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" . +0 . . . . ond “— . *? . + a —e eee ee ee eee I eae aeeere -* ——— = mere ooreeer . é ‘ SSO. ee (P f =aO/ THE ~ QUARTERLY JOURNAL GEOLOGICAL SOCIETY OF LONDON. EDITED BY THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY. 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 prohabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. —Novum Organum, Prefatio. VOLUME THE EIGHTEENTH. 1862. ZO OT PART THE FIRST. PROCEEDINGS OF THE GEOLOGICADSOGIETY. oc SOOO NPN a0 22 Eh OE Poe SRL LONDON : LONGMAN, GREEN, LONGMANS, AND ROBERTS. PARIS :—FRIED. KLINCKSIECK, 11 RUE DE LILLE; BAUDRY, 9 RUE DU COQ, PRES LE LOUVRE; LEIPZIG, T.O. WEIGEL. SOLD ALSO AT THE APARTMENTS OF THE SOCIETY. MDCCCLXII. List OFFICHRS OF THE GEOLOGICAL SOCIETY OF LONDON. PrestVent. Professor A. C. Ramsay, F.R.S. Oice-BPrestvents. Sir P. G. Egerton, Bart., M.P., F.R.S. & L.S. | J. Carrick Moore, Esq., M.A., F.R.S. Sir Charles Lyell, F.R.S. & L.S. Prof. John Morris. Secretaries. Prof. T. H. Huxley, F.R.S. & L.S. Warington W. Smyth, Esq., M.A., F.R.S. Foreign Secretarp. William John Hamilton, Esq., F.R.S. Treasurer. Joseph Prestwich, Esq., F.R.S. COUNGIL, John J. Bigsby, M.D. John Carrick Moore, Esq., M.A., F.R.S. Sir Charles Bunbury, Bart., F. & L.S. | Prof. John Morris. Robert Chambers, Esq., F.R.S. Sir R. I. Murchison, G.C.St.S., F.R.S. & L.S. Ss. L.S. Sir P, G. Egerton, Bart., M.P., F. R.S.&L.S. | Robert W. Myine, Esq., F.R.S. Earl of Enniskillen, D. C. L., ERS. Joseph Prestwich, Esq., F.R.S. Hugh Falconer, M.D., F.R.S. Prof. A. C. Ramsay, F.R.S. William John Hamilton, Esq., F.R.S. G. P. Scrope, Esq., M.P., F.R.S. Leonard Horner, Esq., F.R.S. L. & E. Warington W. Smyth, Esq., M.A., F.R.S. Prof. T. H. Huxley, F.R.S. & L.S. Alfred Tylor, Esq., F.L.S. John Lubbock, Esq, F.R.S. & L.S. Rev. Thomas Wiltshire, M.A. Sir Charles Lyell, ERS. & L.S S. P. Woodward, Esq. Edward Meryon, M.D. Assistant-Hecretary, Librarian, and Curator. T. Rupert Jones, Esq. Clerk. Mr. G. E. Roberts. Library and fHuseum Assistant. Mr. H. M. Jenkins. i Oe, TABLE OF CONTENTS. PART I.—ORIGINAL COMMUNICATIONS. Page Beck zs, 8. H., Esq. On some Natural Casts of Reptilian Footprints in the Wealden Beds of the Isle of Wight and of Swanage .... Binney, E. W., Esq. On some Fossil Plants, showing Structure, from the Lower Coal-measures of Lancashire. (With 3 Plates.) ——. On some Upper Coal-measures, containing a bed of Limestone, ESS ES gl en Botton, J., Esq. On a Deposit with Insects, Leaves, &c., near oe ae er DON CERCA Se SR hs Nc ea CARRUTHERS, W., Esq. On a Section at Junction-Road, Leith .. CxiarxkE, The Rev. W. B. On the Occurrence of Mesozoic and Permian Faunz in Hastern Australia ......... 0.0... ceca Davinson, T., Esq. On some Carboniferous Brachiopoda collected in India by A. Fleming, M.D., and W. Purdon, Esq., F.G.S. ES ESE TOS gy eee oe OO Dawxuys, W. Boyp, Esq. On a Hyzena-den at Wookey-Hole, near I eT arate W'Sfb io. bp 1ae iy Shik Whe oe hae aed a oe Dawson, Dr. J. W. Notice of the Discovery of Additional Remains of Land-animals in the Coal-measures of the South Joggins, ES RE SE BE men —. On the Flora of the Devonian Period in North-eastern TENE EI DECS) eo ie o's ka he ee 8 oot vo eisphe es ves Denison, Sir W. On the Death of Fishes during the Monsoon off aS A li a a Sai ar Everest, The Rey. R. On the Lines of Deepest Water around the MIREERCEUMT Tos opts hee esc a seg eye vs ahs sig he's Fatconer, Dr. H. On the Disputed Affinity of the Mammalian Genus Plagiaulax, from the Purbeck Beds .................. FisHer, The Rey. 0. On the Bracklesham Beds of the Isle of Wight CIES Oe Parent ba: SA AO Gerktg, A., Esq. On the Date of the Last Elevation of Central nv olb Giodid oo 0.50 veo 0 Fela Gawd alee WOR di os GEMMELLARO, Sign. G.G. On the Volcanic Cones of Paterné and EMR IABERAIA), REUAUE oo ssc bins ln's ov o¥ We abioiele ca p'eln'e 445 106 437 274 450 244 25 115 296 453 lv TABLE OF CONTENTS. Page GusnER, Dr. A. On the Petroleum-springs in North America. Es ss treite'| Nisei a -atatahata sos seh dehipe ave ning a Ren OMG IRA acai’ w lage wTenouel Harkness, Prof. R. On the Metamorphic Rocks of the Banffshire Coast, the Scarabins, and a Portion of East Sutherland ...... 331 ——. On the Position of the Pteraspis-beds, and on the Sequence of the Strata of the Old Red Sandstone Series of South Perthshire. 253 On the Sandstones and their associated Deposits in the Vale of the Eden, the Cumberland Plain, and the South-east of Dum- PIOSSHITS: YS Sielar te ce an ees wala tie eee Slee sete Oe setetel alesis gegen 205 Havenrton, The Rey. 8. Experimental Researches on the Granites of Ireland. Part II. On the Granites of Donegal .......... 403 Heer, Prof. O. On certain Fossil Plants from the Hempstead Beds of the Isle of Wight; with an Introduction, by W. PENGELLY, Hag. s@With dh Plates) <5. cl anes ft cake miei pie aurea ate ete 369 Histop, The Rev. 8. Supplemental Note on the Plant-bearing sandstones of Central India: 5. ..t:40. elise is pie ate etal ates 36, 118 Honeyman, The Rey. D. On the Geology of the Gold-fields of Nova Seotia, | Abridged. | cg kiy aificticss bie ie tae co eens eee a. 042 Hut, E., Esq. On Iso-diametric Lines, as means of representing the Distribution of Sedimentary Clay and Sandy Strata, as di- stinguished from Calcareous Strata, with special reference to the Carboniferous Rocks of Britain, (With 1 Plate.)............ 127 Huxuery, Prof.T.H. OnaStalk-eyed Crustacean from the Carboni- ferous' Strata ‘near Paisley) oi Vo... ce « ciepaecs oh sha eee 420 —-. On new Labyrinthodonts from the Edinburgh Coal-field. CW ith D Blate, yin a oi lere\s atater open mseand 4 aisha See meueaetee eae Boncec cll On the Premolar Teeth of Diprotodon, and on a new Species of that Genus, ).(With 1 Plate.) ¢4).).)0 2. : i vesasmpio @ 0x 247 Verrcu, J. G., Esq. On a Volcanic Phenomenon witnessed in IN a og ol ise indi didn: 9 acy a: olsra: a.eha.nc8lohoy & Wairaker, W., Esq. On the Western End of the London Basin; on the Westerly Thinning of the Lower Eocene Beds in that Basin ; and on the Greywethers of Wiltshire................ 258 Waurrtey, N., Esq. On some Flint Arrow-heads (?) from near Baggy cranaren Devon,» (Abstract. |) (iis seve ven ee ie cuiees 114 Wvarrt, J., Esq. On some further Discoveries of Flint Implements » “mm the Gravel near Bedford. [Abstract.] ............ceeee. 113 SIO 5 oc oda cnis ed cress doscevercssncennorensssseres i DMMMMEEMNED AGQTOSS. (00005 c soe cee nese eens sdtberesetcessen XXVii East of Foreign Members .........sseccseccsccsesccsvstsvcecs xx ne i tinaton Modaists ...6 ccc. ccccsecsnscvsstvasces Xxi Donations to the Library (with Bibliography)...... x, 43, 147, 278, 454 EXPLANATION OF THE PLATES. PLATE Pace I CARBONIFEROUS BRACHIOPODA FROM InpIA, to illustrate Mr. Da- TL vidson’s paper on Carboniferous Brachiopoda collected in India ‘ by Dr. Fleming and Mr. Purdon ...............00008- to face page 309 III. WisH-Remarns rrom OretTon AND Fartow, to illustrate the paper by Messrs. Morris and Roberts on the Carboniferous Limestone of Oreton and Harlow 3.5... sacar. anes ss scaler si nasc cree ate 105 IV. ) Srgmnaria VASCULARIS AND LEPIDODENDRON VASCULARE, to illus- NG trate Mr. Binney’s paper on some Fossil Plants from the Lower VI. Coal-measures of Lancashire .4:..562 d5s.0. shee ee Hag VII. Map or Encuanp, WALES, AND PART OF ScoTLAND, to illustrate Mr. Hull’s paper on the Distribution of the Carboniferous Strata. 146 VIII. Sxercu-map oF PART OF THE ANCIENT GLACIERS OF SwITZERLAND, to illustrate Prof. Ramsay’s paper on the Glacial origin of Lakes. 204 1x Reptitian Remains rrom Nova Scorta, to illustrate Prof. Owen’s X paper on Fossil Reptilia discovered in the Coal-measures of the South. Joggins;. Nova Scotia. 2. )c022itoc—.s<2 satecses: Cayuga Lake ... StaJOhN: scassace | St. John ......... se N.-E. America .. } Isle of Wight .. New York ...... ro a oh : New York ...... | SAD) a ES Page. vill Name of Species. Formation. Locality. PLANT (continued). Lepidodendron Chemungense ......... i os steal —— corrugatum. Pl. xi. f.10 ...... : ova Scotia...... Gaspianum. PI. xiv. f. 26-28, Ue ee ANUP]. xvaly DS? wees set sc toaneea sees St. John ......... —— vasculare. Pl. vi. f.1-5 ........ Pee ee: \ Lancashire ...... Lepidostrobus globosus ............seeee Perry, Maine ... Richardsont oso. c.r. 5. -senenneerians Perry, Maine ... Leptophleum rhombicum. PI. xii. £58, ands PE Xvi Tl Do! eenconcstesneck Devonian...... British N. Amer. Lycopodites Matthewi .................- St.John: . ssc : Vanuxemii. - Pl. xvii. f.57 ...... New York ...... Meraphyton(e)) .ccuceacssncdse meteecanasas \ British N. Amer Nelumbium Buchii. Pl. xviii. £19 ... eee } Iste of Wight .. Neuropteris polymorpha. FP1.xv. f.36.| Devonian...... Carlton — eee serrulata. PI. xv.f. 35............ Devonian...... St. John) ccaee: Nymphéea Doris. Pl. xviii. f. 8-11 ...| { Hempstead | iste of Wight Pecopteris (Alethopteris). Pl. xvi. f. 49. St. Johnie —— discrepans. Pl. xv. f. 40 ......... St. Johnsen ee ingens. » Pl. XV. £. 41.......c.0ce00- Sé. JOLIN, -eeeaiere Pinnularia fevalans. PY Met 22). N.-E. America Psilophyton elegans. Pl. xiv. f. 29, 30, SLC 6 Beeps a 0 OR ee Carlton)jeea ae ? ae NOT ROTO OB Soe A Sea acberodene sep : N.-E. America PTIDCEPNS, seisicaeewatuiiaimeseratesmanes Devonian...... Gaspé - iene Rhachiopteris cyclopteroides .........+.. New York ...... pinnata. Pl. xvi.f. 60 ............ New York ...... punctata. Pl. xvi.f.61 ......... New York ...... WUT TAL, Waco casngaeenescccseatieasstst Ohiowss).3.c5 ee tenuistriata. Pl. xiv. f. 32, and Pl. xvi. f.45,46 ...... siseieesiaineeai cose Leer fueghee Seok Ac Babalimeajor,sp(? ses cath as usietees aeaeeees _| { Hempstead } Isle of Wight Selaginites formosus ..............ss0eees Devonian...... Gaspé vo. nae Sequoia Couttsie. Pl. xviii. f.1-7 ... Pen | iste of Wight ... Sigillaria palpebra. Pl. xiii. f. 12...... St. OM) caer acute ————-_ SIMPIIGIEAS...,..cssseeusdensraccucsons Devonian...... Lake Erie ...... —— Vanuxemii. PI. xii.f.7 ......... Oswego ......... vascularis. Pl. iv. f. 1-6, and! |) Lower Coal- : Lid tepals ps SA ee ree AE a ul } measures. | Lancashire ...... Sphenophyllum antiquum ............... St. JOHN) -cacssece Sphenopteris Harttii. Pl. xvi. f. 48.. St; JOhM +... ean —— Hitchcockiana. P\.xvi.f.51 ...| | Perry veneer marginata. Pl. xv.f.38 ..... moe fel St: John’ ..438 Stigmaria exigua. P\. xiii. f.13 ...... New York” ise ACOIGES, VAN. | enssncnaecdceenerts eens | St. John ......00. Syringodendron gracile. P\. xiii. f.14.|} ‘ Devonian...... OBI6! ccatenconeeee Syringoxylon mirabile, Pl. xii. f. 1-5. Lake Erie ...... Trichomanites (?). Pl. xvi. f. 50...... St. JOHM .... wa. Trigonocarpum racemosum. PI. xvi. BAT iser navn saptee soasatein si amen eee ne St. JOHN vevsseat Uphantenia Chemungensis. Pl. xvii sing vein da aen Pasian races hak leant New York & Ohio Page. 318 374 316 324 325 1x Name of Species. | Formation. | Locality. | Page. FoRAMINIFER. Nummulina planulata, var. ced Barené {| Alum Bay, Isle ae 93 wichiana. Wight. Motivsca. (30.) (Brachiopoda.) Pemers eyes, PLi£.6 ............ \ (ener —— subtilita, var. grandis. Pl. i.f.7,8 28 Aulosteges Dalhousii. Pl. ii.f.7 ...... 32 Camarophoria Purdoni. Pl.ii.f.4... 30 Orthis resupinata. Pl.i.f.15 ......... 31 NEE MIET Toes naxinganwesscccensdenes: 31 — costatus. Pl.i.f. 20,21 ......... 31 — Humboldtii. Pl ii.f.6 ......... 32 longispinus. Pli.f.19 ......... 31 — Purdoni. Pl.ii. f.5 ............00. 31 — sSemireticulatus ...............sc00e 31 ———— striatus. PI.1.f. 18 ..........0.00 31 Retzia radialis, var. grandicosta. Pl. i. £.5 _) ae 28 Rhynchonella pleurodon ............... 29 Remit Pits... Pe houtersus anyeue a 29 - Moosakhailensis. Pl. ii. f. 2...... 28 — striata. Pl.i.f.9,10 ............ 28 Spiriferina octoplicata. Pl.i.f. 12,13 29 Streptorhynchus crenistria_ ............ 30 crenistria, var. robustus. PI. i. ee ilalacis banker encanta one sciaes 30 pectiniformis. Pl.i.f.17 ...... 30 Strophalosia Morrisiana. PI. ii.f.8... 32 Terebratula biplicata, var. problema- EN Sa Ol sasivesnnccesscess.ccenss 26 —— (vel Waldheimia) Flemingii. Pl. i. . py seesseseesees POSES se senree eeresesee 26 — Himalayensis. Pl. ii.f.1......... 27 —— subvesicularis. Pl.i.f.4......... lelg 2¥ ( Gasteropoda.) Chiton Burrowianus. Woodcuts, f. 1, 2 234 —— coloratus. Woodcuts, f. 3-6 ...| | Mountain Yocloh: | 234 ——? Woodcuts, f. 7,8 ............... Limestone PE ees: tiae 235 —— (sp.nov.?). Woodcuts, f.9,10 236 CRUSTACEUM. Pygocephalus (?), Woodcut ......... | Coal-measures | Paisley ............ | 421 Name of Species. Formation. Locality. Page. Pisces. (5.) Cladodus. - Pl. iii. f..6 2 .....000.sesenens \ \ Deléodus,. Pl. 0s fae 23, 45 vecscovseces Palatal tooth (Deltodus?). PA. iii. Chchonifer | RM VO O.2s' acheactmscaeprascancs cece Aran # ge + Shropshire ......| 103 Alnnlate. sR GiseBese. com... cect rs ages Pterichthys macrocephalus. PI. iii. | f. 7,8,9; and Woodcuts, f. 1, 2,3... } Reptinia. (12.) Dendrerpeton. Pl.ix.f.15 .......0.... \ 244 Acadianum. Pl.x.f.5-7 ...... 242 Fiylerpeton, “Plax. £.17, 18)......-0-.<: 241 Dawson.) Pix fGen 241 ; : Hy os ed GI ETE gD eH Uo Coal-measures| Nova Scotia ... { 939 ——Lyelli. Pl. ix. £ 1-6, 14, and PLES Ls Adoaseninct acon dderisnssacecriens 238 ie Wymanni. Piaixsto, 112. 13 240 PPP IS ere Lay age J [| 242 Iguanodon Footprints. Woodcuts ...| Wealden......... Hastings.........+. 248 Loxomma Allmanni. Pl. xi.f.1,2 ...| Coal-measures | Gilmerton ......... 291 Pholidogaster pisciformis. P\.xi.f.3,4| Coal-measures | Gilmerton ......... 294 Reptilian Footprint. Woodcuts, f. 2-4| Wealden......... Isle of Wight...... 445 Mammatia. (7.) Cheiromys Madagascariensis. Wood- CUE SAU sian meinpacinasgeseec en cuernaar Recent .........| Madagascar ...... 368 Diprotodon australis? Pl. xxi. f. 1-3 | Tertiary ......... Queensland ......} 422 minor. Pl. xxi. f.4—6 .....0...+:- Tertiaryic. coset: Queensland ...... 422 Hypsiprymnus Gaimardi. Woodcut, io BaaciineerachepecbuaniegcuonToansBce ae ser | MCCEMUEsse eens. Australia .......:.| 366 Plagiaulax Becklesii. Woodcuts,f.1-5, CVI A ieee seen ade coniop sacs SACOM: Purbeck: .......3. Swanage............ 366 —— minor. Woodeut, fed) Sedccees: Purbeck zasccsse: SWANALCsacenenceeee 367 Thylacoleo Carnifex. Woodcuts, fe LON eres oscitnsdsievasnae vr sesigoaseene TGMiATY, vesicneas: Australia ox. .<0se 368 MiscELLANEOUS. Flint Implement. Woodcuts, f. 2-5...|Pleistocene? ...| Wookey Hole, 118 | near Wells. ERRATA ET CORRIGENDA. Part I.—ProcEgEp1nGs. Page XXxxill, line 20, for flints read fluids. Pages Page ” xxxix, lines 3 and 4 from bottom, transpose of which and position of. 16, line 10, for Fluoric read Hydrofluoric. 69, description of the woodcut, for the uwpper* read x. 100, line 28 of Table, for Cricacathus read Cricacanthus. 107, line 3, after as insert in. 109, line 21, for with read as to the woody cylinder in. 131, line 24 from bottom, for vlaley read valley. 133, line 9, after had znsert their. 137, line 35, for Charnworth read Charnwood. ,, last line, insert during the deposition of that rock. 138, line 41, for in read on. 198, line 26, for 685 read 646. ,, line 28, for 1940 read 1979. 201, line 15, for 1992 read 1979; for 1048 read 1229. 238-244. Dr. Dawson having informed the Editor of the Quarterly Journal of the Geological Society that some errors in Professor Owen’s paper on Fossil Reptilia from the Coal-measures of the South Joggins had been caused by an accidental intermixture of the specimens, which was not detected until after the publication of the August Number of the Journal, a complete list of the Hrrata thus rendered necessary has been given in the Appendix at page 244. 263, Diagram-section, for 4° read sea-level ; below b? insert 18, 271, line 8, for Woolwich read the Isle of Sheppey. 275, line 17, add Shaft No. 10. 276, line 11, add Shaft No. 11. 279, last line, and line 7 from bottom, for Hall read Hull. 280, line 28, after Proceedings insert vol. iv. No. 53, 1861. 281, line 24, after Epoch inser¢ (10 plates). 283, line 27, for Tynside read Tyneside. », last line, after portion insert (21 plates). 284, line 4, after grandis.) insert (7 plates). ,; line 6, after portion insert (13 plates). 287, line 27, for Barnell read Burnell. Pages 296-329 inclusive. A delay in the transmission to Dr. Dawson of a proof of his pepe having occurred, the Author’s corrections were not received until after its publication, and the following list of Hrrata has consequently become necessary :— Page 299, line 30, for M‘Clakeney’s read M‘Closkeney’s. » line 30, for Cones read Coves. », line 39, for Fort House read Fort Howe. 305, line 8, second column, for decurrens read discrepans. , line 11, first column, for Goeppert read Lesquereux. xi Page 309, line 26, for Skaneatales read Shenectales. ,, 910, line 4 from bottom, for specimen read specimens. ,», 913, line 14, for Haughton read Houghton. » 914, line 9 from bottom, for pinneformis read penneformis. » », line 7 from bottom, for were read was. » 921, line 25, for Davaillioides read Davallie. 323, line 27, for Rimeriana read Remeriana. », 9324, line 5, for Mr. Lann read Mr. Lunn. » 9») last line, for lineata read hirsuta. », 920, line 12, for znvested read inverted. » 9327, Table, No. 57, for decurrens read discrepans. », 929, Description of Plate XIII. fig. 25, for C. acutwm read C, obliquum. XV. fig. 39, for ob¢usilobus read curtilobus. *) - » fig. 40, for decurrens read discrepans. (See also the Appendix to Dr. Dawson’s paper, p. 329.) ” te 29 ” Page 342, line 8 from bottom, for mispickle read mispickel. ,», 995, line 1, for suppositian read supposition. »» 9 line 7, for that valley read Ghee valley. 400, line 4 from bottom, for E.S.E. read W.S.W. 401, line 2, for N.N.E. read N.N.W. line 8, for H.S.H. read W.S.W. lines 14 & 15, for Dranse and Durance and their tributaries read Drance and its tributaries. 402, line 9, for Durance and Dranse read Drance. ,, 421, line 4, after Paisley insert (Twice the natural size. ). ,», OAl, line 4, before Very insert 6. 3 ” 9 ” Part II.