dorsal vertebra stands 522 Ricuarp Owen, Esq., on the boldly out as a true transverse process from the upper side of the base of each neurapophysis. At the sacral vertebre, however, the transverse processes subside to the level of the neurapophyses ; and, as the caudal vertebre re- cede from the trunk, the articular surface, which, as in the neck, represents, or is in the situation of the transverse process, gradually descends and passes from the neurapophysis to the side of the centrum ; but it is not divided by the longitudinal groove which characterizes the costal surface in the neck. This groove is more marked in some than in other species of Plesiosaurus ; and I have seen Plesiosaurian vertebra undoubtedly cervical, in which no trace of it was visible. The neurapophyses are commonly unanchylosed with the vertebral centres in any part of the spine, and in some instances throughout the cervical, and at the anterior part of the dorsal region, the neurapophyses have appeared to be joined each by an articular surface to the spine above, as they are to the centrum below,—the spines here remaining, apparently throughout life, unanchylosed to the neurapophyses. This condition of the upper ver- tebral elements is rarely seen in any cold-blooded vertebrate, and never in the warm-blooded classes. In those parts of the spine, where the vertebra enjoyed less mobility upon each other than in the neck, the spines become anchylosed to the neurapo- physes at an earlier period. The hemapophyses co-exist with the ribs or paravertebral elements, in the caudal region of the spine, but they continue throughout life to be unattached by bone, either to the centrum above or to each other below; and here also their spine is not developed, and consequently no true chevron-bone is formed in the Plestosauri, 'The hemapophyses are also continued along the infe- rior surface of a great part of the abdomen, forming there the sternal or ab- dominal ribs ; and just as the neurapophyses are developed in the transverse direction to protect the expanded cerebral masses in the cranial region, so here the hamapophyses are in like manner elongated transversely, and their spine is introduced and modified to form a third mesial rib-like bar, con- necting, however, as usual, the lower or distal extremities of the haemapo- physes, and completing the osseous cincture of the abdominal viscera. The tail in the Plescosauri is relatively much shorter than in the Ichthyo- saurt, and I have not observed in any example, that partial dislocation which seems to indicate that it supported a fin in the Ichthyosaurt. There is an obvious reason for the shortness and simplicity of this part of the animal; in the Plesiosauri, thelength and mobility of the neck renders a special apparatus in the tail for producing the lateral movements of the head unnecessary. Structure of the Plesiosaurus Macrocephalus. 523 Such is the general character of the spinal column as regards the compo- sition of the vertebra in the genus Plestosaurus ; and consequently so far the Plesiosaurus Macrocephalus agrees with the better known species : it also presents the same generic peculiarities in the form of the articular sur- faces of the bodies of the vertebra as are described by Mr. Conybeare in the Pl. Dolichodevrus. I now proceed to describe the specific characters distinguishable in Lord Cole’s Plesiosaurus Macrocephalus. Cervical vertebrae. (Pl. XLIV.) The cervical region of the spine in this species exhibits the prominent character of the genus in its great extension. It is, however, only twice the length of the lower jaw, instead of three times the length of the same part, as in the Plesiosaurus Hankinsii; and this difference, arising from the greater development of the head in the Macrocephalus, is associated, Dr. Buckland observes*, with a thicker and stronger character of vertebra in relation to the greater weight they had to sustain. It includes 29 cervical vertebre. In the 20th cervical vertebra of Plesiosaurus Hawkinsii the transverse is to the antero-posterior diameter as 4 to 3. Inthe corresponding vertebra of the Plesiosaurus Macrocephalus the trans- verse is to the antero-posterior diameter very nearly as 2 to 1. The rest of the cervical vertebrae bear a similar ratio to those of the Plestosaurus Hawkinsii; the bodies of the vertebrz therefore in Plesiosaurus Macrocephalus, although by no means so flat as in the [chthyosauri, make an evident approach to the characteristic form of the vertebre in that genus. Mr. Conybeare has justly remarked how difficult it is to determine the number of the cervical vertebre in a Plesiosaur, owing to the gradual transition in their lateral appendages from the con- dition of hatchet-shaped laminz to the ordinary elongated form of ribs. For the purpose of gaining a point of comparison of the different species of Plesiosauri, I would suggest that the vertebra in which the costal articular surface has first entirely left the centrum and passed upon the neurapophysis should be reckoned as the first dorsal. According to this criterion, the number of cervical vertebre in the Plesiosaurus Hamwkinsii will amount to 31, while those of Plesiosaurus Macrocephalus are 29. In the Plesiosaurus Hawkinsii, the hatchet-shaped processes are converted into styliform ribs at the 29th cervical vertebra ; but in the Plescosaurus Macrocephalus they undergo this change of form at the 27th cervical vertebra, and perhaps at the 25th, but this appendage is lost in the skeleton under consideration. Hence we may conclude that the Pl. Macrocephalus has two vertebre less in the cervical re- gion than the Plesiosaurus Hawkinsii, and probably six cervical vertebra less than the Pl. Doli- chodeirus, in which Mr. Conybeare states that ‘“ the thirty-five anterior vertebre exhibit these (hatchet) processes distinctly characterized, and are therefore beyond all doubt cervical t.” The articular surfaces for the ribs on the anterior cervical vertebrze of the Macrocephalus are rela- tively larger and have a more regular lozenge shape than in the Plesiosawrus Hawkinsiu, in which they are elongated in the axis of the vertebra. They are traversed (as mentioned in the general characters of the Plesiosaurian vertebrz) by a longitudinal groove ; this gradually sinks from the middle of the depression towards its lower margin, and at length, at the 23rd cervical vertebra, disappears. * Bridgewater Treatise, ii. p. 30. + Geological Transactions, i. (Second Series) p. 384. VOL. V.—SECOND SERIES. 3 Y lem On ey Ee i oe ee > ee re cle ee bee eer tars 524 Ricuarp Owen, Esq., on the The depressions above the costal surfaces for the lodgement of the bases of the neurapophyses resemble in form those of the Plesiosaurus Hawkinsii, but extend further down upon the side of the centrum. They are coextensive with the antero-posterior diameter of the vertebral body, and are bounded by two lines meeting below, at a right angle. The angle formed by the corresponding lines in the Plesiosaurus Hankinsii is more open. The distance between these neurapophyseal pits and the costal pits in the anterior cervical vertebrz, differs in different species of Plesiosaurus. In the Macrocephalus the interspace is very short, never exceeding half the diameter of the costal pit, even in the most anterior of the cervical vertebre*. In the Plesiosaurus Hawkinsii the in- terspace is equal to double the diameter of the costal pit in the corresponding vertebre. There may also be observed in the Macrocephalus an evident tendency in the surface supporting the cervical vertebrz to rise above the level of the centrum: and this is the more interesting, as in a large species of a yet uncharacterized Plesiosaurus nearly allied to Macrocephalus, (and of which a figure of one of the posterior cervical vertebre is subjoined) the surface on the centrum and the corresponding surface of the neurapophysis do project, as short transverse processes ; and thus approximate to the Crocodilian type. As the seventh, eighth, and ninth vertebree happen to be displaced in the present specimen, and their neurapophyses to be dislocated, the form and depth of the articular depressions for the neurapophyses, as well as the canal for the spinal marrow, are thus brought into view. The cen- trum presents only a plane surface for the spinal chord, the rest of the canal being completed by the neurapophyses laterally, and the expanded base of the spine above. The surface in ques- tion is bounded by two lateral curved lines, having their convexities turned towards each other. Immediately below, and external to this surface on each side, are the deep and roughened pits for the attachment of the neurapophyses. The cervical neurapophyses do not, in any of the Plestosaurs, unite immediately together above the spinal chord and canal, so as to form a continuous bony arch, spanning across that part, but they stand upright from their sockets in the vertebral body, parallel with each other, or only slightly converging at their superior extremities. They terminate above, in young individuals at least, in broad rough articular surfaces parallel with the transverse axis of the vertebra, but sloping down from behind forwards with a slight sigmoid flexure at an angle of 25° with the longitudinal axis of the vertebra. In the same way, therefore, as the rib or appendage to the transverse processes is bifurcate at its proximal extremity, in those cases where the two transverse processes are separately developed on each side of the vertebra, and where the rib is joined to both; so here the spinal appendage of the neurapophyses is bifureate at its proximal extremity, and each fork rests upon the above described oblique articular process of its own side. We have here an analogy between the lateral or costal and the superior appendages of the ver- tebral centre which the Plestosaurus alone has hitherto afforded. But besides the two surfaces developed for these articulations with the neurapophysis, each fork of the spine sends off an articular or oblique process from its anterior and posterior extre- mity; the articular surface looking obliquely upwards and inwards on the anterior process, and downwards and backwards on the posterior process: and thus the spines are locked together throughout the whole vertebral column with the exception of the terminal vertebre of the tail. * T have not as yet seen any Plesiosaurian cervical vertebrz that resemble those of the Pl. Macrocephalus in this character, which is the more applicable and valuable from being presented by the body of the vertebra alone. Structure of the Plesiosaurus Macrocephatus. 525 In adult individuals of the Plesiosaurus Macrocephalus, these separate elements of the supe- rior arch become anchylosed together, as is the case in a great part of the spine in the present specimen. In a Plesiosaurian cervical vertebra, however, measuring seven inches and a half in vertical extent, and three inches and a half in transverse diameter, in the collection of Mr. Hawkins, I find the neurapophyses distinct both from the spine above and the centrum below. But in other cervical vertebre ofa still larger Plesiosaur in the collection of Lord Cole, not only is the spine anchylosed with the neurapophyses, but these are also confluent with the centrum. In the dorsal region in the Plestosaurus Macrocephalus, as in the Pl. Hawkinsii and Pl. Doli- chodeirus, the neurapophyses and spines become anchylosed; but the former elements continue separate from the body of the vertebra throughout the vertebral column in the Macrocephalus. The cervical spines in the P/. Macrocephalus differ in form from those of Plesiosaurus Han- kinsii, in retaining their breadth or antero-posterior extent throughout the neck; their extremi- ties being, as it were, truncate, with the angles slightly rounded off. The powerful ridge of bone which they thus collectively form, is highly characteristic of this species. The consequence of this structure is a diminution of the spinal interspaces necessary for the vertical inflections of the neck; which interspaces are conspicuously present in the Plesiosaurus Hawkinsii, where the end of each cervical spine is, as it were, obliquely cut off at the anterior part, so as to allow the neck to be bent upwards much more extensively than could have been possible in the Macrocephalus*. What, however, the latter species thus lost in mobility, it gained in strength, the quality mainly required in relation to the movements of its more bulky head and jaws. As the powerful neck of the Pl. Macrocephalus, however, possessed extensive mobility in the lateral direction, as is indicated by its position in the fossil, the muscles destined for these move- ments must necessarily have been developed in a corresponding degree ; and we find that adequate provision was made for their fixed points of action, in the superior development of the costal pro- cesses, as compared with those of Pl. Hamkinsii :—these processes present, indeed, throughout a greater part of the neck the characteristic expansion of their distal extremities, which led to their being called hatchet-shaped bones by Mr. Conybeare: but the stem which supports the dilated extremity is proportionally longer in the Macrocephalus ; and it is only towards the base of the neck that the extremities overlap each other, as in the Crocodile. Dr. Buckland has illustrated this peculiarity by placing side by side the figures of the hatchet bones in the Pl. Hamkinsi and Pl. Macrocephalus. These cervical ribs assume the true costal form, as before stated, at the 27th vertebra, where they are short and straight ; behind this part they progressively increase in length, and become bent towards the sternal region. The cervical vertebre gradually increase in all their dimensions, (least so, however, in their antero-posterior extent), as they approach the trunk; but the difference in their size at the two extremities of the neck is less than in the Plesiosaurus Dolichodewrus. Dorsal Vertebre. These are characterised, agreeably with the previous definition, by the absence of articular sur- faces for the ribs at the sides of the centrum, and by the development of a superior transverse process (exclusively supporting the rib) from the base of each neurapophysis. * In the large posterior cervical vertebra of the Plesiosaurus in Mr. Hawkins’s collection, the extremities of the spines are expanded ; and the anterior obliquely-truncated surface is flattened. 3y 2 Se ee eS ee —— etme Rao rte Sara es a me Ce ae: 526 Ricuarp Owen, Esq., on the The number of vertebrz in the present species so characterised is 20: that of the correspond- ing vertebre in the Plesiosaurus Hankinsii, is 25. The vertebrz thus defined include, besides the ordinary dorsal, those which occupy the situa- tion corresponding to the lumbar or ribless vertebrz in the crocodile ; but there are no vertebrae of the trunk wanting ribs in the genus Plesiosawrus, in which structure it approximates the La- certine Saurians. The special characteristic of the dorsal vertebrz of Pl. Macrocephalus, as compared with Pl. Hamkinsii, consists in their being (like the cervical) more flattened in the antero-posterior direc- tion, and more concave at the sides ; in which latter particular they resemble the dorsal vertebre of the Pl. Dolichodeirus more than those of the Pl. Hamkinsii. At the commencement of the dorsal series of vertebra in the present fossil, the bodies of the vertebrz have been subject to a partial dislocation, and begin, as it were, to slide away from the neurapophyses, until the dislocation becomes complete at the sixteenth vertebra: and the articular depressions for the neurapophyses, and the canal for the spinal chord, are again brought into view. In the succeeding vertebrz the bodies gradually get into place again. Here the lower margins of the neurapophyses begin to lose their angular form, and become rounded off, the articular de- pressions presenting a corresponding figure. The transverse processes progressively increase in length towards the middle of the trunk, and again diminish as they approach the tail : the bases of the neurapophyses from which they rise diminish in vertical extent in the same ratio, and leave a greater proportion of the centrum free from their embrace. The increasing length and upward inclination of the transverse processes supporting the ribs, Mr. Conybeare has justly observed, “‘ seem intended to give a wider sweep to the ribs,” and relates to the acquisition of greater ex- pansion of the thoracic-abdominal cavity, where the largest viscera were lodged. The spinous processes at the beginning of the dorsal region diminish in antero-posterior extent, but slightly increase in height: they then increase in both directions to the middle of the back, and afterwards gradually decrease to the tail. Sacral Vertebre. There are no sacral vertebre by anchylosis in the Plestosauri. In the present specimen, the dislocated state of the pelvic bones and corresponding region of the spine, renders it difficult to determine against which of the costal processes of the vertebra the extremities of the iliac bones may have abutted. In a specimen of the trunk of a Plestosaurus Hawkinsii in the British Mu- seum*, the two sacral vertebre are distinguishable by the sudden increase in the breadth of their costal processes, as compared with those immediately pre- ceding and succeeding them. The short sacral ribs in the crocodile present this character in a still greater degree, (as might be expected from its terrestrial habits); but we may per- ceive in the Plesiosaur an evident additional affinity to the Emydo-Saurians, as compared with the Ichthyosaur. The sacral vertebra of the Plesiosaurus Hawkinsw also differ from the lumbar and dorsal vertebra preceding them by * See Plate XXV., Hawkins’s Memoir on Ichthyosauri, &c. Structure of the Plesiosaurus Macrocephalus. 527 a small part of the costal articular surfaces being contributed by the centrum ; these surfaces beginning to sink down again upon the bodies of the vertebra, where the increased breadth of the ribs indicates that they gave attachment to the pelvic arch. Guided by this character in reference to the Pl. Macrocephalus, I find that the costal articular surface begins to descend upon the vertebral body at the fiftieth vertebra (counting from the atlas), and consequently reckon this and the succeeding vertebre as sacral; and their relative position to the dislocated ilium verifies the supposition that the same character, with reference to the costal articular surface, points out the bodies of the sacral vertebre in the Pl. Macrocephalus, as it does those of the Pl. Hawkinsii. It is at this part of the vertebral column, in Lord Cole’s specimen, that the separation of the verte- bral elements from each other, and the displacement of the bodies, again bring into view the surface which supported the spinal marrow, and the articular depressions for the neurapophyses on each side. The surface which supported the spinal marrow is small and flattened, slightly impressed, bounded by two gently-curved lines, whose convexities are turned towards each other. A comparison of the medullary canal at this part and at the cervical region, shows that the usual law of the increase of the spinal chord at the parts where large nerves were required to be given off to supply the locomotive extremities obtained in the extinct Enaliosaurians, as in their existing congeners, The spinous processes are locked together by double oblique articulating surfaces, as described in the cervical vertebre. Of the Tail. Of the tail, there remain in the present specimen the bodies of eight vertebree, with a few of the caudal ribs and hemapophyses. From their position, and the decreasing size of the vertebrae, we may safely judge that the tail had the usual proportions observable in other species of Plesiosaurus. Each of these centres presents on its upper surface the continuation of the spinal canal, bounded by two lateral curved lines, with their convexities turned towards each other; and on each side of the canal a roughened subtriquetral surface for the attachment of the base of the neurapophyses. Below this, on each side of the body, there is a rounded pit for the articulation of the caudal rib. These differ from the costal pits in the cervical vertebra, in not being traversed by a groove. The inferior surface of the centrum presents a slightly concave, transversely oval surface, with- out any longitudinal ridge ; and on each side of the anterior and posterior margins there is a half- articular surface, designed to form, in apposition with the adjoining vertebree, a point of attach- ment for the hamapophyses. The length of that which appears to be the eighth caudal vertebra, is, to its transverse diameter, as 2 to 5. In the Pl. Hawkinsii, I find that the rib has left the neurapopbysis, and slid down wholly upon the centrum at the sixty-first vertebra. In a very perfect tail of a Plesiosaur in Mr. Hawkins’s collection, the hama- pophyses are developed beneath the twenty-eight terminal caudal vertebre, the two or three last small ones only excepted. The bodies of these small terminal caudal vertebre also present an interesting modification of the sur- faces by which they are attached to one another, and if found detached, would en i ea ae eS ee a a Ee nn ee 9g Sn? re ee ea — 528 Ricuarp Owen, Esq., on the hardly be recognised as belonging to the genus Plesiosaurus: they are hol- lowed out like the vertebra of the Ichthyosauri, so as to join by double con- cave surfaces, (as shown in the figure (Pl. XLIV., fig. 6.) of the joints be- tween the twenty-seventh, twenty-eighth, twenty-ninth, and thirtieth caudal vertebre of the skeleton of the Plestosaurus Hawkins in the British Museum). It is interesting to perceive that those vertebra which are most remote from the centre and source of vital energy, present throughout life a lower and earlier type of structure ; such as, from the analogy of the Batrachia, we may assume to have been the feetal condition of all the other vertebre. It is equally interesting to perceive the designed arrest of development at a part of the spine where the elasticity and flexibility retained by that arrest are required for its peculiar functions*. In conformity with the usual course of anatomical descriptions, we have next to consider the bony hoops which encompass the visceral or thoracic- abdominal cavity, and which consist of two parts, called the vertebral and sternal ribs, although these are, in fact, respectively analogous to the costal processes and hemapophyses in the caudal region of the spine, and ought strictly to have been considered as parts of the dorsal vertebre. The verte- bral ribs are evidently but prolonged developments of the osseous appendages of the transverse processes of the vertebrae, which we have already seen to exist in the cervical, sacral, and caudal regions of the spine. They begin from the thirtieth cervical vertebra rapidly to increase in length and strength to near the middle of the abdomen, and then more gradually diminish, and * The caudal hemapophyses have been hitherto described as chevron bones in the Plesiosaurus ; but in all the specimens and casts which I have examined, they have presented the condition of two appendages distinct from one another. In the Pl. Dolichodeirus at the British Museum, the tail rests upon its inferior surface, and the broken spines and costal appendages are alone brought into view. In the cast of the Duke of Buckingham’s specimen, in the Museum of the Geological Society, the only parts resembling chevron bones are the detached neurapophyses, or superior arches. In Plate XXV. of Pl. Hankinsii, in Hawkins’s Memoir, the small chevron-shaped bone below the fourteenth caudal vertebra, does not belong, as might at first sight be supposed, to the under surface of that vertebra, but is the superior arch of the small, displaced vertebra behind it. The true condition of the hemapophyses in the Plesiosaurus is beautifully shown at the sixteenth caudal vertebra of the Pl. Hawkinsi in the British Museum.—(See Plate XXIV. of Hawkins’s Memoir.) The hemapophyses are longer and slenderer than the costal processes ; they slightly taper to their distal extremities, which approach each other by a gentle curve, and were doubtless connected together in the recent state by a cartilaginous or ligamentous substance. In the newly- born whale, the heemapophyses present the same condition, which, however, is a transitory one in this warm-blooded marine animal, in which ossification proceeds to blend the heemapophyses into a single chevron. Structure of the Plesiosaurus Macrocephalus. 529 assume the character of detached transverse processes as they approach the tail. In general form and size, the ribs of Pl. Macrocephalus resemble those of Pl. Hankinsii ; but they seem (in comparison with Hawkins’s fig. 25) to be more suddenly expanded at their upper extremities ; and the anterior ribs here present a bilobed appearance. The articular surface at the proximal or vertebral extremity of the longest ribs (which are about nine in number) is oblong, convex, and roughened for the attachment of cartilage. Counting from the costal appendages, which change the hatchet-shape for the true rib-like form, to the sacral vertebra, there are twenty-two pairs of dorsal and lumbar ribs in the Pl. Macro- cephalus. The sternal ribs, or abdominal hemapophyses, in the present fossil, are partially brought into view on the left side of the abdomen: they seem to be relatively slenderer than in the Pl. Han- kinsii, and are consequently more like those of the Pl. Dolichodevrus ; as in both these species they are connected by an intervening mesial, transverse, sternal bone, of a rib-like form, but pointed at both extremities. This is the representative of the hamapophyseal spine, which is here, in re- lation to the expansion of the abdominal cavity, developed in breadth or transversely, instead of longitudinally or vertically, as in the tail of fishes. Pectoral Extremity. Of the bones composing the sterno-clavicular arch, we easily recognise the broad, expanded coracoid, of which the humeral or articular extremity is seen projecting on the left side of the fossil. This extremity is relatively broader than in the Pl. Hawkinsi, being adapted to a broader joint at the corresponding extremity of the humerus. The notch above the articulation, which receives the humeral end of the clavicle, is shallower than in the Pl. Hawkinsii. The rest of the apparatus is too imperfect to allow of an accurate comparison being carried further. In the bones of the paddle, or radiated appendage of the pectoral arch, the following differences exist between the Pl. Macrocephalus and Pl. Hawkinsu. The humerus is (as has been just observed) less contracted at its proximal extremity: it is altogether less curved backwards, the anterior margin being concave instead of. straight or con- vex, as in Pl. Hawkins. The distal end terminates in a slight but regular convex curve; while in the P/. Hawkinsi the separate facets for the radius and ulna are distinctly marked, and meet so as almost to form an obtuse angle. In the Plesiosaurs generally the radius is nearly straight, while the ulna is bent, with the con- cavity towards the radius; both bones are flattened, as in the other Enaliosaurians. In Pl. Ma- erocephalus the margin of the radius next the ulna is more concave than in Pl. Hamwkinsit, and the bone is relatively broader at its distal extremity, which is terminated by a convex instead of a nearly straight line. The ulna equals in length the radius, as in the Pl. Dolichodeirus, while it never attains the same length in the Pl. Hawkinsii. It is, in the Macrocephalus, relatively broader than in either the Pl. Dolichodeirus or Hawkinsii. It also presents a more complete reniform figure ; the humeral articular surface not being so straight, or so distinctly marked off from the outer convex margin. 530 | Ricuarp Owen, Esq., on the The carpus consists, in Pl. Macrocephalus, of eight, instead of, as in Pl. Hankinsii, six ossicles. The fourth, or additional one in the first or proximal row, is wedged in between the ulna and the third carpal bone, at the outer angle of the carpal joint ; it is much smaller than the rest. The relative sizes, also, of the three normal bones of the first row is different. In the Pl. Hamkinsti the middle one is the largest; the radial, or anterior one, the least. In the Pl. Macro- cephalus the ulnar, or posterior of the three, the largest. The disproportionate size of the two posterior bones in the Pl. Hamkinsit compensates for the shortness of the ulna. In the distal row of the carpus the superadded bone in the Pl. Macro- cephalus is a very small ossicle wedged in between the third or posterior carpal, and the fifth or ulnar metacarpal bones. The metacarpal bones correspond with those of the Pl. Hawkinsii; the radial or anterior one which represents the pollex being the shortest and broadest. Pl. Macroceph. Pl. Hawks. The first metacarpal supports.... 2 (but probably 3) phalanges.. 3 The second metacarpal. ........ Gi wiohkie emis cvcccescecccce Gord. The third ditto ...... se ceeeee 9 csveeee aha cen ctelatbha, sae oTa\s\« 8 or 9. The fourth ditto ..... odie leln'c'n wis | OM skye o aimieleleis aes aie eeicieie tetera The fifth ditto ...-..-+eee. Pe deo ek eae) The evidently natural curve formed by the distal phalanges in Lord Cole’s Pl. Macrocephalus indicates that the paddles had a greater flexibility of this tapering extremity than those of the Cetacea possess. Pelvic Extremity. Of the bones composing the pelvic arch, the outer convex margins of the two pubic bones, small portions of the two ischia, and the femoral extremity of the left ilium are visible. They show that the general form and relative proportions of these bones correspond with those of the better known species of Plesiosaurus. There is, however, an evident difference in the proportion of the length of the pubis to that of the vertebral column. We have enough of the pubis to ascertain that its length somewhat ex- ceeded the length of four of the lumbar vertebre ; while in Pl. Hawkinsii, the length, or antero- posterior diameter of the pubis is only equal to three and a half of the lumbar vertebrz: and this difference evidently does not altogether depend on a smaller antero-posterior diameter of the ver- tebre in the P/. Macrocephalus, but in a greater development of the pubis, which is in relation to the greater size of the hinder paddle in this species. The femur in the Plestosaurus Macrocephalus is relatively longer than in Pl. Hamwkinsii. In the latter it equals the humerus in length ; in the former it exceeds the same bone by one-eighth of its own length. In the Pl. Macrocephalus it is rather more expanded at the distal extremity than in the Pl. Hankinsii; but the difference of form is not so well marked as in the humeri of these two species. * In the enumeration of the Phalangeal bones by Mr. Conybeare (Geological Transactions, i. p- 387.) the metacarpals are included ; the perfect digits of the Pl. Dolichodeirus correspond in number with Pl. Hawkinsii and Pl. Macrocephalus. Structure of the Plesiosaurus Macrocephalus. 531 The bones of the leg have the same distinguishing character as those of the fore-arm, and ihe fibula in all the Plesiosaurs corresponds to the ulna in its peculiar bent figure. In the Pl. Macrocephalus the fibula is, however, relatively broader than in the Pl. Hankinsii, notwithstanding that, like the ulna in the fore-arm its distal extremity is on the same plane with that of the adjoining bone: it is, in fact, fully as broad as it is long, which proportions, com- bined with the characters of the cervical vertebra, distinguish it from the fibula of any other species of Plesiosaurus which I have yet seen. The tarsus consists, in P/. Macrocephalus, of six instead of five bones, as in the Pl. Haw- Kinsit ; it participates in the peculiarity of having three bones which are situated at the anterior, or tibial side of the joint, much smaller than are those of the fibular side, and so placed, in the intervening space between the tibia and tibial metatarsals as to indicate that the foot had a freer inflection forwards, or upon the tibia, than in the opposite direction. This structure, Dr. Buckland has observed to me, would give a compound motion to the pro- pelling stroke of the paddle, similar to that which in skilful rowing is called feathering the oar. In the Pl. Hawkinsii the interspace between the tibia and metatarsals is occupied by a single round and flat bone ; in the Pt. Macrocephalus by two; the additional bone being situated at this part of the tarsus. The metatarsals resemble, in number and disposition, those of the Pl. Hawkinsii, as is shown in the following table : Pl. Macroceph. Pl. Hawks. The first, or tibia] metatarsal supports.... 3 PhAalangesys: Sneatieriren ee 38 MMNERSECOMG ep stateleterevereicleus crotcrelerelereton sores Dy slab suehchoiiere sia) stele etaraletereerets 5 Mle tHird tiles «ores Diei'aldiaislieis: ofeeler eis ate ShGp'9)) Ok. came 8 (Pheftounths more thant. eevee cle siecle eolere c (POD CORO CM One ee ave feneyiors 8 Mbestitthwer-teqsteieisvelers scoododoonododar Shei Obve/pelete cia. clara larelstaraievave etal 6 In general form and proportions of the phalanges of both extremities, a close resemblance subsists between the two species. Of the Head. (Pl. XLV.) I have reserved for the conclusion of the present paper the description of this, the most complicated and difficult part of the skeleton. The relative size of the skull to the body and cervical portion of the spine in the Plesiosau- rus Macrocephalus has already been stated ; but its structure and composition still remain to be spoken of. From its position in the specimen, the composi- tion of the upper and lateral parts only can be examined, but the bones on these surfaces are well defined, and in tolerably perfect condition. The general form of the head is depressed and triangular as in the other Plesiosaurs ; but the breadth of the base of the triangle formed by the posterior part of the head is relatively greater than in the Pl. Hawkinsii. The elongated form of the strong and prominent cranial bones, most of which are seen extending from point to point, with wide interspaces, like the timbers of a scaffolding, indicates the affinity of the Plesiosaur to the Lacer- tine Saurians, and this affinity will be further exemplified in the condition of many of the individual bones. VOL. V.—SECOND SERIES. 3Z 532 Ricwarp Owen, Esq., on the The only parts of the occipital bone visible in the present head are the superior extremity of the supra-occipital, where it is joined to the posterior point of the bifurcation of the parietal, and the point of the right lateral or exoccipital, where it abuts against the suture between the transverse process or fork of the parietal and the tympanic bone. The force which has crushed the head has fractured the parietal just at its point of bifurcation, and the strong transverse forks are separated from each other and from the median or ordinary part of the parietal from which they were continued ; these fractures are also accompanied with a slight disloca- tion of the respective parts. The natural form of the parietal bone in the Plesiosaurus is, however, well displayed in the head figured by Mr. Cony- beare, in the 2nd vol. of the 2nd Series of the Society’s Transactions, (PI. XIX. fig. 2.); and the oblique sigmoid suture uniting the extremity of the parietal process to the tympanic bone is also indicated in that figure at about half an inch from the point of bifurcation. In the Pl. Macrocephalus the transverse processes of the parietal are relatively stouter and longer than in the Plesiosaur there figured, or in the Pl. Hawkinsii. That on the right side in the present specimen forms the most prominent part of the bones of the head. The normal portion of the parietal bone, anterior to the bifurcation, presents a distinct division into two lateral moieties by a sagittal suture. The sides of this suture, or rather harmonia, for it is not denticu- lated, are deep, being formed by the apposition of two ridges of bone which rise and meet to form the longitudinal intermuscular crest which traverses the middle line of the upper surface of the head in this, as in other species of Plesiosaur. Two inches anterior to the bifurcation of the parietal the fora- men which characterizes the parietal in many Lacertine Sauria is plainly indi- cated by the moiety of its circumference which is due to the left parietal ridge, which alone is here preserved. The long diameter of this vascular foramen is three lines. The coronal suture seems here to divide the parietals from the frontals im- mediately anterior to the above foramen, which thus belongs entirely to the parietals, as in the genera Monitor, Lacerta proper, and others ; while in the Ichthyosaurus the corresponding foramen is placed directly upon the coronal suture, as in the genera Iguana and Stellio. The parietals slope away immediately from the median ridge, indicating the extent of the strong temporal muscles which were only separated on the top of the head by the thickness of this ridge. Jn this structure we find the Piesiosaurus resembling the lacertine [guana among existing Saurians, and differing from the Crocodiles and Gavials, which have the tempoial muscles Structure of the Plesiosaurus Macrocephalus. 533 separated by a flattened interspace of the parietal bone. The Plesiosaurs present a still more marked affinity with the Squammate Saurians, and devia- tion from the Loricate tribe, in the posterior bifurcation and median foramen of the os parietale. The general condition of the present fossil indicates it to belong to a young individual, and to this circumstance may be attributed the non-consolidation of the two parietals into a single median bone, as is its condition in all other Saurians. The median frontals extend forward as faras the midspace between the small nostrils, and appear in the Pl. Macrocephalus to terminate in a point between the commencement of the narrow nasal bones. The interfrontal suture is elevated by a ridge continued forwards from that of the interparietal. The outer margin of the median frontal forms the superior boundary of the orbit. The anterior frontal enters into the formation of the anterior and superior angle of the orbit, and is wedged in between the mid-frontal and superior maxillary bones. The posterior frontal, which is here narrower than in the Pl. Hawkinsi, resembles the columnar portion of the corresponding bone in the Crocodile, which bounds the orbit posteriorly and extends downwards to join the malar bone; but this bone is more superficially situated in the Plesiosaurs, which thus resemble more the Lacertine Saurians.. The affinity of the Plesiosaurs to this group and their recedence from the Crocodilian type is more strikingly evinced in the non-extension of the posterior frontal to join the mastoid, and the consequent absence of the osseous ridge which traverses longitudinally the temporal fossa like a second zygoma, and pecu- liarly characterizes the cranium of the Loricated Saurians. The zygomatic portion of the temporal also resembles the Lacertine and deviates from the Crocodilian type in its elongated form and horizontal longi- tudinal position. The inner surface of this bone is seen on the left side of the head, while only that part which joins the malar and posterior frontal remains on the right side in the present specimen. The tympanic bone, in its general form and especially its length, is intermediate to the Crocodilian and Lacer- tine types; while in regard to its strength it exceeds that of all existing Sau- rians. The expanded inferior termination of this important bone, which gives the surface of articulation to the lower jaw, appears in the present specimen to be formed by a distinct osseous piece or epiphysis, but the difficulty of dis- criminating between suture and fracture in a crushed fossil leaves me in some uncertainty regarding this point: I may observe, however, that a supplement- ary bone, but of much smaller size, occupies a corresponding situation in the cranium of the Monitor. 3Z2 534 Ricuarp Owen, Esq., on the From what can be discerned of the structure of the posterior part of the skull in the present specimen, and from the appearance of the lias-matrix which has intruded beneath the tympanic arch, on the right side, into the temporal fossz, there is sufficient evidence that, in the Pl. Macrocephalus, a large opening on each side of the occipital region of the cranium leads be- neath the parieto-tympanic arches into the temporal fossa. This conforma- tion differs from that which is expressed in the posterior view of the restored head of the Plesiosaur, given by Mr. Hawkins in the 23rd Plate of his Me- moir; but repeated and close examination of the skull, both of Lord Cole’s specimen and of the Pl. Hawkinsivi, prove that the Plesiosaurus participated in the Lacertine type of cranial structure and deviated from the Crocodilian *, in the presence of the openings above described. When we come to consider the facial and maxillary bones, the correspond- ence with the Lacertine Sauria begins to diminish, and that with the Croco- diles to increase. This tendency to the higher type of Saurian organization is shown in the strength of the whole maxillary apparatus, in the great rela- tive size of the intermaxillaries, the roughened exterior surface, and the distinct alveolar cavities for the teeth. But the nostrils, in their size and po- sition, combine with the structure of the paddles to indicate the affinity of the extinct Enaliosaurs to the existing Cetaceans, and offer a beautiful example of the adaptation of structure to the peculiar exigencies of a species. The apertures through which the air is respired are placed, in the Pl. Ma- crocephalus, exactly where Mr. Conybeare has described them to be situated in the Dolichodeirus, and where they are placed in the Pl. Hawkinsii, viz. a little anterior to the orbits, near the highest part of the head. In the pre- sent specimen it would seem that the intermaxillaries formed no part of the boundary of the nasal apertures, while in the Crocodiles almost their en- tire circumference is due to these bones. The nostrils in the Plesiosaur are formed by an interspace at the convergence of the anterior frontal, nasal, and superior maxillary bones. In the Lacertine Saurians, a small proportion at least of the boundaries of the anterior nostrils is always formed by the inter- maxillaries, and these orifices are separated by a bony longitudinal partition, as in the Plesiosaur. The intermaxillary suture extends from the anterior part of the nostril forwards to a little more than half-way between the orbit and anterior extremity of the cranium. One of the strongest of the inferior teeth rises just in front of this suture, anda slight notch at that part seems to * This communication is reduced to a very small opening in the Crocodiles in consequence of the form and position of the os tympanicum. Structure of the Plesiosaurus Macrocephalus. 535 correspond with that tooth, and offers a resemblance to a very characteristic structure in the true Crocodiles. The lachrymal bone forms a great pro- portion of the anterior and inferior part of the orbit: the superior maxillary appears to form a small part of the orbital circumference below the lachrymal, and the malar bone rests by an oblique suture upon its posterior extremity ; the posterior margin of the malar is joined to the posterior frontal, thus com- pleting the posterior osseous boundary of the orbit, and to the zygomatic, or temporal bone. The concave articular surface of the lower jaw is well displayed in Lord Cole’s specimen, indicating free and frequent motion of that bone ; the poste- rior process of the angle of the jaw closely resembles that of the Crocodile. The suture between the angular and supra-angular or coronoid process is well displayed, showing the same complicated structure of the lower jaw which Messrs. Conybeare and De la Beche have so admirably illustrated in the allied genus Ichthyosaurus. The coronoid processes, however, rise higher, and form a sharper edge for the insertion of the temporal muscles than in the Crocodiles ; and we have another important indication of affinity to the La- certine, at the expense of departure from the Crocodilian type, in the absence of the vacuity between the angular and supra-angular pieces, which vacuity peculiarly characterizes the Crocodiles. The correspondence in the position of the head in the present specimen with that of one of Mr. Hawkins’s beautiful specimens of the species which I have dedicated to him, and which he has obligingly permitted me to deli- neate (PI. XLV.), enables me to state that, in the Pl. Macrocephalus, the maxillary portion of the cranium is relatively larger, as compared with the cranial portion, than in the Pl. Hawkinsii; that the orbit is nearer the back part of the cranium, and the temporal fossa consequently shorter ; and that the tympanic arches, upon which play the branches of the lower jaw, are relatively much stronger. In all these points, as also in the relative size of the head to the trunk, and in the shorter but stronger neck, we perceive the most admirable illustrations of the laws of organic co-existence ; and at the same time are enabled to trace a closer affinity, in the present species, than in any other hitherto described, to the Crocodilian and Ichthyosaurian types of structure. ve , y i ‘OP ie Oe au | % bokis 9 aiaith ai” Rane wee ilk rel . ; ‘ail fi . i ; ae) a ‘i we” uae ie ’ ' Ky ' vi hie er ere Hib: we ‘f fat Ris. a han ma ‘ea 7 ec . fi” nit A 6 a sp Me vine : ae “ i A ¢ aii ; ‘ pi st 4 iis wis 4 oe he i ai it io rh 4 ay i) } J v 3 cae if nr a ma XXXVIII.—On the Fossils of the Eastern Portion of the Great Basaltic District of India. By JOHN G. MALCOLMSON, Ese., F.G.S. [Read November 15 and December 6, 1837. ] Illustrations, Plates XLVI. to XLVIIL. CONTENTS. Introduction.—Objects of the Memoir, p. 537. General Sketch of the Physical Features, Hy- drography and Geology of the Basaltic and Granitic Districts, p. 538, et seq. The valley of the Nerbudda, p. 538; Go- davery, p. 539; Kistnah, p. 539; Pennar, p. 540. Granite platform between the Kistnah and Go- davery, p. 544. Tron ore, mines, and manufacture of the steel, p. 546. Country between the Sichel Hills and Nagpoor, p: 553, et seq. Origin of Minerals in Trap Rocks, p. 559. Description of the Lonar Lake and analysis of the water, p. 562. Age of the diamond sandstone and argillaceous limestone, p. 568. Inferences respecting the Freshwater Fossils, p- 569. Other districts in India in which similar Fresh- water Shells have been found, p. 570. Description of the Sichel Hills, p. 548, et seq. Relative age of the Laterite and Trap, p. 573. and of the Freshwater Shells, p. 550. INTRODUCTION. THE principal objects of the following paper are, to submit to the Society an account of a series of fossils discovered in the eastern part of the great basaltic district of India ; and to endeavour to arrive at some approximate con- clusion respecting the geological era of this basaltic formation, which, extend- ing over more than 200,000 square miles, conceals, breaks up, or alters all the other rocks from beneath which it has forced its way. Of the eruptions to which this rich and romantic country (formerly including several considerable kingdoms) owes its existing form, a late President of this Society remarks*, that the mind is almost lost in the contemplation “of their grandeur ;” but “that unfortunately the relative age of the eruptions must remain for the present undetermined, no vestiges of secondary or tertiary formations having been de- tected within the region.” Having therefore, in 1832, collected a series of lacustrine fossils, probably referable to the tertiary epoch, from a portion of * See Mr. Murchison’s Anniversary Address, Geological Proceedings, vol. i. p. 454. pie: oS — — eras ert res i Pe ees o= eS 538 J. G. Matcoumson, Esq., on the Fossils of this district extending 140 miles north and south, and having procured others from localities to the north and west of that which furnished my own collection, I am induced to submit the specimens to the Society*. If they should be deemed of sufficient value, I wish a selection to be deposited in the museum, to afford a means of comparison with a duplicate set, which I shall forward to the Asiatic Society of Bengal f. But it is not alone by supplying some data from which to infer the relative age of the great trap formation, that these specimens are valuable. They will afford the means of connecting the great sandstone formations of the south and north of India, containing the celebrated diamond mines of Parteal (Gol- condah,) Bangnapilly, and Panna, as well as the limestones and schists asso- ciated with them ; and which, from the latitude of Madras to the banks of the Ganges, exhibit the same characters, and are broken up or elevated by granite or trap rocks. in no respect differing in mineralogical characters or geological relations. A few remarks on these formations, and the physical geography of the countries in which they occur, will be a necessary intro- duction to a more particular account of that portion of the trap district in which the fossils were found, Mr. Calder’s sketch not being sufficiently de- tailed, and the map attached to his memoir containing some errors of material importance f. GENERAL SKETCH OF THE Puysicat Features, Hyprocrapny, &c. An elevated tract to the north-west of Bundlecund (not included within the range of the Map, PI. XLVI.) may be considered as the geological connexion between the provinces watered by the southern branches of the Ganges and the Deckan, including ail the countries to the south of the Nerbudda. From the north of this plateau, which extends far to the west, a number of great rivers descend, by a series of rapids and falls over sandstone escarpments, into the valley of the Jumna and the Ganges. From the east and south of the same tract, the Mahanuddy river collects a great body of water, and after a compara- tively short course through countvies little known, but containing the diamond mines of Sumblepoor and extensive trap and gneiss formations, empties itself into the Bay of Bengal, not far south of the Delta of the Ganges. The Nerbudda, which flows in an opposite direction, is more interesting in a political and geological point of view; and the extensive countries through which it passes have been more carefully investigated than any other part of the * See Plate XLVII., drawn, engraved, anddescribed by Mr. James de Carl Sowerby. + The series of specimens presented by Mr. Malcclmson to the Geological Society ave been arranged in the foreign department of the museum. t Asiatic Researches, vol. xviii. ~~ the Eastern Portion of the Basallic District of India. 539 Peninsula. This river takes its rise to the west of Amerkantack, and traversing a country of granite, sandstone, and basalt, abounding in iron and the finest dolomitic marbles, reaches the Indian Ocean through the alluvial plains of Guzerat. At Jabulpoor and in the neighbourhood of Saugur, fossil mammalia, shells, and silicified palms have been recently discovered. Fossil shells have also been found in some of the trap hills, which have broken up the sandstone near the sources of the T'aptee. This river is separated from the Nerbudda by a range of basaltic mountains ; and having the same direction as the Ner- budda, its whole course appears to be in the basaltic formation. (See N.W. corner of Map, Pl. XLVI.) All the other great rivers of the Peninsula, including the Godavery, Kistnah, Pennar, and Cauvary issue from the western Ghats, from the summits of which the country slopes gradually to the east, except at the extreme south, where the descent to the plains of the Carnatic is considerable and precipitous. The Godavery (see Map, PI. XLVI.) rises in the basaltic region described by Colonel Sykes, (Geol. Trans. Vol. IV. pt. 2, 1836) and, greatly increased in size, it enters the granitic table land of the Deckan, and flows at the south- ern foot of the Sichel Mountains into a sandstone and argillaceous limestone country. This district is similar to that of Bundlecund and Malwa; it also contains diamonds, and has been much broken up by erupted rocks. From the north, the Godavery derives large supplies of water from the great rivers rising south of the Nerbudda and the Taptee, in basaltic tracts, the soil of which being retentive of moisture, the water is everywhere near the sur- face. From the south it receives only the Munjerah river, which, flowing through arid granitic plains, furnishes but a scanty addition of water, except during the rainy season. Through a pass in the gneiss mountain of Papcon- duh it enters the plains of the Coromandel coast. In this district the sand- stone reappears, at an elevation little above that of the sea ; but basaltic hills, several hundred feet in height, in which marine fossils have recently been discovered, exist almost within the delta formed by its sediment. The Kistnah derives its waters from a number of considerable rivers, rising in the basaltic and gneiss summits of the western Ghats, which condense the greater part of the clouds carried by the south-west monsoon from the Indian Ocean. Flowing through the territories of the southern Mahrattas, a country covered with a rich basaltic soil, and abounding in schistose limestone, sandstone, granitic rocks, and basalt, it enters the granitic platform of the Deckan, the limits of which in this direction are unknown. The limestones and sandstones, however, soon reappear on descending the river, and extend across to the basin of the Pennar, and as far as the ascent to the granitic plat- VOL. V.—SECOND SERIES. AA 540 J. G. Matcotmson, Esq., on the Fossils of form of the Mysore. It is on the banks of the Kistnah that the richest dia- mond mines occur, and that the sandstones acquire their greatest elevation, amounting to more than 3000 feet ; the river passing through mural preci- pices of this rock and of the schistose limestones to be presently described. It then enters the plains of the Carnatic, where the same rocks occur, some- times a little elevated above the level of the sea, at others forming the caps of granite mountains, or broken up by varieties of greenstone and basalt. Thence, passing through a narrow gorge in the gneiss hills of Bezwarrah, it enters the alluvial plains continuous with the delta of the Godavery. Its waters, how- ever, are more loaded with mud than the last-mentioned beautiful river, and the deposit of new land may be seen, by the inspection of a common map, to be proportionably great. The Pennar is comparatively a small stream, but of much geological inter- est, the greater part of its waters being derived from the districts in which the diamond sandstones and the argillaceous limestones, on which they rest, are exhibited in their most characteristic forms, and where they are most easily investigated. 'T’o describe these strata in detail would be out of place here ; but a few of the leading facts must be stated, that the identity of the forma- tions with those of the fossiliferous district, more immediately the object of this paper, may be rendered manifest. Like all the rivers of Southern India, granite is frequently seen in the bed of the Pennar, more especially in its southern branches, where the passes of Ryachottee lead to the granitic table land of Mysore, having an elevation of 3000 feet above the sea, or 2500 above Cuddapah, the principal town of the Pennar basin. With these exceptions, and the occasional appearance of trap through the stratified rocks, the rest of its course, till it approaches the sea, is over rich plains of black and saline alluvium, derived from the decomposition of basalt and of the stratified rocks so often referred to. From these plains numerous table lands, insulated emi- nences, and ranges of hills, having for the most part a direction nearly N.E. and S.W., rise abruptly, presenting mural precipices of difficult access, around the base of which the roads often make extensive circuits. The Nulla Mulla hills extending from the Mysore frontier to the basins of the Kistnah and Godavery, and the minor ranges dependent on them, and having the same composition and direction, are crossed at right angles by the Pennar, which makes its way through them, like the Kistnah, by traversing narrow gorges with perpendicular sides. There is not a more remarkable phenomenon in the district watered by the Pennar than the horizontal summits of many of the ranges, and the distinct manner in which the continuity of the strata can be traced from one hill to the Eastern Portion of the Basaltic District of India. - dA another, although extensive plains intervene ; while, at no great distance, the sandstone which forms the summits of these hills is seen on the same level as the surrounding plains. Numerous instances also occur in which the original continuity of the horizontal summits is easily traced ; the strata on the opposite and nearly perpendicular sides of a valley being similar, but having a considerable dip, the beds descend to the general level of the country. A good example of this is seen, in Section 2, Pl. XLVI., at Chintagoouta and Gun- dicottah. These anomalies were at first quite inexplicable, nothing appearing in the valleys but a rich alluvium, nor on the summits (which are reached with much difficulty) but a sandstone perfectly horizontal, and divided into huge tables by perpendicular partings, sometimes separated several feet from each other, and filled with broken pieces of the rock. This jointed structure is common to the sandstone, the schistose beds on which it for the most part immediately reposes, and the stratified limestone into which these schists pass insensibly ; but the size of the tables so formed, varies from rhombs of a few inches, in the schist and lower part of the sandstone, to enormous masses on the summits of the hills. Nowhere is this structure and the succession of strata, of which it is characteristic, better seen than in the table land in which are si- tuated the celebrated diamond mines of Bangnapilly and others now deserted. The accompanying wood-cut will give some idea of one of these mines. Table Land of Bangnapilly. Schistose Beds passing into Limestone. ~ Diamond Mines in Alluvium. The plains at the base of the table land of Bangnapilly consist ofa rich black alluvium, containing fragments of basalt, jasper, and the various minerals found in the hills. It rests on a fine, compact, dark blue or nearly black limestone, which contains much argillaceous and siliceous matter. This limestone Aa2 542 J.G. Matcoumson, Esq., on the Fossils of abounds with springs, and is in some places so cavernous as to afford passage to subterranean streams. Basalt protrudes in a few places near Bangnapilly. On ascending the hill, the limestone becomes more schistose, and is of a paler colour, gradually approaching in its structure and composition to clay slate, but it is far more friable. On the schist a more or less compact sandstone rests, varying very much in colour, composition, and appearance in different places. Above Bangnapilly it contains the diamond breccia described by Voysey. As far as the shafts which I had an opportunity of observing, enabled me to judge, the breccia is not an interstratified rock, but an intermixture of the common sandstone, in different parts of the same stratum, with larger fragments of older rocks, generally rounded but sometimes angular. It is not, however, the object of this paper to describe the mines and the interesting district in which they occur further than is necessary to exhibit the type of the forma- tion, by the study of which I was enabled to understand more clearly, the less distinct appearances exhibited by the same rocks, where they have been inya- ded or buried by the great basaltic eruptions of Central India. On the oppo- site or west side of the valley, the hill is composed of the same argillo-calca- reous formation ; but, according to Colonel Cullen, “ instead of a sandstone cap, it is crested in its whole Jength with a sharp black ridge of trap rock, formed of loose blocks piled upon each other, the apparent base of which observed a pretty uniform level, nor is the ridge of much depth. Its extreme narrow- ness, deep black colour, and the total absence of all traces of vegetation, formed a singular contrast to the rest of the hills, which were covered with long dry grass and scattered bushes*.” Ata small pass some miles further to the west, the road in ascending, passes over first the dark limestone and a nar- row belt of schist, then trap, which is again succeeded by limestone, and the latter by schist, nearly to the summit, “‘ which is capped with a rock of a beau- tiful flesh colour, with specks and shades of a beautiful green, as if connected with its vicinity to the trap, and of so close and fine a texture as to appear homogeneous even with a lens.”’ “The descent of the pass on the opposite side consists of a clay slate nearly to the foot, where the limestone reappears, and these two rocks continued to alternate with each other to the foot of the second Ghat, which, like all the former, was composed of clay slate capped with quartzose sandstone f.”’ The sandstone exhibits many varieties of grain, colour, and hardness: in some places it is white or red, and can be cut into pillars and slabs of great size and beauty ; in others it is soft and fri- * Colonel Cullen, in Transactions of the Literary Society of Madras, January 1837, p.50. + Ibid. the Eastern Portion of the Basaltie District of India. 543 able, and its inferior beds are not unfrequently schistose, so as to be with difficulty distinguished from the subjacent rock, with which it has in one or two places been observed to alternate. Where the sandstone approaches the great granitic tracts to the south and west, it passes into a compact quartzose rock, as is seen on both sides of the Tripatty Valley. This passage is also observed in other places, as near the Cuddapah diamond mines, where the plentiful occurrence of basaltic peb- bles shows the neighbourhood of the trap. Besides the diamond conglomerate, consisting of a great variety of minerals, seams of rock crystal occur, and a fine white quartz containing argenti- ferous galena, which in former times furnished the country with lead. Specular and micaceous magnetic iron ores, but’containing much peroxide, and common iron pyrites, occur with the galena, As far as I have observed, the sandstone always rests conformably on the schists, although from its jointed structure it occasionally, when elevated, appears to meet the subjacent rock at a more or less obtuse angle. The schists on which the sandstone rests, vary very remarkably in colour, being in different places blue, red, green, or pure white, in which they seem to bear some relation to the incumbent sandstone. They are also occasionally flinty or jaspideous. Sometimes they are wanting, the sandstone resting directly on the limestone, of which the schists are evidently merely the upper beds, and into which they pass insensibly, although it seldom happens that considerable efferves- cence does not occur on examination by tests. It is in many places impossible to say to which portion of the series any particular specimen belongs. Voysey has classed the schists with the sandstone under the name of “(the clay slate formation ;)” I have, however, preferred to designate the deposit “ argillaceous limestone,” aterm used by him in one of his sections as applicable to the limestone, and which well expresses not only the general character of the rock, but that also of the upper schistose beds. The limestone is a compact rock, but the strata are usually thin, and are often intersected by vertical partings, a circumstance which frequently limits its use in ornamental architecture. Its most common colour is a light blue, passing into black ; but it occasionally occurs of anearly pure white, and affords an admirable material for basso-relievos. On this stone the finest sculptures of the ruined city of Amrawuty are executed, and for delicacy of workmanship they have perhaps never been surpassed. Were it not for the occurrence of small crystals of quartz, the same quarries would furnish an excellent lithographic stone. Near Cuddapah the dark variety is the common building stone, and many fine columns, caryatides, and cisterns are composed of it. The stone is applied to the same objects in the southern Mahratta country, and along the course of the Go- davery towards Nagpoor. To the south and east of Cuddapah, a narrow valley, nearly 150 miles in length, extends through the limestone, the strata of which are in some places nearly vertical, but form rounded hills. In others they are capped by sand- stone, which exhibits mural precipices of much grandeur, and almost or en- tirely inaccessible. The strata, for the most part, dip to the N.W., resting on the granite of the Carnatic. This rock is penetrated by many dikes of greenstone, which have evidently been instrumental in elevating the stratified rocks to their present singular positions. Little has yet been ascertained re- garding the thickness of these strata, which differ much even in the same range of hills. The only minerals they have been ascertained to yield, are varieties of quartz and iron pyrites, the latter of which is so abundant in a few 544 J. G. Matcoimson, Esq., on the Fossils of localities, that sulphur is manufactured from it. At Jumulmudagoo I found the limestone interstratified with muriate of soda ; and it is therefore probable, that the salt diffused through the alluvial soil so extensively as to render the water of the Pennar brackish during the hot season, and the inhabitants independent of the sea-coast for a supply of that article, is derived from this source. On emerging from the gorge in the Nulla Mulla range, the Pennar enters the plains of the Carnatic, and near its mouth flows through low hills of late- rite. This deposit rests on the ordinary granite of the Carnatic, with its as- sociated sienites, hornblende schist, quartz rock, and mica slate. It is in a rock composed of a mixture of the last two minerals, that the copper-mines of the Nellore district are situated*._ In the same neighbourhood, the sandstone and argillaceous limestones are little elevated above the sea, and are con- tinuous with the same rocks on each side of the Kistnah. They are broken through by insulated basaltic hills, in the neighbourhood of which subterra- nean sounds and frequent local earthquakes are reported to occur ; an asser- tion I am the more inclined to believe, having myself experienced two slight shocks during a casual visit to the district. Having briefly described some of the more remarkable phenomena exhibited by the southern portion of the great sandstone and argillaceous limestone formations, it will be unnecessary to enter into any detail when we meet with the same rocks to the north of the Godavery in connexicn with the fossil beds discovered in the great basaltic district. GRANITE PLATFORM BETWEEN THE KisTNAH AND GODAVERY. (See Map and Section I.) With regard to the granitic platform of the Deckan, which intervenes be- tween the Kistnah and Godavery, much accurate information is already before the public ; it will therefore be necessary only to observe, that it is intersected by numerous greenstone dikes (sometimes of greenstone porphyry), having for the greater part a direction from 8. by E. to N. by W., and not very dif- ferent from that of several of the ranges of basaltic mountains to the north. These dikes, and the detached masses connected with them, are entirely composed of a crystal- liné compound of hornblende and felspar, without distinct crystals of augite; and I have never * The ores are of various kinds, but the richest is a sulphuret, containing, according to Mr. Prinsep, 69 per cent. of the pure metal. The copper also occurs in a slate which Mr. Oucter- lony, of the Madras Engineers, informs me, was considered in Cornwall to be identical with the Killas. If this slate belongs to the ‘ argillaceous limestone” formation, the fact will be of use in determining the relations of that rock to the gneiss, talc slate, and mica schist ; a subject on which no observations of any value have yet been made. The primary rocks of this district contain magnetic iron ore and corundum, both of which occur in the diamond sandstone. the Eastern Portion of the Basaltic District of India. 545 detected olivine in them*. The rock shows a tendency to separate into spheres composed of concentric layers and into irregular prisms ; and the same structure in some degree occurs in the granite, sy- enite, pegmatite, &c. of the whole of the south of India. The greenstone is exceedingly hard and difficult to work, but it takes a most beautiful and durable polish, as in the magnificent mausoleums of Golcondah, the tombs of Hyder Ali and Tippoo Sultan, at Seringapatam, and in many of the sculptures of the Carnatic pagodas}. Where these dikes rise into hills, the summits only are composed of the compact greenstone, which graduates below into the granite of the surrounding country. Many of the veins of basalt in the passes of the Mysore and Neilgherry mountains differ from these, in possessing the structure of the compact basalt’ of Bombay and other places in the trap countries, and in branching into narrow veins, (often not an inch thick,) which traverse the granite without mixing with it; while the ordinary greenstone dikes of the Deckan are almost always accompanied by separate nodules, of greater or less dimensions, insulated in the granitic mass, the component parts of which appeared to me to be there, in most cases, arranged in larger crystals, and to be more subject to decay, than in other places. I could not resist the inference, that, at the time of the formation of these dikes, the granite was in a state approaching to fluidity; although, as some of the narrow veins can be traced for many miles through the granite, they do not appear to have been formed at the same time. Several small basaltic hills are insulated in the granitic platform in the line of route between Hyderabad and Nirmul, and they are based on decaying gra- nite. Their flat summits and steep sides correspond with the hills of the great trap district ; and the general line of bearing, of the broken ranges of which they appear to form a part, does not differ much from that of the basaltic mountains to the north, or from the greenstone dikes ; but many hills are scat- tered over the plains to the east and west, and cross this line of route in every direction. ‘The lower part of the hills is composed of thin tables or lamine of a sonorous trap, and the upper of globular concentric basalt ; the external lay- ers of which are extremely friable, generally grayish, or soft and soapy to the feel, and are of a greenish tint, except where the stone is much loaded with ferruginous grains of a reddish brown colour. In some places the metallic matter has the appearance of having been partially smelted, and is of a fine red hue. The nuclei of the “ concentric basalt,” which are exceedingly tough, and resist decomposition powerfully, are of a deep black colour, and contain large crystals of olivine, and small kernels of calcedony. The first of these minerals is not found in the soft external coats, yet it is so closely united with the substance of the rock as not to admit of a doubt of its being of contempo- raneous formation, and not, as supposed by Berzeliust, a fragment of a pre-existing stone enve- loped in the liquid matter. Small, but very characteristic specimens of calcedony are of more frequent occurrence in the softer portions of the rock, especially between the concentric nodules ; but they are intimately mixed with their substance. It is remarkable, that I detected no calcareous minerals in similar situations in these hills, although the rock is so impregnated with lime as to * See note to page 575. + It is familiarly known in India as “ black granite.” { Edinburgh Journal of Science, January 1839. 546 J.G. Matcotmson, Esq., on the Fossils of have led to an extensive deposit of calc-tuff (Kunkur), at present forming along its base, and pro- jecting sometimes half a foot from between the partings of the basaltic tables —“ The presence of olivine, the soft wacké in which the globular basalt is imbedded, the less crystalline structure, the passage into a porous amygdaloid, containing calcedonies, zeolites, &c., and the granite in the neighbourhood of all the smaller masses differing little from that at a distance,” may perhaps be sufficient to distinguish these insulated basaltic hills from the greenstone *. On approaching the Godavery, the granite in some degree changes its ap- pearance, containing large and beautiful crystals of red felspar, occasionally imbedded in veins of transparent quartz, clouded with spots and wavy lines of a turbid milky colour. Greenstone dikes are there more common. The river flows over granite, which is intersected by several dikes of greenstone, run- ning more in a north and south direction than those above referred to, and ha- ving many minute white crystals diffused through their substance. The dikes project from 8 to 10 feet above the granite, and are divided into rhomboidal masses by fissures, in which lime is deposited. The bed of the river is co- vered by numerous fragments of calcedonies, zeolites, and other minerals found in volcanic rocks ; and they have been cemented into a more or less solid calca- reous conglomerate. ‘The banks are composed of a black basaltic soil, from the lower part of which, where it rests on the granite, as well as from the divi- sions between the several layers of alluvium, thin slabs of a clayey calc-tuff (Kunkur) project, and are connected above with portions formed round the roots of plants, and below with other layers spread out between the different strata of alluvial earth+. These appearances sufficiently indicate the neigh- bourhood of the basaltic range of mountains, distinguished in Arrowsmith’s large map as the Sichel or Shesha hills, but which are locally known by the name of the Nirmul range, from the large town situated six miles from the difficult pass leading up the steep escarpment presented by their southern face. None of the stratified primary rocks are seen at the foot of these hills in the line of the section ; but twenty miles to the east of Nirmul, and a few miles south of the mountains, hornblende slate occurs, resting on granite and quartz rock. Iron Ore, Mines, and Manufacture of the Steel.—The magnetic iron ore, employed for ages in the manufacture of the Damask steel used by the Persians for sword-blades, is obtained from this schist. The mines I examined, are those of Deemdoortee, but the ore is extensively dis- tributed. The minute grains or scales of iron are diffused in a sandstone-looking gneiss or mica- ceous schist, passing by insensible degrees into hornblende slate, and sometimes containing amor- * Journal of the Asiatic Society of Bengal, February 1836, p. 105. + Further details on this part of the route will be found in some notes explanatory of a collec- tion of specimens presented to the Asiatic Society of Bengal, and published in the Journal of that Institution for February, 1836. the Eastern Portion of the Basaltic District of India. 547 phous masses of quartz. The strata are much broken up and elevated, so that the dip and direc- tion are in no two places the same, and bear no relation to the mountains to the north. Manufacture, §c.—The mines are mere holes dug through the thin granitic soil, and the ore is de- tached without difficulty by small iron crow-bars. It is then collected and broken on projecting masses of granite or quartz by means of a conical-shaped fragment of compact greenstone; but when too hard to yield to this simple instrument, it is previously roasted. The sand thus pro- cured is washed in shelving depressions dug near a tank, and the heavier parts, separated by this process, are exactly similar to Voysey’s specimens of the iron-sand used in the manufacture of Damascus steel at Kona-Sumoondrum, in the same neighbourhood ; but from his published papers, it does not appear that he had seen the rock from which they were derived. In other respects, all the information I could procure, accurately corresponds with that given in his interesting paper*. The ore is then smelted with charcoal in small furnaces, which have often been described, I did not see any flux used; but, although I watched the whole process, from the digging of the ore till it was formed into bars, I will not assert that none was employed. The iron has the remarkable property of being obtained at once in a perfectly tough and malleable state, requiring none of the complicated processes to which English iron must be subjected, previous to its being brought into that state. Mr. Wilkinson, who has investigated the history of Indian steels with much scientific and practical skill, did me the favour to submit to experiment a specimen of this iron as it came from the furnace. He found it to be extremely good and tough, and considered it superior to any English iron, and even to the best descriptions of Swedish. The Persian merchants, who frequent the iron-furnaces of Kona-Sumoondrum, are aware of the superiority of this iron, and informed Dr. Voysey, that in Persia they had in vain endeavoured to imitate the steel formed from it; a failure which could be ascribed only to the difference of the materials used, as the whole process of the conversion into steel was conducted under their own superintendence. It is also probable, that there are few places in India where an ore of equal value is so easily procured ; otherwise its distant inland situation, in a difficult and unsettled country, would not have retained a reputation for so many ages. In the manufacture of the best steel three-fifths of this iron is used ; the other two-fifths being obtained from the Indoor district, where the ore appears to be a peroxide. It is evident, that if the beautiful water of the Damascus blades is derived from the crystallization of the steel, the use of two very different varieties of iron, one of which has been ascertained to be of such admirable quality, must have an important influence on the appearance and quality of the manufacture. As these mines afford a boundless supply of ore easily wrought, and are situated in the neigh- bourhood of vast forests, and near a river navigable for boats during part of the year, it is pro- bable, that at no distant period, when the native government has undergone some amelioration, iron may become an important article of commerce. On this account, and because, although much has been written regarding Indian steel, nothing has yet been brought prominently forward regarding the finer kinds of iron ore with which that country abounds, I will make a few additional obser- vations regarding them. Dr. Heyne has accurately described the manufacture of iron in the Carnatic, to the south of the Pennar river, and he states that it is, when first smelted, extremely brittle, requiring several operations to bring it into a malleable state. I possess specimens of two varieties of ore usedin the district in which he observed the processes, and where I have myself seen them carried on. The one, an iron sand, collected in the beds of rivers, consists of the protoxide, mixed with much of the peroxide ; the other, a red schist, is almost entirely composed of red oxide, but in the centre * Journal of the Asiatic Society of Bengal, vol. i., p. 245. VOL. V.—SECOND SERIES. AB 548 J.G. Matcoumson, Esq., on the Fossils of of the mass it affects the magnet. Not far from where this rock occurs, I collected specimens of hornblende schist, leaving little doubt as to the ores being of the same nature, the former having become altered in situ, in the same manner as some of the superficial strata at Deemdoortee are seen todo. I therefore conclude, that the superior quality of the Nirmul iron depends on the ore being a comparatively pure protoxide. It certainly is not dependent on the nature of the fuel, which is much the same in both places*. Captain Herbert, indeed, long ago suggested, that the superiority of the Gwalior iron over that principally worked in the Himalayahs, depended on the former being a magnetic ore, like that of Sweden; but the first accurate information on the sub- ject was communicated by Dr. Royle to Mr. De La Beche, who states t, on the authority of that gentleman, that magnetic iron ore is extensively diffused in hornblende slate in the central range of mountains in India, and that it also occurs in the Himalayahs. This geological position corre- sponds with that of the Nirmul ore; but the latter does not bear any resemblance, except in its peculiar lustre, to the Menaccanite of Cornwall, to which it is compared by Mr. De La Beche; nor could I detect any titanium in it. With regard to the geological relations of the magnetic iron ore, it is also necessary to observe, that in India it is not confined to the hornblende schist, but is found extensively distributed in the granite and gneiss of the Carnatic and Mysore, in quartz rock near the iron works of Porto Novo; and, as has already been observed, associated with galena in the diamond sandstone of Cuddapah. The discovery of a mineral, so generally confined to the primary rocks, in the great sandstone formation, affords an additional argument in favour of the opinion of those, who consider this rock and the subjacent schists, as equivalents to the older European sedimentary formations, rather than to those of the supermedial order. DEscRIPTION OF THE SICHEL HILLs, AND OF THE FRESHWATER SHELLS. Returning to the line of route, the granite, on approaching to the Sichel hills, hecomes softer and decomposes rapidly ; and the soil gradually changes to the well-known black basaltic mould, known in India by the name of “ cot- ton ground,” and, as usual, it is mixed with calcedonies, zeolites, &. Amongst these minerals were some fragments of a red colour, and considerable specific gravity, though full of irregular cavities, and so like the slag of an iron fur- nace, that I considered them to have had that origin, till I discovered a consi- derable mass of a similar nature protruding from the granite and black soil by which it was covered. Along with these fragments were others of a semivitri- fied matter, containing small white crystals of felspar, and hardly to be distin- guished from a piece of granite fused by Dr. Voysey in the steel furnaces of the neighbouring district. ‘The granite constitutes the surface rock a little further, gradually passing into a black compact basalt, intermixed with many white spots, apparently of felspar. The trap then becomes softer, forming small hills of a cellular amygdaloid, abounding in cavities lined with green * Tron, which has been ascertained to be superior, for many purposes, to the best German iron, has been recently imported from the western coast of India; but the mines from which it was ob- tained have not been examined. Captain Jervis, of the Bombay Engineers, however, informs me, that ores, powerfully affecting the magnet, exist in great quantity at Taygoor, a village of the Koncan, not far from the port from which the iron in question was procured. + Manual of Geology, 3rd Edit., p. 435. the Eastern Portion of the Basaltic District of India. 549 earth, and many of them filled with calcedonies, zeolites, quartz crystals, and, more rarely, calcareous spar, of the same kind as those, so remarkable for their beauty, in the portion of this formation described by Colonel Sykes (Geo- logical Transactions, vol. 4., p.422*). The crystals also occur in seams, or are diffused through the trap ; and in both cases are intimately mixed with its sub- stance. Inthe bed ofa torrent between two of these hillocks, I met with some soft, clayey, schistose fragments, and others of a siliceous character, and of a black bituminous appearance in the centre, containing very perfect specimens of the Paludina Deccanensis (P|. XLVI1I. fig. 20,) and fragments of other shells to be hereafter described. Those which I examined were converted into calce- dony. A laborious research on the hill failed to discover them 2m széz ; but about half-way up the escarpment of the principal mountain, which is very steep, and composed of concentric nodular basalt, imbedded in a soft greenish wacké, a narrow band of a singular quartz rock projected about two feet from the sur- face. It was remarkably scabrous, of various shades of white and red, and had cavities on its surface covered with fine silky crystals. It had every ap- pearance of having been forced into its present situation, when the basalt co- vered and partially melted the bed to which it belonged. Many fragments of this rock were found below with the shells ; and it was again met with, to- gether with the same and other fossils imbedded in basalt, near Hutnoor. The specific gravity of this rock is 2-473, and some of the specimens effervesced feebly in acids, a portion of lime being dissolved ; circumstances in which it corresponds with a similar formation found by Voysey, associated with shells, probably of the same kind, at Medcondah (south of the Godavery), an insulated basaltic hill resting on granite, to which I shall have occasion again to refer. The highest summit of the hills, above the locality of the fossils, is conical, but it is capped by a perfectly horizontal stratified rock, the nature of which I could not determine. It is most probably tabular basalt, although that rock is seldom found in similar situations. Such are the appearances presented on ascending the difficult pass leading up the steep escarpment of the Sichel hills, which form the southern boundary of the eastern portion of the great trap formation of Central India. The hills extend from the junction of the Wurdah and Godavery rivers (the basins of which they separate), till they are lost in the gradual rise of the country to the * A beautiful variety of chabasie, having the angles replaced by triangular or pentagonal faces supporting a rhomboidal surface, of which beautiful specimens abound in certain localities of the western portion of the formation, has not been met with in this neighbourhood; but, like some other minerals of the basaltic district, it is not generally diffused in the rocks where it is most abundant; so that I have travelled for several hundred miles without meeting with it. AB2 oe eee ra SE ee ee SI ER a at aS ee ———— Og Gea 8 ee i 550 J.G. Matcormson, Esq., on the Fossils of west, near Lonar (lat. 20°, long.76°, 30’), in the province of Aurungabad. Their direction is W.N.W., and, as far as can at present be inferred, they seem to be continuous to the east with numerous ranges of basaltic, sandstone, and gra- nitic hills, extending to the Eastern Ghats, at the lower parts of the course of the Godavery. The extreme breadth of the range, from the foot of the Nir- mul pass to the town of Yedlabad, (nearly on a level with the plain country of Berar,) is about 40 miles ; but several smaller hills having for the greater part the same direction, are intimately connected with them to the north, as far as the Wurdah river, which has an elevation of little more than 600 feet above the sea. The Sichel hills are arranged in terraces, with steep sides having projecting spurs, and their summits rise occasionally into conical elevations with rounded or flat tops. They inclose narrow valleys abounding in streams, or support table-lands covered with black soil strewed with trap boulders, and having water everywhere near the surface. A thick wood and grass jungle, composed of very different plants from those common on the granite hills, cover the whole tract, with the exception of the flat summits and some of the terraces, and render it unhealthy for the greater part of the year. The ba- salt of which they are composed, is generally globular, the spheroids being sometimes of great size ; but in many of the water-courses, even of the elevated table-lands, it has a stratified appearance. Small basaltic columns are also met with on the crests of some of the spurs and higher ridges ; and where they oc- cur, no fossils and few minerals are found. Granite not only forms the base of the hills at Nirmul to the seuth, and Yedlabad to the north, but part of the mountains themselves, the basalt being seen to rest on decomposing gra- nite about the centre of the range, in a deep ravine, through which the Koorm river passes ; it also again appears high in the table-land to the north of that river, and in one of the terraces of the northern descent, where the most extensive fossil beds were found. Further detail is unnecessary, as Dr. Voysey’s admirable description of the Gawilghur mountains, forming the north- ern boundary of the great and fertile valley of Berar, as these hills do its southern limits, applies equally well to both ranges*. The fossils were first discovered in situ, near Munoor, in the basaltic table-land north of the Koorm river; and were subsequently found in the descent of the hills towards Hutnoor, and in dif- ferent parts of the Mucklegnudy pass, leading into the Berar valley. They consist of numerous gyro- gonites ; two species of Cypris ; two, or perhaps three, species of Unio ; and many individuals refer- able to the genera Paludina, Physa, and Limnea. (P]. XLVII.) The rock in which they occur, varies in different places. Some of the finest specimens were procured from a red chert with scabrous * Asiatic Researches, vol. xviii. the Eastern Portion of the Basaitic District of India. 551 surface, having silicified shells distributed throughout its substance, or projecting from its surface. The chert is deeply imbedded in the nodular basalt, from which it projects in some places several feet. The finest specimens of Unio occur in a beautiful gray chert, imbedded in the basalt, or resting immediately on it, the under surface being plain and smooth, while the upper is rough, from por- tions of the large shells which project from it. On breaking up one of these masses, it was found to contain entire Unios, many of them having the valves connected and closed, or partially open ; the interior being filled with the same chert, spotted with fragments of shells, minute univalves, and fine specimens of the two species of Cypris, which occur so abundantly. Some parts of the rock exhibit a mixture of sand, clay, and fragments of shells, of very moderate hardness; but the greater portion consists of chert, the materials of which are occasionally arranged in a beau- tiful, light blue, enamel-like substance, around irregular cavities containing crystals of purple quartz. Some portions also exhibit a minute vesicular structure; and the whole appearance of this beautiful rock forcibly impresses the mind with the conviction, that it owes its present appear- ance to the action of the great basaltic eruption, which has enveloped it and the organic remains. The greater number of the shells are converted into chert, but a few retain their original structure ; and in some instances the calcareous matter has been converted into crystals of calcareous spar. Many internal casts of entire shells are found in the substance of the rock, to which they are united at a few points only, a greater or less space being left unoccupied; in others, the entire shell is converted into siliceous matter, retaining the appearance even of the ligaments unaltered ; and fortunately, in a few cases, the hinge and teeth are excellently preserved. Numerous fragments of shelly rock, differing much in appearance, lay scattered about over the table-land ; consisting partly of a fine blood-red chert, like that above described, and con- taining the same shells. The gray chert was more sparingly distributed, and the Unios did not occur in the other fragments. Some of them, composed of a tough white clayey stone, so soft as to soil the fingers, contained Physze, Paludine, and Limnez, mostly converted into calce- dony, but others also retained their original structure, and effervesced with acids. Portions of charred vegetable matter, resembling small fragments of grasses and reeds, occurred in these and the harder cherts. Other specimens are composed of a greenish blue crystalline mass, resembling an ore of copper, (but it is of low specific gravity, and contains no trace of that metal,) and the shells contained in them are converted into the most beautiful crystalline quartz, retaining the form of every convolution of the Physz and Paludine. The cells of this stone are often coated with fine silky crystals. Masses of a hard coarse chert, consist almost entirely of Gyrogo- nites, but contain many of the same Physe and Paludine. This rock appears to have formed beds of about half a foot in thickness ; but it was not discovered zn situ. A stratified rock was however found in the neighbourhood, resembling some specimens of the argillaceous limestone of the dia- mond districts, but consisting of a compact whitish chert, which contained Paludinz, and the finest specimens of Gyrogonites. (Plate XLVII., fig. 1.) Night prevented the connexions of this rock from being determined: the strata were, however, ascertained to be of considerable extent, and to be much buried in the soil; there were also numerous fragments of siliceous rock, partly converted into a black bituminous flint, or a coarse quartzose rock, partially altered into calce- dony, by which most of the shells were also replaced. The masses of red chert protruding from the basalt contained, besides the Testacea, small por- tions of silicified wood, and what I consider to be the fragment of a bone, and of the tooth of a mammiferous animal. The specimens, however, are too imperfect to admit of any certainty as to what they really are; but it is not unlikely that such remains should occur, and I therefore do not suppress what may lead to a more successful inquiry. 552 J. G. Matcoumson, Esq., on the Fossils of On descending towards Hutnoor, granite, presenting a concentric, ligni- form surface, from the unequal decomposition of the quartz and felspar, oc- curs at a short distance from the fossils*. With this exception, the basalt continues of the same character as before, and fragments of red or deep black chert, containing Paludinz, are found in the beds of torrents ; and at Hutnoor they occur in the trap. There is much calcareous matter mixed with the soil, or collected in nodules, and it appears to be derived from the lime contained in the basalt, or between its laminz. On the pioneers at- tached to our camp penetrating, at Elchoda, through some strata of tabular basalt to obtain water for the troops, seams of a pure white, pulverulent lime were found between the layerst. At Hutnoor fragments of a compact blue limestone, not to be distinguished from that of the diamond districts, were collected ; and the rock to which they belonged, was found in the descent from the first of the three principal terraces by which the road leads to the north- ern base of the hills. The strata were much inclined and broken, but the forest was so thick, that I could not trace them for any distance. After de- scending to the second terrace, the surface rock suddenly changes to a white, horizontally-stratified limestone, almost entirely composed of large bivalve shells, the edges of which decomposing more slowly than the cement, the natives have applied to it a name signifying impressions made in clay by the feet of sheep. The thickness of the bed in one place, where it is intersected by a torrent, is 12 feet, and it rests directly on red granite. A great spur, from the upper part of the mountain, extends across the terrace, rising precipitously above the fossiliferous limestone, a few hundred yards from the spot where it rests on granite; and has buried the continuation of the stratum under an accu- mulation of basaltic débris. Where the limestone becomes concealed in the basalt, a friable, gray, cellular mass, resembling ashes, occurs, apparently im- bedded in both these rocks. The fossils are composed of granular limestone, the matrix consisting of calcareous matter mixed with the ash-like substance, and small fragments of granite. Some of the shells are of great size, but they are ill preserved, and I found only one specimen with the valves united. These shells, I erroneously considered to be marine (principally from the appear- ance of those represented in Plate XLVII., fig. 4 to 8, and some of the large flattened specimens). Mr. Lonsdale, however, who had the kindness to examine some of them, considered their general character to be that of fresh- water species. I had previously detected, in a fragment of a compact argillo- * A similar appearance has been observed at the foot of the Nirmul pass, at the iron mines of Deemdoortee, and in Bundlecund. + The same was observed in Bundlecund by Capt. Franklin. (Asiatic Researches, vol. xviii.) the Eastern Portion of the Basaltic District of India. 253 calcareous stone found at the bottom of the little cliff where the granite is seen to underlie the fossils, a number of very perfect Melanie; I therefore re-examined the different specimens, and detected in them fragments of the same kind as those in the limestone; and Mr. Sowerby has since been able to extract from the latter, specimens sufficiently distinct to be identified with the Unio Deccanensis (Pl. XLVII., fig. 4 to 10,) found in the chert at Munnoor, and another species (Unio? twmida, fig. 11 and 12,) not yet discovered else- where. No other fossils were found in this locality. When it is considered, that the accumulation of freshwater shells occurs on the precipitous descent of a mountain range, ascended with much difficulty by travellers, it will be evident that the aspect of the country has been entirely altered since these animals lived. CouNTRY BETWEEN THE SicHEL Hitts anp NaGpoor. Towards the foot of the pass, the rock changes from the nodular basalt to amygdaloid ; and near its junction with the granite, masses of greenstone porphyry, with large crystals of felspar, occur. The granite then reappears, protruding in rounded masses through the soil of the level country around Yedlabad. The bed of a stream near that town is strewed with fragments of blue limestone and schist, resembling those of the basins of the Pennar and Kistnah ; and higher up the stream, a fine white quartzose sandstone, having a few imbedded fragments of quartz, is found im situ. It dips at a slight angle to the south-west*. The surrounding country is covered by a deep basaltic soil, so that the rock on which it rests could not be discovered ; but the argillaceous limestone, passing, in its upper strata, into a greenish or red schist, is traversed by a stream a few miles to the north. Short ranges of trap hills, some of them at nearly right angles to the Sichel mountains, occur to the north-east ; and beyond them, an extensive tract of sandstone has been traced for a great distance along the Wurdah. At Zynad, argillaceous limestone appears on the surface for several miles, and agrees in every particular with the compact marbles of the diamond dis- tricts of the Pennar and Kistnah. The strata sometimes dip at an angle of 40 degrees, but they are in general nearly horizontal, the edges of the layers being disposed in steps on the slopes of gently-rising grounds. Rock crystal and calcareous spar are distributed in thin seams between the strata, as well as through the substance of the rock ; and along the vertical partings of the strata, there are rows of circular cavities, which are generally empty, but are * Minute undulations, resembling those formed by the ripple of running water, were ovserved on this sandstone, in a seam not quite parallel to the line of stratification. 4 Ce ey ae eS Syn ATE oh, phe =e 4 554 J.G. Matcoimson, Esq., on the Fossils of sometimes filled with calcareous concretions. In a few instances, these hollows occur out of the line of fissure, and entirely penetrate the stratum, being con- nected below with horizontal channels of the same kind. On the surface, calc-tuff (Kunkur) is very abundant, often adhering to the strata, or investing fragments of the rock. The same appearances are seen near the diamond mines of Chinoor on the Pennar, where the strata are much disturbed, and basaltic pebbles cover the banks. The only explanation which can be offered of the phenomena in both those distant localities is, that the extrication of gaseous fluids and water from below, had taken place in the lines of fissure, and had dissolved a portion of the limestone, which was again deposited in the great accumulation of tuff and conglomerate so remarkable in these places. That they at all indicate the “ argillaceous limestone” to be of fresh- water origin, could never be imagined by any who had seen the rock in question, which, wherever it occurs in the south of India, is entirely devoid of fossils*. This supposition is confirmed by the phenomena exhibited at the hot-springs of Urjunah, which rise in the same rock, and where bubbles of carbonic acid are extricated through round holes in the mud covering the bottom of the rivulet, the water of which, being loaded with lime, a calcareous tuff is rapidly deposited. A gentle elevation, extending three miles to the east of the village of Zynad, is composed of this limestone, and it rises very gradually towards a small conical summit, composed of coarse vesicular basalt, which has broken through and covered the limestone. A portion of this rock appears to have been displaced in a singular manner. A wall of perfectly vertical stratification, about 3 feet thick, projects nearly as much from the general surface, and consists inter- nally of the same limestone, as that which it appears to cut at right angles, while externally it is singularly irregular and altered, being converted into a beautifully crystalline limestone, with quartz minerals. To the north of this place, as far as the Payne-Gunga river, the country is flat, covered with basaltic soil or rock connected with insulated trap hills, and inter- mixed with jaspers, resembling those so common near Bangnapilly, and perhaps derived from the argillo-calcareous schists occasionally seen in the water- courses. The pebbles of the Payne-Gunga consist mostly of calcedonies of a reddish colour, and of argillaceous limestone, and they are in many places con- solidated into a conglomerate by the calcareous matter with which all the waters of the district abound. In a layer of this conglomerate, projecting from the alluvial soil of which the bank is composed, numerous recent shells are im- bedded. The limestone, and its incumbent schists, are seen north of the river, and they abound in springs and streams loaded with lime, which is deposited * This assertion may, in the progress of knowledge, be found to be erroneous ; but having care- fully looked for fossils during extensive journeys through districts principally composed of this rock, I doubt whether such will be the case. Fossil plants have been reported to be found near Gundycottah ; but these I ascertained to be mere dentritic markings on the surface of the strata. the Eastern Portion of the Basaltic District of India. 555 as calcareous tuff in the water-courses. Masses of the same substance, several feet in height, project from fissures in the rock, or compose conical eminences of white “ Kunkur,” which are scattered over the black basaltic plains. Proceeding a little further towards the Pindee hills, in which the princi- pal of these streams takes its rise, sandstone appears on the south bank of a ravine; and on the opposite side, at a lower level, the “ argillaceous lime- stone” so often mentioned, has been raised by some violent forces into irre- gular gothic arches, overlaid by partially broken but horizontal strata. The spaces within the arches are filled with fragments of the same rock forced from below. Hot springs, having a temperature of 87°, rise through the lime- stone, and globules of gas escape from round holes in the débris and mud covering the bottom of the ravine. On endeavouring to collect a quantity of the gas, there were found to be considerable and irregular intervals between each jet of air. A recent calcareous sandstone is formed in the bed of the stream, by the débris derived frem the quartzose sandstone of the southern bank being agglutinated by the carbonate of lime of the springs. A range of low hills having rounded summits, with conical elevations pro- jecting from their sides, runs in a north-west direction, three quarters of a mile from the hot springs. The cap of these hills, where the Pindee Ghat passes over them, consists of the argillaceous limestone, and the large slabs of which it is composed, are fissured in various directions, slightly convex up- wards ; and when taken in the mass, they have an anticlinal dip. On the sum- mit, the strata are horizontal and in several places are remarkably altered, the argillaceous and siliceous ingredients having arranged themselves into a black chert, anda mixture of calcareous matter with streaks of a white or pale blue enamel resembling calcedony. ‘The central parts of these bands are com- posed of minute quartz crystals ; and irregular drusy cavities, coated with amethystine quartz, occur in the blackened flinty portions. There cannot be a clearer indication of the action of heat on a rock of a mixed character than this, even when seen in hand specimens. The whole of the base of the hill is composed of the usual black concentric basalt, the nuclei of which are exceedingly hard and contain much olivine ; and to its intrusion the altera- tion of the limestone, with its separation from the strata below, is, without donbt, to be ascribed. Many hills composed of concentric basalt are scattered over the neigh- bouring country, in insulated masses or long ranges rising in terraces. and having flattened summits. The sides of the hills between the terraces are steep, and their outline is well defined ; the rock also is black and devoid of vegetation. The terraces occur at very different levels in different hills, rising VOL. V.—SECOND SERIES. Ac 556 J. G. Matcoumson, Esq., on the Fossils of from the same plain; and their whole appearance indicates that their re- markable form is due to the circumstances which attended their elevation ; and that they have not been subjected to any extensive denudation. About five miles north of the hot springs of Urjunah and four miles south of those of Kair, sandstone caps a gently rising ground, covered with basaltic soil. Near the last-mentioned town, many hot springs rise in the argillaceous limestone, which has been remarkably broken up and altered by the globular basalt protruding through it in different places, in masses several of which are only a few yards in circumference. The limestone is, for the most part, nearly horizonal, but it is occasionally more or less inclined, and, as is usual with this formation, it has no regular direction or line of bearing. In a deep well near the village, the water of which is of the usual temperature, the limestone is unaltered ; but above the principal hot spring, some of the most remarkable effects of igneous action in changing a stratified rock, are ex- hibited. The principal part of the small hill is a whitish limestone, the stra- tification of which is obliterated, and the rock projects in irregular masses full of cavities passing deep into the mass of limestone, which is partly crystalline, and in many places mixed or coated with jasper and quartz cry- stals. Much calcareous tuff (‘‘ Kunkur’’) is associated with these altered rocks, and it fills up many of the cavities ; it is also found in the divisions of the nodular basalt, and masses of it, scattered over the surrounding country, are the only remains of springs which have been long closed up. Some por- tions of the rock had the appearance, on the surface, of a semifused brick, and had assumed something of a regular arrangement, while the centre was composed of the limestone little altered. Large masses of porous scoria also lay about. The principal springs issue at the foot of the rising ground, where the rock is most remarkably altered. Their temperature (87°) was the same as that of Urjunah, on the other side of the Pindee hills, and it did not vary during the hot and cold months of 1831 and 1833. The water of this and many other springs is said to be equally copious at all seasons, covering the neigh- bouring country with the richest vegetation, when all beyond is a black and parched waste. On issuing from the rock, the water is sensibly acid, and in one spring, carbonic gas escapes with the water. It is remarkably agreeable to the taste, and sparkles in the glass, as well as where the stream passes over rapids. It contains a little muriate of soda, a minute quantity of sulphates, and much carbonate of lime in solution, which is deposited on boiling, and in the bed of the rivulet, where it has formed considerable masses of rock chiefly composed of the petrified vege- tation of the banks. So quickly is this deposit formed near some little falls, that shells appear to be imprisoned and entombed while adhering to the face of the rock; and tufts of grass are encrusted with sediment while their roots are still alive. If any doubt remained as to the nature of the nodular limestone, known in India by the name of “ Kunkur,” it would be removed by the sight here exhibited of all gradations of this substance actually forming, and varying from the Eastern Portion of the Basaltic District of India. 557 pulverulent lime to a crystalline rock. The water is probably derived from a great depth, the springs having, as already stated, the same temperature as those of Urjunah, and not being ma- terially diminished by the failure of the annual rains. Sandstone forms the surface rock in different directions over the surround- ing country, but I had an opportunity of examining it carefully only at Won, eight miles north of Kair, its junction with the limestone being concealed by basaltic soil, mixed with calcedonies, fragments of that rock, schist, and of a coarse puddingstone, which I did not find in situ. The hill of Won is composed of sandstone, dipping in all directions from the apex, and vary- ing in colour from white to red and yellow. It contains also ferruginous grains or scales, either in seams or disseminated through its substance. Ina fragment of this kind much resembling the cement of the Bangnapilly diamond breccia, a fossil was discovered having a compact structure and deep black co- lour, and it is probably a portion of a hollow, compressed vegetable, the centre of which is filled with the sandstone. It is the only instance that has come to my knowledge of a fossil being found in the sandstone of southern India; and as the rock corresponds in geological position and mineralogical characters with the diamond sandstone, the fact is of considerable interest, even if the formations were not found to be continuous, as will be stated hereafter. The specimen is deposited in the Museum of the Asiatic Society of Bengal. Sandstone, argillaceous limestone, and schist constitute the building-stones of the surrounding country, which is much buried under basalt, and a black alluvial soil containing calcedonies, jaspers, &c. A few miles south of Chick- nee*, (where the fossils were again met with,) the red schist found above the limestone south of the Urjunah hot-springs and in various places of the dia- mond districts of the south, reappears, intermixed with protruding masses of basalt, which have altered it in the most singular manner,—the lime of which it is in part composed, being converted into a fine crystalline mineral, in which the red clay is enveloped or diffused, giving the rock and even hand specimens a very striking appearance. Near Chicknee, the schist rises slightly towards a basaltic ridge, in which the fossiliferous chert is likewise imbedded. The schist is divided into minute rhombs by vertical partings, in which veins of calcareous spar from an eighth to half an inch thick have been formed, and give it a beautiful, reticulated appearance. Lime is found in the schist, and portions of the red clay are enveloped in the crystalline limestone, which contains no magnesia. The fossils occur on the surface, or are imbedded in nodular basalt over several miles, being * Fossils were first found at Chicknee by Mr. W. Geddes, May, 1829. Ac2 erg Nase oe aacygete et pe eo pods os’ Seer eS Ser 558 J. G. Matcoumson, Esq., on the Fossils of found in blocks of indurated clay, chert, and flinty slate. The appearance of the indurated clay is the same as in some of the specimens from the Sichel Hills, but the clay is harder, full of cavi- ties, and in some cases passes into perfect chert, or has waved lines of quartz or opalized matter diffused through the substance of the mass. Many Physz, Paludinz, and a few Limnee of the same species as those already noticed, are found in this indurated clay or imperfect chert. Some of them are entirely converted into calcedony ; others have the lime replaced by quartz, which is finely crystallized and covers the surface of the convolutions; or the columella only is preserved, passing across an empty cast of the shell. In some cases, however, the structure of the fossil is unaltered, and it effervesces in acids. Flinty slate without organic remains occurs in the neigh- bourhood of those amorphous masses, and many fragments of the same kind containing large com- pressed bivalves are scattered about. In one block of this kind, portions of palm wood mineralized by black flint, intersected by fine veins of a light blue opal, (of the same kind as occurs in some of the specimens of fossil wood from Antigua, lately presented to the Society by Mr. Stokes,) was found associated with compressed very thick bivalve shells, probably referable to the same species as those of Munnoor. Every appearance presented by these rocks indicates the action of the semi- fluid basalt on the beds of mud and sand, probably derived from the neigh- bouring sandstones and schists, in which the shells previously existed. At Hingan-ghat*, a few miles further to the north, considerable fragments of silicified palms and other plants were found in a black chert lying on the basalt, and similar masses, but without fossils, were imbedded in it. I met with no organic remains to the north of this town, the whole country as far as the city of Nagpoor being covered with a rich black soil, from which insulated basaltic hills with flattened summits rise abruptly. Of these hills the most remarkable is that of Seetabuldee, which is based on decomposing gneiss and mica slate. To Dr. Voysey’s description t I have no- thing to add ; but as it has been inferred, that the ‘ flattened summits and long flat outline” of the low ranges connected with this celebrated hill, and forming the eastern part of the great trap district, are composed of basalt * In examining with the microscope sections of some of the silicified wood from the district de- scribed, a specimen from the chert of Hingan-ghat appeared to me to be bone, and Mr. Owen, who has had the kindness to examine it, has ascertained it to belong to a mammiferous animal. He has favoured me with the following note on this important fossil : ‘A section of this fossil was prepared sufficiently thin to allow of its being examined by trans- mitted light under a high magnifying power, when it was found to possess the structure charac- teristic of bone. Sections of ‘ Haversian canals,’ with their concentric lines, were everywhere present, interspersed with numerous Purkingian cells or corpuscles: the size and disposition of these characteristic parts of the osseous structure agreed with those of the bones of the Mam- malia. It was highly satisfactory to find the microscopic test as available in demonstrating the presence of bone, when ordinary characters and the unassisted eye would have left the matter doubtful, as it is in reference to the determination of the teeth.”—July, 1839. + Asiatic Researches, vol. xviii. | ¢ Geological Transactions, Second Series, vol. 4th, p. 410. the Eastern Portion of the Basaltic District of India. 559 having the same stratified appearance as that of other parts of the formation, it is necessary to mention, that they are formed of globular basalt such as has been already described, or of basaltic columns of very regular forms, which diverge from the centre of the hill and incline outwards at an angle of 45° with the horizon, or form a figured pavement on the flat summits. Origin of Minerals in Trap Rocks. The lower part of the hill of Seetabuldee itself exhibits a tendency to columnar structure, caused by horizontal and vertical partings, the sides cf which are coated with thin plates of calcedony, and, according to Capt. Jenkins*, of calc spar. These minerals are not confounded with the substance of the basalt, and may be the result of infiltration or sublimation of siliceous and calcareous matters, In no other situation did I meet with an example in which either of these processes would account for the occurrence of the calcedonies, zeolites, calc-spar, &c. found in the amygdaloids and no- dular basalt of India. Almost everywhere, calcareous spar is more rare than siliceous minerals, which would not be the case were they derived from infiltration, if we are to interpret the past by the present operations of nature. Wherever I have met with the basalt, and in the neighbour- hood of every greenstone dike or insulated mass of that rock, and under every layer of basaltic soil in India, calcareous matter is deposited, and has even occasionally a crystalline structure. In the escarpments of the Mysore ghats, veins of basalt, not two inches thick, ramify through the granite, and are coated with a compact layer of carbonate of lime. Voysey found the granite in the neighbourhood of the basalt intermixed with calcareous matter, indications of which I have myself seen, in the deposit of tuff on the summit of granitic logging-stones near greenstone. If, then, we suppose infiltration to have deposited the calcedonies, agates, &c., &c., when chemical action is presumed to have been more powerful than at present, a greater number of the cavities would have been filled with lime than with such intractable substances, which is not the case. These are also frequently intermixed with the basalt in a manner which could have been pro- duced only by their being formed simultaneously. I have seen masses of calcedony, passing into a black mineral not to be distinguished from the surrounding basalt. They also occur in the compact nodules where no fluid could have had access, and even in the cavities of the Seetabuldee basalt, lined by an impervious glassy coat. In this rock, likewise, cale spar occurs, penetrated by needle-like crystals of the same substance, invested with a crust of the basalt and connected with each side of the cavity, and resembling chiastolite in structure. It is indeed impossible to con- ceive how many of the appearances presented by the agates, cornelians, or drusy cavities in cal- cedony, partially or entirely filled by quartz crystals, or a central mass of calc spar, could be formed in the way supposed, as the first coating of silex would effectually close out the further access of the aqueous solution of that substance ; nor could layers so formed, separate into distinct cavities, having both sides covered with quartz crystals, as they are sometimes seen to do. It is, however, only by a careful study of the rocks themselves, that this can be fully understood. I have selected a few specimens to show that the majority, if not all the minerals of the Indian trap rocks, are not formed by infiltration. One of these, perhaps, deserves particular notice; itis a mass of calcedony, 8 or 10 inches in length and 6 or 8 in diameter, of a conical shape, and was found imbedded with its apex downwards between the globular basalt, and impressed with the irregularities of its surface. In another of these specimens the upper part is perfectly flat and * Asiatic Researches, vol. xviii., p. 199. fy 4 ad ee = ee oe Loveseats Se So sess =e Sere ine a yore RL ee net ee oe 560 ‘ J.G. Matcotmson, Esq., on the Fossils of smooth, without any impressions of the basalt, and is composed of a thick covering of cacho- long, parallel stripes of which appear to indicate the slow cooling of the surface. The centre of the mass is composed of quartz crystals, radiating to the centre, which is occupied by calca- reous spar impressing or impressed by the quartz. The mode of its occurrence increases the conviction in my mind, that the only correct theory of the formation of such minerals in trap rocks, is the play of the molecular attractions existing between similar particles of matter. That so eminent an inquirer as Dr. Turner should have asserted that all calcedonies, rock cry- stals, &c., even when occurring in volcanic rocks, are the result of aqueous infiltration *, I can only account for, by the difficulty of explaining how carbonic acid is retained at high tempera- tures, in any other way than by supposing a great pressure to have existed at the time the rock was in an ignited state ; but of the existence of which, proof is often entirely wanting where cry- stals of carbonate of lime occur. The phenomena exhibited by the vesicular trap, scoriz, and porous chert associated with the Indian basaltic and fossiliferous rocks, satisfied me, that at the time of their formation they were subject to no pressure sufficient to retain the carbonic acid of the altered limestones, and of the shells and cale spar inclosed in the geodes; but no other ex- planation presented itself, till I was informed by Mr. Faraday of his beautiful experiment of ex- posing carbonate of lime in perfectly dry air to the heat of the oxy-hydrogen blowpipe, without driving off its carbonic acid. In the simple apparatus employed by him to show that the reten- tion of the acid depended on the absence of moisture, no pressure of any consequence could be exerted on the lime. Guy Lussac has lately published some experiments on the effect of aqueous vapour in assisting the escape of carbonic acid from limestone, and concludes, that its agency is trifling + ; but as he does not appear to have taken the precaution of drying the atmospheric air by passing it through sulphuric acid, as was done by Mr. Faraday, they cannot be considered as invalidating the beautiful results obtained by the latter. His observation, however, that the water contained in limestones is driven off before the carbonic acid and at a much lower heat, is import- ant, in showing that the calcareous matter in a rock exposed to voleanic action may lose its water before the carbonic acid, and be thus reduced to the state of the carbonate of lime in Mr. Fara- day’s platinum tube. These facts will assist in explaining the anomalies observed in the fossils of the district above referred to, which often retain their carbonic acid when portions of the rock in which they occur have been fused by the inclosing basalt, while other portions are vesicular from the escape of gaseous matters. The whole phenomena, indeed, would admit of explanation by supposing, what must in fact have occurred, the presence or absence of moisture during the various degrees of heat to which the rocks were exposed in the progress of the eruption, and in the course of cooling. A shell, in one part of a rock, may thus retain its carbonic acid, while in another portion it may be reduced to quick lime, subsequently carried off by the water, leaving only a cast ; and a third may be replaced by silica, or the form of its convolutions taken by fine quartz crystals, perhaps derived from silica rendered gelatinous by the lime with which it was ignited t. In stating these views, I venture only to express an opinion forced on me by the phenomena under description, and which appear to explain some of them better than the theory of pressure, which, however useful in removing the prejudices against the igneous origin of the trap rocks, * Lecture on the Chemistry of Geology, by Dr. E. ‘Turner, Edin. New Phil. Journal, Oct., 1833. + Annales de Chimie et de Physique, Oct., 1836. { Fora knowledge of the fact, that lime calcined with finely-divided silica, acts like the fixed alkalis in rendering it gelatinous and soluble in weak acids, I am indebted to Capt. Smith of the Madras Engineers, F.R.S. the Eastern Portion of the Basaltic District of India. . 561 has been injurious in leading geologists to admit too easily the existence of aqueous pressure, or extensive denudations of solid rocks, supposed to have confined the carbonic acid at the time of eruption. No doubt pressure is an efficient agent in some cases*, but not in many to which it has been applied. The trap terminates in the line of section, a few miles to the north of the city of Nagpoor, and is succeeded by a red sandstone, the strata of which are bent, fractured, and converted into a compact quartz rock, at the point of contact with the granite which has burst through it. Within a few hundred yards of the ravine where these phenomena were observed, mica slate occurs, and a little beyond, some hills of gneiss. A bed of granular limestone is quarried at the foot of a conical hill of basalt, in part composed of a scabrous quartzose, and calcareous rock, abounding in drusy cavities, calcedonies and cornelians. Further north, granite veins pass through a much-elevated lime- stone, varying in colour from red to gray and black, and the stratification of which is nearly obliterated. The gneiss and mica slate forming the neigh- bouring hills are also penetrated by dykes and masses of granitet. To the north of this district are 50 miles of a wild mountain country, composed of granitic rocks, with trap in the ascents and tops of the passes ; the basalt then reappears, and composes great part of the valley of the Nerbudda. In a direction south-west of Nagpoor, the nodular basalt is the only formation met with as far as Baitool (90 miles), where granitic rocks reappear, but are succeeded by fine-grained sandstones with traces of coal, and penetrated by trap dykes ranging from S.E. to N.Wf. Here, the sandstone rises into mountains, and constitutes what appears to be the continuation of the range forming the division between the valleys of the Taptee and Nerbudda rivers ; and “ indu- rated clay,” containing casts of the same shells as those of the Sichel range, also occurs. Before proceeding to notice more particularly the fossils, and the evidence they afford of the geological era of the intrusion of the basalt, it is necessary to make some observations on the Sichel range, and the connexions of the several formations occurring in the district described. The basaltic rocks of Nagpoor and of the country to the south, have been considered by every ob- server to form the eastern part of the great basaltic formation of Western India, with which it is continuous, and with which it agrees in every particu- lar of general character and mineralogical structure, and in being connected with stratified rocks, which, as far as is yet known, are of the sameage. The only difference is, that towards the eastern limits of the formation, the hills are * Transactions of the Royal Society of Edinburgh, vol. vi., p. 120. t Captain Jenkins, in Asiatic Researches, vol. xviii. { Lieuts. Miles and Finnes, Journal of the Asiatic Society of Bengal, Feb., 1834, and Dr. Spils- bury, August, 1834. EA eT ce RP Se ee Se ee ee Se oe gears ere ty Pees a 2 Pelee oi ra Be SER nat ~~ os iz sa ae we ug Oh baths ie bates ahi th. helene se ees rah Antthan ahi ie 4 hai Ne Bape © an yee 5. a, i F, ; ike Liha eat fia) vai Mts se, Lie i vi hart ad my ii afta at) ay Mane Pri wilh al Ryalucett it beea eh dig a an ba mel) | ft iv 7 a inet it ry ty PPR Walt ey . iis " sy Oa? See wh ‘ans Ae mt a K! Hatt ed PT ie Ah na m2 Anite Caen Ti asta want bike HigulAN Mau t a) i i Neh A HOE ine | [ 599 ] XLI.—On some remarkable Dikes of Calcareous Grit, at Ethie in Ross-shire. By H. E. STRICKLAND, Esgq., F.G:S. {Read March 7th, 1838.] T AM desirous of calling the attention of the Society to some remarkable dikes which penetrate lias schist at Ethie, near Cromarty. The beds of lias at this place have been described by Mr. Murchison in our Transactions*, and their relations are given in the accompanying wood-cut (p.600). These beds are only exposed at low water, and dip towards the sea at an angle which gradually increases in approaching high-water mark, where they become perpendicular. Cliffs of gneiss and red conglomerate rise immediately from the shore, but the broken fragments which are scattered near high-water mark, conceal the actual junction of the lias with these older rocks. The dikes, which are here seen to penetrate the lias, are remarkable for their mineral character, which so precisely resembles that of certain altered quartzose sandstones, that it is impossible to refer them to a purely igneous origin. The substance of which they are composed, is intensely hard. On exa- mining it with a lens, its component particles are distinctly seen, and bear the closest resemblance to ordinary water-worn grains of sand. The stone is penetrated by carbonate of lime, which produces a slight effervesence on the application of an acid; and it has assumed a pseudo-crystalline structure, which exhibits, when held in certain lights, the peculiar lustre of the calca- reous sandstones of Fontainebleau and other places. A careful examination of the locality sufficed to show, that however much this rock might resemble an aqueous product, yet that it forms genuine intru- sive dikes, penetrating the lias shale in all directions. A and B are two dikes (see the wood-cut) which are parallel to the stratification of the lias shale, and their injected origin is not consequently immediately apparent ; but C is a dike which sends off branches in various directions, and in no part of its * Second Series, vol. ii. p. 308. ooh: ae: ee — — iw gletene Pena oo vee ete 600 H. E. Srrickxianp, Esq., on some Dikes at Ethie, Ross-shire. course is parallel to the strata which it penetrates. The thickness of this dike is about one foot, and that of its lateral offsets from three to six inches. D is the largest dike of all, being three feet thick, and ranging parallel to the shore for at least 200 yards. In one place, it also gives off a lateral branch, which extends a few yards and then rejoins the main dike. These several dikes exhibit no variation whatever in their texture or com- position, except being occasionally penetrated by small veins of carbonate of lime. They show no signs of lamination, but are frequently fractured trans- versely to their own direction. The transition is instantaneous from the dike to the lias shale, which seems to have suffered neither alteration nor contor- tion by the intrusion of this extraneous matter. The shale, from its greater softness, has been washed out between the dikes, leaving them to project like walls from one to three feet in height*. I have been the more exact in describing this locality, because the identity of the specimens here exhibited with ordinary stratified sandstone is so perfect, that the clearest evidence was necessary to prove that they had been inserted into fissures of the lias subsequently to its deposition. The sedimentary struc- ture of this rock forbids us to refer it to igneous injection from below, and notwithstanding the complete resemblance of these intrusive masses to ordi- nary plutonic dikes, we have no resource left but to refer them to aqueous deposition, fillmg up fissures which had been previously formed in the Lias. We have no clue to the period at which this insertion of sand into fissures of the lias took place, no fossils having been noticed in the substance of the dikes themselves. In speculating on the causes of this phenomenon, we should bear in mind the total absence of trappean rocks on the eastern coasts of Ross-shire and Sutherland, and the presence of vast masses of granitic and syenitic rocks, which have been shown by Mr. Murchison to have been erupted subsequently to the deposition of the oolitic series. * Mr. Murchison, in his paper on Brora, (Geol. Trans. 2nd Series, vol. ii. p. 304,) mentions a dike of quartz rock as occurring at Kintradwell, on the coast of Sutherland. That gentleman has further informed me, that in company with Professor Sedgwick he noticed similar dikes, both at Ethie and at other places on that coast. [ 601 } XLIT.—On the Connexion of certain Volcanic Phenomena in South America ; and on the Formation of Mountain Chains and Volcanos, as the Effect of the same Power by which Continents are elevated. By CHARLES DARWIN, Eszq,., Sec., G.S., F.R.S. {Read March 7th, 1838.] Plate XLIX. CONTENTS. Intropuction, p. 601. Observations on the earthquake in Chile of Feb. 20th, 1835, p. 601. On the identity of the force which elevates Continents, with that which causes volcanic outbursts, p. 606. On periods of increased volcanic action affect- ing large areas, p. 610. Nature of the earthquakes on the coasts of South America, p. 615. On different kinds of earthquakes ; and conclu- sions regarding those which accompany ele- vatory movements, p. 622, Theoretical considerations on the slow eleva- tion of mountain chains, p. 625. Concluding remarks, p. 629. INTRODUCTION. THE object of the present memoir is to describe the principal phenomena generally accompanying the earthquakes on the west coast of South America ; and more especially those which attended the shock that overthrew the city of Concepcion on the morning of the 20th of February, 1835. These phe- nomena evince, in a remarkable manner, the intimate connexion between the volcanic and elevatory forces; and it will be attempted to deduce from this connexion, certain inferences regarding the slow formation of mountain chains. Observations on the Earthquake in Chile of Feb. 20th, 1835. This earthquake has been the subject of several published memoirs: the sixth volume of the Geographical Journal* contains an admirable account of it by Capt. Fitz Roy, R.N., in which many interesting facts are detailed, and the elevation of a large extent of coast is incontestably proved. The Philosophical * “Sketch of the Surveying Voyage of His Majesty’s ships Adventure and Beagle.” Vol. vi. Part II. p. 311. é 4 PR ie ree: 2 ase Te 602 C. Darwin, Esq., on Volcanic Transactions for 1836, also, contains a memoir on this subject by Mr. Cald- cleugh. I must, therefore, refer to these authors, whose statements, as far as I had an opportunity of observing, I can fully corroborate, for a particular de- scription of the earthquake itself, and of the changes of level which accom- panied it in the neighbourhood of Concepcion. I will add only a few details, and will then proceed to describe the manner in which the southern volcanos of Chile were affected during the shock. The island of Juan Fernandez, situated 360 geographical miles N.E. of Concepcion, seems to have been more violently shaken than the opposite shore of the mainland, and at the same time a submarine volcano, which con- tinued in action during the day and part of the following night, burst forth near Bacalao Head, where the depth was afterwards ascertained to be sixty- nine fathoms. This fact possesses a peculiar interest, inasmuch as during the earthquake of 1751, which utterly overthrew Concepcion, this island was likewise affected in a remarkable manner, considering its great distance from the chief seat of disturbance. If any exact record had been kept of that event, many other points of resemblance would probably have been dis- covered. There is a tradition, that the land was then permanently elevated, and the area affected appears to have been very much the same with that disturbed in Feb. 1835. Molina* also states, that the undulation travelled from the southward; and in this second catastrophe the inhabitants agreed in thinking that it came from S.W., or even more southerly. After an interval of only eighty-four years, it is not at all improbable that the subterranean forces should be directed towards the same identical points. Being anxious to trace the effects of the earthquake to the south, I wrote, shortly after visiting Concepcion, to Mr. Douglas, a very intelligent man, with whom I had become acquainted in the island of Chiloe; and the answer, which I have received since my return to England, is full of curious information. He describes the earthquake, which appears to have been felt over the whole area at almost the same minute, (as far as the clocks of the country can be relied on,) as being very violent, He says, that twenty minutes before the great shock a trifling one was felt, a circumstance which I did not hear of in any other part. He was at the time on the island of Caucahue, (one of the many islets on the inland shore of Chiloe) and at the time wrote down the following remarks in his pocket-book: ‘“ Felt an earthquake at half-past eleven o'clock, motion horizontal and slow, similar to that of a ship at sea going before a high regular swell, with three to five shocks in a minute, somewhat stronger than the continued motion ; direction from N.E.toS.W. Forest trees nearly touched the ground in these directions, but none fell in our vicinity ;—pocket compass placed level on the ground, N. point set to lubbers’ point; remarked that it vibrated during the violent * Compendio de la Historia del Reyno de Chile, vol. i. p. 33. Phenomena in South America. 603 shocks two points to westward and only half a point to eastward; stood at N. when the motion was less violent. Four minutes afterwards, a shock more violent than any of the preceding ones, affecting the compass as before: another violent shock, and then the movements became gradually less distinct, and eight minutes after the first commencement, they entirely ceased.” I have quoted Mr. Douglas’s statement with regard to the compass, although it is not clear how any movement could have forced it to oscillate towards one side more than to another. I presume, however, if the needle with its card had not been acted on by the magnetic force, it would have been thrown in the trough (if such an expression may be used,) of the undulation, that is, in a N.W. and S.E. line, and, therefore, that the recurrence of this tendency, act- ing against the polar attraction, caused the unequal oscillations, as described. In my Journal of Researches*, | have endeavoured to show, that the vorti- cose movement, which in several earthquakes appears to have affected the stones in buildings, possibly may be explained on the same principle, namely, that the stones are so shaken that they arrange themselves according to their forms, in the line of vibration, as the compass would have done, had it not been acted on by the magnetic force. ‘That the movement of the surface was un- dulatory, is shown by the fact, that at Concepcion the walls which had their extremities directed towards the chief point of disturbance generally remained erect, although much fractured ; whilst those extending at right angles to these first lines, were hurled to the ground ; for in the latter case we must suppose, that the whole wall was thrown at the same moment out of its perpendicular by coinciding with an undulation. The fact mentioned by Mr. Douglas of the trees almost touching the ground from the effects of the movement, though very extraordinary, has been noticed by eye-witnesses of earthquakes in other parts of the world+. The circumstance (even supposing it somewhat exaggerated) is the more remarkable, since at Valdivia, which is situated on the coast between this island and the centre of the disturbance at Concepcion, the shock produced no such effects. I was seated in a thick wood there, during the earthquake, and the trees were only slightly shaken. The range of the Cordillera opposite Chiloe, a narrow island ninety miles in length, is not nearly so lofty as in Central Chile, and a few only of the culminant peaks, which are all active volcanos, exceed 7000 feet in height. Mr. Douglas has given me a detailed account of the effect produced on them by the shock. * Journal of Researches during the Voyage of the Beagle, p. 376. + This is mentioned by Dolomeu as a well-known fact during the Calabrian earthquake of 1783. Lyell’s Principles of Geology (5th edition), vol. ii. p. 217. VOL. V.—SECOND SERIES. Al 604 C. Darwin, Esq., on Volcanic The volcano of Osorno had been in a state of moderate activity for at least forty-eight hours previously; Minchinmadom in much the same gentle action as for the last thirty years; and the Corcovado had been quiet during the whole previous twelve months. ‘At the moment of the shock, Osorno threw up a thick column of dark blue smoke, and directly that passed, a large crater was seen forming on the S.S.E. side of the mountain; it boiled up lava, and threw up burning stones to some height, but the smoke soon hid the mountain. When seen again a few days afterwards, it showed very little smoke by day, but by night, the new crater, as well as the old one on its trun- cated summit, shone with a steady light. This volcano appears to have remained in activity throughout the year. The action of Minchinmadom was similar to that of Osorno: two curling pillars of white smoke had been observed all the morning ; but during the shock, numerous small chimneys seemed to be smoking within the great crater, and lava was thrown out of a small one just above the lower verge of the snow. Eight days afterwards this little crater was extinct ; but at night five small red flames were seen in a line, equidistant from each other, like those in the streets of a village. By the lst of March its activity was much diminished ; but on the 26th there was a smart earthquake, and at night the five fires were again seen. A fortnight afterwards the tops of fifteen conical hills could be seen within the wall of the great crater, and at night nine steady fires, of which seven were in a line, and two straggling.” At the time of the great shock, the Corcovado showed no signs of activity, nor was it heard in action after the Cordillera were hidden in the clouds. Mr. Douglas, however, states, that when that volcano was visible a week afterwards, the snow was seen to have been melted around the N.W. crater. On Yantales, a lofty mountain south of the Corcovado, three black patches having the appearance of craters were observed above the snow-line ; and Mr. Douglas did not recollect having seen them before the earthquake. Bearing in mind, that on many occasions, the melting of the snow on a volcano has been the first indication of a fresh period of activity, and that, as 1 shall presently show, the eruptions of the Corcovado and Orsono are sometimes co-instantaneous, I think there can be little doubt that these appearances prove the effects of the great convulsion of the 20th of February to have been felt by these, the most southern volcanos in America. Mr. Douglas states, that on the night of November 11th (ten months after the overthrow of Concepcion), Osorno and Corcovado both burst out in violent action, throwing up stones to a great height, and making much noise. He subsequently heard, that on the same day, Talca- huano, the port of Concepcion, little less than 400 miles distant, was shaken by a severe earth- quake. This latter statement has since been confirmed to me by a gentleman, who was at the time resident in Chile. Here, then, we have a repetition of the same connected action, which was displayed in so remarkable a manner-on the 20th of February. Mr. Douglas in conclusion adds, that on December the 5th his “ attention was arrested by the grandest volcanic spectacle he had ever beheld ; the §.S.E. side of Osorno had fallen in, thus uniting the two craters, which appeared like one great river of fire. Enormous quantities of ashes and smoke were erupted during the succeeding fortnight.” It is therefore evident, that the volcanic chain from Osorno to Yantales (a length of nearly 150 miles) was affected not only at the moment of the great shock of February 20, 1835, but remained in very unusual activity during many subsequent months. Again, on November 7, 1837, two years and three quarters after the overthrow of Concepcion, both Valdivia and San Carlos, the capital of Chiloe, were violently convulsed, even more so, ac- cording to M. Gay*, than in 1835, or on any former recorded period ; this shock was sufficiently * Comptes Rendus, 1838. Séance Juin 11. Phenomena in South America. 605 strong (bastante recio*) at Talcahuano ; and it appears from the evidence of Captain Coste, pub- lished in the Comptes Rendus+, that the island of Lemus in the Chonos Archipelago, 200 miles south of San Carlos, was, by this same earthquake, upraised more than eight feet : describing the present state of the island, M. Coste says, “des roches jadis toujours couvertes par la mer, restant aujourd’hui constamment découvertes.” We see, therefore, that, in 1835,—the earthquake of Chiloe,—the activity of the train of neighbouring volcanos,—the elevation of the land around Con- cepcion,—and the submarine eruption at Juan Fernandez, took place simulta- neously, and were parts of one and the same great phenomenon. Again in 1837 a large part of the same area was violently affected, whilst a district, 200 miles southward of San Carlos in Chiloe, instead, as in 1835, of 300 north- ward of it, was permanently upraised. We must therefore believe, that these two elevations of the land, although not simultaneous, were effects of the same motive power intimately connected together. Although the earthquake of February 1835 was so severe in Chiloe, yet at Calbuco, a village situated on the mainland opposite the northern extremity of the island, it was felt with much di- minished violence, and on the neighbouring Cordillera (near Mellipulli) not at all. Some men who had been employed in the mountains splitting fir-planks, when they returned in the evening to Calbuco and were told of the shock, said, that ‘‘ about the time mentioned, they recollected that they had not been able to strike fair with the axe, and that they had spoilt a board or two, by cutting too deep.” This probably is not so fanciful as it at first appears; at least it shows that, if there were any motion, it was of an exceedingly gentle kind. It is a most interesting circumstance thus to find, that the great columns of smoke shot forth from the tall chimneys of the Andes, re- lieved the trembling ground, which at that moment was convulsed over the whole surrounding country. Mr. Caldcleugh{, has stated in his Memoir, that several volcanos in the Cordillera northward of Concepcion were ina state of great activity after the earthquake. It is therefore remarkable that Vil- larica (near Valdivia), a voleano which is more frequently in eruption than almost any other in the range, although situated in an intermediate position, between those of central Chile and those in front of Chiloe, was not in the least affected. The day was very clear, and although not at the moment of the shock, yet within two hours after it, I attentively watched its truncated summit, but did not per- ceive the least signs of action. This circumstance probably has an intimate relation with the less force of the earthquake in the same intermediate district. In 1837, however, it suffered simi- larly with Chiloe. Although Villarica was passed over in 1835, yet in the account of the earth- quake of 1822 at Valparaiso, it is said, “ at the moment the shock was felt, two volcanos in the neighbourhood of Valdivia (where the earthquake was pretty sharp) burst out suddenly with great noise, illuminated the heavens and the surrounding country for a few seconds, and as sud- * Voyages of the Adventure and Beagle, vol. il. p. 418. + Comptes Rendus, October, 1838, p. 706. { Phil. Transact. for 1836. I likewise was informed by an intelligent person, that he had seen, from the plain near Talca, a volcano in the Cordillera in great activity on the night subsequent to the earthquake. ArQ2 8 See eg FES TIE IE ANS 606 C. Darwin, Esq., on Volcanic denly subsided into their quiescent state*.” The vents in Central Chile, nearer the chief focus of disturbance, were not at the time of that earthquake affected; but according to the information received by Dr. Gillies} in 1836, from a miner who had resided many years in sight of the vol- cano of Maypu, its eruptions were very frequent during the four years immediately subsequent to it. Many other instances are on record of earthquakes having passed over certain districts, in the same manner as we see the eruptive force acted with respect to Villarica. Humboldtt remarks, that the inhabitants of the Andes, speaking of an intermediary ground, which is not affected by the general motion, say with simplicity, ‘ that it forms a bridge” (que hace puente); and he adds, “as if they meant to indicate by this expression, that the undulations were propagated at an im- mense depth under an inert rock §.” On the identity of the force which elevates Continents with that which causes volcanic outbursts. it has frequently happened, that during the same convulsion large areas of the globe have been agitated, and strange noises propagated to countries many hundred miles apart| ; but in these cases, it is not possible to form any conjecture over how wide an extent, any actual change has taken place in the subterranean regions. It is different, when we hear from Humboldt, that at the moment when the volcano of Pasto ceased to eject a column of smoke, the city of Riobamba, sixty leagues to the southward, was overwhelmed by an earthquake ; for the effect here produced certainly cannot be explained by the mere transmission of a vibration. During the Concepcion earthquake, * Journal of Science, Vol. xvii. + The Edinburgh Journal of Natural and Geographical Science, August 1830, p. 317. + Humboldt’s Personal Narrative, Vol. iv. p. 21. English Translation. § Another instance of earthquakes, violently affecting distant regions and passing over the in- termediate country, is mentioned in the ‘‘ True relation of the Earthquake of Lima, 1746.” It is there said (p. 192) that the shock was most violent at Lima and Callao, becoming gradually less along the coast, but that at Guancavelica excessive shocks were felt and noises heard. The editor believes, there is no other place called Guancavelica except the famous quicksilver mines of that name, situated 155 miles to the S.E. of Lima. MacClelland (Report on the Coal Mines of India, p- 43,) mentions some cases of intermediate places being little shaken during great earthquakes. || As examples of the first case, may be adduced the trembling of the ground on the coast of Chile along a space of more than one thousand miles ; and during the Lisbon earthquake in 1755, countries about 3000 miles apart were affected (see Michell on Earthquakes: Phil. Trans. 1760.). With respect to the second case, Humboldt states, that during the eruption at St. Vin- cent’s, subterranean noises were heard on the banks of the Apure, a distance of two hundred and ten leagues. (Person. Narr. Vol. iv. p. 27.) During the eruption of Coseguina in 1835, it is said, that noises were heard at Jamaica, 660 miles distant. q As other instances of the same kind, I may mention the outburst in 1822, of the volcanos near Valdivia at the same moment that Valparaiso, nearly 400 miles distant, was levelled to the ground. Again, in 1746, when Lima was overthrown, three volcanos near Patas and one near Lucanas, the two places being 480 miles apart from each other, burst forth during the same night. (Ulloa’s Phenomena in South America. 607 at one extremity of the area affected, the snow was melted on Yantales and the neighbouring vents renewed their activity; whilst at Juan Fernandez, at the distance of no less than 720 geographical miles from Yantales, an eruption took place beneath the sea ; and soon afterwards the volcanos in the Cordillera, 400 miles to the eastward of that island, burst forth in action,— a large extent also of country, intermediate between these extreme points, being permanently upraised. To form a just idea of the scale of this pheno- menon, we must suppose, during the same hour, Europe to be shaken from the North Sea to the Mediterranean,—a large tract of the eastern coast of England to be permanently elevated,—a train of volcanos on the northern coast of Holland to burst forth in action,—an eruption to take place at the bottom of the sea, near the northern extremity of Ireland,—and the ancient vents of Auvergne, Cantal, Mont d’Or, and others, so long extinct, each to send up to the sky a dark column of smoke. Moreover, as, in Chile, a large part of the same area was two years afterwards most violently shaken, at the same time that Lemus was upraised, so must we imagine that, subsequently also, in Europe, whilst France, from the English Channel to the central pro- vinces, where the volcanos had been excited into long and fierce action, was desolated by an earthquake, an island in the Mediterranean was permanently elevated ;—then should we have the subterranean movements which shook South America on the 20th of February, 1835, and on the 7th of November, 1837, acted in countries with which we are familiar. When first considering these phenomena, which prove that an actual move- ment in the subterranean volcanic matter occurred almost at the same instant of time at very distant places, the idea of water splashing up through holes in the ice of a frozen pool, when a person stamps on the surface, came irre- sistibly before my mind. The inference from it was obvious, namely, that the land in Chile floated on a lake of molten stone, of which the area, as known from the various points in eruption on the day of the earthquake, would be nearly double that of the Black Sea. If this inference be denied, the only alternative is, that channels from the various points of eruption unite in some deep-seated focus, like the arteries of the body in the heart, whence Voyage, Vol. ii. p. 84.) I allude to these cases more particularly, because that distinguished philosopher, M. Boussingault (Bulletin de la Soc. Géolog. Vol. vi. p. 54.), having been much struck with the fact, that the earthquakes which have been. most destructive to human life have been unaccompanied by volcanic outbursts, has, I think, generalized the remark too far. The earthquake of Concepcion in 1835 undoubtedly was one of extreme violence, although, from hap- pening in the day, and from commencing gradually, it caused but few deaths (probably in the whole province not more than 70); nevertheless we have seen, that it was accompanied by co-instanta- neous eruptions from several and very distant points. Be ee SR eR hy BE Ee EAR ae AR TR OES 608 C. Darwin, Esq., on Volcanic an impulse can be transmitted to distant parts of the surface, with nearly equal force. But according to this view, if two separate trains of volcanos in the Andes have any connexion whatever, which seems highly probable from the symmetry of the Cordillera, (and possibly an intimate one, as will pre- sently be discussed,) then the common focus, from which the two main branches are sent off, must be seated at an enormous depth. But all the calculations regarding the depth at which molten rocks must necessarily be met with, if they can be at all trusted *, tend to prove, that the earth’s crust is not much more, and perhaps less, than twenty miles in thickness ; and if this be so, the crust may, indeed, be well compared with a thin sheet of ice over a frozen pool. These considerations are, perhaps, of little weight, but we must bear in mind, that the elevation of many hundred square miles of territory near Con- cepcion is part of the same phenomenon, with that splashing up, if I may so call it, of volcanic matter through the orifices in the Cordillera at the moment of the shock; and as this elevation is only one of a long series, by which the whole coast of Chile and Peru, even for more than a thousand miles, has been upraised several hundred feet within the recent period, (as I endeavoured to show in a paper formerly read to the Society{, and I hope hereafter to prove more fully,) the body of matter added below must have been enormous. When we reflect on this, it is obvious, that the term channel cannot be applied to a means of communication extending beneath a large portion of a continent, and from the interior of the globe to the superficial crust {. The facts appear to me clearly to indicate some slow, but in its effects great, change in the form of the surface of the fluid on which the land rests. * M. Parrot, however, (Mémoires de l’Acad. Imp. des Sciences de St. Pétersbourg, Tom. i. 1831. Science. Math. Phys. et Naturelles) altogether denies that the data are sufficient to form any judgment on this subject. + Proceedings Geol. Soc., Vol. ii. p. 446, Jan. 1837. } Professor Bischoff (Edinburgh New Philosophical Journal, Vol. xxvi. p. 59, 1838.) has even argued that “‘ the immense masses of lava ejected from a single volcano, and the enormous extent in which volcanic actions are felt at the same time, scarcely leave room to doubt that every active volcano is in immediate communication with the whole melted matter in the interior.” How in- comparably stronger this argument is, if applied to the plutonic as well as volcanic rocks, composing the great masses of the Cordillera! but now that we know, that continental elevations are caused by the very same impulses with those which eject lava and scorize through the mouths of volcanos, the argument from the bulk of matter observable in ejected or interjected masses of rock, may be passed over, since the matter added below, when a whole kingdom is permanently elevated, must far exceed that composing either a volcanic hill or the axis of a mountain-chain ; and there- fore we are so much the more strongly urged to look for its source in “the whole melted matter of the interior,” and not in any local receptacle. Phenomena in South America. 609 In a geological point of view, it is of the highest importance thus to find three great phenomena,—a submarine outburst, a period of renewed activity through many habitual vents, and a permanent elevation of the land,—forming parts of one action, and being the effects of one great cause, modified only by local circumstances. When we consider, that the southern volcanos were in eruption some days before the earthquake, and that one of them, Minchinma- dom, has seldom been dormant for the last thirty years, and that they all re- mained active for many months afterwards, we must conclude that the impulse given to them at that moment, was of the same nature with the force which has kept up their activity during the many ages necessary to accumulate the volcanic matter into great snow-clad cones, and which force still continues to add to their height. If the earthquake or trembling of the ground (which, however, we have seen was less near these volcanos than elsewhere) had acted in no other way, than in merely breaking the crust over the lava within the craters, a few jets of smoke might have been emitted, but it could not have given rise to a prolonged and vigorous period of activity. But the power which manifested itself in this renewed action, and to which same power, acting at former periods, the entire formation of these several volcanos has evidently been due, was likewise the cause of the permanent elevation of the land ;—a power, I may remark, which acts in paroxysmal up- heavals like that of Concepcion, and in great volcanic eruptions, in precisely the same manner, for both these phenomena occur only after long intervals of rest, during which the volcano merely casts out, perhaps, a few showers of scoriz, and the land rises with so slow a movement that it is called insen- sible ;—therefore no theory of the cause of volcanos which is not applicable to continental elevations can be considered as well-grounded. Those who believe that volcanos are caused by the percolation of water to the metallic bases of the earth, or simply to intensely heated rock, must be prepared either to give up this view, or to extend it* to the elevation of such vast con- tinents as that of South America. * The arguments in favour of the theory, that steam, produced by the percolation of water to the interior of the cooling planet, is the motive power in volcanic action, has been lately strongly put by Prof. Bischoff in his paper in the Edinburgh Journal (Vol. xxvi. p. 25.). That it must be a modifying cause of great importance seems highly probable; but that it is the primary one of con- tinental elevations, I cannot admit. The phenomenon, as it appears to me, is on far too grand a scale to harmonize with such an explanation. Can the rising of the whole west coast of South America, and of the whole width, at least of the southern portion of it, be explained by the lateral force exerted during the general shrinking of the earth’s crust, modified only by the formation of steam under high pressure, in those parts where water has percolated tothe heated interior ? Such an explanation surely is inadmissible. Thee TERE aed RI OR REE Se ENE PRT ETT REA CSE TE TSS DE ITO EE OS EEE ES SE ST EE NT STE Ie 610 C. Darwin, Esq., on Volcanic On periods of increased Volcanic Action affecting large Areas. Humboldt, when describing certain volcanic phenomena in that part of South America which borders the West-Indian sea, seems to consider, that periods of increased activity affect large portions of the surface of the earth. He has drawn up the two following tables*, to which I have added a third, containing the remarkable events that happened during the years 1834 and 1835: 1811. 1812. 1834, 1835. —— Ist. TABLE OF VOLCANIC PHENOMENA. November. ......The volcano of Pasto began to emit smoke. February 4th.....Destruction of Riobamba. September 27th... Eruption in the West-Indian Islands. Volcano of Guadaloupe. December 14th. .. Destruction of Cumana. 2nd TABLE. May. .......+++Beginning of the earthquakes in the Island of St. Vincent, which lasted till May 12th. December 16th. .. Beginning of the commotions in the Valley of the Mississippi and the Ohio, which lasted till 1813, December. ....- . Earthquake of Caraccas. March 26th. .... Destruction of Caraccas, earthquakes, which continued till 1813. April 30th. ...... Eruption of the volcano in St. Vincent’s, and on the same day, subter- ranean noises at Caraccas and on the bank of the Apure. 3rd TABLE. January 20th. »...Sabiondoy, lat. 1°15’ N. (near Pasto), dreadful earthquake; eighty persons perished ; town of Santiago swallowed up. May 22nd. ......Santa Martha, lat. 11° 30! N.; two-thirds of the town thrown down ; in course of a few days, sixty bad shocks. September 7th. ..Jamaica,—violent earthquake, town not much damaged. January 20th..... Osorno, lat. 40° 31! S. in eruption. Before day-light Aconcagua, lat. 32° 30! S. in eruption. in the morning. Coseguina, lat, 13° N. in terrific eruption, continuing in activity du- ring the two ensuing months. February 12th. ..Earthquake at sea, very strong off the coast of Guyana. February 20th. ..Juan Fernandez, lat. 33° 30! S., submarine eruption. 114 a.m. Concepcion, (lat. 36° 40’ S.), and all the neighbouring towns destroyed by an earthquake; the coast permanently elevated. Volcanos along the whole length of the Cordillera of Chile in eruption. N.B. These volcanos remained in activity for some months subse- quently, and many earthquakes were felt. November 11th...Concepcion, severe earthquake; Osorno and Corcovado in violent action. December 5th. ..Osorno fell in with a grand explosion. * Personal Narrative, Vol. iv. p. 36. I have altered some of the dates in these tables, as they did not agree with the text or with the well-known period of the events. Phenomena in South America. 611 With respect to these tables, it must be observed, that we can never feel sure that the connexion of volcanic phenomena at very distant points is real, until some strongly marked event takes place during the same moment at those points, the intermediate country being likewise affected to a certain degree. In the first two tables, the connexion of the West-Indian vents and the coast of Venezuela may be admitted as almost certain *, nor is the distance very great, being at most only 400 miles. But when, on the one hand, we include Quito, distant from the above area more than 1200 miles, and, on the other, the Valley of the Mississippi, the case is very much more doubtful. The coincidence certainly is very remarkable, both in regard to the commencement and the cessation of the long series of earthquakes which affected South Carolina, the basin of the Mississippi, the Leeward Islands, and Venezuela: yet New Ma- drid is more than 2000 miles from the latter. A repetition alone of such coin- cidences can determine how far the increased activity of the subterranean powers, at points so remote, is the effect of some general law, or of accident. We now come to the third table, with which we are more particularly con- cerned. I have already described in detail the remarkable volcanic pheno- mena which happened, in connexion with each other, on the morning of February 20th, 1835, and likewise during the subsequent year. On January 20th, one month previously, three eruptions, as stated in the table, occurred almost at the same hour in very distant points of the Cordillera. Near midnight on the 19th, the summit of Osorno shone like a great star in the horizon ; and this appearance soon increased into a magnificent glare of light, in the midst of which, by the aid of a telescope, great dark bodies were seen to shoot upward and to fall down in endless succession. When I was at Valparaiso some time afterwards, Mr. Byerbache, a resident merchant, informed me, that sailing out of the harbour one night very late, he was awakened by the captain to see the voleano of Aconcagua in activity. As this is a most rare event I recorded the date. Some time afterwards papers arrived from Central America giving an account of one of the most fearful eruptions of modern timest. ‘‘ On the 19th of Ja- nuary, after twenty-six years’ repose, a slight noise, attended with smoke, proceeded from the mountain of Coseguina. On the following morning (the 20th) about half-past six o’clock, a cloud of very unusual size and shape was observed by the inhabitants to rise in the direction of this volcano.” Enormous quantities of ashes and pumice were then ejected, and the air was darkened, and the ground convulsed, during the three succeeding days. Nearly two months afterwards the volcano was in action. Mr. Caldcleugh observes, that perhaps the only parallel case on record is the well-known explosion of Sumbawa in 1815. When I compared the dates of these three events, I was astonished to find that they agreed within less than six hours of each other. Aconcagua is only 480 miles north of Osorno, but Coseguina is about 2700 north of * Humboldt’s Personal Narrative, vol. ii. p. 226., and vol. iv. p. 36. + Caldcleugh on the volcanic eruption of Coseguina. Philosophical Transactions, 1836, p. 27. VOL. V.