—MuIsce,LaNnEovus. Page 6, after line 35, insert By Fr. von Haver. » LO, line 36, for those read then. », 28, line 5, for seiner read seinen. » 95 line 33, for rom read from. GEOLOGICAL SOCIETY OF LONDON. ANNUAL GENERAL MEETING, FEB. 21, 1862. REPORT OF THE COUNCIL. Tue Council of the Geological Society, in presenting their Annual Report to the Fellows, have great satisfaction in pointing out the increasing numbers and general usefulness of the Society. They have, in common with the entire nation, to lament the loss of H.R.H. the Prince Consort, one of our extraordinary Members, from the small number of whom we have also lost H.M. King Frederick William IV. of Prussia. In all, the Society has lost by death twenty-seven, some of whom were among the oldest and most highly honoured of its Members. But during the past year forty new Fellows have been elected, thirty-four of whom have duly paid their fees, which, with eight previously elected, who have since paid their admission-fees, makes up the considerable number of forty-two new Fellows. . The resignation of three persons has been accepted. Two Foreign Members have died during the past year, and the place of one of them has been filled by the election of a new Member. The total number of Fellows at the close of 1860 was 922; at the close of 1861, 939. During the years 1860 and 1861, some heavy special expenses have been incurred, by order of the Council, which have been defrayed out of a special source of income, viz. the Bequest-fund, of which £500 have been drawn, leaving a balance of £300 yet undrawn. ‘Taking these unusual sources of income and expenditure into account, the Income of the Society for the past year has ex- ceeded the Expenditure by the sum of £125 3s. 8d. The amount of the Funded property of the Society is £4350. Among the unusual items of expenditure may be cited the donation of £70 to Mr. Nichols, the Society’s late clerk, authorized by the General Meeting; £50 ordered by the Council towards the VOL, XVIII. a li ANNIVERSARY MEETING, further arrangement and naming of the Foreign Collections ; £40 19s. for Cabinets for Australian specimens; and a sum of £43 9s. 6d. for the Library. The Council have to announce the completion of Vol. XVII. of the Quarterly Journal, and the First Part of Vol. XVIII. They have authorized the distribution of the Journal to the Foreign Members of the Society. The arrangement of the Foreign Collections has been diligently continued, and for this purpose the second temporary Assistant, engaged at the recommendation of the Special Museum Committee, has been retained up to the present time. The question of the amount and nature of the permanent assistance required for the efficiency of the Library and Museum has engaged the attention of the Council, and is at present in the hands of a Special Committee. With reference to the Greenough Map, the Council have to an- nounce that, after unavoidable delays, the third sheet will soon be ready for publication. Tn conclusion, the Council have to report that they have awarded the Wollaston Medal to Mr. Robert A. C. Godwin-Austen, for his various researches during the last twenty-eight years, illustrating in a very original and remarkable manner the physical geography of a large region of Kurope during by-gone periods, as mainly com- prised under the four following heads :— 1st. For his elaborate “ Memoir on the Geology of the South-east of Devonshire ;” wherein he pointed out the different periods of disturbance from paleeozoic to almost recent times in that complicated tract, as based upon actual observations made between the years 1834 and 1840, both inclusive*. 2ndly. For his observations on the Geology of the South-east of Surrey, which, with his Memoir on the Gravel Accumulations of the Valley of the Weyt, are explanatory of the changes of land and water in the South-eastern region of England and adjacent parts of France; whilst his paper “On the Sands of Farringdon ” treated of that.deposit as an intermede between the Lower Greensand (Neocomian) and the Portland Oolite§, This memoir, together with other papers in our Journal, indicate his views of the probable con- figuration of the land and water in the Western European area during the Mesozoic or Secondary period ||. 3rdly. For his original and striking Memoirs on the Valley of . the English Channel and the superficial accumulations on its coasts, which define the former physical geography of the South of England and adjacent parts of France, particularly during the Pleistocene period. And, 4thly. For his bold and ingenious hypothesis, founded on the relations of the older rocks in the North of France and the South of * Geol. Trans. 2nd series, vol. vi. p. 433, +t Proc. Geol. Soc. vol. iv. pp. 167, oli t Quart. Journ. Geol. Soc. vol. vii. p. 278. Quart. Journ. Geol. Soc. vol. vi. p. 454. i Quart. Journ. Geol. Soc. vol. vi. p. 69, and vl vii. p. 118, ANNUAL REPORT. iii England, which suggested the probable extension of the younger palzozoic (Carboniferous) deposits* beneath the Cretaceous group around our metropolis, to the exclusion, in that area, of the Triassic, Liassic, and Oolitic deposits ft. The balance of the proceeds of the Wollaston Fund has been awarded to Professor Heer, to assist him in his important inyesti- gations into the fossil botany of the Tertiary Strata. Report of the Library and Museum Committee, 1861-62. The Museun. Your Committee have much pleasure. in reporting that several important additions have been made to the Foreign Collection since the last Anniversary. Among them may be noticed the large collections of Rocks and Fossils from several German localities, presented by the President ; a most valuable series of Reptilian and other fossils from the coal of Nova Scotia, presented by Dr. Dawson, F.G.8. Fossils from Gothland, presented by Dr. Lindstrém, and from the Andes by Mr. David Forbes, F.G.8. Also a number of South African specimens, presented by Dr. Bowerbank, Dr. G. Grey, Mr. G. W. Stow, the Royal Geographical Society, and Dr. A. G. Atherstone; while Rocks and Fossils from British localities have been presented by the President and other donors. The Library and Museum Committee stated in their last Report that the collection of European Fossils, occupying 48 cabinets con- taining 336 drawers, had been nearly re-arranged according to the plan determined upon by the Special Museum Committee at their Meeting on the 25th of June, 1860, and that a catalogue of those collections had been prepared by the President, Since that time the remaining Foreign Collections have been similarly re-arranged under the direction of the President and Assistant-Secretary, and Catalogues of them have been made by the President uniform with that of the European Collections, in accord- ance with the wish expressed by the Committee in their last Report. They occupy 68 cabinets, containing 490 drawers as follows :— Cabinets. Drawers. eee 1 Mes Sei Ee Pe 145 Seema KN. eS | 7 a ee 12, North America .. PI aie a iis 144 West Indies ...... he Wa ne ee 39 South America .. oO, a a 22 Australasia ...... A re are 48 Miscellaneous Dh ie exe ce 24 68 490 * Quart. Journ. Geol. Soc. vol. xix. p. 384. t See Notices of the Proceedings of the Royal Institution, part 8. p. 511. a2 iv ANNIVERSARY MEETING. On the 19th of April, 1861, the Council granted the sum of £50 to the Special Committee, to be expended in re-naming the specimens in the European Collections; and the services of Mr. J. W. Salter, F.G.S., Mr. R. Etheridge, F.G.S., of Mr. H. Woodward, and of Mr. 8. P. Woodward, F.G.S., were secured for that purpose. Of the specimens named by them the following have been placed upon tablets, labelled, and numbered; and a detailed catalogue of the contents of each drawer has been made and placed therein. Drawers. Norway ..... taPo PLLA. others ‘ 5 Uddevalla, &c. .... Postpliocene .... 2 Sweden a alawewe. Siburiams ets hes 2 Antwerp ........ sp LIOReNe ee asd, eta 1 TE GUTRING “G2ouieee es: Miocene ......% 2 Paris, Basi ac..uss 4 Hocene 3 diznedeis 9 Normandy jj...) 2 )3"2 ye) masses. i.15 ete 6 North America .... Cretaceous ...... 1 28 The naming of the Tertiary fossils has not yet been verified by Mr. S. P. Woodward: for the accuracy of the rest, Messrs, Salter and Etheridge are responsible. Furthermore, ten drawers of fossils, chiefly from the Kifel and the Rhenish provinces, have been tabletted, labelled, and named, but not arranged zoologically or certified. The Rev. T. Wiltshire, F.G.S., is making progress with the re- naming and re-arrangement of the British specimens of Cretaceous fossils, which he has been good enough to undertake. In addition to the foregoing Report of the work done in the Museum during the past year, the Committee subjoin for the in- formation of the Council the following summary of the present state of the Foreign Collection as a whole, viz. :— 28 Drawers of Fossils are now completely arranged and named. 10 Drawers of Fossils are nearly complete. 479 Drawers of Fossils are arranged, but require naming, And 234 Drawers of Rock-specimens are arranged, but not named. Tol A series of Coloured Maps, illustrative of the Geological Areas to which the several divisions of the Foreign Collection belong, have been provided under the care of the President. Those specimens of Fossils from Foreign localities, which are too bulky to be placed in drawers, have been carefully washed and labelled ; each one has also been packed in a separate paper, and the name, locality, &c. written upon its outside. The glass doors of an old cabinet have been converted into a wall- ANNUAL REPORT. Vv case for the reception of a number of large specimens, chiefly coal- plants from Nova Scotia and Cape Breton. Two new cabinets, ordered by the Council at the cost of £44 14s., have been supplied for the reception of certain of the Foreign Collections ; one, consisting of 24 drawers, contains specimens from the West Indies and South America; the other, consisting of 64 drawers, contains the Australasian Collections. The latter cabinet is placed in the tea-room. The Special Committee have distributed duplicates to public bodies, donations haying been made to the British Museum, the Museum of University College, and the Royal Military College at Sandhurst. A considerable number of duplicates still remains for disposal. In conclusion, the Committee desire to record their sense of the great and unremitting labour (whose value has already been recog- nized by the Council) which the President has. bestowed on the re-arrangement and general superintendence of the Museum. The Inbrary. In addition to the usual increase by donation and purchase, the Library has received important additions in consequence of the special yote by the Council of £35, for the purchase of various desiderata, among which may be mentioned— Kaup’s ‘ Urweltliche Siugethiere,’ Pander’s Monographs upon Silurian and Devonian Fishes, Sartorius’s ‘Atlas von tna,’ Rammelsberg’s ‘Mineralchemie,’ Carus and Engelhardt’s ‘ Bibliotheca Zoologica,’ H. D. Rogers’s ‘Geology of Pennsylvania,’ Ure’s < Dic- tionary of Arts, Manufactures, and Mines,’ and Dumont’s Geological Map of Europe. The supply of periodicals by exchange, gift, and purchase con- tinues to be large. Books and pamphlets, presented or purchased, have, as usual, been catalogued, shelved, and, when necessary, bound. The Assistant-Secretary reports that he has received valuable assistance in the Library and Museum from Mr. Jenkins and Mr. Stair. The Committee are glad to find that, though on an average above 100 works are simultaneously absent from the Library, and in use by the Fellows of the Society, but one case of irregularity in the return of such books has come under their notice, one Member of the Society, notwithstanding repeated applications, having as yet failed to return a work taken out by him two years ago. JOHN J. BIGSBY. ROBERT W. MYLNE. THOMAS WILTSHIRE. THOMAS H. HUXLEY. ‘vi ANNIVERSARY MEETING. Comparative Statement of the Number of the Society at the close of the years 1860 and 1861. Dec. 31, 1860. Dec. 31, 1861. Compounders .......... 1 VS eno 126 Residents ss .4 Ais eee Ae Soe ee ee 225 Non-residents .......... BSL GN ae 535 864 886 Honorary Members ...... URES UC de 4 Foreign Members........ GIO! Noe Ree ae 49 Personages of Royal Blood 3B—58 ww we — 1-54 922 940 General Statement explanatory of the Alteration in the Number of Fellows, Honorary Members, &c. at the close of the years 1860 and 1861. Number of Compounders, Residents, and Non-residents, Pecember Sist, L860 oP eee eee 864 Fellows reported as dead in two successive Reports, B59 sand SCO Kye cline erga ee eee 2 Fellows not included in last Report (Residents) .. “2 Add Fellows elected in 1860 and) Residents ........ 0 paid im 2661 245%. 268 oc Non-residents .... ae Residents ........ 13 ; -, | Res.-compounders.. 2 Add et elected and paid in 2 Non-restionta "i. Sete een: Wee ateee Bigot gna | Non-res.-com- Kg OULaeria t/a. sae 4 — 34 Add Fellow re-admitted °%.).). 01/22). dane eee 1 Odd Deduct Compounders deceased.... 2... 0.0. cee ee eee 3 Residents a Sey rn hy ON A ae. 6 Wemeareannlendteet He NU ean: Sete Uaioe 10 Residents resioned |. rove. Pe SAGA RR 3 — 22 889 Number of Honorary Members, Foreign Members, and ) 58 Personages of Royal Blood, Dec. 31, 1860...... f Add Foreign Member elected during 1861 .......... 59 Deduct Foreign Members deceased ..............-005 2 Honorary Members deceased ...............- i Personages of Royal Blood deceased ...,...... 2 — 6565 AS above | %.. vs 54 ANNUAL REPORT. Vil Number of Fellows liable to Annual Contribution, as Residents, at the close of 1861, with the alterations during the year. Number at the close of 1860 ........ cc ccce se eeeees 214 Add Elected and paid in 1860, but not included in last SE ee eae ohare eras ee a Add Fellow counted as Non-resident in making out last 1 Report 2... see ee eee eet e eee eee eee ane es | Add Elected in former years, and paid in 1861........ ig SEMUEE-RUUUIGLOU 2... ec geet se ee entree res 1 Non-residents became Residents ........... ee ay — 20 234 . a eee nee 6 ip isis chs .0a oy AWE ib AS bea oe 3 . — 9 As above,..... _ 225 DrcrAsED Fettows. rs ‘sonages of Royal Blood (2). His Royal Highness the Prince Consort, His Majesty the King of Prussia. Compounders (3). Dr. Fitton. | FF. Perkins, Esq. Lieut.-Gen. Sir C. Pasley. Residents (6). T. W. Atkinson, Esq. J. Otté, Esq. Sir W. Cubitt. Dr. A. R. Sutherland. Lieut.-Col. Dawson. G. E, H. Vernon, Esq. Non-residents (10). Sir A. de Capel Brooke, Bart. EK. Hodgkinson, Esq. Sir T. Cartwright. W. Hutton, Esq. J.J. Forrester, Esq. J. MacAdam, Esq. A. Hambrough, Esq. Col. Hon. M. L. Onslow. Rey, Prof. Henslow. Rey. J. M, Traherne, Foreign Members (2). M. Cordier, | M,C, Lardi. The following Persons were elected Fellows during the year 1861. January 9th.—William Charles Lacy, Esq., Gloucester; Robert Dukinfield Darbishire, Esq., B.A., 1 Heald Grove, Rusholme, Manchester ; George Charles Wallich, M.D., 17 Campden Hill Road, Kensington. Vili ANNIVERSARY MEETING. January 23rd.— William Weston, Esq., of Birkenhead. February 6th.—William Rutherford Ancram, Esq., 75 Inverness Terrace, Kensington Gardens; Thomas William Jeffcock, C.E., Woodside, Sheffield. aha 20th.—J. Frederick Davis, Esq., Walker Iron-works, New- castle-upon-Tyne; John Frederick Collingwood, Esq.,13 Old Jewry Chambers; Joseph Milligan, Esq., F.L.S., Hobart Town, Tas- mania; Henry Porter, M.D., Fellow of Queen’s College, Bir- mingham, Peterborough ; Richard Charles Oldfield, Esq., Bengal Civil Service, Farley Hill, Reading. March 6th.—Francis George Shirecliff Parker, Lieut. H.M. 54th Regiment, Roorkee; J. Gwyn Jeffreys, Esq., F.R.S., 25 Devon- shire Place, Portland Place. April 10th.—James Hector, M.D. Edinb., 13 Gate Street, Lincoln’s- Inn-Fields. 24th.—Daniel Mackintosh, Esq., Chichester; Richard Payne Cotton, M.D., Fellow R. Coll. Phys. Lond., 46 Clarges Street, Piccadilly. May 8th.—Robert Mills, Esq., F.S.A., Rochdale ; Edmund William Ashbee, Esq., 14 Rutland Street, Mornington Crescent; Captain Willoughby Osborn, C.B., Madras Army, Brunswick Hotel, Jermyn Street. 22nd.—Silas Bowkley, Esq., Mining Engineer, Batman’s Hill, near Bilston, Staffordshire ; John Edward Forbes, Esq., 3 Faulkner Street, Manchester ; Captain Francis Walker Henry Petrie, H.M. 1ith Regiment, Portsmouth, June 5th.—Joseph Tolson White, mee Mining Engineer, Wake- field, Yorkshire; William Boyd Dawkins, Esq., B.A., Jesus College, Oxford. —— 19th.—John Atkinson, Esq., Mem. Phil. Geol. Soc., Man- chester, Thelwall near Warrington; Major Nathaniel Vicary, Westgate, Wexford; Lord Rollo, 18 Upper Hyde Park Gar- dens. November 20th.—Charles Sanderson, Esq., C.E., Engineer-in-Chief, Bombay and Baroda Railway, Surat, Bombay ; Ralph Tate, Esq., Teacher of Natural Science, Philosophical Institution, Belfast, 42 Eglington Street, Belfast; James Ray Eddy, Esq., C.E., Carleton Grange, Skipton; Henry Worms, Esq., of the Inner Temple, 27 Park Crescent, Portland Place ; Haddock Dennys, Esq., 3 Perey Terrace, Lower Road, Islington. December 4th.—Samuel Harradan, Esq., 6 Westbourne Terrace, Barnsbury, London; Frederick Merryweather Burton, Esq., Gainsborough ;. Jonathan Sparrow Crowley, Esq., Lavender Hill, London, 8.W.; William Henry Paine, Esq., Stroud, Gloucester- shire; Edwin Witchell, Esq., Stroud, Gloucestershire; Henry Tibbats Stainton, Hsq., F.L.S., Mountsficld, Lewisham, Kent ; Captain Auguste Frederic Lendy, F.L.S.,° Sunbury House, Sunbury, Middlesex ; Isaiah Booth, Esq., Mining Engineer, Oaks Colliery, Oldham ; Don Ramon da Silva Ferro, Consul for Chile, 43 Moorgate Street, H.C, ANNUAL REPORT. ix The following Personage was elected a Foreign Member. Professor Gustav Bischof, University of Bonn. The following Donations to the Musrvum have been received since the last Anniversary. British Specimens. Specimens of Corals from the Lias; presented by the Rev. P.. B. Brodie, F.G.S. Two specimens of Flint with mammillated surface from church- tower, in illustration of Mr. Rose’s observations, published in the Proc. Geol. Assoc., No. 5, p. 624; presented by the Rev. J. 8. Henslow, F.G.S. 313 specimens of British Rocks and Fossils; presented by L. Horner, Esq., Pres.G.S8. Specimen of Cyrena-bed from New Cross; presented by J. Sparks, Es Specimens of Mountain-limestones (rocks and fossils) from cuttings at Casterton, near Kirkby Lonsdale, on the line of the Lune Valley Railway; presented by G. Jackson, Esq. Large mass of Anthracosia, from Coal-bed near Oldham ; presented by J. O. Middleton, Esq. Plant-bed from Upper Tilestones of Kidderminster, with Lycopodites (Pachytheca spherica) ; presented by Mr. G. E. Roberts. Cast of Flint-Implement from Icklington; presented by J. Evans, Esq. Suite of Fossils from Coniston Limestone and Shale; presented by J. O. Middleton, Esq. Boulders from the Gravel of Kelsey Hill and the Boulder-clay of Paul Cliff, near Hull; presented by J. Prestwich, Esq., F.G.S., and F. J. Smith, Esq., F.G.S. Two specimens of Boulders (Granite) from the West Rosewarne Mine, Gwinear, Cornwall; presented by H. C. Salmon, Esq., F.G.S. Specimens of Bones and Rocks from the Cuttings and Tunnels of the Worcester and Hereford Railway; presented by the Rev. W. S. Symonds, F.G.8. Specimen of Conglomerate with Tin-stone, from Relistian Mine, Cornwall; by A. Majendie, Esq., F.G.S. Specimens of Bones of Mammalia, from Wickham-lane Brick-field ; presented by W. E. Dawson, Esq. Specimens of Ventriculites, Serpule, &c., Upper Greensand, Compton Bay, Isle of Wight; presented by Major R. J. Garden, F.G.S. Foreign Specimens. 105 specimens of Foreign Rocks and Fossils; presented by L. Horner, Esq., Pres.G.S. Specimens of Fossils from the Bolivian Andes; presentcd by D. Forbes, Esq., F.G.S, x ANNIVERSARY MEETING. A group of Kraussia rubra from Algoa Bay, and specimens of Fossil Ferns, &c., from South Africa; presented by Dr. A. G. Ather- stone. A suite of specimens from Natal, collected by A. Holden, Esq. ; presented by the Royal Geographical Society. Nine specimens of Flint-Tools with specimens of Gravel, Brick-earth, and Bones from St. Acheul, Amiens; presented by T. R. Jones, Ksq., F.G.S. A suite of Rocks and Fossils from Western Australia; presented by' T. F. Gregory, Esq. Specimens of Titaniferous Iron-sand from Tianat, New Zealand, and of Stream-tin, South Australia ; Prosenved by Prof. Tennant, EGS. - Specimens of bee in Stalactite Bue Natal ; presented by Major . RJ. Garden, F.G.8. -- - Suite of Fossils from Pangadi, inten BReSeE iar by Captain Stoddard. Suite of: Fossils from Sunday River, South Africa ; presemind by G. W. Stow, Esq., and Captain Rock. Specimens from the Bryozoan Limestone of Mount Gambier, South Australia; presented by the Rev. J. E. Woods, F.G.S. 118 specimens of Rocks and Fossils from 26 localities in Saxony, 35 specimens of Rocks and Fossils from 15 localities in Bohemia, and 7 specimens of Fossil Plants from Giningen ; presented by L. Horner, Esq., Pres.G.S8. Specimens of Fossils from near Harrow, on the River Glenelg, Victoria ; presented by the Rev. J. H. Woods, F.G.S. A suite of Upper Silurian Fossils from Gothland ; presented by Dr. Lindstrom. Specimens of Volcanic Rocks from Lipari and Ascension ; ae by Sir C. Bunbury, Bart., F.G.S. Twenty Rock-specimens from Borneo; presented by Mr. Russell. Fossil Bird-bone and Fossil Bone of Mammal from New Zealand ; presented by Prof. Huxley, Sec.G.8. Ten specimens of Wealden Coal, &c., from Obernkirchen, Dornberg, Osterwald, &c.; presented by T. R. Jones, Hsq., F.G.S. Specimens of Dicynodon from Cradock, South Africa; presented by Dr. G. Grey. Specimens of Fossil Bones from Lunel Viel; presented by M. Chrestien. Specimens of Fossils yas South Africa; presented by Dr. Bower- bank, F.G.S. Specimens of Posidonie, Jurassic and Devonian, from Germany ; presented by T. R. Jones, Esq., F.G.S. Specimens of Rocks from the Interior of Australia, collected by Mr. Macdougall Stewart; presented by Sir R. I. Murchison, W PGs: Cuarts, Maps, ETC. PRESENTED. Section of a Well at Hastings; Section of Mr. Gurney’s Well at Red Hill; Section of the Well at the Northampton Water-works ; ANNUAL REPORT, © xi Section of a Well at Warnham, Sussex ; Section of Well at Birken- . head Water-works ; presented by G. R. Burnell, Esq., F.G.S. Section of Well at Thames Bank ; presented by T. R. Jones, F.G.S. Geological Map of Western Australia, from the researches of Messrs. Gregory ; presented by J. Arrowsmith, Esq., F.R.G.S, MS. Geological Map of Cornwall and part of Devon, showing the strike of the Slate-beds, 1858 ; presented by R. Whitley, Esq. Carte Hydrologique de la Ville de Paris, par M. Delesse; presented by M. Delesse, For.M.G.S. Carte Géologique souterraine de la Ville de Paris, 1858. A, Delesse, For.M.G.8. Carte des anciens Glaciers du Vowwnaik Italien des Alpes, par Gabriel de Mortillet ; presented by M. G. de Mortillet. Carte Géologique de la Néerlande, Nos. 19, 20; presented by the _ Geological Commission of the Netherlands. Sixty-six Hydrographic Charts and Plans; presented by the Ministre de la Marine, Paris. Geological Map of a portion of Central India; Saugor and Nerbudda Territories; presented by Prof. Oldham, E.G. S., Director of the Geological Survey of India. Geological Map of a part of Bundelcund ; H. B. Medlicott, Esq., F.G.S. Map of Sarawak; presented by Mr, Russell, F.G.S. Physical Atlas of Great Britain and Treland, by Walter McLeod, F.R.G.S.; presented by W. M*Leod, Esq. Carte Physique et Industrielle de la Néerlande (in' 15: sheets); presented by the Geological Commission of the Netherlands. Karten und Mittheilungen des Mittelrheinischen Geologischen Ve- reins: Section Dieburg von F. Becker und R. Ludwig. Presented _ by the Geological Society of the Middle Rhine. Map of the British Coal-fields, showing the extent and depth of the Coal-formation, by E. Hull ; presented by E, Hull, B.A., F.G.S. Geological Survey of Great Britain. Vertical Section, Sheet 26, Horizontal Sections, Sheets 58 to 61. Whole sheets, Nos, 12 and 13. Quarter sheets, Nos. 45 N.W.—53 N.E.; 53 S.E.—63 S.E.; 80 N.W.; 82-89 S.W. Chart of the British Isles, showing the Lines of Deepest water, and Lines of Depression and Elevation, 1861. The Rev. R. Everest, F.G.8. Schoolkaart voor de Natuurkunde en de Volksvlijt van Nederland. 1860. 15 sheets. Dr. W. C. H. Staring. Photograph of a remarkable surface of Coal-measure Sandstone at Swansea; presented by M. Moggridge, Esq., F.G.8. Lithographed Panoramic View of the Kashmir Mountains, by T. G. Montgomerie, 1859 ; presented by R. Godwin-Austen, Esq., F.G.S. The following Lists contain the Names of the Persons and Public Bodies from whom Donations to the Library and Museum have been received since the last Anniversary, February 15, 1861. xii ANNIVERSARY MEETING. I. List of Societies and Public Bodies from whom the Society has received Donations of Books since the last Anniversary Meeting. Basel, Natural History Society of. Berlin, German Geological Society at. » Royal Academy of Sciences at. Berwick. Naturalist’s Field Club. Bogota. Natural History Society of New Granadians. Bordeaux, Société Linnéenne de. Boston (U. 8.), Natural History Society of. Breslau. Silesian Society for Fa- therland Knowledge. ——. Imperial Leopold Aca- demy of Naturalists of Ger- many. British Government. British Museum, Trustees of. Brussels. L’ Académie Royale des Sciences. Caen. Socicté Linnéenne de Normandie. Calcutta. Geological Survey of India. Bengal Asiatic Society. Cambridge (Mass.). American Academy of Arts and Sciences. Canada, Geological Survey of. Cherbourg, Société des Sciences Naturelles de. Christiania, Royal University of. Copenhagen. Royal Danish Aca- demy of Sciences. Cornwall, Royal Polytechnic So- ciety of. Darmstadt. Geological Society of the Middle Rhine. Dijon, Academy Sciences of. Dorpat, Natural History Society of. ; Dublin, Geological Society of. , Royal Irish Academy at. of Natural Edinburgh, Royal Society of. France, Geological Society of. Frankfurt, Senckenberg Natural History Society of. —— (Kentucky). Geological Survey of Kentucky. Geneva. LaSociété de Physique et d’Histoire. Halle, Saxony and Thuringian Natural Society in. Hamburg. Natural History So- ciety. Hanau. Natural History Society of the Wetterau. Heidelberg, Natural History So- ciety of. Hobart Town. Geological Survey of Van Diemen’s Land. India, Secretary of State for. Lausanne. Société Vaudoise des Sciences Naturelles. Leeds, Philosophical Society of. Liége, la Société Royale de. * Liverpool. Lancashire and Che- shire Historical Society. , Philosophical Society of. , Geological Society of. London Commissioners for the Exhibition 1861-1862. London. Geological Survey of Great Britain and Ireland. . Royal Astronomical So- ciety. . Royal Asiatic Society of Great Britain. , Art-Union of. British Association. —, Chemical Society of. College of Surgeons of England. . College of Physicians of England. . Royal Geographical Society. ——. Geologists’ Association. ed e ANNUAL REPORT. London, Royal Horticultural So- ciety of. Institute of Actuaries of Great Britain and Ireland. . Institute of Civil Engineers. —. King’s College. ——, Linnean Society of. ——,, Mendicity Society of. ——.,, Meteorological Society of. ——,, Microscopical Society of. —, Photographic Society of. ——, Paleontological Society of. ——,, Royal Society of. ——. Royal Institution of Great Britain. —. Science and Art Depart- ment. : —, Statistical Society of. , Zoological Society of. ——. London Institution. —. Board of English Ord- nance. Louis. Academy of St. Louis. Lyons, les Commissionnaires Hy- drométriques de. Madrid, Academy of Sciences of. Manchester, Geological Society of. Melbourne. Mining Surveyors of Victoria. Colonial Mining Journal, Milan, Imperial Institute of. Montreal, Natural History So- ciety of. Moscow, Imperial Academy of Naturalists of. Munich, Academy of Sciences of. Netherlands, Geological Com- mission of. New Haven (U.8.). Editor of American Journal of Science. New York. Cooper Union for Advancement of Science and -, State Library of. ——, Lyceum of Natural His- tory of. Xi Offenbach, Natural History So- ciety of. Palermo. Agricultural Society of Sicily. Paris, ’Académie des Sciences de. , Depot Générale d’Annales des Sciences Naturelles a. , Dépot de la Marine a. ——. Impériale Zoologique d’Ac- climatation. . L’Ecole des Mines. Pesth, Academy of Sciences of. Philadelphia, Academy of Na- tural Sciences of. Plymouth Institution. Puy-en-Velay, la Société d’Agri-~ culture et Sciences du. Stockholm, Academy of. St. Petersburg, Imperial Aca- demy of. Stuttgart. Fatherland Natural History Society of Wurtem- berg. Toronto (Government of Canada), Public Library of. . Canadian Institute. Turin, Academy of Sciences at. Tyneside Naturalists’ Field Club. Vienna, Geological Institute of. , Imperial Academy of. Warwickshire Naturalists’ Field Club. Washington. United States War Department. . Smithsonian Institution. Wiesbaden. Natural History So- ciety of the Grand Duchy of Nassau. Yorkshire (West Riding). Geo- logical and Polytechnical So- ciety. , Philosophical Society of. ANNIVERSARY MEETING. II. List containing the names of the Persons from whom Donations to the Library and Museum have been received since the last. Anniversary. American Journal of Science and Art, Editor of the. Arkansas, Governor of. Arrowsmith, J., Esq. Atheneum Journal, Editor of the. Atherstone, Dr. A. G. Atlas Newspaper, Editor of the. Austin, Major, F.G.S. Barrande, M. J., For.M.G.8. Beke, Dr. Belt, T., Esq. Biden, W. D. Binkhoorst, M. Bland, T., Esq., F.G.S. Botfield, B., Esq., M.P., F.G.S. Bowerbank, Dr., F.G.S. Bristow, H. W., Esq., F.G.S. Bronn, Prof., For.M.G.S. Bunbury, Sir C., Bart., F.G.S. Burnell, G. R., Esq. Cabral, Don. Carpenter, Dr. W. B., F.G.S. Chapuis, M. F. Charlton, Mr. Chemist and Druggist, Editor of the. Chrestien, M. Clarke, Rev. W. B., F.G.S. Colliery Guardian, Editor of the. Critic, Editor of the. Cumming, Rev. J. G., F.G.S. Daubeny, Dr., F.G.S. Daubrée, M. A. Davidson, T., Esq., F.G.S. Dawson, Dr. J. W., F.G.S. Dawson, W, E., Esq. Delesse, M., For.M.G.S. Deshayes, Prof, For.M.G.8. Deslongchamps, ME. ais Hon, M.G.S, Evans, J., Esq., F.G.S. Favre, M. A. Ferrel, W., Esq. Forbes, D., Esq., F.G.S. Forbes, Poe E. G. Ss . Fournet, Prof, Freke, Dr. Gabb, Dr. Garden, Major, F.G.S. Gaudry, M Gemmellaro, Sig. G. G. Geologist, Editor of the. . Gibb, DrG, DL Gr Se Godwin-Austen, R., Esq., F.G.S. pGrank Dr: Gray, Dr. Asa. Gregory, T. F., Esq. Grey, Dr. G Guyot, Dr. Haast, J., Esq. Hall, Prof., For.M.G.S. Hauer, H. von. _Haughton, Rev. §., F.G.S. Hébert, M. E. Hector, Dr., F.G.S. Heer, Prof. ‘0: Helmersen, G. von, For. M. G. S. Henslow, Rey. J. 38., EGae: Henwood, W. J., E.GS. Hopkins, E., Esq., F.G.S. Horner, L., Esq., Pres.G.8. Horton, W. S., Esq., F.G.S. Hull, E., Esq., F.G.S. Huxley, Prof. T. H., Sec.G.8. Jackson, G., Esq. Jamieson, T. F., Esq., F. GS. Jeffreys, J. G., Esq. »» EGR. Jones, T. R., Esq., F.G.S. Kine, Prom vs -Lartet, M., For.M.G.S. . Lea, Dr. I. Lindsay, Dr. ANNUAL REPORT. xV Lindstrém, Dr. G. ’ Literary Gazette, Editor of the. Prestwich, J., Esq., F.G.S. London, Edinburgh, and Dublin | Quarterly Journal of Microsco- Philosophical Magazine, Editor of the. London Review, Editor of the. Longman and Co., Messrs. Longman, W., Esq., F.G.S. Lovén, M. 8. Lubbock, J., Esq., F.G.S. Lyell, Sir C., F.G.S. McAndrew, J., Esq. M‘Leod, W., Esq. Majendie, A., Esq., F.G.S. Marcou, M. J. Mechanics’ Magazine, Editor of the. Michelin, M. Middleton, J. O., Esq. Mining Review, Editor of the. Moggridge, M., Esq., F.G.S. Mortillet, M. Murchison, Sir R. I., V.P.G.S. Naumann, Dr. C. F., For.M.G.S. Newberry, J. 8., Esq. New Zealand Examiner, Editor _ of the. Nicol, Prof. J., F.G.S. Oldham, Dr., F.G.S. Ordway, A. Owen, Prof. R., F.G.S. Parker, W. K., Esq. Perry, M. Perthes, B. de. — Pictet, M. F. J. Pirona, Dr. Porter, Dr., F.G.S. pical Science, Editor of the. Quarterly Journal of the Chemical Society, Editor of the. Ramsay, Prof, A. C., F.G.S. Reeve, L., Esq., F.G.S. Russell, Prof. Rutimeyer, Dr. ‘Salmon, H. C., Esq., F.G.S.. Sandberger, Dr, Sars, Dr. M. Scharff, Dr. Schvarez, Dr. Scott, R. W., Esq. Sorby, H. C., Esq., F.G.S8. Sparks, J., Esq. _. Stoddard, Captain. Stoliczka, M. F. Stoppani, A. Stow, G. W., Esq. Street, G., Esq. Studer, Prof. B., For.M.G.S. Suess, Prof. HK. Symonds, Rev. W. S., F.G.S. Tennant, Prof. J., F.G.8. Tylor, EK. B., Esq: Tyson, P., Esq. Weizel, T. O. Whitley, N., Esq. Whitley, R., Esq. Willis and Sotheran, Messrs. Woods, Rey. J. E., F.G.S. Zigno, Signor A. de. Xvi ANNIVERSARY MEETING. List of Pargrs read since the last Anniversary Meeting, February 17th, 1861. 1861. Feb. 20th.—On the Coincidence between the Stratification and Foliation of the Altered Rocks of the Scottish Highlands, by Sir R. I. Murchison, V.P.G.8., and A. Geikie, Esq., F.G.S. On the Relations of the Strata of somo parts of the Scottish Highlands (South of the Caledonian Canal) and in the North of Ireland, by Prof. Harkness, F.G.S. ‘March 6th.—On the Succession of Beds in the Hastings Sand, by F. Drew, Esq., F.G.8. On the Permian Rocks of South Yorkshire, and their Paleontological relations, by J. W. Kirkby, Esq.; communicated by T. Davidson, Esq., F.G.8. March 20th.—Notes on a Collection of Fossil Plants from Nagpur, by Sir C. J. F. Bunbury, F.G.S. On the Age of the Fossiliferous Thin-bedded Sand- stone and Coal of the Province of Nagpur, India, by the Rev. Stephen Hislop; communicated by the President. On the Relative Positions of certain Plants in the Coal-bearing beds of Australia, by the Rev. W. B. Clarke, F.G.S. April 10th.—On Elevations and Depressions of the Earth in North America, by Dr. Abraham Gesner, F.G.S. On the Geology of the Country between Lake Su- perior and the Pacific Ocean (between the 48th and 54th parallels of latitude) visited by the Government Exploring Expedition under the command of Captain J. Palliser (1857-60), by J. Hec- tor, M.D.; communicated by Sir R. I. Murchison, V.P.G.S. April 24th.—On the Occurrence of the Cyrena fluminalis, together with Marine Shells of Recent Species, in beds of Sand and Gravel over beds of Boulder-clay near Hull; with an Account of some Borings and Well-sections in the same District, by J. Prestwich, Ksq., Treas.G.8. On the “Symon Fault” in the Coalbrook-dale Coal- field, by M. W. T. Scott, Esq., F.G.S. May 8th.—On two Bone-caverns in the Montagne du Ker at Mas- sat, in the Department of the Ariége, by M. Alfred Fontan ; communicated by M. Lartet, For.M.G.8. Notes on some further discoveries of Flint Imple- ments in Beds of Post-pliocene Gravel and Clay; with a few Suggestions for Search elsewhere, by J. Prestwich, Esq., Treas.G.S. ——_——_———— On the Corbicula (or Cyrena) fluminalis geologically considered, by J. Gwyn Jeffreys, Esq., F.G.S. May 22nd.—On the Geology of a part of Western Australia, by ¥. T. Gregory, Esq.; communicated by Sir R. I. Murchison, V.P.G.S. On the Zones of the Lower Lias and the Avicula con- torta Zone, by C. Moore, Esq., F.G.S. June 5th.—On the Occurrence of large Granite Boulders, at a Great ANNUAL REPORT. Xvi 1861. Depth, in West Rosewarne Mine, Gwinear, Cornwall, by H. C. Sal- mon, Esq., F.G.S. June 5th.—On an erect Sigillaria from the South Joggins, Nova Seotia, by Dr. J. W. Dawson, F.G.S. ————_——- Note ona Carpolite from the Coal-formation of Cape Breton, by Dr. J. W. Dawson, F.G.S., —_——_—_———— On some of the Higher Crustacea from the British Coal-measures, by J. W. Salter, F.G.S. —_________ On a Reconstructed Bed on the top of the Chalk and underlying the Woolwich and Reading Beds, by W. Whitaker, B.A., F.GS. June 19th.—On the Lines of Deepest Water around the British Isles, by the Rey. R. Everest, F.G.S. On the Old Red Sandstone Rocks of Forfarshire, by James Powrie, Esq., F.G.S. —_— On the Ludlow Bone-bed and its Crustacean Remains, by J. Harley, M.B.; communicated by Prof. Huxley, Sec.G.8. On the Outburst of a Volcano near Edd, on the African Coast of the Red Sea, by Capt. R. L. Playfair; commu- nicated by Sir R. I. Murchison, V.P.G.S. ———_—__——-. Notice of the Occurrence of an Earthquake on the 20th of March, 1861, in Mendoza, Argentine Confederation, South America, by C. Murray, Esq. ; communicated by the President. —_——_—__— On the Increase of Land on the Coromandel Coast, by J. W. Dykes, Esq.; from a letter to Sir C. Lyell, F.G:S. Noy. 6th.—On the Bone-caves of Lunel-Viel, Herault, by M. Marcel de Serres; communicated by the President. ——_—_—_——. On the Petroleum-springs of North America, by Dr. A. Gesner, F.G.S. —__—_———. On a Volcanic Phenomenon witnessed at Manilla, by J. G. Veitch, Esq.; communicated by Dr. Hooker. ———— Notice of the Discovery of Additional Remains of Land Animals in the Coal-measures of the South Joggins, Nova Scotia, by Dr. J. W. Dawson, F.G.S. Nov. 20th.—On some Volcanic Cones at the foot of Etna, by Prof. Gemmellaro; communicated by Sir C. Lyell. On the Deposits at Bovey Tracey, Devon, by J. H. Key, Esq.; communicated by Sir C. Lyell, F.G.S. ———_————. On some Carboniferous Brachiopoda from the Pun- jab, by T. Davidson, Esq., F.G.S. Dec. 4th.—On the Bracklesham Beds of the Isle of Wight Basin, by the Rey. O. Fisher, F.G.S. 1862. Jan. 8th.—On the Carboniferous Limestones of Oreton and Farlow, Clee Hills, Shropshire, by Prof. J. Morris, V.P.G.S., and Mr. G. E. Roberts ; with a note on a new Plerichthy ys, by Sir P. de M. Grey Egerton, Bart., F.G.S. —__— On some Fossil Plants showing Structure, from the b VOL, XVIII. XViii ANNIVERSARY MEETING. 1862. Lower Coal-fields of Lancashire, by E. W. Binney, Esq., F.R.S., ¥.G.S. Jan. 22nd.—On the further Discovery of Flint Implements in Gravel near Bedford, by J. Wyatt, Esq., F.G.S. | On Flint Arrow-heads (?) from the Drift in North Devon, by N. Whitley, Esq.; communicated by J. 8. Enys, Esq., F.G.S. On the Hyena-den at Wookey-hole, near Wells, by W. Boyd Dawkins, Esq., F.G.S. After the Reports had been read it was resolved,— That they be received and entered on the minutes of the Meeting ; and that such parts of them as the Council shall think fit be printed and distributed among the Fellows. It was afterwards resolved,— 1. That the thanks of the Society be given to Sir R. I. Murchison, Prof, John Phillips, and G. P. Scrope, retiring from the office of Viee- President. 2. That the thanks of the Society be given to Dr. J. D. Hooker, Prof. W. H. Miller, Prof. J. Phillips, Major-General Portlock, and T. Sopwith, Esq., retiring from the Council. After the Balloting-glasses had been duly closed, and the lists examined by the Scrutineers, the following gentlemen were declared to have been duly elected as the Officers and Council for the ensuing year ;— OFFICERS. i PRESIDENT. Professor A. C. Ramsay, F.R.S. VICE-PRESIDENTS. Sir P. G. Egerton, Bart., M.P., F.R.S. & LS. Sir Charles Lyell, F.R.S. & L.S. J. Carrick Moore, Esq., F.R.S. Professor John Morris. SECRETARIES. Prof. T. H. Huxley, F.R.8. & LS. Warington W. Smyth, Esq., M.A., F.R.S. FOREIGN SECRETARY. William John Hamilton, Esq., F.R.S. TREASURER. Joseph Prestwich, Esq., F.R.S. ANNUAL REPORT. xix COUNCIL. John J. Bigsby, M.D. Sir Charles Bunbury, F.R.S. & LS. Robert Chambers, Esq., F.R.S.E. & LS, Sir P. G. Egerton, Bart., M.P., F.R.S. & LS. Earl of Enniskillen, D.C.L., F.R.S.. Hugh Falconer, M.D., F.R.S. William John Hamilton, Esq., F.R.S. Leonard Horner, Esq., F.R.S. L. & EF. Prof. T. H. Huxley, F.R.S. & LS. John Lubbock, Esq.,F.R.S.&L.S, Bart., Sir Charles Lyell, F.R.S. & L.S. Edward Meryon, M.D. John Carrick Moore, Esq., F.R.S. Prof. John Morris. Sir R. I. Murchison, G.C.8t.S., F.RS. & LS. Robert W. Mylne, Esq., F.R.S. Joseph Prestwich, Esq., F.R.S. Prof. A. C. Ramsay, F.R.S. G. P. Scrope, Esq., M.P., F.R.S. Warington W. Smyth, Exq., M.A., F.R.S. Alfred Tylor, Esq., F.L.8. Rey. Thomas Wiltshire, M.A. S. P. Woodward, Esq. b2 xX LIST OF THE FIFTY FOREIGN MEMBERS OF THE GEOLOGICAL SOCIETY OF LONDON, 1n 1862. Date of Election. 1817. Professor Karl von Raumer, Munich. 