—SECOND SERIES. AR Ce a Re RE PE TE TE EL NT I ne ane re errs te Pe Se a eemre a ee 612 C. Darwin, Esq., on Volcanic Aconcagua. It may be asked, were these three eruptions, which burst through the same chain of mountains, in any respect connected, or was the coinci- dence accidental? We cannot be too cautious in guarding against the as- sumption that phenomena are connected, because they happen at periods bearing some determined relation to each other. If we wished to show that the subterranean forces acted after periods of a century, as has sometimes been believed, we might adduce the case of Lima, violently shaken by an earth- quake on the 17th of June, 1578, and again on the very same day in 1678 ; or the eruptions of Coseguina in the years 1709 and 1809, which are the only two on record previous to that of 1835. Again, we might urge, on such erounds, that the Guatimala convulsions follow, at the interval of one year, those near Pasto; fora district in the neighbourhood of the latter place was overthrown by a violent shock precisely one year before the explosion of Coseguina ; both having occurred on the 20th of January. Cosme Bueno imagined that this relation actually did exist between the subterranean move- ments in Guatimala and Peru, and this case makes one more to the list which I have subjoined* as extracted from Humboldt. “With respect to the simul- taneous eruptions of Aconcagua and Osorno, there is little difficulty in ad- mitting that they may have been connected, because in this same region, and only a month subsequently, volcanos further apart were affected by the same impulse. There is nevertheless this remarkable difference in the two cases ;—the last, or that of February the 20th, was a period of commotion throughout the kingdom of Chile, while the simultaneous eruption of Acon- cagua and Osorno appears to have been unaccompanied by any general movement in the subterranean regions. ‘This eruption, probably, was the first indication of those great volcanic disturbances which ensued exactly one month afterwards; for it seems to be a very general occurrence in earth- quakes, that weak spasms precede the worst convulsions. Thus, in 1822, on the 4th of November, Copiapo (lat. 27° 10') was visited by a severe shock, which damaged many houses ; and was followed the next day by a much more violent earthquake, which nearly destroyed the town, and did considerable * Mexico. Peru. Difference of time. (Lat. 13° 32’ North. (Lat. 12° 2’ South.) 30th of November, 1577. 17th of June, 1578. Six and a half months subsequent. 4th of March, 1679. 17th of June, 1678. Eight months in advance. 12th of February, 1689. 10th of October, 1688. Four months in advance. 27th of September, 1717. 8th of February, 1716. Seven and a half months in advance. Humboldt’s Personal Narrative, Vol. ii. p. 227. These facts perhaps tend to show that periods of increased volcanic energy are common to remote parts of the continent ; but as the order of priority is not constant, I cannot believe any other law is indicated. Phenomena in South America. 613 injury to that of Coquimbo, in lat. 29° 50'*. On the 19th of the same month Valparaiso was almost destroyed. Other instances} might be brought forward to show that most earthquakes, though appearing sudden, are in truth parts of a prolonged action, as evinced both by the events which precede and those which follow it. Although, possibly, we may allow that the eruptions of Aconcagua and Osorno, occurring in the middle of the same night, were connected together, and formed a part of the great subsequent disturbances,—yet what must we conclude respecting their coincidence with Coseguina, so immensely remote ? The case is rendered far more extraordinary by two of the three volcanos being generally quiescent. Coseguina, according to Mr. Caldcleugh, burst forth after twenty-six years of repose ; and Aconcagua so seldom manifests any signs of activity, that it had even been doubted whether any part of this gigantic mass, with an altitude of more than 23,000 feet, is of volcanic origin. To illustrate the case: if we suppose Stromboli and Vesuvius to be in violent eruption on the same hour of the night, little would be thought of the coinci- dence; but it would be otherwise if this should happen with Vesuvius and Etna; and our surprise would be greatly increased if we afterwards heard that Hekla, after twenty-six years’ repose, had burst forth at the same time with tremendous explosions. Nevertheless, if such a coincidence had occurred in Europe, a country possessing no unity of character, and the two points not being more than 2000 miles apart, it is very doubtful how far the phenomenon would have been worthy of consideration. But the case is different in America, where the volcanic orifices all fall on one great wall or fissure, (for the Andes may be in- differently so called,) and where the immensity of the level area on the eastern side, proves with what wonderful equability the subterranean forces have acted on this portion of the globe. Moreover, when a line of coast more than two thousand geographical miles in length has been elevated (as I hope here- after to prove) within a period so recent, that, as compared to the countless past ages of which we possess records in the works of nature, it may be * Journal of Science, Vol. xvii. + Several distinct cases are known in which springs and wells have been affected, their water rendered turbid, and altered in quantity, previously to bad earthquakes. This was observed at Lisbon in 1755 ; and in New England during two or three days before a shock, “ the waters of some wells were rendered muddy and stank intolerably.” (Michell, Philosophical Transactions, 1760, p. 44.) Humboldt and others have noticed, that the wells in the neighbourhood of Vesuvius are affected previously to its bad eruptions. These facts appear explicable, on the idea of a slight stretching or movement taking place in the crust, before its tension is overcome, a fissure formed, and, as a consequence, an earthquake or eruption caused. Courrejolles, also, has remarked in his memoir on earthquakes (Journal de Phys., Tom. Ixiv. p. 106.), that great earthquakes are almost always preceded by lesser ones. 4x 2 wee a re ee es 614 C. Darwin, Esq., on Volcanic reckoned as unity ; on such a coast it ceases to be improbable, in any ex- cessive degree, that the many impulses which together have produced the one grand effect, should sometimes have been absolutely simultaneous. It has long been remarked, that the vents throughout the Cordillera may be grouped into several systems. Thus we have already shown, that the extreme southern volcanos are connected with those of Central Chile; and I was in- formed by an intelligent resident that he had seen Aconcagua and two vol- canos northward of it, in great activity together:—we thus have a portion of the Andes 780 geographical miles in length (about the distance from the south of England to Vesuvius) forming one connected system. Ulloa * states, that when Lima was overthrown in 1746, three volcanos near Patas and one near Lucanas burst forth ; these places being 480 miles apart from each other. Moreover, Arequipa, to the south, has twice (1582 and 1687) been affected by severe earthquakes simultaneously with Lima. ‘The distance between Arequipa (where there is an active volcano) and Patas is rather more than 600 miles; and this perhaps may form a second system. Humboldt says, “ it appears probable that the higher part of the kingdom of Quito, and the neighbouring Cordillera, far from being a group of distinct volcanos, constitute a single swollen mass, an enormous volcanic wall stretch- ing from north to south, and the crest of which exhibits a surface of more than six hundred square leagues. Cotapaxi, Tunguragua, Antisana, and Pi- chincha, are placed in this same vault, on this raised ground.’ He after- wards shows, from the phenomenon already alluded to, of the cessation of the column of smoke at the moment when Riobamba was overthrown, the con- nexion of these volcanos with those of Pasto and Popayan. This joint system is rather less than 300 miles in length. Again, to the north at Guatimala, Mexico, and California, we have three groups of volcanos, each system being a few hundred miles apart. The connexion between the vents in each separate system has been, in some places, plainly shown, and is extremely probable in all ; but what relation the different systems bear to each other is more doubtful. I am not aware of any fact on record, similar to the contemporaneous eruption of Osorno and Aconcagua with Coseguina. It must not, however, be overlooked, that such events may have happened every year since the Spanish conquest, without the coincidence having once been detected. Excepting from the concurrence of two accidents, I should never have known of this case. On that same night every vent in the Cordillera might have shown transient signs of activity, and six months afterwards it would have been as impossible to have discovered * Ulloa’s Voyage, English Translation, Vol. ii. p. 84. + Personal Narrative, Vol. iv. p. 29. Phenomena in South America. 615 that such had happened, as to have ascertained whether the next day were bright or clouded. There are some active and some nearly extinct craters, in the interval between the Chilian and Peruvian systems, (which is the longest of any, being 900 miles,) but they are situated in countries very thinly peopled, and in some parts entirely desert ; and who is there in such cases to record phenomena, which, even if beheld, are thought of little consequence ? Returning to the third table, I feel no doubt that the volcanic phenomena which occurred in S. America sometime previously as well as subsequently to the months of January and February 1835, were far more numerous than the average proportion during an equal length of time. This remark applies to the two tables copied from Humboldt. In looking at the dates of these events, it must be remembered that each date represents only the moment when the crust of the earth has given way beneath the force, which in some cases has already shown its action, and invariably continues to do so during a period, often of considerable length. Under this point of view, the earth- quakes of Caraccas and New Madrid, of Coseguina and Concepcion, may be considered as actually contemporaneous. From these various circumstances, I am strongly inclined to believe, that the subterranean forces manifest their action beneath a large portion of the South American continent, in the same intermittent manner as, in accordance with all observation, they do beneath isolated volcanos,—that is, remaining for a period dormant, and then bursting forth throughout considerable districts with renewed vigour. Nature of the Earthquakes on the Coasts of South America. I will now more particularly consider the nature of the earthquakes which occur at irregular intervals on the coast of South America. It cannot be otherwise than difficult to trace their precise origin, but the following con- siderations, as it appears to me, lead to one conclusion alone—namely, that they are caused by the interjection of liquefied rock between masses of strata. Ulloa, in his travels*, says, “Experience has sufficiently shown, especially in this country (South America), by the many volcanos in the Cordillera which pass through it, that the bursting of a new burning mountain causes a violent earthquake, so as totally to destroy all the towns within its reach, as happened at the opening of the volcano in the desert of Carguagoazo. This tremulous motion, which we may properly call an earthquake, does not so usually happen in case of a second eruption, when an aperture has been before made, or, at least, the motion it causes in the earth is comparatively but small.” + * Ulloa’s Voyage, Vol. 11. p. 85. ¢ Michell, in his remarkable paper on Earthquakes in the Philosophical Transactions for 1760, 616 C. Darwin, Esq., on Volcanic Although the bursting forth of a new vent may invariably be accompanied by an earthquake, the converse is not true; for if it were, at Valparaiso, Con- cepcion, Lima, Caraccas, and other places, in the immediate neighbourhood of the part most violently shaken, an eruption must always have taken place, which, even if we suppose it to have occurred beneath the sea, is improbable in the highest degree. But we may suppose that these earthquakes are owing to some phenomenon analogous to volcanic eruptions. ‘This opinion is much strengthened by the fact, that great earthquakes, like great eruptions, gene- rally recur only after long intervals of repose, and they thus lead us to believe, that the subterranean force is relieved by either in the same manner. ‘This, indeed, is the direct opinion of the inhabitants of the whole west coast of South America, who are firmly convinced of an intimate relation between the sup- pressed activity of the volcanos in the Andes and the tremblings of the ground. We have, also, seen that, when the island of Chiloe was strongly shaken, some men at work on the flanks of the Cordillera, between the volcanos of Osorno and Minchinmadom, (which both sent up dark columns of smoke, like signals to mark the new period of violence,) were quite unaware of the great convul- sion, which then caused the shores of the Pacific to vibrate throughout a space of more than a thousand miles. There is, however, one difference, although more apparent than real, be- tween earthquakes like that of Concepcion, and those alluded to by Ulloa. In the former, it has almost invariably happened, at least in those on the South American coast, that a vast number of shocks have followed the first great convulsion*, and these, as well as the accompanying subterranean noises, having proceeded from the same quarter with the first shock, are therefore undoubtedly due to the very same cause, only acting with somewhat less intensity. Thus, even in the first twenty-four hours after the earthquake of (p. 580,) has quoted this same passage in confirmation of his view, that ‘the eruptions of voleanos which happen at the same time with earthquakes may, with more probability, be ascribed to those earthquakes, than the earthquakes to the eruptions, whenever at least the earthquakes are of con- siderable extent.” The term earthquake is here used to express the cause of the trembling of the ground. Sir James Hall, in his celebrated memoir on “ Heat modified by compression,” (Edin. Phil. Trans., Vol. vi. p. 166,) distinctly states ‘ that the earthquakes which desolate countries not externally volcanic, indicate the protrusion from below of matter in liquid fusion, penetrating the mass of rocks ;” but he does not extend this view, which is the same which I hold, to any comprehensive generalization, or restrict it to any particular class of earthquakes. * Courrejolles, in his Memoir on Earthquakes, (Journal de Physique, Tom. liv. p. 106,) says, “Les grands tremblemens de terre sont presque toujours précédés et suivis quelque temps avant Michell (Philosophical Transactions, 1760, p. 10) has given ” et aprés par de petites secousses, some instances of successive minor shocks, which appeared to travel from the same point, whence the previous more violent ones had come. Phenomena in South America. 617 1746 at Lima, no less than 200 horrible (I use the language of its historian) shocks were counted. Now in the other case, Ulloa says, that when the ori- fice of eruption is once formed, the earth becomes nearly tranquil ; yet we well know, that the volcano itself almost invariably continues in great activity for many weeks afterwards. Had Ulloa, however, stood near the crater itself, he would undoubtedly have felt those small tremors, which accompany each fresh explosion, as described by others who have been so circumstanced. The tremors, therefore, seem analogous to the secondary shocks ; and, this being so, the phenomena in the two cases are in every respect closely similar. In a primary volcanic outburst, we know the cause to be the explosion of liquid and aeriform matter, first through solid strata, and afterwards through a nearly open passage ; hence we are led to conclude, that the cause of the simple earthquake, with its secondary shocks, are explosions of a similar nature, which, however, do not open a passage, but rend successively portions of the superincumbent masses. At Concepcion, where the streets run in two series, at right angles to each other, the walls were affected, as already observed, according to their direc- tion. This was strikingly exemplified in the cathedral, where the great but- tresses, built of solid brickwork, were cut off as if by a chisel, and hurled to the ground; whilst the wall, to support which they had been vainly built, though much shattered, stood erect,—for the latter had its extremity directed towards the point whence the vibration travelled, but the buttresses were in lines parallel to the undulation. Nearly similar circumstances were observed * in 1822 at Valparaiso. At the great earthquake of Caraccas the direction of the vibration was E.N.E. and W.S.W., and some definite direction appears to have been observed in almost every violent earthquake. Now, it may be asked, could a vibration, which had travelled upwards through the earth from a profound depth, be felt on the surface, as if it had come from a given point of the compass, and could it likewise determine the overthrow of walls accord- ing to their direction with respect to any such point ? It appears to me clearly not; but that a vibration to produce such effects must be transmitted from the rending of strata, at a point not very deep below the surface of the earth. Earthquakes generally affect elongated areas. In the shock of 1837, in Syria, the vibration was felt “on a line 500 miles in length by 90 in breadtht.” Humboldt t remarks, that earthquakes follow the coast of New Andalusia in the * See Miers’s Travels in Chile, Vol. i. p. 392. + Proceedings of Geological Society, p. 540. April 5th, 1837. ~ } Personal Narrative, Vol. ii., p. 224. 618 C. Darwin, Esq., on Volcanic same manner as they do that of Peru and Chile. Thus, at Valparaiso in 1822, the movement was felt along 880 miles of the shore of the Pacific; and at Con- cepcion, in 1835, for the greater length of more than 1000 miles ; but on no occasion has the shock been transmitted across the Cordillera to a nearly equal distance. In 1835 the rocking of the ground was so gentle at Mendoza, that an old man, one of the inhabitants, (and every one in these countries is pos- sessed with an almost instinctive power of perceiving the slightest tremor,) told me, that for some time he mistook the movement of the ground for a giddiness in his head, and that he called out to his friends that he was going to die. At Concepcion, Valparaiso, Lima, and Acapulco*, the residents believe that the disturbance generally proceeds from the bottom of the neighbouring sea; and thus they explain the unquestionable fact}, that the inland towns are generally much less injured than those near the coast. It does not appear, that the disturbance proceeds from any one point, but from many ranged in a band ; otherwise the fact of the linear and unequal exten- sion of earthquakes would be unintelligible. Thus, in 1835, the island of Chiloe, the neighbourhood of Concepcion, and Juan Fernandez, were all violently affected at the same time, and more so than the intermediate di- stricts. In mountainous countries, such as New Andalusia, Peru, and Chile, when earthquakes follow coast lines, they may be said to extend parallel to the littoral chain of mountains. The last consideration I shall enter on, as indicating the cause of earth- quakes, is, that in South America they have sometimes (if not, as I believe, ge- nerally t) been accompanied by elevations of the land ; but this, judging from the Lima shock of 1746, does not appear to be a necessary concomitant, at least to a perceptible amount. It might at first be thought that, at Concepcion, the uplifting of the ground, which accompanied the first and great shock, would by itself have accounted for the whole phenomenon of the earthquake. The great shock, however, during the few succeeding days, was followed by some hundred minor ones (though of no inconsiderable violence), which seemed to come from the same quarter from which the first had proceeded ; * At Acapulco, Humboldt says, the shocks come from three different quarters, the west, north-west, and south. (Polit. Essay on the Kingdom of New Spain; English Translation, Vol. iv. p. 58.) + Almost every author, from the time of Molina, makes this observation. See Molina’s Com- pendio de la Hist. del Reyno de Chile, Vol. i. p. 82. ; My belief is grounded on the fact that, on the same coasts, and within the same period, in which a vast number of earthquakes are recorded, there exist proofs of an elevation of the land; although the rise is not known to have been connected with any particular earthquake. Phenomena in South America. 619 whilst, on the other hand, the level of the ground certainly was not raised by them; but on the contrary, after an interval of some weeks, it stood rather lower than it did immediately after the great convulsion,—a consequence, perhaps, of the settling down of the shaken ground. In the same manner, in 1822, at Valparaiso, the permanent change of level in the rocks on the coast was observed the morning next after the great shock ; though the earth con- tinued to tremble at intervals for many days. In these instances of change of level we have, then, a clear indication of some cause of disturbance, super- added to that which produced the vibrations, and which, it is highly probable, would accompany the simple elevation of the coast in mass. From these considerations, we may, I think, fairly conclude, with regard to the earthquakes on the west coast of South America, Ist. That the primary shock is caused by a violent rending of the strata, which seems generally to occur at the bottom of the neighbouring sea. 2nd. ‘That this is followed by many minor fractures, which, though ex- tending upwards nearly to the surface, do not (excepting in the comparatively rare case of a submarine eruption) actually reach it. 3rd. That the area thus fissured extends parallel, or approximately so, to the neighbouring coast mountains. Ath. That when the earthquake is accompanied by an elevation of the land in mass, there is some additional cause of disturbance. And lastly, That an earthquake, or rather the action indicated by it, re- lieves the subterranean force, in the same manner as an eruption through an ordinary volcano. Now, what constitutes the axis, where visible, of most great mountain- chains? Is it not a wedge-formed linear mass of rock, which scarcely any geologist disputes was once fluid, and has since cooled under pressure? Must not the interjection of such matter between masses of strata have re- lieved the subterranean pressure in the same manner, as an ejection of lava and scoriz through a volcanic orifice? 'The dislocation having been effected in that portion of the upper crust of the earth, now forming a mountain, must not superficial vibrations, proceeding from a focus not deeply seated, have been propagated over the surrounding country? And, whatever direction these dislocations took, would not an area, elongated in the same line, have been affected by the vibration ? In drawing this parallel, I state my belief, that those earthquakes, with their secondary shocks, which are attended by such phenomena as accom- panied the earthquake of Concepcion in 1835, are caused by the rending of great masses of strata, and their interjection by fluid rock ;—a process which must have formed one step in a line of elevation. VOL. V.—SECOND SERIES. AL 620 C. Darwin, Esq., on Volcanic The inhabitants of Concepcion believed, that the vibrations proceeded from the south-west, in which quarter subterranean noises were likewise frequently heard. It is, therefore, a most interesting circumstance, that the island of Santa Maria, situated 35 miles distant in this direction, was found by Captain Fitz-Roy to have been elevated to nearly three times the height that the coast near Concepcion was upraised. At Tubul, S. by E. of Santa Maria, the land was raised 6 feet; at the southern extremity of the latter island, 8 feet; in its middle, 9 feet; and at its northern extremity, upwards of 10 feet*. These measurements, which were made with extreme care by Cap- tain Fitz-Roy, seem to point out an axis of elevation in the sea off the north- ern end of Santa Maria. There is one remark, which I must introduce here. The motion of the earth, on February 20th, 1835, at Valdivia, appeared to me like that of a crust, spread over an undulating fluid; and in my Journal, I have compared the motion to the bending of thin ice, beneath a moving weight. After- wards, when I became convinced that the crust there does rest upon a sea of molten rock, my first impression regarding the movement was strongly con- firmed. Michell long since observed, (Phil. Trans., 1760, p. 8) that ‘the motion of the earth in earthquakes is partly tremulous and partly propagated by waves, which succeed one another, sometimes at larger and sometimes at smaller distances ; and this latter motion is generally propagated much further than the former.’ This distinction, I believe, is strictly true. Professor Phillips+ argues that rocks, although elastic in their parts, are “ very imper- fectly so in their mass, owing to the numerous divisions which intersect them. Composed of such materials,” he says, ‘‘ the crust of the earth does not, and in fact hardly can, vibrate, in the ordinary sense of this term; the motion observed is more similar to the undulation of a flexible lamina over an agi- tated liquid.” The result arrived at by this reasoning thus coincides with mine, drawn from the impression on my senses; and it, at first, appears to explain, in a very satisfactory manner, the propagation to greater distances of the long and gentle undulations than of the vibrations, by the transmission of the former in the subterranean fluid, and of the latter in the crust of the earth. With respect, however, to the supposed want of elasticity in the crust of the earth, taken in mass, I cannot agree with Professor Phillips. Michell, (Phil. Trans., 1760, p. 35,) when he adduces the fact of the great vibration, or rather oscillation, during gales of wind, of steeples, and even towerst, which may be said to be composed of a vast number of strata of different densities, and which are frequently traversed by fissures or faults, leaves * Geographical Journal, Vol. vi. p. 327. + Lardner’s Encyclopedia, Geol., Vol. ii. p. 209. Phenomena in South America. 621 scarcely any doubt on the mind that a similar and much greater vibration might be transmitted from the depths of the earth, where the parts must be pressed together with incomparably greater force than in any building. Plausible as is the foregoing explanation of the two kinds of movements, I do not believe it to be the correct one ; for if an undulation be ever produced in the subterranean fluid expanse, we can hardly conceivea more powerful cause of it, than the upward rush of a great body of molten rock and aériform matter from the lowest abyss of a volcano: but we know that eruptions on an enormous scale have happened through old vents, even in areas subject to far-extended and undulating earthquakes, without such movements having been produced. From this consideration, and from the fact that the force of earthquakes appears to have a definite relation to the thickness of crust ruptured, as we may con- clude from the great difference in the effects caused by an eruption through an old, and one through a new orifice, I do not conceive we are justified in admitting the hypothesis of an undulating fluid. The two kinds of movements may, possibly, be explained, by considering that when the crust yields to the tension, caused by its gradual elevation, there is a jar at the moment of rup- ture, and a greater movement may be produced by the tilting up of the edges of the strata and by the passage of the fluid rock between them. In breaking a long bar of steel, would not a jar be caused by the fracture, as well as a vibration of the two ends when separate ? Mr. Hopkins*, in his Researches on Physical Geology, has demonstrated, that when an elongated area is elevated by a force acting equally beneath all parts, if the strata yield, fissures must be formed parallel to its longer axis, and other minor ones transverse to it. Knowing then with certainty, that the coast of Chile, near Concepcion, was elevated on the 20th of February, and likewise that the area affected by the earthquake was elongated ;—bearing also in mind, that several of these elevations have occurred, as attested both histo- rically and by the extensive beds of recent species of shells, at the altitude of some hundred feet, we are absolutely compelled to believe, that the area (with- out we assume that the strata possessed extraordinary powers of extension) was at that time fissured in lines, the principal of which were parallel to its longer axis. If, however, the elevatory force acted unequally in different parts, as was the case in Chile, we can understand, from the admirable generalization of the same author, that separate fissures might be formed, which would produce at the same instant, in distant places, separate shocks, perhaps of different in- tensities. Hence we need not suppose, that the shocks felt more strongly at Juan Fernandez, Concepcion, and Chiloe, than at intermediate points, pro- * Transactions of the Cambridge Philosophical Society, Vol. vi. Part I. AL2 622 C. Darwin, Esq., on Valeunec ceeded from any one focus, but that they were generated in each separate district,—the vibrations probably having, in each case, different directions *. This explanation is, I think, far more satisfactory than that offered by Hum- boldt, of the supposed inertness of an intermediary mass of rock, in transmit- ting to the surface vibrations from a deeply-seated focus. On different kinds of Earthquakes ; and conclusions regarding those which accompany Elevatory Movements. I confine the foregoing observations to the earthquakes on the coast of South America, or to similar ones, which seem generally to have been accom- panied by elevation of the land. But, as we know that subsidence has gone on in other quarters of the world, fissures must there have been formed, and there- fore earthquakes. J think, it would be highly advantageous to geology, if the au- ther who has followed out the effects of an elevatory force, would consider those produced by the failure of support in the arched surface of the globe. The earthquakes of Calabria, and perhaps of Syria, and of some other countries, have a very different character from those on the American coast. When Molina, the historian of Chile was in Italy, he was much struck with this dif- ference; he says+, in Chile even the smaller shocks extend over the whole kingdom, and are propagated horizontally, whilst those which he felt at Bo- logna, were of small extension, but instantaneous, and commonly explosive. I will add, that in the accounts collected by Mr. Lyellt of the earthquakes of Calabria, Lisbon, and some other places, portions of the surface are de- scribed as having been absolutely engulphed, and seen no more: but this does not appear to have happened in any of the earthquakes on the west coast of South America. If the fluid matter, on which | suppose the crust to rest, should gradually sink instead of rising, there would be a tendency to leave hollows, and therefore a suction exerted downwards; or hollows would be actually left, into which the unsupported masses might be precipitated with the violence of an explosion. Such earthquakes, we may conclude, from what has been shown in the foregoing part of this paper, would seldom be accom- panied by eruptions, and never, probably, by periods of renewed volcanic * At Concepcion the line of vibration appears to have been N.W. and S.E., coming from S.W. At Mocha, (an island between Concepcion and Valdivia), from the manner in which water oscil- lated in the bottom of a boat drawn up on shore, the vibration must have been N. and S. coming from either E. or W. For the facts alluded to, see Capt. FitzRoy’s account of the Voyages of the Adventure and Beagle, volume ii. p. 414. + Compendio de la Historia del Reyno de Chile, Vol. i. p. 36. t Principles of Geology, 5th edit. Vol. ii. Book ii. Chap. xiv. Phenomena in South America. 623 energy. According to M. Boussingault *, those earthquakes in South America which have been most destructive to human life, that is, which have been most sudden and violent, have not coincided with volcanic eruptions. He adduces several instances, including the shocks felt at Caraccas in 1812; but, according to Humboldt}, the connexion between the subterranean disturbances at that place and the West Indian vents can hardly be doubted. M. Boussingault’s remark, indeed, although perhaps generally true, should be taken with some reserve; for had the earthquake of Concepcion happened at night, thousands of persons must inevitably have perished. In a line of fracture, produced by subsidence, the distortion and overthrow of the strata would probably be even greater than in one of elevation, from the cir- cumstance, that as soon as the weight of the mass overcame its cohesion, and it began to sink, there would be no counterbalancing power, like gravity during elevation, to check the movement, excepting, indeed, the lateral pressure of the masses together, and this would only add to the disturbance. There would be, in this case, no axis of injected plutonic rock, or at least not one protuberant above the general surface ; and thus we may explain the extreme disturbance in the strata of countries which are only hilly, like parts of Great Britain ; and the oc- currence there of such axes of elevation, as they are generally called, but which probably, in most cases, would be more appropriately termed axes of subsidence. If the theory which I have given of the cause of the earthquakes on the west coast of South America be true, we might naturally expect on the same principle to find proofs of successive formation in the many parallel ridges, of which the Cordillera is composed. In the parts of Central Chile which I examined, this is true, even with regard to the two main lines ; of which one is partly formed of inclined beds of conglomerate, consisting of pebbles de- rived from the rocks of the other. I have also evidence, but of a less satis- factory kind, that some of the exterior lines of mountains are altogether of subsequent date to the more central ridges. Moreover, in all parts of the Cordillera, there are proofs of an equable elevation im mass to a very great altitude. I was so much struck with this latter fact, connected with what I imagined must have taken place during the Concepcion earthquake, that I came to nearly the same conclusion, which Mr. Hopkins has demonstrated by his mathematical researches, namely, that mountain-chains are only subsidiary and attendant phenomena on continental elevations. If this be so, and few, after having read Mr. Hopkins’s memoir, will dispute it ; then, as it is certain continental elevations have certainly taken place on a great scale within the * Bulletin de la Soc. Geol., Vol. vi. p. 54. + Personal Narrative, Vol. ii. p. 226, and Vol. iv. p. 6, English Translation. 624 C. Darwin, Esq., on Volcanic recent period, so, as certainly, must masses on the lines of fracture have been unequally lifted up and let down,—that is, some steps in the formation of a mountain-chain have been produced. I may here ask, when Mr. Hopkins* says, he “can in no way conceive the successive formation of parallel fissures, without hypotheses respecting the mode of action of the elevatory force, which are infinitely too arbitrary to be admitted for an instant,’ has he considered the effects of long intervals of rest, during which the injected rock might become solid? Would not the crust in such case yield more readily on either flank, as I believe it must have done in the Cordillera, than on the line of an axis composed of solidified rocks, such as granite or porphyry? An extremely slow elevation of the land, with long intervals of rest, being the only kind of movement of which we have any knowledge, the slow cooling of that portion of the liquefied rock which is propelled into the upper parts of the crust, cannot be considered an arbi- trary assumption. From the facts stated in this paper, we may safely conclude, that volcanic action, even on a very grand scale, as in the Andes, is only one effect of the power which elevates continents, at the slow rate at which the South Ame- rican coast is now rising. In looking back to the past history of the world, we learn from Mr. Lyell+, that there have been volcanic eruptions during every epoch, from that of the Cambrian formations to the present day. The ancient eruptions seem to have been accompanied by all the circumstances which attend modern ones ; nor is there any evidence, as remarked by the same au- thor, that the quantity of matter ejected, in the greater number of ancient cases, was excessive. Therefore, we must conclude that continental elevations, one of the effects of the same motive power which keeps the volcano in action, has ordinarily gone on, since those ancient days, at the same slow rate as at pre- sent, and, consequently, as above inferred, the step-like formation of moun- tain-chains. It may, therefore, be questioned, whether we are justified in admitting the hypothesis of a paroxysmal elevation of any mountain-chain, without distinct proofs in each particular case, that a series of impulses, like those, which now acting frequently on the same lines, rend the earth’s crust, * Abstract of a Memoir on Physical Geology, by W. Hopkins, Esq., M.A., p. 31. + Elements of Geology. In the 24th chapter, Mr. Lyell has collected instances of volcanic eruptions in each of the great epochs of the geological history of Europe. The argument, which follows in the text, is the same with that advanced by this author in the Principles of Geology, (Book I. Chap. v.) but Mr. Lyell more particularly applies it to the earthquakes and convul- sions, ‘‘ caused by subterranean movements, which seem to be merely another portion of the vol- canic phenomena.” Phenomena in South America. 625 and elevate unequally portions of it, could not have effected the observed effects. It is, however, a subordinate question, whether there exist proofs of paroxysmal violence in some mountain-chains ; the important fact which appears to me proved, is, that there is a power now in action, and which has been in action with the same average intensity (volcanic eruptions being the index) since the remotest periods, not only sufficient to produce, but which almost inevitably must have produced, unequal elevation on the lines of frac- ture. Theoretical Considerations on the slow Elevation of Mountain-Chains. The conclusion that mountain-chains are formed by a long succession of small movements, may, as it appears to me, be rendered also probable by simple theoretical reasoning. Mr. Hopkins has demonstrated, that the first effect of equably elevating a longitudinal portion of the crust of the earth, is to form fissures, parallel to the longer axis (with others transverse to them, which may here be neglected) of the kinds represented in the accompanying diagram (No. 1.), copied from that published in the Cambridge Philosophical N No. 1 an A mobo usar A M Transactions. But he further shows, that the square masses, now disjointed, will,—from the extreme improbability of the force uplifting them, when sepa- rate, equably, or from their settling down afterwards,—assume some such posi- tion as that given in Diagram No. 2. In the Cordillera, which may be taken N’ a N’ M’ as a good example of the structure of a great mountain-chain, the strata in the central parts are inclined more commonly at an angle above 45°, than beneath it ; and very often they are absolutely vertical. The axis of the lines of dislocation is formed of syenitic and porphyritic masses, which, from the 626 C. Darwin, Esq., on Volcanic number of dikes branching from them, must have been fluid when propelled against the lower strata*. If then we suppose Diagram 2 to represent the section of the Cordillera before its final elevation, I may ask, how is it pos- sible, that some of the masses of strata should be placed vertical, and others absolutely overturned, by the action of the flud rock, without the very bowels of the earth gushing out? Should we not have one enormous deluge of volcanic matter, instead of wedge-formed, injected masses of solid crystalline rock? On the other hand, if we suppose the loftiest chain of mountains to be formed by a succession of shocks similar to those of Concepcion,—a few stronger and many slighter ones, separated from each other by long intervals of time,—then we may believe, that the formation of a fissure through the whole thickness of the crust would be the effect of many efforts on the same line, and that during the intervals, the rock first injected would become cooled. When, therefore, the tension (which, according to Mr. Hopkins, acts on the lower surface firstt) caused the upper part to crack, the fissures, if on the same line, would meet the consolidated extremity of a dike, instead of the fluid mass below. In those cases, however, where the fissure happened to traverse at once the entire crust, a volcano would be formed, such as that near Juan Fernandez during the Concepcion earthquake. On the same principle, after the masses of strata had been very gradually lifted into the position represented in Diagram 2, the rock beneath the anticlinal axes, from having been propelled beyond its former subterranean isothermal line, would be cooled, and, if sufficient time were allowed, it would be consolidated. In this manner the strata, each new fracture being firmly cemented by the cooling of the injected rock, might be overturned into any possible position, and yet, from a gradually thickening crust being formed over the fluid mass, on which the whole is believed to rest, the earth would be protected from a deluge of lava. If this reasoning be sound, we may deduce this remarkable conclusion, that in a mountain-chain, having an axis of plutonic rock, which was propelled upwards in a fluid state, where the strata betray the effects of * According to M. Boussingault (Bulletin de la Soc. Geol., Tom. vi. p. 55), this is not the case in the Cordillera of the Equatorial regions. He states that trachyte there forms the base of the mountains, and that it has been protruded in a consolidated form. But can the deep-seated axis of a gigantic mountain-chain be composed of trachyte,—a rock essentially volcanic? If we could penetrate to greater depths, it cannot be doubted we should find the trachyte graduating into some plutonic rock ; and one may be allowed to suspect that its junction with the superincumbent strata would present very different appearances from that of the trachyte;—the trachyte, indeed, we may well imagine to be the crust of such plutonic rocks cooled under little pressure, and forced upwards on the surface of the molten mass, in a solid form. + Cambridge Philosophical Transactions, Vol. vi. pp. 43-45. Phenomena in South America. 627 the most violent action, although it be on a gigantic scale, there we have the best evidence of an almost infinite series of small movements*. I will enter on only one other consideration connected with this subject. From having in my mind the proportional thickness of the strata, usually given in sections in geological works, I felt much surprise, when I crossed the Cordillera, and found highly-tilted anticlinal lines succeeding one another at short distances, that the rock composing the axis was not to be met with, ex- cept in patches in the valleys. If we suppose parts of the strata in Diagram 2 to be placed vertically, the rock of the axis would necessarily be exposed in wide spaces ; but here, I believe, is the source of error,—geologists have not always sufficiently considered the thickness of the mass upturned, in re- lation to the distance of the parallel anticlinal lines one from another. In the Cordillera, in a width of about sixty miles, there are eight or more anticlinal lines; and thus the centres of the troughs and of the ridges are about four miles apart. Now, if we suppose the upturned crust to be only four miles thick, (which is somewhat more than can actually be seen,) the strata, when placed vertically, will occupy as great an horizontal extension as they did before they were disturbed. In Diagram 3, which I beg it may be understood is given merely to illustrate this one point, I have taken portions of ‘strata of the same exact length as those in Diagram 2; but | have increased their thickness, so that it equals the distance of the anticlinal lines from each other ; —we shall now see that not only the whole axis is covered, but that the masses cannot be forced into their former horizontal limits. I have not, however, allowed for the immense abrasion which, under such circumstances, the lower * Humboldt has insisted on the fact, that in double chains of mountains, such as form large portions of the Andes, the lofty parts of one line correspond with the lower parts of the other. Such symmetry of structure is hardly conceivable on the idea of mountains having been formed by paroxysmal violence; but if we consider the whole range as the effect of a widely-extended elevation,prolonged during many ages, it is easy to understand, that if one line be weak, and con- sequently be subjected, for a long time, to disturbance from the subterranean force, it is probable that during so much the less time will the parallel and approximate one be affected. VOL. V.—SECOND SERIES. AM Caaenrrr ee 628 C. Darwin, Esq., on Volcanic angles would suffer, nor for the denudation and rounding of the upper ones, This supposed crushing together of such gigantic fragments will, perhaps, explain the utter confusion, which must be familiar to every geologist who has examined any great mountain-chain*. I must here add, that according to these views, which I believe are correct, the theoretical part of the fore- going argument, namely the difficulty of confining during any paroxysmal movement the fluid matter within the crust, is weakened ; yet I believe the principle holds good, for, in order to break up and throw over portions of very thick crust, as in Diagram 3, there must have been great horizontal extension, and this, if sudden, would have caused as many continuous outbursts of vol- canic matter, as there now are axes of solid rock. Moreover, when we con- sider, first, that the fragments must have stood for one instant separate from each other, and, secondly, that the force necessary to turn over and crush to- gether at one effort these immense masses, must have been in proportion enormously great to that required merely to lift them,—it cannot, I think, be doubted for a moment, that if the force had acted suddenly, these portions of the earth’s crust would have been absolutely blown off, like fragments of rock by gunpowder ; but this has not happened, and, therefore, the force did not act suddenlyf. If we grant that the earthquake of Concepcion on the 20th of February marked one step in the elevation of a mountain-chain ; then, as during the twelve succeeding days there were counted upwards of three hundred shocks, which proceeded from the same quarter with the great shock, so the fluid stone * In the Cordillera, the axis of plutonic rock is less exposed in the principal, than in the subor- dinate lines ; some strongly marked exceptions, however, occur. In the former, also, the strata are mostinclined. As, according to the views here advocated, the formation of a mountain-chain is due to innumerable impulses, the highest part must generally have felt the greatest num- ber of impulses, and therefore its stratification would generally be most disturbed. And if a great part of the disturbance be due to the lateral force resulting from the compression of the great thick portions of the earth’s crust, then the central lines, or those which have several ridges on both sides of them, would be most crushed together, and consequently the strata would be most closely packed over them. I can understand on no other principle, the circumstance of the rock of the axis being visible not on the loftiest, but on the secondary lines of a mountain-range, which very frequently occurs. + Mr. Hopkins moreover argues, (Abstract of a Memoir on Physical Geology, p. 15,) that if the elevatory force had the character of an impulsive action, it “ would produce the most irregular phenomena, and such as would be altogether without the sphere of calculation. I exclude, there- fore, the hypothesis of this kind of action, not as involving in itself any manifest improbability, but as inconsistent with the existence of distinct approximations to general laws in the resulting phenomena.” In other parts the author shows that such approximations do exist in nature.—See also Phil. Mag. 1836, Vol. viii. p. 234. Phenomena in South America. 629 must have been pumped into the axis by as many separate strokes ; nor did the process cease for many subsequent months*. In the central ridges of the Cor- dillera, there are masses of compact unstratified rocks, half again as lofty as Etna, and I believe, from the reasoning above given, that they were formed by steps nearly as slow as those indicated by the innumerable layers of volcanic matter accumulated on the flanks of the Sicilian mountain. In the volcano, that is, a mountain which has been ruptured in its incipient state, the fluid stone being brought to the surface is rapidly cooled, and hence successive layers are formed; but in the axis of plutonic formation (or subterranean volcano, if it may be so called), the injected matter, not being rapidly cooled, is blended into one huge conical pile. This whole view is nothing more than an application of Hutton’s doctrine of the repetition of small causes to produce great effects ; and which Mr. Lyell has already brought distinctly to bear on this particular subject. The action of the elevatory force, as known by beds of littoral shells, suc- cessive lines of aqueous erosion on cliffs of solid rock, and terraces rising one above another, seems everywhere to have been prolonged, although inter- mittently : in the volcano, the structure of the mountain, as well as all history, bespeaks the same fact with respect to the eruptive force. During the Con- cepcion earthquake, we have seen that these powers, so analogous in their ac- tion, were absolutely parts of one common phenomenon. Bearing in mind Mr. Hopkins’s demonstration, if there be considerable elevation, there must be fissures, and, if fissures, almost certainly unequal upheaval, or subsequent sinking down,—the argument may be finally thus put :—mountain-chains are the effects of continental elevations ; continental elevations and the eruptive force of volcanos are due to one great motive power, now in progressive action ; therefore the formation of mountain-chains is likewise in progress, and at a rate which may be judged of by either phenomenon, but most nearly by the growth of volcanos. Concluding Remarks. With these views, if we look at a map of America, and observe the con- tinuity of the great chain of the Andes, and its lesser parallel ones, in which from lat. 55° 40’ South to 60° North, a space of little less than 7000 miles, the volcanic forces either now are, or recently have been, in action,—and likewise the symmetry of the whole,—we shall be deeply impressed with * In an extract from a letter, dated Concepcion, May 6th, that is seventy-six days after the great earthquake, there is this passage :—‘ It is only since a few days, that a day has passed without a shock, and even yesterday we had one.” Am 2 630 C. Darwin, Esq., on Volcanic the grandeur of the one motive. power, which, causing the elevation of the continent, has produced, as secondary effects, mountain-chains and vol- _eanos. The same reasons which led me to the conviction, that the train of connected volcanos in Chile and the recently uplifted coast, together more than 800 geographical miles in length, rested on a sheet of fluid matter, are ap- plicable with nearly equal force to the areas beneath the other trains. We see that these areas are connected by one uniform chain of mountains, from many distant points of which fluid rock is yearly ejected; and as there are proofs that nearly the whole west coast of South America has been elevated within a period geologically modern, and that this movement, in some parts at least, has extended across the continent,—keeping, also, in mind the probability, that during periods of increased subterranean action, such as those indicated in the foregoing tables, the whole western part of the continent has been al- most simultaneously affected, it appears to me, that there is little hazard in assuming, that this large portion of the earth’s crust floats in a like manner on a sea of molten rock. Moreover,—when we thiak of the increasing tem- perature of the strata, as we penetrate downwards in all parts of the world, and of the certainty that every portion of the surface rests on rocks which have once been liquefied ;—when we consider the multitude of points from which fluid rock is annually emitted, and the still greater number of points from which it has been emitted during the few last geological periods inclusive, which, as far as regards the cooling of the rock in the lowest abysses, may probably be considered as one, from the extreme slowness with which heat can escape from such depths ;—when we reflect how many and wide areas in all parts of the world are certainly known, some to have been rising and others sink- ing during the recent wra, even to the present day, and do not forget the in- timate connexion which has been shown to exist between these movements and the propulsion of liquified rock to the surface in the volcano ;—we are urged to include the entire globe in the foregoing hypothesis. To the belief in these large seas of molten rock, not to speak of an entire concentric layer so constituted, it has been objected, that if its fluidity be to- lerably perfect, (which there is good reason to think is the case from what we see of the junction of the plutonic with the metamorphic formations,) the lava ought to stand (supposing a comparative examination possible) at nearly equal heights, within neighbouring volcanic orifices. To this I may answer, if it be permitted me to assume that the subsiding as well as the rising areas rest on a fluid surface, that whatever the power is which causes one to rise and another to sink, acts with unequal force (greatly modified, also, by unequal resistance) in different parts of even a very limited area. The main strength of the earth- Phenomena in South America. 631 quake of February 20th, 1835, passed over Valdivia, but affected the districts north and south of it; and it appears that this town, until November 1837, had been less injured by the innumerable shocks which devastated Chile than any other; yet the subterranean abysses directly beneath it are in connexion (as shown by the action of Villarica in 1822) with the district to the North, which has been so often convulsed ; and in November 1837, at the same time that an island far southward was upraised eight feet, it was shaken by an earthquake so violent that it escaped utter ruin only from the houses being built of wood. The comparative freedom from disturbance of Valdivia on the 20th of February, cannot be attributed to the action of Villarica, for we have seen that this volcano was quiet ; nor indeed is there any reason why such an effect should be attributed to its action, since the eruptions of Osorno and Minchinmadom did not save the northern parts of Chiloe, though they occupy the same relative situation with regard to them, which Valdivia does to Villarica. Shall we then say, that Valdivia escaped so long the subterranean disturbances, some of which affected simultaneously regions north and south of it, solely on account of the greater strength of the crust in that part? This appears to me a cause quite inadequate ; and the direct supposition is better, that as within the same period one part of the continent has been elevated more than — another, so the lava has been propelled by the action of this force more pow- erfully towards some, than towards others, of the volcanic orifices which penetrate it. The secular shrinking of the earth’s crust has been considered by many geologists a sufficient cause to account for the primary motive power of these subterranean disturbances ; but how it can explain the slow elevation, not only of linear spaces, but of great continents, I cannot understand. With the same view, some highly important speculations have recently been advanced,—such as changes of pressure on the internal fluid mass, from the deposition of fresh sedimentary beds, and even the attraction of the planetary bodies on a sphere not solid throughout ; but we can see that there must be many agents, modi- fying all such primary powers; and the furthest generalization, which the consideration of the volcanic phenomena described in this paper appears to lead to, is, that the configuration of the fluid surface of the earth’s nucleus is subject to some change,—its cause completely unknown,—its action slow, in- termittent, but irresistible. to 2S Pete eye ee ee a ee TS, re ee 4, piles.» Petia: Uae Tabak, cy a ‘ ee ¢ NA sh ar a I Fa i Virw x hors," AK ar ras eG he ee eS, ke ‘ie et ae me eth ee we er er a gait hal AP pale eco eee RRO PS a, te MA Anny a er ‘i ete oe Pasa tae ey RTS Sy A de a via ld a ee Wn dtas) a Beye ia h0% HA Nba, ter gare emg ote ae! aie Bae at ro Beto tg tselemaly |p ah | - be TO an aL ‘ 5 PE aS Big coco oe wi " Pacinianadie 7 oan ae oe gh inviolate iowa Nie. i ial “wee Bashir: > | BY eit nits Jo Hod: Hea: (halal as = Aa ar pine? te Haut Ve anny ag ra Si tiny hail . F, sinh SS i ae Bt a es) > Cee Spd okies | 7 [ 633 ] XLIII.—On the Physical Structure of Devonshire, and on the Subdivi- sions and Geological Relations of its older stratified Deposits, &c. By Rev. ADAM SEDGWICK, M.A., F.G.S., F.R.S., &c. Woodwardian Professor of Geology in the University of Cambridge ; And RODERICK IMPEY MURCHISON, Esq., F.R.S., V.P.G.S. [Read June 14th, 1837. ] Prates L. to LVIII. CONTENTS. Part I. INTRODUCTION, p. 633. Cuapr. I.—Description of the five geographical regions of Devonshire, p.634. Cuar. I1.—Successive deposits between the north coast of Devonshire and the culmi- ferous series, p. 638. Cuapr. II].—Succession of deposits between Dartmoor and the south coast of Devon, p- 649. 1. Section from the east side of Dartmoor to Torbay, p. 650. - Section from Dartmoor to the Plymouth ch) limestone, p. 653. 3. Section from the Plymouth limestone to Bolt Head, p. 656. 4, Section from Berry Head to Start Point, p- 659. Conclusions, p. 662. Slate-rocks of Cornwall, p. 664. Cuapr. IV.—Culmiferous series. Its relations to the other formations,—structure,— fossils, &c., p. 669. Lower culm-measures, p. 670. Upper culm-measures, p. 677. Plants, p. 681. Cuar. V.—On the granite of Dartmoor, p. 685. Part II. On the classification of the older stratified rocks of Devonshire and Cornwall, (Read April 24, 1839.) p. 688. PART I. INTRODUCTION. IN a communication made to the British Association during its meeting at Bristol (1836), we first pointed out (by help of a section extending from the north coast of Devon to Dartmoor) the true geological position of the great culmiferous deposits, which occupy so large a portion of that county. In this paper our object is more extensive ; for we not only attempt to describe the ie. 12sec SS ee SS ee ee 634 Professor Sepewick and R. I. Murcuison, Esq., on the order of the successive formations north of Dartmoor, but also, as far as we are able, to bring them into comparison with the formations which are ex- panded from the south side of the Dartmoor granite to Start Point, and to the other headlands of the south coast of Devon. We believe that our pre- sent attempt is almost entirely new ; for though some portions of the county have been described in considerable detail, yet the several parts have not been brought into any distinct comparison with one another; and in all the pub- lished geological maps, the greater part of the slate-rocks have been repre- sented under one colour, without an attempt either to separate them into distinct formations or to mark their succession*. Still less has any attempt been made to bring them into a strict geological comparison with the other mountain groups of England and Wales. Our present object is to exhibit a synopsis of the evidence by which the successive formations are determined. But in future and longer communications, we hope to lay more ample details before the Society, and to describe a large number of organic remains, by help of which, the successive deposits may be referred still more precisely to their true place in the series of British formations, inferior to the carboniferous groups. We are aware of the great difficulty of our task, and if we can suc- ceed in taking only the first step towards its accomplishment, our labours will be well rewarded f. Cuar. I.—Five Geographical Regions of Devonshire. (See Map, Pl. L.) Considered geologically, and under the most general point of view, Devon- shire may be divided into at least five distinct geographical regions. * Mr. Greenough represents the slate-rocks under two colours. But the separation is founded on mineral characters and not on age; for even a portion of the culm series, altered near the gra- nite, is represented of the same colour with the oldest slate-rocks of Cornwall. Rev. J. J. Conybeare made also a separation of the Cornish and Devonian slates into two groups, partly on the same principle, and certainly with no reference to any ascertained order of superposition. His papers, which he did not live to finish, contain some excellent details. Mr. H. T. De la Beche, in the first edition of the Ordnance Map of Devon, (which had been published sometime before our examination of the county,) included (with the exception of the district of Start Point) the whole slate series and the culm-measures under one colour, not attempting any separation of them. + The details alluded to in the Introduction are now given in Part II. of this paper. The whole text of Part I. is printed (withthe exception of verbal corrections and an expansion of one or two mere mineral descriptions,) from the communication made by the authors in June 1837. A few sentences at the end of it, in which the oldest rocks of North and South Devon were placed provisionally in the Upper Cambrian and Lower Silurian system, are now omitted, as the authors, after a more mature examination of the fossils, are convinced that, so far, their first conclusions were erroneous. This omission will be alluded to again in the Introduction to Part II. (June 13839.) Physical Structure and older stratified Deposits of Devonshire. 635 ist. One of them extends through the most eastern portions of the county ; and is almost exclusively made up of deposits belonging to the formations of new red sandstone and green sand*. ‘To describe any portion of this region forms no part of our present object. But we may just observe, that the new red sandstone is expanded through a part of it, in a series of rich valleys and low well-wooded plains, which are prolonged northward to the coast of Somer- setshire ; while the green sand forms, almost without exception, the summits of high barren tabular hills. These two characters, and the horizontal position of the strata, at once distinguish this first region from all the others. 2nd. The second region occupies all the most northern parts of the county ; being bounded to the east by the Vale of Taunton, and the plains of new red sandstone above-mentioned, extending thence to the coast of Somerset- shire; to the north and west by the sea-coast ; and to the south, by a line commencing at remington Pill on the south side of the Barnstaple river, thence ranging through a low undulating region in a direction about east and by south, (passing about two miles north of South Molton, Bampton, and Holcombe Rogus,) so as finally to terminate in the above-mentioned plain of the new red sandstone. Along a considerable part of the north coast runs an irregular chain of ragged hills, intersected by some valleys of exquisite beauty, and forming a noble series of perpendicular cliffs and bluff headlands. One or two of the highest points of this coast chain, between Minehead and Combe Martin, reach an elevation of about twelve hundred feet. In the interior of this region is a succession of still loftier elevations, (Dun- kery Beacon attaining the height of more than 1600 feet,) which in some places put on the character of a mountain chain. But what we chiefly wish to observe is, that these interior ridges form a regular crest or water-shed, which (with a few inconsiderable deviations) ranges as far as the meridian of Ilfracombe, in a direction almost exactly parallel to the southern boundary above indicated. From many parts of this water-shed, the country descends towards the south by a succession of long sweeping inclined planes; giving to the country an external character which is remarkably contrasted with the features of the great undulating region that lies expanded further towards the south. 38rd. The third region commences immediately on the southern limit of the * The tertiary basin of Bovey Tracey, chiefly occupying a depression among the older strata, may perhaps seem an exception to these remarks. It is, however, too inconsiderable in extent to be noticed in a general sketch like the present. VOL. V.—SECOND SERIES. AN 636 Professor Sepewick and R. I. Murcuison, Esq., on the second, and occupies a great superficial area ; extending in Jength, from the plains of the new red sandstone, in the drainage of the Hx, to the western cliffs of the county ; and in breadth, from the southern limits of the second region (as above described) to the northern flanks of Dartmoor and the hilly country S.W. of Launceston. The northern limit of this great area is there- fore sufficiently well-defined for our present purpose. Its southern limits are not so easily described ; the strike of the beds having (through a considerable extent) been interrupted and distorted by the protrusion of the Dartmoor gra- nite; we may, however, state in a few words,—that the western extremity of the boundary-line runs into the sea immediately to the south of Boss Castle harbour, in the county of Cornwall, and ranging thence in a direction bearing a little to the south of east, it passes about a mile and a half to the south of Launceston, crosses the Tamer still further to the south, and just skirting the great mining-field north of Tavistock, abuts against the granite of Dart- moor. From this junction, the boundary-line is defined by the northern and north-eastern edge of the granite as far as the Bovey basin. The remainder of the line, from the Bovey basin, round the north end of Haldon, to the drain- age of the Ex, is too complicated to admit of a clear description without the help of a good map. But the deposits of the third region are not confined to the limits here indicated, as they form an outlying mass resting on the lime- stone to the south of Newton Bushel*. The whole of the great area inclosed between these boundaries is occupied by rocks of one formation, the greatest part of which are thrown into violent undulations, exhibiting an incredible number of anticlinal and synclinal lines, generally running, with the strike of the beds, nearly east and west. These con- tortions are not merely seen in the cliffs and quarries, but they have produced an impress on the whole surface of the region ; which, without containing any hills of great elevation, is thrown into an almost continuous succession of undulations, resembling the waves of a tumultuous sea. These characters, however, disappear near the northern and southern boundaries of the region, where the beds generally acquire a more steady dip, and, as we shall hereafter show, form the bottom of a great trough, so as to repose on all the other stra- * The whole south boundary of the culm-measures was re-examined, by one of the authors, in 1836, after the Bristol meeting above mentioned. To the N.E. of the Newton limestone (and beyond the limits of this outlier) he found the older fossiliferous slates stretching towards Dart- moor. Hence he concluded, that the culm-measures did not extend, on the flanks of the Dartmoor granite, to the south of the Bovey basin. Since that time, however, Mr. Austen has traced, and laid down on a map communicated to the Geological Society, a considerable band of the culm series, skirting the granite from the north-west end of the Bovey basin to the hills west of Ash- burton and Buckfastleigh. Physical Structure and older stratified Depesits of Devonshire. 637 tified, as well as unstratified rocks, with which they come in contact. The great series of rocks, therefore, which occupy this third region, are the newest depo- sits of our north and south section : and without prejudging their place in the British system, we may describe them conveniently as the culmiferous series, inasmuch as all the culm works of the county have been opened in them. The extent and true geological position of this great deposit had been ge- nerally misunderstood ; for though certain beds of culm had been long known and extensively worked in North Devon, yet they had always been described as mere bands subordinate to the old greywacké system ; and had never been regarded either as occupying a great overlying trough, or as composing a distinct formation. Hence, also, the black limestones which appear on both sides of the great trough and form a part of the base of the culm-series, had been confounded with the other calcareous bands of the inferior groups. Ath. The fourth region into which we divide the county of Devon is occu- pied by the granitic rocks extending through the whole of Dartmoor. 5th. The fifth and last region includes all the remaining portion of the county ; bounded towards the north, partly by the granite of Dartmoor, and partly by the southern skirt of the culm measures ; and towards the south, by the long line of cliffs extending from Babacombe Bay to the west side of Plymouth Sound. We think that the five regions, above enumerated, form natural subdivisions, —not laid down artificially, to facilitate description, but well characterized, both by their geographical features and their physical structure. Passing over the first region, we shall proceed to describe the second or hilly region of the north coast ; showing, by help of natural sections, into what groups it may be conveniently subdivided. We purpose afterwards, in like manner, briefly to describe the fifth or southern region, to establish its sub- divisions, and to bring them, as far as we are able, into comparison with the subdivisions of the second region. We shall then be prepared to describe the culmiferous rocks of the third region, and to show the relation they bear to all the rocks against which they abut, or on which they rest. In this way, after briefly noticing the general position of the Dartmoor granite, among the surrounding strata, and the characteristic phenomena at its junction with them, we hope to determine the whole sequence of the formations between the north and south coast of the county. Our task does not, however, terminate here ; for by help of all the analogies with which we are acquainted, and more especially by help of the structure and organic remains of the several formations, we shall, in future communica- tions, endeavour to bring them into comparison with the older groups of other AN2 638 Professor Sepewicx and R. I. Murcutson, Esq., on the regions. Before this can be effected, much no doubt remains to be done. We possess large materials, bearing on these questions, which have as yet been very imperfectly examined. All we can do at present is, to make a first approxima- tion to the solution of these difficult questions. ‘That they press upon us for an answer cannot be doubted, when we consider that no one has yet attempted any rigid comparison between the older rocks of Cumberland, Wales, and Devonshire ; that the antiquity of the slate rocks of Devonshire and Cornwall has generally been estimated by their mineral characters or by their vicinity to the granite—means which are not merely inconclusive, but often lead to conclusions which are absolutely false; and lastly, that the culmiferous series (occupying more than one-third of the whole superficial extent of Devon- shire) has, under the name of greywacké, been confounded with formations, to some of which, at least, it bears no analogy, either in position, mineral structure, or organic remains. Cuap. I].—Successive Deposits between the North Coast of Devon and the Culmiferous Series. Before we attempt any description or classification of these several deposits, we think it expedient to give a general account of their extent, and the places they occupy in the actual sections of the country. It will be seen, that our bound- ary lines (Map, PI. L.) inclose a small portion of the north-west corner of So- mersetshire, which is too intimately connected with our second region to be entirely overlooked. Our examination commenced with the northern part of the Quantock Hills, which, although beyond the limits of the country indicated in the preceding portion of the paper, must also be briefly noticed. ‘The north- eastern flanks of these hills are composed of a soft, unctuous slate, not un- usually ofa red colour, here and there highly calcareous, and sometimes passing into thick, irregular masses of limestone partaking of the prevailing colours of the neighbouring rock*. From beneath these, rises a system of beds which oc- cupies the central and higher portions of the hills, and (as far as we could make out, from our hasty examination of a country so much covered with vegeta- tion) is composed of hard, and sometimes coarse sandstone, alternating with more fissile, micaceous masses of finer structure, and with masses of soft, rotten slate, resembling the prevailing rocks of the upper group above de- * In the language of the workmen, the thick beds of red limestone are called trug ; and the thinner beds, after passing into a soft, glossy, unctuous slate, are called pavey. The soft, earthy slates generally pass, in Devonshire, under the name of shillat. Physical Structure and older stratified Deposits of Devonshire. 639 scribed on the north-eastern flanks of the principal ridge. In the northern portions of these hills (where they are highest and best-defined) the strike conforms to their principal direction ; but further south, where they are lower and more expanded, the subordinate beds undulate, and seem to lose all regular bearing. After crossing the plain of new red sandstone, which forms the western side of the Quantocks, we found a repetition of nearly the same rocks, viz. a series of reddish, soft slates, in some places highly calcareous, and con- taining beds of limestone, resting on an inferior system of harder texture, enclosing many beds of flagstone, shillat, and reddish sandstone, here and there almost passing into a conglomerate form. The upper series is well exhibited on the eastern skirts of Croydon Hill. The lower, with all its mo- difications, is finely exposed in Croydon Hill, Grabbist Hill, and North Hill, and is of very great thickness. In several parts of North Hill and Grabhis Hill, the strata are violently contorted, and the lines of disturbance are in va- rious directions ; yet on the whole, the strike of the beds seems to be nearly W.N.W. Part of Croydon Hill is thrown up in the form ofa great elliptical dome, and the calcareous bands form a portion of an elliptical curve sweeping round the eastern extremity of its longer axis; and it perhaps deserves re- mark, that the axis is nearly parallel to the principal direction of the strata in North Hill and Grabbist Hill. In this part of Somersetshire, the strata are contorted, the hills discontinu- ous, and the sections broken ; yet the main fact, we have just stated, viz. the existence of a lower formation of coarse, arenaceous rock, often of a red colour and of an upper formation of calcareous slate, is established on sufficiently clear evidence, and leads us at once to consider the structure of North Devon. The strata of North Hill are cut off from the coast by the valley of Porlock, which probably owes its origin to one of the great breaks or contortions, that mark the neighbouring region. ‘The same system of beds, however, reap- pears on the west side of the bay, and is continued to a headland a little north- east of Lynmouth, forming a noble succession of red cliffs, and a well-defined ridge running parallel to the coast. Along the whole of this line, the beds strike about W.N.W., and dip into the sea, at a great angle, about N.N E. If we make a traverse to the south from any part of the coast above men- tioned, west of Porlock, we find at the distance of a few miles, though the strike continues about W.N.W., that the prevailing dip is reversed to the south. From this we discover, that an anticlinal line runs nearly parallel to the strike of the beds, and to the mean direction of the coast between Porlock and Countesbury Foreland. We further discover, that the meaa direction of 640 Professor Sepewicx and R. I. Murcuison, Esq., on the the beautiful gorge down which the waters of Exmoor Forest descend to Linton, very nearly represents the direction of the anticlinal. A great feature like this may almost always be traced to some geological cause ; and we find that the strata bordering on the gorge are nearly horizontal, while those to the north and south of it continue for many miles to have a prevailing dip re- spectively to the N.N.E.andS.S.W. ‘The pommel of the saddle is not repre- sented bya mere line, but by a broad space, within which the strata are nearly horizontal, and on opposite sides of which their dip is not only reversed, but greatly increased in quantity*. We may however state, with sufficient cor- rectness, that the anticlinal line passes into the sea down the Valley of Rocks immediately west of Linton: for to the south of it, the beds acquire a steady southern dip; and to the north of it, though their dip for some way is very slight, a little beyond Linton they have, after some remarkable contortions, a high northern pitch. It is in consequence of this anticlinal position, that the coarse red arenaceous greywacké of North Hill, and of the cliffs between Porlock and Countesbury, is repeated over again, and occupies the whole suc- cession of great red cliffs, extending from the west end of the Valley of Rocks to Combe Martin+. Were we to draw two lines respectively from the Valley of Rocks and Combe Martin, in the direction of the strike, we should nearly define the range of the arenaceous system on the south side of the Lyne, as far as Exmoor Forest; and thence the same system is traced (though not without some interruptions) through the highest peaks of Somersetshire into Croydon Hill. After the preceding statements, it must be obvious, that we class the gorge of the Lyne among valleys of elevation. 'The causes, whatsoever they were, which produced the anticlinal lines and regular strike of North Devon, acted also, in the region just described, on the hard, brittle beds of red, arenaceous greywacké ; and thereby produced an enormous rupture along the line of con- trary flexure, to which the present gorges of the Lyne owed their first origin f. This region illustrates also another point in geology:—when chains are well-defined, the anticlinal lines are generally steady in their direction, and nearly coincident with the strike of the beds; but the end of a chain of hills, * See the north end of Section 1 (PI. LI.), from the Foreland near Linton to Dartmoor. + Ibid. { Valleys of elevation (or, in other words, anticlinal lines traced through a country, not by ridges but by depressions originating in a fracture of the strata) are by no means uncommon among our older formations. They abound in the highest parts of North Wales; and in Me- rionethshire, an anticlinal line, about thirty miles long, is traced through its whole course by a suc- cession of valleys. The actual pommel of the saddle (in the form of an anticlinal ridge) is only seen in one single spot. Physical Structure and older stratified Deposits of Devonshire. 