1818. Professor G. Ch. Gmelin, Tiibingen. 1819. Count A. Breunner, Vienna. 1819. Sign. Alberto Parolini, Bassano. 1822. Count Vitiano Borromeo, Milan. 1823. Professor Nils de Nordenskiold, Helsengfors. 1825. Dr. G. Forchhammer, Copenhagen. 1827. Dr. H. von Dechen, Oberberghauptmann, Bonn. 1827. Herr Karl von Oeynhausen, Oberberghauptmann, Breslau. 1828. M. J. M. Bertrand de Doue, Puy-en-Velay. 1828, M. Léonce Elie de Beaumont, Sec. Perpétuel de l’Instit. France, For. Memb. R.8., Paris. 1828. Dr. B. Silliman, New Haven, Connecticut. 1829, Dr. Ami Boué, Vienna, 1829, J. J. d’Omalius d’Halloy, Namur. 1832. Professor Hilert Mitscherlich, For, Mem. R. 8., Berlin. 1839, Dr. Ch. G. Ehrenberg, For. Mem. R. S., Berlin. 1840. Professor Adolphe T. Brongniart, For. Mem. R. S., Paris. 1840. Professor Gustav Rose, Berlin. 1841. Dr. Louis Agassiz, For. Mem. R.8., Cambridge, Massachusetts. - 1841, M. G. P. Deshayes, Paris. 1844, Professor William Burton Rogers, Boston, U.S. 1844, M. Edouard de Verneuil, Paris, 1847, Dr. M. C. H. Pander, Riga. 1847. M. le Vicomte B. d’Archiac, Paris, 1848. James Hall, Esq., Albany. 1850. Professor Bernard Studer, Berne. 1850, Herr Hermann von Meyer, Frankfort on Maine. 1851. Professor James D. Dana, New Haven, Connecticut. 1851. Professor H. G. Bronn, Heidelberg. 1851. Colonel G. von Helmersen, St. Petersburg. 1851. Hofrath W. K. Haidinger, For. Mem. R. 8., Vienna. 1851. Professor Angelo Sismonda, Zin. 1853. Count Alexander von Keyserling, Reval. 1853. Professor Dr. L. G. de Koninck, Liége. 1854. M. Joachim Barrande, Prague. 1854, Professor Dr, Karl Friedrich Naumann, Leitpsic. XXi 1856. Professor Dr. Robert W. Bunsen, Hetdelberg. 1857. Professor Dr. H. R. Goeppert, Breslau. 1857. M. E. Lartét, Paris. 1857. Professor Dr. H. B. Geinitz, Dresden. 1857. Dr. Hermann Abich, S¢. Petersburg.. 1858, Dr. J. A. E. Deslongchamps, Caen. 1858. Herr Arn. Escher yon der Linth, Zurich. 1859. M. A. Delesse, Paris. 1859. Professor Dr. Ferdinand Roemer, Breslau. 1860. Professor Dr. H. Milne-Edwards, For. Mem. R. S., Paris. 1861. Professor Gustav Bischof, Bonn. 1862. Senor Casiano di Prado, Madrid. 1862. Baron Sartorius Waltershausen, Gottingen. 1862. Professor Pierre Merian, Basie. AWARDS OF THE WOLLASTON-MEDAL UNDER THE CONDITIONS OF THE “ DONATION-FUND ”’ ESTABLISHED BY WILLIAM HYDE WOLLASTON, M.D., F.RB.S., F.G:S., &c., “To promote researches concerning the mineral structure of the earth, and to enable the Council of the Geological Society to reward those individuals of any country by whom such researches may hereafter be made,”—“ such individual not being a Member of the Council.” 1831. Mr. William Smith. 1849. Mr. Joseph Prestwich, jun. 1835. Dr. G. A. Mantell. 1850. Mr. William Hopkins. 18386. M. L. Agassiz. 1851. The Rev. Prof. A. Sedgwick. - Capt. P. F. Cautley. 1852. Dr. W. H. Fitton. sah or H. Falconer. 1853 ee le Vicomte A. d’Archiac, 1838. Professor R. Owen. ’ (M. E. de Verneuil. 1839. Professor C. G. Ehrenberg. 1854, Dr. Richard Griffith. 1840, Professor A. H. Dumont. 1855. Sir H. T. De la Beche. 1841. M. Adolphe T. Brongniart. 1856, Sir W. E. Logan. 1842. Baron L. von Buch. 1857. M. Joachim Barrande. . M. E. de Beaumont. ~q J Herr Hermann von Meyer. 1843. fa A. Dafténoy. iat ae POLST dial 1844, The Rey. W. D. Conybeare. | 1859. Mr. Charles Darwin. 1845. Professor John Phillips. 1860. Mr. Searles V. Wood. 1846. Mr. William Lonsdale. 1861. Prof. Dr. H. G. Bronn. 1847. Dr. Ami Boué. 1862, Mr. Robert A. C. Godwin- 1848. The Rey. Dr. W. Buckland. Austen, EsTIMATES for INCOME EXPECTED. £86 £ Hae Due for Subscriptions on Quarterly Journal (con- sidered good) eeceeceteeeetssescestetoessaesceeseceoeseees 50 0 a) Due for Authors’ Corrections ...cccccscccccsscssseces 18 17 OF Due for Arrears (See Valuation-sheet) csesodesiiee, LEP ba. 10 ; - 196 13 O Ordinary Income for 1861 (estimated). Annual Contributions :— 222 Resident Fellows at £3 38. ceccccccccseeee 699 6 O 48 Non-resident Fellows at £1 11s, 6d. ... 75 12 0 otal — 774 18 0O Admission-fees (supposed) .......«. NBCU CARE Spéonoponecabed sore, 200 0 O Compositions (Supposed) c.ccccceseseees eeevenssecvcsenaesccnseuces isn Dividends On Consols .....scccccesssccessccsccce Cdeedacsaucsesecacene: (hol alone Sale of Transactions, Proceedings, Geological Map, Li- brary-catalogues, and Ormerod’s Index ...rc.cccceserseceeersee 50 0 Sale of Quarterly Journal ........0.0. seeuaaee siecasetaweeants Sesngeee .. 200 0) Due from Longman and Co. in June...ccccs.scscsccsccesterecececees 60 4 Balance due from Bequest-Fund on account of Expenditure on Map, Museum, and Library.......s.sseseeseers eegesearesesene 106 17 3 £1870 9 7 JOSEPH PRESTWICH, Treas. Feb. 5, 1862. the Year 1862. EXPENDITURE ESTIMATED. £ead£ 8 d. General Expenditure : Taxes and Insurance .........e..eeee seoese 40 0 0 House-Repairs .......cccecees ssssevcssee 20 Q Q DIE, cg gies cass eee ce eapecseaeartca, a0. .0 e Fuel op cuescesccccess cctercessiccecsecews So O O ccc. scaks x08 anaes ite es 35 0 0 Miscellaneous House-expenses .....-+++- oes 50 0 0 Stationery ....... aes stag oe Car helene scooee 30 0 0 Miscellaneous Printing, including Abstracts.... 30 0 0 Tea for Meetings........ raiais saia/ota 9 wigeee erat 20 0 0 —— 290 0 0 Salaries and Wages : Assistant-Secretary ....-.2-seccsesess beaase 200 0 0 DURGA Sales ow oc tdccbaadc aces Seensbace 90 0 0 Assistants in Library and Museum.........6.. 100 0 0 EUMEMG Pda co S See dee sd ece dee ccsiseceds 90 0 0 AS ene norrnercmer errr - 40 0 0 Occasional Attendants ......... cueascceaen £0 @ A SRE Rnd) so neces dencces haga sesssee 30 0 0 570 0 O Library : Ordinary and Special Expenditure ......ccccccssseseesre 10 O O Museum: Ordinary Expenditure ...... seeeesese séscessssseessssssore 50 O O Diagrams at Meetings .......+06 aes esseaey sea icas duscagusceessaccceas” & O O Miscellaneous Scientific Expenditure ......sccceccsscencscscssseees 50 O O Publications: Quarterly Journal .........+4. becsecestbscdvaseses s«- 630 0 O ps Transactions .:....< SEU CLEC ECOREL EET CBee ae iicsde LG OO Pe Geological Map, special expenditure.........64 gent BU, ©, -O £1775 O O Balance in favour of the Society ......... dda ssoencscessconconcees 95 9 7 £1870 9 7 Income and Expenditure during the INCOME. Go.8 oo Balance at Banker’s, January 1, 1861 ...... write 19 :BikO Balancein' Clerk's, hands t2%4 Se Sis, oss ns oe eles Cammpositinnsirecermeds GGT. wi, Sore isx: cnawiloe keene 141 15 O Arrears of Admission-fees .......0.2+ .eu0+s teh 50 8 O Arrears of Annual Contributions ...... ees type en te ee Admission-fees for 1861 ........ weenie 6 as © 9,0,9:8 9, inky ere Annual Contributions for 1861, viz.— Sit p 204 Resident Fellows .........£636 16 6 36 Non-Resident Fellows ... 5119 0 —— 688 15 6 Dividends on'Oonsols you eee eo Seb 3) ag bs phon) Dividends on New South Wales Bond... Lf aa —— 139 3 0 Publications : Longman and Co., for Sale of Quarterly Journal Ute AEE apoB aS 644s coda sdodddcans en 63 12 3 Sale of Transactions ....0.s.:ccesccsevescs 16 8 0 Sale of Proceedings ..-<...- ssc oc ene sees 010 0 Sale of Journal, Vols. 1-6 .......--eeeeeee 10° 26 4 Moles Paboues bo) meee 1717.6 i Vols A3o15) conmeo ee byaee 19 9 0 aS 0) Gy er Saad Goronirecers 50.12 6 Vol. UF* secs weune ue nancies 94 10 10 Sale of ‘Geological NTA) Crraale olavsyaiewletatalsi=is op Oul2ere Sale of Library-catalogues ........+es+see. 218 6 Sale of Ormerod’s Index ....-eseeeveeees 3.5 4 ——— 285 18 8 Journal-Compositions oie nabuiieniaair was esvecs LS aO Ese Portion of the Greenough and Brown Bequest- Fund, ordered by the Council to be sold out on account of Special Expenditure on Map, Library, Museum, and House- repairs, as per general estimates for the a ae ols) ky ne Roe eS PE AES ER AM RON, Ac 490 2 Donation irom) May, Alired Uvlor.... 4. . ase caer 5210 0 We have compared the Books and Vouchers presented to us with these Statements, and find them correct. ALFRED TYLOR, f ‘#ditors. —-£2178_9_0 Feb. 1, 1862. * Due from Messrs. Longman and Co., in addition to the above, On Journal, Volkov lls. oi ctee iter b nels ect oision ote «es OO 49 Due from Fellows for Journal Subscription ...........+.6.- 50 0 tT Balance due from the Bequest-Fund for expenditure on war Library, and Museum........++0.. ain idlciauate apimte oie ganwn's, LOGIE £217 6 salbo on _ Year ending December 31st, 1861. EXPENDITURE. General Expenditure : POD te a ge dl TREES ce vets sé ca'nee SACs Ke wears nd'elete nt Dee Zoro 4 MPO UNUEANCE oc on ccc ec ceanccerncess 3.0 0 House-Repairs :—Ordinary .... £15 14 6 Special ...... 148 4 6 ——_——. 163 19 0 RUMI Sigal yaw eo ceivs'na c'sle cn mo'e vs 34 3 0 SES rer er 32 18 9 Miscellaneous House-expenditure, including Postage-stamps ....-e.eeeceee cine cee 4 7 Mins inc ss sean ss pcvnsives aes 23 17 2 Miscellaneous Printing ....--secssesecere 20 8 6 Tea for Meetings ...ecccceseevecevesess 1715 8 —— 41115 0 Salaries and Wages: Assistant-Secretary ...c.ceececcccccvece 200 0 0 RE alee es aic'c esis ad weiec weiss o cie'e 0 76 5 O Assistants in Library and Museum ........ 91 0 0 En as alia ciwiw coins < wie ateim © a ocie 90 0 0 MME oy has ch avn a ict nie Give o Heme a < 40 0 0 Donation to Mr. Nichols ..... gates e mts 70 0 0 Occasional Attendance....... Cristo bine oe ais 2119 6 RE Bila n'a sia ws aie'p a's, arene a Siaiehate 25.) 9 ——- 61410 3 Library :—Ordinary Expenditure........ 56 6 2 Special ditto g eisai ans eae SOEOH IG ———- 99 15 8 Museum :—Ordinary Expenditure ...... 3713 9 Special, Foreign Collection .. 50 O O wato,) Cabinets «60:25 sets 4019. 2 —— 128 12 9 Diagrams at Meetings ........ Pg ett 4 Faie< eee nur Ue LO) Miscellaneous Scientific Expenses .............. oui ied deal ook) Publications : MEME NIA als cco n ess oced bd sdevceks 55 4 3 Transactions ae Ormerod’s Tudex Bieta 6. <5 Proceedings and Abstracts .............. By OG Rev OIS, VII.—KIL. oovececcccicnee be OT 3 Be Wels, KUL KV bs o'ss ttveecdess 20 8 - BE Ea nin wid givin middie earewiats_ 0’ 40S «7 i ae Ee See ChbS, "Sy 10 6938 1 6 Balance at the Banker’s and at Messrs. Longman’s, Pee GOL 2. ces eta aaeetie ch cle ae lv s oo AG as Ao OS ok Balance in Clerk’s hands ...........0000%. 5 ore 19S: TS £2178 9 O Oe ee ‘punj-jsanbog uMoIg pue ySnousely dy} WOIf SuUIUTeMIEI QOSF JO soueleq oy} Sepnjout sigy, x “GOST “G24 WS = = “SIT, * ausIc) > L GIStF Se iL HOIMALSHad Hddsor (peusig —— [‘papnjous aay ZOU St $Uu012 -payngng pjosun fo yaojs pun ‘aanjwuiny ‘hsorg “17 ‘suoyaayog osauapy ayp fo amon ay, “EN I O 91 Ler 0 0 O06 (ht? SHOINGUUOD jenuuy jo sleally 0 91 Lg poo’ pasaptsuod) saaj-uoIssiupy Jo sively 0) O xOSEP eenceceseseseteeecuee c6 ye ‘sjosuo4y eae —: Ayiedoig pepuny Il SI 61 CORLL ADHD HHH TH HES RSH HHH HOHOHEHHF GOH BOSTES spuey i> A) Fe) ul soueleg I 9 GOL FO eect eres ee) OLD KAS S$ Jayued Ul eouRleg O ZTE St crrcstreseseeseseee* TeuUIMOL UI SUOTZIIIIOD ,SIOYjNY OJ ond 0 O OG ciittttttttteeeesereeeseeeeees TeTLINOF 0} S1oqlIosqng WO. ang b ZL Glaprrrrrrrrscscrerrsscsevrers AQQIDOG OY} JO INOALJ UL soURTeg |r 6 09 "TIAX OA ‘eumnor uo “09 pue ueUIsUOT ‘sissap] WoL ang Do Es. og *SsLaaqd “pS *"ALUDAOUg “LOST ‘uaquavag ISTE { ALUMAOUT S.ALAIOOG AHL 40 NOILVAIVA 0 O OSEP 6 FL GOF 6 FI COF eewuvenseeveseeseseasssonecessesataessrorseeses egqttgd Jad g GQ F TE ererrseesceeseeceees = (NUNJ-UOISLT[OM) S,Jayueg ye soueleg pate ‘eee “PT “ST F8O1F JO punj-uoljzeuod ey} UO spuspita 0 OL OL TO9ST ‘UuOIg ‘Jog 0} papreMe [Epa P[OD SUTYM}g Jo sop seseeveveceeseseeaeneseseseseseoeess — DUNJ-UOIVUO(] WOISE] Te Clipe eee eee ee’ PORT “oad nel “Jolg.o}, pupa y | Les 01 te “[OM aq} UO “TOST Arvenuer jo 4ST ‘s,royuRg ye couRleg ae Say ce *SINANWAVG aa *SLdISOTY *LNQOODY-LSAUy, PROCEEDINGS AT THE ANNUAL GENERAL. MEETING, 2isr FEBRUARY, 1862. AWARD OF THE WotnAsTON MEDAL, The Chairman, Srr Roperick Murcuison, then addressed Mr. Gopwin-AvstEn as follows :— Mr. Gopwix-Avsten,—Valuing as I do the services you have rendered to geological science, I consider myself very fortunate in occupying this chair to perform the duty of the President in his unavoidable absence, by placing the Wollaston Medal in your hands. Although there are two points in your numerous writings in which I have differed from you, viz., your theory of the synchronism of the Upper Silurian and Devonian rocks, and your view of the lacustrine or terrestrial nature of the Old Red Sandstone, yet even in these views I admire your originality of thought; whilst on all other grounds I am bound to say that I am convinced of the soundness of your speculations. In truth, all your associates, as well as myself, are aware that you have distinguished yourself during a long series of years by your successful inquiries into the former changes of land and water from the Palzozoic age to modern times. Persistently keeping that great object in view, you have put forth well-founded hypotheses, based on actual and numerous observations, which have raised the philosophical character of our science. Your sedulous study of the organic remains, as well as the materials of the beds themselves of each formation which you have examined, and your laborious tracings of various lines of dislocation, have all been made subservient to that one great end; and I am therefore proud to announce that you are this day justly rewarded with the Wollaston a aeaee as being pre-eminently the physical geographer of bygone periods. In your latest remarkable researches, you have, by fair inductive XXYVlli PROCEEDINGS OF THE GEOLOGICAL SOCIETY. reasoning, brought to the mind’s eye of geologists the high probability of the extension of Upper Paleeozoic, if not of Carboniferous strata beneath the surface of the Tertiary and Cretaceous rocks surrounding our metropolis; and you have thus made the value and importance of our science apparent even to the commercial classes of the country. Pray receive this Medal as the hearty expression of our approba- tion; and may it stimulate you to extend to the study of the subsoil of those foreign lands into which you are about to travel the same energy and talent which enabled you to elaborate so ingeniously and so skilfully the former changes of land and water over so large an area in the west of Europe. Mr. Gopwin-AvstEn, on receiving the Medal, thus replied ;— I have so frequently been a member of the Council of this Society when the award of the Wollaston Medal has been under considera- tion, I so well know how many qualifications have been taken into account in its adjudication, that I am enabled to appreciate in the fullest the very high honour which I now receive, at your hands, from this Society. I am proud of such a record of the estimation in which the part which I have taken in our common work has been held by you. But when I speak in this way of the Wollaston Medal, I beg that you will feel assured, and by no idle form of words, that I should almost regret the honour if I thought for a moment that I could thereby deceive myself. I know how very unequal are the degrees of merit of those who receive the same honours; and I can myself, aswell as anybody, draw the broad line which must separate me from others whom you have already placed in that distinguished list. You have been pleased, Sir, to refer to some of those contributions which have been favourably considered by the Council. I will not follow you over that ground; but perhaps I may be allowed to say this much, that in every contribution I have endeavoured to work out and apply what has been seen and recorded to some of the ulti- mate aims and objects of geological investigation. It may have been no very difficult matter to restore the physical features of the north hemisphere for the Tertiary, or even for the Cretaceous and Oolitic periods of past time. The Permian area and that of old Coal-growths are both easy enough of definition. But, standing before you as I now do, I am forcibly reminded that when it came to the consideration of those vast masses of early Paleozoic deposit, now raised up into the mountains of Wales, so large a portion of which go to form your Silurian series, that then for the first time all landmarks seem to disappear, and that I was driven to steer for a Western Atlantis older and larger far than that of Plato. Such speculations may by some have been thought hazardous; but little by little this Western sub-Atlantic land has acquired wonderful distinctness, and towards this chapter in ancient geography those re- searches which you haverecently been engaged in in the north-western regions of these our British Islands have lent a most important aid. ANNIVERSARY ADDRESS. XXixX You have alluded to the period of my connection with this Society : twenty-seven years become a serious retrospect to every man. I might perhaps not have thought so much of it, but it now strikes me that I lived too much in the Castle of Indolence: this Medal almost seems to reproach me by the suggestion that I might and ought to have donemore. However, weare told “ that it is never too late to mend ;” and I hope to bear away this Medal, not as a solatium for labours that are ended, but as an incentive to work which may yet be accomplished. AWARD OF THE WoLLASTON DoNATION-FUND. In delivering the purse containing the balance of the proceeds of the Wollaston Fund to Prorrssor Huxtery, the Chairman said :— Mr. Secrerary,—In handing to you the purse containing the proceeds of the Wollaston Fund, and in requesting you to convey it to Professor O. Heer, it is enough for me to remind the Meeting that this eminent botanist and entomologist has rendered great services to geology by his remarkable works on the ‘ Tertiary Insects of Oeningen and Radoboj,’ by his ‘ Tertiary Flora of Switzerland,’ by his ‘ Vegetation and Climate of the Tertiary Period,’ and recently by throwing light on the true age of the lignite deposit of Bovey Tracey. For these important works Professor Heer is indeed well entitled to any honour we can give him; and these proceeds are awarded to him to enable him to prosecute with greater ease his praiseworthy and enlightened researches. The Chairman next, before reading the following letter from the President, regretting his unavoidable absence in Italy, expressed his sense of the eminent services rendered to the Society since its foun- dation by Mr. Leonard Horner. Florence, 11th February, 1862. To Sir Roderick I. Murchison, F.R.S., Vice-President of the Gieo- logical Society. My pear Sm Ropericr,—You are aware that it was indispensable for me to leave England last autumn to pass the winter in Italy, for the benefit of a member of my family who had been long in bad health. As senior Vice-President, you will, I hope, be in the chair at the ensuing Anniversary, and I request that you will assure the Meeting that no other consideration would have induced me to absent myself from my duties as President. The honour conferred upon me of being elected a second time to the highest office in the Socicty I felt as a very great distinction. It is now nearly fifty-four years since I began to take an active part in the affairs of the Society ; and to have been called upon to exert myself for its honour and interest, I felt as a renewal of the pleasure of my younger days. XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY. I beg you to convey my very sincere thanks to the Members of the Council and to the Society at large for the kind support I uni- formly experienced