641 or the outskirts of a physical region (such, for example, as the termination of the old rocks of Somerset and Devon, in the plain of the new red sandstone) is often marked by the greatest possible confusion, both in the direction and dip of the strata. The reason of this is obvious ; for in such situations, the strata are exhibited in the very regions, in which antagonist forces were just on the point of overcoming those very forces from which the chains themselves, and all their accidents, were originally derived. This remark is, we think, well illustrated by the irregular undulations of North Hill, the interruption of Porlock Bay, the dome-like elevation of Croydon Hill, and, perhaps we may add, by the outlying ridge of the Quantocks. It appears from what we have stated, that the lowest beds in this part of North Devon must be sought in the anticlinal region, and in the deep gorge of the Lyne. Accordingly, we there find a gradual passage into a lower sy- stem of soft, chloritic, fossiliferous slates, alternating with many harder, arena- ceous bands. The upper part of the group is seen in the horizontal beds of the Valley of Rocks; the lower portion only in ascending the deep cleft of the Lyne. It is interesting, as forming the base of the old rocks of North Devon, and as being the lowest fossiliferous and calcareous slaty group; but its whole thickness is nowhere exposed to view, and we are left to other evi- dence as to its place in a descending series of formations. We have before stated, that the red arenaceous system, with a steady dip (about S. by W., or S.S.W.), extends from the Valley of Rocks to Combe Martin. Just as we turn the headland leading into the Combe, a new group presents itself, constituting a succession of cliffs of different colour and form, the highest beds of which run into the sea about a mile west of Ilfracombe Harbour. This group, near the coast, contains eight or nine distinct calcareous bands, some of which are extensively worked for use ; and many parts of it are highly fossiliferous. Its average breadth is about a mile and a half, measured horizontally and in a direction transverse to the strike ; and it may be traced without difficulty into the interior (especially by help of the calcareous bands), first in a direction about S.S.E., then along the south flank of Exmoor Forest, in a direction nearly east and west. We afterwards meet with it along the water-shed crossing the turnpike-road from Minehead to Dulverton ; and from that point (as before stated) it forms a great elliptical curve, sweeping round the eastern and north-eastern flanks of Croydon Hill. In this way we have a complete proof that the calcareous slates of Somersetshire, bordering on the Croydon hills, are the equivalents of those at Ilfracombe; and that the coarse red greywacké of Croydon Hill is also the equivalent of the red beds of the same structure on the coast between Combe Martin and the Valley of the 642 Professor Sepewickx and R. I. Murcuison, Esq., on the Rocks. This is precisely the same conclusion which we attain, in a different way, by first identifying the formations of Croydon Hill with those of North Hill, and so linking them with the coarse red rocks of the Devon coast, on the north side of the great anticlinal line of the Lyne*. The identification of the Ilfracombe system with the calcareous bands on the north-east flanks of the Quantocks, is not so complete; but it is, we think, highly probable, both from the lie of the country and the structure of the component beds. We have been the more particular in the preceding account, because it seems necessary to a clear understanding of the stratification of the region, and of the evidence presented by our transverse section. The calcareous slate system of Ilfracombe, though interrupted by some vio- lent contortions, dips, on the whole, to a point a few degrees west of south ; and is succeeded, in the ascending order, by a great formation of rocks, in which a slaty character predominates more decidedly than in any of the pre- ceding systems. ‘This slate group generally dips at a high angle, and is of very great thickness ; less, however, than might at first be supposed from its breadth, which is not less than four or five miles, inasmuch as many of its beds are repeated again and again by a succession of anticlinal and synclinal planes, ranging exactly with the strike ofthe country. It may be separated into two natural divisions: the lower abounding in a greenish chloritic schist, much intersected by quartz veins, and generally too soft and shivery to be used for roofing-slate ; the upper containing also many soft fissile beds, resem- bling those just mentioned, but abounding also in thick, arenaceous beds, some of whichare red and variegated, like the hard arenaceous bands east of Combe Martin, while others are gray and greenish gray. The glossy slates of the lower division terminate on the coast near the north end of Morte Bay ; and some hard, greenish gray, or purple, micaceous flagstones, form the highest por- tions of the upper division, and are, by a well-defined southern dip, carried under the next succeeding headland of Baggy Point. * If we are correct in identifying the red sandstones and hard arenaceous rocks of Croydon Hill, Grabbist Hill, and North Hill; and if we have correctly linked the rocks of North Hill with the red arenaceous rocks which strike from Porlock Bay to the Foreland ; it then follows inevitably, that the red sandstone of the Foreland is the equivalent of the red sandstone between the Valley of Rocks and Combe Martin. Mr. De la Beche (Report on the Geology of Devon and Cornwall, 1839) places the red sandstone of the Foreland under the Linton system. We cannot at present accept this interpretation of what we allow to be a difficult and disturbed natural section. Our interpretation of the phenomena is explained in the text, and illustrated by the accompanying section (Pl. LI. fig. 1.). The question is, fortunately, one of no real moment, as there is now no difference of opinion respecting the geological position of the several groups of strata with organic remains, upon which all general questions of classification must ultimately depend. Physical Structure and older stratified Deposits of Devonshire. 643 The beds of the great double group, just described, range across North Devon, along with the calcareous system on which they rest, and are finely exposed in the cuttings of the new road from Minehead to Dulverton, where they agree so well with the corresponding parts of the coast section, that nearly the same description might serve for both localities. The upper arenaceous beds are well seen in the river gorges to the north of Dulverton. We have not traced this system further to the east ; but it appears to range through Brandon Hill, and the elevated ground on the south side of the calcareous bands of Croydon Hill, towards the plain of the new red sandstone. The fifth and last group of the northern region of Devon, commences on the coast, in the headland called Baggy Point, where the beds dip S.S.W. at a great angle. Many of them are composed of an arenaceous and siliceous flag- stone, of a brownish gray colour ; but they are neither so thick nor so firm in texture as the siliceous beds of the lower group, and are distinguished from them also by ferruginous earthy bands, with numerous casts of organic re- mains, which are wanting in the former. In rounding Santon Down, we find a system of brown earthy slates and flagstones thrown into a succession of vio- lent undulations ; but on skirting the marshes still further towards the south, in the direction of Barnstaple, they acquire a steady dip to a point about south by west ; and with the same dip, they are seen in some low earthy cliffs oppo- site Fremington Pill, near Barnstaple, on the south side of the river, and are thereby carried under the base of the great culmiferous series. By referring to the accompanying Map, it will be seen, that the breadth of this fifth group, near the coast, measured ona line perpendicular to the strike, is not less than three or four miles. Following its range towards the east, it is seen underlying the culmiferous rocks to the north of South Molton ; and the upper portion of it passes under the same rocks between Dulverton and Ex Bridge. (See Sect. fig. 4. Pl. LJ.). Still further in the prolongation of the line of strike towards the east, the mineral character of the group undergoes a considerable change. The brown and gray arenaceous flagstones of its in- ferior portion, often pass into a red sandstone, hardly to be distinguished from the red sandstone of the second group ; and its upper portion at the same time passes into a beautiful bright red and variegated earthy slate, which underlies the culm series, and is well exposed in a rivulet between Trace Bridge and Stawley. Considered as a whole, this fifth group is distinguished by its lower arenaceous flagstones, with ferruginous bands of rottenstone, full of organic remains ; by the dull colour and more earthy texture of its slaty beds; by its brown flagstones, covered with impressions of encrinital stems ; by its calca- reous bands, sometimes passing into great lenticular masses (provincially called VOL. V.—SECOND SERIES. 40 eS Ee 644 Professor Sepewick and R. I. Murcutson, Esq., on the junks) of nearly pure limestone; and by its numerous, but generally ill- preserved, fossils. Many parts of it so exactly resemble the Caradoc sandstone, that we were, at first sight, led to place it provisionally in that part of the Silurian system. Mineral Structure, Thickness, Fossils, &c. of the preceding Five Groups. In the preceding sketch, we have endeavoured to convey a true notion of the distribution of the natural groups into which the strata of a portion of North Devon may be divided, and of the evidence we have of their order of superposition. We must now add a few words on their structure, fossils, and other characters, by help of which, we may hope eventually to compare them with other rocks of the British series. (See Map, PI. L., and Sections !, 2, and 4, Pl. LI.) 1. Our lowest group, as above stated, is seen in the lower part of the Valley of the Lyne, and in the Valley of Rocks, and the cliffs west of Linton. Ascending the valley from Lynmouth, the beds on both sides the river dip nearly north, but at a small angle*. The most striking of them are composed of a hard, close-grained, greenish and reddish siliceous sandstone, much inter- sected by nearly vertical, transverse joints, slightly micaceous, and here and there traversed by earthy, cellular bands, marking the dip, and full of casts of fossils. These harder beds alternate with and pass into soft fissile and chloritic beds, much intersected by planes of cleavage, which hang towards the south—a direction opposite to the true dip of the beds. A little below Waters’-meet, the beds are so much contorted that it is difficult to draw any conclusions from their dip; and some of them are highly calcareous and fossiliferous. ‘The organic remains are, * The same dip is seen in the cliffs on both sides of Lynmouth, and extends a considerable way both to the east and west. Following the base of the cliff towards the Foreland, this northern dip continues about half a mile; and we reach a point where, in the lower part of the cliff, is a hard, bluish flagstone, with calcareous veins and some obscure fossils ; and in the upper, a hard, reddish gray gritstone, with many quartz veins. We supposed, when on the spot, that these calcareous beds were a prolongation (by the northern dip) of some similar beds seen in ascending the gorge of the East Lyne. Beyond the point of the coast above mentioned, commence some remarkable contortions ; and the dip at the base of the cliff is reversed to the south, for about a quarter of a mile, when a series of magnificent contortions, by which the beds are almost twisted into re-en- tering curves, and enormous masses are almost compressed into ellipsoids, are again seen in the cliffs, where the coast turns and trends more directly towards the north. Beyond this part of the cliff, there is a steady dip to a point about N.N.E., and at a great angle, and it is continued into the reefs at the furthest point of the Foreland. Considering the enormous thickness of the coarse red grits which extend into the Foreland, we do not see how they can be correctly packed under the Linton calcareous group, consistently with the dips above indicated. Our interpretation probably requires a downcast fault to the north, cutting through the contorted beds. Mr. De la Beche’s explanation seems, on the contrary, to require an upcast fault to the north. In a previous note (p. 642) we have endeavoured to show that our explanation harmonizes with the general structure of the district. Physical Structure and older stratified Deposits of Devonshire. 645 however,‘almost entirely destroyed by cleavage-planes cutting obliquely through them. On the banks of the tributary of the Lyne, south from Waters’-meet, the slates become so highly calca- reous, that an attempt was made to burn them for lime; and we have been informed, that along the same strike of country, similar beds have been found in Exmoor Forest. In the higher parts of this group, the hard gritty and siliceous bands, generally of a dull gray colour, continue to alternate with the slaty and chloritic beds, and are in some places very fossiliferous, as may be seen in the Valley of Rocks, and at the great Castle-Rock on the coast ; near which the series ends—being carried by a southern dip under the second group. A passage, indeed, seems to be made into the red upper group, through the intervention of some bands of red, earthy schist, alter- nating with micaceous and siliceous flagstone. In the absence of any visible base, it is impos- sible to estimate the entire thickness of the formation, we have been describing; but from the lowest beds in the gorge of the Lyne to the crests of the hills overhanging the Valley of Rocks, and still more to the beds of passage above indicated, there is a thickness of many hundred feet. Among the fossils obtained from this group (unfortunately in the form’ only of casts, and gene- rally ill-preserved) we have many corals, an Orthis, and two Spirifers ; but as we shall return to this subject, we will not, for the present, attempt to describe our imperfect list. 2. The most striking characters of the second group are its coarse texture, and red or purple colour. These colours are partly derived from the red oxide of iron diffused through the beds, and partly from the veins of the same mineral which traverse the cliffs, and are washed far and wide by the waters. Indeed, some of the beds themselves (where no veins intersect them) are so impregnated with an earthy oxide of iron, that they are dug up entire, and the richest parts of them are extracted for the furnaces*. Cases like these are, however, to be regarded as rare exceptions. The coarser beds are generally thick, irregularly jointed, and break into rude, shape- less, angular fragments; and their colours vary through white, gray, greenish gray, variegated, and purple, to deep red. The coarsest varieties, at North Hill and in some parts of the Quan- tocks, pass into a conglomerate of red sandstone, with quartz pebbles, not distinguishable from the conglomerates of the old red sandstone. Some of the hills west of Porlock are. covered with a white sandstone of this formation, fragments of which lie bleaching on the moors, and might be mistaken, at first sight, for grits of the coal formation. The fine sandstones contain, however, fragments of clay-slate, and not unusually pass (through the intervention of purple, variegated, micaceous, flaggy grits, exactly like the flaggy beds of old red sandstone) into red slate, grey- wacké, and greywacké slate; among which, bands of fine, glossy clay-slate are here and there interpolated. Considered as a whole, and from mineral characters only, we might compare some parts of this group with the most characteristic portions of the old red sandstone. Other parts we might compare with the red arenaceous beds of St. Abb’s Head and the Lammermuir chain ; with the red sandstones and schists of the Longmynd, Lyth, and Haughmond Hills of Shropshire ; and with some of the coarser portions of the Upper Cambrian System, as developed in South Wales. The whole thickness is exposed only in the coast section; extending, as before stated, from the west side of the Castle Rock to Combe Martin. The dip is steadily towards the south ; and there are, we believe, few breaks or dislocations by which the same beds are repeated over again. The breadth of the formation, measured transversely to the strike, is nearly three miles; the thickness of the group must, therefore, be very great. Considered as a whole, it is neither cal- * There is a work of this kind on the south side of the red sandstone plain, about two miles from Timberscombe, in Somersetshire ; and similar works were once carried on in the hills north of Combe Martin. (See Map.) 402 646 Professor Sepewick and R. 1. Murcuison, Esq., on the careous nor fossiliferous ; but by these words, we mean to state only that we found no fossils in it, and that at least they are very rare. We must remember, however, that it is interpolated in a fossiliferous system; and that a better search might probably bring to light a few fossils among the finer strata, alternating with the coarser red sandstones. 3. The next group of calcareous and fossiliferous slate is of very complicated mineral structure. The first beds are coarse and siliceous, and contain fragments of large, heart-shaped, bivalve shells. These are succeeded by clay-slate, more or less arenaceous, all dipping, as before, about S.S.W., and at a considerable angle. Ascending by the valley of Combe Martin to Yellaton (a distance of about a mile and a half), we cross not less than eight or nine courses of highly calcareous slate, in some places passing into great bunches of bluish crystalline limestone, with many contempora- neous veins. The limestones have some traces of organic remains, which occur also in abundance, but generally as casts, in the neighbouring calcareous slate. One of these calcareous courses immediately south of Combe Martin, is not less than 60 feet thick. In general, they are much thinner ; and none of them are very continuous in the direction of the beds; but contracting to an edge, and expanding, several times, along the line of strike, they occasionally appear more like huge lenticular masses of semi-crystalline limestone, interpolated irregularly among the cal- careous slates, than true alternating beds. Four or five of these calcareous courses have been traced, by our friend Major Harding, through the headland which separates Combe Martin from Ilfracombe. The cliffs on both sides of Ilfracombe Harbour are interesting, from their great complexity of structure. Some of them are made up of alternating strata of hard siliceous sandstone; and beds of soft, glossy, yellowish green, chloritic slate: others are composed of dark-coloured clay-slate, with quartz veins, alternating with hard quartzose beds. Some parts are devoid of calcareous matter; others abound in it; and among the earthy slates, west of the harbour, are thin bands of limestone, almost made up of encrinital stems. Among the caicareous slates, we find quartz veins, sometimes ranging in long stripes, nearly parallel to the beds; sometimes in irregular zig-zags nearly transverse to them; and in one or two instances thin veins of arragonite range nearly parallel to the strike. In the cliffs west of the harbour, where the structure is thus complicated, the beds are violently contorted: still further west, they acquire the prevailing dip (S.S.W.), by which the distinct courses of calcareous slate, with great lenticular masses of limestone, are brought down to the coast; and the whole mass plunges under the next higher group. The phenomena of slaty cleavage may be studied among these cliffs to great advantage. The average dip of the beds is about 35° to the S.S.W.; and among all the more fissile beds, we have a cleavage dipping to the same point, but at a greater angle; perhaps on the average as much as 60° or 70°. These cleavages affect also the calcareous beds, and make it almost impossible to ascertain their true dip in the quarries, where the contiguous strata are not exposed. The cleavage planes are not merely posterior to the beds, but are of a date posterior to those movements which produced the contortions : for there are several places, where these planes pass, without deviation in their strike and inclination, through a succession of violently-contorted beds. We may remark, also, that when any part of these beds is brought into such a position, that the cleavage becomes a tangent plane, the fissile texture will then coincide with the true bedding of the rock, and again separate from it, as the contorted beds deviate from the unvarying cleavage course. All the neighbouring coast is intersected by joints, often forming a succession of great parallel open fissures. Of such there are two sets,—one to which we give the name of dip-joints is nearly transverse to the strike, and most frequently in a vertical or very highly-inclined position ; the other set (or strike-joints) is nearly coincident with the strike, and generally inclined at a Physical Structure and older stratified Deposits of Devonshire. 647 great angle to the planes of the strata, and hence, where the strata dip to the south, these joints generally underlie to the north. This double system of joints divides many parts of the beds into a great series of rhombohedral solids. The cleavage-planes, in no instance which we observed, were parallel to these joints. Hence, also, it follows, that the jointed structure and fissile structure are not to be confounded. Almost all solid rocks have more or less of a jointed structure; but a small number of them have a transverse fissile structure. The two structures may, and do often, coexist, but, in all descriptions of old rocks, ought to be carefully distinguished from one another. Such are the phenomena presented by this group in the only sections in which the successive parts are well exhibited. In its range towards the east, it is for many miles very ill exposed ; being much covered by the vegetation and alluvial matter near the flanks of the higher ridges formed of the harder beds of the second group. Between Timberscombe and Dulverton it crosses the road, as above stated, at the water-shed, and contains, at least, three distinct calcareous courses. Further east it again declines in elevation ; and the calcareous portion skirting the south flank of Croydon Hill is principally represented by one very widely expanded course of limestone, which is extensively worked. To the east and north-east of Croydon Hill it is again subdivided into several distinct courses of calcareous slate and limestone. These are precisely the phenomena we might have expected in such a formation. The structure seems to be most complicated towards its western extremity. Assuming the breadth of the formation at a mile and a half, and the average dip at 35°, we shall (after deducting for a few local contortions) have a very great thickness for this group. Stems of Encrinites and portions of corals are among the abundant fossils of this group. Some of the calcareous slates of Ilfracombe are almost covered with the Favosites polymorpha, which is so abundant in the Torbay limestone. There are in this group also a Producta, several species of Spirifers, and other fossils, to which we shall refer in the sequel. 4. We have little to add to what we have already said, respecting the structure of the next su- perior group. The lower portions, which abound in soft chloritic slates, exhibit very fine examples of slaty cleavage, as distinguished both from joints and planes of stratification. For example, in the cuttings for the new road in the hills south of Ilfracombe, the cleavage has a nearly uniform dip at a great angle to the S.S.W. or S. by W.; while the strata, as may be made out from the stripe, are here and there violently contorted. ‘The same facts are still more clearly illustrated on the coast near Morte Point, and in descending into Morte Bay from the north. This part of the series abounds in large, white quartz veins ; several of which affect a kind of rude parallelism to the strike of the beds, but others are in undefined oblique directions. They are all to be re- garded as veins of segregation, by some means or other superinduced on the rock, during the passage into its present solid state. The upper and more arenaceous portion of this group, occupying the middle and southern end of Morte Bay, is ill exposed on the coast; but it may he considered to terminate in some thick and very hard beds of gray, greenish gray, and purple-coloured sandstones, alternating with thin beds of chloritic and purple glossy slate. These beds may be traced along their strike through North Buckland, and thence, skirting the south end of the hills containing the old manganese works, towards Muddiford. Notwithstanding the many contortions of the chloritic slates, and some undulations (especially as shown in the sections on the road from Dulverton to Minehead) of the upper and harder rocks, the prevailing dip is towards the south ; and the whole thickness of this group is very great, per- haps greater than that of any of the other divisions into which we have separated the deposits, we are describing. In no part of it did we observe any organic remains. 5. There is no definite line of separation between this and the preceding group: for beds of Se 648 Professor Sepewick and R.1. Murcuison, Esq., on the siliceous sandstone, resembling those last described, continue for some way as we ascend the hill which runs out into Baggy Point. Gradually, however, the alternating glossy slates almost dis- appear, and the strata put on the form of gray and brownish gray micaceous flagstones ; and asso- ciated with them, near the top of the hill, are some cellular ferruginous bands, with numerous obscure casts of fossils. Doubling Baggy Point and descending to the north side of Croyde Bay, slaty masses again abound, which, though very fossiliferous, and of much more earthy texture than those of the preceding group, have generally a true slaty cleavage. These cleavage-planes strike very nearly, though not always exactly, with the beds; and in this part of the coast they generally incline at a high angle towards the north, the prevailing dip of the strata being towards the south. Phenomena of this kind are always instructive, and are more especially so on the coast of Santon Down, where the beds are highly fossiliferous and thrown into a succession of undulations. In this part of the coast, many of the rocks conform so nearly to the mineral type of the lower division of the Silurian system, that the descriptions of the slaty varieties of the Caradoc sandstone of Shropshire and Herefordshire might be applied to this Devonian series, almost word for word. The lower or middle portion of the group, we are describing, may be easily followed along its strike into the interior of the country ; and there are two quarries in it which deserve notice. One of them, first noticed by Major Harding, is near the inn by the road-side at Marwood, and ex- poses a set of strong beds of brownish gray and greenish gray sandstone; at the partings of which are several ferruginous, cellular, and earthy bands with numerous casts of fossils. The other is at Sloly, nearly three miles north of Barnstaple, and close to the turnpike road. It deserves notice from the structure of its coarse and thick beds of greenish gray and brownish gray sandstone, separated by the bands of earthy slate and shale ; and still more from the vegetable fossils disco- vered in it by Major Harding and the Rev. D. Williams, which will be described in another place. In both the above quarries the dip is almost south; but a little nearer Barnstaple, similar beds are reversed and thrown into undulations. Lastly, the highest portion of our present group passes into a deposit of soft and rather earthy slates with subordinate bands of sandstone, and occupies generally a low tract of country skirt- ing the northern boundary of the culm measures. It is very fossiliferous, and sometimes highly calcareous, passing, as before mentioned, into irregular masses (or junks) of limestone. These however, are seldom worked, in consequence of the immediate vicinity of the great open quarries of black limestone, found in the lower portion of the overlying formation. In consequence of the undulations above noticed, and of the interruptions caused by the wide marshes bordering on the Barnstaple river, it is very difficult to make any approximation to the whole thickness of this group. We have, however, evidence enough to show, that the thickness must be very great, without taking into account the lower undulating masses. Beyond Dul- verton, in its range towards the plain of the new red sandstone, it becomes much more ferru- ginous, and is greatly modified in mineral structure, as we have already pointed out. Among the fossils of the lower part of this group (Marwood quarries) are shells of the genera Cucullceea, Cypricardia, and Bellerophon. One species very closely resembles Bellerophon globa- tus of the old red sandstone. Nearly on the same line (Sloly quarry) occur the vegetable impres- sions above noticed. By far the greatest number of fossils occur, however, in the upper part of this group; and among them, we noticed innumerable crinoidal stems, many fragments of Trilobites, Orthoceratites, Terebratulz, many Spirifers, a few spined Producte, &c. &c. A more detailed account of these fossils is reserved for a future communication. Physical Structure and older stratified Deposits of Devonshire. 649 Such are the groups into which we have divided the deposits in the northern region of Devonshire. They are founded on analogies of mineral structure, on superposition, and on the existence of successive calcareous and fossiliferous bands ; and it is important (at least till they are better known) to keep them distinct from one another. Some of the lines we have drawn, are, perhaps, artificial and arbitrary ; but so are some of those which divide our best known, secondary formations. Without something like the arrangement we have adopted, it would be difficult to give any clear description of the great deposits of the northern region ; still less could we hope to bring them into comparison with the successive groups in South Devon. At all events, we have shown that all the groups above described are inferior to the culm-mea- sures of our third region, a fact with which we were unacquainted, when we commenced our task. Cuap. III].—Succession of Deposits between Dartmoor and the South Coast of Devon, &c. &c. (See Map, Pl. L., and Sections, Pl. LI.) Ifa line be drawn (in a direction about east and west) from the limestone cliffs near Plymouth to the limestone cliffs of Berry Head, at the south end of Tor Bay, it will cut off the great south promontory of Devon, which terminates in three remarkable headlands,—Bolt Head, Prawle Point, and Start Point. Now, as in all this promontory the strike of the beds is nearly east and west, and the prevailing dip is south, it appeared to us that the coast-section from Ply- mouth to Bolt Head, and a corresponding section from Berry Head to Start Point, must probably cross the same succession of deposits. We examined both these sections, and our expectations were realized. North of the line above mentioned, the strike and dip of the strata are by no means regular. They gradually become affected by the granite of Dartmoor, and on dou- bling its southern end they are bent towards the N.E. In this way, rudely conforming to the mean boundary of the granite, they sweep round the south-eastern side of Dartmoor with a north-eastern strike and a prevailing south-eastern dip, as far as the basin of Bovey Tracey. If, however, we make a traverse from this side of the granite to the cliffs of Tor Bay, we gradually lose this regularity of strike and dip. The strata have been much disturbed at different periods, and exhibit many axes of elevation (probably de- rived from great protruding masses of trap) which conform to no given direc- tion. The contorted beds of Tor Bay (which have been described in memoirs 650 Professor Sepewick and R. 1. Murcuison, Esq., on the read before this Society *) are fine examples of what we are here stating, and many others are exhibited in the interior of the district. In spite of this confu- sion, we easily ascertain that the limestone rocks of Tor Bay and Berry Head belong to the highest strata of the older formations on the south-eastern side of Dartmoor. Now the limestone series at Berry Head (both from the evidence of the coast section and from the evidence of the section along the estuary of the Dart) is found to plunge under the slate region, which is expanded through the great south promontory. From which it follows, that a section first from Dartmoor to Berry Head, and then continued from Berry Head (coastwise) to Start Point, must cross all the old stratified deposits of South Devon. We think there is no doubt that the Plymouth limestone is exactly or very nearly the equivalent of the limestone of Berry Head. Hence (after what has been said respecting the strike and dip of the country) it must be obvious, that a trans- verse section from the granite of Dartmoor to the Plymouth limestone, and then continued from that limestone (coastwise) to Bolt Head or Start Point, would also give a nearly perfect series of the strata of South Devon. We examined the several lines above-mentioned ; and in the essential details of the corresponding parts, they appeared to agree perfectly, some of the lowest beds only being wanting on the line from Dartmoor to Plymouth. Our limits pre- clude minute details; but we will, in a few words, endeavour to describe the facts which are exhibited on those lines of section, and seem essential to our classification. 1.—Sections from the east side of Dartmoor to Berry Head, &c. &c. Commencing with the section from Dartmoor to Torbay, we pass over the stratified rocks im- mediately in contact with the granite; for in that association, whatever part of the series they may belong to, (and under this remark we include the culm-measures as well as all the older for- mations,) they become so entirely metamorphic as to lose all their distinctive characters. But at a little distance from the granite, (for example, on the north side of Ivy Bridge, and on the east side of a line drawn from Ugborough to Buckfastleigh) there are extensive tracts of a rock which deserves notice. It is hard, brittle, and porcelaneous; sometimes passing into a compact fel- spar, sometimes into a flinty slate or Lydian stone, not unusually resembling the well-known altered coal-shales in contact with trap dykes. We have no doubt that these rocks have been in- durated by the action of the granite, as in following them in the ascending order, they gradually pass into the common dark-coloured roofing-slate of this country. Higher in the ascending sec- tion, the slates become calcareous, and here and there pass into masses of bluish gray limestone. Two or three distinct bands of this kind may be seen in the neighbourhood of Ugborough ; and in the range of the strata northwards, the calcareous portions unite into one leading mass, and swell out so much as to make, in the neighbourhood of Ashburton, a great feature in the district. The * See Mr. De la Beche’s Memoirs, Transactions of Geological Society, 2nd Series, vol. iii. part 1, p. 160. Physical Structure and older stratified Deposits of Devonshire. 651 Ashburton limestone contains a few corals and some unascertained casts of shells. Immediately under one of the coral beds of the Ashburton quarries, is a remarkable band of highly carbona- ceous black shale. The neighbouring beds of limestone are of a dark colour and very much re- semble true carboniferous limestone. ‘They do not, however, burn (like the dark beds of moun- tain limestone) into white lime, and therefore do not derive their chief colouring matter from carbon*. Still higher in the ascending section, the calcareous bands disappear, and we have again a suc- cession of soft glossy slates (in some places used for roofing), with very few distinctive mineral characters, and generally without any cleavage, separate from the lamin of deposit. The upper part of this series again becomes calcareous ; obscure casts of organic remains are found abun- dantly in some parts of it; and among indurated slates associated with trap, which seem to under- lie the limestone of Newton Bushel, are fine impressions of an undescribed Trilobite. The fossiliferous slaty beds introduce the great upper or Torbay limestone, which is magnifi- cently developed both in the interior of the country and on the coast. The nature of this communication not admitting of minute details, we have so far omitted all description of the various trap rocks which occur on our lines of section. Some are of the nature of dykes, and appear to have been protruded at different times prior to the eruption of the gra- nite, which (as was pointed out by Mr. Austen) they never penetrate. Other trappean masses are not only parallel to the beds of schist, but are associated with plutonic sediment passing into, and alternating with, the slaterocks. Insuch cases, we concluded (as we had done before in num- berless instances seen in Cumberland and Wales) that the plutonic and aqueous rocks were con- temporaneous. In the slaty series between the Ashburton bands and the great upper limestone on the east side of South Devon, we may often remark, that the higher portions become arenaceous, and sometimes pass into a coarse red sandstone, not to be distinguished from the old red sandstone. Instances of this kind are exposed in Babbacombe Bay, in the hills N.W. of Totness, and on the banks of the Dart. Neither is this series altogether devoid of calcareous matter and beds of limestone, as may be seen in several sections to the north-west of Totness. We considered these beds as mere offsets from the great limestone ; but Mr. Austen has since shown us sections, which prove that at least some of them are true members of the middle slate series. ‘They cannot, we believe, be traced far on the lines of strike, as many transverse sections give no indication of them. A more import- ant fact, however, in the history of this great slaty group is the frequent occurrence of organic remains in the beds as they approach the great upper limestone. This fact (of which examples may be seen near Ogwell, near Pomeroy Castle, in the cliffs east of Torquay, at Mudstone Sands, &c. &c.) shows that the slates and overlying limestone belong to one uninterrupted series of de- posits ; for in other situations the slates are very rarely fossiliferous. The upper limestone in the eastern parts of South Devon generally ap- pears in the form of great unconnected masses, more or less tabular, crowning the hills and surmounted by no newer deposits. In its structure, as well as * Among the shales which divide the beds of the great upper limestone of South Devon, about two miles north of Tetness, we found a few thin lamine of bright coal. Examples of this kind are, we believe, very rare; but there are similar appearances in the Hooe limestone quarry, near Plymouth. VOL. V.—SECOND SERIES. 4p 652 Professor Sepewick and R.1. Murcuison, Esq., on the position, it strongly reminded us of the masses of great scar limestone which rest unconformably on the slate rocks of Cumberland and Westmoreland. From this circumstance, and perhaps still more from some of its fossils, it has been occasionally confounded with the carboniferous limestone. But a portion, at least, of its fossils, more especially its corals, separate it from that limestone ; and the association of its lower beds with calcareous slates passing into the lower slaty system of South Devon, entirely preclude it from being grouped with any part of the true carboniferous system. The coast sections, however, seem to put the question out of all doubt. We have no hesitation in identifying the great limestones of Newton Bushel, Babbacombe Bay, and Torbay. Now the great limestone at the south end of Torbay, after exhibiting a number of contortions, and spreading out into a succession of mural precipices at Berry Head, is finally (at Mudstone sands) bent into a great arch which brings up the lower calcareous slates on which it rests, and causes the southern flap of the great limestone saddle to dip under the slate formation which is expanded towards the south along the shores of Start Bay. The same order of super- position is also indicated at Galmpton Creek on the eastern shore of the Dart, as well as at intermediate spots along the southern boundary of the limestone. (See Section 6.) Thus we find, that the great upper limestone of South Devon is fairly inter- polated between two great groups of slate rocks. Under such circumstances we are not surprised to discover that the calcareous beds have a continual tendency to thin out and come to an edge. This phenomenon (as also in North Devon) is best seen in the line of strike. Sometimes, however, we may see the beds thinning off in the line of dip; so that a mass of limestone will, in a vertical section, look like an acute wedge, driven in between the laminz of the slates. Cases of this kind do not produce any ambiguity, as the longer dimension of these wedges of limestone is always in the direction of the dip. The great limestone of Berry Head thins off in the direction of the Dart, and beyond the river seems to be replaced by several thin calcareous bands, alternating with the slate. further west, these calcareous bands disappear : but a similar system, very nearly, if not exactly, on the same line of strike, is revived, and becomes of great thickness, on approaching Plymouth Sound*. * Our accompanying section (P]. LI., fig. 8.) shows the lower (or Ashburton) limestone. The beds below this limestone are concealed by an overlying band of culm-measures, as we after- wards learnt from a section by Mr. Austen, and have represented on his authority. ‘The small trough of culm-measures overlying the great upper limestone was observed by us in 1836, and is alluded to at its proper place in the text. Physical Structure and older stratified Deposits of Devonshire. 653 2.—Section from Dartmoor to the Plymouth Limestone, &c. (Pl. LI., fig. 9.) If we cross the country from the south end of Dartmoor to Plymouth, we have a less perfect section than that above described, for the lower calcareous, or Ashburton, bands have almost disappeared. This may be easily accounted for; as even the thickest bands of the limestones, which are interpolated in the slate series, continually thin off; and in this case some of them may have been cut away by the encroachment of the granite. Commencing with the boundary of the granite, we first meet with highly altered slates pene- trated by granite veins, and tilted at a great angle. These, through various gradations, pass into the hard slates of Ivy Bridge, which, in the ascending order, finally pass into the ordinary dark lead-coloured slates, exactly like the courses overlying the Ashburton limestone. In most parts of South Devon, slates are obtained from planes parallel to the laminz of de- posit; and, generally speaking, the transverse planes of slaty cleavage are incomparably less developed than among the schistose rocks of North Devon. But in a quarry about two miles south-west of Ugborough, we found very instructive examples of transverse cleavage, the planes of which had the exact strike of the beds, but were inclined at a much greater angle. Other, more inclined beds (both in the same and neighbouring quarries), were gradually brought into a position nearly coincident with that of the slaty structure, and then ceased to show any oblique cleavage planes ; a fact, which clearly shows, that the cleavage planes were superinduced on the beds after their dislocation. We remarked, also, that the best slates were obtained, not from the lamine of deposit, but from the oblique planes. Near Ridgeway (on the Plymouth road) are several courses of trap, which range very nearly with the beds; and a little to the north are quarries of slate, associated with trap. One of them gives some obscure traces of an oblique cleavage, and exposes purple and dark leaden-coloured slates, which are much indurated, and spotted exactly like the altered chiastolite slates of Cum- berland. On the south side of the quarry, close to the trap, is a chloritic slate, with a few crystals of felspar; yet this chloritic slate seems, by most regular gradations, to pass into the or- dinary dark-coloured slate. We need not dwell on details familiar to all who have examined the great slaty regions of England, but state at once, that, by a regular dip to the south, the whole slate series is carried under the Plymouth limestone. In other respects this and the preceding section agree in their general details. The Plymouth limestone is composed of a great succession of thick, well-defined beds, dipping south, at an angle averaging at least 30° or 35°; and as its superficial breadth amounts in some places nearly to a mile, and it is not repeated by any great contortions, its thickness must be very considerable. Notwithstanding this, if we follow it to the east, along the line of strike, it comes to an edge at the distance of about four miles ; and if we follow it in the opposite direction to the Cornish side of the Sound, it thins off still more rapidly; so that before we reach White Sand Bay, it has dwindled down to a few inconsiderable red beds of calcareous sandstone, containing Encrinites and other fossils; and further along the Cornish coast we lose all traces of it. A few masses of limestone, comparatively of inconsiderable extent and thickness, break out here and there, nearly on the line of strike between Plymouth and Berry Head, and seem to represent, in Ap? 654 Professor Srpewick and R. I. Murcuison, Esq., on the a degenerate form, the great upper limestone of South Devon. At Plymouth the strike is very nearly east and west; but following the strata towards the east, we find them gradually deflecting a few degrees towards the north, which necessarily throws the limestone of Berry Head a little to the north of the Plymouth limestone. Before we proceed to describe our remaining sections, we may briefly notice some of the characters of the South Devon limestones. 1, Where the sections are complete, they are interpolated in a great slaty series, and, indeed, very often pass into mere calcareous slates, subordinate to the general mass: parts even of the Plymouth limestone pass into mere cal- careous slates. Its bottom beds pass into the strata on which they rest: its upper beds, in like manner, are exactly parallel to, and pass into, those by which they are overlaid. Hence, the present inclined position of the calca- reous masses is due to the same causes which produced the present position of the slates. 2. The want of continuity in the limestones proves, that the causes which produced them acted less generally than the mechanical causes that gave rise to the layers of mud and sand out of which the slate series originated. It is difficult to speculate about the origin of calcareous slates where organic remains are almost wanting ; but many parts of the upper limestone seem to be, in a great measure, due to the action of animals which once inhabited shells and corals. Now, the coral reefs and shell beds of the ancient sea must have been formed at the same inclination with the beds of sand and mud which were contemporaneous with them, and consequently were once nearly level. 3. There is a strong resemblance in the mineral structure of all the upper limestones of South Devon: at one extreme they are earthy and slaty ; at the other perfectly crystalline. ‘The most crystalline portions seem to have been formed about masses of abraded corals ; and many of the hardest and thickest beds have more or less of a brecciated structure, as may be seen in some of the well-known Devon marbles. A colour derived from red oxide of iron is often irregularly impressed on the beds of limestone ; and as the same colours are found in the next overlying group, as well as in some of the beds, inferior to the great limestone, this circumstance often produces a striking appearance in the range of the deposit through the country. The limestone was probably consolidated sooner than the slate, and hence may have offered planes of greater resistance, during successive periods of elevation. It is to this cause that we attribute the existence of some flexures in the inferior slates, which hardly seem to affect the great overlying masses of limestone, and produce what we regard as a deceptive appearance of discordant stratification. What makes this explanation more probable is the fact, that the thin beds of lime- Physical Structure and older stratified Deposits of Devonshire. 655 stone, and the calcareous slates, partake of all the complicated flexures of the slate series. The contorted beds of Purbeck limestone, associated with tabular masses of Portland rock, are examples of similar phenomena among secondary strata. 4. In some of the larger masses of limestone, the crystalline action, during the process of solidification, has almost obliterated every trace of deposit. All of them are more or less traversed by open joints ; and some of the Plymouth beds are intersected by vertical north and south dip-joints of great regularity. The limestones are also occasionally divided into laminz by oblique lines of cleavage, like those before noticed near Ilfracombe. Fine examples of this structure occur in several places north of Totness, and in the hills on the east side of Brixham; and the phenomena are the more remarkable, because an oblique slaty cleavage is very rarely seen among the neighbouring slate rocks. A certain quantity of calcareous matter seems in some instances to favour the development of this structure. For example ; along the whole course of the Dart below Totness, the beds are generally without the least trace of an oblique slaty cleavage ; but at East Cornworth Creek, a band of limestone is dislocated, dolomitized, and tilted at a great angle to the north, and is over- laid by some calcareous slates, which, near the beach, dip north, at a small angle, and have a distinct cleavage, inclining south at 45°. An exactly similar phenomenon may be seen in a small mass of calcareous slate imbedded in the great contorted red sandstone south of Plymouth ; and there, also, the neigh- bouring strata are entirely without any transverse cleavage. 5. Before we quit the subject, we may notice one or two peculiarities of structure which are seen, though rarely, in South Devon, but very abundantly in the calcareous slates of the Cornish coast, west of Padstow. A slight change of colour generally marks the passage from one bed of slate to another; and hence, when several beds are cut through by an oblique cleavage plane, the surface of the slate so obtained is marked by a set of parallel stripes indicating the course of the beds. It is also clear, that slates obtained from lamine par- allel to the bedding can never show a striped surface of the same nature. But some slaty rocks (e.g. on the coast of South Devon, near Avon Mouth, and on the north coast of Cornwall) have what may be called a false stripe, which is at first sight very deceptive. They are derived from beds, the fine laminz of which, in passing into a solid state, have been forced, by crystalline or mechanical forces, into wavy lines or flutings, sometimes nearly constant in their prevailing direction. Slates cleft off from such beds show stripes of co- lour parallel to the flutings, and are to be distinguished from the true stripe only by being worse defined and less uniform in their direction. That these SS SS SS = = =a a= 656 Professor Sepewick and R. I. Murcuison, Esq., on the wavy lines were produced by tension, seems probable when we follow their course, and see it marked by minute joints, filled generally with quartz. We never saw an example of this false stripe in any roofing-slate of Wales or Cumberland ; and the two kinds of stripe very seldom occur together. ‘There are slates also from South Devon and the north coast of Cornwall, which give clear indications of a second cleavage plane affecting the elementary structure of the rock. We speak of a structure never, as far as we know, seen in the old Cambrian slates, and entirely distinct from the small double joints which so often separate individual beds into rhombohedral solids. This second cleavage is indicated by innumerable striz (looking as if made by a sharp instrument like a very fine comb) running through the chloritic flakes that separate the laminations. With care, a cleavage (generally with a rough surface) may be obtained along these striae, which occur indifferently both with the false and true stripe above described. The crystalline forces producing these striz have also produced mechanical tension, as the striza may be sometimes fol- lowed into minute partings, generally filled with quartz. On the river above Padstow are some beautiful examples of these complicated structures. A low cliff shows a set of contorted beds of calcareous slate traced by lines of organic remains: the beds are cut by oblique cleavage planes, producing striped slates. There is a second cleavage indicated by the parallel striz, and the whole mass is divided into rhombohedral solids by a double set of open joints, which do not coincide either with the série or the stripes. 6. Lastly, before we proceed to the other sections, we may briefly notice the organic remains of the South Devon limestone. The corals in the Tor Bay, Newton Bushel, and Plymouth limestones, are very abundant ; some of the species, more especially the beautiful feather-like coral (Favosites poly- morpha), abounding at all the places above mentioned. Several species of Spirvfers, Terebratula, and other shells, bivalve and univalve, are, we believe, common to them all, as might be expected among beds nearly of the same age; but we purpose to return to this subject, when we have better specific evidence. Some of the red coraline, calcareous slates of South Devon cannot be distinguished, either by structure or fossils, from the calcareous slates near Ilfracombe. 3.—Coast Section from the Plymouth Limestone to Bolt Head*. (P1.LI. fig. 5.) 1. We commence with this section, as offering the clearest evidence of superposition, and the best exposure of the successive beds; and after describing it, we shall briefly notice the corre- * The section is supposed to be made on a straight line ; to which the phenomena on the actual Physical Structure and older stratified Deposits of Devonshire. 657 sponding section from Berry Head to Start Point. The upper beds of limestone are seen at Mount Ratten, and are overlaid by a great, red, arenaceous group, which may be subdivided as follows: (1.) Over the limestone is a brown and yellow earthy slate, with pyritous stains and iron veins, some of which run, in the form of strings, nearly north and south. This mass alternates three times with beds of impure limestone ; and the last bed occurs at Dunstan Point, where it thins out to an edge among the impure earthy slates. Several fossils have been found by Mr. Hennah in this part of the section, which may be considered as forming a kind of passage from the limestone to the superincumbent beds. (2.) From Dunstan Point to Withy Hedge, the section shows a yellowish gray and bluish gray soft slate (shillat), with some quartz veins and coarse arenaceous bands. (3.) Immediately over the preceding, and extending about three-quarters of a mile to Bovisand Bay, is a formation of bright red, and sometimes variegated sandstone, thick-bedded, and of coarse texture, but subdivided by bands of soft, glossy, red slate, and red micaceous flagstone. This division, in many parts, is exactly like the old red sandstone; and though thrown into vio- lent contortions, it dips, on the whole, towards the south, and is of great thickness. It is overlaid by a reddish slate and flagstone, which gradually passes into the next superior division. (4.) On the south side of Bovisand Bay, the slates become so earthy as to pass into the form of shale, with many small nodules of ironstone; and these are surmounted by variously-coloured earthy slates, alternating with reddish arenaceous bands, as seen in the cliffs of Crownall Bay, near the southern end of which is a patch of new red conglomerate, resting unconformably on the edges of the older strata}. (5.) Beyond Crownall Bay is reddish slate and flagstone, and coarse red sandstone, occasionally contorted and penetrated by large quartz veins; the contortions chiefly seen in the strongest and coarsest beds. These gradually pass into reddish, grayish, and greenish gray chloritic slates, with hard quartzose bands and quartz veins. They strike about EH. by N. towards Wembury, are of great thickness, and may be considered as beds of passage into the next superior group. Though the wpper limit of the preceding group is ill-defined, it is, on the whole, very distinctly marked by its coarse arenaceous bands and its prevailing red colour: and as its breadth, measured on a line transverse to the strike (from Mount Batten to the cliffs opposite the Mew Stone), is about three miles, and its average dip is not lessthan 35°, its thickness (notwithstanding the occa- sional contortions) myst be very great. In its mineralogical characters, as well as in its thickness, it bears the closest resemblance to the red arenaceous rocks in the cliffs east of Combe Martin, the second group of our North Devon section. 2. The next group occupies the whole coast, from the cliffs opposite the Mew Stone to Hope Cove, near Bolt Tail—a distance, following the sinuosities of the coast, of more than twenty miles ; coast section are referred by a series of lines drawn, from the respective points, parallel to the strike. Most of the places mentioned are found on the accompanying Map, Pl. L. + Soon after our return from Devonshire, in 1836, we were informed by Dr. Moore, of Ply- mouth, that he had discovered organic remains in this part of the series. One of the authors revisited, along with that gentleman, this part of the coast in 1838. The fossils chiefly occur in the ironstone nodules, and are generally both obscure and waterworn. We remarked among his specimens a 7'urbinolia (?), and several other species of corals; two or three species of Orthocera- tites; one or two casts of univalves; and some fragments of trilobites. Among the red cliffs of Crownall Bay, only to be approached at low water, are also many fossils, such as. stems of Eneri- nites, fragments of corals, and comminuted shells, in an impure bed of reddish limestone, partly traversed with quartz veins. Near the calcareous bands were some transverse planes of slaty cleavage—appearances very rare in this part of Devonshire. 658 Professor Sepewick and R. I. Murcuison, Esq., on the but the actual breadth of this group, measured on a line at right angles to the mean bearing of the beds, is not more than five or six miles. The ascending section ‘commences with the beds of passage above noticed; but to the south of the Yealm, the prevailing rocks are made up of a light gray and greenish gray chloritic schist, with quartz veins and quartzy concretions, and with subordinate hard arenaceous beds; and they prevail all the way to Stoke Point, with a steady dip about S.S.E. Several of these beds seem to strike into the cliffs between Stoke Point and Erme Mouth, and are repeated over again; but south of the Erme there is a steady ascending section for about two miles. In the cliff between the Avon and the mouth of the rivulet that descends from the, north side of Ringmore, there are some anticlinal and synclinal lines, which we have attempted to represent in our section (Pl. LI. fig. 5.). On the whole, however, the ascending series gains towards the south. The prevailing rock is a fine, greenish gray, and leaden-coloured glossy schist, and the prevailing dip is about S.S.E. or S. by E. Near Fishery the beds exhibit the minute striz which (in certain cases) we have considered as an indication of a second cleavage; here, however, there is no principal cleavage oblique to the bedding. The same series is also marked by beautiful flutings producing the pseudo stripe. Opposite Borough Island, near Avon Mouth in Bigbury Bay, the contortions are marked by a shattered cliff, with quartz veins and numerous joints; but further south, to a point about half a mile beyond Avon Mouth, there is a steady dip to the south, or south by east. We there meet with a synclinal line, which throws the beds into a trough, and produces a northern dip, that prevails, almost without interruption, to Hope Cove, where the whole group terminates abruptly against a formation of chlorite and mica slate. Along the lines of strike, several of the more schistose beds are worked for roofing-slate, not generally of good quality ; and, in all the instances that we saw, the slates are derived from planes parallel to the bedding. Immediately to the north of Hope Cove the beds are hard, quartzose, and dark-coloured ; and on approaching the junction, they are altered and shattered, and pene- trated in all directions by quartz veins. The actual junction is not parallel to either formation, but may be traced, at low water, in broken, zig-zag lines, showing the extreme derangement where the two masses are brought into contact. They seem mutually to wedge into and penetrate one another; and on the south side of the headland forming the junction, is a great mass of black- veined slate notched in among the beds of the older system. From the lowest beds of this group to the highest (south of Avon Mouth), there is a breadth of four or five miles, measured on a line perpendicular to the strike. Hence, notwithstanding the contortions above noticed, the thickness of the deposit must be very great, especially when we consider the high mean inclination of the beds, which is greater than that of the preceding group. The junctions on the Kingsbridge river take place on Jow ground, and give no new information; but if we follow the strike across the promontory from Hope Cove to Start Bay, we may see the two formations in the cliffs south of Tor Cross. The phenomena are there much more simple than at Hope Cove: neither the upper nor the lower system is unusually mineralized, and there is no confusion in the dip, The lower beds (composed, on that part of the coast, of fine quartzose, chloritic slate), though highly inclined, and in some places contorted, dip regularly towards the beds of the upper argillaceous slates, which also, for a considerable way, dip steadily to the north ; put the immediate contact is unfortunately concealed. 3. To complete our section, it only remains for us to describe the crystalline group which ex- tends to the extreme southern points of Devon. Immediately to the south of the junction at Hope Cove, the crystalline slates are extremely Physical Structure and older stratified Deposits of Devonshire. 659 altered and mineralized. Some are yellow, earthy, and pyritous; others have become entirely earthy, are of a bright red colour, and, in their strike through the country, may be tracked through the fields by the red colour of the soil. Others, again, are partially indurated; and we may here and there extract from them hard, laminated bands of quartz and chlorite; and among them are irregular masses of earthy, pyritous, decomposing chlorite. The beds, however, soon acquire a more usual mineral structure; undulate towards the south; at Bolt Tail become nearly vertical; and afterwards pass, in a highly-inclined position, and after repeated undulations, to the extreme southern headlands. The prevailing dip is, however, to the north; and the strike is nearly true east and west. In mineral structure, this group is entirely different from anything we have described in the sections either of North or South Devon. It is highly crystalline, and essentially composed of quartz, mica, and chlorite; the three minerals being frequently found together. Near its northern limit are some fine-grained, well-bedded rocks of blended quartz and chlorite, sometimes used as a building stone. More frequently it rises in large flaky masses, coated beautifully with mica and chlorite, and is used as a coarse flag-stone and coping-stone. In other places, from the oc- currence of joints, the blocks are obtained in rude prisms, provincially called pencils, not unusu- ally coated with red oxide of iron. The masses have both small and great contortions, so that it is difficult to find beds with smooth plane partings. Towards the south, however, (e. g. near Prawle Point,) we obtained beautiful and finely-laminated chlorite slate; and there are similar specimens of mica slate. On the whole, mica seems to abound more towards the southern, and chlorite towards the northern, extremity of the group; but the different varieties are so con- stantly mixed together, that it is impossible to divide the crystalline series into two formations. Felspar does not appear to exist as an essential constituent, nor did we see a single block to which we should give the name of gneiss. Pyrites is found in many of the beds; and oxide of iron not merely coats the joints, in some cases producing what the workmen call iron pencil, but the mineral exists in regular veins traversing the micaceous slate. The finest example is at Sea- combe Sands, (near the mouth of the rivulet that descends from West Prawle,) where there is a vein of iron ore about four feet wide, and another smaller vein near it. It strikes nearly east and west, and underlies nortb, at an angle of 50°. Had it been more nearly vertical, it might, perhaps, have been worked to profit. On the east side of Gunnor Head, near Prawle Point, is a similar vein striking north and south, and underlying west at a great angle. Works have been opened in this vein, but are deserted. There is also an iron vein at Stenhall, on the east side of Bolt Head, and another about two miles further west. This beautiful but anomalous group is probably of metamorphic structure, and had entirely escaped notice before the commencement of the elaborate county survey of Mr. De la Beche. 4.—Section from Berry Head to Start Point. (PI. LI. fig. 6.) It only remains for us to describe in a few words the section connecting the Torbay limestone with the crystallized slates of Start Point. We have before stated that the limestone of Berry Head is thrown into an arch which brings up the inferior slates in the cliff of Mudstone Sands (p. 652); and the same arch is continued in the calcareous system towards Galmpton. The earthy slates of Mud- stone Sands become more and more calcareous and fossiliferous in the ascending section, and so gradually pass into the limestone. In the same manner, on the north side of Galmpton Creek we VOL. Y.—SECOND SERIES. Ae 660 Professor Sepewick and R. 1. Murcuison, Esq., on the meet with the following ascending section: Ist, red sandstone and slate; 2nd, red, gray, and leaden-coloured earthy slate, almost passing into shale; 3rd, red and gray indurated shale and calcareous slate, with organic remains, and passing into the limestone. It is therefore obvious that the great limestone is intimately linked to the lower slaty system. — On the south side of the great saddle of Mudstone Sands the limestone again appears in the cliffat Sharkham Point with a high southern dip. The beds are confused and contorted by the passage of a great vein of iron that is worked, in the limestone, as far as Upton. A very little south of the iron vein is an interpolated mass or dyke of trap which breaks out, here and there, in some ridges ranging to- wards a point north of South Down. Beyond the trap, the beds of limestone are seen in the cliff with a very rapid dip to the south; but some of them appear to thin off and almost to come to an edge in the line of dip. The scale of our section enables us to represent these phenomena only in a general way. Notwithstanding the confusion on the coast produced partly by the iron vein and trap, the general mass of the limestone from Sharkham Point to Upper Brixham dips uneqivocally south, and so passes under the great slaty group that is expanded towards the mouth of the Dart. From all which we conclude, that the limestone of Berry Head has exactly the same general relations to the slate series of South Devon, as the Plymouth limestone*. 1. The beds immediately over the limestone of Sharkham Point are made up of a gray glossy slate, dipping at a great angle about south by east. They are succeeded by gray, greenish gray, and variegated soft earthy slate, alternating with sandy red and variegated micaceous flag-stone, which occasionally passes into coarse thick beds. Some of the beds exhibit remarkable contor- tions, and a series of specimens might be selected from them which would be almost identical with a corresponding series from the beds of the first group over the Plymouth limestone. The red sandstone does not, however, here predominate so much as it does near Plymouth. The rocks above described prevail as far as Man Sands; or the south side of which is a soft silky gray slate, exhibiting at one single spot obscure traces of organic remains. This slate is over- laid, near the top of the high cliff going over to Scabbacombe Sands, by coarse arenaceous red rocks, like those above described. But they are again succeeded by a fine soft gray and greenish gray shillat, which, with many changes of texture and with many quartz veins and alternations of quartzose, arenaceous bands, is continued to the mouth of the Dart. On the whole, we think we may place the southern limit of our present group at Scabbacombe Sands : so defined, it is very nearly the representative of the red arenaceous group, above described, over the Plymouth limestone. Tt is, however, less perfectly developed than the corresponding Plymouth group, and, though on the same general line of strike, is a little further north, in consequence of a gradual change in the run of the beds. The rocks south of Galmpton on the Dart agree in their general character with those of the present group; the boundary of which may be placed on the north side of Dartmouth, but, from * On the north side of Mudstone Sands, the calcareous beds overlying the slates have a distinct slaty cleavage, which does not affect the inferior slates at the top of the cliff. Among some slightly undulating beds, are dip-joints pointing between north and magnetic north ; afterwards the beds have a steady dip about magnetic north ; and the dip-joints, which abound, are exactly magnetic north and nearly vertical. At the same place are magnetic east and west joints (strzke-joints), the planes of which are inclined magnetic south, 40°; that is to a point opposite to the dip of the beds, a very usual case. Not far from these beds are some masses of very coarse red sandstone, which seem to be subordinate to the earthy slates below this limestone. | ——— Physical Structure and older stratified Deposits of Devonshire. 661 the continual changes of mineral structure, no two distant sections can agree in their more minute details. The further range of the arenaceous series westward seems to be marked by the hard, irregularly bedded, gray quartzose rocks of Morleigh Down and Black Down, first noticed by Mr. De la Beche*. 2. Over the preceding group, and not separated from it by any well-defined limit, is expanded a slate formation of vast thickness. Soft glossy chloritic slates prevail, and alternate with arena- ceous bands, and near Redlop Cove with a remarkable ferruginous whet-slate. Near Stoke there are some beds of flaky or semiconcretionary structure, like many beds associated with contempo- raneous porphyries in Wales and Cumberland. Here, however, we saw no traces of trappean rocks. A little sonth of Stoke are some very fine beds of chloritic slate, exhibiting those wavy lines among the lamine, which produce what we have called a false stripe ; but there were no examples of an oblique slaty cleavage. For a considerable way north of Street the dip is reversed to N.N.W., but soon after recovers, and dips about magnetic south at a great angle. No calcareous beds fit for use are found in this series; but near Slapton it is overlaid by horizontal masses of new red conglomerate, which has been burnt for lime. ’ Near Torcross the dip is reversed to the north; and in a cliff to the south of it is a gray, greenish gray, and blue slate, with many quartz veins, generally parallel to the beds, but continually thinning out and running into filamentous veins. With these beds we found some long, flat, cal- careous concretions : but we did not observe any organic remains, in this or any other part of the group. On the whole, the mineral phenomena, on this part of the coast, though differing in a thousand accidents, agree in all their essential circumstances with those exhibited by the corre- sponding group in Bigbury Bay. 3. For some way beyond the beds last described, the dip is nearly north at a great angle—on the average not less than 60°. A long flat region then conceals the relations of the strata; beyond which the crystalline group, commencing more than a mile south of Tor Cross, occupies the coast to the extremity of Start Point. ‘The highest beds of this group are nearly perpendicular—they are then thrown into cortortions—and then for a considerable way along the southern cliff have a steady dip to the north at an angle of about 50°. Still further south they exhibit the same modi- fications of mineral structure that we remarked in the cliffs between Bolt ‘Tail and Prawle Point. At their northern limit they are certainly less crystalline than at their southern. Some of the beds contain many elongated concretions of quartz, spangled with flakes of mica or coated with chlorite, alternating with laminz of dark chlorite slate; and associated with these are beds of very fine dark clay slate, of a structure intermediate between the slates of the second group and the crystalline slates of Start Point. It is obvious from what is stated, that there is no true passage between this and the preceding group; nor are the phenomena at the junction so instructive as those which occur at Hope Cove. Such is the succession of rocks exhibited in transverse sections of South Devon ; the whole ascending series being divided into four groups : 1. The slate-rocks bordering on Dartmoor, many parts of which are indu- rated and altered in structure by the action of the granite. * Ina traverse from Totness to Kingsbridge we crossed a series of red arenaceous slates which seemed to represent, under a different type, the great upper limestone and its associated red grit. Near Kingsbridge the beds are highly inclined and thrown into great undulations, caused per- haps by the same disturbing forces which produced the undulations near Avon mouth. 4Q 2 662 Professor Sepewick and R. I. Murcuison, Esq., on the 2. A great zone of slates, more or less calcareous, and with subordinate beds of limestone: the lower portion containing the Ashburton bands; the upper containing the great Plymouth and Tor Bay limestone. The upper portion also contains occasional beds of red slate and sandstone ; which some- times appear under the limestone, and sometimes seem to take its place along the lines of strzke. 3. A great arenaceous group, containing many beds of red and variegated sandstone. 4. A group, with many courses of soft, glossy slate ; sometimes indurated, and used for roofing-slate ; alternating with coarse quartzose bands ; without any subordinate beds of limestone, and apparently without fossils. These four groups complete the ascending series, and are, together, of an enormous thickness. 5. Lastly; a crystalline group of micaceous and chloritic slate, unlike any other formation in North or South Devon; not co-ordinate with any of the groups above described ; probably of metamorphic structure, and due to some obscure axis of elevation, which has passed near the southern promontories of the county, and interrupted the succession of the regular ascending series. Conclusions. 1. Comparing together the regions of North and South Devon above de- scribed, we find many points of resemblance, and some points in which their structure is remarkably contrasted. | For example, trap rocks abound on some portions of the southern sections, but are never found in the northern. Again, in the northern region, a true transverse slaty cleavage is constantly developed among all the finer deposits ; while in the southern, these cleavage planes are almost wanting, and nearly all the roofing slates are obtained from lamine parallel to the stratification. Yet in South Devon, systems of parallel joints are as common as in North Devon. What physical conditions have led to this remarkable difference of structure we do not at present inquire. 2. Judging both from the mineral structure and organic remains of the two regions, we are justified in affirming that neither of them exhibits any very old class of slate rocks. For example, none of the groups, either of the northern or southern sections, are to be compared with the rocks of Snowdonia or the green slates of Cumberland ; without including in our comparison the still lower group of Skiddaw Forest. 3. The preceding details show that there are many points of physical re- Physical Structure and older stratified Deposits of Devonshire. 663 semblance in the successive groups of North and South Devon ; and that there is a near resemblance in many of the fossils, especially the corals. Hence we should provisionally refer them to one system. But as there are no sections connecting them unequivocally with well-ascertained formations, a more exact comparison and place of the several groups must depend on a future examina- tion of the fossils. 4. Attempting, however, provisionally to bring the groups of North and South Devon into direct comparison, we were first induced to compare the highest calcareous group of North Devon (No. 5.) with the great upper lime- stone of South Devon. The two formations in a part of their range are asso- ciated with red sandstone ; several of their fossils approach the carboniferous type, and some of their corals are specifically the same. But we were led to reject this hypothesis, chiefly because it left the great upper group of the South Devon slates (No. 4) entirely unaccounted for in North Devon. 5. The Ilfracombe calcareous slates very closely resemble (as above stated) some of the upper calcareous slates of Plymouth and Tor Bay. But if we rigidly identify the Ilfracombe limestone with the upper limestone of South Devon, we have the great red arenaceous group of Plymouth entirely unac- counted for in North Devon. On the other hand, the great red arenaceous group of North Devon (No. 2.) is, in its magnitude and general structure, almost identical with the great red arenaceous group over the Plymouth lime- stone. Notwithstanding our distrust of mere mineral characters, we seize on these groups as our best terms of comparison. On that hypothesis, the lower divisions of the South Devon section would be geologically lower than the lowest members of the North Devon section ; (which may be easily admitted when we regard the vast thickness of the descending series between Avon Mouth and Dartmoor (see PI. LI., fig. 5 & 9.)); and the calcareous slates of Linton would be nearly on the parallel of the Plymouth limestone. 6. Not, however, to push these analogies too far, we would, in a general way, bring the great calcareous and arenaceous series, between the North Devon Foreland and IIfracombe inclusive, into comparison with the arenaceous and calcareous groups on Plymouth Sound ; on which hypothesis the lower groups of South Devon are unrepresented in North Devon ; and the slate rocks south of the Ilfracombe limestone (group No. 4.) may be compared in a ge- neral way with the great upper slate group of South Devon. We throw out these conclusions merely as provisional, and to be confirmed or invalidated by a more complete examination of the organic remains in the several groups. 664 Professor Sepewicx and R.1. Murcuison, Esq., on the Slate Rocks of Cornwall. Before we proceed to describe the culmiferous series, we must notice the relations of the successive groups of North and South Devon, above described, to the slate rocks of Cornwall. The Plymouth limestone, as before stated, thins out toan edge in Whitesand Bay, being there represented by some in- considerable beds of red calcareous sandstone and calcareous slate, with frag- ments of encrinital stems, and a few other organic remains. Nor does it again appear on the south side of Cornwall; being apparently cut off by the trending of the coast to the north-west of its line of strike. But the lower division of the fossiliferous slates of South Devon does pass into Cornwall, and gradually deflecting to the south-west, ranges through the cliffs at the mouth of the Looe River, through the hills near Talland, and thence by the hillabove _ Lantivet Bay to the mouth of the Fowey river. The same calcareous slates reappear on the other side of the river, and are traced continuously through Greber Head, the south-eastern promontory of St. Austell Bay. At all the above-named places fossils are abundant, though generally in the form of casts, and sometimes much obscured by cleavage. From the beds near Fowey we obtained several specimens of a large, deeply-ribbed spirifer, casts apparently of terebratulz, stems of encrinites, and several fragments of corals. The same calcareous slates, sometimes passing into impure limestone, reap- pear near Veryan, and thence descend into the cliff towards the north end of Gerran’s Bay—the last place where we found any traces of organic remains on the south coast. At Gerran’s Bay the strike deviates so much towards the south, that none of the calcareous slates pass through the cliffs that extend to St. Anthony’s Head. In their further range, they again undergo a considerable flexure towards the west, which brings them nearly to the mouth of the Helford river; from which they strike, on the north side of the great plateau of caverns to the opposite coast of the Lizard district. After what we had seen in South Devon, we were not surprised at disco- vering occasional traces of fossils along the lines above indicated. We were, however, astonished at the extraordinary number of organic remains in some parts of the country hitherto described as not fossiliferous. The calcareous slates are not confined to the line here indicated, but break out, on the eastern side of Cornwall, at considerable distances from the coast*. * For example, there is limestone imbedded in slate about half a mile south of Hessenford ; also at Catchfrench, a mile and a half above Hessenford ; and at Coldrenick, a little east of Clicker Tor, &c., &c. Physical Structure and older stratified Deposits of Devonshire. 665 To the east of Looe, a section from the coast to the nearest granite exhibits on the whole a descending series ; yet we do not think that any of the beds of such a section ought to be placed at a lower geological level than the lowest slaty group of South Devon. In the cliffs west of Looe there are many fine green, chloritic slates, alter- nating with greenish quartzose beds, penetrated by quartz veins, which have a prevailing dip about S.E. by S. But at Ore Point is a striped rock, with numerous red and green bands, alternating with coarse green, quartzose beds, much penetrated by white quartz veins. The dip is reversed to a point about N.N.E., and is not less than 70° or 80°; and some of the beds have a true slaty cleavage inclined towards the same point, but at an angle of not more than 50°. The coarse striped beds, sometimes alternating with bands of nearly pure quartz (very instructive, from their mineral structure, and from a number of poor mineral veins nearly parallel to a series of north and south joints), are continued nearly with the same inclination to Polparrow. At the entrance of Polparrow Harbour, the coarser quartzose beds are overlaid by a beautiful rock, with a perfect transverse cleavage, producing a fine-striped slate. The beds dip north, at a great angle, while the cleavage planes dip also north, but at a much smaller angle. Hxamples of this kind occur very rarely in South Wales; and we never remarked a similar case in the North of England ; for whatever be the inclination of the beds, the cleavage planes are generally inclined at a greater angle*. As the same prevailing northern dip is continued to the mouth of the Fowey river, it is obvious that the beds above described are inferior to the fossil- iferous group. Similar indications of a northern dip are seen in a part of the coast section on the east side of St. Austell Bay. Commencing a section at Greber Head, and coutinuing it from thence through the head of St. Blazey Bay to the gra- nite, we have the following order : 1. A series of quartzose and chloritic beds, continued to a cave under Combe Farm, with a prevailing dip towards the south. At that place there are large east and west joints, perhaps marking the presence of a fault; and beyond them the dip is reversed to magnetic north. The same phenomenon is also seen about a quarter of a mile south of Polkeris. 2. An ascending series, with a northern dip at a great angle, continued to Polmere Cove, where there appears to be a great break among the stratat. The fossiliferous slates are in the lower part of this group. * On the coast west of Padstow we found a still more remarkable example, viz. a calcareous slate, dipping unequivocally at an angle of 40°, intersected by true horizontal cleavage planes, producing a beautiful striped slate. + Somewhere near the line of break, and probably connected with it, is a great channel of 666 Professor Srepewick and R. I. Murcuison, Esq., on the 3. A series of highly mineralized beds, with a southern dip, and extending to the granite. This division is traversed by some elvans, and numerous metalliferous veins ; but there is no proof that it is of an older date than the second group: indeed, judging from the sections, it only seems to represent the upper part of that group reversed and mineralized by the granite, and by the causes, whatever they may have been, which produced the mineral veins. The section from the Dodman point to the St. Austell granite, exhibits still more striking phenomena, in the following order : 1. A series of rocks dipping to the south-east, and extending from the Dodman to the cliffs south of Porthmellion. 2. A series of nearly similar rocks, extending to the cliffs south of Mevagissey, and exhibiting several anticlinal and synclinal lines—their most prevailing dip being, however, to the north side of the strike. 3. A long ascending series, continued close to the granite, in which there is a decidedly prevailing dip, and generally at a great angle, towards the north. From the preceding facts, it appears that a line of elevation, nearly on the strike of the beds, has thrown the greater part of the Killas between Veryan Bay and Looe into an irregular trough ; and that the crystalline, metalliferous slates skirting the south side of the St. Austell granite, instead of being among the oldest, are among the very newest stratified rocks of the south-east side of the county. Nor does the mineral structure of the country throw any difficulty in the way of this conclusion. Many of the beds south-west of St. Austell are coarse, arenaceous, and sometimes ef a red colour. Near Pentowan there is a series of coarse brown grits, almost resembling coal-measure sandstone ; near Mevagissey and Porthmellion there is a eoarse, dark-coloured slate, with specks of mica between the layers, much penetrated by quartz veins and alternating with arenaceous flagstone; further towards Gerran’s Bay are thick courses of quartz rock closely resembling the masses of quartz rock in the great arenaceous group of South Devon; and in Gerran’s Haven we meet with many very coarse arenaceous beds deeply impregnated with yellow hy- drate of iron, alternating with bands of yellowish red and dark blue earthy schist. The ferruginous beds are carried to the west side of the promontory, where they are associated with masses more coarse and mechanical than those above described ; and the quartz rock reappears in a rugged elevation south of Boswingran, and near Carhaise Bridge. We mention these facts to show the mechanical nature of many portions of this deposit. Other alternating portions have the usual characters of the finer chloritic slates of Cornwall. manganese and iron, which ranges near the following places: Polmere, west side of Tywardreath Hill; East Polmere ; Terras Hill, on the north side of Lostwithiel ; and Restormel Ground ;—the course being about N.N.E. Physical Structure and older stratified Deposits of Devonshire. 667 The same group on the north side of the Lizard serpentine also contains calcareous beds ; not, however, passing into true beds of limestone ; nor have organic remains been yet found associated with it. Among its upper beds are masses of coarse arenaceous rock, and beds of a very coarse red conglomerate ; and south of Mawnan it contains a few very thin carbonaceous lamine *. Before our visit in 1836, Mr. De la Beche had completed his survey of the north side of Cornwall, and laid down his results in admirable detail on the sheets of the Ordnance map}. These he kindly communicated to us ; so that in the few spots we visited to the south of Padstow, we only trod in his steps ; on which account we avoid all details respecting this part of the north coast. ‘The section from the slate rocks north of the Lizard to the cliffs north of St. Ives Bay, appeared to us symmetrical. On both sides the Aidlas is thrown off by the granite ; and among the slaty and arenaceous beds which appear not far from Godrevey Island, are some cellular calcareous beds with ferru- ginous bands containing obscure traces of organic remains. One of the larger arenaceous masses reminded us of the Pennant stone of Bristol. We think we may safely consider these beds as very nearly the equivalents of a part of the group, north of the Lizard, which strikes into the coast near the mouth of the Helford river. All the country round St. Agnes is so altered by the granite of Cligga point, by injected Elvan dykes, and by innumerable metalliferous veins, that we attempt not to define its exact geological relations—only remarking by the way, that after the facts stated above, we have no right to place the more crystalline slates of that district in any system lower than the groups above described. Before our examination of the north coast, Mr. De la Beche had collected fossils from New Quay and other localities near the coast ; also on the Padstow river, even so far up as the neighbourhood of Bodmin. We traced the cal- careous slates with Encrinites, corals, and other fossils, through the cliffs north of Mawgan Porth; and the series is continued into Permizen Bay, west of Padstow, where we had seen the calcareous slates with fossils during a former visit to the county (1828). South of the Padstow river there are many irre- gular contortions ; and the strike and dip undergo many changes, so that the fossiliferous slates are spread over a wide surface. It is obviously (after what we stated respecting the position of the beds south of St. Austell Moor) almost impossible to find any transverse section that will clear up the relations of the * See Transactions of the Cambridge Philosophical Society, vol. i. p. 295. + This map is not yet published ; but a reduced copy of it appears in the lately published Re- port on the Geology of Devonshire and Cornwall. (1837.) VOL, V.—SECOND SERIES. AR i : {} | } ib | {\ 1 { i ; | | | 668 Professor Sepewick and R. 1. Murcuison, Esq., on the fossiliferous slates on the corresponding parts of the north and south coast. Provisionally, we identify the calcareous slates of New Quay, Padstow, &c., with the calcareous slates of Looe and Fowey. We see no reason whatever for considering one series older than the other ; but fora final determination of the question we must look to a future examination of the fossils. The best fossils we possess from the coast near St. Columb Porth, we owe to the kind- ness of our friend Mr. Carlyon of Mawgan. Among them are Encrinites, two or three species of Orthoceratites, and several species of corals, &c. The fossiliferous slates near Tintagel (first noticed many years since by Pro- fessor Buckland and Rey. J. J.Conybeare), cannot perhaps be connected by the direct evidence of sections with any of the preceding calcareous groups. The most remarkable fossil in these slates is a very large broad-ribbed Spirifer; and we found a similar fossil among the highly crystalline lamine of the slates near Lesnewth, in the range of the slaty mass several miles further to the east. Calcareous slates, very nearly on the same line, after doubling (along with a great series of inferior beds) round the granite, are carried by a strike about E.S.E. to the quarries near Trenalt and South Petherwin. From the very numerous fossils in these quarries (among which are many large broad-ribbed Spirifers, Producte, Terebratule, two or three species of Orthoceratites, many corals, Encrinites, &c.,) on the whole, nearly resembling those of the great upper limestone of South Devon ; we should place these calcareous slates in an upper group of the great slaty series: and the conclusion is confirmed by the fact, that a section from South Petherwin to the granite, in a direction transverse to the strike (¢.e. about S.S.W.), exhibits for five or six miles a regular descending series. ‘These calcareous rocks are, in respect to the great overlying culm-trough, exactly in the same position with the calcareous slates of Barnstaple ; but on this fact, considering the ambiguous relations of the base of the culm-measures to the rocks on which they rest, we do not at present build any inference. From the preceding details we conclude, that whatever classification be given of the slate rocks of South Devon, must also include all, or nearly all, the slate rocks of Cornwall. They form one continuous system, the several parts of which admit no comparison as to age, except that which is sanctioned by the evidence of sections and fossils. The slates of Cornwall are, on the whole, more crystalline than the slates of South Devon,—a fact, however, on which no classification can be founded, as the upper groups, when near the granite, are as crystalline as the lowest. Again, many of the subordinate beds in Cornwall are as mechanical in structure as the very coarsest beds in South Devon. Physical Structure and older stratified Deposits of Devonshire. 669 The general absence of transverse slaty cleavage, in the parts of the coun- ties we are comparing’; the occasional appearance of that structure, especially among the calcareous portions; the occasional appearance of a second oblique cleavage plane ; systems of dip-joints and strike-joints changing with the change of strike ; and many other common accidents of structure (not to mention mineral veins, elvans, contemporaneous trappean rocks, &c. &c.), may also be considered collectively to bear out our previous conclusion. We have thus cleared the way for a description of the great overlying culm-mea- sures of the central region of Devon. Cuar. 1V.—Culmiferous Series, Its relation to the other Formations, Struc- ture, Fossils, &c. (Plate LI. fig. 1, 2, 3, & 4.) We have before stated that this series occupies a great trough, the axis of which ranges nearly east and west ; and we have also indicated its north and south boundary in general terms. A formation may, however, be deposited in a trough, and yet the beds on its opposite sides may not exactly correspond. But in this instance there is no such ambiguity ; for the bottom beds of the series have a peculiar mineral structure and are characterized by great beds of black calcareous shale and black limestone, with peanhes fossils, and these appear on both sides of the great trough. That these lower beds rest on the highest group (No. 5.) of our northern section we have already given abundant proof. ‘They are overlaid by an enormous thickness of contorted beds of shale and sandstone ; and, by a re- versal of the dip, are finally brought out again to the surface and seen resting on the slate rocks of Cornwall and Devon, and on the northern flank of Dart- moor. The trough is therefore symmetrical, and the true bottom beds of the whole series may be studied in detail either on its northern or southern boun- dary. We have, therefore, a most unequivocal proof that the culm-measures are newer than any of the stratified groups associated with them. It may be contended, that there is a passage from the base of the culm- measures into the old slate rocks of Cornwall and Devon ; and there may well be a mineralogical passage where both formations alternate with trap, or ap- proach the granite, and so become metamorphic: but passages of structure proving a real continuity of deposit must always be difficult to establish among old slaty rocks, where similar beds recur at such enormous intervals. We must, however, allow that dark slaty beds and indurated shales occur in seve- ral places (for example, near South Petherwin ; in a mining work on a moor 4r2 a age SOATEST ee 670 Professor Sepewickx and R. I. Murcuison, Esq., on the west of Lammerton ; and at the western end of Wheal Friendship * ;) at the base of the culm series, which it is extremely difficult to separate from the lower rocks ; but there is no ambiguity as to the order of superposition. In. like manner, in North Devon, the beds of the highest group above described (No. 5,) pass regularly under the base of the culmiferous rocks, without the intervention of any conglomerate, or other appearance marking an interrup- tion of deposit. But when one shaly mass rests on another, and is mecha- nically derived from it, we need not wonder at such a mineral passage. We have seen the old red sandstone on the coast of Caithness resting on gra- nite and forming a most distinct mineral passage into it: and it was from overvaluing such apparent passages, that Macculloch was, for many years, led to regard the old red sandstone of the northern coasts of Scotland, asa part of his primary system. On the whole, therefore, we consider these supposed passages of little value in determining the age of the culm series, which we shall endeavour to discuss on other evidence fF. Lower Culm Measures. The lower part of this series is made up of dark-coloured shale ; sandstone, sometimes coarse, but very rarely passing into a conglomerate; siliceous flagstone ; and calcareous shale, here and there, containing subordinate beds of black limestone. The several members of the group are irregularly developed, and one part is expanded at the expense of the others; but the calcareous portion is very constant, and its position is near the top of the lower division. Where the bot- tom shales rest on the earthy slates of the older groups, it is not always possible to determine the exact boundary of the two formations. This difficulty, however, such as it is, very seldom occurs; as the inferior group abounds in fossils, while the culm slates are without fossils, and are also distinguished by their structure, being black and pyritous, and by occasional anthracitic stains between the lamine. * The western end of Wheal Friendship, (an east and west copper vein,) near St. Mary Tavy, undoubtedly runs into the lower culm-measures; the inferior and productive sinkings are pro- bably in the older slates. On the other hand, Wheal Betsey, a north and south lead vein of the same mining field, is entirely in the lower culm shales and grits. We first thought an important inference might be drawn from this fact; but we afterwards found several east and west copper veins, further north, in the undoubted culm-measures. + We forbear to describe the confused junctions near Chudleigh ; where one of the great fos- siliferous limestones of South Devon is surrounded by, and might seem to be imbedded in, the culmiferous rock. The phenomena are easily explained by the intervention of a fault. Neither do we purpose to describe in any detail the complicated junctions near Ugbrook Park, or an out- lying basin of culm-measures south of Newton Bushel. All that side of Devon is extremely dis- located ; but the phenomena may be all explained, when the true order of superposition has been once settled on the evidence of uninterrupted sections. Physical Structure and older stratified Deposits of Devonshire. 671 These shales, in the ascending sections, frequently become semi-indurated ; and in that condition are generally thin-bedded, and the separate beds are divided into innumerable prismatic masses by small transverse joints. In the softer varieties these masses are generally rhombohedral. Again, the indurated shales pass into rather thin-bedded, hard, siliceous bands, each of which becomes sepa- rated into cuboidal divisions ; and the surfaces of the beds have what the workmen call a diced form, resulting from the intersection of parallel cross joints. This structure seems to be derived, in a great measure, from a tendency to a concretionary structure. These harder bands are often of a dark colour, and the partings are coated with earthy carbon, which stains the fingers. It is among the little transverse cracks and joints of the harder beds that a white earthy mineral greatly abounds. The white divisional planes are due sometimes to carbonate of lime ; but through a considerable tract running near the base of the culm series (between Barnstaple and South Moulton) the white mineral is chiefly composed of earthy Wavellite ; and occasionally the broken transverse joints exhibit the ra- diating crystals of that mineral in great perfection*. Still larger parallel joints, affecting the whole series, also occur ; but these we are not at present describing. The same hard bands vary, however, greatly in colour, where the carbon is not present; and in several places they pass into a light gray, siliceous, brittle, jointed flagstone: and again, in some remarkable instances, they become almost white and porcellaneous, resembling a kind of china stone. Again the siliceous beds pass into a regular thick-bedded sandstone, resembling a coarse gray-wacké, or a grit of the coal measures : these latter varieties are, however, on the northern boundary (from which our present descrip- _ tions are chiefly taken) to be considered as the exception rather than the rule, and as subordinate to the carbonaceous shales and flagstones. The beds forming the base of the culm series are somewhat differently developed on the south- ern boundary, in their range from the Cornish coast towards Dartmoor. We first meet with a highly carbonaceous and pyritous shale, dipping at a great angle from the chloritic and fossiliferous slate group of Tintagel. These alternate with coarse quartzose bands, sometimes thickly bedded, and resembling coarse beds of gray-wacké. The whole system is much intersected by joints, and traversed by Jarge quartz veins+; and has so much the look of an old rock, that it has always been regarded as a regular part of the old slate series of Cornwall. The mineral character, how- ever, as well as the superposition, is sufficiently distinct ; and in several places (for example, on the north side of Boscastle) the coarser bands resemble a coal grit, are stained with carbon, and contain many very thin lamine of that substance {. Some of the shales are also calcareous, and contain masses of a variety of rottenstone, like that in the limestone shales of Derbyshire; but none of them contain any fossils resembling those of the older Tintagel slates. Among the higher beds of the series, we have a great development of black, semi-indurated shales; but no true bands of black limestone ; and the whole group is violently contorted. Following this bottom group to the east, along the line of strike, we still find the dark lower shales more or Jess carbonaceous, and with traces of bright anthracitic laminz ; and here and there (though rarely) with obscure traces of vegetable fossils§. And along the same line, further * The same mineral occurs among the indurated coal shales of South Wales. + These veins are sometimes several feet in thickness. They usually run parallel to the beds for some way, and then come to an edge, or break off into small strings, ramifying through the neighbouring beds in all directions. { These beds, or some resembling them near Boscastle, were first described by Dr. Boase, in the Transactions of the Geological Society of Cornwall, vol. iv. p. 426. § The descriptions of the preceding paragraph are taken from the lower culm beds near Bos- 672 Professor Sepewick and R. 1. Murcuison, Esq., on the east, the siliceous beds become so much expanded as greatly to predominate over the rest, and to give a character to the features of the country. ‘Thus we cross, on the road towards Launceston, great tracts of arid soil resting on gray gritstone, which lies bleaching on the surface, and reminds us of the sterile ridges of a millstone grit country. Partly in consequence of a thickening of this bottom series, and partly in consequence of a de- viation in the strike towards the south, this remarkable deposit of gritstone is carried to the south of Bren Tor; and from thence, deviating considerably towards the north, and skirting the mining- field of St. Mary Tavy, passes into the high ridge of Black Down, and abuts against Dartmoor. Further towards the north-east, all the bottom grits and shales of the culmiferous system come up to the granite in succession, as may be seen in a traverse from Oakhampton to Tavistock ; and the higher beds of the group then sweep round the northern promontory of the granite. In this part of their course they are greatly altered in structure, and have even been mistaken for primary rocks. Their changes in structure are, however, due to two causes. 1st. They alternate with many beds of trap, and have their texture greatly changed in consequence. But surely no one will now contend that, on this account, they ought to be cut off from the other culm measures on their strike. 2ndly. When near the granite, the whole system becomes highly metamorphic. Should any one contend that the hard crystalline series between the coarse culm measures south of Oakhampton and the granite of Dartmoor, belong to a distinct group; we may reply, that the hypothesis is contradicted by the strike of the beds, and, above all, by the existence of beds of indurated black shale passing into Lydian stone, and black culmiferous limestone, (incontestably a portion of the true lower culm group, not yet described,) which pass through the heart of this altered group. And we might add, that, in the accidents of stratification, and in the existence of fine seams of Wavellite in the joints of the black indurated shales, we have additional analogies confirming our statement. The complete demonstration of the general correctness of our views is, however, to be sought on the flanks of the granite hills to the south-west of Oakhampton. A traverse in that direction shows us the successive members of the group we are describing, as they range towards the granite one after another ; and each, as it approaches the central rock, is found to undergo an appropriate change. ‘Thus the dark shales put on the form of Lydian stone, and sometimes of compact felspar; and the quartzose bands, under the same conditions, are converted into a hard crystalline quartz rock. Close to the granite, the changes are more complete ; the masses become utterly metamor- phic, and put on the form of white compact felspar, micaceous crystalline slate, castle. In their eastern prolongation, the pyritous shales near the bottom of the series become, in some instances, much indurated, and in a quarry about a mile from Launceston, on the South Petherwin road, are used for roofing slate. They contain vegetable impressions, and are of very bad quality, being injured by disseminated pyrites. The slate of Yeolm bridge (about two miles north of Launceston) is of much better quality, being derived from much harder beds, with a transverse cleavage plane, producing a smooth striped slate. The rock may, perhaps, be indurated by the neighbouring trap, which does not, however, appear in the quarries. It contains some organic remains, and is in a much higher part of the series which we are describing than the in- durated pyritous shales above noticed. Physical Structure and older stratified Deposits of Devonshire. 673 gneiss, &c. &c. Nor is this all. The granite sends out veins into the altered beds, of which we found an example, not merely in the metamorphic beds of contact, but in a black, indurated shale, at a considerable distance from the junction, in one of the ravines south-west of Oakhampton. — Moreover, there is an Elvan dyke (precisely like the Cornish Elvan) still further north, in the central portion of the culm measures, far above the group now under notice*. Phenomena like these, where cause and effect are so clearly brought toge- ther, are of no small interest. ‘The metamorphic group is one of the most instructive we have ever examined, inasmuch as we can trace it through all its gradations : and the facts we have stated prove to demonstration, that the gra- nite is not older than the stratified series. And that it is not contemporaneous with the altered group, which is made up of a long series of mechanical de- posits, is too obvious to require a proof. ‘There remains, therefore, only one conclusion, (sanctioned by all the changes of position and structure, as well as by the protruded veins,) that the granite in mass is a rock of protrusion, and of a date posterior to the development of, at least, all the lower divisions of the culm measures. We must now briefly describe the black shales and limestones which form the upper division of our present group, and are, indeed, its most characteristic and important members. ‘These beds have so many characters in common, that the same descriptions will serve, with a few exceptions, for the black lime- stones both on the north and south side of the great culm trough ; and on both lines it is extensively worked in a succession of large open quarries, in several of which are vertical sections more than 100 feet deep. This upper division is regularly bedded, and essentially composed of black carbonaceous shale, tra- versed by numerous irregular white veins of calc-spar, and alternating with beds of black limestone. The limestone is also filled with white veins ; and being of a rather earthy structure, is only distin- guished from the calcareous shale by close inspection. Among the more calcareous bands some are fossiliferous, containing a great abundance of at least two genera of bivalve shells; one a Posidonia, the other of a genus not ascertained, but regarded, by those who have examined it, as a marine shell. Inthe same part of the series are Gonialites of at least two species, both of which are unquestionably marine, and (according to Professor Phillips) identical with Goniatites of the Yorkshire coal-field. And there is a negative fact also of great value. This culm limestone contains no fossils resembling those of the groups inferior to the culm series. The beds in ques- tion are therefore not more distinguished by their structure from all the calcareous strata of the inferior groups, than they are by their fossils. Yet the black culm-limestones and the calcareous slates of the older system, sometimes range almost side by side. This shows the absolute neces- * This Elvan was first laid down by Mr. De la Beche. | | ee 674 Professor Sepewick and R. I. Murcutson, Esq., on the sity (whatever may be its age) of mapping the whole culm series by a colour distinct from that of the older slates. The group we have been describing is of great thickness, and the calcareous portions are several times repeated on the same section ; and not only in the shales, but also among the limestone bands, are thin lamine of culm, but in no instance so thick as to be of economical use. It is difficult to esti- mate the whole thickness of this portion of the lower culm group, because the beds are repeated by contortions, which in some instances are so violent as to exhibit many salient and re-entering angles like those of a fortification agate. On the whole, however, the limestones and associated black shales plunge away from the older rocks, and gradually disappear under the upper culm-measures. On the south side of the culm-trough, the shales both above and below the black limestone are occa- sionally used for roofing slate. Thus, on the banks of the Lyd, near Coryton, there is a line of slate quarries apparently wnder the neighbouring range of the black calcareous rock, which, though excessively contorted on the small scale, (a single bed exhibiting five or six zig-zags in one escarpment,) dips on the whole about magnetic north; and at Cory Park, immediately over the same contorted limestone, there is a very good striped slate derived from a true cleavage-plane. The beds dip magnetic north 35°, and are cut by fine vertical dip-joints : but the cleavage-planes dip magnetic south about 25° or 30°. Here, again, the cleavage-planes are less inclined than the beds— a phenomenon, perhaps, unknown in the north of England. We observed no beds of like quality in any part of the culmiferous rocks along their northern edge. We think that the southern calcareous bands are in general thicker than the northern ; but the changes of mineral structure (excepting the meta- morphic portion near the north end of Dartmoor) are more striking on the northern boundary. For example, near Bampton, there are several quarries, where the shales become indurated, have a conchoidal fracture, and a red colour, and sometimes pass into chert ; and near the same quarries the calca- reous shales are associated with manganese, and the limestone bands are more crystalline, and become of a lighter colour. These localities also exhibit con-. tortions of great complication ; but in that respect they are not anomalous. Lastly, at Holcombe Rogus, we have a most extraordinary combination of sharp anticlinal ridges and contorted beds of limestone of great thickness, in which the black shale, which generally forms about three-fourths of the escarpments that are worked for lime, has almost disappeared, or at least be- come quite subordinate*. * In nearly all the great quarries of black limestone, some of which are of great extent and grandeur, both on the north and south boundary of the culm system, not only are there. consider- able portions which are rejected as mere waste; but even in the richer portions with the true lime- stone bands, there is seldom more than a third or fourth part which is actually burnt for lime. The alternating bands of dark indurated shale (frequently riddled through in all directions by white veins) are used for flagstones or coping-stones. To prevent misapprehension, we may also state that the culm-limestone (though far more persistent than the limestone junks of the lower groups) often comes to an edge, or passes into mere calcareous shale. Hence quarries for economical use cannot be opened indifferently on every part of the strike ; and indeed along the coast of Cornwall the limestone has disappeared from the section. Physical Structure and older stratified Deposits of Devonshire. 675 We were at first doubtful with what rock we were to class the Holcombe Rogus limestone ; but after a second visit in 1836, when we were better ac- quainted with all the varied characters of the lower culm-measures, we did not hesitate to place it in that part of the series. For it comes within the strike of the culm.measures ; and it contains many beds resembling the limestone at Bampton (which is unquestionably a culm-limestone, and may be regarded as a connecting link between the ordinary black limestone and that of Holcombe Rogus). It rests on rotten pale-coloured and red shale, with bands resem- bling china stone, exactly like some beds on the line of the wavellite rock above described. Again, it alternates with bands of red unctuous shale, (which be- come indurated and pass into red flagstones,) and with bands of chert; and among its beds in one of the quarries is found a considerable portion of earthy manganese : in all which respects it is analogous to the Bampton limestone. Lastly, in the extreme paucity of its fossils, and their absence from the accom- panying shale, as well as from its general structure, it is entirely unlike any of the limestones subordinate to the older group under the culm series*. Hence we think it certain that this limestone is a part of the lower culm group ; differing from the other culm-limestones in being much more largely developed, at the expense of the shales and flagstones, and, as a natural consequence, differing also in being more pure and crystalline. It is repeated in six or seven distinct ranges of elevated or contorted beds and anticlinal ridges, within a space of three or four miles in length and breadth. In consequence of these replica- tions, it is difficult to conjecture what is the whole number of its beds or their aggregate thickness}. In the grand anticlinal ridge (about a mile and a half south of Holcombe Rogus) there is a quarry at Canon Leigh that exposes a face of limestone rock about 150 feet thick: it is composed of a series of very thick, jointed, and shattered beds of a dark grayish blue colour, weathering like mountain-limestone, and alternating with thinner bands associated with hard red shale and chert. Among several of the subcrystalline beds we ob- served what may be considered a characteristic appearance in these quarries, viz. the dissemination of a series of distinct crystals of carbonate of lime through the more earthy base of the rock. It perhaps deserves remark, that * We found a few fragments of encrinital stems in the limestone ; but since the preceding de- scription was written, Major Harding has found in it the characteristic Posidonia, which completes the evidence for our conclusion. + The several ridves o{ limestone vary considerably in their strike ; some ranging nearly east and west, others N.E. and S.W. Indeed, all the phenomena of this contorted district may be con- sidered as instances of what has been before stated, respecting the great derangement of the older rocks, as they approach the plains of the new red sandstone. YOL.V.—SECOND SERIES. As OES Bn eS a om - BEY Sete manne ils 4 d $)) ¢ 676 Professor Sepewick and R. I. Murcuison, Esq., on the among some contorted beds not far from the north end of the canal tunnel, we found some thick amorphous bands of dolomite. We are aware of the extreme difficulty of conveying a distinct notion of the true aspect of a rock by mere verbal descriptions ; but we may certainly say in general terms, that the great escarpments near Holcombe Rogus re- semble mountain-limestone. And were we to seek for terms of comparison to describe the ordinary appearance of the black culm limestone (as seen. be- tween Bampton and Barnstaple, or along the south boundary of the culm- measures), we might compare it to the black beds of shale limestone in Derby- shire, or to some of the thin-bedded earthy limestones at the bottom of the carboniferous series in Craven ; and more correctly still, to the darker varieties of the Irish calp. But we distinctly wish it to be understood, that we use these terms merely as descriptive, and with no view of prejudging the ques- tion respecting the age of the lower culm group. In consequence of the contortions in this group (mere particularlyin its upper calcareous shales) it is difficult to form any correct estimate of its average thickness: we think that on the whole it is much thicker on the southern than it is on the northern boundary of the great trough. On both sides of Laun- ceston the group is chiefly increased by the great expansion of the lower grits: and were we to make a transverse section from the lower beds of the whole series on the south side of Bren Tor to the northern limit of the cal- careous shales, we must pass, notwithstanding the contortions, through an ascending series which cannot be estimated at less than two or three thousand feet in thickness, and is we think considerably more *. * To make the previous descriptions better understood, we subjoin the following section of the lower culm series where it is exhibited on the largest scale. The section commences about two miles north of Tavistock and ends with the culm limestone on the north side of the great west road —a distance of about eight miles. It exhibits the following ascending order : . Lower shales and grits, the latter of very great thickness. . Trap of Bren Tor, part of it recomposed and regularly bedded. . Thin-bedded jointed rock, here and there penetrated by manganese and by trap. . A more slaty culm shale, having two courses of roofing slate. . Black culm limestone, overlaid by roofing slate, and by indurated thin-bedded shale and siliceous bands much jointed,—penetrated irregularly by manganese. 6. The same series, repeated over again (by a flexure and a fault) on the north side of Lew- water. 7. Upper limestone, and commencement of the higher division of the culm-series. cr B O98 1 It is possible that the upper limestone may be only a repetition of the lower by a second great fault. The country is ill-exposed ; but there is nothing in its form or in the dips of the beds to indicate such a fault. The thickness from the bottom shales to the first range of black limestone is, we believe, much greater than what is statedin the text. (See Pl. LI, fig. 7.) Physical Structure and older stratified Deposits of Devonshire. 677 Upper Culm-Measures. This group, essentially composed of sandstone and indurated shale, is ex- panded through all the undescribed portions of the great culm trough, and indeed occupies nine-tenths of its whole surface. It is of very great, but un- ascertained, thickness ; being perpetually interrupted, coiled upon itself, and repeated over again, by violent contortions, forming an incredible number of anticlinal and synclinal lines, ranging nearly east and west with the strike of the beds*. No words can exaggerate the number and violence of these contortions—sometimes in regular undulating curves—sometimes in curves broken at their points of contrary flexure, and exhibiting a succession of cusps, like regular pointed arches—sometimes, though more rarely, thrown into salient and re-entering angles, generally of local extent and only affect- ing particular beds. Indeed, we have some examples of such angles in thick beds of shale, where the massy sandstones, above and below them, are not at all contorted. These contortions become less violent as we approach the lower groups on the southern and northern outskirts of the formation. Thus, on leaving the lower group near Oakhampton and making a traverse towards the north, we cross, for some miles, a great ascending series of the upper culm group, in which the prevailing dip is north, and in which there are comparatively few undulations. And in like manner, in a traverse from the northern boundary (for example along either of the roads from Barnstaple to Bideford), we have a great ascending series of beds, and a prevailing dip to the south. Hence, though it be impossible to ascertain the whole thickness of the group, we are sure that it is very great; and respecting the general order of superposition we find no difficulty. Whatever may be the age of the upper culm series, it is uncontestably the highest group of our general north and south sections f. We have stated that the essential components of this group are sandstone and shale; some- times exhibited in numerous thin bands, sometimes in thick well-defined masses. The sandstones are generally close grained, and full of irregular joints; and are coated over with ferruginous stains, * Wear the eastern boundary of the formation (as has been already stated) these lines are more irregular in their direction ; and, as might be expected, there are many subordinate tracts (gene- rally, however, of small extent) where the beds are in inextricable confusion, and their strike is irreducible to any system. + A curious example of this kind (noticed in Mr. Greenough’s map,) occurs at Mill Hook, on the coast of Cornwall. { See the sections from the Foreland to Dartmoor, and from Marwood to South Petherwin. (Pl. LL, figs. 1 & 2.) As 2 : ‘ ' ' f ; 678 Professor Sepewicx and R. J. Murcutson, Esq., on the exactly like bands of coal-grit. They are often gray, or brownish gray, and sometimes greenish gray, and are occasionally stained by red heematitic joints. And on the north side of Portledge Bay there is a series of sandstones and alternating shales of a deep red colour, which produce a distinct feature in the county, and may be traced for many miles along the strike, all the way preserving their peculiar mineral character. The system is traversed here and there by quartz veins, sometimes passing in well-defined transverse lines, and sometimes reticulated through the whole mass of the rock. Many of the thick gray beds exhibit, on their weathered and water-worn surfaces in the sea cliff, a number of spherical light-coloured spots, indicating an approach to a concretionary structure. Specks of sil- very mica are disseminated through many of the masses, on lines parallel to the bedding; and sometimes the mineral becomes so abundant that the rock has a flaggy structure, and resembles the coarse flagstone, so commonly used as a roofing slate in all our coal countries. The thinner beds alternate with, and pass into, a laminated arenaceous shale, with fine ripple marks at the partings. This last variety is sometimes (for example, on the coast of Bideford Bay, south of the Popple Bank,) continued through a thickness of many hundred feet ; with hardly an interruption from the thick hard coarser beds of sandstone. The shales vary from a sandy, micaceous, laminated flagstone, to a soft slate-clay, not distin- guishable from a common shale of our true coal-measures. Sometimes they exfoliate into innume- rable thin flakes; sometimes their weathered surfaces decompose into thin transverse prismatic masses, like the forms of starch. Many of them are pyritous, and are coated superficially with a white efflorescence or with brown ferruginous stains, precisely in these respects resembling coal shales. Among them are, here and there, dark carbonaceous bands which stain the fingers, generally in the form of mere lamine ; and near the junction of the shales with the harder flagstones, the dark Jaminz often contain innumerable obscure vegetable impressions much discoloured by decompo- sing pyrites: occasionally, but more rarely, the dark shales contain glossy plates, having the lustre of plumbago, in which case they seem to pass into the state of culm. The best examples of these glossy plates are, however, seen in the shales of the lower culm group already described. Impressions of plants are also found occasionally among the strong beds of sandstone; for ex- ample, in a quarry by the road-side about half-way between Barnstaple and Bideford*. In Ugbrook Park, near Chudleigh, there is a large development of culm sandstone as coarse as mill- stone grit, and passing into a conglomerate form ; and over it are some beds of more thin-bedded, gray sandstone, not to be distinguished from a coal-measure sandstone, and containing very fine vegetable impressions, among which are well-marked Calamites. Indeed, through the whole of the upper group we are describing, vegetable impressions, though rarely so perfect as to give anything like specific characters, are extremely abundant. Nodules of clay-ironstone are occasionally associated with the hard beds of sandstone; and sometimes they occur in beds, or rows, subordinate to the shaly bands. Among the accidental beds we may also notice calcareous shale passing into thin, impure bands of limestone, of which we saw an example near Hatherleight. All the beds above described are intersected by nume- * These gritstones may be called the wpper culm grits, to distinguish them from the coarse grits of the lower division, in which we never discovered any Calamites. The upper grits are diffused through the whole upper division of the series, but perhaps abound most in the part that first succeeds the black limestone and shale. ¢ See the section from the Foreland to the granite of Dartmoor. (Pl. LI., fig. 1.) Similar Physical Structure and older stratified Deposits of Devonshire. 679 rous open joints, which in the coarser contorted beds are very irregular in their directions. But when the beds have a finer flaggy or shaly structure, the joints often become parallel, (espe- cially in a direction nearly transverse to the strike) so as to separate the strata into prismatic masses. The description above given of the culm-measures, is copied from memoranda made on the spot during our traverses through the formation. The prevailing characters of the formation are the same throughout, and with very few excep- tions (which occur chiefly in the metamorphic portions), there is no difficulty in identifying it by its mineral characters alone. Its dark colour, the imperfect induration of the shale beds, the absence of slaty cleavage*, the coarse me- chanical nature of the bands of sandstone, and the perpetually recurring con- tortions, enabled us to follow it throughout, to trace it round the N.K. flank of Dartmoor, and to make out the boundaries of certain outliers of it which occur near Newton Bushel. And when we combine with these characters the very frequent occurrence of vegetable fossils, we can seldom fail to make out the place and limits of the deposit among the older rocks of Devonshire. There are other appearances in the very external aspect of the county to help us in determining the superficial extent of the culm series. ‘The conti- nued undulations of the whole region, where the contorted strata are expanded in a numberless succession of ridges, prolonged east and west like the anti- clinal and synclinal lines of the inferior strata—the great extent of a yellow, sterile, and, we believe, pyritous clay, producing a cold, fruitless soil, exactly like that among the cold lands of our coal-measures | ;—these characters often enable us, at a glance, to separate this formation from all the other deposits of the country. Such are the prevailing characters of the two groups into which we have divided the culmiferous series ; and such are the prevailing characters of the subordinate parts: and whatever may be their place in the general scale of British formations, this at least is certain,—that they are more recent than any of the other deposits, described in our transverse section, from the north to the south coast of Devon, and that they are overlaid by no rocks older than the thin impure beds of limestone are found in several other places in the upper culm-measures. We are indebted to Mr. Austen for the following localities; viz. Chittlehampton, Romansleigh, King’s Nympton and Bishop’s Nympton, High Bickington, Horridge Moor, Instow, and Harwood. * We have already described some exceptions to this rule in the shales of the lower group, east of Launceston; and similar exceptions occur in the metamorphic portions near Oakhampton. + The sulphate of iron in the pyritous clays, where it meets with the roots of the oak, sometimes produces streams of natural ink, which discolour the deep cuttings of the soil, by the sides of the cross roads, to a considerable distance. 680 Professor Sepewicx and R.1. Murcuison, Esq., on the new red sandstone. So far we may state our grounds of conviction with un- limited confidence. Neither can they be classed with any of the other forma- tions with which they are associated; as has, we think, been sufficiently proved in the previous portions of this paper. But in approaching the definite question—what is the exact epoch of the culm-measures ?—we must fortify ourselves with some more specific evidence, which might indeed have been incorporated in the preceding general description, but which we have de- ferred to this place, in order that the facts it offers might appear in a more prominent form. In addition, then, to the thin carbonaceous bands above noticed, there are, on the coast near Bideford, and extending from thence along the line of strike — far into the interior of the county, some much thicker bands of culm, which have for many years been extensively worked. This fact was known by all persons who had examined the structure of North Devon; but we believe Mr. De la Beche was the first who made the Society acquainted with vege- table fossils, derived from these localities, sufficiently well marked to admit of a botanical description or comparison with the vegetable fossils of other formations. Near the coast, the culm appears to have been worked on two lines very near each other; and on the north side of the culm beds is a very ferruginous grit in a highly-inclined position, and exactly parallel to the culmiferous shales*. When we visited the coast during the past summer (1836), they were extracting no culm for domestic use ; but were working one pit, sunk, we believe, on the southern line of culm, for the sake of a highly carbonaceous and unctuous shale, which runs side by side with a thin band of pure culm, and is extensively sold as a black pigment. The same culm beds have been traced eastward through the S.W. end of Bideford ; and they were formerly much worked there in pits which are now deserted. About two miles to the east of the town there have also been very extensive works, which were partially re-opened last summer (1836), but with what success we have not heard. At that place, there are three highly- inclined beds of culm, designated by the names of south, middle, and north veins,—all of which dip south. The south vein, or paint vein, is about three feet wide, and on its north side is a carbonaceous shale, used for paint. The whole bed is very impure, and contains little good culm fit for burning. The middle vein is fifteen fathoms north of the former, and is about four feet thick on the average, but expands, in some places, to twenty feet, and in.others is pinched out to a few inches, * See Pl. LI., fig. 3. Physical Structure and older stratified Deposits of Devonshire. 681 the culm appearing here (precisely as in the contorted culmiferous strata of Pembrokeshire) in large spheroidal masses, much shattered and broken, as if they had undergone irregular com- pression among the contorted beds of sandstone. Some parts of this bed are very good for domestic use. The north vein is forty fathoms north of the preceding. It is two feet wide on the average, and is liable to similar variations with the middle vein; and it has been much worked, though it is not of so good a quality as the former. The pit we examined was sinking on the south side of the middle vein. The sole of all the culm beds is sandstone, rather close-grained, and in some places ferruginous ; and the roof is composed of indurated shale (called shil- lat): but in the middle vein the shale roof sometimes passes into a gray mi- caceous flagstone, mixed and stained with glossy culm, and is exactly like a grit of the culm measures of Pembrokeshire. Plants are found in all these overlying shales ; and carbonaceous impressions (sometimes with distinct traces of vegetable structure) occur also in the sandstones, both of this and the other localities. These mineral details are copied, word for word, from our memorandums made on the spot, and are enough for our present purpose*. It only remains for us to give a list of the fossil plants, many of which are now before the Society. PLANTS IN THE CULM STRATA OF DEVON, DETERMINED BY PROFESSOR LINDLEY. DEVONSHIRE. OTHER LOCALITIES. Asterophyllites foliosa, Foss. Flora, Pl. 25.f. 1. Jarrow Colliery, Newcastle-on-Tyne. Calamites undulatus. Ad. Brongniart, Veg. Low Moor, Yorkshire. Radnitz, Bohemia, &c. Foss., Pl. 17, fig. 1, 4. C———. Species resembling C. arenaceus, Ad. Brongn. Cyperites bicarinata. Foss.Flora, PI]. 43. f.1,2. Upper coal measures, Salop. Neuropteris gigantea. Sternb. Tent. Flor. One of the most abundant coal plants in Ger- Primord. Tab. 22. Ad. Brong., Pl. 69. many and in England. Foss. Flora, Pl. 52. (Osmunda gigantea, Sternberg Flor. der Vorw. Filicites linguarius, Schloth. Flor. der Vorw., Tab. 11. fig. 23.) Neuropteris cordata. Ad. Brongn., Pl. 64. Upper coal measures, Salop, and common in fig. 5. Foss. Flora, Pl. 41. the English and French coal-fields. * There are many old deserted works much further towards the east. The attempts to work the culm beds near their eastern limit have hitherto failed to reward the adventurers with any profit. The last attempt was made upon a very thin bed in the hills about two miles north-west of Bradwick. 682 Professor Sepewicx and R. I. Murcuison, Esq., on the DEVONSHIRE. OTHER LOCALITIES. Pecopteris lonchitica. Foss. Flora, Pl. 153. Upper coal measures, Salop. ‘One of the P. blechnoides § lonchitica. Ad. commonest of the plants of the coal forma- _ Brongn., Pl. 84.f.1-7. Scheuch- tion, as the opposite list of authorities indi- zer. Herb. Diluv., p. 74. Filicites cates, occurring in great numbers in a variety lonchiticus. Schloth. Flor. der of mines in France, Bohemia, Silesia, and Vorw., Tab. 11. f. 32. Aletho- England; very abundant in the culm mea- pteris lonchitidis et A. vulgatior. sures of Pembroke.” Sternb. Flor. der Vorw., Tab. 55. This species is perhaps the most abundant of the Bideford Plants. Pecopteris muricata. Ad. Brong. Veg. Foss., Coal Mines of Argin, near Valenciennes, and Pl. 95. fig. 3 and 4. near Wittin, Saxony. Poacites cocoina. Foss. Flora, Pl. 142 B. Coalbrook Dale and other Salopian coal-fields, and also in the Lancashire coal near Bolton; a very remarkable species of palm. (See Lindley and Hutton.) In addition to these plants clearly exhibiting the characters on which fossil species are deter- mined, there is a considerable quantity of impressions of coarse, sedge-like, or grassy vegetables, which, though not easily defined, are apparently identical with fragments very common in the Pembrokeshire coal-field. We would here also call attention to the fact, that every species of these Devon plants which is well preserved has at once been identified by Professor Lindley with well-known and previously-published vegetable forms of the true carboniferous era. Among these, the Pecopteris lonchitica and Neuropteris cordata may safely be cited as among the most common and characteristic plants of nearly all the European coal-filds. On the whole, considering that the culmiferous rocks of Devon form a distinct group, with a peculiar mineral type (unlike the older groups, but nearly resembling the culmiferous beds of Pembrokeshire)—that they overlie ail the other groups, and are overlaid by no rock newer than the new red sandstone—that, notwithstanding the paucity of fossils in the black limestone (in which respect it resembles the calp of Ireland), there are in it one or two species not separable from known mountain-limestone fossils,—and, finally, that the flora of the upper culms, as far as it has been ascertained, agrees spe- cifically with the known flora of the carboniferous period ; we think we have strong direct evidence to establish our position, “ that the upper culm strata of Devon are the geological equivalents of the ordinary British coal-fields.’’ Our conclusion is drawn from direct evidence, and can only be assailed by direct conflicting evidence, of which we have not yet discovered any trace. Besides the plants of the strata which we refer to the true carboniferous series, other fossil vegetables have been discovered since our first visit to De- vonshire, in the sandstone beds of Sloly quarries, north of Barnstaple, which are near the base of the fifth group of our North Devon section; and, there- fore, far below the culmiferous series. This discoverv was first communicated to us bv Maior Hardine. of Ilfra- Physical Structure and older stratified Deposits of Devonshire. 683 combe, to whose exertions we have already alluded*. He forwarded to us, several months since, a few stems of plants from Sloly quarries, accompanied by casts of shells from the sandstone rocks of Marwood ; and had this memoir not been unavoidably retarded, we should have announced his discovery at the commencement of the year. Meanwhile, however, the Rev. D. Williams having revisited the same locality, has procured a more abundant and perfect supply of fossil plants from it, which he has sent to the Geological Society to illus- trate a memoir of his own; and he has kindly permitted us to examine them. On referring these plants to Professor Lindley, we were favoured by him with the following opinion ;— “T am of opinion that these remains are not susceptible of specific identification; you can only approximate to their determination: 1, 2, 3, 4, 5, are probably portions of the same species, and are undoubtedly a Stigmaria or a Lepidodendron; the absence of all trace of a hollow axis, and the similarity of their surface to that of decorticated Lepidodendra, induce me to decide for the latter. 6. Is probably another portion of the same plant; but this is uncertain. 7. Is more analogous to some states of Sternbergia than to any other fossil I am acquainted with. It agrees with that genus remarkably in the intermixture of strong longitudinal fibres and coarse cellular substance; and at all events may be safely considered as the remains of some ar- borescent Moncolyledon. 8. Is so imperfect that it is hardly safe to refer it to Calamites ; and yet the apparent obliquity of the only articulation that the specimen exhibits, is so much that of Calamites Voltzii of Ad. Brongniart, as to render it probable that it may belong even to that species. 9. Has on one side the evident impression of a Lepidodendron; on the other side it is striated like Calamites arenaceus? perhaps it was the latter moulded on one side upon the stem of the former. 10. Was possibly a portion of No. 7, with the cortical integument less decayed; on the lower left hand side, quite at the edge, is a small part of the surface, which will nearly match a part of No. 7. If these conjectures are correct, the whole of the specimens are referable to genera of the coal measures ; but whether they are specifically the same, I cannot say.” Such are the remarks of Professor Lindley on the fossil plants of Sloly quarries ; and we contend that they oppose no real difficulties to our previous conclusions respecting the age of the culm beds. Should true coal plants be discovered in the lower group (North Devon, section No. 1), they would not, we think, upset conclusions founded on so much direct evidence. ‘They would, however, prove one of two things—either that such plants had an unusually wide geological range ; or that the group below the culm measures was of a more recent date than we first imagined ; and formed (as has indeed been * Supra, p. 648. VOL. V.—SECOND SERIES. AT 684 Professor Sepewick and R. I. Murcuison, Esq., on the supposed from the evidence of sections) a true passage into the lower division of the overlying trough. The only fact which could materially disturb our proposed classification, would be the discovery of a series of plants among the culm beds, unlike the fossil flora of the true coal-fields, and resembling the fossil flora of some well-ascertained lower formation. But such a series never has been, and we believe never will be, discovered in Devonshire*. The culm series, considered as a whole, cannot be properly classed with the inferior groups ; as it has a distinct position, a different structure, and a peculiar suit of organic fossils, animal as well as vegetable. It must there- fore be represented, hereafter, on our geological maps by, at least, one distinct colour. So far we conclude with perfect confidence. The enormous development of this series, the absence of the old red sand- stone and mountain-limestone in their more usual form, and the fine slate rocks in some parts of the lower culm group, may seem to make its geologi- cal base somewhat doubtful. Again, the parallelism of position of the lower group and the formations on which it rests (both on the north and the south sides of the great trough), and ils apparent passage into them, tend to increase this doubt. Provisionally, then, and as a measure of caution, we are willing to place the base line of the culm series in a geological position, not yet perfectly defined. But, we repeat, no such ambiguity attaches to the upper part of the culm series; as all the vegetable fossils derived from it, are identical with published species, before obtained, from the true coal measures overlying the mill-stone grit. Again, as the members of the whole culmiferous series (including both the upper and lower divisions) appear to have originated in one uninterrupted succession of operations, have a nearly common type, and partake of the same accidents, we certainly think that they must all be classed together. And if this reasoning be correct, the lower groups of black shale and limestone (what- ever be the supposed ambiguity of the base line) must also be classed with the true carboniferous system. In its structure and in the paucity of its or- ganic remains, it resembles the calp, or argillaceous limestone, at the base of the carboniferous system of Ireland ; and the specific characters of its fossils, as far as they go, do not invalidate but confirm the conclusion we have drawn. * Some new facts have come to light (since the spring of 1837) connected with this subject, to which we refer in the second part of this communication. Physical Structure and older stratified Deposits of Devonshire. 685 Cuar. V.—Granite of Dartmoor ; its Structure and Relations to the Stratified Rocks, &c. It only remains for us to describe in a few words, the Dartmoor granite and the phenomena presented at its junction with the other stratified forma- tions :— Ist. It presents the large porphyritic structure, the contemporaneous cry- stalline portions, and veins of schorl ; the portions liable to decomposition from the disappearance of the alkaline constituent of the felspar ; the hemitrope crystals of albite ; and in short, almost all the other well-known accidents of structure, which have so often been remarked in the Cornish granite. In- deed, there can be no doubt, that, from Dartmoor to Land’s End, all the larger protuberances of granite belong to one common system of formation ; and they present the like phenomena at their junction with the stratified rocks. 2nd. There are other accidents of structure, common to the granite of De- vonshire and Cornwall, which we may also notice—more especially the joints. Every one who had written on the granite of these counties, had noticed the occasional prismatic, or cuboidal, forms of the rock ; and Dr. McCulloch en- deavoured to account for these phenomena on the hypothesis of interfering spheroidal concretions. Since that time, Mr. Fox and Mr. Enys have shown, that two leading sets of these joints are nearly perpendicular to the horizon ; and have (in the western parts of Cornwall) given bearings with respect to the points of the compass,—one set being nearly magnetic N. and S., and the other nearly magnetic EF. and W.; while a third set are nearly horizontal*. Nor did their remarks end here; for they showed, by the peculiarities of its cleavage, and the prevalent arrangement of the larger felspar crystals, that these joints were due to a crystalline arrangement affecting the whole mass of the granite. These arrangements, however, fail on the outskirts of the granite ; more especially in the deviation of the tabular joints, which, in such cases, often assume a kind of dome-like shape, conforming rudely to the actual surface of the country. Dr. Boase has also dwelt largely on these subjects, and shown that many of the accidents of structure, especially many master-joints, are common to the granite and the rocks in contact with it f. Now all these important peculiarities of structure (first observed in the western parts of Cornwall) are equally true of the granite and contiguous rocks of Dartmoorf. * See Phil. Mag. May 1833. + See various Memoirs by Dr. Boase in the Transactions of the Royal Geological Society of Cornwall. t From the mean of our observations we should place the bearing of the principal north and Ayr2 686 Professor Sepewick and R. I. Murcutson, Esq., on the The leading system of joints is the same with that observed in Cornwall, whether we examine the granite or the altered rocks that are close to it. This remark applies to the culm measures, as well as to the older slates; and the fact seems to show, that the joints (common to the granite and contiguous slates) must be contemporaneous. But it by no means follows from this con- clusion, that we should thence infer, as has been done by Dr. Boase, that the granite and the contiguous slate rocks are also contemporaneous. Such a conclusion is manifestly contradicted by the facts stated in the preceding parts of our paper. | 3rd. Granite veins, passing from the central mass into the superimposed stratified rocks, are found on all sides of Dartmoor. We have seen them above Ivy Bridge, injected among the oldest slates of Devonshire ; and near Oak- hampton, we have seen them in like manner, penetrating the culm measures : and they are finely exposed in the beautiful gorges of the Teign and the Dart, where those rivers descend from the granite to the culmiferous series. These examples, to which we could add many more, are sufficient for our purpose. Now these veins, taken in general, are mere prolongations of the central granite, inseparable from it, and contemporaneous with it; they cannot therefore (as the granite is one mass) be contemporaneous with stra- tified rocks of different ages. Consequently they are true veins of injection, and the granite was protruded at a time, posterior to all the other stratified systems. Again, the beds and masses of trap, associated with the stratified rocks, do not penetrate the granite (as they do in the Isle of Arran and many other places) but are uniformly cut off by it. This seems to prove that the injected trappean masses obtained their present position among the slates before the granite existed in its present form; and the same conclusion is still more certain when applied to the stratified, or recomposed, trappean rocks which alternate with the slates. Ath. The strata round Dartmoor are not all mantle-shaped. On the north- western and north-eastern sides of it, their str¢ke is not much altered by the granite; and the successive beds may be said to abut against, rather than south joints about five degrees east of magnetic north. Mr. De la Beche, in his recently pub- lished Report, gives many accurate details connected with this subject, which on the whole confirm the statements first given by Mr. Enys and Mr. Fox. A person after reading these statements might perhaps be disappointed on commencing an examination of the granitic hills of Cornwall, and finding the joints often quite anomalous in their directions. For reasons already stated, such an examination must aot begin on the outskirts of the granitic hills, and no mean directions can possibly be established, except on a large number of averages. (1839.) Physical Structure and older stratified Deposits of Devonshire. 687 mantle round the central rock : yet the ends of these abutting strata are per- fectly metamorphic. This fact we think important, as it proves to demonstra- tion, that these strata are, in the strictest sense, metamorphic, and do not belong, as has been supposed, to a system of deposits older than the less cry- stalline beds, which are further from the granite. 5th. There have been two distinct regions of elevation in the country above described ; one commencing in the great granitic mass of Dartmoor and ex- tending into Cornwall,—the other, nearly parallel to, and not far from, the north coast of Devonshire. The compression of the central mass in North Devon, by the elevation and protrusion of the rocks on these two lines, may perhaps have been among the means which produced the contortions of the great culm-trough. 6th. Lastly, as a general conclusion from all the previous details, it appears that the rocks of Devon and Cornwall belong to three periods of formation. The oldest includes the various groups of slate rocks, and, at least, a part of the associated traps. The next includes the culm series, the upper division of which contains fossils identical with those in the upper division of the true coal measures. The granite belongs to the newest period ; but (on evidence not discussed in this paper) probably assumed its present position among the rocks above described, before the deposit of the new red sandstone. 688 Professor Sepewick and R.1. Murcuison, Esq., on the On the Physical Structure of Devonshire, and on the Subdivisions and Geological Relations of its older stratified Deposits, &c. [Read April 24th, 1839.] PART II. On the Classification of the older stratified Rocks of Devonshire and Cornwall, &c. In a former communication we described the mineral structure, and the order of superposition, of the successive groups of rocks which are crossed by a section from the north, to the south coast of Devonshire; and by following the beds (along their line of strike) into Cornwall, we were enabled, within certain limits, to bring the kellas (or slate rocks of that county) into comparison with some of the lower Devonian groups. In this way, we ascertained the existence of a great culmiferous trough, superior to all the other groups in North Devon, and distinguished from them both by its physical structure and its organic remains. Hence we concluded, that the culmiferous series must be represented, for the future, in our geological maps by a distinct and appropriate colour. We had stated the same conclusion, and on precisely the same evidence, at the meeting of the British Association in 1836. We further concluded, that, at least, all the upper portion of this series was of the age of the great coal-formations of England; inasmuch as all its vegetable fossils, as far as they were ascertained, agreed specifically with undoubted coal plants. ‘To this conclusion we still adhere ; and we re- gard the culmiferous rocks as forming a true geological horizon, to which either the ascending or descending series of deposits may be referred. Again, in the arrangement of the several groups below the culm-trough, as they appear on the North Devon section, we have no modifications to suggest ; and the very illustrations which were before suspended (1837), to explain the actual succession of the deposits, will serve our purpose at this moment. Since our first notice of this section in 1836, Mr. De la Beche has exa- mined the country in great detail; and his arrangement of the several fossil- iferous groups, inferior to the lower culm beds, agrees with our own*. The * There is one unimportant exception to this remark which we have noticed in our former paper (see p. 642, note). It fortunately does not affect the position of the fossiliferous groups, or any question connected with their classification. Physical Structure and older stratified Deposits of Devonshire. 689 same may, we believe, be said generally of the arrangement given by Mr. Williams. We shall, therefore, for the future, refer to the successive groups in the North Devon section with entire confidence. The only questions which can now arise, must refer to their age and classification,—not to their relative position. To our four sections, illustrating the structure of South Devon, we make no material change or addition ; with one exception, however, viz. the interpola- tion of a small band of culm measures between the Ashburton limestone and the granite—discovered by Mr. Austen since our visit in 1836, and repre- sented (PI. LI., fig. 8.) on his authority, as has indeed been already stated in a note to our former paper. Neither have we any material change to make in our comparison of the deposits of North and South Devon. Considered as a whole, we still think that they belong to one system of formation; and that the lowest group of South Devon is lower than the lowest group of North Devon. But as for our comparison of the subordinate groups (though still the best that we can offer), we only throw it out as provisional, being chiefly founded on mineralogical characters, and those perhaps not of a very conclu- sive kind. Lastly, we have no change to make in our description of the fossiliferous groups of Cornwall. They are very nearly on a parallel with groups exhi- bited in the sections of North and South Devon ; and the fossiliferous slates of both counties belong to one system. We do not encumber ourselves with any details respecting the more crystalline and (as we believe) altered slates ; but we have, in our former paper, shown that they are not, merely on account of their structure, to be regarded as older than the calcareous and arena- ceous deposits. After these preliminary remarks we proceed (agreeably to a promise given in our former paper) to re-examine the classification of the respective groups inferior to the culm measures ; and we begin by expressing our entire con- viction that the true equivalents in the several disjointed sections can only be made out by zoological evidence. We were at first led to the opinion, that the series of deposits we are de- scribing, were to be placed below the Silurian system, partly from the re- semblance of the highest group (No. 5 of the North Devon section) to the Caradoc sandstone; and perhaps still more from the mineral structure and slaty cleavage of many parts of the lower groups. At that time we had not sufficient boldness to adopt the only other alternative, and throw all the old slates of Devon, and the (supposed) primary slates of Cornwall, into the epoch 690 Professor Sepewick and R. 1. Murcutson, Esq., on the of the old red sandstone. We were aware, indeed, that several of the South Devon fossils conformed nearly, perhaps specifically, to the type of the carbon- iferous limestone. But on the other hand, no one was able to define the de- scending range of such organic forms; especially as it was asserted, that they reappeared in the south of Ireland, in beds alternating with true greywacké— or rocks supposed to be older than the old red sandstone. Hence we placed, provisionally, but with no satisfaction to ourselves, or confidence in our evi- dence, all the older fossil groups of Devon and Cornwall in that great but ill- defined interval that exists between the Caradoc sandstone and the older slates of North Wales. Since 1836 we have received repeated proofs of the insecurity of our first hypothesis. Thus, Mr. De la Beche (1837) exhibited fossil plants from the quarries of Marwood (PI. LI., sec. 2.) one of which Professor Lindley identified with Stzgmaria ficoides, a very common coal- plant ; and near the same place we had ourselves found a Bellerophon, not to be distinguished from B. lobatus of the old red sandstone. Again, Mr. Lonsdale, after an extensive examination of the fossils of South Devon, had pronounced them, more than a year since, to form a group intermediate be- tween those of the Carboniferous and Silurian systems, and hence he con- cluded that the fossiliferous rocks of South Devon were subordinate to the old red sandstone. This view could be effectually maintained only by one who knew the fossils of the Silurian system. The work in which those fossils are described, proves that the fossils of the Silurian and carboniferous systems are quite distinct. It also proves that the fossils of the old red sandstone of Herefordshire are of a peculiar type; and, at the same time, it points out a want of zoological continuity in the development of organic forms between the epochs of the carboniferous and Silurian deposits. There is, indeed, a true zoological transition between the highest group of the Silurian system and the lower part of the old red sandstone ; but between the middle and upper groups of the old red sandstone and any part of the carboniferous limestone no such transition had been discovered. These facts were well known to Mr. Lonsdale, and hence his conclusion respecting the age of the South Devon limestone was based on incomparably better evidence than the mere specific resemblance of some of its fossils to those of the carboniferous limestone: for he contended, as above stated, that the organic remains of South Devon formed a connecting link between the carboniferous and Silurian fossils ; and thus supplied that zoological continuity which before had been sought for, but never found. But this is not the whole of the evidence by which we were gradually led Ea Physical Structure and older stratified Deposits of Devonshire. 691 to distrust the views, we had first entertained respecting the age of the older stratified groups above described. For one of the authors, during the sum- mer of 1838, re-examined a part of the great transverse section of Devon- shire, and was more than ever convinced that, with some ambiguous excep- tions, there was on each side of the great trough a true passage from the jower division of the culm-measures into the inferior fossiliferous group. Thus the section from Marwood across the culm series to the calcareous slates of South Petherwin seemed to be perfectly symmetrical (PI. LI. fig. 2.), the iower beds of the culm-measures being repeated (as described in our pre- vious paper) on both sides of the trough ; from beneath which emerge on the respective sides, and in a regular uninterrupted sequence, the calcareous slates of Petherwin and Barnstaple. Now, if this view be correct, it follows, almost inevitably, from our own evidence, that the calcareous slates in question must be very near the upper limit of the old red sandstone; and this con- clusion being once admitted, we should have little difficulty in classing, not merely the calcareous rocks of North Devon, but also the fossiliferous slates of South Devon and Cornwall, with the old red sandstone. To the preceding facts, bearing on the classification of the older rocks of Devon and Cornwall, we might add some remarks on the mineral structure of the two counties—on the existence of red conglomerates among the beds of the Cornish Aillas—and on the large tracts, both of North and South Devon, filled with rocks identical in structure with the most ordinary forms of old red sandstone. But we forbear to dwell on such facts as these, wishing to build our present conclusions chiefly on zoological evidence. Guided then by the evidence already stated, and the conclusions to which it seemed to point, we have re-examined the fossils obtained, either by our own labours or by the assistance of our friends, from the two counties ; and the conclusion arrived at by Mr. Lonsdale respecting the age of the South Devon limestone, we now apply without reserve both to the five groups of our North Devon section, and to the fossiliferous slates of Cornwall. This is undoubtedly the greatest change which has ever been attempted at one time, in the classification of British rocks. But all the facts brought to light by those, who have laboured in the same field with ourselves, were gra- dually leading towards the same point; and the establishment of the Silurian organic types must before long have made the change inevitable*. So far from thinking ourselves rash and hasty in drawing the preceding * The reasons for the new classification of those stratified rocks of Devon and Cornwall which are below the culm-measures, were briefly stated by the authors in a paper published in the Phi- losophical Magazine for April 1839. VOL. V.—SECOND SERIES. Au 692 Professor Sepewick and R. 1. Murcutson, Esq., on the conclusion, we think we may rather be accused of being over-cautious and tardy in accepting evidence, however opposed to commonly received opinions. But, on this score, we may state.in our justification, that a considerable part of our fossil evidence has been but recently brought to light. Several of the organic remains, from the neighbourhood of New Quay, on the north coast of Cornwall, which we owe to the kindness of Mr. Carlyon, and many other good specimens given to us by our friend Mr. Pattison of Launceston, have been but very recently submitted to a careful examination; and the beautiful collection of Plymouth fossils committed to our care by Mr. Hennah, was only unpacked, in consequence of unavoidable delays, during the present spring. An examination of this collection by one of the authors, assisted by Mr. Lonsdale, Professor Phillips, and Mr. James Sowerby, confirmed the previous conclusions of Mr. Lonsdale, which were chiefly founded on Mr. Austen’s collection; and, as before stated, led the way to our proposed classi- fication of the Cornish and Devonian formations*. At first, we did not intend to give any map among the illustrations of this paper ; as it was thought that any of the published geological maps of England would enable the reader to follow our details. But it has now been thought better to give a reduced map of the country we describe, chiefly taken from the corrected Index geological map attached to Mr. De la Beche’s Report on the Geology of Cornwall and Devon; in order that we may convey, at a single glance, the connexion between the structure of Devonshire and Cornwall, and the directions in which our several sections are drawn. All details of structure are, however, intentionally avoided, and the stratified groups are all repre- sented by two colours. In this way we mean to convey our belief, that the inferior groups all belong to one system, viz. that of the old red sandstone. There may, indeed, among the lowest rocks of the two counties, be some which belong to a still lower system. But if such there be, we are unable to point them out; and we think it best and safest, as far as regards their classification, to merge them all at present in one common colour. Neither did we at first intend to publish any figures of the fossils derived from the several groups above described. But it was urged, that a paper pro- posing such great changes in the classification of our older rocks would not be well received, or even understood, without more graphic proofs than mere * Since this paper was read, Mr. Williams has permitted us to examine his excellent col- lection of fossils from Cornwall and North Devon. We may allude to them generally as con- firming our views; but none of them will appear among the illustrations of this paper, as their specific descriptions are, we trust, hereafter to be given by Professor Phillips. + See Plate L. Physical Structure and older stratified Deposits of Devonshire. 693 verbal descriptions. In the subjoined plates (PI. LII. to LVIII.) we have therefore figured some of our best fossils. The figures and determination of the fossil shells are all by Mr. James Sowerby: any notice we may take of the corals will be given on the authority of Mr. Lonsdale. We might perhaps now content ourselves by simply giving a list of the fos- sils derived from the respective deposits, and then leave the reader to draw the proper conclusion from the facts before him; but we think it advisable, in the first place, to put our evidence in a more general and popular form. In our previous paper, the successive groups are described in the ascending order in which we first observed them, during our traverse from the north to the south coast of Devon. But in noticing the fossils, it is almost necessary (as our sections have no well-defined base) to take a reversed order, and com- mence with the upper division of the culm-measures. 1. Culm Measures.—In the first place, then, we have nothing to Tl to the evidence given by the vegetable fossils of this upper division of the culm- measures, or to the conclusions we drew from it. On this point, therefore, we merely refer to our former communication (supra, p. 669, et seq.). The black limestone of the lower division contains many shells of the genus Poszdonia, three or four species of Gonzatites, and two or three other genera not yet well ascertained. Now the genus Posedonza is found abundantly both in the upper and lower limestone shales, of the true carboniferous series of England and Ireland: for example, in the calp of Ireland, which is in the place of the lower shales, and in the upper limestone shales of Northumberland, not far below the millstone grit. There is a species in Northumberland, which makes a very near approach to a species very abundant in the black culm limestone. Again, of the Goniatites of the culm limestone, there are three species very closely related to those of the mountain limestone*. Among them is one which Pro- fessor Phillips is unable to separate from the G. Henslowi, found in the great scar limestone of the Isle of Man ; and it deserves remark that this species occurs also in the Petherwin group, below the culm-measures,—a fact which tends to prove the reality of a passage from the base of culm-measures into the next inferior group. Where then shall we place the culm limestone, and carbonaceous shales that form a part of it? If we arrange them with the upper shales of the moun- tain limestone, then nearly the whole culm-trough of Cornwall and Devon will be the equivalent of the middle and upper divisions of our true carboniferous series. This view was adopted by Prof. Phillips when he published his index map of the British Isles. But if we identify the black, calcareous, culm shales * Report on the Geology of Cornwall, &c. p. 117. 