from them on all occasions. So long as life and health may be left to me, I shall continue my devotion to geological science, and my attachment to the Society which has done so much to promote it. I am, my dear Sir Roderick, Faithfully yours, Lronarp Horner. The Chairman then proceeded to read the following Obituary Notice of Dr. Fitton. The record of the decease of Fellows of the Geological Society is naturally commenced this year with a sketch of the life of one of our most distinguished leaders. The late Dr. W. H. Frrron, who was born in Dublin in January 1780, and died in London on the 13th May, 1861, at the mature age of 81, was truly one of the British worthies who have raised modern geology to its present advanced position. Descended from an ancient family in Cheshire, whose tombstones are still to be seen in the parish church of Gawsworth, Dr. Fitton’s ancestors had been long settled in Ireland. As a little boy, he fre- quented the same school in Dublin as Thomas Moore, the poet, and Robert Emmett, the United Irishman ; and already in 1798, through his proficiency in classics, he gained the Senior Scholarship of Trinity College, which he held till 1803, whilst as early as 1799 he became Bachelor of Arts in that University. Even in those troublous times, as I am informed by his old friend, that distinguished linguist and geographer, the Rev. G. Renouard, young Fitton began to collect fossils, in doing which, having been unjustly suspected to be a rebel, he was for a short time kept in military durance. From letters addressed to his learned friend, the Rev. J. Rogers, of Mawnan, in Cornwall, we learn that he made visits to that county to acquire a knowledge of its mineral structure ; and in one of these letters, dated from Trinity College, Dublin, in November 1807, we find that he had then determined the heights of the principal Irish mountains by barometrical admeasurement. In that letter he also speaks of an associate who has since given to the world the best geological map of Ireland—our eminent fellow-labourer the present Sir Richard Griffith. Originally destined for the church, Mr. Fitton was soon attracted to the medical career and the pursuits of physical science by entering into the studies of the University of Edinburgh (1808-9), then so justly celebrated for its great philosophical teachers. There it was that he formed intimacies with other students of medicine who after- wards reached the summit of their profession. Attending the lectures of Professor Jameson, he then made the acquaintance of the Rev. Dr. John Fleming and other young men of science. There it was also that he learnt to admire the writings as well as to imbibe the ANNIVERSARY ADDRESS. XXXi liberal sentiments of Sydney Smith, Jeffrey, Brougham, and the founders of that ‘ Edinburgh Review’ to which in subsequent years he himself became a distinguished contributor. Removing to London in 1809 or 1810, he kept house with his widowed mother and his three sisters—studying medicine and chemistry assiduously, and associating with all the rising men of science in that day, par- ticularly with Wollaston, Holland, Roget, Chambers, Bright, and others, In 1811 Dr. Fitton commenced to write on our science by commu- nicating, through our respected President, Leonard Horner, to the then young Geological Society a memoir * On the Geological Struc- ture of the Vicinity of Dublin,” which appears in the 1st volume of our Transactions (Old Series). Again, in ‘ Nicholson’s Journal’ of 1813 we find one of his essays on the Geological System of Werner, as doubtless derived from his Scottish studies in the days of Jameson, Hall, Hutton, and Playfair; and in the following year he wrote upon the Porcelain Rocks of Cornwall, which he had personally examined, and also gaye out his yiews on a new system of ventilating mines, In 1812 he removed with his mother and sisters to Northampton, to which place he was attracted chiefly through the patronage of the then Earl and Countess Spencer, and in the hope of succeeding to the practice of the venerable Dr. Kerr, the father of Lady Davy. Practising for eight years as a physician at Northampton, it appears that in 1816 he was admitted “ad eundem” M.D. of the University of Cambridge. In 1817 Dr. Fitton began that series of articles in the ‘Edinburgh Review,’ to which he contributed at intervals until the year 1841, and which proved him to be a just and enlightened commentator on the progress of geological science during the eventful thirty years of which he treated. Thus, when we look back to his first article, which analysed the ‘ Transactions of the Geological Society’ since its establishment in 1804 up to the publication of a new volume in 1817, or refer to his review in the following year of the first geolo- gical map of England, and the other original efforts of William Smith, we at once see how happily he seized upon and illustrated the prominent features in the foundations of our science, and the establishment of that British nomenclature which has become so generally current. Then again in 18238, when he indited his stirring pages on Buckland’s ‘ Reliquie Diluviane,’ or in 1839, when he reviewed the ‘ Elementary Geology’ of Lyell, and put forth so much knowledge respecting the Huttonian theory of the earth, or in 1841, when he reviewed the succession of palsozoic periods, as explained in the Silurian System of Murchison*, we see how vigor- ously he watched over and rejoiced in the progress of all inquiries which unfolded the history of bygone ages and enabled us to read off the ancient legends of the former inhabitants of the earth, as * Dr. Fitton also contributed to the ‘Edinburgh Review’ two articles con- nected with his profession as a medical man, viz. ‘‘ Report on Lunatic Asylums,” vol. xxviii, May 1817, and “ Larrey’s Surgical Campaign,’’ vol. xxxi. No. 62, March 1819. XXXii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. well as the mutations by which the present outline of our planet has been brought about. The researches, however, by which the name of William Henry Fitton will be most surely handed down to posterity are those by which, during twelve active years of his life (from 1824 to 1836), he laboriously developed the true descending order of succession from the Chalk downwards into the Oolitic Formations, as exhibited in the south-east of England* and in the adjoining parts of France. Before these labours commenced, geologists had confused notions only as to the order of the strata beneath the Chalk, as well as of the imbedded fossil remains of each stratum. It was Fitton who made the Greensand Formations his own, by clearly defining the position and character of the Upper and the Lower Greensands, as separated by the Gault. On this point, the writer of this sketch may well gratefully testify to the clearness and truthfulness of the views of his lamented friend, and the hearty zeal with which they were communicated; for it was through the instruction given to him in the field by Dr. Fitton, in 1825, that he was enabled to write his first paper in the ‘ Transactions’ of this Society. Ever striving to advance his favourite science, Dr. Fitton was the zealous instructor not only of young geologists, but also of many travellers and naval officers; and among those to whom he volunteered to give practical lessons, Captain Philip King, R.N., Admirals Sir © John Franklin and Sir George Back, as well as Sir John Richard- son, may be eited. Healso devoted much of his time to the writings of his friends, invariably labouring zealously to improve their com- positions. | Such gratuitous efforts, the care of a family, and other occupations necessarily delayed the completion of his great work on the Green- sand Formations ; but at length those memoirs were completed, both by very elaborate details regarding the succession of these deposits in various parts of England, in separating them from the iron- sands of the inferior Wealden Formation, and also by showing how that great freshwater deposit passes down into the Purbeck beds, and from them into the Portland Rock. On various occasions of his life Dr. Fitton displayed much honesty of purpose and a strong sense of the value of independence of cha- racter. Of his associates who survive, Herschel and Babbage, as well as Lyell and myself, can well remember when H. R. Highness the Duke of Sussex was suddenly brought forward as a candidate for the Chair of the Royal Society, that among the large body of men of science who then stood forward to vindicate the rights of their order, no one was a more ardent supporter of Herschel, in opposition to the Royal Prince, than the warm-hearted and honest Fitton, united as he then was with Wollaston, Robert Brown, and all the notabilities in science. One of the claims of Dr. Fitton on the gratitude of geologists is, that after having been the Secretary of the Society during some. * Trans. Geol. Soc., 2nd series, vol. iv. pp. 103 to 388, t Trans. Geol. Soc., 2nd series, vol, ii. p. 97. ANNIVERSARY ADDRESS. XXXili years of his life, no sooner did he attain the honour of our Chair, than he established the publication of those ‘ Proceedings’ which are the true synopsis of our labours, and have been imitated by the Royal Society and most of the scientific societies in the metropolis. He was also the first of our Presidents who adopted the practice of deliver- ing an Anniversary Address, which under his management was a well-composed and accurate sketch of the progress we had made. Let me here add, that his two addresses contained much good matter in a very small compass ; for the first of them occupied eleven pages, and the second twenty-two pages only of our ‘ Proceedings.’ In the first of these, Dr. Fitton energetically adverted to the then imperfect condition of our knowledge concerning the distribution of plants upon the former surfaces of the globe during epochs of geolo- gical deposition, as well as to the variations which such distribution may have undergone from changes of climate, either by alteration of internal temperature or elevation above the sea. ‘Then let us turn to his just eulogy of the labours of von Buch, Humboldt, and McCulloch, in supporting the theory of Hutton, as illustrated by Playfair and Hall, and verified in Anglesea by the striking observa- tions of Henslow, as well as by Davy’s experiments on the flints in the cavities of crystals. Then, again, let us look at his well-merited encomium on the wondrous effect in the progress of English Geology as produced by the publication of the ‘Outlines of Eneland and Wales,’ by Conybeare and Phillips, which volume was well said by him to have had an effect to which nothing since the institution of the Geological Society and the diffusion of geological maps could then be compared. With just pride did he affirm that that work “ acquired a new and a more dignified interest when we reflected that this island is in a great measure a general epitome of the globe, and that the observer who made himself familiar with its strata and the fossil remains which they include, had not only prepared himself for similar inquiries in other quarters, but was already acquainted by anticipation with what he may expect to find there.” It can with truth be said that this advice and the exhortation which followed, calling upon all those who had leisure, health, and talent for such inquiries to carry them out, were truly the incitements which roused the then Secretary . of the Geological Society, who pens this sketch, to undertake ex- plorations abroad by which he has endeavoured to bring the struc- ture of other countries into direct comparison with those of our own land. It is indeed most gratifying to one of the olden time to reperuse in the address of Dr. Fitton of 1829 the brief, touching, and just eulogy which he pronounced on the character of our then recently deceased Member, the illustrious Wollaston. The words came from his heart, and specially marked the penctration, correct judgment, and high moral character of the deceased philosopher. Dr. Fitton further signalized his presidency by drawing to the Society and engaging in its service, as Assistant Sccretary, ‘that re- -markable man William Lonsdale, whose acquaintance it was my good VOL, XVIIT. c XXxXiV PROCEEDINGS OF THE GEOLOGICAL SOCIETY. fortune to have made in the field, and to have recommended strongly to the notice of the President. To no one man certainly has our body been more indebted than to the excellent and gifted Lonsdale, whether for his publications, his conduct of our affairs, or the zealous and disinterested labour he bestowed in aiding and improving the works of his associates. Retiring from active participation in our business during the last few years of his life, Dr. Fitton still earnestly watched and ap- preciated our progress, and no act was ever more grateful to the feelings of the Council and of the then President, Mr. W. Hopkins, than when in 1852 they conferred on their veteran associate the highest honour in their gift, the Medal founded iF his dear friend Wollaston. United in marriage in the year 1820 to Miss James, a most amiable lady, who brought to him the means of a comfortable ex- istence, Dr. Fitton not only reared his five sons and three daughters with untiring solicitude, but, just as in previous years he had been the solace of his venerable mother, so he continued to be the pride of his sisters, the youngest of whom, Miss Sarah Fitton, still living, possesses much of the genius of her lamented brother, and has dis- tinguished herself in natural-history pursuits. Giving throughout his life constant proofs of his hospitable and generous disposition, he opened his house during his Presidency to all the Fellows at evening soirées, when his cheerful and joyous countenance and kind manner encouraged many a beginner. Fol- lowing the example of Sir Joseph Banks, who was probably the most popular President the Royal Society ever possessed, Dr. Fitton, as well as his predecessor, Mr. Greenough, held these agreeable scientific conversazion. on Sunday evenings. Up to that time, few persons thought there was any sin in so spending the latter part of a Sabbath eve; but remonstrances commencing on the part of the rigid sabba= tarians, a stop was put to those instructive and innocent recreations ; and the only remaining relic of that which was so long the custom of this land is now confined, as far as I know, to the social Sunday- evening meetings of the Dilettanti Society of Antiquaries. It is however fair to observe, that the parties of Sir Joseph Banks, Mr. Greenough, and Dr. Fitton were composed chiefly of a few scien- tific men; the large and mixed assemblies which now flock to the soirées of the Presidents of Societies being scarcely compatible with the quiet of an English Sunday night. In conclusion it may well be said, that Dr. Fitton was so single- minded, guileless, and affectionate, that every one who knew him loved him ; and as his memory is cherished by all his contemporaries, so is this the fitting occasion to record, however imperfectly, the virtues and deeds of so good a man and so sound a geologist. Dr. Fitton became a Fellow of the Royal Society in 1815; and he was also a Fellow of the Linnean, Astronomical, and Royal Geographical Societies, ANNIVERSARY ADDRESS. © XXXV Mr. W. W. Smyth, Secretary, next proceeded to read the follow- ing Obituary Notices. Sir ArtHur pe Capett Broke, Bart., of Oakley Hall, in North- amptonshire, although not a contributor to the literature of our science, is known to the world as the author of several valuable books of irayels, some of which were magnificently illustrated. More parti- cularly may be cited his‘ Travels in Lapland and to the North Cape,’ and his ‘ Sketches of Spain and Morocco,’ The Rey. James B. Precor Dennis took his degree as a member of Queen’s College, Oxford, and resided for many years at the town of Bury St. Edmunds. Mr. Dennis devoted much of his time to microscopical researches bearing on geology, such as examinations into the structure of bone, and was the author of papers commu- nicated to our Society and to the ‘Journal of Microscopical Science.’ He died at the early age of 45. General Sir C. W. Pastry, K.C.B. This veteran officer, who died 19th April, 1861, at the age of 80, was actively engaged in warlike operations as a Royal Engineer for many years in the Mediterranean and in the Peninsula, commencing with the defence of Gaeta in 1806. After his publication of a work on Chatham’s military policy, which excited great interest at the time, he was appointed in 1812 Di- rector of the Engineer Establishment at Woolwich, which was established at his instigation for the training of the young officers in Practical Military Engineering; and he devoted himself to nu- merous inquiries in solving the application of science to the military art, and became the author of several works on purely professional subjects, as well as of one ‘On Limes and Cements,’ which exhibits a great amount of industry in the examination of the various mineral substances of this and of other countries, which had been or might be employed for such purposes. When it was determined in 1839 to attempt the removal of the wreck of the ‘ Royal George’ at Spit- head, the operations were confided to Colonel Pasley, who, during the years 1840-1-2, succeeded so fully in accomplishing the object— igniting charges of gunpowder by the galvanic battery—that he became the chief authority on similar subjects, and his results con- tributed greatly to the success with which galvanic blasting has since been introduced on a large scale into various engineering operations. The Rey. Joun Srevens Hunstow. Among the scientific men of the present century there are few whose career has been so fraught with usefulness to the public as that of the late Professor Henslow. He was born at Rochester in 1796, and at a very early age dis- played a love of natural history, which was inherited from his father, who practised in that town as a solicitor. In 1818 he gra- duated at Cambridge as 16th wrangler, and declining to compete for the higher academic position, which, with his mathematical c2 XXXV1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, powers, he might easily have attained, he studied chemistry under Professor Cumming, mineralogy under Dr. Clarke, laboured hard at geology as an original inquirer, and became a Fellow of this Society in 1819. In 1821, at the early age of 23, he communicated to the Society his “ Supplementary Observations on Dr. Berger’s Account of the Isle of Man,” containing a map and sections, to the preparation of which he had devoted his spare time whilst spending two long vacations in the island with pupils. At about the same period he was led to explore the geology of Anglesey, and embodied the results in a most elaborate paper, printed in the first volume of the ‘Cambridge Philo- sophical Transactions.’ This paper raised its author at once to a high position among observers, and may to this day be quoted as a model of truthful and sagacious scientific research. It possesses also rare merit, as combining with great power of co-ordinating physical features skill and accuracy in the application of chemistry, mineralogy, mathematics and drawing to the illustration of a very complicated region. In 1822 he was appointed to the Professorship of Mineralogy, a post which he held for three years, and in 1825 resigned it in order to succeed Professor Martyn in the chair of Botany, asubject to which he had devoted much labour for some years preceding. His lectures inaugurated a new era in botanical teaching at the University, and, aided by frequent excursions, awakened interest in a study to which some of the mathematicians of Cambridge had hitherto hardly ac- corded the dignity of a science. In this career, as well as in the character of a country clergyman, when appointed by the Crown, in 1833, to the rectory of Hitcham in Suffolk, his admirable personal qualities endeared him to all who were brought in contact with him, and enabled him successfully to overcome difficulties which would have presented serious obstacles to a man endowed with less perseverance, mental power, and invari- able good temper. Among the special services which he rendered to the scientific world must be particularly noticed the clear and judi- cious arrangement which he imparted to the Cambridge Botanical Museum, to the collections in the Royal Gardens at Kew, and to the Museum of Ipswich, which last, planned and carried out under his guidance, stands out in striking contrast to so many of our local museums as an institution in which the objects preserved have really an educational and scientific value. The attention of Professor Henslow was constantly directed to subjects of geological interest, and frequently to phenomena little observed by others, of perhaps obscure character, but into the caus- ation of which his ingenuity delighted to inquire. Of this order was the peculiar disintegration of flints, and the concentric bands of various colour often found in flint and other silicious pebbles. And he was equally ready in turning to practical account the results of his scientific observations. Thus his acquaintance with the chemistry of agriculture enabled him at once to appreciate the value to the farmer of the phosphate-nodules which abound in the Tertiary ANNIVERSARY ADDRESS. XXXVIi Formations of the Eastern Counties. No credit, no reward, no con- sideration, even as the discoverer, was claimed by him, but he at once freely gave the widest publicity to his discovery ; and the result has been that an enormous store of wealth has accrued alike to landlord and tenant over a very large area of country, whilst up to the day of his death no acknowledgment was ever made of his services to the public weal. His sympathies were enlisted in every branch of science, and in many educational efforts. He was one of the first Examiners in the University of London, and was up to the last an efficient member of its Council. He aided actively in the Society for the Diffusion of Useful Knowledge, and in the working of the Ray Club and Palaon- tographical Society ;. and when assistance was needed for the pub- lication of a useful work, or the relief of the needy in his own pro- fession, or among naturalists, the kindly heart of Professor Henslow was never appealed to in vain. . JosepH JAMES Forrester, created, for his services in develop- ing the resources of Portugal, Baron de Forrester in that country, was a man of unusual vigour of intellect, who, in his capacity of a vine-grower in the Alto Douro district, paid much attention to the geological character of the subsoils. Several works published by him on the capabilities of Portugal and on the port-wine trade, and the elaborate map of the river Douro, which he exhibited at the Universal Exposition of Paris in 1855, attest the perseverance of his obser- vations, and awakened a regret that, apart from his loss as an active and useful citizen of the world, we should so soon have lost a pro- mising Fellow of the Society. It was one of his great pleasures to ascend and descend the Douro in his own boat, sketching and photo- graphing the granite rocks, and the peculiarities of their junction with the clay-slate; and it was in one of these expeditions that he was unfortunately drowned, at the age of 51, by the upsetting of his boat in the rapids. Mr. Wri1u1am Horton, of West Hartlepool, was remarkable as one of the chief contributors to the geology and fossil botany of our northern coal-fields. In 1830 he communicated to the Natural History Society of Newcastle “ Notes on the New Red Sandstone,” and in the next following years contributed to our Society papers “On the Stratified Basalt associated with the Carboniferous Forma- tions of the North of England,” “ On Coal,” and “ On the Occurrence of certain Minerals in Northumberland.” James MacApam was born at Belfast in January 1801, and died Ist June, 1861. His family belonged to the commercial class, and he was himself actively engaged in business throughout his life. From boyhood he had a taste for classics, for continental literature, and for different departments of physical science. In early life he attended some of the college classes in the Royal Academical Tnstitution of Belfast, and after a lapse of some years, amid the XXXVIlii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. turmoil of commerce, he became a graduate of Trinity College, Dublin. He was one of the eight original founders of the Natural History and Philosophical Society of Belfast, established in 1821 ; he took an active part in promoting the erection of their museum in 1830, and filled the office of President of that Society at the time of his death, He was also one of the founders of the Botanic Garden at Belfast. He took a warm and active interest in the various educational and scientific institutions of his native town, and his time and advice were ever at the service of the young who were entering on their studies and stood in need of the encouragement and assistance of their seniors. In this and various other ways, he exerted great local influence for the promotion of physical science, and especially of geology, his own favourite pursuit. For a long period, the intervals of relaxation from business were steadily devoted by Mr. MacAdam to. the investigation of the geo- logical structure of the north of Ireland ; the results being occasionally made known through the Geological Society of Dublin, the volumes of whose ‘ Transactions’ bear testimony to his industry and ability as a geologist. The most important of his papers published there is one upon the structure of a very interesting district in the county of Donegal. But the service rendered to our science by his papers is perhaps less important than one which he was not spared to complete. By personal exertion continued through upwards of twenty years, and by expending considerable sums of moneyin employing intelligent collectors, he had succeeded in bringing together a vast assemblage of fossils from the Upper Secondary Rocks of Ireland; and in the arranging and naming of these he was still actively engaged at the time of his last illness. This collection is believed to contain many rare and not a few new species. It was intended to be employed in illustrating a memoir on the north-east of Ireland, to be contri- buted to our Society under the joint authorship of himself and Dr. Bryce of Glasgow, formerly of Belfast. A paper by the latter gentleman, on a portion of the Antrim coast, has already appeared in our ‘ Transactions ;’ and we may hope that he will in a short time carry out the plan arranged between him and his departed friend, and thus, while completing the survey of that coast, make known the riches of this fine collection of fossils, and the various important observations, hitherto unpublished, which have been made by our late associate. Eaton Hopexinson, F.R.S., Professor of the Mechanics of Engi- neering in the University College, London, was born at Anderton, near Northwich in Cheshire, on the 26th February, 1789, and died at Eaglesfield House, Manchester, on the 18th June, 1861. He lost his father in childhood, and was sent to the grammar-school at Northwich. He was originally intended for the church; but his mother’s circumstances having compelled him to renounce this pro- jee ect and enter into trade, he went to reside in Manchester. During s residence in that city for nearly half a century, he devoted his ANNIVERSARY ADDRESS. XXX1X time to making experiments on the strength of iron, stone, and wood, and gave to the world the formule for solid and hollow pillars of iron, which have been adopted in England and the Continent, and which are now the basis of calculation for all structures made of that metal, Mr. Hodgkinson was probably the most laborious and care- ful experimenter that has ever devoted himself to the study of the laws which regulate the strength of materials; and all his great labours were given to the investigation of truth for its own sake, without any pecuniary returns, but at a considerable loss to himself. He was for some years President of the Manchester Literary and Philosophical Society, in whose Memoirs most of his papers appeared. Although he did not write much on geology, he was warmly attached to the science, and possessed a good collection of coal-measure plants, which he delighted in showing to his friends. In private life his simple habits and kindly disposition endeared him to a large circle of acquaintances, who have sustained a loss which will not soon be replaced. Taomas Witt1am Arxrnson became a Fellow of this Society in 1859, on his return from the long wanderings in Asiatic Russia, described in his ‘Travels in Siberia.’ Originally an architect, he added high qualifications as an artist to the energy and endurance that distinguished him as a traveller. It may, however, be regretted that his connection with our Society had not commenced before rather than after his travels, destined as he was to visit so many of the most interesting districts of the Altai and of the chains bordering on the Kirghiz Steppe. Sir Cuartes Fettows was born in 1799, and became well known to the public on producing, in 1838, the Journal of his ‘ Excursions in Asia Minor,’ memorable for the discoveries of ancient buildings in the valley of the Lycian Xanthus. He subsequently published several other works on the antiquities of the same region, in the exploration of which he was associated with Edward Forbes, Captain Graves, and Captain Spratt. Sir Charles resided latterly in the Isle of Wight, where he took a leading part in the question of the estab- lishment of a local museum, geological and antiquarian, at Caris- brook Castle. M. L. A, Necker pr Saussure, elected in 1808 a Foreign Member of the Society, was at one time Professor of Mineralogy at Geneva ; and although for the last twenty years he had buried himself in close retirement at Portree in the Isle of Skye, where he died, was in the earlier part of his life an active contributor to scientific literature. In our own volumes he published papers ‘‘ On a probable Cause of certain Earthquakes,” and on the geological laws which govern the of which metalliferous deposits with regard to the rock-formations position of the crust of the earth is formed. His ‘ Travels in Scotland,’ published in Paris in 1821, record his observations made in 1806, 1807, 1808, in the scientific part of which sl PROCEEDINGS OF THE GEOLOGICAL SOCIETY, work he endeavours judiciously to describe and explain phenomena without having recourse to the extreme views of either Werner or Hutton, between whose rival schools the controversy at that time ran high. In the ‘Edinburgh Philosophical Journal’ and in the ‘ Bibliotheque Universel’ he published views on mineralogy which he afterwards gave to the world, in 1835, under the title of “ Le Régne Minéral ramené aux méthodes de P'Histoire Naturelle.” © In this work he avoided the extreme views of previous authors, who had ascribed too great importance exclusively to external properties or to mere composition, and in a series of analytical tables conferred a great boon on the student working practically at the discrimination of minerals. THE ANNIVERSARY ADDRESS. By Pror. T. H. Hoxtry, Src.G.8., &., &. Mercnants occasionally go through a wholesome, though trouble- some and not always satisfactory, process which they term “ taking stock.” After all tho excitement’ of speculation, the pleasure of gain, and the pain of loss, the trader makes up his mind to face facts and to learn the exact quantity and quality of his solid and reliable possessions. The man of science does well sometimes to imitate this procedure ; ; and, forgetting for the time the importance of his own small win~ nings, to re-examine the common stock in trade, so that he may make sure how far the store of bullion in the cellar—on the faith of whose existence so much paper has ‘been circulating—is really the solid gold of truth. i The Anniversary Mecting of the Geblosieal Society seems to be an occasion well suited for an undertakings of this kind—for an in- quiry, in fact, into the nature and the value of the present results of paleontological investigation ; and the more so, as all those who have paid close attention to’ the late multitudinous discussions, in which palsontology is implicated, must have felt the urgent neces- sity of some such scrutiny. First in order, as the most definite and unquestionable of all the results of paleontology, must be mentioned the immense extension and impulse given to botany, zoology, and comparative anatomy by the investigation of fossil remains. Indeed, the mass of biological facts has been so greatly increased, and the range of biological speculation has been so vastly widened, by the researches of the geologist and paleontologist, that it is to be feared there are naturalists in existence who look upon geology as Brindley re- garded rivers. ‘ Rivers,” said the great engineer, “were made to feed canals ;” and geology, some seem to think, was solely created to advance comparative anatomy, ANNIVERSARY ADDRESS. xli _ Were such a thought justifiable, it could hardly expect to be received with favour by this assembly. But it is not justifiable. Your favourite science has her own great aims independent of all others; and if, notwithstanding her steady devotion to her own progress, she ean scatter such rich alms among her sisters, it should be remembered that her charity is of the sort that does not im- poverish, but ‘ blesseth him that gives and him that takes.” Regard the matter as we will, however, the facts remain. Nearly 40,000 species of animals and plants have been added to the Sy- stema Nature by paleontological research. This is a living popu- lation equivalent to that of a new continent in mere number; equi- valent to that of a new hemisphere, if we take into account the small population of insects as yet found fossil, and the large pro- portion and peculiar organization of many of the Vertebrata. But, beyond this, it is perhaps not too much to say that, except for the necessity of interpreting paleontological facts, the laws of distribution would have received less careful study ; while few com- parative anatomists (and those not of the first order) would have been induced by mere love of detail, as such, to study the minutiz of osteology, were it not that in such minutie lie the only keys to the most interesting riddles offered by the extinct animal world. These assuredly are great and solid gains. Surely it is matter for no small congratulation that in half a century (for paleontology, though it dawned earlier, came into full day only with Cuvier) a subordinate branch of biology should have doubled the value and interest of the whole group of sciences to which it belongs. But this is not all. Allied with geology, paleontology has estab- lished two laws of inestimable importance: the first, that one and the same area of the earth’s surface has been successively occupied by very different kinds of living beings; the second, that the order of succession established in one locality holds good, approximately, in all. The first of these laws is universal and irreversible; the second is an induction from a vast number of observations, though it may possibly, and even probably, have to admit of exceptions, As a consequence of the second law, it follows that a peculiar relation frequently subsists between series of strata, containing organic re- mains, in different localities. The series resemble one another, not only in virtue of a general resemblance of the organic remains in the two, but also in virtue of a resemblance in the order and character of the serial succession in each, There is a resemblance of arrange- ment; so that the separate terms of each series, as well as the whole series, exhibit a correspondence. Succession implies time; the lower members of a series of sedi- mentary rocks are certainly older than the upper; and when the notion of age was once introduced as the cquivalent of succession, it was no wonder that correspondence in succession came to be looked upon as correspondence in age, or ‘‘ contemporaneity.” And, indeed, so long as relative age only is spoken of, correspondence in succession 7s correspondence in age; it is relative contemporaneity, xlii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. But it would have been very much better for geology if so loose and ambiguous a word as ‘ contemporaneous”’ had been excluded from her terminology, and if, in its stead, some term expressing similarity of serial relation, and excluding the notion of time altogether, had been employed to denote correspondence in position in two or more series of strata. In anatomy, where such correspondence of position has con- stantly to be spoken of, it is denoted by the word “ homology” and its derivatives ; and for Geology (which after all is only the anatomy and physiology of the earth) it might be well to invent some single word, such as “ homotaxis ” (similarity of order), in order to express an essentially similar idea. This, however, has not been done, and most probably the inquiry will at once be made—To what end burden science with a new and strange term in place of one old, familiar, and part of our common language? The reply to this question will become obvious as the inquiry into the results of paleontology is pushed further. Those whose business it is to acquaint themselves specially with the works of paleontologists, in fact, will be fully aware that very few, if any, would rest satisfied with such a statement of the conclusions of their branch of biology as that which has just been given. Our standard repertories of paleontology. profess to teach us far higher things—to disclose the entire succession of living forms upon the surface of the globe; to tell us of a wholly different distribution of climatic conditions in ancient times; to reveal the character of the first of all living existences; and to trace out the law of pro- gress from them to us. It may not be unprofitable to bestow on these professions a some- what more critical examination than they have hitherto received, in order to ascertain how far they rest on an irrefragable basis, or whether, after all, it might not be well for paleontologists to learn a little more carefully that scientific “ ars artium,” the art of saying ‘“‘T don’t know.” And to this end let us define somewhat more exactly the extent of these pretensions of paleontology. Every