402 694 Professor Sepewickx and R. 1. Murcuison, Esq., on the with the calp of Ireland, or the lower limestone shales of England, the culm series of Devon will, as a whole, be very nearly the equivalent of our en- tire carboniferous series. Considering, however, the enormous thickness of the whole culm-measures and the paucity of fossils in all the inferior beds of its lower division, we continue to place its base in a doubtful position. This is a measure of necessary caution, especially when we bear in mind the ex- treme difficulty, in the northern parts of our island, of drawing any precise line of demarcation between the base of the coal-measures and the old red sandstone*. Before the sections of North Devon had been made out, the culm-measures were naturally included in the vast deposit of graywacké, of which we knew neither the beginning nor the end. But to merge them in that series now, is to reject all the direct evidence we possess, and all the analogies supplied by the corresponding parts of our island. Lastly, there seems now to be no difference of opinion as to the superficial distribution of the culm-measures ; for the boundary line indicated roughly by us in 1836, and more in detail in our previous paper, agrees, as far as it goes, with that lately published by Mr. De la Beche. 2. Fossils of Petherwin and Barnstaple-—The fossiliferous slates in the neighbourhood of these two places rise immediately from beneath the base of the culm-measures. Their position is therefore symmetrical, and, as be- fore stated, they appear on the whole to form a mineral passage into the overlying system. In this way, we establish a mineralogical connexion be- tween the North Devon and Cornish sections. But the connexion is made incomparably more secure by help of the fossils. Those we have obtained from Barnstaple, Croyde Bay, Marwood, &c. (all of them places in the highest division, No. 5, of our North Devon section,) certainly agree as a group with those of Petherwin, and have many species in common, as will ap- pear by our lists. It is enough for our present purpose to quote the follow- ing; Spirifer attenuatus, S. bisulcatus, Orthis interlineata, Atrypa concen- * The difficulty we have pointed out does not arise from any doubt respecting a great principle of classification, but merely involves the adjustment of a boundary line. One of the best illustrations of this difficulty is seen on the east coast of Scotland, north of St. Abb’s Head. The old red sand- stone first appears as a conglomerate, resting transversely on the edges of the graywacké; and then passes so insensibly into the red carboniferous rocks, that, through a considerable extent of coast, it is hardly possible to draw any well-defined line between the two formations. We may, however, observe by the way, that there are several pretty extensive tracts coloured as old red sandstone in Macculloch’s Geological Map of Scotland, which we believe every geologist who was guided by the English types would class with the lower division of the mountain limestone ; and there are one or two places in Dumfries-shire, where we think he has confounded the new with the old red sandstone. — en Oe Physical Structure and older stratified Deposits of Devonshire. 695 trica, A. decussata, A. striatula; also a smooth and a plaited species ; Leptena caperata, L. scabricula? Pectens.n. Pallastra s.n.* All these shells are found both among the calcareous slates of Petherwin and in the calcareous slates near Barnstaple ; and several of the species common to both localities are extremely abundant. That there are several species among the Petherwin fossils which have not been yet found among those of Barnstaple, takes not at all from the force of our direct evidence. It deserves remark, that there are several species in these upper groups which do not appear in the lower; and among those we may notice the Goniatites and the Endosiphonites+, (Clymenia of Munster,) as they seem to point towards the types of the carboniferous period. In the lower division of the Barnstaple calcareous slates occur the Marwood fossils, given in our lists, among which are several species of Cucullea. These sliells are associated with the genus Bellerophon, one of which, as be- fore stated, cannot be distinguished from the Bellerophon globatus of the old red sandstone. Very nearly on the strike of the Marwood beds occur the fossil plants of the Sloly quarries. According to Professor Lindley, (ante, p- 683.) one of the species belongs either to a Stigmarza or a Lepidodendron ; while others are new or incapable of determination. Professor Henslow, who has recently examined a good series of fossil plants from the same locality, in- forms us, that he is able out of them to distinguish three or four species, not one of which he believes to have been described in the published works of Sternberg, Brogniart, or Lindley. Either of these results would fall in with our present views. We undoubtedly consider the Sloly beds as out of the limits of the carboniferous series, and therefore we should expect that its fossils would conform to an older type. On the other hand, the appearance of a few species of the true carboniferous fossils in the upper division of the old red sandstone would be in perfect harmony with what we know of the geological distribution of organic forms. But the assumption that the ordinary species of coal-measure plants may exist in the old graywacké rocks of an entirely distinct period, takes for granted conditions which are not supported by the evidence of the Devonian sections, as we now interpret them. We are unwilling to push our present remarks any further; but we can * Some of the fossils quoted are of doubtful species ; but the doubt does not apply to the iden- tification of the individual specimens from the opposite sides of the culm-trough. + The appropriate name of Endosiphonite had been given to the genus by Mr. Ansted before he was acquainted with the previous discovery of Count Munster. The name Clymenia is by no means so good; but having the priority, ought to be retained. We cannot but regret that the original name (Planulites) was rejected by Count Munster, as it harmonizes with the general no- menclature of fossil Cephalopodes, better than his present name Clymenia. 696 Professor Sepewicx and R. I. Murcuison, Esq., on the hardly avoid surmising that the peculiar plants of the “ terrain d’anthracite inférieur’”’? of Professor Voltz, and those of a supposed similar age in Brit- tany and other parts of France, may eventually be found to be on the same parallel with this portion of our North Devon series. 3. Inferior Groups of the North Devon Section—The number of fossils hitherto collected is far too small to justify us in affirming to what extent the fossils of the Ilfracombe calcareous slates (North Devon Section, No. 3.) differ from those of Barnstaple. A few species are certainly common to both, among which we may quote two species of Leptena anda Pecten (see the list). Corals abound in the Ilfracombe slates, though the species are not numerous. The Favosites polymorpha (never yet discovered in the mountain limestone, or below the upper Silurian groups,) is the most abundant. With itis another entirely new species, which also abounds in the Cornish fossiliferous strata beneath the culm-measures. On the whole we may state, on the authority of Mr. Lonsdale (from whom alone we have derived any accurate information on this head), that the Devonian corals are all either of species peculiar te these groups or such as occur only in the higher part of the Silurian system. Immediately below the Ilfracombe calcareous slates, are some hard strong beds, with numerous impressions of a large cordiform bivalve, unlike any- thing we remarked in the overlying beds. From the lowest group of all (North Devon Section, No. 1.) we have very few well-preserved fossils : among them are many beautiful casts of a Fenestella, and among the bivalves is an Orthis of a new species, and a Spirifer identical with one found near Barnstaple (Sp7- rifer attenuatus ?). Such is the summary of the evidence given by the fossils of the North Devon section ; and imperfect as we acknowledge it to be, we think it sufficient to bear out our proposed classification ; especially as we know of no conflicting fossil evidence that is in any way opposed to it. 3. South Devon and Cornwall.—tIn the comparison of the mineralogical groups of North and South Devon, we can add nothing to what has been stated in a former paper. We could not bring the great upper South Devon limestone into direct comparison with the calcareous zone of Barnstaple ; because, in that case, the great slate formation, which overlies the Plymouth limestone, would have no representative in North Devon. We therefore provisionally placed the great calcareous group of South Devon on a parallel with the lower fos- siliferous groups toward the northern extremity of our section. The fossils appear on the whole to bear out this classification. First, then, as to the South Devon corals.—None of them have been found in the mountain limestone, several are new or not known to occur in the Si- Physical Structure and older stratified Deposits of Devonshire. 697 lurian system, and some agree specifically with corals of the highest Silurian groups. On this point we rely on Mr. Lonsdale’s determination ; and we give it in his own words : Favosites polymorpha, (Goldfuss, PI. XXVII. f. 4. Silur. Syst., Pl. XV. f. 2.). Common in the Plymouth* and Ogwell* limestones, and it occurs also at Barton and Torquay, and in slate at New Quay, Cornwall. spongites (Goldf., Pl. XXVIII. f. 1. Silur. Syst., Pl. XV. f. 8, 9.). Plymouth and Ogwell limestones. ———— ? ramosa, (Brassart). The Rev. D. Williams’s cabinet. Near Chudleigh. — Gothlandica, (Goldf., Pl. XXVI. f. 3. Silur. Syst., Pl. XV. bis, f. 3, 4.). Plymouth limestone ; apparently scarce. fibrosa, (Goldf., Silur. Syst., Pl. XV. bis, f. 7.). A single imperfect specimen of this species is in Professor Sedgwick’s collection from Fowey ; it occurs also at Barton, near Mary Church. Porites pyriformis +, (Ehrenberg, Goldf., Pl. XXI. f. 7. Silur. Syst., Pl. XVI. f. 2.), Common Pa the Ogwell limestone ; it occurs also near Plymouth, and Mary Church. Pl. LVIII. g. 4. Cyathophyllum turbinatum, (Goldf., Pl. XVI. f. 8. Silur. Syst., Pl. XVI. f.11.). A fragment in the Rev. R. Hennah’s collection. i cespitosum +t, (Galdf., Pl. XIX. f. 2.). Very common near Plymouth and Ogwell; it occurs also near Torquay. PJ. LVIII. f. 8 to 8d. : Astrea (Favastrea) helianthoides, (De Blainville, Cyathophyl. helianthoides, Goldf., Pl. XX. f. 2.). Two specimens in calcareous slate from near Plymouth in the Rev. R. Hennah’s collection, and one in limestone in the Museum of the Geol. Soc. ; presented by the late Mr. Harvey. —— (————__) pentagonat, (De Blainville, Cyathophyl. pentagonum, Goldf., Pl. XTX. f, 3.). Plymouth, Ogwell, and Torquay limestones ; not very. abundant. Pl. LVIII. fel sy lias —— (Siderastrea, De Blainville,) Hennahii +, (sp. n.). Plymouth limestone and Barton Quarry near Mary Church. Pl. LVIII. f. 3 to 3b. Strombodes vermicularis, (Cyathophyl. vermiculare, Goldf., Pl. XVII. f. 4.). Common in the Plymouth and Ogwell limestones. Pl. LVIII. f. 7, 7 a. Stromatopora polymorpha +, (Goldf., Pl. LXIV. f. 8.). Two specimens from Appleway and near Teignmouth, in the collection of Mr. D. Sharpe. Pl. LVIII. f. 2. Coscinopora placenta 2+, (Goldf., Pl. IX. f. 18.). Common in the Ogwell and Plymouth lime- stones; it occurs also at Torquay, Whatcomb, Appleway, and Newton Bushel. Pl. LVIII. f.5 todd. Turbinolia? celticat, (Lamouroux, P]. LX XVIII. f. 7, 8.). Dinas Cove, Padstow, Berry Pomeroy, and Fowey. Pl. LVIII. f. 6. Fenestella antiqua +, (Gorgonia antiqua, Goldf., Pl. XXXVI. f. 19. Silur. Syst., Pl. XV. f. 15-18.). Common at Fowey, Petherwin; in yellow rotten slate in the neighbourhood of Plymouth; in North Devon the fossil occurs at Saunton, Linton, ? and north of Barnstaple. Pl. LVIII. f. 10 to 10b. Cystiphyllum Damnonienset, (sp. n.). Very abundant near Ogwell ; it occurs also near Ply- mouth, but sparingly. Pl. LVIII. f. 11 to 11b. Scyphia turbinatat, (Goldf., Pl. Il. f. 13.) Slate near Plymouth. Pl. LVIIT. f.9. The most abundant of the above species in the limestones of South Devon are Favosites poly- morpha, Porites pyriformis, Cyathophyllum cespitosum, Strombodes vermicularis, Coscinopora placenta, and Cystiphyllum Damnoniense, only the three first of which have been noticed in the Silurian System of England. The limestones are further characterized by the total absence of Catenipora escharoides, and by the absence or extreme scarceness of many of the corals most abun- dant in the Wenlock and lower Silurian formations. —_ ——— * The specimens from the Plymouth limestone, are principally in the cabinet of the Rev. R. Hennah ; those from the Ogwell limestone in that of Mr. R. A. C. Austen ; and those from Barton, near Mary Church, and Teignmouth, in the collection of Mr. Daniel Sharpe. + ‘The species thus distinguished are figured in Pl. LVIII., either on account of their being new, or characteristic of the Devonshire limestones. 638 Professor Sepewicx and R.1. Murcuison, Esq., on the Coupling this account with the near resemblance of some of the South Devon shells to known fossils of the mountain limestone, we at once establish our main position, that the South Devon fossils are of an intermediate type between those of the Silurian and carboniferous systems. It also follows from the same evidence, that the North and South Devon corals belong to rocks which are very nearly on the same parallel, as the most abundant corals of the lower North Devon groups agree specifically with the most abundant corals of the Plymouth and Tor Bay limestones. As far as regards the fossil shells, we must refer to the accompanying lists. We may however remark, in our present summary, that we have shells in the Plymouth limestone which make a near approach to Terebratula Wilsoni, Atrypa orbicularis, Orthis depressa, Pileopsis vetustatis, Nerita Haliotis, and Orthoceratites circularis, of the upper Silurian rocks. Most of them, however, when closely examined, present some points, we think, of specific difference. On the other hand, this limestone contains some genera and species very nearly resembling certain fossils (such as Pecten dissimilis (Phil- lips), P. plicatus (Sowerby), P. arenosus (Phillips), Terebratula acuminata (Sowerby), Producta analoga (Phillips), &c. &c.) of the carboniferous lime- stone. Lastly, we may remark, that many species in the Plymouth limestone (and those, we believe, the most abundant) are quite distinct from the fossils both of the carboniferous and Silurian systems ; among which we may point out a very large Atrypa, Buccinum spinosum, a large Natica, and several small univalves. (See the Lists.) We have many fossils from the neighbourhood of Newton Bushel, chiefly, however, in the form of siliceous casts: we forbear, however, to dwell on them, as Professor Phillips and Mr. Austen are, we believe, both engaged in their description. Some of them agree specifically with shells of the Ply- mouth limestone ; others are new; several of them nearly approach the forms ~ of the mountain limestone (as we learn from the description of Mr. Austen, and the recently published “ Report” of Mr. De la Beche); and the corals, at least the most abundant species, agree with corals of the Plymouth and IIfra- combe limestones. Such is a brief summary of the results arising out of an examination of the South Devon fossils ; and the conclusion to which they point appears to us absolutely inevitable, viz. that the South Devon series is intermediate between the carboniferous and Silurian systems, and consequently on the parallel of the old red sandstone. After the details of our previous communication, it is evident that all the calcareous slates on the south-eastern side of Cornwall are of the age of the owest group of the South Devon section, and therefore probably in the lower Physical Structure and older stratified Deposits of Devonshire. 699 portion of the old red sandstone. On the north-western coast of the county, we were preceded by Mr. De Ja Beche, and we must refer our readers to the many excellent details of his ““ Report.” A few of our fossils from both coasts will appear in the appended lists ; and, imperfect as they are, they appear to sanction our general views. The Petherwin, and we think also the highly crystalline Tintagel slates, appear to be of the age of the Barnstaple slates, and are therefore in the upper part of the old red sandstone. Such is a ge- neral summary of the evidence on which our proposed classification is founded ; and the result is given in our accompanying map. (PI. L.) ConcLupine Remarks, &c. Having stated the grounds on which we have endeavoured to establish the classification of the stratified rocks of Devonshire and Cornwall, it may be well, before we quit the subject, to notice certain objections that have been urged against our views. 1. In the first place, our evidence mav be considered defective, from the absence of the carboniferous limestone, which in many parts of the British Isles has so striking a position between the coal measures and the old red sandstone. To this we might reply, by pointing out several instances in the central counties of England, where the carboniferous system rests on the lower formations, without the intervention of any bands of limestone. We would, however, rather appeal to a more general fact—that the mountain lime- stone, after forming in the north of England a great succession of beds, and rising into mountains of considerable elevation, gradually thins out in its pro- longation towards the south ; so that in South Wales it occupies but one well- defined band, and at length so entirely dies away in the western extremity of Pembrokeshire, that the overlying culm measures and hard grits rest, in one district, immediately on older rocks, without the intervention of any calcareous matter whatsoever. With such a fact before us, we have no reason to be surprised at the absence of the mountain limestone, where the culm measures reappear in Devonshire and Cornwall. Considering the enormous thickness of the culm measures of these coun- ties, it is by no means improbable that the mountain limestone is there repre- sented by contemporaneous deposits of a different mineral type. For surely it is now needless for us to prove that rocks, identical in geological position, may entirely change their lithological structure, as they pass from one county to another. A change of structure, however, implies a change of conditions during the time of the deposit; and such a change might greatly modify the forms of animal life. In this way we might, perhaps, explain the absence of VOL. V.—SECOND SERIES. Ax 700 Professor Srpewick and R. I. Murcuison, Esq., on the many of the best-known mountain-limestone fossils from the carbonaceous shales and sandstones of the lower culm measures of Devonshire. 2. Again, it has been objected, that the fossils of the Devonian groups, now classed with the old red sandstone, are not the same with the known fossils of that formation. We allow that the fossil fish of the old red sandstone have not yet been dis- covered among the Devonian rocks. But how can we build any conclusion on such a mere negative fact? The same genera and species are not distri- buted through the whole extent of every formation. Moreover, who can tell that fossil fish will not hereafter be discovered among the calcareous slates of Devonshire? But there isa more positive objection to be noticed, viz. that the known fossil shells of the old red sandstone differ greatly from those we have obtained from the Devonian groups. To this we may reply, that the shells hitherto described from the old red sandstone are derived exclusively from its very lowest beds, which probably do not appear on any of our pre- vious sections. These objections are, however, of little weight against the broad fact (which, in truth, forms the sum and substance of our evidence), that the fossils described in this paper are of a type intermediate between the types of the carboniferous and Silurian systems*. 3. The extreme change, among the formations we have described, of the ordinary mineral type, is another objection to our views. It has been noticed in various parts of our two memoirs, and considered at some length in our paper, of April last, in the Philosophical Magazine ; we need not, therefore, dwell upon it now. But we may briefly state, that as the old red sandstone exhibits so many changes of structure, in its range from the Orkneys to the north side of the Bristol Channel, we have no difficulty in admitting still fur- * Were it true, that species abounding in the mountain limestone, and disappearing in the de- scending sections, appeared again in still lower parts of the gray-wacké series; there would then be comparatively little weight in our evidence, or certainty in our conclusions. But we have no such antagonist fact now to contend with. In a paper, published (April 1839) in the Philoso- phical Magazine, we expressed our hopes that the views of classification we then threw out might cast some light on the structure of the south of Ireland ; and before our paper was struck off, we became acquainted with the contents of a memoir by Mr. C. W. Hamilton, to which we alluded in a postscript. At the very meeting which followed that on which our present paper was read before the Geological Society, Mr. Griffith exhibited a copy of his Geological Map of Ireland, and read a memoir, illustrated by sections, and accompanied by fossils; by help of which he showed, we think, to demonstration, that there is no anomalous recurrence of the carboniferous fossils among the true gray-wacké rocks of the south of Ireland. His sections of the rocks im- mediately below the mountain limestone exhibited a broken, imperfect series; most instructive, however, in one respect, as showing an undoubted ascending passage into the limestone. | : | | | | Physical Structure and older stratified Deposits of Devonshire. 01 ther changes, if supported by the evidence of fact or rational analogy. What difficulty is there in believing that a marine formation should, in one part of the world, have gone forward so tranquilly as to allow all the ordinary opera- tions of animal life ; while, in another part, the deposits of the ocean were in- terrupted or modified by rude mechanical movements, incompatible with the existence of organized beings? We see no difficulty whatsoever in the mi- neral structure of what we now regard as the old red sandstone of Devon- shire and Cornwall. The classification we adopt is derived from its own appropriate evidence; and it at the same time removes the greatest difficulties presented by the unexplained phenomena of our older formations; gives a natural sequence and meaning to their history ; and, we may add, gives a symmetry to the disposition of the colours on our geological maps, which they never had before. The strongest proofs are given in this and our previous paper, of the insuffi- ciency of mineral character, taken alone, to determine the epoch of any doubtful formation : and as the term gray-wacké has done much disservice to geology, by inducing observers to merge, under one unmeaning name, deposits be- longing to distinct periods in the history of the earth, we venture to hope that the word may henceforth be discarded as a term of classification. Used for the mere purpose of mineral description, we can of course make no similar objections to it. 4. Lastly, we may remark, that in all the descriptions, both of this and our previous paper, we have, for obvious reasons, drawn our analogies from the nearest formations of our own island. But we cannot forbear expressing our belief, that the series of rocks of Devonshire and Cornwall, above described, may serve to clear up some of the difficulties in the classification of the older formations of the continent of Europe, where the old red sandstone has seldom been found, at least in what has been hitherto regarded as the ordinary British type. But now that the old red sandstone has been exhibited in such a different form, on such a vast scale, and with its own series of organic remains, we have little doubt that its true equivalents will be found distributed through various parts of Europe. ‘To obtain, as far as possible, satisfaction on some of these points, is the first task we propose to ourselves during the investigations of the approaching summer. Though the term old red sandstone, when designating great groups of rocks like the Cornish kzllas and Devonian slates, should involve no error of classification, still it would, mineralogically, be most inappropriate. We pur- pose therefore, for the future, to designate these groups collectively by the name Devonian system, as involving no hypothesis, and being agreeable to Ax2 702 Professor Sepewick and R. I. Morcuison, Esq., on the analogy. Thus the terms Carboniferous system, Devonian system, Silurian system, and Cambrian system, will represent a vast and apparently uninter- rupted sequence of deposits ; each having, as a whole, zoological and (often also) mineralogical characters of its own, yet each passing into the system next in order by almost imperceptible shades of difference. The old palgo- zoic rocks appear, therefore, notwithstanding their enormous scale, and the wide diffusion of the same organic types, to have been formed in subor- dination to the same laws which, in after periods, produced the more clear succession of our secondary formations. Foreland. Dartmoor. English Channel. SSN. SES Section from the Foreland on the Bristol Channel to the English Channel. For the details of the portion between the Foreland and Dartmoor, see Plate LI. fig. 1. Physical Structure and older stratified Deposits of Devonshire. 703 LIST OF ORGANIC REMAINS principally contained in the Cabinet of the Rev. R. Hennah, F.G.S., or collected by the Authors. The Corals have been determined chiefly from Specimens in the possession of Mr. Austen and Mr. Daniel Sharpe. A MS. Catalogue of Devonshire Fossils by Mr. Austen has also been used in preparing the Table-—May 30, 1840. Groups anp Locatirizs. AuTHORS AND REFERENCEs. : GENERA AND SPECIES. Culm Barnstaple | Lower Groups The numerals refer to the plates which illustrate the ,| Measures, |and Petherwin| N. Devon, Lower Groups, South Devon, memoir, p. 693. | Group, p. 694. p- 696. p. 696. Puants, p. 681. P. blechnoides & P. lonch.A. Brongn. 84. : ne f. 1-7. Filic. lonchiticus, Schloth. Flor. Bidef Pecopteris lonchitica............ d. Vorw. 11. f.32. Alethopteris lonchi- ¢ Bide ord. tid. &A.vulgat.Sternb.Flor.d.Vorw.55. ee — MULICACA coccsccesceese* Jal Leieoyiyeaay OU Ih Bip tn Oia caccodosecegooone Ibid. ‘ A. Brongn. 85. Foss. Fl. 202. Dela Beche, Ibi ———— Beri ..rese0e0 gets Rep. pe luo. ccvcesedeies taste attectasenes bid. aren Sternb. Tent. Fl. Primord. 22. A.B : Neuropteris gigantea............ { an Rate Fl. aeen ete tie Capea’ Ibid. ee VOONUATA ccacccseercneee AY Brongn. 64, f. 5. Foss. Fl. ‘41 Sobonccaoones Ibid. a A. Brongn. 72, f. 1,73. Foss. Fl. 4, 9, De : Loshii «..... oqga¢e { laiBeche; Rep. 1265 0--..sseceres-seerene Ibid. A. Brongn.71,72, f. 2. Foss. Fl. 183, 197, : heterophylla...... { 200. De la Beche, Rep. p.126. ...... Ibid. Sphenopteris latifolia .........+ ..|A. Brongn. 57, f. 1-4. Foss. Fl. 156,178. | Ibid. =. MACUL Bs cocneciteocse A. Brongn.57,f.5. DelaBeche, Rep.p.126.| Ibid. Calamites undulatus ............++: No LBHONVA IG is tin Woes gaocagoqcaccocooaseodnee Ibid. ee ATENACCUS! cc'ccccceceoe A. Brongn. QHetanln (LOp tse Oteencdacees Ibid. IPOACIECS COCOINA ...cocceccccoves ses Hosseolloraspl 4 Qu pecacescecsasneeneece moses | ML DIGs Asterophyllites foliosa ............ Mosse Mloran25rcsccwseucecedsucssestscctorssere Ibid. Cyperites bicarinata ............++. Boss:hloras 43st l= Se cscecccscesecerccsnsnecs Ibid. For observations on the Sloly Vejgetable Remains, see pp. 683, 695. Cora.s, p. 697. Scyphia turbinata .............. pee Golds 2; fags Vill) OW. acme sctenaseeeeee PA becroctepces tere Seasdiee stely-tepewaemocs Plymouth. (way, Torquay. Coscinopora placenta? ........... Goldf.95 °F; 182 TiVILDD. 5=dk. ceccseccasccecmens|seecese cee se sanccaceesces|scceeesnenemet Ibid. Ogwell, Newton, Apple- ; : ie a Gee Cove Padstow, Berry Petraia (Munster) celtica ......... TurbinoliaLamx.Exp.M.78,f.7,8. LVIII.6,|........s00[seeereeeeanseee|eeeeeeeeeeseens Pomeroy, Crownall Bay. Strombodes vermicularis ...... ee CyathophwylsG oldfaslijaits ep le Allien aasees | Reseeeeneere leceete eesti: |aaeaeetiaeeaeee Plymouth, Ogwell. Cystiphyllum Damnoniense...... DAA 010 a OT] ameenpetceoonoarecacone vab.cocacoctood Decoceustuad abononndeccapoe dare daogdaDdhan Ibid. Ibid. Newton. Cyathophyllum turbinatum ...... Goldf. 16; #9. SilursiSyst. 10) fplileae csrelegsessee. of |-cnceecmeerens|eneseensatenes Ibid. ; ——_——— cespitosum......|Goldf.19,f.2. Silur.Syst.16,f.10. LVIIL8-d.).....cscce.fecceeeseeeeeees Ilfracombe. bid. Ibid. Torquay. quadrigeminumis| Golda 1S vt Onn aceesecencseeteneesececctenetees neonecteeesa|seausceacerents Ibid. De Bl. Man. d’Actin. 375. Cyathophyl. i Astrea pentagona .......+s..006. { Goldf. 19, f. 3. LVI. 1 Danner eas! merece ep ece peveeoocrrinone Pockercachootc Ibid. Newton. ——-- helianthoides...... aren | Maaco oan: Be (uiadnoo ig \ daectrccdocl shaconocee aoe Ibid. _|Ibid. er rennahil. ooceccscocoocace, MUWIDT < Seb: scaticecesstons eke ootetenescesc en aoe ee ray as Ibid. Ibid. Barton. Marychurch. Porites pyriformis.........ssssees. Ehrenb. Silur. Syst. 16, f. 2¢. LVILL. 4-f, fosc......c.,|esseseeeesesse. Ibid. _ Ibid. Favosites polymorpha... ......... Goldf." 27, £14. /Silur. Systepl psig. 2emeeneer herees ane lanaeonetn sce Ilfracombe. |[bid. Newton, Barton, Torquay, SPONgItES <- ccasooonn aggoaneoe NCODACARCOC HA papacnben|aanen WY Yai OY Coe nan en a Pe ee sewetaee wre Leds o[ See eek Ibid. |) Avicula Damnoniensis .........++- ND pT ere ae a vedauese COE REOCOCOSSAECOd 1 Daan! Ibid. Subradiata -secsce6. Sose ds LOD Sant ccheed eee sc Sestssllsandseddddacaccesscncecticss Been a Petherwin pectinoides .......+. saneee DVay Dame vestacaceee atecee Sauladeledddecestes ottres|cemene eeeeee(lb, Barnst } Posidonia lateralis,..... Remeuse case (lDpilicscetcncvesscaveeccses weneddaddvesesatentes ---In* Barnst. | Becheri...... Seasvewesisos| Mull Dei34 Valey 4a. |coacee eieeseccidede dhocdsosucos Ibid. TUDEECH Ata Nos ccios ts soees LAaBy ved Novscsces Weeeeecvescecwessdeetcenes ++eeeee|Budle nt Balmbro’. CLE NEXIS scceccccscccess sone (MLM lA iacswerccsewes Seesevcsadccctusecwecseeenzte Sdeccecdeee Barnstaple transversus ......... cectese| Lal Navaueryeceseese contain thin beds of impure limestone, 678 note. account of the bands of culm near Bideford, 680. = fe on eee —— OE, the plants obtained from, 681. — considered to be the equivalent of the ordinary British coal-fields, 682, 688. Upper lias shale, description of, at Easington Heights, 215. characteristic fossils, 215, 221. systematic list of the fossils, 219. -——-——~ section of the beds, 221. Upper Silurian rocks, notice of, in Coalbrook Dale, 419. Urgub, structure of the country near, 592, 593. conical hills near, 593. Utch-hissar, description of the country near, 592. conical hills of, 592. V. Valdivia, motion of the ground at, during the earthquake Feb. 1835, compared to the bending of a sheet of ice, 620. Valley of rocks, notices respecting, 640, 641, 644, 645. Valleys, between granite hills, north coast of the St. Lawrence, occupied by beds of gravel, sand and clay, 89. of elevation, remarks on, 640 and note. Vegetable organics, notice of, in the Bermudas, LS. INDEX. 753 Verschoyle, Archdeacon, notices on the geology Volcanos and earthquakes, apparent connexion of, of the north coast of Mayo and Sligo, 149. Vertebra, Mr. Owen on the composition of a, 518. Vertebral column, exposition of the general cha-~ racters of the, in Plesiosauri, 521. Veryan Bay and Looe, Killas thrown into a trough between, 666. Villarica, volcano of, not affected during the out- bursts in the Cordilleras and the earthquake, 1835, 605, 631. action of, during the earthquake, 1822, 605, 631. Volcanic eruptions, proofs of distinct periods of, in Cutch, 312. -—————- recent outbursts of, inCutch, 316. -————- have occurred at all ‘epochs in the earth’s history, 624. outbursts, considered to be effects of the same force as that which elevates conti- nents, 606, phenomena, tables of, by A. de Hum- boldt and Mr. Darwin, 610. rocks, structure of, in part of Asia Minor, 584, 591, 592, 594, 595. —————— and trappean rocks, account of, in Cutch, 306. Volcanos, on the formation of, as one of the effects of the same power by which continents are elevated, 601. in South America, contemporaneous outbursts of, 604. — Osorno, Minchinmadom, Cor- covado, Yantales, &c. Feb. 1835, 604, 607. Osorno and Corcovado, Nov. 1835, 604. Osorno, Aconcagua and Cose- guina, January 1845, 611, 612. ——————————— not equally affected during periods of renewed energy, though situated on the same chain, 605. of the Cordillera may be grouped into systems, 614. the vents of each system probably united, but no proofs that the systems are, 614, and earthquakes, apparent connexion of, in South America, 602, 611. in South America; eruptions of Osorno, Cor- covado, &c. and the earthquakes of Feb. and Nov. 1835, 604, 606. near Valdivia, and the destruction of Valparaiso, 1822, 606 note. ——_——_____—_———— of Patas and Lucanas, and the overthrow of Lima, 1746, 606 note, 614. ———__—\_—__——— of Pasto and the de- struction of Riobamba, 606. proofs of connexion not always decisive, 611, 612. observation of Ulloa re- specting the connexion of, 615. Voysey, Dr., notice of his discovery of fossil freshwater shells in India, 570. by, of the country near the Taptee, 571. on the — rivers Kistnab and Pennar, 574. WwW. Warwick, remarks on the upper portions of the new red sandstone system near, 337. sandstone of, described, 342. — occupies the same po- — sition as the sandstone of Ombersley and Bromsgrove, 342, 345. fossils found in, 343. concluding observations respecting, 345. Warwickshire, description of the upper forma- tions of the new red sandstone system in, 331. Water, account of supplies in the Bermudas, 120. Waterford, county, description of the metallife- rous deposits in the transition series of, 24. ee transition series in, 12. mountains, highest point of, above the level of the sea, 6. Waters’-meet, notices respecting the strata near, 644. Wavellite obtained in Devonshire from the lower culm measures, 671. found in coal shales in South Wales, 671 note. 754 Weaver, Thomas, Esq., on the geological relations of the South of Ireland, 1. notice on the carbonife- rous series in the United States, by, 58 et seq. note. Wedgewood, planation of the process by which cinders and Esq., remarks on his ex- other substances become buried, 507. Weeley Barracks, section of a well at, 369. Wenlock shale and limestone, account of, in Coal- brook Dale, 419. Wetherell, N. Esq., observations by, on a well dug on the side of Hampstead Heath, 151. Wheal Betsey lead vein, situated in the culm measures, 670 note. —_.— Friendship copper vein, notice of its being situated in part in the culm measures, 670 note. Wherstead, section of a well at, 382. White chalk, account of, at Stevensklint, 247. - freshwater limestone, description of, in Asia Minor, 584, 589, 590, 595. ——- Hills, Gamrie, notice of patches of drained peat moss around, 148. - Nab, section of great oolite at, 231, 237. Whitton, section at, 379. Wickham Market, section of a well at, 377. Williams, Rev. David, on the raised beaches in Barnstaple or Bideford Bay, 287. notice of his finding vegetable remains in the quarry at Sloly, 648, 683. »—— collection of Devonshire and Cornish fossils, 692 note. Williamson, W. C. Esq., on the distribution of —_——_" fossil remains on the Yorkshire coast from the lower lias to the Bath oolite, 223. Willisham, sections of welis at, 379. Witnesham, section of well at, 379. Won, description of the hill of, 557. Wood, account of a piece of recent beech, partly petrified by carbonate of lime, 207. INDEX. Wood, account of a piece of recent beech, partly petrified by carbonate of lime, further notice of, 213. analysis of one of the petrified portions, 208. similar appearance in a specimen of silici- fied wood from Antigua, pointed out by Mr. R. Brown, 208. Woodbridge, sections of wells near, 382. Woolverstone, sections near, 381. Woombridge, section of beds in the coal shaft at, below the flint coal, 479. pit, next the engine, section of, 480. sections at, 475. Worcestershire, description of the upper forma- tions of the new red sandstone system in, 331. Wrekin, account of the faults on the flanks of the, 458. —__——— structure of the, 449. Wright, Romley, Esq., on the Brown Clee Hill, 125. Y. Yantales, phenomena presented by, Feb. 1835, 604, 607. Yealm, notice of the beds south of the, 658. Yew-tree pit, Calcut field, Broseley, section of, 481. 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Mémoires de la Société Géologique de France, tome The Geological Society of premier, deuxiéme partie. 4to. Paris 1834. France. Bulletin de la Société Géologique de France, tome 6, feuilles 5—20. SCO OOS COCOA Table des Matiéres et des Auteurs pour le quatriéme vo- lume du Bulletin de la Société Géologique de France, par M. Clement Mullet. 8vo. 1834. aha ists! eave Wins Sass. 0 Liste des Membres de la Société Géologique de France en Mars 1835. 8vo. fia wire Uslens Ss «b%02s Rapport sur les Travaux de la Société Géologique de France pendant les Années 1832 et 1833, par M. Puil- lon de Boblaye, tome 4. 8vo. Paris 1834. = = = =. cavevecees Bye Résumé des Travaux de la Société Géologique de France et des progrés de la Géologie en France depuis le ler Novembre 1833, jusqu’au ler Novembre 1834, par M. Rozet. 8vo. Paris 1835, woe 22. Illustrations of the Botany and other Branches of the Natural History of the Himalayan Mountains, and of the Flora of Cashmere, by J. F. Royle, Esq., F.L.S., G.S., part 8. 4to. London 1835. The Author. 23. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., vol. 29, no. 1, October 1835. 8vo. New Haven 1835. The Conductor. 1836. Jan, 1. Newton and Flamsteed ; being Remarks on an Article in no. 109 of the Quarterly Review, by the Rev. William Whewell, M.A., Fellow and Tutor of Trinity College, Cambridge. 8vo. London 1836. The Author. Catalogue of Fossil Fish in the Collections of Lord Cole and Sir Phiip Grey Egerton, arranged alphabetically, 1836. Jan. 7 16. 17. 19. VOL. V.—SECOND SERIES. 6. Last of Donations. BOOKS. with References to the Localities, Strata, and published Descriptions of the Species, by Sir Philip Grey Eger- ton, Bart., F.G.S. 8vo. Chester 1836. Des Cométes en général et de la formation de leurs queues, par M. T. Virlet. 18mo. Avesnes 1835. Mr. A. Nattali’s Catalogue of Books for 1836. 8vo. London 1836. Transactions of the Royal Academy of Lisbon, vols. 1 to 10, and part 1 of vol. 11. fol. Lisbon 1797—1831. Rules and Regulations for the Government of the Athe- num, with an Alphabetical List of the Members, &c. for 1835. 12mo. London 1835. . Proceedings of the Royal Society of London, no. 22, Session 1834-1835. 8vo. On the Genus Chama, with Descriptions of some Spe- cies apparently not hitherto characterized, by W. J. ‘Broderip, Esq., F.G.S., &c. From the tions of the Zoological Society, vol. 1. 4to. London 1835. Descriptive and Illustrated Catalogue of the Physiological Transac- Series of Comparative Anatomy contained in the Mu- seum of the Royal College of Surgeons in London, vol. 3, part 1.—Nervous System and Organs of Sense. 4to. London 1833. . Proceedings of a General Meeting of the Royal Asiatic Society, held on Saturday, 16th January, 1836. 8vo. . Transactions of the Geological Society of Pennsylvania, vol. 1, part 2. 8vo. Philadelphia 1835. . ‘ Newton and Flamsteed,” being Remarks on an Article in No. 109 of the Quarterly Review, 2nd edition ; to which is added, Two Letters occasioned by a Note in No. 110 of the Review ; by the Rev. William Whewell, M.A., Fellow and Tutor of Trinity College, Cambridge. 8vo. London 1836. Narrative of an Excursion to the Lake Amsanctus, and to Mount Vultur in Apulia, in 1834, by Charles Daubeny, M.D., F.R.S., Professor of Chemistry and Botany. 8vo. Oxford 1834. Notices of Communications to the British Association for the Advancement of Science at Dublin in August 1835. 8vo. London 1836. An Account of the Mining Districts of Alston Moor, Weardale, and Teesdale, in Cumberland and Durham, comprising Descriptive Sketches of the Scenery, Anti- quities, Geology, and Mining Operations in the upper B DONORS. The Author. The Aithor. Mr. A. Nattali. The Royal Academy of Lis- bon. The Athenzum Club. The Royal Society. The Author. The Royal College of Sur- geons. The Royal Asiatic Society. The Geological Society of Pennsylvania. The Author. The Author. The British Association. List of Donations. 1836. BOOKS. Dales of the rivers Tyne, Wear, and Tees, by T. Sop- with, Land and Mine Surveyor. 8vo. Alnwick 1833. Feb. 19. Geological Sections of Holy-field, Hudgil Cross Vein, and Silver Band Lead Mines, in Alston Moor and Teesdale, by T. Sopwith, Land and Mine Surveyor. 4to. and plates, fol. Newcastle 1829. 24, Essai sur la Constitution Géognostique du St. Gothard, par M. Charles Lardy. 4to. . 27. Bulletin de la Société Géologique de France, tome 6, feuilles 1, 2. 8vo. Paris 1836. Medical and Physical Researches, or original Memoirs in Medicine, Surgery, Physiology, Geology, Zoology, and Comparative Anatomy, by Richard Harlan, M.D., F.L.S., &c. 8vo. Philadelphia 1835. The Mechanics’ Magazine, Museum, Register, Journal, and Gazette, no, 645, December 1835, containing Mackintosh’s Electrical Theory of the Universe. 8vo. London 1835. 11. Twenty-five copies of Mr. W. S. B. Woolhouse’s Tables of Continental, Lineal, and Square Measures. A Catalogue of 7385 Stars, chiefly in the Southern He- misphere, prepared from Observations made in the years 1822—1826, at the Observatory at Paramatta, New South Wales, founded by Lieut.-General Sir Tho- mas Macdougall Brisbane, K.C.B., F.R.S., Pr. R.S. Ed. The Computations made and the Catalogue constructed by Mr. William Richardson, of the Royal Observatory at Greenwich. Printed by Order of the Lords Com- missioners of the Admiralty. 4to. London 1835. Proceedings of the Royal Society of London, no. 23, Session 1835-1836. 8vo. Transactions of the Society for the Encouragement of Arts, March 8. 16. 19. Manufactures, and Commerce, vol. 50, part 2, 1835. 8vo. London 1835. Illustrations of the Geology of Yorkshire, by Professor Phillips, F.R.S., G.S., &e., part second, Mountain Limestone District. 4to. London 1836. Bryant’s Catalogue of Books for 1836. 8vo. London 1836. On the Occurrence of the Megalichthys in a bed of Can- nel Coal, in the west of Fifeshire, with Observations 2S on the supposed Lacustrine Limestone at Burdie House, by Leonard Horner, Esq., F.R.S. L. & E., F.G.S., &c. Ato. April 4, The Third Annual Report of the Royal Cornwall Poly- technic Society, 1835. 8vo. Falmouth 1836, DONORS. The Author. The Author. The Author. The Geological Society of France. The Author. T. S. Mackintosh, Esq. Mr. J. Weale. The Lords Commissioners of the Admiralty. The Royal Society. The Society of Arts. The Author. Mr. J. Bryant. The Author. The Royal Cornwall Poly- technic Society. 1836. April 6. 19. 25. May 2. List of Donations. BOOKS. Mémoire de Physiologie Agricole sur la Végétation des Céréales sous de hautes températures, par M. Ed- wards, de l'Institut de France, &c., et M. Colin, Pro- fesseur a l’Ecole Royale Militaire de Saint-Cyr, &c. 8vo. Versailles 1836. The American Journal of Science and Arts, vol. 29, no. 2, January 1836, conducted by Benjamin Silliman, M.D., LL.D., &c. 8vo. New Haven 1836. Memoirs of the Royal Academy of Lisbon, vol.11, part 2, fol. Lisbon 1835. Journal of the Royal Asiatic Society of Great Britain and Ireland, no. 5, March 1836. 8vo. London 1836. On an Artificial Substance resembling Shell, by Leonard Horner, Esq., F.R.S. L. & E., with an Account of an Examination of the same by Sir David Brewster, LL.D., F.R.S., &c. 4to. From the Transactions of the Royal Society, 1836, part 1. London 1836. Dictionnaire Géographique de la Province de la Flandre, Orientale, par M. Vander Maelen, F.G.S., &c. 8vo. Bruxelles 1834. Lettre sur 1’Etablissement Géographique de Bruxelles, fondé en 1830,par Vander Maelen.18mo. Bruxelles1836. Ouvrages publiés par l’Etablissement Géographique de Bruxelles. 12mo. Bruxelles 1836. . Journal of the Bahama Society for the Diffusion of Know- ledge, November 1835. 8vo. Bahama. Proceedings of the Royal Asiatic Society of Great Britain and Ireland, March 19th, 1836. 8vo. 8. Mr. A. Nattali’s Catalogue of Books for 1836, part 2. 8vo. 10. . Illustrations of the Botany and other Branches of Natu- ral History of the Himalayan Mountains, and of the Flora of Cashmere, by J. Forbes Royle, Esq., F.G.S., &e. part 9. fol. London 1836. ). The Royal Society in the 19th Century, by A. B. Gran- ville, M.D., F.R.S., G.S., &c. 8vo. London 1836. Explication de trois planches d’Ammonites, par M. Leo- pold de Buch. 4to. Explication de deux planches de Spirifer et d’Orthis ; par M. Leopold de Buch. fol. 1836. . Mémoires pour servir a une Description Géologique de la France, redigés par ordre de M. le Directeur de l’Ad- ministration Générale des Ponts et Chaussées et des Mines, sous la Direction de M. Brochant de Villiers, par MM. Dufrénoy et Elie de Beaumont, tome 3. 8vo. Paris 1836. B2 DONORS. The Author. The Conductor. The Royal Academy of Lis- bon. The Royal Asiatic Society. L. Horner, Esq., F.G.S. M. Vander Maelen, F.G.S: The Bahama Society. The Royal Asiatic Society. Mr. A. Nattali. The Author. The Author. The Author. eeeeooveece The Authors. List of Donations. BOOKS. Report of the Directors of the Manchester Mechanics’ Institution, and Proceedings at the Annual Meeting of the Members, held in the Theatre of the Institution, Cooper-street, on the 25th February 1836. 8vo. Man- chester 1836. . Transactions of the Zoological Society of London, vol. 1, part 4, 4to. London 1836. Proceedings of the Zoological Society of London, from June to December, 1835. 8vo. . Nouvelles Annales du Muséum d'Histoire Naturelle, ou Recueil de Mémoires publiés par les Professeurs de cet Etablissement et par d’autres Naturalistes sur ]’Hi- stoire Naturelle, l’Anatomie, et la Chimie, tome 4. 4ieme livraison. 4to. Paris 1835. Liste des Dons faits 4 la Bibliothéque du Muséum d’Hi- stoire Naturelle pendant l’année 1835. 4to. Paris 1836. . Geological Notice on the New Country passed over by Captain Back during his late Expedition, by W. Henry Fitton, M.D., F.R.S., G.S., &c. 8vo. London 1836. . Journal of the Royal Geographical Society of London, vol. 6, part 1, 1836. 8vo. London 1836. Analyse de la partie du Traité sur la Chaleur, de M. Poisson, qui se rapporte 4 la Chaleur Terrestre, par M. Auguste de la Rive. 8vo. Paris 1835. Recherches sur les Organismes Inférieures, par M. F. Dujardin. 8vo. Paris 1835. Hermés, Journal des Nouvelles Scientifiques, &c. no. 1 —6. 4to. Paris 1836. . A popular Description and History of the Giraffes or Camelopards, now exhibiting in the Zoological Gar- dens, Regent’s Park, with an Account of their Nubian Attendants, and the Adventures of M. Thibaut, who procured them in Africa, by a Naturalist. 8vo. Lon- don 1836. » The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., &c., vol. 30, no. 1, April 1836. 8vo. New Haven. A Geological Sketch of the Tertiary Formations of Gra- nada and Murcia, in Spain, with Notes respecting the Primary, Secondary, and Volcanic Rocks in the same District, by Charles Silvertop, Esq., F.G.S., &c. 8vo. London 1836. Abbildung und Beschreibung einiger neuen oder wenig gekannten Versteinerungen aus der Kalkschieferforma- tion von Solenhofen, von Dr. Eduard Riippell. 4to. Frankfurt a Maine 1829. DONORS, The Manchester Mechanics’ Institution. The Zoological Society. The Natural History So- ciety of Paris. The Author. The Royal Geographical Society. The Author. The Author. M. F. Dujardin. Mr. Booth. The Conductor. The Author. The Author. 1836. Last of Donations. BOOKS. June 10. Osservazioni Fisico-Geognostiche fatte in un Viaggio per 13. 14, 16. 21. diversi luoghi delle Provincie di Terra di Lavoro e di Abruzzo, nella State del 1834, dai Signori Gussone e Tenore, per disposizione della Reale Academia di Scienze. 4to. An Address delivered at the Fifth Annual Meeting of the Geological Society of Dublin, on the 10th of February, 1836, by Richard Griffiths, Esq., President of the Society, F.G.S., &c. 8vo. Dublin 1837. Schloss Hainfeld, or a Winter in Lower Styria, by Capt. Basil Hall, R.N., F.R.S., &c. Svo. Lond. & Edin. 1836. Mémoires de la Société Linnéenne de Normandie, publiés par M. de Caumont, Correspondent de l'Institut, &c. vol. 4, pour 1829—1834. 8vo. Caen 1835. Séances publiques de la Société Linnéenne de Normandie tenue a Falaise, le 5 Juin, 1834, et a Bayeux le 4 Juin, 1835. 8vo. Caen 1834-1835. Transactions of the American Philosophical Society held at Philadelphia for promoting Useful Knowledge, New Series, vol. 5, part 2. 4to. Philadelphia 1836. Address of Earl Stanhope, President of the Medico-Bo- tanical Society, on the Anniversary Meeting, January 16th, 1836. 8vo. London 1836. Notice of the Academy of Natural Sciences of Philadel- phia, with an Appendix, 3rd edit. 4to. Philadelphia 1856. The Mining Review and Journal of Geology, Mineralogy, and Metallurgy, conducted by Henry English, Esq., F.G.S., no. 8, June 1836. 8vo. London 1836. A Letter to the Right Hon. Thomas Spring Rice, M.P., Chancellor of His Majesty’s Exchequer, &c. &c., con- taining a Plan for the better Management of the Bri- tish Museum, by John Millard, employed for eight years in preparing a new General Index to all the col- lection of MSS. in the British Museum. 8vo. Privately printed 1836. Excursions illustrative of the Geology and Natural Hi- story of the Environs of Edinburgh, by William Rhind, M.R.S., &c., 2nd edit. 12mo. Edinburgh 1836. . Abhandlungen der Koniglichen Akademie der Wissen- schaften zu Berlin, aus dem Jahre 1835. 4to. Berlin 1836. Bericht iiber die zur Bekanntmachung geeigneten Ver- handlungen der Kéniglichen Preus. Akademie der DONORS. I] Signore Tenore. The Author. The Author. The Linnean Society of Normandy. The American Philosophi- cal Society of Philadel- phia. The Medico-Botanical So- ciety. The American Philosophi- cal Society of Philadel- phia. The Conductor. The Author. The Author. The Berlin Academy. Last of Donations. 1836. BOOKS. DONORS. Wissenschaften zu Berlin im Monat Januar 1836. 8vo. Berlin 1836. The Berlin Academy. June 24. Bulletin de la Société Géologique de France, tome 6, feuilles 21—25, et tome 7, feuilles 8—10. 8vo. Paris The Geological Society of 1836. France. July 2. Proceedings of the Royal Society of Edinburgh, Nos. 8 The Royal Society of Edin- and 9. 8vo. burgh. Proceedings of the Royal Society of London, nos. 24 and 25, 1835-86. 8vo. : The Royal Society. Analyse des Travaux de la Société Linnéenne de Bor- deaux, par M. J. L. Laporte, pendant les Années The Linnean Society of 1832—1834. 8vo. Bordeaux 1835. Bordeaux. 7. Discours sur la Méthode suivie actuellement dans I’Etude des Sciences, par Marcel de Serres, Professeur de Mi- néralogie et de Géologie 4 la Faculté des Sciences de Montpellier. 8vo. Montpellier 1834. The Author. Mémoire sur la question, de savoir, si des Animaux Ter- restres ont cessé d’exister depuis l’apparition de Homme, et si 1Homme a été contemporain des Es- péces perdues, ou du moins qui ne paraissent plus avoir des représentans sur la Terre, par M. Marcel de Serres, tiré de la Bibliotheque Universelle. 8vo. 1834.(Dup.) .......0. Observations sur les Rhinocéros Fossiles et Humatiles, ou Rapport fait a la Faculté des Sciences de Montpellier par M. Marcel de Serres, chargé de présider la Dis- sertation Inaugurale de M. de Christol, intitulée “ Re- cherches sur les Caractéres des Grandes Espéces de Rhinocéros Fossiles.” 8vo. i Unieweln oe Observations sur la Licorne des Anciens, par M. Marcel de.Serres.. v0. 4/1 -) - = cA ee ee cece eeees Essai sur la question, de savoir, sil’Observation faite dans les Mines de Houille duCanada et de la Baie de Baffin de Plantes analogues a celles qui vivent maintenant dans les Régions Equatoriales, annoncent un Changement dans I’Inclinaison de |’Ecliptique? par M. Marcel de Serres. (Dup.) eeeceees ee Discours sur les Differences des Dates données par les Monumens et les Traditions Historiques, et celles qui resultent des Faits Géologiques, par M. Marcel de Serres, ,Svo.,, Lonlouse 1835. © . |!) /O RD eeeeiee os Observations sur les grandes espéces d’Ours des Ca- vernes, par M. Marcel de Serres. 8vo. BAICIAOGACC Les Animaux et les Végétaux dont on ne retrouve plus les Analogues a la Surface de la Terre, peuvent-ils étre 1836. July 15. 23 dug. 4. 10. 26. 13. List of Donations. BOOKS. considérés comme les Souches des Races actuelles ? par M. Marcel de Serres. 8vo. Toulouse 1835. Sixth Report of the Scarborough Philosophical Society. 8vo. 1836. Some Remarks on the Study of Geology and on the pre- sent State of the Science, by the Rev. Leonard Jenyns, M.A., F.L.S., F.G.S., &c. From the Magazine of Zoology and Botany. 8vo. List of Premiums for 1836-7 and 1837-8, offered by the Society for the Encouragement of Arts, Manufac- tures, and Commerce. 8vo. London 1836. The Journal of the Asiatic Society of Bengal, vol. 4, 1835, edited by James Prinsep, F.R.S., Secretary of the Asiatic Society. 8vo. Calcutta 1835. Premier et Second Mémoires sur les Echinides, par M. Charles des Moulins, Correspondant de la Société Lin- néenne de Bordeaux. 8vo. Bordeaux 1835. Proceedings of the Royal Asiatic Society of Great Britain and Ireland, May 1836. 8vo. On the Geology of Auvergne, particularly in connexion with the Origin of Trap Rocks and the Elevation Theory, by Professor Forbes. From the Philosophical Journal for July 1835. 8vo. London 1835. Transactions of the Linnean Society of London, vol. 17, part 3. 4to. London 1836. . List of the Members of the Linnean Society for 1836. 4to. . Descriptive and Illustrated Catalogue of the Physiologi- cal Series of Comparative Anatomy contained in the Museum of the Royal College of Surgeons in London, vol. 3, part 2.—Connective and Tegumentary Systems and Peculiarities. 4to. London 1836. On the General Magnetic Relations and Characters of the Metals, by Michael Faraday, D.C.L., F.R.S., &c. 8vo. London 1836. On a peculiar Voltaic Condition of Iron, by Professor Scheenbein of Bale, in a Letter to Mr. Faraday, with further Experiments on the same subject, by Mr. Fa- raday, communicated in a Letter to Mr. Phillips. 8vo. London 1836. Reply to Dr. John Davy’s “‘ Remarks on certain State- ments of Mr. Faraday, contained in his ‘ Researches in Electricity,’ by Michael Faraday, D.C.L., F.R.S., &c. 8vo. London 1836. On the History of the Condensation of the Gases, in Re- ply to Dr. Davy, introduced by some Remarks on that DONORS, The Author. The Scarborough Philoso- phical Society. The Author. The Society of Arts. The Asiatic Society of Ben- gal. The Author. The Asiatic Society of Great Britain. The Author. The Linnean Society. The Royal College of Stir- geons. The Author. The Author. The Author. List of Donations. 1836. BOOKS. of Electro-Magnetic Rotation, by Michael Faraday, Esq., D.C.L., F.R.S., &c. in a Letter to Richard Phil- lips, Esq., F.R.S., &c. 8vo. London 1836. Aug. 26. Ona supposed new Sulphate and Oxide of Antimony, by Michael Faraday, D.C.L., F.R.S., &c. 8vo. Lon- don 1836. Letter from Mr. Faraday to Mr. Brayley on some for- mer Researches relative to the peculiar Voltaic Con- dition of Iron, re-observed by Professor Schcenbein, supplementary to a Letter to Mr. Phillips. 8vo. Lon- don 1836. Sept. 1. Forség til et Grundrids af Mineraliernes Climatologie, ved H.C. Strém. 12mo. Aftryk af Magazinet for Natur-Videnskaberne. 2. Fifth Report of the British Association for the Advance- ment of Science, held at Dublin in 1835. 8vo. Lon- don 1836. Philosophical Transactions of the Royal Society of Lon- don, for the year 1836, part 1. 4to. London 1836. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., vol. 30, no, 2, July 1836. 8vo. New Haven 1836. 10, Contributions to the Geology of the Tertiary Formations of Virginia, by W. B. Rogers, Professor of Natural History in the University of Virginia, and Henry D. Rogers, Professor of Geology in the University of Pennsylvania, F.G.S. 4to. Pennsylvania 1835. Report of the Geological Reconnoissance of the State of Virginia, by William B. Rogers, Professor of Natural Philosophy in the University of Virginia. 8vo. Phila- delphia 1836. On the Falls of Niagara and the reasonings of some Au- thors respecting them, by Henry D. Rogers, Professor of Geology in the University of Pennsylvania, F.G.S. 8vo. Report on the Geological Survey of the State of New Jersey, by Henry D. Rogers, 2nd edit. 8vo. Phila- delphia 1836. 27. Bulletin de la Société Géologique de France, tome 7, feuilles 11—16. 8vo. Paris 1836. 29. Journal of the Bahama Society for the Diffusion of Know- ledge, nos. 11—14, from April to July 1836. 8vo. Baha- ma 1835. Bohn’s Catalogue of Books for 1836. 8vo. London 1836. Oct. 10. Allen and Co.’s Select List of Publications for 1836. 12mo. London 1836. DONORS. The Author. The Author. The British Association. The Royal Society. The Conductor. The Authors. The Author. The Author. The Author. The Geological Society of France. The Bahama Society. Mr. J. Bohn. Messrs. Allen and Co. 1836. Och Tile 12. 17. 21. 22. Nov. 10. 14. 16. 18. 19 Last of Donations. BOOKS. Geology and Mineralogy considered with reference to Natural Theology, by the Rev. Wm. Buckland, D.D., Canon of Christ Church, and Reader in Geology and Mineralogy in the University of Oxford. (Being the 6th of the Bridgwater Treatises.) 2 vols. 8vo. London 1836. Mémoires présentés par divers Savans a |’Académie Royale des Sciences de l'Institut de France: Sciences Mathématiques et Physiques. Tome 6. 4to. Paris 1835. Mémoires de l’Académie Royale des Sciences de ]’Insti- tut de France, tome 13, 4to. Paris 1835. Geological Text Book, for aiding the Study of North American Geology ; being a Systematic Arrangement of Facts collected by the Author and his Pupils, under the Patronage of the Hon. Stephen Van Rensselaer ; by Amos Eaton, M.A., Senior Professor in Rensselaer Institute, &c. 2nd edit. 8vo. Albany, New York, and Troy, 1832. . Théorie des Volcans, par le Comte A. de Bybandt Pal- stercamp. 3 vols. 8vo, with Illustrative Maps, &c, Paris 1835. A Descriptive Catalogue of the Objects of Geology, Natural History, and Antiquity (chiefly discovered in Sussex) in the Museum attached to the Sussex Scien- tific and Literary Institution at Brighton; by Gideon Mantell, Esq., LL.D., F.R.S., G.S., &c. 8vo. London 1836. Italiens Tertiar-Gebilde und deren Organische Ein- schliisse. Vier Abhandlungen, von Dr. Heinrich G. Bronn, Professor in Heidelberg. 8vo. Heidelberg 1831. Memoirs of the Royal Astronomical Society, vol. 9. 4to. London 1836. Transactions of the Zoological Society of London, vol. 2, part 1. 4to. London 1836. An Account of some Fossil Crustacea which occur in the Coal Formation, by John Scouler, M.D., F.L.S. From Thomson’s Records of General Science, vol. 1. 8vo. Journal of the Royal Geographical Society of London, vol. 6, part 2. 8vo. London 1836. Journal of the Royal Asiatic Society of Great Britain and Ireland, no. 6, October 1836. 8vo. London 1836. VOL. V.—SECOND SERIES. Cc DONORS. The Author. The Academy of Sciences of Paris. The Author. The Author. The Author. The Author, The Royal Astronomical Society. The Zoological Society of London. The Author. The Royal Geographical Society. The Royal Asiatic Society. List of Donations. 1836. BOOKS. Nov. 22. A Geological Survey of Berwickshire, by David Milne, Esq., Advocate, Edinburgh. 8vo. Edinburgh 1835. 24. A Catalogue of the Fellows, Candidates, and Licen- tiates of the Royal College of Physicians, London. 8vo. 1836. 26. Report from the Select Committee to the House of Com- mons on the Cause of Accidents in Mines; together with the Minutes of Evidence and Index. folio. 1835. Report from the Select Committee to the House of Com- mons on the State of the Coal Trade; together with Minutes of Evidence and Appendix. folio. 1836. On the Geological Position and Association of the La- ~terite or Iron Clay Formation of India; with a De- scription of that Rock as it is found at the Red Hills, near Madras; by Robert Cole, Esq., of the Madras Medical Establishment, &c. 8vo. 1832. 29. Die Versteinerungen des Norddeutschen Oolithen Ge- birges, von Fredrich Adolph Roemer. 4to. Hanover 1836. Dec. 1. Arboretum et Fruticetum Britannicum, or Trees and Shrubs of Britain, Native and Foreign, Hardy and Half-Hardy, Pictorially and Botanically delineated, and Scientifically and Popularly described; by J. C. Loudon, Esq., F.G.S.; for the year 1836. 8vo. Lon- don 1836. The Magazine of Natural History, and Journal of Zoo- logy, Botany, Mineralogy, Geology, and Meteorology ; conducted by J. C. Loudon, Esq., F.G.S., &c.; for the year 1836. 8vo. London 1836. The London and Edinburgh Philosophical Magazine, and Journal of Science: Third Series; by Sir David Brewster, K.H., LL.D., F.R.S. L. and E.; Richard Taylor, F.S.A., L.S., G.S., Astr. Soc., &c.; and Ri- chard Phillips, F.R.S. L. and E., F.G.S., &c.; for the year 1836. 8vo. London 1836. The Horticultural Magazine, and General Register of all Useful and Interesting Discoveries connected with Natural History and Rural Subjects; conducted by Joseph Paxton ; for the year 1836. 8vo. London 1836. Comptes Rendus hebdomadaires des Séances de ]’Aca- démie des Sciences; par MM. les Secrétaires perpe- tuels; for the year 1836. 4to. Paris 1836. Repertory of Patent Inventions, and other Discoveries and Improvements in Arts, Manufactures, and Agri- culture, for the year 1836. 8vo. London 1836. DONORS. The Author. The Royal College of Phy- sicians. Robert Hutton, Esq., F.G.S. The Author. The Author. The Author. The Conductor. Richard Taylor, Esq., F.G.S. The Conductor. The Royal Academy of Sciences, Paris. The Proprietor. 1836. Dec. 3. 5. 14, Wie 10. Feb. He alt List of Donations. BOOKS. The Entomological Magazine for 1836. 8vo. London 1836. Sheets F, G, H, and I, of Dr. J. Lhotsky’s Journey to the Australian Alps. 8vo. Sydney 1836. Nouveaux Mémoires de la Société Impériale des Natu- ralistes de Moscou, tome 4. 4to. Moscou 1835. Bulletin de la Société Impériale des Naturalistes de Mos- cou, tome 9. 8vo. Moscou 1836. Report of the Expedition for exploring Central Africa from the Cape of Good Hope, June 23rd, 1834, under the superintendence of Dr. A. Smith. 8vo. London 1834, Proceedings of the Royal Society of London, no. 26. 1836. 8vo. Considerazioni Geologiche sullo Zolfo, del Socio Profes- sore C. Gemmellaro. Lette nella tornata ordinaria, del 19 Dicembre, 1833. 4to. Messina 1833. . Sixiéme Rapport Annuel sur les Travaux de la Société d’Histoire Naturelle de |’Ile Maurice, par M. Julien Desjardins. 8vo. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., &c. vol. 31, no. 1. October 1836. 8vo. New Haven 1836. . Mr. A. Nattali’s Catalogue of Books, in various Lan- guages and every Branch of Literature, for 1837. 8vo. London 1837. Transactions of the Institution of Civil Engineers, vol. 1. 4to. London 1836. An Address delivered at the Anniversary Meeting of the Royal Society, on Wednesday, Nov. 30th, 1836, by H. R. H. the Duke of Sussex, President. 4to. Bulletin de la Société Géologique de France, tome 7, feuilles 11-16, et Table des Matiéres et des Auteurs. 8vo. Paris 1836. Mémoires de la Société de Physique et d’Histoire Natu- relle de Geneve, vols. 1-4, and vol. 7, part 2. 4to. Geneva 1821-1828, 1836. Transactions of the Royal Society of Edinburgh, vol. 13, part 1. 4to. Edinburgh 1836. Some Enquiries in the Province of Kemaon, relative to the Geology and other Branches of Natural History, by John M‘Clelland, Assistant-Surgeon, and Member of the Medical and Physical Society of Calcutta. 8vo. Calcutta 1835. c 2 DONORS. Francis Walker, F.G.S. Esq., The Author. The Imperial Society of Naturalists of Moscow. The Society for Exploring Central Africa. The Royal Society. The Author. The Author. The Conductor. Mr. A. Nattali. The Institution of Civil Engineers. The Royal Society. The Geological Society of France. The Natural History So- ciety of Geneva. The Royal Edinburgh. Society of William Jerdan, Esq. List of Donations. 1837. BOOKS. Feb. 1, Supplement to the Account of the Rev. John Flamsteed, the First Astronomer Royal, by Francis Baily, Esq., F.R.S., &c. 4to. London 1837. 4. Transactions of the Society for the Encouragement of Arts, Manufactures, and Commerce, vol. 51, part 1. 8vo. London 1837. Description Physique des Iles Canaries, suivie d’une In- dication des principaux Volcans du Globe, par Léopold de Buch. Traduite de l’Allemand par C. Boulanger, Ingénieur des Mines. 8vo. With an Atlas, folio. Paris 1836. Des Cavernes, de leur Origine et de leur Mode de For- mation, par M. Théodore Virlet, Ingénieur des Mines. 12mo. Avesnes 1836. De l’Origine des différens Combustibles Minéraux et des Bois Fossiles qui se rencontrent ala Surface du Globe, par M. Théodore Virlet. 12mo. Notice sur les Marbres, par M. Théodore Virlet. 12mo. Proceedings of the Royal Society of London, no. 27, Nov. 1836, 8vo. Some Enquiries in the Province of Kemaon, relative to the Geology and other Branches of Natural History, by John McClelland, Assistant-Surgeon, and Member of the Medical and Physical Society of Calcutta. 8vo. Calcutta 1835. 18. Catalogue des Espéces et Variétés de Mollusques Ter- restres et Fluviatiles, observés jusqu’a ce jour 4 l’état vivant, dans la Haute et la Basse Auvergne, Départe- mens du Cantal, du Puy de Dome et celui de la Haute Loire ; suivi d’un autre Catalogue des Espéces Fos- siles recueilles récemment dans les diverses Formations Tertiaires des mémes Départemens ; par J. B. Bouillet. 24. Synopsis of the Family of the Naiades, by Isaac Lea, Member of the American Philosophical Society. 8vo. Philadelphia 1836. March 8. Philosophical Transactions of the Royal Society of Lon- don for 1836, part 2. 4to. London 1837. Transactions of the Cambridge Philosophical Society, vol. 6, part 1. 4to. Cambridge 1837. A Catalogue of Quadrupeds and Birds in the Museum of the Cambridge Philosophical Society. 8vo. Cambridge 1837. Madras Journal of Literature and Science; published under the auspices of the Madras Literary Society DONORS. The Author. The Society of Arts. M. C. Boulanger. The Author. The Royal Society. Messrs. Richardson & Co. The Author. The Author. The Royal Society. The Cambridge Philoso- phical Society. 1837. March 8. 22. 27 List of Donations. BOOKS. and Auxiliary Royal Asiatic Society; edited by the Secretary. No. 18, October 1836. 8vo. Madras. Bulletin de la Société Géologique de France, tome 7, feuilles 20-23. 8vo. Paris 1837. The Analysis of Inorganic Bodies, by J. J. Berzelius. Translated from the French edition by G. O. Rees. 8vo. London 1833. Memorie della Societa Italiana delle Scienze residente in Modena, tomo 21, parte Matematica. 4to. Modena 1836. Napoleon in Council, or the Opinions delivered by Na- poleon in the Council of State; from the French of Baron Pelet (de la Lozére), translated by Capt. Basil Hall, R.N. 8vo. Principles of Geology, by Charles Lyell, Esq., F.G.S., 5th edition, 4 vols. 12mo. London 1837. Ueber das Fossile Genus Nerinea, von Herrn Prof. Voltz. Uebersicht und Abbildungen der bis jetzt bekannten Nerinea-Arten, von H. G. Bronn. 8vo. An Ornithological Letter to William Swainson, Esq,, F.R.S., by Charles Waterton, Esq. 8vo. Rodd’s Catalogue of Books for 1837. 8vo. Descrizione Geognostica della Costa Meridionale del Valle di Messina, del Professore Carlo Gemmellaro. 4to. 1834. Considerazioni Geologiche sullo Zolfo, del Socio Profes- sore C. Gemmellaro. 4to. 1833. Bulletin de la Société Géologique de France, tome 8, feuilles 5-9. 8vo. 1837. Geognostische und physikalische Beobachtungen tiber die Vulkane des Hochlandes von Quito, von Alexander von Humboldt. 8vo. Berlin 1837. From the Annalen der Physik und Chemie, Band xxxx. no. 2. Die teutschen Salzwerke und das Salzregale, von J. E. Ritter von Koch-Sternfeld. 8vo. Munich 1836. Mémoires de la Société Géologique de France, tome deuxiéme, premiére partie. 4to. Paris 1836. . Observations addressed to those interested in either Rail- ways or Turnpike Roads, by Alexander Gordon, Esq. 8vo. London 1832. . Observations on the Geology of the United States of America; with some Remarks on the Effect produced on the Nature and Fertility of Soils by the Decompo- sition of the different classes of Rocks, and an Appli- DONORS. Madras Literary Society. The Geological Society of France. The Translator. Societa delle Scienze di Mo- dena. Capt. Basil Hall, R.N. The Author. Herr H. G. Bronn. The Author. Mr. T. Rodd. The Author. The Author. The Geological Society of France. The Author. The Author. The Geological Society of France. The Author. List of Donations. 1837. BOOKS. cation to the Fertility of every State in the Union in reference to the accompanying Geological Map. 8vo. Philadelphia 1817. April 15. Report of the Geological Reconnoissance of the State of Virginia, by William B. Rogers, Professor of Natural Philosophy in the University of Virginia. 8vo. Phila- delphia 1836. Report of the Geological Survey of the State of New Jersey, by Henry D. Rogers, F.G.S., Professor of Geology and Mineralogy in the University of Penn- sylvania, &c. 8vo. Philadelphia 1836. Contributions to the Geology of the Tertiary Formations of Virginia, by William B. Rogers, Professor of Natu- ral History in the University of Virginia, and Henry D. Rogers, F.G.S., Professor of Geology and Mine- ralogy in the University of Pennsylvania. 8vo. Penn- sylvania 1835. History of the Inductive Sciences from the earliest to the present Times, by the Rev. William Whewell, A.M., Fellow and Tutor of Trinity College, Cambridge, Pres. G.S. 3 volumes. 8vo. London 1837. Mémoires de la Société des Sciences Naturelles de Neu- chatel, tome 1. 4to. Neuchatel 1835. . Vues illustratives de Phénoménes Géologiques observés 19. sur le Vésuve et Etna pendant les années 1833 et 1834, par Dr. H. Abich. fol. Paris 1837. Proceedings of the Royal Society of London, no. 28. 8vo. Proceedings of the Royal Society of Edinburgh, no. 10, 1836-1837. 8vo. Transactions of the Royal Irish Academy, vol.17. 4to. Dublin 1837. Proceedings of the Royal Irish Academy, nos. 1 and 2, 1836-1837, and no. 3, 1837. 8vo. Plan, By-Laws, &c., of the New Haven Verd Antique Marble Company. 8vo. 1837. American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., vol. 31, no. 2, Ja- nuary 1837. 8vo. New Haven 1837. . Reports of the Scarborough Philosophical Society, for 1834, 1835, 1836. 8vo. Scarborough. Observations on Mineral Veins, by Robert Were Fox. 8vo. Falmouth 1837. 3. Description d’un Crane Colossal de Dinotherium gigan- teum, trouvé dans la Province Rhénane du Grand Duché de Hesse-Darmstadt ; précédée d’une Dissertation Gé- 28); BONORS. The Author. The Author. ‘The Author. The Authors. The Author. : Society of Natural Sciences of Neuchatel. The Author. The Royal Society. The Royal Society of Edin- burgh. The Royal Irish Academy. The New Haven Verd An- tique Mining Company. The Conductor. The Scarborough Philoso- phical Society. The Author. May 1837. 6. 9. 2Ke 31. List of Donations. BOOKS. ologique sur les Formations fossiliféres du Bassin Ter- tiaire du Rhin Moyen, avec Atlas; par M. A. de Klip- stein, Prof. de Minéralogie 4 l'Université de Giessen, et M. J. J. Kaup, Directeur du Musée d’Histoire Na- turelle de Darmstadt. On the Temperatures and Geological Relations of cer- tain Hot Springs, particularly those of the Pyrenees, and on the Verification of Thermometers, by J. D. Forbes, Esq., F.R.S.S. L. & E., F.G.S., &c., Professor of Natural History in the University of Edinburgh. 8vo. Fourth Annual Report of the Royal Cornwall Polytechnic Society. 8vo. Falmouth 1836. Bulletin de la Société Géologique de France, tome 8, feuilles 10-12. 8vo. Paris 1837. De Goniatitis in Montibus Rhenanis Occurrentibus, by Dr. Beyrich. 4to. Berlin 1837. Beitrage zur Kenntniss der Versteinerungen des Rhein- ischen Ubergangsgebirges, Erster Heft, von Ernest Beyrich. 4to. Berlin 1837. Asiatic Researches, or Transactions of the Society esta- blished in Bengal for enquiring into the History, the Antiquities, the Arts and Sciences, and Literature of Asia, vol. 19, part 1. 4to. London 1837. Catalogus Conchyliorum Regni Neapolitani que usque ad huc reperit A. Scacchi. 8vo. Neapoli 1836. Allen and Co.’s Catalogue of Books in Oriental Literature for 1837. 12mo. London 1837. A Guide to Geology, by John Phillips, F.R.S., G.S., Prof. of Geology in King’s College, London, &c. 3rd. edit. 12mo. London 1837. Sixth Annual Report of the Council of the United Service Museum. 8vo. London 1837. A Narrative of Missionary Enterprises in the South Sea Islands, with Remarks upon the Natural History of the Islands, Origin, Languages, Traditions, and Usages of the Inhabitants, by John Williams, of the London Missionary Society. 8vo. London 1837. A Narrative of the Operations for the Recovery of the Public Stores and Treasure sunk in H.M.S. Thetis, at Cape Frio, on the Coast of Brazil, on the 5th Decem- ber, 1830. To which is prefixed, a concise Account of the Loss of that Ship. By Captain Thomas Dicken- son, R.N., at that time commanding H.M. sloop, DONORS. Professeur A. de Klipstein. The Author. The Royal Cornwall Poly- technic Society. The Geological Society of France. The Author. eeeereeeeee The Asiatic Society of Ben- gal. The Author. Messrs. Allen and Co. The Auther. The Council of the United Service Museum. The Author. List of Donations. 1837. BOOKS. Lightning, employed in effecting the above Salvage. 8vo. London 1836. June 1. The Gardener’s Magazine, and Register of Rural and Domestic Improvement, no. 87, June 1837, conducted by J. C. Loudon, Esq. 8vo. London 1837. 2. Annual Report of the Council of the Yorkshire Philoso- phical Society for 1836. 8vo. York 1836. Fourth Annual Report of the Royal Cornwall Polytechnic Society. 8vo. Falmouth 1837. Jahrbuch fiir 1837. Herausgegeben von H. C. Schu- macher, mit Beitragen von Bessel, Hassen, A von Humboldt, Moser, Oblers, und Pomelier. 8vo. Journal of the Royal Geographical Society of London, vol. 7, part 1. 8vo. London 1837. Annual Report of the Committee of the Birmingham Phi- losophical Institution, 1836. 8vo. Birmingham 1836. Report on the Present State of our Knowledge with re- spect to Mineral and Thermal Waters, by Professor Daubeny, M.D, 8vo. 1836. Transactions of the Philosophical and Literary Society of Leeds, vol. 1, part 1. 8vo. London 1837. Conchyliologie Fossile du Bassin de l’Adour, ou De- scription des Coquilles Fossiles qui ont été trouvées dans les Terrains Marins Tertiaires aux environs de Dax, (Dep. des Landes), par M. le Docteur Grate- loup. 8vo. Bordeaux 1837. Mémoire de Géo-Zoologie sur les Oursins Fossiles (Echi- nides) qui se rencontrent dans les Terrains Calcaires des Environs de Dax, par M. le Docteur Grateloup. 8vo. Bordeaux 1836. 20. American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., vol. 32, no. 1, April 1837. 8vo. New Haven 1837. 22. Die Gebirgsmasse von Davos. Ein Vortrag gehalten in der Geologischen Section der Versammlung der Allge- meinen Schweizerischen Naturforschenden Gesell- schaft in Solothurn den 26 July 1836, von Professor B. Studer. 4to. 23. Supplement to the Flora Metropolitana, or Botanical Rambles within Thirty Miles of London, by Daniel Cooper, A.L.S. 12mo. London 1837. 30. Notice sur le Grés Bigarré de la Grande Carriére de Soultz-les-Bains, par M. Voltz. 4to. July 1. Coup d’ceil Général et Statistique sur la Métallurgie DONORS. The Author. The Conductor. The Yorkshire Philoso- phical Society. The Royal Cornwall Poly- technic Society. Alex. de Humboldt, For. Mem. G.S. The Royal Geographical Society. The Birmingham Philoso- phical Institution. The Author. The Philosophical and Li- ° terary Society of Leeds. The Author. The Author. The Conductor. The Author. The Author. The Author. 1837. July 1, . The Farthings of Queen Anne. List of Donations. BOOKS. considerée dans ses rapports avec l’Industrie, la Civili- sation et la Richesse des Peuples, principalement en. Europe, &c., par Théodore Virlet, Ingénieur Civil des Mines, &c. 8vo. Paris 1837. Mémoire sur divers Couches de Terrain nouvellement découvertes aux Environs de Paris, entre la Craie et lArgile Plastique, par Charles D’Orbigny. Bulletin de la Société Géologique de France, tome 8, feuilles 13-15, 1836 4 1837. 8vo. Paris 1837. . Proceedings of the Zoological Society of London, from October to December 1836. 8vo. Transactions of the American Philosophical Society held at Philadelphia, for promoting Useful Knowledge, vol. 5, new series, part 3. 4to. Philadelphia 1836. The whole of the Va- rieties of the Farthings which are extant, and which are in the British Museum, described; also a List of her Pattern Halfpence, by William Till, M.N.S. 12mo. London 1837. . Proceedings of the Royal Society of London, 1837, no. 29. 8vo. Journal of the Royal Asiatic Society of Great Britain and Ireland, no. 7, May 1837. 8vo. London 1837. Royal Asiatic Society.—Proceedings of the Committee of Agriculture and Commerce, &c., for April and May 1837. 8vo. Proceedings of the Royal Irish Academy for the year 1836-1837, part 1. 8vo. Library Catalogue, and Regulations of the Telford Pre- miums of the Institution of Civil Engineers. Minutes of the Proceedings for the Session 1837. 8vo. London 1837. Aufenthalt und Reisen in Mexico in den Jahren 1825 bis 1824, Bemerkungen iiber Land, Produkte, Leben und Sitten der Einwohner, und Beobachtungen aus dem Gebiete der Mineralogie, Geognosie, Bergbaukunde, Meteorologie, Geographie, &c., von Joseph Burkhardt, F.G.S., &c. Mit einem Vorworte von Dr. J. Noggerath. Erster und Zweiter Band, mit Tafel 1 bis 11. Stuttgart 1836. Sur les Singes Fossiles, Rapport fait 4 l’Académie des 8vo. Sciences, par M. de Blainville. 4to. The Suburban Gardener and Villa Companion, &c., by J. C. Loudon, F.L.S., H.S., &c., no. 2, July 1837. 8vo. London 1837. VOL. V.—SECOND SERIES. D DONORS. The Author. The Author. The Geological Society of | France. The Zoological Society. The American Philoso- phical Society. The Author. The Royal Society. The Royal Asiatic Society. The Royal Irish Academy. The Institution of Civil Engineers. The Author. ’ The Author. The Conductor. 23. 31. Sept. 1. or 30. 30. List of Donations. BOOKS. . Om de Bornholmske Kulformationer, af G. Forchhammer, Professor. 4to. . Memoirs of the Royal Academy of Sciences of Lisbon, vol. 12, part 1. 4to. Lisbon 1836. . Proceedings of the Royal Asiatic Society of Great Britain and Ireland, May 1837. 8vo. Ancient and Modern Alphabets of the popular Hindu Languages of the Southern Peninsula of India, by Cap- tain Henry Harkness, M.R.A.S. Bulletin de la Société Géologique de France, tome 8, feuilles 16-20, 1836-37. Madras Journal of Literature and Science, published un- der the auspices of the Madras Literary Society and Auxiliary Royal Asiatic Society ; edited by the Secre- tary to the Asiatic Department ; no. 12, July 1836, and no. 14, January 1837. 8vo. Madras. Transactions of the Linnean Society of London, vol. 17, part 4. 4to. London 1837. . Royal Asiatic Society. —Proceedings of the Committee of Agriculture and Commerce, Aug. 1837. 8vo. . Betrachtung des Feldspathsystems in der viergliedrigen Stellung, von C. S. Weiss. 4to. 1835. Uber eine versteckte gegenseitige Beziehung zwischen den Krystallsystemen des Feldspathes und des Kalk- spathes, von C. 8. Weiss. 4to. 1833. . Address of Earl Stanhope, President of the Medico-Bota- nical Society, for the Anniversary Meeting, January 16th, 1837. 8vo. London 1837. . American Journal of Science and Arts, conducted by Ben- jamin Silliman, M.D., LL.D., vol. 32, no. 2, July 1837. 8vo. New Haven 1837. Philosophical Transactions of the Royal Society of Lon- don, for the year 1837, part 1. 4to. London 1837. Proceedings of the Royal Society of London, no. 29, April to June 1837. 8vo. Nuove Ricerche sul noto Fenomeno delle Colonne per- forate dalle Foladi nel Templo di Serapide in Puzzuoli, del Signore Ernesto Capocci. 4to. The Sixth Report of the British Association for the Ad- vancement of Science, held at Bristol in August 1836. 8vo. London 1837. Observations sur ]’Influence des Cométes sur les Phéno- ménes de l’Atmosphére, addressées 4 M. Arago, par T. Forster. 8vo. Aix-la-Chapelle 1836. Osservazioni Geognostiche e Mineralogiche intorno ad DONORS. ' The Author. The Royal Academy of Lisbon. The Royal Asiatic Society. The Author. The Geological Society of France. The Auxiliary Royal Asia- tic Society. The Linnean Society. The Asiatic Society. The Author. The Medico-Botanical So- ciety. The Conductor. The Royal Society. The Author. The British Association. The Author. 1837. List of Donations. BOOKS. alcune Valli delle Alpi del Piemonte, del Professore di Mineralogia, Angelo Sismonda. Oct. 10. Elements of Chemistry, by the late Edward Turner, M.D., Sixth Edition, enlarged and revised, by Profes- sor Liebig, and Wilton G. Turner, part 1. 8vo. Lon- don 1837. Catalogue of the Library of the United Service Museum, 8vo. London 1837. Description d’une Collection de Minéraux formée par M. Henri Heuland et appartenant 4 M. Ch. Hampden Turner de Rooksnest, par A. Levy, trois volumes 8vo. avec un Atlas de 83 planches. fol. London 1837. Remarks on Mathematical or Demonstrative Reasoning ; its connexion with Logic, and its application to Science, Physical and Metaphysical, with reference to some re- cent publications; by Edward Tagart, F.G.S. 8vo. London 1837. . Address of the Council of the Worcestershire Natural History Society, delivered at their Fourth Anniversary Meeting, on Wednesday, May 24th, 1837, by Hugh E. Strickland, Esq., F.G.S. 8vo. 1837. . La Mosaique Franeaise, Recueil Hebdomadaire de Lit- térature, Sciences, Beaux Arts, &c., publié par Henri Bonnias, no. 1, Novembre 1837. fol. London 1837. . A Medico-Topographical, Geological, and Statistical Sketch of Bolton and its Neighbourhood, by James Black, M.D., of the Royal College of Physicians, London. . On a New Genus of Land Shells, by John Edward Gray, Esq., F.R.S., &c. A Synoptical Catalogue of the Species of certain Tribes or Genera of Shells contained in the Collection of the British Museum, and the Author’s Cabinet, with De- scriptions of the New Species, by John Edward Gray, FE.R.S., &c. A Catalogue of the Fellows, Candidates, and Licentiates of the Royal College of Physicians of London. 4to. London 1837. - A Journey from Sydney to the Australian Alps, under- taken in the months of January, February, and March 1834, by Dr. John Lhotsky (Sheets B, C, D, & E.) 8vo. Sydney. No. 1 of a Periodical, entitled “ Information for the Peo- ple,” by Dr. John Lhotsky. 8vo. Sydney 1837. 16, Letheea Geognostica, oder Abbildung und Beschreibungen p 2 ww DONORS. The Author. The Editors. The Council of the United Service Museum. H. Heuland, Esq., F.G.S. The Author. The Author. The Editor. The Author. The Author. The Author. The Royal College of Phy- sicians. The Author. 1837. List of Donations. BOOKS. der fiir die Gebirgs-Formationen bezeichnendsten Versteinerungen, von Dr. H. G. Bronn. 8vo. Stutt- gart 1835. Nov. 25. Recherches sur les Ossemens Fossiles de la Russie, par 13. G. Fischer de Waldheim. 4to. part]. Moscow 1836. Index and Table of Contents of vol. 3 of Abstracts of the Papers printed in the Philosophical Transactions of the Royal Society of London, from 1830 to 1837 inclusive. 8vo. London 1837. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., vol. 33, no. 1. 8vo. New Haven 1837. . Transactions of the Cambridge Philosophical Society, vol. 6, part 2. 4to. Cambridge 1837. . A Catalogue of Fossils from the Mountain Limestone of Great Britain, by William Gilbertson, Esq. Essays on Unexplained Phenomena, by Graham Hutchi- son, Esq. 8vo. Glasgow 1838. Traité Elémentaire de Géologie, par M. Rozet, seconde partie—Géogénie. 8vo. Paris 1837. De I’Etat Stationaire de la Philosophie Naturelle, ou Indi- cations des Recherches a faire dans l’Astronomie et la Physique, par J. W. Schmitz. 8vo. Paris et Brux- elles 1837. Beschaffenheit der Erde. Hypothese, von F. Julius Brede. 8vo. Altona 1837, Selections from the Natural History of the Quadrupeds of Paraguay and the River la Plata, comprising the most remarkable Species of South, America. Translated from the Spanish of Don Felix de Azara, with Notes, by William Perceval Hunter, Esq., F.G.S. Journal of the Royal Geographical Society of London, vol. 7, 1837, part 2. 8vo. London 1837. Philosophical Transactions of the Royal Society of Lon- don, for the year 1837, part 2. Ato. The Mining Review, and Journal of Geology, Mineralogy, and Metallurgy, conducted by Henry English, Esq., F.G.S., &c. no. 10. 8vo. London 1837. Address of His Royal Highness the Duke of Sussex, K.G., &c. &c. &c., the President, read at the Anniversary Meeting of the Royal Society, on Thursday, Nov. 30th, 1837. 8vo. Table showing the mean temperature, as also the mean height of the Barometer in each month in the 34 years ending 30th June 1837, with the extremes of each and DONORS. The Author. The Author. The Royal Society. The Conductor. The Cambridge Philosophi- cal Society. Mr. George Sowerby. The Author. The Author. The Author. The Author. The Translator. The Royal Geographical Society. The Royal Society. The Conductor. The Royal Society. 1837. Last of Denations. BOOKS. the days on which such extremes occurred, by Joseph Templeman, of the Colonial Secretary’s Office, New- foundland. Dec. 18. Arboretum et Fruticetum Britannicum, or Trees and Shrubs of Britain, Native and Foreign, Hardy and Half Hardy, pictorially and botanically delineated, and sci- entifically and popularly described, by J. C. Loudon, for the year 1837. 8vo. London 1837. Loudon’s Magazine of Natural History, conducted by Edward Charlesworth, Esq., F.G.S.,—New Series for the year 1837. 8vo. London 1837. The London and Edinburgh Philosophical Magazine and Journal of Science, Third Series, by Sir David Brew- ster, K.H., LL.D., F.R.S., L. and E., &c.; Richard Taylor, Esq., F.S.A., L.S., G.S., Astr. Soc., &c.; and Richard Phillips, F.R.S., L. & E., F.G.S.; for the year 1337. 8vo. London 1837. The Repertory of Patent Inventions, and other Discoveries and Improvements in Arts, Manufactures, and Agri- culture, for the year 1837. 8vo. London 1837. The Entomological Magazine for 1837. 8vo. London 1837. The Suburban Gardener and Villa Companion, by J. C. Loudon, F.L.S. H.S., &c., nos. 1 to 7, June to Dec. 1837. 8vo. London 1837. Comptes Rendus Hebdomadaires des Séances de |’Acadé- mie des Sciences, par MM. les Secrétaires perpetuels, for the year 1837. 4to. 1837. . An Inaugural Address delivered in the Theatre of the Islington Literary and Scientific Society, on the open- ing of the New Building, Nov. 16th, 1837, by J. J. J. Sudlow, Esq. Journal of the Royal Asiatic Society of Great Britain and Ireland, no. 8, Dec. 1837. 8vo. Remarks on the Geology and Mineralogy of Nova Scotia, by Abraham Gesner, Esq. 8vo. Halifax, Nova Scotia 1836. Catalogue of the Minerals in the United Service Museum. 8vo. London 1837. N. A. Nattali’s Catalogue of Books for 1838. 8vo. Lon- don 1838. Essay on the Antiquity of Hindoo Medicine, by J. Forbes Royle, M.D., Professor of Materia Medica in Kings College, London. DONORS. The Author. The Author. The Conductor. R. Taylor, Esq., F.G.S. The Proprietor. Francis Walker, Esq. The Author. The Academy of Sciences of Paris. The Islington Literary and Scientific Society. The Royal Asiatic Society. The Author. The Council of the United Service Museum. Mr. Nattali. The Author. List of Donations. 1838. BOOKS. DONORS. Jan. 4, A System of Geology, with a Theory of the Earth, and an Explanation of its Connexion with the Sacred Re- cords, by John Macculloch, M.D., F.R.S., &c., 2 vo- lumes 8vo. London 1831. John Willimot, Esq., F.G.S. Geognostische Profile, von C.J. E. Freiherrn von Schwe- rin. 8vo. Miinchen 1829. alc biate wie es Report on the Probability of the Occurrence of Coal and other Minerals in the Vicinity of Lancaster, addressed to the Lancaster Mining Company, by John Phillips, , F.R.S., G.S., &c. The Author. Proceedings of the Royal Society of London, no. 30, Nov. 1837. 8vo. The Royal Society. Defence of the Resolution for omitting Mr. Panizzi’s Bi- bliographical Notes from the Catalogue of the Royal ‘ Society. 8vo. Address to Her Majesty referred to in the Address of His Royal Highness the Duke of Sussex, President of the Royal Society. 8vo. The London Medical Gazette, no. 14, containing a Letter by the Rev. W. Whewell on his History of Discoveries Rev. Prof. Whewell, Pres. in the Nervous System. 8vo. G.S. Account of Mr. Whewell’s Researches onthe Tides. 8vo. . 17. Elements of Chemistry, including the recent Discoveries and Doctrine of that Science, by the late Edward Tur- ner, M.D., Sixth Edition, enlarged and revised, by Justus Liebig, Professor of Chemistry in the University of Giessen, and Wilton G. Turner, part 2. 8vo. Lon- don 1838. The Editors. The Malacological and Conchological Magazine, part 1, conducted by G. B. Sowerby, F.L.S., &c. The Conductor. Rules and Regulations for the government of the Athe- nzum, with an Alphabetical List of the Members for 1838. The Athenzeum Club. Feb. 1. Catalogue des Espéces et Variétés de Mollusques Terres- tres et Fluviatiles observés jusqu’a ce jour a |’état vivant dans la Haute et la Basse Auvergne ; suivi d’un autre Catalogue des Espéces Fossiles recueillies récemment dans les diverses Formations Tertiaires des mémes Dé- partemens, par J. B. Bouillet. 8vo. Clermont Ferrand 1836. The Author. Practical Observations on the Asphaltic Mastic, or Cement of Seyssell, now extensively employed on the Continent for Pavements, Roofing, and Flooring, for Hydraulic Works, &c., by F. W. Simms, Civil Engineer and Sur- 1838. Feb. 1. March 3. List of Donations. BOOKS. veyor, late of the Royal Observatory, &c. 8vo. Lon- don 1837. A Systematic and Stratigraphical Catalogue of Fossil Fish in the Cabinets of Lord Cole and Sir Philip Egerton, Bart., together with an Alphabetical and Stratigraphical Catalogue of the same Species, with Reference to their published Figures and Descriptions, by Sir Philip Grey Egerton, Bart., M.P., F.R.S., F.G.S. 4to. London 1837. Plates of Dr. Buckland’s Bridgwater Treatise, 1836, 4to. edition. Some Account of Two Visits to the Mountains in Essex County, New York, inthe years 1836 and 1837, with a Sketch of the Northern Sources of the Hudson, by W. C. Redfield. From the American Journal of Science, vol. 2, no. 33. A Report of the Geological Survey of Connecticut, by Charles Upham Shephard, M.D. 8vo. New Haven 1837. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., &c., vol. 33, no. 2, January. 8vo. New Haven 1838. . Proceedings of the Zoological Society of London, nos. 49 to 57. 8vo. Annales des Mines, ou Recueil de Mémoires sur l’Exploi- tation des Mines, et sur les Sciences et les Arts qui s’y rapportent, tome 12, cinquiéme livraison de 1837. 8vo. Paris 1837. Considérations sur la Nature des Végétaux qui ont cou- vert la Surface de la Terre aux diverses Epoques de sa Formation, par M. Adolphe Brongniart. 4to. Paris 1838. Rapport fait a l’Académie des Sciences, par M. de Blain- ville, sur un Nouvel Envoi de Fossiles, provenant du Dépot de Sansan, Département de Gers. Flora Metropolitana, or Botanical Rambles within Thirty Miles of London, being the Results of Excursions in 1833-34-35, more particularly in the Counties of Sur- rey and Kent, chiefly from actual Observation and the latest Authorities.—With a Supplement containing an Index of both Latin and English Names, Time of Flow- ering, Colour of Flower, &c., by Daniel Cooper, A.L.S., Curator to the Botanical Society of London, &c. 12mo. London 1837. Supplement to the Flora Metropolitana, 12mo. DONORS. The Author. The Author. Dr. Buckland. The Author. The Author. The Conductor. The Zoological Society. The Council of Mines. The Author. The Author. The Author. 1838. List of Donations. t BOOKS. March 3. A List of the Land and Freshwater Shells found in the Environs of London; extracted from the Flora Metro- politana, by Daniel Cooper. 12mo. London 1838. 6. Annals of Natural History, or Magazine of Zoology, Bo- 8. 10. 12. 15. Wie 24. tany, and Geology, being a Continuation of the “ Ma- gazine of Zoology and Botany, and Sir W. J. Hooker’s Botanical Companion ;” conducted by Sir W. Jardine, Bart., P. J.Selby, Esq., Dr. Johnston, Sir W. J. Hooker, Regius Professor of Botany, and Richard Taylor,F.L.S. ; no. 1, new series, March 1838. 8vo. London 1838. Proceedings of the Royal Society of London, no. 31, 1837-38. 8vo. Report on the Physical Condition of the Assam Tea Plant, with reference to Geological Structure, Soils, and Cli- mate, by John McClelland, Esq., Assistant Surgeon, Bengal Establishment, and Member of the Asiatic and Medical Societies of Calcutta. Presented to the Agri- cultural Societies of Calcutta, 8th February, 1837, by desire of Lord Auckland, Governor-General of India. From the Transactions of the Agricultural and Horti- cultural Society of India, vol. 4. 8vo. 1837. Transactions of the Royal Academy of Berlin, for the year 1835. 4to. Berlin 1836. Proceedings of the Royal Academy of Berlin from 8th May 1836 to 29th June 1837. 8vo. The Hunterian Oration, delivered in the Theatre of the Royal College of Surgeons, the 14th Feb. 1838, by Ben- jamin Travers, F.R.S., &c. &c. 4to. London 1838. Septicme Rapport Annuel sur les Travaux de la Société d’Histoire Naturelle de I’Ile Maurice, lu a la Séance Anniversaire du Mercredi, 24 Aofit 1836, par M. Ju- lien Desjardins, Secrétaire et l’un des Membres Fonda- teurs de la Société, &c. 8vo. Liste des Membres qui composent la Société d’Histoire Naturelle de Ile Maurice, ler Septembre 1836. 8vo. Madras Journal of Literature and Science, published un- der the auspices of the Madras Literary Society and Auxiliary Royal Asiatic Society ; edited by the Secre- tary to the Asiatic Department; nos. 15, 16, 17, for April, July, and October 1837. 8vo. Madras 1837. Catalogo delle Collezioni Orittologica ed Oreognostica, del fu Professore Cav. Matteo Tondi, Direttore del Mu- seo di Mineralogia di Napoli, Professore di Orittologia ed Oreognosia nella Regia Universita degli Studj, &c. &c. 8vo, Napoli 1837. DONORS- The Author. Richard Taylor, Esq. The Royal Society. The Author. The Royal Academy of Ber- The Author. The Author. M. Julien Desjardins. The Madras Literary So- ciety. J. B. Heath, Esq. List of Donations. 1838. BOOKS. Mar. 28. Proceedings of the Numismatic Society, 1836-1837. 8vo. Experimental Researches in Electricity, eleventh series, by Michael Faraday, D.C.L., F.R.S., &c. 4to. The Wonders of Geology, by Gideon Mantell, LL.D., F.R.S., in two volumes, 12mo. London 1838. 6. Address to the Members of the Berwickshire Naturalists’ Club after the Sixth Anniversary Meeting, held at Nor- ham, Sept. 20th, 1837, by the Rev. John Bird of Ye- tholm, President. 8vo. The Journal of the Royal Geographical Society of Lon- don, vol. &, part 1. 8vo. London 1838. Journal of the Geological Society of Dublin, vol. 1, parts 2 and 3. 8vo. Dublin. Notice sur la Famille des Bulléens dont on trouve les dépouilles Fossiles dans les Terrains Marins supérieurs du Bassin de l’Adour, aux Environs de Dax (Landes), précédée de Considérations Générales sur cette Famille et du Tableau des Genres et des Espéces connus, soit a Vétat Vivant, soit a état Fossile, par M. le Docteur Apr. Grateloup. 8vo. Bourdeaux 1837. Discours sur les Sciences et sur les Arts, et sur l’influ- ence qu’ils exercent sur les progrés de la civilisation, prononcé ala Séance Publique de Académie Royale des Sciences de Bourdeaux, par M. le Docteur Grate- loup. 8vo. Bourdeaux 1837. Isocrinus und Chelocrinus, zwei neue Typen aus der Ab- theilung der Crinoideen, von Hermann von Meyer. 4to. 10. Beitrage zu Eryon, einem Geschlechte fossiler lang- schwanziger Krebse, von Hermann von Meyer. 4to. Abweichungen von der Fiinfzah] bei Echinideen nachge- wiesen durch einen vierzahligen Cidariten und durch einen sechszahligen Galeriten, von Hermann von Meyer. 4to. Recherches sur les Ossemens Fossiles du Grés Bigarré de Soultz-les-Bains, Bas Rhin, par M. Hermann von Meyer. 4to. 16. Specimen Zoophytologize Diluviane, Auctore Joanne Michellotti. 8vo. Aug. Taurinorum 1838. 20. Proceedings of the Royal Irish Academy, nos. 7—10. 8vo. Memoir of the late President of the Royal Irish Academy, by the Rev. J. H. Singer, D.D., Secretary of the Aca- demy. 8vo. 1838. 1. Bulletin de la Société Géologique de France, tome 9, feuilles 6-9. 8vo. Paris 1838. VOL. ¥Y.—SECOND SERIES. E May Donors. The Numismatic Society. The Author. The Author. The Berwickshire Natural- ists’ Society. The Royal Geographical Society. The Geological Society of Dublin. The Author. eoovoeseee oes The Author. The Royal Irish Academy. eeooeoeereoe reese eee ee Ho ee The Geological Society of France. 1838. May June ile 6. List of Donations. BOOKS. Proceedings of the Royal Society of London, nos. 30, 31, and 32. 8vo. Transactions of the Historical and Literary Committee of the American Philosophical Society, held at Philadel- phia, for promoting Useful Knowledge, vol. 2. 4to. Philadelphia 1838. The Zoology of the Voyage of H. M.S. Beagle, un- der the command of Captain Fitzroy, during the years 1832-36. Published with the Approval of the Lords Commissioners of Her Majesty’s Treasury. Edited and superintended by Charles Darwin, Esq., M.A., F.G.S., &c. No. 1, part 2.—Mammalia, by George R. Waterhouse, Esq. 4to. London 1838. Das Siebengebirge und seine Umgebungen, nach den in- teressanteren Beziehungen dargestellt, von J.G. Zehler. 12mo. Crefeld 1837. Proceedings of the Royal Irish Academy, no. 11, and a List of the Members. 8vo. Mémoires de la Société de Physique et d’Histoire Na- turelle de Genéve, tome 8, premiére partie. 4to. Ge- néve 1838. Bulletin de la Société Géologique de France, tome 9, feuilles 10-14. 8vo. Paris 1838. Proceedings of the Numismatic Society, 1836-37. 8vo. Second Report of the Geology of the State of Maine, by Charles T. Jackson, M.D. 8vo. Augusta, 1838. Fifteenth Report of the Whitby Literary and Philosophical Society, presented at the Annual Meeting, Oct. 31, 1837, with a List of the Officers and Members, and of Donations presented to the Museum, 8vo. Whitby 1837. Eighth Report of the Scarborough Philosophical Society, to Aug. 31, 1837. Scarborough 1837. Transactions of the Society of Arts, Manufactures, and Commerce, vol. 51, part 2. 8vo. London 1838. Programma da Real Academia das Sciencias de Lisboa, annunciado na Sessao Publica de 15 de Maio de 1838, para o Anno de 1839, Ascent to the Summit of Mont Blanc on the 22nd and 23rd of August, 1837, by Henry Martin Atkins, Esq. . American Journal of Science and Arts, conducted by Ben- jamin Silliman, M.D., vol. 34, no. 1, April 1838. Annual Report of the Council of the Yorkshire Philoso- phical Society for 1837. 8vo. York 1838. Fifth Annual Report of the Royal Cornwall Polytechnic Society, 1837. 8vo. Penzance 1838. DONORS. The Royal Society. The American Philosophi- cal Society. C. Darwin, Esq., Sec. G.S. ‘ M. F. W. Heeninghaus. The Royal Irish Academy. The Natural History Soci- ety of Geneva. The Geological Society of France. The Numismatic Society. The Author. The Whitby Literary So- _ ciety. The Scarborough Philoso- phical Society. The Society of Arts. The Lisbon Academy. The Editor, through John Kenyon, Esq., F.G.S. The Conductor. The Yorkshire Philosophi- cal Society. The Royal Cornwall Poly- technic Society. 1838 8. List of Donations. BOOKS. June 14, Transactions of the Royal Irish Academy, vol. 18, part 1. July 16. 18. 19. 4to. Dublin 1838. Researches in Assyria, Babylonia, and Chaldza, forming part of the Labours of the Euphrates Expedition, by William Ainsworth, Esq., F.G.S., &c. 8vo. London 1838. Journal of the Royal Geographical Society of London, vol. 8, part 2. 8vo. London 1838. Address to the Royal Geographical Society of London, delivered at the Anniversary, 21st May, 1838, by Wil- liam R. Hamilton, Esq., F.R.S., President. 8vo. Lon- don 1838. Notizie intorno a due Fossili trovati nei Colli di San Stefano Roero, del Professore Angelo Sismonda. 4to. Torino 1838. Osservazioni Geologiche e Mineralogiche sopra i Monti posti tra la Valle di Aosta e quella di Susa in Piemonte, del Professore di Mineralogia, Angelo Sismonda. 4to. Torino 1838. . Experimental Researches in Electricity, twelfth and thirteenth series, by Michael Faraday, Esq., D.C.L., F.R.S., F.G.S., &c. From the Philosophical Trans- actions, 1838, part 1. 4to. London 1838. . The Zoology of the Voyage of His Majesty’s Ship Beagle, under the command of Captain Fitzroy, R.N., during the years 1832 to1836. no. 1 of part 3, Birds, by John Gould, Esq., F.L.S., &c. 4to. London 1838. Memorie di Matematicae di Fisica della Societa Italiana delle Scienze residente in Modena, tomo 21, parte con- tenente le Memorie di Fisica. 4to. Modena 1834. State of New York, no. 161, in Assembly, February 11, 1837. Communication from the Governor relative to the Geological Survey of the State. 8vo. Albany 1837. Philosophical Transactions of the Royal Society of Lon- don for 1838, part 1. 4to. . A Letter intended (one day) as a Supplement to Lockhart’s Life of Sir Walter Scott, by Charles Bucke; printed for private circulation. 8vo. London 1838. Society for the Encouragement of Arts, Manufactures, and Commerce. Premiums for the Sessions 1838-1839 and 1839-1840. Proceedings of the Royal Irish Academy for the year 1837-1838, part 2, nos. 12 and 13. 8vo. Six copies. 8vo. London 1838. 26. Outline of the Geology of Ireland, by Richard Griffith, Esq., F.G.S. L. & D.; extracted from the Second Re- » 29 E «@ DONORS. The Royal Irish Academy. The Author. The Royal Geographical Society of London. The Author. The Author. The Author. C. Darwin, Esq., Sec. G.S. The Italian Scientific So- ciety resident at Modena. J. C. Warner, Esq. The Royal Society of Lon- don. The Author. The Society for the Encou- ragement of Arts, &c. The Royal Irish Academy. 1838. July 28. 13. 14, Aug. 16. Last of Donations. BOOKS. port of the Commissioners appointed to inquire into the manner in which Railway Communications can be most advantageously promoted in Ireland. fol. London 1838. Description Nautique des Cotes de l’Algérie, par M. A. Bérard, Capt. de Corvette ; suivie de Notes par M. de Tessan. 8vo. Paris 1837. List of Members of the British Association for the Ad- vancement of Science, to which are added, a List of the Officers, Rules of the Association, and Contents of the Reports already published. 2 copies. 8vo. London 1838. On the Primary Forces of Electricity, by Richard La- ming, Esq., M.R.C.S. (From the London and Edin- burgh Philosophical Magazine and Journal of Science, June 1838.) 8vo. London 1838. Essai sur les Soulévemens Jurassiques, second cahier, contenant la Carte Orographique et Géologique des Soulévemens du Jura Bernois, accompagnée d’une De- scription Systématique, par J. Thurmann. 4to. Por- rentruy 1836. Geognostiche Wanderungen, von Bernhard Cotta. 2 Theile. 8vo., Dresden und Leipzig 1838. . Elements of Geology, by Charles Lyell, Esq., F.R.S., Vice-President of the Geological Society of London, 12mo. London 1838. Madras Journal of Literature and Science, no. 18, Janu- ary to March 1838. 8vo. Madras 1838. . Reports of a Committee for investigating the Coal and Mineral Resources of India. 8vo. Calcutta 1838. Studien des Gottingischen Vereins Bergmannischer Freun- de; im Namen desselben herausgegeben von Joh. Friedr. Ludw. Hausmann. Vierten Bandes erstes Heft und zweites Heft. 8vo. Gottingen 1837-1838. Gottingische gelehrte Anzeigen, unter der Aufsicht der Kongig]. Geselschaft der Wissenschaften, nos. 6—9, 1837; 146, 147, 1837, and 14, 15, 1838. 12mo. Got- tingen 1837-1838. Mémoire sur les Coquilles Fossiles des Mollusques ter- restres et fluviatiles (de la Classe des Trachélipodes) observées dans les terrains tertiaires du Bassin de YAdour, faisant suite 4 la Conchyliologie fossile de ce Bassin, par M. le Docteur Grateloup. 8vo. Bour- deaux 1838. Actes de la Société Helvetique des Sciences Naturelles DONORS. The Author. Dépot Général de la Ma- rine Frangaise. The British Association for the Advancement of Sci- ence. / The Author. The Author. C. Lyell, Esq., V.P.G.S. The Author. Madras Literary Society. J. MacClelland, Esq. Prof. Hausmann. The Author. 1838. Sept. 30 $1. 3. 8. List of Donations. BOOKS. reunie 4 Neuchatel, 22de Session, 1837. 8vo. Neu- chatel 1837. Proceedings of the Institution of Civil Engineers, Session 1838. 8vo. London 1838. Geognostiche Wanderungen, von Bernhard Cotta. 2 Theile. 8vo. Dresden und Leipzig 1838. Three Expeditions into the interior of Eastern Australia, with Descriptions of the recently-explored region of Australia Felix and of the present Colony of New South Wales, by Major T. L. Mitchell, F.G.S., M.R.G.S., Surveyor-General, in two volumes. 8vo. London 1838. Observations on the Genus Unio, together with Descrip- tions of New Genera and Species in the Families Naiades, Colimacea, Lymnzana, Melaniana, and Peristomiana, by Isaac Lea, Esq., Mem. of the American Phil, Soc., &c., vol. 2. 4to. Philadelphia. State of New York, no. 200, in Assembly, Feb. 20, 1838. Communication from the Governor relative to the Geo- logical Survey of the State. With Plates, detached. 8vo. Albany 1838. The Zoology of the Voyage of H. M. Ship Beagle, under the command of Capt. Fitzroy, R.N., during the years 1832 to 1836, published with the approval of the Lords Commissioners of the Treasury ; edited and superintended by Charles Darwin, Esq., Sec. G.S., &c. Mammalia, by Geo. R. Waterhouse, Esq., Curator of the Zoological Society of London; no. 2 of part 2. 4to. London 1838. . Transactions of the Linnean Society of London, vol. 18, part 1, with a List of the Society, 1838. 4to. London 1838. Lethzea Geognostica, 9te Lieferung (Bogen 49-60) als Rest. pp. 769 to 960, von H. G. Bronn. 8vo. Stuttgart. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., LL.D., aided by Ben- jamin Silliman, jun., A.B. vol. 34, no. 2, July 1838. 8vo. Newhaven 1838. The Journal of the Royal Asiatic Society of Great Bri- tain and Ireland, no. 9, August 1838. 8vo. London 1838. Royal Asiatic Society, Proceedings of the Committee of Agriculture and Commerce; note by the Chairman at a Meeting of the Committee held on the 24th May 1838. 8vo. London 1838. DONORS. M. Agassiz. The Institution of Civil Engineers. The Author. The Author. The Author. Professor Vanuxem and Mr. Conrad. Charles Darwin, Esq., Sec. G.S. The Linnean Society. The Author. The Conductors. The Royal Asiatic Society. List of Donations. 1838. BOOKS. DONORS. Sept. 8. Catalogue of the Chinese Library of the Royal Asiatic Society. The Royal Asiatic Society. Abhandlungen der Kéniglichen Akademie der Wissen- schaften zu Berlin, aus dem Jahre 1836. 4to. Berlin The Royal Academy of 1838. Berlin. 12. Proceedings of the Royal Academy of Berlin, from July 1837 to June 1838. 8vo. Berlin 1837-1838, = 8 ....... a Aaraie bse Pain 20. Report of the Seventh Meeting of the British Associa- tion for the Advancement of Science, held at Liverpool in September 1837. 8vo. London 1838. The British Association. 21. Transactions of the American Philosophical Society held at Philadelphia for promoting Useful Knowledge, new series, vol. 6, part 1. 4to. Philadelphia 1838. American Phil. Society. ' Annales des Mines, ou Recueil de Mémoires sur )Ex- ploitation des Mines et sur les Arts qui s’y rapportent, troisiéme série, tome 13, 3 livraison de 1838. 8vo. L’Administration des Paris 1838. Mines. 28. Mémoire sur les Rochers Calcaires innombrables épars dans les Environs de la Roche, et jusqu’au lit de l’Arve, et sur les Blocs de Granit qui les accompagnent, par J.-A. De Luc. 4to. The Author. Oct. 3. The Economy of a Coal Field; an Exposition of the Objects of the Geological and Polytechnic Society of the West Riding of Yorkshire, and of the best means of attaining them, by James F. W. Johnston, M.A., F.R.SS, L. and E. 8vo. Durham 1838. The Author. 6. Allen’s Select List of Publications. 12mo. London 1838. Messrs. Allen and Co. Mémoires couronnés par l’Académie Royale de Bruxelles, tomes 5, 6, 7, 8, 9, 10, 11, 12, 13. fol. Bruxelles 1824 The Royal Academy of —1838. Brussels. Nouveaux Mémoires de l’Académie Royale des Sciences et Belles-Lettres de Bruxelles, tome 10. fol. Brux- elles 1836-1837. Annales de l’Observatoire de Bruxelles publiés aux frais de lEtat, par le Directeur, A. Quetelet, tome 1, deux- iéme partie. 4to. Bruxelles 1837. Bulletin de l’Académie Royale de Bruxelles de la Séance du 4 Novembre 1837, jusqu’a la Séance du 4 Aoit 1838. 8vo. Bruxelles 1837-1838. ‘ Annuaire de l’Académie Royale des Sciences et Belles- Lettres de Bruxelles, 1836-37-38. 18mo. Bruxelles Ce USSO—S6. Memmi bk eee I ee reais amMens fetete cre Sas 7. Royal Geological Society of Cornwall, Twenty-fifth Royal Geological Society Annual Report of the Council. 8vo. Penzance 1838. of Cornwall. The Analyst; a Quarterly Journal of Science, Litera- 1838. Oct. 12. 26 27 Dec 2 or List of Donations. BOOKS. ture, Natural History, and the Fine Arts, edited by Edward Mammatt, Esq., F.G.S., no. 25, October 1838. 8vo. London 1838. Mémoires pour servir a une Description Géologique de la France, rédigés par ordre de M. le Directeur de Y Administration Générale des Ponts et Chaussées et des Mines, sous la direction de M. Brochant de Vil- liers, Inspecteur-Général au Corps Royal des Mines, par MM. Dufrénoy et Elie de Beaumont, tome 4. 8vo. Paris 1838. Lethzea Svecica, seu Petrificata Sveciz, Iconibus et Cha- racteribus illustrata a W. Hisinger. 4to. Holmia 1837. Mémoires de la Société Géologique de France, tome troisiéme, premiere partie. 4to. Paris 1838. Annual Report of the Leeds Philosophical and Literary Society for 1837-38. 8vo. Leeds 1838. . Discurso lido em 15 de Maio de 1838, na Sesso publica da Academia Real das Sciencias de Lisboa, por Joa- quim José da Costa de Macedo. . Verhandlungen der Gesellschaft des vaterlandischen Mu- seums in Bohmen in der sechszehnten allgemeinen Versammlung, am 18 April 1838. 8vo. . A List of Members of the Royal College of Surgeons in London. 8vo. London 1838. . The Zoology of the Voyage of H. M. Ship Beagle, under the command of Captain Fitzroy, during the years 1832 to 1836, edited and superintended by Charles Darwin, Esq., M.A., Sec. G.S., &c. Mammalia, by George Waterhouse, Esq., no. 3 of part 2. 4to. Lon- don 1838. Annales des Mines, ou Recueil de Mémoires sur ) Ex- ploitation des Mines et sur les Sciences et les Arts qui s’y rapportent, rédigées par les Ingénieurs des Mines, troisieme série, tome 14, 4iéme livr. de 1838. 8vo. Paris. List of the Linnean Society of London, 1838. 4to. Lon- don 1838. Transactions of the Cambridge Philosophical Society, vo]. 6, part 1. 4to. Cambridge. Del Sollevamento e dell’ Avvallamento di alcuni Terreni, Discorso di D. Paoli. 8vo. Pesaro 1838. Antonii Bertoloni, M.D., Commentarius de itinere Nea- politano, estate anni 1834 suscepto. 8vo. Bononiz 1837. DONORS. The Author. The Authors. The Author. Geological Society of France. Leeds Philosoph. Society. The Royal Lisbon Aca- demy. The Society of the Father- land Museum of Bohemia. The Royal College of Sur- geons. Charles Darwin, Esq., Sec. GS. L’Administration des Mines. Linnean Society. Cambridge Philosophical Society. The Author. I] Sig. Tenore. 17. 20. Last of Donations. BOOKS. - Essai sur la Statistique Générale de la Belgique, composé sur des Documents publics et particuliers, par Xavier Heusehling, Premier Commis au Ministére des Fi- nances, et publié par Ph. Van der Maelen, Fondateur de l’Etablissement Géographique de Bruxelles. 12mo. Bruxelles 1838. Catalogue Général de lEtablissement Géographique de Bruxelles, fondé par Ph. Van der Maelen. The Journal of the Geographical Society of London, vol. 8, part 3, 1838. 8vo. London 1838. Transactions of the Zoological Society of London, vol. 2, part 2. 4to. London 1838. Proceedings of the Zoological Society of London, from Oct. 10th, 1837, to July 10th, 1838. 8vo. The American Journal of Science and Arts, conducted by Benjamin Silliman, M.D., L.L.D., &c., For. Mem. G.S., &c., aided by Benjamin Silliman, junr., A.B., vol. 35, no. 1, October 1838. 8vo. New Haven. Bulletin de la Société Géologique de France, tome 9, feuilles 15 219 et 20a 22. 8vo. Instructions pour ]’Exploration Géologique de l’Algérie, rédigées par M. Elie de Beaumont, adoptées par |’Aca- démie des Sciences, le 19 Mars 1838. 4to; et In- structions pour les Géologues de |’Expédition qui se rend dans le Nord de l'Europe, rédigées par M. Elie de Beaumont. 4to. Comptes Rendus Hebdomadaires des Séances de I’Aca- démie des Sciences, par MM. les Secrétaires Perpe- tuels, for 1838. 4to. Paris 1838. Arboretum et Fruticetum Britannicum, by J. C. Loudon, Esq., F.L.S., the numbers published during 1838. 8vo. London 1838. The Magazine of Natural History, new series, conducted by Edward Charlesworth, Esq., F.G.S., formerly by J.C. Loudon, Esq., F.L.S., &c., for 1838. 8vo. Lon- don 1838. The London and Edinburgh Philosophical Magazine and Journal of Science, conducted by Sir David Brewster, K.H., LL.D., F.R.S. L. and E., &c., Richard Taylor, Esq., F.S.A., L.S., G.S., &c., and Richard Phillips, Esq., F.R.S. L. and E., F.G.S., &c., for 1838. 8vo. London 1838. The Repertory of Patent Inventions, and other Disco- veries and Improvements in Arts, Manufactures, and Agriculture, for 1838. 8vo. London 1838. DONORS. M. Van der Maelen, F.G.S. . The Geographical Society of London. The Zoological Society. The Conductors. The Geological Society of France. The Author. The Academy of Sciences of Paris. The Author. The Conductor. Rich. Taylor, Esq., F.G.S. The Proprietor. 1838. List of Donations. BOOKS. Dec. 20. Observations on Limes, calcareous Cements, &c., by Col. 1839. Jan. 9 Feb. 1 C. W. Pasley, R.E., F.G.S. Dictionnaire Géographique du Luxembourg, par M. Ph. Vander Maelen. . The Silurian System, founded on Geological Researches in the counties of Salop, Hereford, &c., by Roderick Impey Murchison, Esq., F.G.S., &c. Instructions pour les Géologues de Expédition qui se rend dans le Nord de |’Europe, rédigées par M. Elie de Beaumont. 4to. Paris 1838. Instructions pour l’Exploration Géologique de |’ Algérie, rédigées par M. Elie de Beaumont. 4to. Paris. The Zoology of the Voyage of H. M. Ship Beagle, under the command of Captain Fitzroy, R.N., during the years 1832 to 1836, edited and superintended by Charles Darwin, Esq., Sec. G.S. no. 2, part 3. 4to. London 1829. Proceedings of the Royal Society, no. 35. 8vo. Mr. A. Nattali’s Catalogue of Books for 1839. 8vo. London 1839. Lethoea Geognostica, von G. H. Bronn, p. 481 to end. 8vo. plates 4to. Stuttgart 1838. A Sketch of the Geology of Fife and the Lothians, in- cluding detailed descriptions of Arthur’s Seat and Pentland Hills, by Charles Maclaren, Esq., F.R.S.E. 12mo. Edinburgh 1839. Monographia Chalciditum, by Francis Walker, Esq. 8vo. London 1839. Memoirs of the Royal Astronomical Society, vol. 10. 4to. London 1839. Observations on some new Organic Remains in the Flint of Chalk, by the Rev. J. B. Reade, M.A., F.R.S., 8vo. London 1838. Memoirs of the Wernerian Society, vol. 4, parts I and 2 ; vol. 5, part 1; and vol. 7. 8vo. Edinburgh. Elements of Chemistry, including the recent Discoveries and Doctrines of the Science, by the late Edward Tur- ner, sixth edition, enlarged and revised by Justus Liebig, Ph. D., and Wilton John Turner, Ph. D. Part 3, no. 1, Organic Chemistry, by Professor Lie- big. 8vo. London 1839. Report on the Geology of Cornwall, Devon, and West Somerset, by H. T. De la Beche, Esq., EVR:S.; &e:; Director of the Ordnance Geological Survey; published VOL. V.—SECOND SERIES. F DONORS. The Author. The Author. _ The Author. M. Elie de Beaumont, For. Mem. G.S. Charles Darwin, Esq., Sec. G.S. The Royal Society. Mr. Nattali. The Author. The Author. The Author. The Royal Astronomical Society. The Author. The Wernerian Society. Wilton John Turner, Esq. The Lords Commissioners 1839, Feb. March List of Donations. BOOKS. by order of the Lords Commissioners of Her Majesty’s Treasury. 8vo. London 1839. 1. Address to the Members of the Berwickshire Natural- ists’ Club, delivered at the Anniversary Meeting held at Ford, 19th September, 1838, by Dr. Clarke, Presi- dent. 8vo. Institution of Civil Engineers, Annual Report. sion 1839. 8vo. Annales des Mines, troisiéme série, tome 14, 5° livrai- son, 1838. 8vo. Paris 1838. Lehrbuch der Geognosie und Geologie von Karl Ciasar v. Leonhard, mit Abbildungen. 8vo. and plates 4to. Stuttgart 1835. Charts, Sailing Directions, and Tide Tables, published by direction of the Lords Commissioners of the Admi- ralty. 8vo. and 4to. 1838. ; Ses- The Spas of Germany, 2nd edition, by A. B. Granville, M.D., F.G.S. 8vo. London 1838. A Conchological Manual, by G. B. Sowerby, jun. 8vo. London 1839. Illustrazione di un Nuovo Cetaceo Fossile proposta dal Medico Giounni Domenico Bruno. 4to. Bulletin de la Société Géologique de France, tome 9, feuilles 23-27. 8vo. Paris 1838. American Journal of Science and Arts, conducted by Dr. Silliman, For. Mem. G.S. vol. 32, no. 2. 8vo. New Haven 1838. On the Courses of Hurricanes, with Notices of the Ty- foons of the China Sea, and other Storms, by W. C. Redfield, Esq. From the American Journal of Sci- ence and Arts, no. 2, vol. 25. Observations on Roman Coin Moulds discovered in England and France. From the 3rd no. of the Nu- mismatic Chronicle. 8vo. London 1839. Rapport sur les Travaux de la Carte Géologique, pendant l'année 1838, par A. H. Dumont. 12mo. Extrait du tom. 5 des Bull. Acad. Roy. de Bruxelles. . Abhandlungen der Kéniglichen Akademie der Wissen- schaften zu Berlin, aus dem Jahre 1836. 4to. Berlin 1838, - aus dem Jahre 1833. 4to. Berlin. Illustrations of the Botany and other Branches of the Natural History of the Himalayan Mountains, and of the Flora of Cashmere, by J. Forbes Royle, M.D., V.P.R.S., F.G.S., &c. &c., part 10. 4to. London, DONORS. of Her Majesty’s Trea- sury. The Berwickshire Natural- ists’ Club. The Institution of Civil Engineers. L’Administration des Mines. Rev. Wm. Bilton, F.G.S. Capt. Beaufort, R.N., Hon. Mem. G.S., by direction of the Lords Commis- sioners of the Admiralty. The Author. The Author. The Author. The Geological Society of France. The Conductor. The Author. The Author. The Author. The Royal Berlin. eeere eerste aes The Author. see ee sewer ee Academy of 1839, March 13. 18. List of Donations. BOOKS. . The Zoology of the Voyage of H. M. Ship Beagle, under the command of Captain Fitzroy, R.N., during the years 1832 to 1836, edited by Charles Darwin, Esq., M.A., F.R.S., &c., Naturalist to the Expedition. No. 2 of part 1, Fossil Mammalia, by Richard Owen, Esq., F.R.S., &c. 4to. London 1839. Lectures on Comparative Anatomy, delivered in the University of London during 1833, by Robert E. Grant, M.D., &c., Professor of Comparative Anatomy and Zoology in the University of London. Taken in short-hand writing from his oral demonstrations, and published in the Lancet for 1833-34. 8vo. On the Principles of Classification as applied to the Pri- mary Divisions of the Animal Kingdom, by Robert E. Grant, M.D. 8vo. General View of the Characters and Distribution of Ex- tinct Animals, by Robert E. Grant, M.D., &c. 8vo. On the Foot-marks of Cheirotherium in the New Red Sandstone of Stourton Hill, by Dr. Grant. (From the Liverpool Mercury, August 24, 1838.) . Philosophical Transactions of the Royal Society of Lon- don for the year 1838, part 2. 4to. London 1839. Proceedings of the Royal Society of London, no. 36. Bulletin de la Société Géologique de France, tome 10, feuilles 1-4. 8vo. Emanuelis Swedenborgii Opera Philosophica et Mine- ralogica. Tres tomi fol. Dresde et Lipsize 1734. Nouveaux Mémoires de Académie Royale des Sciences et Belles Lettres de Bruxelles, tome 11. 4to. Brux- elles 1838. Mémoires couronnés par l’Académie Royale des Sciences et Belles Lettres de Bruxelles, tome 11 et 14. 4to. Bruxelles 1837, 1838. Bulletin de Académie Royale des Sciences et Belles Lettres de Bruxelles, 1838, nos. 9—12. 8vo. Bruxelles. Annuaire de l’Académie Royale des Sciences et Belles Let- tres de Bruxelles, 1839, 5iéme année. 18mo. Bruxelles. Proceedings of the Royal Irish Academy, no. 15, 1839. 8vo. Royal Asiatic Society of Great Britain and Ireland, Pro- ceedings of the Committee of Commerce and Agricul- ture, 1838. 8vo. London 1839. First Report on the Geological Survey of the Province of New Brunswick, by Abraham Gesner, Provincial Geo- logist, &c., 1839. 8vo. Saint John 1839. F 2 DONORS. Charles Darwin, Esq., Sec. G.S. Professor Grant, M.D. F.G.S. eeeereeee esses ee eoeeees The Geological Society of France. Leonard S. Coxe, Esq., F.G.S. The Royal Academy of Brussels, The Royal Irish Academy. The Committee of Cor- merce and Agriculture ef the Asiatic Society. The Author. 1839. List of Donations. 4 BOOKS. March 18. The Journal of the Royal Geographical Society of Lon- 26, 30. April 2. 3 15 May 1 4, May 4. don, vol. 9, part 1. 8vo. London 1839. Buenos Ayres and the Provinces of the Rio de la Plata, by Sir Woodbine Parish, K.C.H., F.R.S., F.G.S., &c.. 8vo. London 1839. Proceedings of the Botanical Society of London, vol. 1, part 1. 8vo. London 1839. A Treatise on Crystallography, by W. H. Miller, M.A., F.R.S., F.G.S., F.C.P.S., Fellow and Tutor of St. John’s College, and Professor of Mineralogy in the University of Cambridge. 8vo. Cambridge 1839. . Outlines of Comparative Anatomy, by Robert E. Grant, M.D., F.R.S., F.G.S., &c., parts 1—4; and Essays on Zootomical Subjects, by Robert E. Grant, M.D. 8vo. London. Classification of the Older Stratified Rocks of Devon- shire and Cornwall, by the Rev. Professor Sedgwick, F.R.S., F.G.S., and Roderick Impey Murchison, Esq., F.R.S., F.G.S. From the Philosophical Magazine, vol. 14. 8vo. London 1839. Dictionnaire Géographique de la Province de Limbourg ; Etablissement Géographique de Bruxelles, fondé par Ph. Vander Maelen. 8vo. Bruxelles 1835. Ninth Report of the Scarborough Philosophical Society, August 31, 1838. 8vo. Scarborough 1838. . The Naturalist; illustrative of the Animal, Vegetable, and Mineral Kingdoms ; edited by Neville Wood, Esq. ; nos. 8—12 of vol. 2; 17—19 and 23 of vol. 3; and 25, 26, and 29 of vol. 4. 8vo. London 1835-38. Annales des Mines, ou Recueil de Mémoires sur ]|’Ex- ploitation des Mines, et sur les Sciences et les Arts qui s’y rapportent; rédigées par MM. les Ingénieurs des Mines; troisiéme série, tome 14, 6° livraison de 1838. 8vo. Paris 1838. . Bulletin de la Société Géologique de France, tome 9, feuilles 28-32. 8vo. . Journal of the Geological Society of Dublin, vol. 1, part 4. 8vo. Dublin 1838. . The Zoology of the Voyage of H. M. Ship Beagle, under the command of Capt. Fitzroy, R.N., during the years 1832 to 1836; edited and superintended by Charles Darwin, Esq., M.A., F.R.S., Sec. G.S. No. 3 of part 1, Fossil Mammalia, by Richard Owen, Esq., F.R.S., F.G.S., &c. 4to. London 1839. Account of an Intermitting Brine Spring discharging DONORS. The Royal Geographical Society. The Author. The Botanical Society of London. The Author. The Author. The Authors. M. Vander Maelen, F.G.S. The Scarborough Philoso- phical Society. The Editor. L’Ecole des Mines. The Geological Society of France. The Geological Society of Dublin. Charles Darwin, Esq., Sec. G.S. 1839. May 2 Ww 31. June 2. 4, List of Donations. BOOKS. Carbonic Acid Gas, near Kissingen, in Bavaria, by Professor Forbes, F.G.S. From the Edinburgh New Philosophical Journal, no. 52. 8vo. Edinburgh 1839. Foreign Monthly Review, and Continental Literary Journal, no. 1, May 1839. 8vo. London 1839. Proceedings of the American Philosophical Society, vol. 1, no. 6. 8vo. Philadelphia 1838. Report of the Local Secretaries of the Meeting of the British Association at Newcastle. 8vo. Newcastle 1839. Bulletin de la Société Géologique de France, tome 10, feuilles 5 4 9. 8vo. Conchyliologie Fossile du Basin de l’Adour, 4° et 5° Mémoires, et Tableau Statistique des Coquilles Uni- valves Fossiles trouvées dans les Couches Tertiaires du Basin de l’Adour, par M. le Docteur Grateloup. 8vo. Bordeaux 1838. Researches on the Development, Structure, and Dis- eases of the Teeth, by Alexander Nasmyth, Esq., F.L.S., F.G.S. 8vo. London 1839. Proceedings of the Royal Irish Academy, no. 16, 8vo., and a List of the Members. 8vo. Dublin 1838. Reply to Professor Bischoff’s Objections to the Chemical Theory of Volcanos, by Charles Daubeny, M.D., &c. 8vo. Wonders of Geology, by Gideon Mantell, LL.D., F.R.S.,_ 3rd edit. 12mo. London 1839. The London and Edinburgh Philosophical Magazine and Journal of Science, conducted by Sir David Brewster, K.H., LL.D., F.R.S. L. & E., &c., Richard Taylor, Esq., F.S.A., L.S., G.S., &c., and Richard Phillips, Esq., F.R.S. L. & E., F.G.S., &c.; for the months of January to June 1839. 8vo. London 1839. The Repertory of Patent Inventions, and other Disco- veries and Improvements in Arts, Manufactures, and Agriculture, for the months of January to June 1839. 8vo. London 1839. The Magazine of Natural History, New Series, conduct- ed by Edward Charlesworth, F.G.S., &c. ; for the months of January to June 1839. 8vo. London 1839. Comptes Rendus Hebdomadaires des Séances de |’Aca- démie des Sciences, par MM. les Sécrétaires perpe- tuels, Premier Semestre; January to June 1839. Ato. Paris 1838. DONORS. The Author. The Publisher. The American Philoso- phical Society. J. F.W. Johnston, Esq. The Geological Society of France. The Author. The Author. Royal Irish Academy. Dr. Daubeny. The Author. Richard Taylor, Esq., E.G.S. The Proprietor. The Conductor. The Academy of Sciences of Paris. List of Donations. II. Donations to the Collections of Maps, Sections, &c. 1835. MAPS, &c. June 19. Pilote Frangais, 3 vols. folio. Exposé des Travaux relatifs 4 la Reconnaissance Hydro- graphique des Cotes occidentales de France. Mémoire sur les Atterages des Cotes occidentales de France. Le Pilote de I’Ile de Corse; 32 cartes et plans en feuilles. Description Nautique des Cétes de la Martinique; 20 cartes et plans en feuilles. Sheet 63 of the Ordnance Map, in continuation of the Trigonometrical Survey of Great Britain. . Esquisse Orographique de l'Europe, par J. H. Bredsdorff et O. N. Olsen, en 1824, corrigée et considérablement augmentée par O. N. Olsen en 1830; gravée par P. J. Sept. 9. Sechusen. The Ordnance Townland Survey of the County of Fer- managh, in 42 sheets, with Title and Index. A Lithographic Drawing of Ollacrinus, a new Genus of Encrinite, discovered by G. Cumberland, jun. Esq., in August 1826, in the Limestone near Riddle, Lanca- shire. A rough Sketch, by Noggerath, of the part of the Eifel between Adenau and Wittich. . Arrowsmith’s Map of La Plata, the Banda Oriental, and Chile. Carte Géologique du Département de la Manche, dressée en 1825, 1826, 1827, par M. A. de Caumont. A specimen plate, illustrative of Natural History, by Mr. G. B. Sowerby, jun. : Six Views in the Zoological Gardens, by Mr. Scharf. A Portrait of Sir F. W. J. Herschel, M.A., F.R.S., G:S., ccc. 16. 1836. Jan. 20. An Impression of a Lithographic Drawing of a Fossil Turtle, in a Nodule of Harwich Cement Stone. No. 52 of the Ordnance Map, in continuation of the Tri- gonometrical Survey of Great Britain. DONORS. The Director-General of the Depot de la Marine de France. eee ee reese eresereseres The Master-General and Board of Ordnance. M. O. N. Olsen. Lieut.-Col. Colby, F.G.S., by order of His Excel- lency the Lord-Lieutenant of Ireland. G.Cumberland,Esq.,F.G.S. Lieut. Nelson, R.E. W. Parish, Esq. Sec. G.S. M. A. de Caumont. Mr. G. B. Sowerby, jun. Mr. Scharf. Rev.R.Sheepshanks,F.G.S. Edw. Charlesworth, Esq., F.G.S. The Master-General and Board of Ordnance. List of Donations. 1836. MAPS, &c. Feb. 8. The Ordnance Townland Survey of the County of Ar- magh, in 34 sheets, with the Title and Index sheet. Map of the County of Sutherland, constructed by direc- tion of His Grace the Duke of Sutherland, on the basis of the Trigonometrical Survey of Scotland. An Impression of an Engraving of Dentaliwm Saturni (Heeninghaus), discovered in the Transition Limestone April 5. 14, of Gerolstein. 20. Sheet 1 of a Geological Map of Saxony. The Ordnance Townland Survey of the County of Mona- ghan, in 36 sheets, with Title and Index sheet. . Map, Section, and Book of Reference of the intended Midland Counties Railway. . An Impression of a Lithographic Portrait of Charles Lyell, Esq., P.G.S. . Admiralty Charts, Sailing Directions, and Tide Tables, published during the years 1834-1835. . July 12. Ordnance Townland Survey of the County of Louth, 27 sheets, including Title and Index sheet. Sept. 28. Sheets nos. 51 and 60 of the Ordnance Map, in continua- tion of the Trigonometrical Survey of Great Britain. Nov. 12. Ordnance Townland Survey of the County of Donegal, in 112 sheets, including the Title and Index. Dec. 17. Sheets 72 and 109 of the Ordnance Map, in continuation of the Trigonometrical Survey of Great Britain. 1837. Mar, 18. Admiralty Charts, Sailing Directions, and Tide Tables, published during the year 1836. May 3. Section and Plans of the Chester Junction, Chester and Trewe, and the Manchester South Union Railways. 6. Theoretical Table of the most general European succes- sion and disposition of the Strata and Rocks which compose the Crust of the Earth, by Alexander Brong- DONORS. His Excellency the Lord- Lieutenant of Ireland. His Grace fhe Duke of Sutherland. M. F. W. Heeninghaus. Professor Rich, by order of the Council of Mines of Saxony. Lieut.-Col. Colby, F.G.S., by order of His Excel- lency the Lord-Lieute- nant of Ireland. Thos. Edw. Dicey, Esq. Mr. Thos, McLean. Capt. Beaufort, R.N., Hon. Mem. G.S., by order of the Lords Commissioners of the Admiralty. Lieut.-Col. Colby, R.E., F.G.S., by order of the Lord-Lieutenant of Ire- land. The Master-General and Board of Ordnance. Lieut.-Col. Colby, R.E., F.G.S., by order of His Lord- Lieutenant of Ireland. The Master-General and Board of Ordnance. Excellency the Capt. Beaufort, R.N., Hon. Mem. G.S., by order of the Lords Commissioners of the Admiralty. Sir Philip Grey Egerton, Bart., M.P., F.G.S. List of Donations. 1837. MAPS, &c. niart, Professor of Mineralogy in the Museum of Na- tural History, Paris. May 4%. Tabular View of the Distribution of the characteristic Organic Remains of the Jura Limestone in Germany, by Leopold de Bach, For. Mem. G.S. 9. Ordnance Townland Survey of the County of Meath, in 55 sheets, including the Title and the Index. Fifteenth Section of the Geological Map of Saxony. June 14. Sheet no. 59 of the Ordnance Map, in continuation of the Trigonometrical Survey of Great Britain. 20. Ordnance Townland Survey of the County of Leitrim, in 40 sheets, including the Index and the Title. Oct. 23. A Print from a Portrait of Dr. William Smith. An impression from an Engraving of a Portrait of Dr. Mantell. Jan. 16. An Engraving of the Skeleton of the Irish Elk, from near Waterford, from a Drawing by Professor Phillips. Feb. 1. Ordnance Townland Survey of the Counties of Sligo and Longford, in 78 sheets, including Title and Index. Admiralty Charts, Sailing Directions, and Tide Tables, published during the year 1837. May 1. Map of the Maritime County of Mayo in Ireland, on va- rious Bases and Trigonometrical Operations, exhibiting Barometrical Observations of the Mountains, the Le- vels, and Depths of the Bogs and Lakes, with Astro- nomical Observations, Physical Sections, and Profiles of the Country ; executed by order of the Grand Jury, and terminated in 1817, by William Bald, F.R.S.E., M.R. Geog, Soc., Paris, F.G.S., M.R.1.A. June to oe 49, 50, 66, 67, 68, 72, of the Ordnance Map, in Nov. 1. continuation of the Trigonometrical Survey of Great Britain. July 28. Sheet 10 of the Geological Map of the Kingdom of Saxony, Oct. 24. Two Lithographic Impressions of a Drawing of Pentacri- nites Briareus and of the Palo de Vaca, or Cow Tree, from an original sketch by Sir R. Ker Porter; litho- DONORS. M. Alex. Brongniart, For. Mem. G.S. M. Leopold de Bach, For. Mem. G.S. Col. Colby, R.E., F.G.S., by order of His Excel- lency the Lord-Lieute- nant of Ireland. The Directors of the Royal Saxon Mines. The Master-General and Board of Ordnance. Col. Colby, R.E., F.G.S., by order of the Lord- Lieutenant of Ireland. Dr. W. Smith. Mr. Samuel Stepney. Professor Phillips, F.G.S. Col. Colby, R.E., F.G.S., by order of the Lord- Lieutenant of Ireland. Capt. Beaufort, R.N., Hon. Mem. G.S., by order of the LordsCommissioners of the Admiralty. William Bald, Esq., F.G.S. The Master-General and Board of Ordnance. The Council of Mines of Saxony. ‘ 3 ' PhS) List of Donations. MAPS, &c. graphed on English Lias, and printed with Fossil Sepia on paper manufactured from Musa textilis. . Ordnance Survey of the County of Westmeath, in 42 sheets, including the Title-page and Index. . Map of the settled part of the colony of New South Wales, showing the situation of the principal rocks, by Major T. L. Mitchell, F.G.S. Fourth sheet of the Geological Map of Saxony. Geological Map of Germany and the neighbouring States, and Geological Map of the N.W. of Germany, by Friedrich Hoffmann. . Map of the Silurian region and adjacent counties of Eng- land and Wales geologically illustrated, by Roderick Impey Murchison, Esq., F.G.S., (mounted and framed). Lithographic Print of the Orthagoriscus Mola or Sun Fish, washed ashore at Scarborough during a gale on the 27th November, 1838. The original in the Scarborough Museum. . Impressions from three Lithographic Plates of Devonshire Fossils. Ill. SPECIMENS. Specimens from Uddervalla. Rock specimens from Teneriffe. A collection of specimens from the Virgin Islands, made DONORS. John Murray, Esq., South- ampton. Col. Colby, R.E., F.G.S., by direction of His Ex- cellency the Lord-Lieute- nant of Ireland. MajorT.L. Mitchell, F.G.S. The Council of Mines of Saxony. Rev. Prof. Whewell, P.G.S. R.I.Murchison, Esq. F.G.S. Edw. Hebden, Esq., on the part of the Scarborough Museum. R. A. C. Austen, Esq., F.G.S. Donations to the Cabinet of Minerals. DONORS. Charles Lyell, Esq., P.G.S. at the request of the Royal Geographical Society of The Royal Geographical London, by Robert Schomburgk, Esq. . A collection of specimens from the Cerro de Pasco, made by Don Mariano Rivero. . Specimens from Beauvais. Fossils from the inferior oolite of Leckhampton Hill, near Cheltenham. Additional specimens from the strata between the chalk and the Oxford oolite, in the south-east of England. . Fossils from Malta, Fossils from the chalk at Gravesend. VOL. V.—SECOND SERIES. G Society. Don Mariano Rivero. Gideon Mantell, F.G.S. Esq,., Capt. Mudge, R.E., F.G.S. W.H. Fitton, M.D., F.G.S. — Collins, Esq. Joseph Prestwich, jun., Esq., F.G.S. 14, 24, List of Donations. SPECIMENS. Specimens from the newer pliocene beds in the neigh- bourhood of Brighton. . Specimens of fishes from the chalk. . Ammonites perarmatus and fossils from the chalk, upper green-sand, &c. Fossils and flints from the chalk. Fossils from the gault of Neuchatel, Switzerland. Specimens from the Rhine. Fossils from Cerigo. Fossils from Blackdown and Wiltshire. A specimen from the plastic clay near Chatham. A slab of new red sandstone with impressions of fish, from Rhone Hill, near Dungannon. . Specimens from the gravel of Bollingdon Hill, Essex. Specimens of vegetable remains from the coal-mines at Sydney, Cape Breton. Fossil fishes from the coal-measures at Wardie near Newhaven, Stoney Hill near Musselburgh, and the Edmonstone Colliery near Stoney Hill. Specimens from the chalk of Beachy Head, and from the Hastings Beach. . Specimens from the chalk of Hemel Hempstead. Fossils from Blackdown and Bognor. Remains of a recent sheep imbedded in indurated clay. 5. Fossils from the limestone shale of Pembrokeshire. 8. Specimens of selenite from the sands of the plastic clay 20. at Bishopstone Cliff, between Herne Bay and Reculvers. . Fossils from Cornwall. Fossils from the neighbourhood of Bodmin. Specimen of earthy phosphate of iron from Boyland, near Long Stratton, Norfolk. Specimens of syenite from veins traversing mica slate-and chalk near Goodland Cliff and Torr Eskert, to the south of Fair Head, Antrim. Fossils from the strata below the chalk in Buckingham- shire and Oxfordshire. Fossils from the lower limestone shale and the upper Si- lurian beds of Pembrokeshire. DONORS. GideonMantell,Esq.,F.G.S. J. Kenyon, Esq.,in the name of the late Mrs. Kenyon. R. Cuming, Esq. Professor Agassiz. Lieut. Nelson, R.E. Lord Nugent. Miss Benett, of Norton House. G. S. Nicholson, Esgq., F.G.S. Thomas Green, Esq. John Brown, Esq., F.G.S. J. B. Ford, Esq. Major-General Lord Gree- nock, F.G.S. Woodbine Parish, Esq., Sec. G.S. H. C. White, Esq., F.G.S. Miss Benett, House. of Norton Messrs. White, Francis, and Francis. Earl of Cawdor, F.G.S. W.Richardson,Esq., F.G.S. H. T. De la Beche, Esq., For. Sec. G.S., in the name of the Ordnance Geological Survey. Dr. Potts. S. Woodward, Esq. Rich. Griffith, Esq., F.G.S. W.H. Fitton, M.D., F.G.S, Earl of Cawdor, F.G.S. 1836. Jan. 20. Feb. 3 Apr is: May 1. List of Donations. SPECIMENS. Fossils from Bognor. ‘ Specimens of sandstone, with impressions of plants, from the neighbourhood of Whitfield. Fossils from Van Diemen’s Land. Fossil plants from the coal-measures at Barnsley, York- shire. 3. Specimens from the Island of Ascension. Fossils from the neighbourhood of Cheltenham. . Specimen of bone breccia and fossils from Cerigo. . Large fragment of bone from the base of the diluvial cliffs near Southwold, Suffolk. Cast of the united atlas and axis of an Ichthyosaurus. . Mesotype from Mount Ecchio, near Verona. Petrified wood, with hazel nuts, from a sub-marine forest and bog on the Irish coast, described in the Geological Transactions, vol. 4, p. 443. Remains of the mastodon, mammoth, hippopotamus, pig, ox, and deer, from the Sevalik Mountains, at the southern base of the Himalayas, between the Sutluj and the Ramgunga rivers. Specimens from the Lipari Isles, Etna, &c. Fossils from Hordwell Cliff. Head of Ichthyosaurus communis. Selenite from Prince Regent’s Inlet, lat. 73° 27' 23", long. 10° 50’ 34", . Fossils from the green-sand and the transition limestone of Devonshire. Specimens from the coal-measures and the Silurian system of Coalbrook Dale. . Specimens from the lias at Lyme Regis. Specimens from the marlstone near Lyme Regis. Coal shale, with Goniatites Listert, from the Bradford coal-field. Specimens from the London clay, near Chalk Farm. Specimen of Anadonta Parishii. DONORS. James Laird, M.D., F.G.S. Rev. Archdeacon Scott, F.G.S. Richard W. Hay, Esq. W. Taylor, Esq., F.G.S. Mrs. Warren, in the name of the late Dr. Warren. Capt. Mudge, R.E., F.G.S. Lord Nugent. Edw. Charlesworth, Esq., F.G.S. Sir Philip Grey Egerton, Bart., M.P., F.G.S. James Yates, Esq., F.G.S. eoveoeeeoevrereeeseeeeeren Capt. ProbyCautley,F.G.S. Hon. JohnStewart Wortley, F.G.S. CharlesStokes, Esq.,F.G.S. Marquis of Northampton, F.G.S. Capt. Sir Edw. Parry, R.N., F.G.S. R.A.C. Austen, Esq., F.G.S. Joseph Prestwich, jun., Esq., F.G.S. Visct. Cole, M.P., F.G.S. Viscount Cole,M.P.,F.G.S. and’ Sir Philip Egerton, Bart., V.P.G.S. Grey M.P., Visct. Oxmantown, F.G.S. N. T. Wetherell, Esq., F.G.S. Woodbine Parish, Esq., Sec. G.S. 1836. May 22. 23. June July 390. ae at Sep. 13. 2ile Nov. 16. ive Dec. 8 6 14 1837. Jan. 1. List of Donations. . SPECIMENS, Scaphites Hillsii, from the lower green-sand, Maidstone. Remains of the elephant, &c. from Bollingdon Hill, Essex. Specimens from the crag. . Specimens from the chalk at Buxton, Norwich. Specimens of fossil wood from Egypt. Additional remains of the mastodon, mammoth, &c., from the Sevalik Mountains. Specimens from Balmen, Badra and Linput, in Cutch, from Sinde and the banks of the Indus. Specimens from the northern side of Kunour, lat. 32° 30’, long. 78°, in the Himalayas. Specimens from the chalk of Gogmagog Hill, near Cam- bridge. Specimens from the chalk of various parts of England. Fossils from the chalk near Hemel Hempstead. Fossils from the limestone of Teignmouth. Specimen of a fossil crustaceous animal, from the coal formation near Glasgow. Specimens of fossil wood found in rounded boulders of cornbrash at the summit of the Blisworth Ridge, Northamptonshire. . Specimens of coal plants from Cape Breton. . A collection of specimens from Guiana, collected by Robert Schomburgk, Esq. . Specimens of fossil wood from Van Diemen’s Land. . Fossils from Barbadoes; casts of shells from Australia ; and a specimen of new red sandstone found in the fen- land of Lancashire, at the depth of 512 feet. Specimens from the new red sandstone and conglomerate at Allesley, Warwickshire. Specimens of granite from Penrhyn, Cornwall. Specimen of ammonites in flint, from Box Hill near Dorking. Specimens of a fossil tree at Allesley, Warwickshire, and of the new red sandstone in which it was found. Boulders from the sea-shore at Barcelona. Shelly limestone from the old Roman quarries near Tar- ragona. A specimen of iron pyrites from the peat associated with the warm springs of Egra. DONORS. Marquis of Northampton, F.G.S. Elliston Allen, Esq. Edw. Charlesworth, Esq., F.G.S. John Wright, Esq. Lord Prudhoe. Captain Cautley, F.G.S. Lieut. Burnes, H. E. I. C. Service. Lieut. Vicary. N. B. Dennys, Esq. Henry Gregory, Esq. H. C: White, Esq., F.G.S. J.K. Harvey, Esq., F.G.S. John Scouler, M.D., FE.L.S., &c. Richard Creed, Esq. — Brown, Esq. The Royal Geographical Society, and Robert Schomburgk, Esq. — Williamson, Esq. G. B. Greenough, Esq., V.P.G.S. James Yates, Esq., F.G.S. Geo. Rennie, Esq., F.G.S. Rev. Prof. Buckland, D.D., F.G.S., and Jas. Yates, Esq., F.G.S. W.P. Hunter, Esq., F.G.S. eeeereeses A. B. Granville, M.D., F.G.S. 1837. Jan. List of Donations. SPECIMENS. 1. Specimens from the freshwater deposit at Grays; speci- mens from the plastic clay at Woolwich and Upnor; and a specimen of fossil wood from Bayswater. 1. Specimens from Cutch. Polished agates. Specimens from Barbadoes. Casts of fossils from France. . Specimens from the chalk of Norfolk, and recent shells. Specimens from Cornwall. Specimens from Finland and Norway. Specimens from Sarn Badrig, Cardigan Bay. A collection of British and foreign specimens. - Specimens of stalagmite from Gibraltar. . Specimens from the crag of Suffolk. Pentacrinites Briareus, from the lias, Lyme Regis. Fossils from the mountain limestone of Ireland. Specimens from Grignon, Hauteville and Bordeaux, in France, and Piacenza, in Italy. Polished specimens of the limestone of Kilkenny, and a boulder of the Hertfordshire pudding-stone ; and granite from Newry, on the road to Belfast. Hippurite from Perigord. Specimens from the coal-measures of Burdie House, and limestone from Glen Tilt. Specimens of granite, and of garnets in mica-slate, from between Dunkeld and Blair. Polished specimens of fossil wood from Antigua. 2. Osseous breccia from Cerigo. Feb. Feb. 23 Mar. 9) April 5. 19. May 1. 3 17 31 June 1. 15 23 24, July 6. . Specimens of coal plants from Rotherham. . Specimens from Faxoe. A suite of geological specimens from New Jersey. . Tooth of a mastodon from the crag of Norfolk. Recent corals from Bermudas. . Ammonites Lenesiensis, from Shakspeare’s Cliff, Dover. . Specimens of coal shale with vegetable impressions, from the coal-measures at Rhymney, near Merthyr Tydvy]l. Fossils from the mountain limestone in the Isle of Man. A collection of fossils and rocks from Cutch. Specimens from Sicily, Vesuvius, and from the neigh- bourhood of Naples. DONORS. John Morris, Esq. Lieut. Col. Sykes, F.G.S. G. B. Greenough, Esq., F.G.S, Joseph Cowhurst, Esq. M. Puzos. C. B. Rose, Esq. James Yates, Esq., F.G.S. Fras. Walker, Esq., F.G.S. Lieut. Sheringham, R.N. Miss Lousada. L. H. Petit, Esq., F.G.S. John Brown, Esq., F.G.S. Visct. Cole, M.P., F.G.S., and Sir Philip Egerton, Bart., M.P., F.G.S. Visct. Cole, M.P., F.G.S. Chas. Stokes, Esq., F.G.S. W. P. Hunter, Esq., F.G.S. S. P. Pratt, Esq., F.G.S. W. P. Hunter, Esq., F.G.S. oe eres eoe se ee ee eeseeseee Maj. Gen. Sir Pat. Ross, G.C.M.G., K.C.H. W.F. Forbes, M.D. — Roberton, Esq. Dr. Forchhammer, For. Mem. G.S. Prof. H. D. Rogers, F.G.S. Rey. John Gunn. L.S. Coxe, Esq., F.G.S. F, Bonney, Esq. Thomas Williams, Esq. Capt. Bentham. Capt. Grant, F.G.S. John Auldjo, Esq., F.G.S. List of Donations. 1837. SPECIMENS. July 25. Fossils and specimens of rocks from the eastern portion of the great basaltic district of India. 26. Specimens from the country between Madras and Neil- gherries, and from other parts of India. Aug. 3. Specimens from Cape Horn, the Straits of Magellan, &c. Specimens from the pitch lake at Trinidad. 9. Specimens of iron ore from Cornwall. 24. A polished slab of the fossil tree at Cragleith. 26. Specimens from the Gold Coast. 30. A stag’s horn from the Preston and Wyre railway, Lan- cashire. Specimens of the Whitby and Whitehouse building-stone, and of the Whitby porcelain earth, in contact with a whinstone dyke. Sept. 8. Casts of Basilosaurus, the Saurian of Missouri. Oct. 4. Specimens from the Dead Sea. 21. Specimens from near the trap dyke, Penrhyn slate-quar- ries, Bangor. A collection of specimens from Australia. Specimen of Ficoides. Fossil from the mountain limestone, the oolitic and creta- ceous systems of England. A stone brought up with the lead, in 80 fathoms water, upon the edge of the bank about 50 miles east from Cape St. John, Slater Island. Specimens from Madras, Beder, &c. 1838. Jan. 3. Specimens from Madeira. 17. Vertebra of a Plesiosaurus from Terry’s Pits, Hasely Mill, Oxfordshire ; with a fragment of a stag’s horn from the same locality. 31. Specimens from the slate of Devonshire. Feb. 1, Specimen of the asphaltic mastic. Specimens from Bognor. Mar. 21. A mass of Ostrea gregarea from near Oxford. Specimens of copper ore and malleable iron from South- ern Africa. DONORS. J. G. Malcolmson, Esq., F.G.S. Dr. Benza. Charles Collett, Esq., R.N., by Capt. Beaufort, R.N., Hon. Mem. G.S. Gilpin Gorst, Esq., F.G.S. Benj. Tucker, Esq., F.G.S. Messrs. Walker & Burgess. Capt. Vidal, R.N., by Capt. Beaufort, R.N., Hon. Mem. G.S. Decimus Burton, Esq., F.G.S. Whitby Stone Company. R. Harlan, M.D. Henry Beek, Esq. Mr. John Morris. Major T. L. Mitchell, F.G.S. Mrs. Maj.-Gen. Le Cou- tier. Miss Benett, of Norton House. Capt. Beaufort, R.N., Hon. Mem. G.S. Robert Cole, M.D. Wm. Christie, jun., Esq. Rev. T. Birkett. Henry MacLauchlan, Esq., F.G.S. T. W. Simms, Esq. James Laird, M.D., F.G.S. Rev. Prof. Buckland, D.D., V.P.G.S. Capt. Alexander. 1838. Mar. April 8. ON. May 21. ile List of Donations. SPECIMENS. Stratigraphical model of the Under Cliff, Isle of Wight. Rock specimens from the Seychelles Islands. Fossils from the Himalayas. Specimens from Upper Assam. Cast of Hamites articulatus, from the oolitic formation, Normandy. 8. Specimens from the North Lancashire coal-field. 9. Cast of the head of the Mastodon longirostris, from Eppleshein. Specimens from Boulogne and Guernsey. Specimen of Plagiostoma from the Gulf of California. . A specimen of Dapedium orbis (Agassiz), from Barrow- upon-Soar. . Specimens from Central France. Specimens of obsidian, manganese containing silver and native quicksilver, from Mexico. Remains of fossil fishes from Goldworth Hill, near Guildford. Fossils from Bognor. Trilobites, corals, and rock specimens from Hudson’s Bay. Specimens from St. Helena. Fossils from the chalk of Berkshire. Shells from the crag of Felixstow. Geological specimens from Columbia River and other parts of North America. Specimens from Gibraltar, and minerals from Cornwall. Fossil infusoria and artificial and natural silica from recent infusoria, and glass, manufactured from living infusoria. The collection of minerals, fossils, and geological speci- mens belonging to the late Nathaniel John Winch, Esq., Hon. Mem. G.S. Fossils from the lower green-sand. Belemnites from Mount Joli. Fossils of the mountain limestone from Kirby Lonsdale and Clitheroe. Specimens of fish-scales in flint. Specimens from Underbarrow, near Kendal. . Cast of bones of reptiles discovered by Dr. Mantell in Tilgate Forest. Fossil Pinnas from Honey Pen Hill, near Bristol. DONORS, - L. L. Ibbetson, Esq., F.G.S. J. Harrison, Esq. Sir T. D. Acland, Bart., F.G.S. John MacClelland, Esq. Marquis of Northampton, F.G.S. Charles Dawes, Esq. Sir P. G. Egerton, Bart., M.P., F.G.S. Robert Cole, Esq., F.G.S. — Hodges, Esq. Rev. John PyeSmith, D.D., F.G.S. G. P. Scrope, Esq., M.P., F.G.S. John Taylor, Esq., Treas. G.S. Allan Sibthorpe, Esq. James Laird, M.D. The Earl of Selkirk. R. F. Seale, Esq., F.G.S. R. Grantham, Esq., F.G.S. Rev. Belford Dennys. Earl of Selkirk. Capt. Beaufort, R.N., F.G.S. Prof, Ehrenberg. Bequeathed by the late N.J. Winch, Esq., Hon. Mem. G.S. Dr. Mantell, F.G.S. John Vincent, Esq. Rev. J. W. Fisher, F.G.S. Dr. Reade. Gilpin Gorst, Esq., F.G.S. Dr. Mantell, F.G.S. G. Cumberland, jun. Esq. List of Donations. 1838. SPECIMENS. DONORS. Nov. 17. New red sandstone from Birkswell, Warwickshire. R. I. Murchison, Esq., \, V.2.G:S; Cast of the jaw of a Cheeropotamus. Rev. W. D. Fox. Fossil turtle, from Harwich. S. R. Heseltine, Esq. Gryphea sinuata, from the lower green-sand. Mr. Binsted. Casts of Calymene Blumenbachi, Asaphus caudatus, and Encrinites moniliformis. Mr. Deck, F.G.S. Specimens from Christiana. Rev. W. Bilton, F.G.S. Specimens from Western Africa, between Sierra Leone and Fernando Po, collected by Capt. Vidal, R.N. Capt. Beaufort, R.N., Hon. Mem. G.S. Dec. 20. An Index Geological Map of the British Isles, by John Phillips, Esq., F.G.S. J.W. Lowry Esq. 1839. Jan. 9. Specimens from the Island of Ascension, collected by Lieut. Bedford, R.N. RarsGacdocs Seance Specimens of chalcedonic flints from Wiltshire. Rev. Charles Watkins. 28. Specimens from Lisbon. W. Edward Logan, Esq., F.G.S. 27. Specimens from Southern Africa and the Cape de Verde Islands. Lieut. Nelson, R.E. Specimen of limestone from Bermuda, inclosing a Cyprea vitellus. Lieut. Symonds, R.E. Feb. 26. Bones from the crag of Easton and Bulchamp Pit, Suf- folk. Capt. Alexander, F.G.S. Corals from the mountain limestone of Lough Erne. ' Viscount Cole,M.P.,F.G.S. Mar. 18. A specimen of polished agate from Constantinople. Edw. Clark, Esq., F.G.S. Plants from the Pembrokeshire coal-field. Henry Still, Esq., F.G.S. Minerals from Nova Scotia. Abraham Gesner, Esq. 27. Casts of Echini and shells. Professor Agassiz. Fossils from the lias near Cheltenham. R. B. Grantham, Esq., F.G.S. A polished specimen of Spongus labyrinthus in flint, from Marquis of Northampton, . Sussex. F.G.S. i Section of an Alcyonite in flint. Rev. Charles Watkins. 4 Apr. 10. A collection of fossil shells from the Apennines. Sig. Michellotti. | 15. Impression in tin-foil of Nereites Cambrensis. Rev. J. B. Reade. Shells from the recent deposit on the banks of the St. Lawrence. Cha. Lyell, Esq., V.P.G.S. Fossils from the Ludlow formation near Ludlow. Rev. W. R. Evans. Shells from the Pampas of Buenos Ayres. Sir Woodbine Parish, i K.C.H., F.G.S. Fossils from the London clay. N.T. Wetherell,Esq.,F.G.S. May 22. A slab of new red sandstone from Eaton, Cheshire, with Sir Philip Egerton, Bart., ripple marksand impressions of Cheirotherium footsteps. M.P., F.G.S. 1839. May 22. A collection of fossils from the south of Ireland. June 5. 1835. June 23. 1836. Apr. 19: 1837. Mar. 21. 9. fe May June 1. Slab with impressions of plants from Philadelphia, and fossils from Cornwall. Fishes from the old red sandstone of the counties of List of Donations. Murray, Nairn, Inverness, and Banff. Casts of Ammonites Hensloni. 1V. Miscellaneous. MISCELLANEOUS. A specimen basket. Bust of the late Professor Playfair. Two specimens of an artificial substance resembling shell. Geological model of the Isle of Wight. Geological intersector by Prof. John Phillips, F.G.S. Cinder from a burnt hay stack. Roman coin-mould found at Lingwell Gate, near Wake- field, containing infusoria. Bust of Dr. William Smith. Model of Clare Island, on the Coast of Mayo, Ireland. Two Denarii of Geta and Antoninus Pius. H R. Griffith, Esq., F.G.S. Dr. Mantell, F.G.S. J. G. Malcolmson, Esq., Rev. G. Gordon, and Wil- liam Staples, Esq. Mr. Deck, F.G.S. DONORS. Capt. Chapman, Roy. Art. Leonard Horner, Esq., F.G.S. J. W. Lowry, Esq. Prof. J. Phillips. Sir W. Parish, K.C.H., F.G.S, Rev. J. B. Reade. W.P. Hunter, Esq., F.G.S. William Bald, Esq., F.G,S, Mr. W. Tilt. ) a oe HU Ce et he aah hic i f otc Fe ek Cae AmB tANL he Hen Hn. okie bechanstieae é fy a o, ‘ ‘ ane Ae are is bavi ik sna ll i \ rey i ian Usby eb tvles ae to “dict Val i, ed VOaAR VA You Pi cr (hb Pvirebed reel te ea Woisaias! hp LHILviah eCoE RCDR, Latin Gag LO Te Dap ena MOT a) ONT Goa Poe nid cree . = - EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 6,7 and 8. Vertebre, natural size: p. 352. Fig. 9. Chevron bone, natural size: p. 353. %g. 10. Rib, natural size: p. 353. Fig. 11. Fragment of a coracoid: p. 354. Fig. A. represents part of the dental bone of Sawrodon lanciformis, magnified three times: fig. B. portion of the upper jaw and detached teeth of Sawrodon Leanus. They are both taken from the plate which illustrates Dr. Hay’s Memoir on the Saurodon. Amer. Phil. Trans., New Series, Vol. iii. p. 471. Pl. XVI. Pirate XXX.: p. 354. Fig. 1 to 6 reduced to one-half, Fig. 7 to 12, natural size. Fig. 1, la. Humerus: p. 354. Fig. 2. Radius: p. 354. Fig. 3, 4, 4a. Femurs: p. 355. Fig. 5. An Ischium: p..355. Fig. 6. A Tibia: p. 356. Fig. 7, 7a. A Fibula: p. 356. Fig. 8 to 13. Metacarpal or Metatarsal bones and uncial Phalanges : p. 356. PLATE XXXI. Illustrates the Rev. W. B. Clarke’s paper on the Geological Structure and Phenomena of the county of Suffolk, &c.: p. 359. WOOD-CUTS To illustrate Mr. Strickland’s paper on the Geology of the Thracian Bosphorus: p. 385. Section from Constantinople to Symplegades : p. 385. Section of a conglomerate near Filbornou, consisting of angular fragments of trachyte, imbedded ina tufaceous paste and traversed by veins of calcedony : p. 389. Section on the north side of Anadoli-fanar: p. 392. PLATE XXXII. Map and Sections to illustrate Mr. Strickland’s Memoir on the Geology of the neigh- bourhood of Smyrna: p. 390. PLATE XXXII. Map and Sections illustrative of Mr. Strickland’s paper on the Geology of Zante : p- 403. PLATE XXXIV. To illustrate Mr. James de Carle Sowerby’s paper on Crioceratites Bowerbankii and Scaphites gigas: p. 409. Fig. 1. Crioceratites Bowerbankii : p. 410. Fig. 2. Scaphites gigas: p. All. EXPLANATION OF THE PLATES AND WOOD-CUTS. PLATES XXXV. to XLI. Illustrate Mr. Prestwich’s Memoir on Coalbrook Dale: p. 413. _Priate XXXV. Map on the scale of one inch to a mile, the topography being copied from the Ordnance Map. Pirate XXXVI. Sections, horizontal scale 2 inches to a mile. Fig. 1. Longitudinal section from the Wharf, near Lilleshall Hill, at the northern ex- tremity of the coal-field, to Shirlot Hill. %g. 2. Transverse section through Lilleshall Hill. Fig. 3. West and east section through Donnington Field. Fig. 4. Transverse section from a little south of Hadley to Woodhouse Hill. Fig. 5. West and east section from Buckatree Hall to the Great East Fault. Fig. 6. West and east section from Wrekin Farm to Randley. Fig. 7. West and east section from a little west of Primrose Hill to Brans Farm. Fig. 8. West and east section from the Devil's Dingle to near Homer Farm. Fig. 9. Transverse section from a little south of Coalbrook Dale to Sutton Hill. Fig. 10. Transverse section from a little west of Benthall Edge to a little south of Sutton Maddock. Fig. 11. West and east section from Wenlock Edge to Old Park. Fig. 12. West and east section from Westwood Common to Apley Park. Fig. 13. Diagonal section from N.N.W. to S.S.E., or from Cluddley to Dunvall. Fig. 14. North and south section from near Hadley to a little south of Willey. Fig. 15. N.N.W. and 8.S.E. section through the Wrekin to the Severn. Fig. 16. West and east section from Henley Farm to Pendlestone Rock. PuateE XXXVI. Diagram illustrative of the principal coal-shafts in their range from north to south, of the changes in the mineral composition, thickness and number of the beds; also of the nature and distribution of the organic remains. The vertical scale is to the horizontal in the proportion of about 26 to 1, in order to represent every bed. Pirate XXXVIII. Fossil Plants from the coal-measures described by Mr. John Morris and engraved hy Mr. James de Carle Sowerby. Fig. 1. Halonia disticha, n. s. Length of specimen 4 feet ; width from 4 to 6 inches. Stems and leayes unknown. EXPLANATION OF THE PLATES AND WOOD.-CUTS. Stem? internal structure unknown, replaced by sandstone. wd Ig. External structure; stem flattened, sinuous, with bifarious ascending protube- rances, somewhat conical and obliquely truncated, the apex of each forming a nearly circular scar, with a depressed lateral cavity ; the side of each scar marked by a transverse depression; surface of the stem thickly covered with small oblong or irregular shaped projecting cicatrices, disposed in a quincunxial order, which become elongated and larger as they approach the protuberances. In the older portions the cicatrices are less prominent. The resemblance of this specimen in some characters to Halonia has induced us to place it in that genus; although it differs in the smaller number of protube- rances which are found on the surface, the bifarious position of which will at once distinguish it from all the other species. 2. Bechera chareformis, (Sternberg, t. 55, f. 3, 5.) B. delicatula®? Sternb. t. awe 49. f. 2. Stem striated, jointed, verticillately branched, branches dichotomously whorled, leaves subulate. This specimen is the same as Sternberg’s figure, t. 55, and his B. delicatula ap- pears to be only an imperfect variety of the same species. g. 3. Stigmaria ficoides. 'The portion of stem of which the figure is a transverse section, is in more perfect preservation than the specimens of S¢tigmaria usually are found ; it is of a nearly cylindrical form, about 44 inches diameter, the exter- nal surface exhibiting the usual markings of this curious plant; the internal part, with the exception of a vascular cylinder (also mineralized), being replaced by clay ironstone. In the Fossil Flora, t. 31—36, are figures and descriptions of St¢gmaria_ficoides, and at t. 156 is shown the structure of the same; and although we cannot add much new information to that previously given by Prof. Lindley, it has been thought advisable to have another section represented with a view of showing what has hitherto not been well illustrated in the published figures of its structure. The internal cylinder in the specimen (fig. 3.) is eccentric, and consists of wedge- like portions of vascular tissue, the rounded origin of which, internally, is well- defined ; these wedges are generally of equal or nearly equal size, but they occa- sionally become confluent by the joining of two or more of them together. The form of the space necessarily left, or interstices between the sections where these are distinct, varies a little, in some cases being of nearly equal breadth through- out, and in others becoming narrower outwards and appearing to terminate or contract about the middle of the vascular tissue, beyond which they again fre- quently widen outwards: these spaces often contain portions of oblique and smaller vascular cords, apparently arising at different depths in the vertical cylinder; the origin and connexion of which with the cylinder is shown in the oblique section, where a single series of vessels is seen passing from it surrounded by tissue of smaller diameter. Pl. XX XVIII. fig. 8 a. In no specimen yet examined has the course of the oblique cords been abso- lutely ascertained, but there can scarcely be any doubt, as suggested by Mr. Brown (to whom we are also indebted for the above observations,) that these vessels after 3 EXPLANATION OF THE PLATES AND WOOD-CUTS. arising from the cylinder passed to the tubercles of the surface, through the thick cellular tissue which once probably occupied the larger space in the original plant. ‘The discovery of these smaller oblique vessels is an interesting feature in the ana- tomy of Stigmaria; and they have also been pointed out by Mr. Brown as ex- isting in Anabathra, and one of these is actually figured by Mr. Witham in his work!, but considered by him (p. 41.) as a section of a medullary ray. ‘The ana- logous vessels existing in Lepidodendron Harcourtiz, as figured by Mr. Witham’, appear to arise from the outer part of the vascular cylinder. A somewhat simi- lar arrangement is also found in that division of Lycopodiacee, consisting of Psilo- tum and Tmesipteris : in those genera, the vascular eplnden, from which the oblique cords proceed, includes a central pith °. Fig.3b. Shows that the vessels are much smaller at the internal rounded portions of the wedges. Fig. 3c. Exhibits the oblique cords, consisting of smaller vessels surrounding vessels of larger diameter nearly equal to those forming the vertical tissue. Fig. 3a. Is an oblique section which exhibits the connexion of these vascular cords with the vertical tissue. Stigmaria melocactoides, Sternberg, Flor. der Vorw. p. 38. Stem deformed, 6 to 8 inches thick, with the apex rounded, pertuse, and filled with sandstone; leaves unknown, cicatrices like S. ficoides. This I believe may prove to be a terminal portion of S. ficoides. Sternberg considers Phytolithus verrucosus of Steinhauer, Martin, and Parkin- son as a synonym of this species ; but it rather appears to be only a terminal por- tion of S. ficoides. Fig. 4. Carpolites Zamioides, n.s. ‘The figure is somewhat similar to the Bothreden- dron punctatum, Fossil Flora, t. 218, and which is considered to have been a cone ; an opinion that can scarcely be entertained of our specimen; the ovate and com- pressed form of which is more analogous to the seed of some species of Zamia or even Palms. Fig. 12. Carpolites Helicteroides, n.s. Fruit ovato-lanceolate, attenuate at both ends ; polycarpous?, Carpella 4 or 5, twisted spirally but not closely together. The apparent resemblance of this specimen to the cast of a fruit of Helicteres has suggested the specific name, although its affinity to that genus may be very doubtful. The above name was given to the specimen figured previously to our having een a somewhat similar fossil described by Presl in the last part of Sternberg’s Flora der Vorwelt, where it is placed under the genus Paleoxyris of Brongniart, from its supposed resemblance to the inflorescence of the recent Xyris, an opinion scarcely borne out by the general appearance of this fossil; it has therefore been retained under Carpolites for the reason stated above. The two species already » On the Internal Structure of Fossil Vegetables, 2nd Edit. t. 8, f. 12. * Trans. of the Nat. Hist. Soc. of Newcastle, 1832. * Ad. Brongniart, Hist. des Végét. Foss. v. ii. p. 44, 45. EXPLANATION OF THE PLATES AND WOOD.-CUTS. figured of this remarkable form have been obtained from the new red sandstone of Bamberg. 3 Fig. 5. Antholites anomalus, n.s. Flower spiked, more crowded towards the apex, calyx apparently shorter than the petals ?, furnished with a small lanceolate bract ; stigma or Carpella? bilocular, elevated upon a long curved filament. The absence of more defined characters renders the affinity of this plant doubt- ful. It has some resemblance to the flowers of Orobanche or even Scitaminee as Hedychium, which have, however, large fleshy bracts. In the Bromeliacee are flowers of a somewhat similar shape, but they are not furnished with the long filamentous appendage which appears to be characteristic of this fossil. The genus Lacis has a two-celled Carpella upon a long pedicle, but the flowers are rather different from our specimen. Cyclopteris semiflabelliformis, ns. Pl. XX XVIII. fig. 7. Frond pinnate?, leaves entire, half-fanshaped ; veins distant, diverging, dichotomously furcate. This specimen has some affinity to the leaf of Salisburia adiantifolia, but differs from it in the veins being more numerous and more generally furcate along the up- per margin, which is entire and not deeply cleft as in Salisburia. It more closely resembles the lower leaves of Otopteris acuminata, var. brevifolia, Foss. Flor. t. 208. Lycopodites? longibracteatus, n.s. Pl. XXXVIII. fig. 8, 9, 10, 11. Stem round, marked by the cicatrices of the fallen leaves, which are close, lozenge-shaped, and spirally disposed. Fructification in terminal imbricated spikes, thecze reniform, minutely tubercu- lated, each attached by its centre to the base of a long, lanceolate, foliaceous bractea. The thecz resemble in shape those of the recent genus Stachygynandrum, but as the capsules vary in form in different parts of the spike in that genus, it is difficult to assign its affinity to that division of the Lycopodiacee. The capsules, Pl. XXXVIII. fig. 8, 8 a. of this species, neither bituminized nor mineralized, but in a state of brown vegetable matter, are very abundant in some of the coarser sandstones of the coal-measures. Puates XX XIX. and XL. Fossil shells from the coal-measures described and engraved by Mr. James de Carle Sowerby, F.L.S. Tig. 1. Donax® suleata. Subtriangular, convex; anterior side rounded ; posterior Fig. side produced, pointed ; beaks prominent ; in the cast there is a furrow descending obliquely from each beak towards the posterior angle. Length in some specimens 1 inch 4 lines ; width 13 inch. The name of this fossil is but temporary, neither the structure of the hinge nor the external surface being known. 2. Venus? carbonaria. Obovate, convex ; anterior side rounded ; the posterior side truncated, squarish ; beaks rather prominent; shell most gibbose towards the beaks. EXPLANATION OF THE PLATES AND WOOD-CUTS. Length | inch 4 lines, width 1} inch. These casts have much the aspect of Mactre; the hinge is unknown. Fig. 3. Nucula equalis. ‘Transversely elongated, convex, marked with concentric ridges ; anterior side rounded; posterior separated by a ridge and truncated ; beaks nearest the anterior side. Width twice the length, which is a quarter of an inch; 3a. is 3 b. magnified twice. Fig. 4. Nucula accipiens. Transversely oval, convex, concentrically striated ; beaks nearest the anterior side. : Length 3} lines, width above 4 lines. Fig. 5. Nucula acuta. 