one is aware that Professor Bronn’s ‘ Untersuchungen’ and Professor Pictet’s ‘'Traité de Paléontologie’ are works of stan- dard authority, familiarly consulted by every working paleontologist. It is desirable to speak of these excellent books, and of their distin- guished authors, with the utmost respect and in a tone as far as possible removed from carping criticism; indeed, if they are spe- cially cited in this place, it is merely in justification of the assertion that the following propositions, which may be found implicitly or explicitly in the works in question, are regarded by the mass of palzontologists and geologists, not only on the Continent but in this country, as expressing some of the best-established results of pale- ontology. Thus :— Animals and plants began their existence together, not long after the commencement of the deposition of the sedimentary rocks, and then succeeded one another in such a manner that totally distinct ANNIVERSARY ADDRESS. xliit faunz and flore occupied the whole surface of the earth, one after the other, and during distinct epochs of time. A geological formation is the sum of all the strata deposited over the whole surface of the earth during one of these epochs: a geo- logical fauna or flora is the sum of all the species of animals or plants which occupied the whole surface of the globe during one of these epochs. . The population of the earth’s surface was at first very similar in all parts, and only from the middle of the Tertiary epoch onwards began to show a distinct distribution in zones. The constitution of the original population, as well as the numerical proportions of its members, indicates a warmer and, on the whole, somewhat tropical climate, which remained tolerably equable throughout the year. The subsequent distribution of living beings in zones is the result of a gradual lowering of the general tempe- rature, which first began to be felt at the poles. It is not now proposed to inquire whether these doctrines are true or false; but to direct your attention to a much simpler though very essential preliminary question—What is their logical basis ? what are the fundamental assumptions upon which they all logically de- pend? and what is the evidence on which those fundamental proposi- tions demand our assent ? These assumptions are two: the first, that the commencement of the geological record is coeval with the commencement of life on the globe; the second, that geological contemporaneity is the same thing as chronological synchrony. Without the first of these assumptions there would of course be no ground for any statement respecting the commencement of life; without the second, all the other statements cited, every one of which implies a knowledge of the state of dif- ferent parts of the earth at one and the same time, will be no less devoid of demonstration. The first assumption obviously rests entirely on negative evidence. This is, of course, the only evidence that ever can be available to prove the commencement of any series of phenomena; but, at the same time, it must be recollected that the value of negative evidence depends entirely on the amount of positive corroboration it re- ceives. If A B wishes to prove an alibi, it is of no use for him to get a thousand witnesses simply to swear that they did not see him ‘in such and such a place, unless the witnesses are prepared to prove that they must have seen him had he been there. But the evidence that animal life commenced with the Lingula-flags, e. g., would seem to be exactly of this unsatisfactory uncorroborated sort. The Cambrian witnesses simply swear they “haven’t seen anybody their way ;” upon which the counsel for the other side immediately puts in ten or twelve thousand feet of Devonian sandstones to make oath they never saw a fish or a mollusk, though all the world knows there were plenty in their time. But then it is urged that, though the Devonian rocks in one part of the world exhibit no fossils, in another they do, while the lower xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Cambrian rocks nowhere exhibit fossils, and hence no living being could have existed in their epoch. To this there are two replies: the first, that the observational basis of the assertion that the lowest rocks are nowhere fossiliferous is an amazingly small one, seeing how very small an area, in com- parison to that of the whole world, has yet been fully searched: the second, that the argument is good for nothing unless the unfossili- ferous rocks in question were not only contemporaneous in the geo- logical sense, but synchronous in the chronological sense. ‘To use the albz illustration again. If a man wishes to prove he was in neither of two places, A and B, on a given day, his witnesses for each place must be prepared to answer for the whole day. If they can only prove that he was not at A in the morning, and not at B in the afternoon, the evidence of his absence from both is nil, because he might have been at Bin the morning and at A in the afternoon. Thus everything depends upon the validity of the second assump- tion. And we must proceed to inquire what is the real meaning of the word ‘“ contemporaneous” as employed by geologists. To this end a concrete example may be taken. The Lias of England and the Lias of Germany, the Cretaceous rocks of Britain and the Cretaceous rocks of Southern India, are termed by geologists ‘‘ contemporaneous” formations; but when- ever any thoughtful geologist is asked whether he means to say that they were deposited synchronously, he says ‘‘ No,—only within the same great epoch.” And if, in pursuing the inquiry, he is asked what may be the approximate value in time of a “great epoch ”— whether it means:a hundred years, or a thousand, or a million, or ten million years—his reply is, “I cannot tell.” If the further question be put, whether physical genteel ig in possession of any method by which the actual synchrony (or the reverse) of any two distant deposits can be ascertained, no such method can be heard of; it being admitted by all the best autho- rities that neither similarity of mineral composition, nor of physical character, nor even direct continuity of stratum, are absolute proofs of the synchronism of even approximated sedimentary strata: while, for distant deposits, there seems to be no kind of physical evidence attainable of a nature competent to decide whether such deposits were formed simultaneously, or whether they possess any given differ- ence of antiquity. To return to an example already given. All’ competent authorities will probably assent to the proposition that physical geology does not enable us in any way to reply to this question—Were the British Cretaceous rocks deposited at the same time as those of India, or are they a million of years younger or a million of years older? Is paleontology able to succeed where physical geolegy fails? Standard writers on paleontology, as has been seen, assume that she can. They take it for granted, that deposits containing similar organic remains are synchronous—at any rate in a broad sense; and yet, those who will study the eleventh and twelfth chapters of Sir Henry ANNIVERSARY ADDRESS. xly De la Beche’s remarkable ‘ Researches in Theoretical Geology,’ pub- lished now nearly thirty years ago, and will carry out the arguments there most luminously stated to their logical consequences, may very easily convince themselves that even absolute identity of organic contents is no proof of the synchrony of deposits, while absolute diversity is no proof of difference of date. Sir Henry De la Beche goes even further, and adduces conclusive evidence to show that the different parts of one and the same stratum, having a similar composition throughout, containing the same organic remains, and having similar beds above and below it, may yet differ to any con- ceivable extent in age. Edward Forbes was in the habit of asserting that the similarity of the organic contents of distant formations was primd facie evidence, not of their similarity, but of their difference of age ; and holding as he did the doctrine of single specific centres, the conclusion was as legitimate as any other ; for the two districts must have been occupied by migration from one of the two, or from an intermediate spot, and the chances against exact coincidence of migration and of imbedding are infinite. 7 In point of fact, however, whether the hypothesis of single or of multiple specific centres be adopted, similarity of organic contents cannot possibly afford any proof of the synchrony of the deposits which contain them; on the contrary, it is demonstrably compatible with the lapse of the most prodigious intervals of time, and with interposition of vast changes in the organic and inorganic worlds, between the epochs in which such deposits were formed. On what amount of similarity of their faunze is the doctrine of the contemporaneity of the European and of the North American Silu- rians based? In the last edition of Sir Charles Lyell’s ‘ Elementary Geology’ it is stated, on the authority of a former President of this Society, the late Daniel Sharpe, that between 30 and 40 per cent. of the species of Silurian Mollusca are common to both sides of the Atlantic. By way of due allowance for further discovery, let us double the lesser number and suppose that 60 per cent. of the species are common to the North American and the British Silurians., Sixty per cent. of species in common is, then, proof of contempo- raneity. Now suppose that, a million or two of years hence, when Britain has made another dip beneath the sea and has come up again, some geologist applies this doctrine, in comparing the strata laid bare by the upheaval of the bottom, say, of St. George’s Channel with what may then remain of the Suffolk Crag. Reasoning in the same way, he will at once decide the Suffolk Crag and the St, George’s Channel beds to be contemporancous ; although we happen to know that a vast period (even in the geological sense) of time, and physical changes of almost unprecedented extent, separate the two. But if it be a demonstrable fact that strata containing more than 60 or 70 per cent. of species of Mollusca in common, and compara- tively close together, may yet be separated by an amount of geolo- xlvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY. gical time sufficient to allow of some of the greatest physical changes the world has seen, what becomes of that sort of contemporaneity the sole evidence of which is a similarity of facies, or the identivy of half a dozen species, or of a good many genera? And yet there is no better evidence for the contemporaneity as- sumed by all who adopt the hypotheses of universal faunze and flore, of a universally uniform climate, and of a sensible cooling of the globe during geological time. There seems, then, no escape from the admission that neither physical geology nor paleontology possesses any method by which the absolute synchronism of two strata can be demonstrated. All that geology can prove is local order of succession. It is mathematically certain that, in any given vertical linear section of an undisturbed series of sedimentary deposits, the bed which lies lowest is the oldest. In any other vertical linear section of the same series, of course, corresponding beds will occur in a similar order; but, however great may be the probability, no man can say with absolute certainty that the beds in the two sections were synchronously deposited. For areas of moderate extent, it is doubtless true that no practical evil is likely to result from assuming the corresponding beds to be synchronous or strictly contemporaneous ; and there are multitvdes of accessory circumstances which may fully justify the assumption of such synchrony. But the moment the geologist has to deal with large areas or with completely separated deposits, then the mischief of confounding that “ homotaxis” or “ similarity of arrangement,” which can be demonstrated, with “synchrony” or “identity of date,”’ for which there is not a shadow of proof, under the one com- mon term of “ contemporaneity”’ becomes incalculable, and proves the constant source of gratuitous speculations. For anything that geology or paleontology are able to show to the contrary, a Devonian fauna and flora in the British Islands may have been contemporaneous with Silurian life in North America, and with a Carboniferous fauna and flora in Africa, Geographical pro- vinces and zones may have been as distinctly marked in the Paleozoic epoch as at present, and those seemingly sudden appearances of new genera and species, which we ascribe to new creation, may be simple results of migration. It may be so; it may be otherwise. In the present condition of our knowledge and of our methods, one verdict—* not proven, and not proyeable’—must be recorded against all the grand hypotheses of the paleontologist respecting the general succession of life on the globe. The order and nature of terrestrial life as a whole are open questions. Geology at present provides us with most valuable topographical records, but she has not the means of working them up into a universal history. Is such a universal history, then, to be regarded as unattainable? Are all the grandest and most interest- ing problems which offer themselves:to the geological student essen- tially insoluble? Is he in the position of a scientific Tantalus— doomed always to thirst for a knowledge which he cannot obtain? ANNIVERSARY ADDRESS. xivii The reverse is to be hoped; nay, it may not be impossible to in- dicate the source whence help will come. In commencing these remarks, mention was made of the great obligations under which the naturalist lies to the geologist and paleontologist. Assuredly the time will come when these obliga- tions will be repaid tenfold, and when the maze of the world’s past history, through which the pure geologist and the pure paleonto- logist find no. guidance, will be securely threaded by the clue fur- nished by the naturalist. All who are competent to express an opinion on the subject are at present agreed that the manifold varieties of animal and vegetable form have not either come into existence by chance, nor result from capricious exertions of creative power ; but that they have taken place in a definite order, the statement of which order is what men of science term a natural law. Whether such a law is to be regarded as an expression of the mode of operation of natural forces, or whether it is simply a statement of the manner in which a supernatural power has thought fit to act, is a secondary question, so long as the existence of the law and the possibility of its discovery by the human intellect are granted. But he must be a half-hearted philo- sopher who, believing in that possibility, and having watched the gigantic strides of the biological sciences during the last twenty years, doubts that science will sooner or later make this further step, so as to become possessed of the law of evolution of organic forms— of the unvarying order of that great chain of causes and effects of which all organic forms, ancient and modern, are the links. And then, if ever, we shall be able to begin to discuss, with profit’ the questions respecting the commencement of life, and the nature of the successive populations of the globe, which so many seem to think are already answered. The preceding arguments make no particular claim to novelty ; indeed they have been floating more or less distinctly before the minds of geologists for the last thirty years; and if, at the present time, it has seemed desirable to give them more definite and syste- matic expression, it is because paleontology is every day assuming a greater importance, and now requires to rest on a basis whose firmness is thoroughly well assured. Among its fundamental con- ceptions, there must be no confusion between what is certain and what is more or less probable*. But, pending the construction of a surer foundation than paleontology now possesses, it may be in- structive, assuming for the nonce the general correctness of the ordinary hypothesis of geological contemporaneity, to consider whether the deductions which are ordinarily drawn from the whole body of paleontological facts are justifiable. The evidence on which such conclusions are based is of two kinds, negative and positive. The value of negative evidence, in connexion with this inquiry, has been so fully and clearly discussed * “Te plus grand service qu’on puisse rendre 4 la science est d’y faire place nette avant d’y rien construire.”