'Transversely ovate, convex, concentrically striated, anterior extremity rounded, posterior extremity produced, pointed. Length 1} line, width 23 lines; 5a. is 5 b. magnified twice. An elegant small shell. Fig. 6. Unio Urii, (Fleming’s British Animals, 417. Ure’s History of Rutherglen and Kilbride, 311. t. 16. f.4.). Transversely much elongated, very convex, wavy; posterior extremity rather pointed ; beaks near the small anterior side. The general form approaches to cylindrical. Width 23 times the length, which is about 1+ inch. Fleming has confounded this with Unio ovalis of Martin (Petrif. Derb. t. xxvii. f. 1, 2.) which is quite distinct. Fig. 7. Unio Ansticet. Very convex, wavy, curved, anterior side longest, forming a lobe ; posterior side obtuse, gaping? Surface concave towards the front; beaks near the anterior extremity. 7a. Reduced figure to show the front of the shell. Length 12 inch, width 2% inches. This has much the form of a Mya. Fig. 8. Unio parallelus. 'Transversely elongated, rather flattened, wavy; sides almost equally rounded; front and back straight, parallel; beaks near the anterior ex- tremity. 8a. Shows the depth of the valves. Length 1 inch 4 lines, width 21 inches. Fig. 9. Unio dolabratus. Subquadrate, wider than long, rather flat with an oblique convexity along the middle, even ; anterior side small, rounded ; the posterior side flattened and truncated ; beaks near the anterior side. Length id lines, width about 13 inch. Fig. 10. Unio modiolaris. 'Transversely elongated, convex, even, with an oblique obtuse keel along the middle; anterior side small, rounded ; the posterior trun- cated, flattened ; beaks near the anterior side. Length $ inch, width about twice as much, Fig. 11. Unio Phaseolus. _'Transversely much elongated, three times as wide as long, even, convex ; anterior side very small, pointed ; the posterior flattened, rounded, Length 3 lines, width 7 lines. Fig. 12. Unio aquilinus. 'Transversely ovate, curved, flattened, rugged; posterior side pointed; beaks near the rounded anterior side, Length half the width, which is 14 lines, EXPLANATION OF THE PLATES AND WOOD.-CUTS. Fig. 13. Unio centralis. Transversely oval, rather convex ; beaks nearly central. Length 11 lines, width 17 lines. Fig. 14, Unio robustus. Obovate, convex, strongly marked wih lines of growth, nearly as long as wide ; posterior extremity rather pointed. Length | inch 5 lines, width nearly 13 inch. Fig. 15. Modiola carinata. Obliquely aaeaea: valves boat-shaped, deep; anterior lobe small. Length 11 lines, width more than } an inch. Tig. 16. Mytilus triangularis. Triangular, with a rounded front, rather flattened, keeled towards the beaks. Length 11 lines, width about 93 lines. Fig.17. Avicula quadrata. Quadrangular, convex, keeled; anterior lobe small, pointed ; front rounded. Length about an inch, width nearly the same. Fig. 18. Avicula modiolaris. Obliquely elongated, compressed ; keeled towards the beaks ; anterior lobe pointed. =: Length 8 lines, width 4} lines. Fig. 19. Pecten gentilis, Oblong, convex, smooth, with 15 slightly-elevated rays, which are alternately long and short ; ears middle-sized, equal. Length 5 lines, width 5 lines. A small neat shell. tg. 20. Pecten scalaris. Oblong, convex, concentrically striated, radiated, radii about 15, acute. Length 6 lines, width 5 lines. Fig. 21. Spirifera bisuleata, (M.C. t. 494.) This specimen shows the impressions of the internal spiral appendages, which, together with the long hinge-line, charac- terize the genus Spirifera. Fig. 22. Globulus vetusius. Globose, smooth ; spire pointed ; umbilicus very small, open. Height 11 lines, diameter 9 lines. Fig. 23. Littorina? obscura. Oblong, umbilicated? smooth? spire elevated ; whorls rather flattened on the sides. Height 14 lines, diameter 10 lines. The specimens are imperfect casts ; they resemble the L. itorea: but are more elongated and have the whorls more distinct. Tig. 24. Turritella? clavata. 'Turreted, conical, smooth; whorls about 8, flat. Height 10 lines, diameter 5 lines. This being only part of a cast, the genus cannot be ascertained with certainty. Fig. 25. Turritella? minima. 'Turreted, conical, ribbed; ribs obtuse, about 16 to each whorl; whorls about 10. Height 7 lines, diameter 23 lines. Tig. 26. Polyphemus? fusiformis. Fusiform, smooth ; aperture half the length of the shell, narrow; columella curved ? Height about 24 inches, diameter above an inch. EXPLANATION OF THE PLATES AND WOOD.-CUTS. This is the internal cast of a shell of a very unusual form,—we have referred it to Montfort’s genus Polyphemus, as bearing the nearest resemblance to it of any we know. ‘he curvature is possibly the effect of fracture. Priate XL. Fig. 1. Trochus? Usocona. Conical, with a broad base, marked with obscure concen- Fig. 71g. Fig. tric ridges; whorls about 5, their upper parts convex, the lower concave, with a broad band in the hollow; edge of the base obtuse. Height 2 inches, diameter nearly 3 inches. The broad band around this shell would lead us to place it as a Plewrotomaria, did the lines of growth indicate that there ever was a deep sinus in the edge of the aperture. 2. Conularia quadrisulcata, (M.C. t. 260. f. 3—6. Silur. Syst. p. 626. PI. XII. f.) Many of the specimens in ironstone have smooth furrows between the crenated ridges, as shown at fig. 2 a., in others the furrows are crossed by stria, as at fig. 2b., and both these forms may sometimes be found in one specimen, and arise from the presence or absence of a thin, dark brown skin or covering, the interior of which is smooth and the exterior wrinkled ; the ridges are often denticulated or notched. See ante, p. 442. 3. Orthoceras scalpratum. Lanceolate, compressed, smooth, slightly curved, with the edges angular, the inner one sharp; septa numerous; siphuncle small, near the obtuse edge. Diameter 14 inch. *. 4, Represents the interior of a small Orthoceras with numerous septa, and a nearly marginal siphuncle. 5. 5a.and 5b. Nautilus clitellarius. Globose, umbilicated, septa numerous, much bent in the middle, truncated and not recurved at the ends; siphuncle central ; umbilicus small, cylindrical; aperture above twice as wide as long. The length of the aperture is 14 inch, the width 23 inches. Diameter of the shell 23 inches. Fig.5. A front view of a specimen in which only a few chambers have been filled with ironstone, and it may be remarked that most of the specimens are preserved in the same manner. The whole of the shell has decayed away, and with it all the inner whorls have disappeared : the ironstone not having entered them, that por- tion of the ironstone which fiJled the umbilicus wanting support has been subse- quently broken and pressed into the cavity left by the shell. Fig. 5a. is a lateral view of a similar specimen, Fig. 5 b, shows the remarkable curvature of the septa. 6. Nautilus concavus. Subglobose, umbilicated, concave on the front; septa slightly arched; siphuncle central; umbilicus large; aperture nearly twice as wide as long. Length of the aperture 7 lines, width 1 inch, Diameter of the shell 1 inch 4 lines, EXPLANATION OF THE PLATES AND WOOD.-CUTS. The simple curve of the septa and concave front distinguish this Nautilus. Fig. 7. Nautilus subsuleatus, vay. (N. subsuleatus, Phill. Geol, Yorks. ii. 233, in part.) This appears to be the same species as the limestone specimen figured by Prof. Phillips ; but as it has a shorter aperture, we have thought best to distinguish it as a variety. That author refers to Coalbrook Dale as one of the localities of his species, so probably he had seen the shell before us. Fig. 8. Nautilus armatus. Discoid, strongly ribbed, ribs elevated into tubercles ; septa numerous. Diameter of the shell about 23 inches. There is only just enough preserved of this shell to show that the septa are en- tire, and that the ribs almost form spines; it much resembles Ammonites armatus of the Lias. Fig. 9. Nautilus faleatus. Discoid, inner whorls exposed ; the front convex; sides nearly flat; the outer edge of each whorl obtusely angular, the inner edge inclined towards the preceding whorl, the space between crossed by many arched ribs; septa simply concave; siphuncle central; aperture nearly square, but 6-sided, with two of the sides very small. Length of the aperture 1 inch. Diameter of the shell about 2§ inches. Fig. 10. Bellerophon hiulcus, var. (B. hiuleus, Fleming’s British Animals, 338.) This differs from the specimens found in the mountain-limestone (M.C. t. 470. f. 1.), in having indistinct concentric strize crossing those which are parallel to the lines of growth, and in all the strize being sharper. Fig. 11. Bellerophon Navicula. Globose, expanded, keeled, and flattened on each side of the keel, smooth; columella solid, produced ; whorls rapidly increasing. Diameter 53 lines. The form of the aperture resembles the section of a boat, whence the name. Puate XLI. Remains of insects and fishes: p. 440. Engraved by Mr. James de Carle Sowerby. Fig. 1 to 4. Limulus anthrax. This fossil is considered by Dr. Milne Edwards to be a new species of Limulus. Fig. | represents a nearly perfect specimen, with two of the legs extending from under the body: in figures 2 and 3 the shield is believed to have been separated ; but Dr. Milne Edwards states that it is difficult to account for the three short horns exhibited by each specimen: figure 4 is a detached shield. Fig. 5 to 7. Limulus rotundatus. ‘This fossil is also considered by Dr. Milne Edwards to be a new species of Limulus. Fig. 6 is the counterpart of figure 5. The membrane connecting the spines, and the circular outline of the animal, are considered to be peculiar. Fig. 8. Limulus trilobitoides. (Buckland.) Fig. 9. Apus dubius. 'The only living animal to which Dr. Milne Edwards could refer 1 EXPLANATION OF THE PLATES AND WOOD-CUTS. this specimen is the Apus corniformis, of the rivers of central and southern Eu- rope. The remains represented in figures 1 to 7 are considered by Dr. Milne Edwards of great interest, as they exhibit characters intermediate between the living Limulus and the extinct Trilobite. Fig. 10 and 11. Bones of the head of a Megalichthys. (See ante, p. 443.) Fig. 12, a tooth, and fig. 13, a spine, are assigned provisionally to the genus Hybodus ; the characters of the allied coal-measure genus Diplodus not being yet published by M. Agassiz. Fig. 14. A tooth of a Cochliodus. Fig. 15. A spine, assigned with doubts to the genus Pleuracanthus, the state of preservation of the specimen not being good. ‘The spine is round but com- pressed, and is armed with two opposite rows of teeth. There are no traces in the specimen of the groove mentioned by M. Agassiz as one of the distinguishing characters of the genus. WOOD-CUTS. Fig. 1 to 4. Diagrams of the effects of faults in the coal-measures: p. 453. Fig. 5. Diagram of the effects of lateral pressure produced by faults, from the Holy- well pits, Malinslee: p. 454. Fig. 6. Section of changes of level produced by dislocation in the “ best coal” Mea- dow pits, Madeley: p. 454. Fig. 7. Diagram of a step-like dislocation at Priorslee, due apparently to unequal hardness in the strata: p. 454. Fig. 8 to 10. Diagrams of complicated dislocations: p. 454. Fig. 11. Plan of minor faults and fractures inclosed between two principal faults, the Boundary and Ketley: p. 455. Diagram of the minor faults which flank the Ketley fault near Donnington Wood fur- naces: p. 456. WOOD-CUTS To illustrate the notice of Capt. Cautley and Dr. Falconer on the remains of a Fossil Monkey from the Sevalik Hills: pp. 499-501. Fig. 1 and 3. The Fossil Astragalus, natural size. Fig. 2 and 4. Astragalus of the Semnopithecus Entellus, natural size. WOOD-CUT Explanatory of Mr. Darwin’s paper on the Formation of Mould: pp. 505, 506. EXPLANATION OF THE PLATES AND WOOD-CUTS. PLATE XLII. Illustrates Mr. Owen’s paper on the Dislocation of the Tail at a certain point, observ- able in the Skeleton of many Ichthyosauri: p. 511. All the tails represented in the accompanying plate belong to skeletons of Ich- thyosaurt now in London and formerly in the collection of Mr. Hawkins: and these illustrations will not lose force from the fact of their being taken from figures of those skeletons published without any reference to the structure or hypothesis in question. Upper right-hand figure from a specimen found in the lias at Walton in Somer- setshire. (See Mr. Hawkins’s work on Ichthyosauri and Plesiosauri: p. 32. PI. XVII.) Lower right-hand figure, from a specimen found in lias at Lyme Regis. (See Mr. Hawkins’s work, p. 25. Pl. VII.) cree ae ene See the Second Part of Mr. Hawkins’s work. Left-hand lower figure from a specimen found in lias at Walton in Somersetshire. (See Mr. Hawkins’s work, p. 34. Pl. X XI.) PLATES XLIII. to XLV. Illustrate Mr. Owen’s memoir on the Specimen of Plesiosawrus Macrocephalus (Cony- beare) in the collection of Viscount Cole: p. 515. Pirate XLII. Reduced figure of Lord Cole’s specimen, with comparative outline sketches of the paddles of Plestosaurus Dolichodeirus and P. Hawkinsii: p. 515, et seq. Prats XLIV.: p. 518. Fig. 1. Diagram of vertebral elements: p. 518. Fig. 2. Caudal vertebra of a Python: p. 518. Fig. 3. Cervical vertebra of a Pelican: p. 518. Fig. 4. Cervical vertebra of Plesiosaurus Hawkinsii, natural size : p- 523, Fig. 5. Cervical vertebra of Plestosaurus arcuatus, natural size. Fig. 6. Section of terminal caudal vertebrae of Plesiosaurus: p. 528. Prave XLV.: p. o3l. Head of Plestosaurus Hawkinsii and of Plesiosaurus Maerocephalus. PLATES XLVI. and XLVII. Illustrate Mr. Malcolmson’s memoir on the Eastern Portion of the Great Basaltic Di- strict of India: p. 537, 2 Vv EXPLANATION OF THE PLATES AND WOOD.-CUTS. Prate XLVI. Map and Sections. The Map is intended only to assist the reader in following the description con- tained in the paper, and to exhibit a general view of the distribution of the rocks occurring between the Taptee and Pennar rivers. However imperfect this slight sketch confessedly is, it is hoped, that by embracing almost all the information yet obtained respecting this extensive region, it will correct the erroneous opinion en- tertained by many, of the simplicity of the geological structure of the South of India, and afford a nucleus around which additional and connected observations may be gradually arranged. It has been found impossible to employ more than two colours for granite, gneiss and mica, chlorite and hornblende schists ; for although many good obser- vations have been made on the distribution of these rocks in certain parts of the country, yet the boundaries have not, in general, been clearly distinguished, nor is it always easy to do so. Where the stratified primary rocks prevail more abun- dantly than granite, a purple tint has been employed. The Diamond sandstone and argillaceous limestone appear to constitute parts of one formation, and it has therefore been thought better not to distinguish them in a map of such small dimensions; though an attempt to do so has been made in the sections. The laterite is introduced only where it occurs resting on basalt, at Beeder in the Deccan; its limits are unknown. Near Nellone, a nearly similar formation rests on the primary rocks, and is probably formed from their decomposition én situ. The trap is represented the same colour as in illustrations to Col. Sykes’s Memoir on the Deccan, (Vol. iv. Pl. XX VI.) to enable the reader to connect the district represented in Col. Sykes’s map with that contained in the accompa- nying map. The section, fig. 1, at the top of the plate, extends from Bundlecund, beyond the north boundary of the map, to the Bangnapilly diamond-mines, situated be- tween the 15th and 16th degrees of north latitude. Section, fig. 2, extends across the Peninsula from the coast near Atchera (lat. about 16°) to Madras. Pirate XLVII. Organic remains collected by Mr. Malcolmson, and described and engraved by Mr. James de Carle Sowerby: p. 550. Fig. 1. Chara Malcolmsonii. Oblong, spheroidal, with 10 ribs; three of the ribs are produced at the apex. Natural size and magnified. This capsule is composed of 5 tubes, each of which is curled twice round. The figures represent a cast of the interior, the tubes being split down, and the outer halves broken away and left in the chert. The specimens are silicified and consti- tute almost the entire mass of the rock, in which they occur associated with Physe and Paludine. EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 2. Cypris cylindrica. Twice as wide as long, almost cylindrical; front very slightly concave; the outer surface, which is very rarely obtained, is punctured. Fig. 3. Cypris subglobosa. Subglobose, triangular, inflated ; front concave. The outer surface of this Crustacean is punctured as in C. cylindrica. Both species occur abundantly in grey chert, with the Unio Deccanensis and other shells; and in various specimens of chert and indurated clay containing Gy- rogonites, Paludine, Physe, and Limnei, from the Sichel hills. The fossils are converted into calcedony. Fig. 4 to 10. Unio Deccanensis. Transversely oblong, rather compressed ;_ margin internally waved ; shell very thick ; surface finely striated. Fig. 6 is in limestone from the northern descent of the Sichel hills; the others are in chert from Munnoor. Natural size. This species has often a ridge, which bounds the posterior portion, and is vari- able in size and elevation; it is most conspicuous in the limestone specimen, fig. 6, and in a cast in chert from Munnoor, fig. 7. Fig. 8 is possibly a very young indivi- dual, before the margin had assumed its wavy form. Fig.9 is from a part of a group of many individuals of nearly one size, badly preserved in the same lime- stone as fig. 6; but as they are regularly oval, and do not show a waved margin, they may belong, as well as fig. 10, which is in grey chert from Munnoor, to a species distinct from U. Deccanensis. Some flattened specimens from this lime- stone are 24 inches broad. Fig. 11 and 12. Unio tumida. 'Transversely obovate, smooth, gibbose; posterior ex- tremity rather pointed ; beaks near the anterior rounded extremity. Natural size. The section of the two valves united is regularly heart-shaped. The shell is rather thin, and it has something of the contour of Cyrena. It occurs in the same limestone with fig. 6, and the substance of the shell is replaced by cal- careous spar, which cannot be broken so as to show the hinge. Fig. 13. Limnea subulata. Subulate, elongated, smooth ; spine equal in length to the body; whorls five. In a nearly white, soft, siliceous stone, from Munnoor and Chicknee. Natural size. Fig. 14, 15 and 16. Physa Prinsepit*. Ovate, rather elongated, smooth, spire short ; body-whorl largest upwards. Fig. 16, in a soft siliceous stone from Munnoor. Fig. 14 in chert from Munnoor, and fig. 15 in chert from Chicknee ; the drawing re- presents the shell as wider than it is. Many of the specimens are crushed. The largest, fig. 15, are 2} inches long and upwards of an inch broad. Natural size. Fig. 17 to 19. Melania quadri-lineata. Subulate, whorls about eight, with four striz upon each; aperture nearly round. Fig. 17, in grey limestone from the same lo- cality as 6 and 11. Fig. 18, in softish chert from Chicknee, associated with Physa Prinsepi. Fig. 19, in fine reddish grey chert, protruding from basalt near Munnoor, appears rather shorter in form than the others, but the spine is not perfectly exposed nor entire. Natural size. * Mr. Sowerby has, with much propriety, named this fossil after Mr. James Prinsep, F.R.S., and Secre- tary to the Asiatic Society of Bengal ; to whom Oriental science and literature are more indebted than to any other individual.—J. G. M. EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 20 to 28. Paludina Deccanensis. Short, conical, pointed, rounded at the base ; whorls 5 or 6, slightly convex, aperture round, Fig. 21 is in chert from Munnoor ; and figs. 20 and 22 in indurated clay from between Munnoor and Hutnoor, the cavity of the shells being filled with caleedony. The young shell has a slight carina shown in fig. 20. Fig. 23 appears to be a crushed specimen; it is in laminated, indurated clay, Munnoor. This shell occurs, with Physa Prinsepii, in a beautiful green siliceous mineral at Munnoor; at Chicknee, and at the bottom of the Neer- mull pass. All the specimens natural size. WOOD-CUTS. Section of the Bangnapilly Diamond Mines: p. 541. Section of the Lonar Lake and surrounding rocks: p. 562. WOOD-CUT. Map of part of Mazunderan to illustrate Dr. C. M. Bell’s Geological Notes of a Jour- ney from Tehran across the Elboorz Range to the Caspian, and back to Tehran along the course of the Heraz River: pp. 577, 581. PLATE XLVIII. Map and Sections to illustrate Mr. W. J. Hamilton’s memoir on part of Asia Minor between the Salt Lake of Kodj-hissar and Cesarea of Cappadocia. The map is constructed from original documents. The descriptions engraved on the plate explain sufficiently the range and nature of the Sections: p. 583 et seq. WOOD-CUT To illustrate Mr. Strickland’s notice of some remarkable Dikes of Calcareous Grit, at Ethie, in Ross-shire: pp. 599, 600. PLATE XLIX. Outline Map of part of the western coast of South America to illustrate Mr. Darwin’s memoir on the connexion of certain voleanic phenomena in South America; and on the formation of Mountain Chains and Volcanos, as the effect of the same Power by which Continents are elevated: p. 601 e¢ seq. WOOD-CUTS. Diagrams copied principally from Mr. Hopkin’s memoir on Researches in Physical Geology, (Trans. Phil. Soc. Cambridge, vol. vi. pp. 45, 51.) to illustrate slow ele- vatory movements in the formation of mountain-chains: p. 625. Diagram explanatory of the effect which would be produced if the thickness of the crust of the earth, upturned by elevatory movements, were equal to the distance between the anticlinal lines: p. 627. PLATES L. to LVIII. Illustrate Prof. Sedgwick and Mr. Murchison’s memoirs on the Physical Structure of Devonshire, and on the Subdivisions and Geological Relations of its older stra- tified deposits: p. 633 et seq. EXPLANATION OF THE PLATES AND WOOD-CUTS. Puates L. and LI. Map and Sections of Devonshire and Cornwall. Prates LII. to LVII. Organic remains engraved and described by Mr. James de Carle Sowerby. May, 1840. Pruate LII. (Fossils from Barnstaple.) Fig. 1. Posidonia (Bronn.) lateralis. Compressed, transversely elongate-ovate, con- centrically ridged; umbones very near the anterior extremity; ridges angular. Width about 23 times the length, which is 1$ inch. Loc. Venn Lime Quarry, near Barnstaple. Fig. 2 and 3. Posidonia Becheri. (Goldf. Petref. 119. t. exiii. f.6a@. Bronn. Leonh. Zeitsch. f. Mineralog. 1828, April, t. ii. f. 1—4:.) Compressed, ovate, concentrically ridged, and finely striated ; posterior slope straight ; ridges numerous; umbones nearest the anterior side. Width in pro- portion to the length as 7 to 4. Its length is about 13 inch. Fig. 3 is from a specimen with fewer ribs. Loc. Venn Quarry. Swimbridge Quarry. Fig. 4. Posidonia Becheri, var. (Goldf. loc. cit. f. 6 b. c.) Slightly convex, obovate, with the posterior extremity nearly square; concentrically ridged and finely striated ; umbones close to the anterior extremity. Width rather more than the length, which is nearly 14 inch. Loc. Venn Quarry. We have seen specimens of this shell from Herborn, near Dillenberg, and Schelke in Westphalia, where other species of the genus are also found. We can hardly believe this and the preceding to be the same species; but we yield to Goldfuss, who has had more specimens to examine than have come under our observation. Fig. 5. Posidonia tuberculata, Compressed, obovate, approaching orbicular, concen- trically ridged, and marked down the middle with three or four longitudinal ribs, which form more or less distinct tubercles as they cross the ridges. Length not 21 inches, and width full 2 inches. Loc. The specimen figured is from Buddle, near Bamborough. We have examined one from Devonshire, which has the tubercles much more strongly marked. Fig. 6 and 7. Orthoceras cylindraceum. A much elongated, smooth species, with ra- ther distant septa. The specimens are too imperfect to be positively identified ; the name must therefore be considered only as temporary. Loc. Vennand Swimbridge Quarries. Fig. 8 and 9. Goniatites carbonarius. Although we have seen many specimens of - EXPLANATION OF THE PLATES AND WOOD-CUTS. this shell, they have been mostly sections in various oblique directions, so that we have been unable to determine satisfactorily its shape or the form of its septa; all that we can ascertain is, that the general form of the shell is a depressed spheroid, with a large angular umbilicus, sinuated septa, and a smooth surface. It does not agree with any described by Count Munster. Loc. Venn Quarry ? Fig. 9 represents, upon the same mass with a specimen of G. carbonarius, two small individuals which resemble the G. stenolobus of Phillips, (Geol. of Yorkshire, Pl. XX. f. 7-9.) ; but they are still more globose, have a finely striated surface and a small umbilicus. Prate LIII. (Fossils from Barnstaple, Petherwin, Ilfracombe and Marwood.) Fig. 1 and 2. Pecten nexilis. Suborbicular, slightly convex, inequilateral, finely ra- diated ; ears large, nearly equal, that on the anterior side less distinctly radiated than the other ; ribs very numerous, elevated, smooth, and thin. A pretty species, of which we have seen only one or two specimens. Itoccurs with Leptena caperata (fig. 4) and several other shells in slate from New Ifracombe near Barnstaple, and Barnstaple. Fig. 2 is a magnified view of the same. Fig. 3. Pecten transversus. 'Transversely obovate, very slightly convex, radiated, radii in threes, crossed by numerous regular lines of growth; ears large and nearly equal. Length about 1 inch, width nearly 13 inch. The great width of this shell is a prominent feature. Loc. Barnstaple. Fig. 4. Leptena caperata. Half-elliptical, very convex, concentrically wrinkled, spi- nose, margin not much deflected ; one valve very convex, the other almost equally concave; hinge-line rather longer than the width of the shell; spines adpressed, those near the hinge-line very long. The concentric ruge are lost towards the centre of the shell. Loc. Abundant at Barnstaple and Petherwin; also in New Ilfracombe Road, near Barnstaple. This species a good deal resembles L. scabricula (M.C. t. 69, f. 1.), but is well distinguished by the numerous concentric ruge and the smallness of its spines. Fig. 5, 16. Leptena sordida. 'Transversely elongated, rather convex, irregularly striated, hispid? muscular impressions occupying half the internal area; hinge-line nearly as long as the width of the shell, its angles rounded. Width variable, sometimes nearly double the length. Of this shell we have but very imperfect specimens, and the exterior is badly preserved ; the portions which remain show it to have been very irregular. These specimens have been inadvertently engraved with fossils from Barnstaple. Loc. Linton. Fig. 6. Atrypa oblonga. Oblong-oval, convex, smooth; front produced, elevated ; the elevation narrow. Loc. Barnstaple. EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 7. Spirifera calcarata. Semicircular, with extended cuspidate smooth sides, sul- cated, very convex; front scarcely at all elevated; ribs numerous, rounded, wiih about nine on the front bounded by two deep furrows; area probably very narrow. Width more than twice the length. This approaches closely to S. attenuata, M. C., but is distinguished by the sudden contraction of the sides, and the very slight elevation of the front ; still we have some doubts of its being distinct from the many varieties of that species. The characters are taken from a single internal cast. Loc. Barnstaple. Fig. 8. Spirifera disjuncta. This, which is a cast of the inside of the upper valve, appears to belong to the species thus named, and is a good illustration of the in- ternal structure of the genus, exhibiting the beak, the muscular impressions, the central striated foramen, and also the hinge area with its striated structure. For a further description, see Pl. LIV. figs. 12 and 13. Loc. Barnstaple. Fig. 9. Spirifera inornata. Fusiform, compressed, smooth, obscurely radiated on the sides; the front even; beaks obscure. Length scarcely more than } of the width. This is so much crushed and distorted, that it is impossible to give a full de- scription ; butit appears to be distinct from every other species, approaching nearest in form to the Orthés (Spirifera) alata of the Silurian System, Pl. 22, f. 7. Loc. Ilfracombe. Fig. 10. Orthis plicata. 'Transversely elongated, depressed, plaited; plaits numer- ous, sharp; width twice the length. This resembles O. radians (Silur. Syst. Pl. 22, f. 11), but has much more nu- merous plaits. Loc. Barnstaple. Fig. 11. Orthis interlineata, A distorted cast, which may easily be mistaken for O. canalis (Silur. Syst. Pl. 22, fig. 8) or O. testudinaria (figs. 9 and 10). Fuller details are given in the description of the Petherwin fossils, Pl. LIV., Fig. 14., where better specimens are figured. Loc. Leary, N. Devon, &c. Figs. 12—15. Calymene. Figs. 12, 13, 15, Barnstaple. 14, Saunton. Figs. 17—21. Crinoidal remains. 17, Barnstaple. 18, 19, 21, Redruthen Steps, in St. Eval. 20, Lower St. Columb, Perth. Fig. 22. Avicula Damnoniensis. Obliquely ovate, with a square projecting ear, very convex, short, striated ; anterior side small, obtuse; hinge-line rather shorter than the width of the shell; beaks large, convex near the anterior extremity ; poste- rior slope and ear destitute of the fine longitudinal striz which ornament the rest of the shell. Abundant in the soft ferruginous sandstone in which the fossils of Marwood Quarry are all imbedded. Fig, 23. Cucullea unilateralis. Obliquely ovate, gibbose, smooth ; posterior side ob- lique, flattened ; beaks nearest to the anterior side. The cast,figured shows the impression of the internal lamina peculiar to the genus. 1 EXPLANATION OF THE PLATES AND WOOD-CUTS. The species is very abundant. Loc. Marwood Quarry, where the shells of this and the following species of Cucullea are often replaced by quartz. Fig. 24. Cucullea Trapezium. Transverse, obtusely trapezoidal, oblong, irregularly convex, smooth; anterior side rounded; posterior large, truncated, and longer than the rest of the shell. Length about 3ths of the width. Loc. Marwood Quarry. Scarce. Fig. 25. Cucullea angusta. Squarish, rather wider than long, convex, smooth; an- terior side rounded, the posterior truncated, square ; beaks central. A cast has the impressions of the lateral teeth, which confirm the genus. Loc. Marwood Quarry. Figs. 26, 27. Cucullea Hardingii. Transversely oval, with the posterior side trun- cated, gibbose, smooth, nearly twice as wide as long ; beaks nearest the anterior side. Loc. Marwood Quarry. Fig. 27 is an end view of a smaller specimen. Fig. 28. Pullastra? antiqua. Transversely elongato-ovate, slightly convex, concen- trically striated, striz distant ; posterior extremity slightly and obliquely truncated. Length about 3 the width. Loc. Marwood Quarry. Fig. 29. Leptena prelonga. Obovate, longer than wide, convex, with a depression along the middle, coarsely and irregularly striated; beak of the larger valve in- flated and overhanging the smaller one, whichis concave ; margin much deflected ; hinge-line shorter than the width of the shell; a few slight concentric waves pro- ceed from it. Loc. Croyde Bay, ina harder stone than the Marwood Bay fossils. Fig. 30. Bellerophon globatus. (Silur. Syst. Pl. Il. fig. 15.) We can perceive no difference between this fossil and some specimens from the lower beds of the old red sandstone. Loc. Marwood. Fig. 31. Crinoidal casts abundant at Croyde Bay. Prate LIV. Fig. 1. Avicula (Monotis, Bronn) subradiata. Obliquely ovate, with one rectangular ear smooth, with a few concentric lines, and radiated principally along the middle; one valve flat, the other convex; anterior extremity rounded, small. Width con- siderably more than the length. Loc. Petherwin. Frequent. Fig. 2. Avicula Pectinoides. Suborbicular, flattish, radiated ; ears very large, square ; the posterior slightly sinuated. This specimen, which is very imperfect and worn, resembles A. Neptuni (Goldf. Pet. CCXVI. fig. 4), but wants the numerous concentric striae which ornament that EXPLANATION OF THE PLATES AND WOOD-CUTS. species. We possess fragments which retain this structure, but are not sure they belong to the present species. Loc. Petherwin, Barnstaple. Fig. 3. Leptena Fragaria, var. If this fossil be referrible to the species described in Pl. LVI. figs. 5, 6, it is a very strongly-marked variety ; but we are not satisfied that it is a distinct species, although the tubercles are more elongated—allowance must be made for the state of preservation. Loc. Petherwin (abundant). Fig. 4. Atrypa hispida. Transversely oval, compressed, furnished with concentric fringes of spines. i Loc. Petherwin. Fig. 5. Atrypa decussata. Subglobose, slightly compressed; front even, straight; surface concentrically striated and decussated ; beak of the lower valve very little prominent, with a trifling angle on each side. Loc. Petherwin. Fig. 6. Atrypa indentata.. Transverse, obovate, with an indented front; the edge of the lower valve elevated; its beak small, prominent. The front of this shell appears as if impressed by the finger, whence its name : the elevation in the margin of the lower valve does not affect the surface of the other; this may serve to distinguish it from A. obovata (Silur. Syst. Pl. VIII. fig. 9), to which it bears a very close affinity. Loc. Petherwin (with the last, abundant), Barnstaple. Fig. 7. Atrypa subdentata. Orbicular, slightly convex, rather longer than wide, with a pointed three-plaited raised front; beak minute. Loc. Petherwin. Fig. 8. Atrypa Unguiculus. Hemispherical, rather wider than long, with an inflated beak, smooth ; front emarginate ; lower valve very convex, its beak channelled ; upper flat, with a central impressed line. This pretty shell occurs abundantly in the Petherwin strata, and is very cha- racteristic of them; it is frequently twice the size of the specimen figured. Loc. Petherwin, Barnstaple. Fig. 9. Atrypa triangularis. Triangular, with two folds in the front, beak scarcely prominent. Very much crushed and distorted casts in soft ferruginous stone. Loc. Petherwin. Fig. 10. Atrypa striatula. Suborbicular, convex, finely striated. A large species. Loc. Petherwin, Barnstaple, Fowey ? Fig. 11. Spirifera extensa. Fusiform, convex, radiated ; about 7 ribs ‘are elevated in the middle of the upper valve ; its beak small; radii numerous, commencing along the hinge-line. Loc. Barnstaple, Barnstaple Bridge, Saunton, Petherwin. Figs. 12, 13. Spirifera disjuncta. Semicircular, with an emarginate front, very con- vex, radiated ; upper valve with about 12 ribs, much raised in the front, forming 9) Fig. Fig. Fig. EXPLANATION OF THE PLATES AND WOOD-CUTS. a rounded elevation ; ribs rounded, numerous, about 25 on each side the middle ; beaks remote; hinge-area broad, curved, its edges nearly parallel. This differs from S. bisulcata (M. C. t. 494, f. 1) in its less convexity, more numerous striz, and broader hinge-area; and from S. bésulcata of Phillips (Geol. of Yorkshire, Pl]. IX. fig. 14), not of M. C. (which it very nearly resembles), in the greater regularity and number of the ribs *. The specimens of this shell are so generally distorted, that its true form is seldom to be clearly made out; and this, added to the difficulty which already exists of determining between the most perfect specimens of different species, renders it very difficult to ascertain to what species they belong. Perhaps even the S. gigantea from Tintagel (Pl. LV. figs. 1 to 4) may be distorted individuals of this species. Loc. Barnstaple and Petherwin. 14. Orthis interlineata. Suborbicular, compressed, with the front straight, finely radiated, marked with lines of growth interrupting the radii, which increase in num- ber towards the margin; larger valve not very convex ; its beak but slightly pro- minent ; the smaller valve with a shallow depression ; muscular impressions nearly parallel in the convex valve, impressions of the hinge-teeth in the other, broad. This species, when its internal structure is considered, forms a link serving to connect five species already described in the Silurian System. In the irregularity of its striz, and apparently wide form, it approaches O. data (Silur. Syst. Pl. XXII. fig. 10); in the depression and hinge-teeth of the lower or flatter valve it re- sembles the O. orbicularis of the Upper Ludlow (PI. V. fig. 16), and O. canalis of the Lower Silurian (Pl. XX. fig. 8); and these species are the exact analogues of the O. lunata of the Ludlow (Pl. V. fig. 15), and the O. testudinaria of the Caradoc (Pl. XX. figs. 9, 10): all of which, by a careful study of their internal characters, may be at once decided upon when all other characters fail. Loc. Petherwin (abundant), Leary, N. Devon, Barnstaple, Morebath, Land- lake, Cornwall. 15. Atrypa fallax, (Ter. pleurodon. a. Phill. loc. cit. t. xii. figs. 25, 26.) This species so exactly agrees with specimens of an Atrypa we have from Preston by favour of W. Gilbertson, Esq., that we cannot doubt its identity ; and this appears to be a shell that Professor Phillips has united with several others, under the name of Ter. pleurodon; it is, however, a genuine Atrypa, though so like the genus Terebratula that we have designated it fallax. Loc. Petherwin, Barnstaple. 16. Pleurotomaria aspera. Conical, short ; whorls convex with a rounded keel, marked above the band by four principal, and as many intermediate ridges, and beneath it by several smaller ones, all crossed by sharp lamine, which produce a reticulated surface ; band narrow, reticulated. * The Terebratulites aperturatus (Schloth. Nachtr. t. XVII. fig. 1) differs from this species in having a strong rib on each side the depression in the lower valve, and in possessing a triangular area. It is abun- dant in the Eifel, and much resembles the shell before us. EXPLANATION OF THE PLATES AND WOOD-CUTS. A handsome shell an inch in diameter. Loc. Petherwin; Landlake, Cornwall. Fig.17. Terebra nexilis. Subulate, acute, longitudinally striated ; whorls flat; strize Fig. Fig. gently bent twice. A neat shell, much resembling Rissoa Lefebvrei (Levéillé in Mém. de la Soc. Géol. de France, vol. ii. part 1, p.40, Pl. II. fig. 25) ; but the strize are finer, the shell more elongated, and the sides of the whorls flatter, than in the specimens we have examined of that fossil. Loc. Petherwin (frequent). 18. Goniatites vinctum. Discoid ; inner volutions two-thirds exposed ; sides of the whorls flat ; their inner edges abrupt; front rounded, encircled by a thread-like keel ; inner whorls crossed by straight undulations ; lobes of the sépta three on each side, that on the middle of each side by far the longest ; ovate, pointed. The specimen before us, though very imperfect, is clearly distinguished from G. Henslowi (M. C. t. 292), by having but three instead of four lobes on each side ; and from G. subarmatus, (Munster, Plan. und Goniat. Tab. VI. f. 2.) to which it is closely allied, by the ovate form of the lobes, which in that fossil have their sides straight, and the whorls in that species do not increase so rapidly. We have had the good fortune to see, in the Rev. Mr. Williams’s rich collection of Cornish fossils, several new and interesting species of Goniatites and Cly- menia in company with a species resembling Nautilus (Goniatites?) complanatus (M. C. t. 261.), which he has however reserved for future publication. 19. Clymenia (Endosiphonites, Ansted) levigata. (Planulites levigatus, Munster, Plan. und Goniat. T. I. f. 1.) A large smooth shell, with many whorls, and only a slight sinus on either side of each septum. Our specimens are not so large as that figured by Count Munster, nor is the wave in the septum placed so near the front of the whorl. Fig. 19 a. Clymenia linearis. (Pl. linearis, Munst. loc. cit. T. I. f. 5, 6. ene carinatus and minutus. Ansted Camb. Phil. Trans. vol. vi. Pl. VIII. f. 1, 2, 3.) This well-marked species is abundant in the Petherwin beds, and is distinguished from the preceding by the deep acute-angled sinus in the side of the Peptuiats and also by its striated surface and linear keel. Having examined the Cambridge specimens, we can see no reason for supposing the H. minutus a distinct species, especially as we have found on it the charac- teristic keel of E. linearis, or for altering the original specific name given by Count Munster. Loc. Petherwin. Fig. 20. Orthoceras striatulum. Rather rapidly tapering, ornamented with prominent transverse rings, crossed by numerous fine threads, which alternate with still finer lines ; annulations sharp, oblique, rather more distant than the septa. This has a close affinity with Orthoceras Tubicinella of the Plymouth limestone (Pl. LVII. f. 29.) ; but the threads are closer and finer, and it appears to be a larger species. At first sight it looks much like C. annulatum (M. C.t. 133.) ; but the longitudinal lines, and want of transverse scales, easily distinguish it. EXPLANATION OF THE PLATES AND WOOD-CUTS. Loc. Petherwin. It appears to be abundant, and very variable in size. Fig. 21. Orthoceras. This specimen, though very imperfect, was figured on account of the very curious longitudinal mark which crosses the edges of the septa, giving it the aspect of the alveolus of a Belemnate. Fig. 22. Orthoceras. A remarkably crushed specimen, so as to resemble a form of Belemnite common in the Lias. Similar occurrences are not unfrequent in the _ Upper Ludlow Rock of the Silurian series. Figs. 23, 24. Fragments of two species of Calymene. Fig. 24 much resembles C. tuber- culata (Silur. Syst. Pl. XIV. fig. 4.), but differs from that species in the number of lenses to the eye, which are but few in the present specimen. Similar frag- ments are not very uncommon in a soft stone at Petherwin. Puate LV. Figs. 1 to 4. Spirifera gigantea. Convex, radiated ; sides cuspidate ; radii numerous, proceeding from the hinge-line ; about nine or ten are elevated in the front, which is deeply emarginate ; lines of growth rather conspicuous, crossing the ribs. This magnificent species, which occurs nearly nine inches wide in micaceous slate at Tintagel, seems to be intermediate in character between S. disjuncta PI. LIV. f. 12, 13, and S. calearata, P|. LI. f. 7. The specimens we have examined are all destitute of shell, and the casts are covered with plates of mica, which lie flat on the surface and give it a glittering aspect; and they are so distorted in the direction in which the slate has been pressed, that they may easily be taken for many different species. The ribs are about as numerous as in the 8. Verneuillit, and are very regular. Fig. 1 is a specimen pressed laterally and flattened ; a cast of the interior of the lower valve, natural size. Fig. 2 is a young individual, showing the outside of the same valve; natural size. Fig. 3 is a specimen of the same valve, reduced to half its length. Fig. 4 shows the upper valve laterally compressed, and folded down upon one of its sides ; natural size. We have already given our opinion that this may be the S. Barumensis, but the cuspidate sides may probably entitle it to rank as a distinct species. Loc. Tintagel. Figs. 5 to 7. Spirifera costata. (S. speciosa of the Eifel?) Elongated-fusiform, con- vex, costated ; coste prominent, thick, about five or six on each side the middle, in which two are elevated and approximate ; lower valve with a deep broad depres- sion bounded by two strong ribs; hinge-area broad, its edges parallel. Length not ith of the width. The specimens we have seen of this fine Spirifera are all imperfect, and we cannot speak with certainty as to the surface ; lines of growth appear to cross the ribs, but they may be plaits occasioned by pressure. Occurs with groups of corals, fragments, &c., in a soft slaty stone at Fowey, and at Tintagel in a hard blue slate with the former species, and at Looe. EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 8. Part of the pelvis of a crinoidal animal. Occurs in a hard, flinty, slate rock, traversed by veins of Quartz at Looe. Prate LVI. Fig. 1. Corbula Hennahit. 'Transversely elongate-ovate, with a slightly projecting ' beak, smooth, convex, valves somewhat unequal; posterior side obliquely trun- cated, anterior pointed ; twice as wide as long. There appears no likelihood to us of this shell being referrible to the genus Lembulus, to which it was assigned by Dr. Leach; its unequal valves, if this be not accidental, indicate its affinity to Corbula. Loc. Mount Wise. Fig. 2. Cardium aliforme, var. (M. C. t. 552. f. 2. Goldf. Petr. 213. Tab. CX LII. f. 1. Pleurorhynchus minax and aliforme of Phillips, Geol. of Yorks. 210. Pl. V. f. 27. Bucardites hystericus, Schloth. Nachtrage. t. XX. f. 1.) One of the many varieties of C. aliforme. Goldfuss has done well in keeping them all together. We can see no reason for separating them into distinct species, or for adopting a new generic name. Loc. Stonehouse Hill. Fig. 3. Leptena analoga. (Phill. loc. cit. Pl. VIL. f. 10. Producta anomala, Sowerby. See Encyc. Metrop. loc. cit.) The worn specimen before us we presume to belong to this species. We have seen a most beautiful internal cast from Barnstaple in the eollection of the Rev. D. Williams. Loc. Plymouth, Barnstaple. Fig. 4. Leptena rugosa, His.? (Dalm. Act. Holm. 1827, 106. Tab. I. f.1.) We refer this shell with uncertainty to Dalman’s species, of which we have not seen well- authenticated specimens ; its more even form distinguishes it from L. depressa. (M. C. t. 459. f. 3.) Loc. Plymouth. Fig. 5, Leptena Fragaria. Hemispherical, with slightly projecting sides, concentri- cally waved, nearly smooth, pustulated ; beak of the convex valve pointed ; hinge- line rather shorter than the width of the shell. This species approaches very closely to Producta pustulosa (Ph. loc. cit. Pl. VII. f. 15.), or perhaps more nearly to P. rugata (Ph. Pl. VII. f. 16.); but, wanting the deep concentric rugz which mark these species, we have called it Fragaria, from the collection of pustulose tubercles (probably the bases of spines) which cover its surface pretty regularly ; it is however highly probable that all are varieties of one species. Loc. Plymouth, Petherwin ? Fig. 6 is probably the young of the preceding species; the tubercles are more numerous in proportion to the size. Loc. Plymouth. Fig. 7. Leptena interrupta. Semicircular, very gibbose, concentrically ribbed ; longi- EXPLANATION OF THE PLATES AND WOOD-CUTS. tudinally and finely striated ; striae interrupted by the concentric ribs; hinge-line equal to the width of the shell; beak somewhat produced. A small species, nearly akin to LZ. punctata (M. C. t. 328). Loc. Plymouth. Fig. 8. Atrypa juvenis. Broad-ovate, slightly convex, smooth, curved, longer than wide ; front somewhat pointed; valves nearly equal, the lower curved upwards with a minute beak. A small, rather flat species, distinguished by its narrow front, and by being curved. Loc. Plymouth. Fig. 9. Atrypa lacryma. Subglobose, smooth, longer than wide; front straight or slightly waved, scarcely raised except at the edge, which is deeply sinuated by the projection of the inferior valve, the central furrow of which is broad, flat and bounded by two sharpish ridges ; its beak not prominent; side rounded. An obscurely-marked species ; very convex, and with nearly equal valves. Loc. Plymouth. Figs. 10, 11. Strigocephalus (Bronn) giganteus. (Terebratula gigantea, Sowerby. See Encyc. Metrop. loc. cit.) Suborbicular, convex, smooth, with a straight pointed beak ; valves nearly equal ; area beneath the beak a right-angled triangle, flat; foramen narrow. Almost all the specimens we have seen of this noble shell, which is often six inches in diameter, are much distorted ; its true form appears to be round. It very nearly resembles the genus Atrypa, but differs from it in the presence of an area between the beaks ; this species is distinguished by its small straight beak, and its flatter shape, from the Strigocephalus porrectus, which is plentiful in the Plymouth limestone, and is (Ter. porrecta, M.C. t. 576. f. 1.) Strigoc. Burtini of continental authors. A specimen with a slight depression along the lower valve we once distinguished by the name of Ter. Hennahiana (see Encyc. Metrop. loc. cit.), but subsequent examination has shown it to be a variety. In some internal casts the muscular impressions appear to have been strong, and the shell has been coated inside with rhomboidal crystals of carbonate of lime, which give it a decussated appearance. Loc. Plymouth, Newton Bushell. Figs. 12, 13. Atrypa plebeia. Transversely obovate, with a produced front, smooth, not very convex; front slightly elevated, without a depression in the lower valve ; beak but little prominent. This is a common species and varies in form ; it was formerly (see Ency. Metrop. loc, cit.) considered to be the young of A. glabra (M. C. 269. f. 1.), but the regular convexity of the lower valve and small beaks distinguish it. Loc. Mount Wise, Plymouth. Fig. 14. Atrypa triloba. Tetrahedral, with rounded angles, 3-lobed, plaited ; upper valve extremely gibbous ; lower nearly flat; front much elevated, with about 12 EXPLANATION OF THE PLATES AND WOOD.-CUTS. plaits, its sides smooth; lateral lobes reflexed, obscurely plaited. Length and width nearly equal, the depth rather less. Somewhat resembling the most extravagant but small varieties of A. Pugnus (M. C. t. 497.) ; but it is more triangular, the plaits are rounder, less elevated, con- tinued almost to the beak, and more numerous; it is more like 7. flexistria (Ph. loc. cit. Pl. XII. f. 33, 34:). A handsome shell. Loc. Plymouth. Fig. 15. Atrypa Pugnus (M. C. t. 497.). A flattened variety of this very variable species. See also Fig. 18. Loc. Plymouth. Fig. 16. Atrypa protracta. ‘Triangular, longer than wide, lateral angles rounded ; beak produced acute; sides flattened, front elevated with about 4 plaits, its sides smooth. Loc. Plymouth. Fig. \7. Atrypa crenulata. Pentagonal, compressed, smooth; front broadly and sud- denly elevated, crenulated by numerous small plaits near its margin; sides smooth; beak scarcely any. A neat species. , Fig. 18. Atrypa Pugnus (M.C. t. 497.). Another variety of the mountain-limestone shell, rather narrower than usual; other varieties also occur here. Loc. Mount Wise. Figs. 19 and 20. Atrypa desquamata. Oblong, with a straight front, gibbous, deeply striated ; striae increasing in number towards the margin; front obtuse, gently and broadly raised at the edge without elevating the surface; shell longer than wide ; upper valve deeper than the one with the projecting beak. This shell, which is very abundant in the Plymouth limestone, varies exceedingly in size, coarseness of striz, and convexity. In some young individuals the form is nearly globose, while in others it is compressed and lenticular. Loc. Plymouth. Figs. 21 and 22. Atrypa desquamata var. compressa, Suborbicular, compressed ; sides nearly rectangular ; margin nearly even; valves equal. This differs from the first variety in being flatter and broader ; the upper valve, not being very convex, does not hang over the beak of the lower so much as in the more convex variety (Fig. 20.), wherefore this seems to have a more projecting beak, which, when broken, appears to have a flat area. Both the varieties approach so near to A. affinis (M. C. t.324.), and more espe- cially to the Eifel specimens of that species, that, were it not for the total absence of concentric scales, the much more even margin, and the oval not triangular con- tour, we should continue to refer them to the same species. One of the varieties was formerly called 7. affinis (in the Encyc. Metrop. Joc. cit.). Fig. 23. This is evidently a young shell; we cannot distinguish it from some specimens of A. aspera (Silur. Syst. Pl. XII. f.5.), but most probably it is a young individual of the A. desquamata. Loc. Plymouth. EXPLANATION OF THE PLATES AND WOOD.-CUTS. Fig. 24. Atrypa cuboides. Subglobose, striated; front raised, very flat, with a deep square sinus in the margin, edges sharp, projecting ; striz numerous, shallow, about 15 are elevated; beak small, acute ; lower valve small, nearly flat, with a large projecting square appendage filling the sinus in the upper one ; striz nume- rous, shallow, extending to the beaks, those on the side much curved. The parallel striz on the front are a striking character. Loc. Plymouth, also in the Eifel. ‘ig. 25. Atrypa latissima. Transversely elongated, smooth, convex, with rather pointed dependent sides ; front elevated, broad, rounded and furrowed, furrows shallow, many very obscure on the sides. Nearly related to A. platyloba (M. C. t. 496, f. 5, 6.), but the front is rounder, and the furrows much less distinct. Loc. Plymouth. Puiate LVII. Fig. 1. Atrypa squamosa. Lenticular, ribbed, squamose. The ribs are thick, sometimes forked, and are crossed by concentric thin la- minz; they vary in number, and are sometimes so numerous that it is difficult to draw a line of demarcation between this species and J. aspera of Schlotheim, which again passes into A. affinis (Silur. Syst. Pl. VI. f. 5. M.C. t. 324.). Loc. Plymouth. ‘This shell appears to characterize a stratum of limestone in the Eifel. Fig. 2. Atrypa impleta. Transversely elongated, ventricose, furrowed; sides rounded; front elevated with six furrows ; beaks slightly prominent, much wider than long. The furrows on the surface are shallow and extend to the beaks, the ribs be- tween them are rounded. Loc. Plymouth. Fig. 8. Atrypa spherica. Spherical or rather obovate, transverse, ventricose, plaited ; edge of the front deeply sinuated, with five elevated ribs; beak small, adpressed. Rather wider than long. Loc. Plymouth. Fig. 4. Atrypa implexa. Obovate, transverse, plaited. Front straight, flat; margin of the front and sides broad ; the toothed edges of the valves deeply locked into each other; plaits numerous, acute. At first sight this may be taken for Atrypa Wilsoni (M. C.), but it is not so cy- lindrical, neither is the front so deeply sinuated. Loc. Plymouth and the Eifel. Figs. 5 and 6. Atrypa primipilaris, Schloth. (Von Buch. Terebr. 68, T. II. p. 29. Spirifer pentagonus, Sower. See Encyc. Metrop. loc. cit.) Pentagonal, convex, plaited ; front elevated, with three or more plaits, margin flattened ; a deep angu- lar furrow runs along the middle of the lower valve, bounded by two angular ridges ; beak prominent. Fig. 6 represents a young shell. Loc. Plymouth, Eifel. Fig. 7. Spirifera (2) erenistria, Phill. (Geol. of Yorksh., 216, Pl. IX. f. 6. Sp. reticu- Fig. Fig. ald ig. Fig. EXPLANATION OF THE PLATES AND WOOD-CUTS. lata, Sowerby. See Encycl. Metrop., doc. cit.) This shell is not very uncommon in the mountain-limestone of the north of England and of Ireland; it also occurs at Matlock. The Irish specimens are often large, with deflected margins, which, with other circumstances, induce us to believe this shell will prove to be a Leptena. Loc. Plymouth. 8. Spirifera nuda. Semicircular, with prominent beaks, smooth, the middle ele- vated, with a furrow on each side of it; edge obtuse. Loc. Plymouth. 9. Spirifera pulchella. Hemispherical, convex, smooth, with three large rounded ribs ; edge sinuated; beak of the lower valve large, incurved. This resembles Sp. erispa (Silur. Syst., Pl. XII. f. 8.), but is smooth and has fewer ribs. Loc. Plymouth. . 10. Spirifera subconica, var. (Anomites subconicus, Mart. Pet. Derb. Pl. XLV. f. G6.) This is smaller and has a more curved beak than Martin’s shell, but we think it is the same species. Loc. Plymouth. 11. Spirifera affinis. Lenticular, ribbed, ribs numerous, branched and crossed by concentric thin lamin ; hinge-line shorter than the width of the shell; beak of the lower valve prominent, with a triangular flat area. The prominent beak and large triangular area distinguish this from Aérypa as- pera, Schloth. (Silur. Syst., Pl. XII. f. 5.) which it much resembles ; it is a re- markable shell. Loc. Plymouth. 12. Orthis tenuistriata. Semicircular, with the front straight, striated ; one valve regularly convex, the other flatter; hinge-area parallel, narrow. The fineness of the striza and the regular convexity, joined with the parallel area, at once distinguish this and make us doubtful whether it be not a Leptena; traces of spines are indistinctly visible. Loc. Morebath. 13. Pileopsis vetusta (M. C. t. 607). The specimen figured is more involute and even than the shell in Min. Conch., but examples pretty frequently occur much more like that figure at Mount Wise, &c. Loc. Plymouth. . 14, Nerita deformis. Subhemispherical, obliquely flattened; whorls rapidly in- creasing, finely striated ; inner lip uneven, aperture ovate. This was formerly published (see Encyc. Metrop., doc. cit.) under the name of NV. spirata (M. C. t. 463, f. 1, 2.) ; but it is not so transverse or ventricose, and the spire, though imperfect, could not have been so depressed. Loc. Stonehouse Hill. 15. Nerita speciosa. Conical, depressed, smooth? ; whorls rapidly increasing, the upper ones very convex, the lower rather square, with a central spiral depres- sion above, concave beneath; aperture subtrapezoidal? Height and diameter about equal, often 3 inches. c EXPLANATION OF THE PLATES AND WOOD-CUTS.. This fine shell was published (see Encyc. Metrop., doc. cit.) as a var. of N. spi- rata; but the size of the spire, the square form of the lower whorls, and its great size, entitle it to the rank of a species. Loc. Mount Wise, Plymouth, where it occurs of all sizes. Fig. 16. Pleurotomaria impendens. Conical, short, spirally striated, base concave ; whorls rather flat above,—the lower overhung by the angular base of the pre- ceding whorl; the stria which encircle the whorls are less distinct towards the upper margin. The imperfect specimens we possess of this shell will not allow us to draw up a full description. Loc. Plymouth. Fig. 17. Pleurotomaria cirriformis ? (M.C. t. 171, f.2. Huomphalus delphinuloides ? Auct.) An imperfect water-worn cast is all we possess of this shell; the true P. cirriformis is found at Paffrath, and has the above name applied to it by conti- nental authors. Loc. Plymouth, also in the mountain-limestone. Fig. 18. Turbo subangulatus. Conical, elongated ; whorls about six, convex, marked with three obscure spiral ridges on each; aperture nearly circular. This which occurs with the last is in the same bad state of preservation. Loc. Plymouth. Figs. 19 and 20. Turbo cirriformis, Sower. (see Encyc. Metrop., loc. cit.) Conical, short, oblique, smooth; apex obtuse; whorls slightly rounded, most prominent below; aperture circular. Height and diameter equal, about } an inch. An obscure, yet neat species, common at Stonehouse Hill. Fig. 21. Murex Harpula (M.C. t, 578, f. 5.). Young individuals of this pretty species are frequent in the Plymouth limestone. Loc. Stonehouse Hill, also Bradley. Fig. 22.. Terebra Hennahii, (Ter. Hennahiana, Sower.,see Encyc. Metrop./loc.cit.). Sub- ulate, longitudinally and very finely striated, whorls slightly convex, striae gently bent twice. Diameter not much above } of the height, which is but 3ths of an inch. Very like 7. nevilis of the Petherwin beds (Pl. LIV. f. 17.), but with still finer and less bent stria, so that Rissoa Lefebvrei, T. nexilis, and the present species will form a neat series of species characteristic of these beds. Loc. Stonehouse Hill. Fig. 23. Buccinum acutum (M.C. t. 566, f. 1.). This is very imperfect, but cannot be distinguished from the shell figured in Min. Conch., which is found in Queen’s County, Ireland. Loc. Stonehouse Hill. Fig. 23 a. Buccinum imbricatum (M. C. t. 566, f. 2.). Imperfect specimens, common in this locality. Loc. Stonehouse Hill, also Bradley, near Newton Bushel. Figs. 240 27. Buecinum spinosum (M. C. t. 566, f. 4). These specimens are variously distorted, but are all evidently referrible to this species, which we have seen also Fig. Fig. Fig. EXPLANATION OF THE PLATES AND WOOD-CUTS. from the Eifel, and we may remark, that this locality presents the most complete analogy with the Devonian beds. Loc. Plymouth and Bradley, frequent. 28. Orthoceras cylindraceum? An imperfect specimen. We have called it the same as that in the black limestone of N. Devon (PI. LII. f. 6, 7), though the smooth species are so much alike that without good specimens we would not pre- tend to determine positively any one. Loc. Newton Bushel, with Brontes flabellifer, Goldf. 29. Orthoceras Tubicinella. Slowly tapering, ornamented with prominent trans- verse oblique rings, which are crossed by numerous thread-like ribs without inter- mediate ones, giving it exactly the aspect of the recent Tubicinella Balenarum; section circular. This very pretty species bears a good deal of resemblance to O. striatulum (Pl. LIV. f. 20), but the longitudinal ribs are much thicker and more prominent than in that species ; it resembles too the O. rugosum, Flem. (Phill. d.¢., Pl. XXI. f. 16.), but in that beautiful shell the rings are more distant, and the longitudinal ribs are elevated into spines at short intervals. Loc. Plymouth. 30. Remains of an Asaphus or Trinucleus? common at Newton Bushel. It is remarkable that no trace of the position of the eyes remains on the cast, which is also the case with the genus T’rinucleus, Murchison. : . 31. Pelvis of Cupressocrinites? We have seen two specimens of the pelvis in the Plymouth limestone, and one of the arm of this curious animal from Collump- ton, where also large specimens of Brontes flabellifer occur. Loc. Plymouth, Collumpton, Prate LVIII. Corals from the limestones south of Dartmoor, described by Mr. Lonsdale. The specimens are principally in the cabinets of Mr. Austen, Mr. Daniel Sharpe, the Rev. R. Hennah, and the Woodwardian Museum, Cambridge. g. 1, la, Astrea pentagona (De Blainville, Man. d’Actinologie, p. 375). Cyathophyllum pentagonum (Goldfuss, Petref. p. 60, Tab. 19, f. 3.). Stars irregular in size and shape, but well defined, both on the weathered sur- face (Fig. 1.) and in a polished section (Fig. 1 a.), the boundaries being formed by zig-zag lines connecting the ends of the rays. On a weathered surface, the centre of the star presents a radiated boss; but in a polished section it consists of car- bonate of lime, into which the longer rays project more or less, according to the state of preservation. Rays numerous, equal in breadth and uniform in character, but alternately long and short, the termination of the latter assisting to define the centre of the star. From the irregularity in the shape of the star, the length of the rays varies considerably. Character of the perfect terminal star not known. Loc. Newton Bushel, ‘Torquay, Plymouth. 2. Stromatopora polymorpha (Goldf. Petref. Tab. 64, f. 8.). Form irregular, mammillated or branched ; composed of concentric layers, united at irregular di- Ki EXPLANATION OF THE PLATES AND WOOD-CUTS. stances by vertical filaments. The horizontal section (Fig. 2.) presents more or . less perfectly, perforated centres, from which irregular tubes diverge, also the terminations of the filaments, and portions of the concentric layers. Loc. Appleway and near Teignmouth. . 8,36. Astrea Hennahii (Sp. n.). Stars not defined either on a weathered surface (Fig. 3.) or in a polished section (Fig. 3 a.). On the former, the centre of the star presents a radiated boss, in the latter, fine converging lines. Rays about thirty-six, unequal in length and breadth, and of a crenulated structure. The rays of one star unite with those of the ad- joining stars, the junctions being more or less regular according to their position with respect to the angles of the stars. The rays are alternately long and short, the latter terminating around the central portion of the star, and the former which swell out at the same boundary suddenly become attenuated beyond it, and are prolonged as fine laminz to a reticulated centre. The vertical section (Fig. 3.) is composed of perpendicular close-set parallel lamellz united by innumerable trans- verse plates (Fig. 3 0.). ; Loc. Barton Quarry, Newton, Plymouth. .4, 4 f. Porites pyriformis, Ehrenberg. Astrea porosa (Goldfuss, 21, f.7.) Porites pyriformis (Silur. Syst. Pl. XVI. f. 2.). This fossil abounds in the Devonian limestones as well as in the Silurian system ; but specimens of the perfect coral, or in that state in which it is presumed the polype ceased to add to its strong fabric, appear to be véry rare. I have seen only a few belonging to Mr. Austen’s collection. In the young state, and during the period when additions were made to its vertical dimensions, the coral con- sisted of circular tubes, with a projecting ‘margin, from which twelve rays pro- ceeded and united in the centre; and the interstices between the circular tubes were occupied by smaller polygonal ones, open at the upper end. In the state in which it is supposed the polype ceased to add to the structure of the coral, the fossil (Fig. 4, 4 a. 4c. 4d. 4 e.) presents in the place of the circular depressed tubes, a raised boss, the margin of which is a sunken and not a projecting line; and the intervals between the twelve rays of the immature coral are occupied by convex surfaces, separated by fine furrows. ‘These bosses are surrounded at irre- gular distances by polygonal ridges, giving the coral the aspect of a series of stars in close contact (Fig. 4.).. The ridges and the whole of the surface, which in the young specimens consist of open tubes, are formed of convex papilla preserving in greater or less perfection the angular form of the tube. The right half of Fig. 4 c. exhibits the usual character of the coral, except that the projecting margin of the circular tubes is wanting ; the left half of the same spe- cimen presents imperfectly the character of the mature coral. Fig. 4 d. has been drawn from a partly polished specimen, the remainder giving examples of the radi- ated boss, but without the bounding polygonal ridges. Fig. 4f. is a magnified representation of the polished surface, and Fig. 4 e. of the bosses. Fig. 4 exhibits the character of the perfect coral, and Fig. 4 a. is a magnified portion of the same specimen. Fig. 4 . displays the internal structure of the fossil. EXPLANATION OF THE PLATES AND WOOD.-CUTS. From the above characters, believed to be new among lamelliferous corals, it is inferred that this fossil does not belong to the genus Porttes; but it has been thought advisable not to propose, at present, a new one for it. Loc. Newton Bushel, Marychurch, Plymouth, &c. Figs. 5 to 5 d. Coscinopora placenta? (Goldfuss, Pl. IX. f. 18.). Prof. Goldfuss described the fossil which he has called Coscinopora placenta from apparently a single and probably an imperfect specimen, and was therefore unable to detail fully its characters, It is with considerable hesitation that the Devonian fossil has been assigned to the same genus and species; but it has been thought better to do so provisionally than to propose a new generic appellation. The coral represented in Figs.5to 5d. consists of amorphous masses, composed of very thin concentric layers, traversed horizontally and obliquely by irregular vermi- form cavities, and perforated vertically by cylindrical tubes, which penetrate the whole depth of the specimen, and are bounded by a white circle forming the sub- stance of the tube (Figs. 5,5 a.56.5d.). The distance between the layers is about equal to their thickness; and the layers are united by vertical filaments of variable form and dimensions, the interstices having a punctured appearance (Fig. 5 a.). In some specimens the vertical section is banded, being crossed by stripes of a darker colour (Fig. 5 a.). This fossil varies greatly in character, according to its state of preservation or mineralization. In some specimens, all structure has nearly disappeared, except the vertical tubes, and the coral then agrees with Goldfuss’s description (C. das- coidea, poris orbiculatis equalibus, interstitiis levibus). Other specimens might be mistaken for masses of Stromatopora concentrica, except that the tubes with careful search may always be found (Figs. 5 6. 5 c. 5 d.) ; and the resemblance is still stronger in some masses consisting of gray carbonate of lime, traversed at distant intervals by concentric bands of the decomposed coral. Loc. Newton Bushel, Torquay, Appleway, Plymouth, &c. Perrata (Munster, MS.). Fig. 6. Petraia Celtica. Turbinolia Celtica (Lamouroux, Expos. Méthod. Pl. LVIII. f.7, 8.). (See ante, p- 697.) Turbinated ; external cast smooth ?; internal cast composed of thick lamelle, with two indistinct rows of papillze and a furrow down the middle. An abundant coral in the slate rocks of Cornwall, but it rareiy presents more than flattened casts of the interior. It is placed in this genus because it agrees generically with specimens labelled Petraia from the continental collection of Count Munster. Loc. Dinas Cove Padstow, Berry Pomeroy, and Fowey. A large coral differing from the above, principally in size, occurs in slate rocks at New Quay, and near Newton Bushel. Fig. 7. Strombodes vermicularis. Cyathophyllum vermiculare? (Goldfuss, Petref. Tab. 17, f. 4). Cylindrical, straight or curved, externally traversed by vertical ridges, marking EXPLANATION OF THE PLATES AND WOOD-CUTS. the position of the internal lamella, and by concentric rugz and fine lines (Fig. 7.). Internally formed of numerous lamellz, which are spirally contorted in the centre, and bifurcate as they radiate more or less regularly to the circumference (Fig. 7 a.). No central cavity crossed by chamber-like septe, that part of the coral being occu- pied through its whole height by the spiral lamelle (Fig. 7 a.). Loc. Plymouth and Newton Bushel, abundant. Figs. 8 to 8 d. Cyathophyllum cespitosum (Goldfuss, Tab. 19, f. 2.). An abundant coral in the Devonian limestones, but seldom well preserved, the exterior portions having been in general removed by atmospheric action. Fig. 8 a. represents a common weathered specimen; 8 ¢. a section of a similar branch ; 8 b.a section of one in which the exterior has been less effectually removed. Fig. 8 represents a specimen of hard limestone, in which the matrix has preserved the exterior portions of the coral. Fig.8 d.is a vertical section, exhibiting transverse chamber-like plates, and part of another branch or individual, which had sprung from a gemmule deposited on the side of the main coral, and not originated in the subdivision of the older animal. The sections, Figures 8 b. 8 ec. and 8 d. in the ab- sence of the central style, sufficiently distinguish this coral from one of similar ex- ternal form, abundant in the mountain-limestone. Loc. Newton Bushel, Plymouth, Torquay, &c. Fig. 9. Scyphia turbinata (Goldfuss, Petref. Pl. II. f. 13.). Two pyritous specimens imbedded in slate, from the vicinity of Plymouth, are in the cabinet of the Rev. R. Hennah. Fig. 10. Fenestella antiqua? (Silur. Syst. Pl. XV. f. 15, 18.). Gorgonia antiqua (Goldfuss, Petref. Pl. XXXVI. f. 19.). This is also an abundant coral in the slate rocks of the Devonian system; but the essential characters are seldom preserved. It presents generally a more or less deli- cate net-work (Fig. 10) or cast of the interior surface of the coral ; and occasionally impressions of the bifurcated lamella of the exterior surface (10.a.). Casts of the pores have been also observed in a few instances, and their arrangement led to the belief, when first noticed, that the coral belonged to a new, well-distinguished species of Fenestella. Instead of being arranged in two rows, separated by a ridge or projecting angle, as in Fenestella antiqua (Silur. Syst. Pl. XV. Fig. 16. Goldf. Pl. XXXVI. f.9.), the pores or their casts are in contact and disposed alternately, so that the projecting curve of one pore occupies the space between two pores in the adjacent row (Fig. 10 4.). On examining however some crushed specimens of Fenestella from Meinershagen, the characters of the Devonian co- ral and of Fenestella antiqua were noticed in portions of each specimen; and though the detached fragments could not be proved to have been once united, yet little doubt can exist of their being portions of the same coral, and that the q alterations in character must be ascribed to changes in the animal at different pe- riods of growth. Fig. 10d. is a portion of Fig. 10 a. mag. Loc. Petherwin, Fowey, Plymouth, in soft yellow slate, Newton Bushel, Saunton, Linton, &c. Fig. 11 to 11 6. Cystiphyllum Damnoniense (Sp. n.). EXPLANATION OF THE PLATES AND WOOD-CUTS. Turbinated or cylindrical; terminal cup occasionally very deep, occasionally shallow, covered with bladder-like tubercles, traversed in some specimens by radi- ating lamelle ; external surface marked with concentric ruge and faint vertical lines ; internal structure very irregularly vesicular, often without any indications of radiating lamellz ; but in some specimens there are indications of them (Fig. 11 8.), and in others they are quite distinct (Fig. 11 a.). Fig. 11 represents a portion of a fine group, with three young corals attached to the side of an old one. Loc. Newton Bushel, very abundant, the coral occurs also at Plymouth. WOOD-CUT. Section from the Foreland in the Bristol Channel to the English Channel: p. 702. Pirates LIX. and LX. Illustrate Mr. Stokes’s paper on some species of Orthocerata: p. 705. Pruate LIX. Fig. 1. Actinoceras Lyonii, p. 707. Figs. 2 and 3. Actinoceras Richardsonii, longitudinal and transverse sections, p. 708. Fig. 4. Actinoceras Simmsii, one third the natural size, p. 708. Fig. 5. Transverse section of Actinoceras Simmsii, p. 708, and note +, also p. 712. Fig. 6. Magnified portion of the coral investing A. Stmmsii, p. 708, note +, and p. 712. Prare LX. Fig. 1. Ormoceras Bayfieldit, p. 709. Fig. 2 and 3. Longitudinal sections of Huroniea, p. 710. Fig. 4. Exhibits a peculiarity in the structure of Orthocerata. The specimen is from Russia, p. 712. Fig. 5. Huronia Portlockii, p. 710. Pruate LXI. Illustrates Col. Sykes’s paper on fossils procured by Capt. Smee and Col. Pottinger in Cutch and the Desert to the north-east of Cutch, p. 715. The shells have been engraved and the description prepared by Mr. James de Carle Sowerby, F.L.S. Fig 1. Astarte major. Elliptical, convex, concentrically furrowed when young ; fur- rows numerous; beaks small, near the anterior side; lunette broad, flat, deeply sunk; ligament long, sunk. Length from 2 inches 4 lines to 2 inches 8 lines, width 43 inches. This species varies much in the proportions of its length and breadth, and the anterior side is sometimes formed as if truncated. The figure represents a very wide variety diminished to 2rds its size. EXPLANATION OF THE PLATES AND WOOD-CUTS. Fig. 2. Astarte compressa. Nearly orbicular, wider than long, flattish, concentrically ribbed; lunette deep, small ; beaks small, near the anterior side; edge toothed. Length 14 inch, width 1 inch 5 lines. A species very closely resembling this is found at Cross Hands in Gloucester- shire in the inferior oolite. Fig. 3, 3a. Astarte rotunda. Orbicular, concentrically ribbed ; beaks central; lunette sunk; margin toothed. Length 2 lines, width the same. Nearly like A. elegans (M. C. t. 137, f. 3.), but it is so much imbedded in the stone that its characters cannot be clearly determined. Fig. 3 a. is magnified. Fig 4, 4a. Corbula pectinata. 'Trigonal, rounded, gibbose, longitudinally striated, concentrically ribbed ; posterior extremity separated in the form of a small lobe, pointed ; ribs thin, much elevated. Lunette deeply sunk, not defined; beak in- curved. Length and width nearly equal, from 3 an inch to an inch. Fig. 4 shows the impression of the hinge-tooth. This differs from Corbula lyrata (ante Grant, Pl. XXI., f. 13.), which is also from Cutch, in having numerous thin striz and thin ribs. It occurs loose and in masses with several other shells in a red limestone. Fig. 5. Trigonia Smeeii. 'Transversely much elongated, posteriorly truncated, con- vex, concentrically ribbed; the posterior surface distinguished by an obscure ridge, and furnished with twice as many ribs as the other part; ribs obtuse, sel- dom interrupted ; beaks near the anterior extremity, which is rounded. Length 2 inches 5 lines, width 4 inches. The figure is reduced to 2rds the natural size. Fig. 6, 6a. Tornatella striata. Ovate, pointed, transversely punctato-striated ; one obscure plait on the columella. Height 23 lines, diameter 1} line. Much resembling Phasianella striata (Fitton, in vol. iv. Pl. XVIIIL., f. 15.), but the apparent plait on the columella, if it be not the effect of fracture, distinguishes it. Fig. 6a. is magnified. Fig. 7. Terebratula microrhyncha. Subtetrahedral, rounded, plaited, lower valve nearly flat, plaits angular, 28 or 30, of which about 9 are raised in the front; beak of the lower valve very small, its aperture inclined inwards, and its sides smooth and sunk. Length 2 inches, width 1# inch, depth of the valves united 1} inch. A large species, distinguished from 7. nobilis (Grant, Pl. XXIL., f. 14.) by the greater number of plaits. Fig. 8. Ammonites Maya. Discoid, convex with a rounded front, umbilicated, radiated ; umbilicus conical, smooth within; radii rather numerous, slightly elevated 2-, 3- or 4-partite, bent over the edge of the umbilicus; aperture rounded-sagittate with truncated angles. Diameter 7} inches, width of the aperture 3} inches, its length 4 inches. This is an intermediate species between 4. formosus (Grant, Pl. XXIII. f. 7.), and A. Herveyi (M. C.), a variety of which also occurs with this. Its sides are flatter than in the 4. Herveyi, although the front is round, and the ribs less raised. Fig. 9. Ammonites calvus. Discoid; inner whorls two thirds exposed, nearly crossed by rounded ribs, and plaited over their fronts; outer whorls crossed by prominent rounded ribs, their front rounded, plain ; aperture oval, impressed by the preceding EXPLANATION OF THE PLATES AND WOOD-CUTS. whorl. Diameter 7 inches, width of the aperture 1} inch, its length 21 inches. A larger specimen measures 9} inches across, and is less plaited and ribbed. The figure is drawn 3rd of the natural size. Very near A. decipiens (M. C.), but the whorls increase more rapidly and envelope each other more. Fig. 10. Ammonites Pottingerit. Discoid, thick, costated; inner whorls exposed ; front nearly flat; ribs sharp, prominent, split into two or three over the front; aperture transversely obovate. Diameter 43 inches, width of the aperture | inch 8 lines, its length 1 inch 2 lines. Avery distinct species, cast in coarse limestone, replete with large grains of quartz. Fig. 11. Ammonites fissus. Discoid, costated ; whorls rapidly increasing, the inner Fig. exposed. Cost large, obtuse, either forked or simple, with an intermediate short rib passing over the front, which is convex and prominent ; aperture ovate. Dia- meter 44 inches, width of the aperture 1 inch 5 lines, its length 13 inch; the figure is reduced to one half. 12. Ammonites torquatus. Discoid, costated ; inner whorls exposed ; coste nu- merous, generally split into two as they pass over the rounded front, sometimes single, and (in large specimens) occasionally trifid ; inner edges of the whorls in- curved ; aperture orbicular; whorls about five. Diameter 2% inches, width of aperture | inch, its length the same. In large specimens are indications of a thickened edge having been formed to the aperture at various periods of growth. It is like A. annulatus vulgaris (Zieten, Pl. IX. f.1.), and also A. colubrinus major (Id. Pl. IX. f. 3.), but distin- guished by the incurved inner margin from both, as well as from a similar species found in the Himalaya Mountains. Fig. 13. Ammonites Fornix. Discoid, compressed, (when young, keeled,) undulated ; inner whorls 3rd exposed, their exposed parts smooth; margin convex, smooth, with a row of minute tubercles on each side, and a slender keel, which are lost in the external whorls ; undulations bent back in the middle of the sides, divided to- wards the margin; aperture sagittate, elliptical, Diameter 2 inches, width of aperture 7 lines, its length 1 inch 2 lines. Fig. 14 a. to f. Nummularia exponens. Very flat, thin, granulated, whorls few ; septa rather distant, visible through the shell ; chambers twice as long as deep. Diameter of the shell frequently more than an inch. Fig. 14 f. is a magnified section. When young, this Nummulite is lenticular ; when old, it is concave in the centre, ri ist it 4 id yee * - a a » wf He iy 5 i Rie Scena <8 ae ng, ae a ees ae Ww aig ee eee eet en a a an 1 et eA ‘au ¥ Ni: on Saces sell. Spl . ne = hire rite patho" 1 Mh E pace sti ip fk uP : ’ ui ht utes Me a] wiles rain - —o * vet ava x7 ‘adi ont, ens a4 re Aoi Tint ey ics ho tern’ fas EME A, yeh al Ay Pee NH a Shaaban we, he oie, oc) ft WE TE Oh tag PLATES AND MAPS IN ILLUSTRATION OF VOLUME V. SECOND SERIES, OF THE TRANSACTIONS OF THE GEOLOGICAL SOCIETY OF LONDON. LONDON: PRINTED BY R. AND J. E. TAYLOR, RED LION COURT, FLEET STREET SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY, SOMERSET HOUSE. 1840. Geol Trane, 24 Seria Vol.V FL XIX. ~Ay— NERKORT IA Lon, COALBROOK DALE. New Red” anaes iS aise Kinnersley . Ms Pipeayetone tien iS stan lod Coat — | ; | Carboniferous Limestone ~ tion oS Brats : os — Iiltes halt House : | rd Fiocks Wappenchall < L . 5, — 5 suits } Se 4 Rocks Hadliey Horton Wve epee © s ee ‘| \rimartone | (a) ae S ( 1 4 3s FH ) Wenlock Rocks ‘ 7 Vy 5 FS thale j \ . Z : ? ee 5 | prensl New Lodge \ Z Ce r a — Tea ree 4 Trap Hard sclasts < 5 - . WW Se gk os omen) Gat, , with plants Trap Grantte = ; Vj : o@ = od, = Ts : : x | to. Daretnaor : NINE, to SS. z : “« SSE Stephens Launceston Vt Potherwin po — ! > = a 7 GJ : J s/h WOLD LT Len FT Trop Trup Slaty Limestone Tup a s u ue e yo. ' Carboni¥erous Rocks Dewan Dan Rook = Granite 2 Upper 4 i Group 5 } Fig. 5. io 0m TE Ue aii te) he vk Ub ana) Bion tart Head TE efit Pp. 656. Ss | Bolt Head Yeurdon Stake Loint Erme Mouth Hopes ve Mouth ‘ 3 ; : 5 5 rE Ward: Schiae Giloribe i Mi State 2 . ane: | Sauber : < . E 4 a hlor and Mica Slates Staty Rocks Limestone ded Nanustone i Ennthk taste Ege Chlervtte Sehirt Gla Maa Th ete State with Quarte Yeuns (ifacamonpliic Molekesy m ] . fig. 8 From Dartmoor to Abbots Kerswelt. From Heath 1 N. of Tavistock to Thistle Brook (Lower Culm Measures’ " p-652 note! : 3 & ee NW OW ate’ = ¢ Dartiaoor ea as S.E.b B. = Ber | : iy fh > 2 eS 3 > altered Culm Measures? | eas ? ta " = 5 ; acs e 5 eS Pee Dawns : Culm trough) North of 23> tin, T Phistte Abbotelierswell - J Fault? Trap Trap Trup Limestone Limestone Explanation of Colours. © ax that wed inthe Map: but the Devonian System (Old Red Suntstone! which in the Map is represented | | | i} H i) 1 | ‘ | | The Carboniferous Svsten — Gdin Measures &e! is represented in all the Sections by the same black: tint 5 hy a reddish brown.is in the Sections divided into groups cach distinguished by a separate colour Ceol Trans.28 Series Volt VFLLll. DEVONSHIRE. (\q, \" \ Cx wt A S aan “Ss TAD ! : ! rd nna ‘te: Geol Drans, 2 Series Vol VLALM. DEVONSHIRE. an Ys igy) MLE LM sis itt al Ceol. Trans. 20 Sexes, Vol. * ——— UPL LIN a Geol. Trans. 2 as vries. VaLVKLLV. CORNWALL. (\ | AWE A AN v7 RY \: i % AA i f 1 ik } ‘ y { i Cool Trans. 22 Series Vol. VAAL VT. DEVONSHIRE. : LL ENS [ALLLNDISSN SS Ji) a : Grol. Trans. 2% Series Val VFt. LVL. ~ DEVONSHLILRL. Ceol Drans: 2?” Serves. Vol: V Lb: 32. . Frans Geol. Sow. 2 Aeris lols LL.59 Line of section Fig. 0 Zeitter, Sculp Goel Poe otha bbsL60. Ved Siw Geol, Trans.2” Series Vol VP? LANL. i , | i i ) i | h 1 I i : 1 H i fi Taal 7) / ; t il MN LIBR 5 (T/A scl Ml CALIF ACAD OF the tsi Sa peer cSicas