—Cuvier, xlvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY. in an address from the chair of this Society*, which none of us have forgotten, that nothing need at present be said about it; the more, as tho considerations which have been laid before you have certainly not tended to increase your estimation of such evidence. It will be preferable to turn to the positive facts of palsontology, and to in- quire what they tell us. We are all accustomed to speak of the number and the extent of the changes in the living population of the globe during geological time as something enormous; and indeed they are so, if we regard only the negative differences which separate the older rocks from the more modern, and if we look upon specific and generic changes as great changes, which from one point of view they truly are. But leaving the negative differences out of consideration, and looking only at the positive data furnished by the fossil world from a broader point of view—from that of the comparative anatomist who has made the study of the greater modifications of animal form his chief business—a surprise of another kind dawns upon the mind; and under this aspect the smallness of the total change becomes as astonishing as was its greatness under the other. There are two hundred known orders of plants ; of these not one is certainly known to exist exclusively in the fossil state. The whole lapse of geological time has as yet yielded not a single new ordinal type of vegetable structure. The positive change in passing from the recent to the ancient animal world is greater, but still singularly small. No fossil animal is so distinct from those now living as to require to be arranged even in a separate class from those which contain existing forms. It is only when we come to the orders, which may be roughly esti- mated at about a hundred and thirty, that we mect with fossil animals so distinct from those now living as to require orders for themselves; and these do not amount, on the most liberal estimate, to more than about ten per cent. of the whole. There is no certainly known extinct order of Protozoa; there is but one among the Ccelenterata—that of the rugose corals ; there is none among the Mollusca; there are three, the Cystidea, Blastoidea, and Edrioasterida, among the Echinoderms; and two, the Trilobita and Eurypterida, among the Crustacea; making altogether five for the great subkingdom of Annulosa. Among Vertebrates there is no ordinally distinct fossil fish: there is only one extinct order of Amphibia—the Labyrinthodonts; but there are at least four distinct orders of Reptilia, viz. the Ichthyosauria, Plesiosauria, Pterosauria, Dinosauria, and perhaps another or two. There is no known extinct order of :Birds, and no certainly known extinct order of Mammals, the ordinal distinctness of the ‘‘ Toxodontia ” being doubtful. The objection that broad statements of this kind, after all, rest largely on negative evidence is obvious, but it has less force than might at first be supposed; for, as might be expected from the * Anniversary Address for 1851, Quart. Journ. Geol. Soc. vol. vii. t See Hooker’s ‘Introductory Essay to the Flora of Tasmania,’ p. xxiii. © » ANNIVERSARY ADDRESS. xlix circumstances of the case, we possess more abundant positive evidence regarding Fishes and marine Mollusks than respecting any other forms of animal life; and yet these offer us, through the whole range of geological time, no species ordinally distinct from those now living ; while the far less numerous class of Echinoderms presents three, and the Crustacea two such orders, though none of these come down later than the Paleozoic age. Lastly, the Reptilia present the ex- traordinary and exceptional phenomenon of as many extinct as existing orders, if not more; the four mentioned maintaining their existence from the Lias to the Chalk inclusive. Some years ago one of your Secretaries pointed out another kind of positive paleontological evidence tending towards the same con- clusion—afforded by the existence of what he termed “ persistent types ” of vegetable and of animal life*. He stated, on the authority of Dr. Hooker, that there are Carboniferous plants which appear to be generically identical with some now living; that the cone of the Oolitic Araucaria is hardly distinguishable from that of an existing species; that a true Pinus appears in the Purbecks and a Juglans in the Chalk; while, from the Bagshot Sands, a Banksia whose wood is not distinguishable from that of species now living in Aus- tralia had been obtained. Turning to the animal kingdom, he affirmed the tabulate corals of the Silurian rocks to be wonderfully like those which now exist ; while even the families of the Aporosa were all represented in the older Mesozoic rocks. Among the Mollusca similar facts were adduced. Let it be borne in mind that Avicula, Mytilus, Chiton, Natica, Patella, Trochus, Discina, Orbicula, Lingula, Rhynchonella, and Nautilus, all of which are existing genera, are given without a doubt as Silurian in the last edition of ‘Siluria’; while the highest forms of the highest Cephalopods are represented in the Lias by a genus, Belemnoteuthis, which presents the closest relation to the existing Loligo. The two highest groups of the Annulosa, Insecta and Arachnida, are represented in the Coal either by existing genera or by forms differing from existing genera in quite minor peculiarities. Turning to the Vertebrata, the only paleozoic Elasmobranch Fish of which we have any complete knowledge is the Devonian and Car- boniferous Plewracanthus, which differs no more from existing Sharks than these do from one another. Again, vast as is the number of undoubtedly Ganoid fossil Fishes, and great as is their range in time, a large mass of evidence has re- cently been adduced to show that almost all those respecting which we possess sufficient information are referable to the same subordinal groups as the existing Lepidosteus, Polypterus, and Sturgeon; and that a singular relation obtains between the older and the younger Fishes ; the former, the Devonian Ganoids, being almost all members _ ™ See the abstract of a Lecture “On the Persistent Types of Animal Life,” in the ‘ Notices of the Meetings of the Royal Institution of Great Britain,’ June 2, 1859, vol. iii. p. 151, d 1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. of the same suborder as Polypterus, while the Mesozoic Ganoids are almost all similarly allied to Lepidosteus*. Again, what can be more remarkable than the singular constancy of structure preserved throughout a vast period of time by the family of the Pycnodonts and by that of the true Coelacanths; the former persisting, with but insignificant modifications, from the Carbonife- rous to the Tertiary rocks, inclusive; the latter existing, with still less change, from the Carboniferous rocks to the Chalk, inclusive. Among Reptiles, the highest living group, that of the Crocodilia, 1 19 represented at the early part of the Mesozoic epoch by species identical in the essential characters of their organization with those now living, and differing from the latter only in such matters as the form of the articular facets of the vertebral centra, in the extent to which the nasal passages are separated from the cavity of the mouth by bone, and in the proportions of the limbs. And eyen as regards the Mammalia, the scanty remains of Triassic and Oolitic species afford no foundation for the supposition that the organization of the oldest forms differed nearly so much from some of those which now live as these differ from one another. It is needless to multiply these instances; enough has been said to justify the statement that, in view of the immense diversity of known animal and vegetable forms, and the enormous lapse of time indicated by the accumulation of fossiliferous strata, the only circumstance to be wondered at is, not that the changes of life, as exhibited by positive evidence, have been so great, but that they have been so small. Be they great or small, however, it is desirable to attempt to estimate them. Let us therefore take each great division of the animal world in succession, and whenever an order or a family can be shown to have had a prolonged existence, let us endeavour to ascer- tain. how far the later members of the group differ from the earlier ones. If these later members, in all or in many cases, exhibit a certain amount of modification, the fact is, so far, evidence in favour of a general law of change; and, in a rough way, the rapidity of that change will be measured by the demonstrable amount of modification. On the other hand, it must be recollected that the absence of any modification, while it may leave the doctrine of the existence of a law of change without positive support, cannot possibly disprove all forms of that doctrine, though it may afford a sufficient refutation of many of them. The Protozoa.—The Protozoa are represented throughout the whole range of geological series, from the Lower Silurian formation to the present day. The most ancient forms recently made known by Ehrenberg are excessively like those which now exist: no one has ever pretended that the difference between any ancient and any modern Foraminifera is of more than generic value; nor are the * ‘Memoirs of the ssid net Survey of the United Kingdom.—Decade x. Preliminary Essay upon the Systematic Arrangement of the Fishes of the Devo- nian Epoch,’ ANNIVERSARY ADDRESS. hi oldest Foraminifera either simpler, more embryonic, or less differen- tiated than the existing forms. The Celenterata.—The Tabulate Corals have existed from the Silurian epoch to the present day, but 1 am not aware that the ancient Heliolites possesses a single mark of a more embryonic or less differentiated character, or less high organization, than the existing Heliopora. As for the Aporose Corals, in what respect is the Silurian Paleocyclus less highly organized or more embryonic than the modern Fungia, or the Liassic Aporosa than the existing members of the same families ? The Mollusca.—In what sense is the living Waldheimia less embryonic, or more specialized, than the paleozoic Spirifer; or the existing Rhynchonelle, Cranie, Discine, Lingule, than the Silurian species of the same genera? In what sense can Loligo or Spirula be said to be more specialized or less embryonic than Belemnites ; the modern species of Lamellibranch and Gasteropod genera than the Silurian species of the same genera ? The Annulosa.—The Carboniferous Insecta and Arachnida are neither less specialized nor more embryonic than those that now live, nor are the Liassic Cirripedia and Macrura; while several of the Brachyura which appear in the Chalk belong to existing genera, and none exhibit either an intermediate or an embryonic character. The Vertebrata.—Among fishes I have referred to the Coelacanthini (comprising the genera Celacanthus, Holophagus, Undina, and Ma- cropoma) as affording an example of a persistent type; and it is most remarkable to note the smallness of the differences between any of these fishes (affecting at most the proportions of the body and fins, and the character and sculpture of the scales), notwithstanding their enormous range in time. In all the essentials of its very peculiar structure, the Macropoma of the Chalk is identical with the Celacanthus of the Coal. Look at the genus Lepidotus, again, per- sisting without a modification of importance from the Lias to the Eocene formation, inclusive. Or among the Teleostei—in what respect is the Berywz of the Chalk more embryonic or less differentiated than the Beryw lineatus of King George’s Sound? Or to turn to the higher Vertebrata—in what sense are the Liassic Chelonia inferior to those which now exist? How are the Cretaceous Ichthyosauria, Plesiosauria, or Pterosauria less embryonic or more differentiated species than those of the Lias? Or lastly, in what circumstance is the Phascolotherium more em- bryonic, or of a more generalized type, than the modern Opossum ; or a Lophiodon, or a Paleotherium, than a modern Tapirus or Hyrax? These examples might be almost indefinitely multiplied, but surely they are sufficient to prove that the only safe and unquestionable testimony we can procure—positive evidence—fails to demonstrate any sort of progressive modification towards a less embryonic or less generalized type in a great many groups of animals of long-continued geological existence. In these groups there is abundant evidence of variation—none of what is ordinarily understood as progression ; and, hii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. if the known geological record is to be regarded as even any consider- able fragment of the whole, it is inconceivable that any theory of a necessarily progressive development can stand, for the numerous orders and families cited afford no trace of such a process. But it is a most remarkable fact, that, while the groups which have been mentioned, and many besides, exhibit no sign of pro- gressive modification, there are others, coexisting with them, under the same conditions, in which more or less distinct indications of such a process seem to be traceable. Among such indications I may remind you of the predominance of Holostome Gasteropoda in the older rocks as compared with that of Siphonostome Gasteropoda in the later. A case less open to the objection of negative evidence, however, is that afforded by the Tetrabranchiate Cephalopoda, the forms of the shells and of the septal sutures exhibiting a certain increase of complexity in the newer genera. Here, however, one is met at once with the occurrence of Orthoceras and Baculites at the two ends of the series, and of the fact that one of the simplest genera, Nautilus, is that which now exists. The Crincidea, 3 in the abundance of stalked forms in the ancient formations as compared with their present rarity, seem to present us with a fair case of modification from a more embryonic towards a less embryonic condition. But then, on careful consideration of the facts, the objection arises that the stalk, calyx, and arms of the paleeozoic Crinoid are exceedingly different from the corresponding organs of a larval Comatula; and it might with perfect justice be argued that Actimocrinus and Hucalyptocrmus, for example, depart to the full as widely, in one direction, from the stalked embryo of Comatula, as Comatula itself does in the other. The Echinidea, again, are frequently quoted as exhibiting a gradual passage from a more generalized to a more specialized type, seeing that the elongated, or oval, Spatangoids appear after the spheroidal Echinoids. But here it might be argued, on the other hand, that the spheroidal Echinoids, in reality, depart further from the general plan and from the embryonic form than the elongated Spatangoids do; and that the peculiar dental apparatus and the pedicellarize of the former are marks of at least as great differentiation as the petaloid ambulacra and semitee of the latter. Once more, the prevalence of Macrurous before Brachyurous Podophthalmia is apparently a fair piece of evidence in favour of progressive modification in the same order of Crustacea; and yet the case will not stand much sifting, seeing that the Macrurous Podoph- thalmia depart as far in one direction from the common type of Podophthalmia, or from any embryonic condition of the Brachyura, as the Brachyura do in the other; and that the middle terms be- tween Macrura and Brachyura—the Anomura—are little better re- presented in the older Mesozoic rocks than the Brachyura are. None of the cases of progressive modification which are cited from among the Invertebrata appear to me to have a foundation less open to criticism than these; and if this be so, no careful reasoner would, I think, be inclined to lay very great stress upon them. Among ANNIVERSARY ADDRESS. li the Vertebrata, however, there are a few examples which appear to be far less open to objection. It is, in fact, true of several groups of Vertebrata which have lived through a considerable range of time, that the endoskeleton (more particularly the spinal column) of the older genera presents a less -ossified, and so far less differentiated, condition than that of the younger genera. Thus the Devonian Ganoids, though almost all members of the same suborder as Polypterus, and presenting nume- rous important resemblances to the existing genus, which possesses biconcave vertebre, are, for the most part, wholly devoid of ossified vertebral centra. The Mesozoic Lepidosteide, again, have at most biconcave vertebre, while the existing Lepidostews has Salamandroid, opisthoceelous, vertebree. So, none of the Paleozoic Sharks have shown themselves to be possessed of ossified vertebrae, while the majority of modern Sharks possess such vertebre. Again, the more ancient Crocodilia and Lacertilia have vertebre with the articular facets of their centra flattened or biconcave, while the modern mem- bers of the same group have them proccelous. But the most remark- able examples of progressive modification of the vertebral column, in correspondence with geological age, are those afforded by the Pyenodonts among fish, and the Labyrinthodonts among Amphibia. The late able ichthyologist Heckel pointed out the fact, that, while the Pycnodonts never possess true vertebral centra, they differ in the degree of expansion and extension of the ends of the bony arches of the yertebre upon the sheath of the notochord; the Carboniferous forms exhibiting hardly any such expansion, while the Mesozoic genera present a greater and greater development, until, in the Tertiary forms, the expanded ends become suturally united so as to form a sort of false vertebra. Hermann von Meyer, again, to whose luminous researches we are indebted for our present large know-~ ledge of the organization of the older Labyrinthodonts, has proved that the Carboniferous Archegosaurus had very imperfectly deve~ loped vertebral centra, while the Triassic Mastodonsaurus had the same parts completely ossified*. The regularity and evenness of the dentition of the Anoplothe- rium as contrasted with that of existing Artiodactyles, and the assumed nearer approach of the dentition of certain ancient Carni- ' vores to the typical arrangement, have also been cited as exempli- fications of a law of progressive development, but I know of no other cases based on positive evidence which are worthy of particular notice. What then does an impartial survey of the positively ascertained truths of paleontology testify in relation to the common doctrines of progressive modification, which suppose that modification to have taken place by a necessary progress from more to less embryonic forms, or from more to less generalized types, within the limits of the period represented by the fossiliferous rocks ? * As this Address is passing through the press (March 7, 1862), evidence lies before me of the existence of a new Labyrinthodont (Pholidogaster), from the Edinburgh coal-field, with well-ossified vertebral centra, 2 liv PROCEEDINGS OF THE GEOLOGICAL SOCIETY. It negatives those doctrines ; for it either shows us no evidence of any such modification, or demonstrates it to have been very slight ; and as to the nature of that modification, it yields no evidence whatsoever that the earlier members of any long-continued group were more generalized in structure than the later ones. To a certain extent, indeed, it may be said that imperfect ossification | of the vertebral column is an embryonic character ; but, on the other hand, it would be extremely incorrect to suppose that the vertebral columns of the older Vertebrata are in any sense embryonic in their whole structure. Obviously, if the earliest fossiliferous rocks now known are coeval with the commencement of life, and if their contents give us any just conception of the nature and the extent of the earliest fauna and flora, the insignificant amount of modification which can be demonstrated to have taken place in any one group of animals or plants is quite incompatible with the hypothesis that all living forms are the results of a necessary process of progressive develop- ment, entirely comprised within the time represented by the fossili- ferous rocks. Contrariwise, any admissible hypothesis of progressive modification must be compatible with persistence without progression through indefinite periods. ‘And should such an hypothesis eventually be — proved to be true, in the only way in which it can be demonstrated, viz., by observation and experiment upon the existing forms of life, the conclusion will inevitably present itself, that the Palaeozoic, Meso- zoic, and Cainozoic faune and flor, taken together, bear somewhat the same proportion to the whole series of living beings which have occupied this globe, as the existing fauna and flora do to them. Such are the results of paleontology as they appear, and have for some years appeared, to the mind of an inquirer who regards that study simply as one of the applications of the great biological sciences, and who desires to see it placed upon the same sound basis as other branches of physical inquiry. If the arguments which have been brought forward are valid, probably no one, in view of the present state of opinion, will be inclined to think the time wasted which has been spent upon their elaboration. THE QUARTERLY JOURNAL OF THE GEOLOGICAL SOCIETY OF LONDON. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Novemser 6, 1861. The following communications were read :— 1. Note on the Bonn-Caves of Lunet-Viet, Heravtt. By Monsieur Marcet pve Serres, Professor at the “ Faculté des Sciences,” Montpellier. (Abridged. ] Tue discovery of the bone-caves on the Mazet estate, near Lunel- Viel, already dates back thirty-eight years. Since then I have visited some twenty others, of which the names are solely known by the descriptions given of them by myself and my collaborateurs. The femur of an Aurochs brought me by Colonel Prost and Captain Rompleur, R.E., led me to presume that it had been transported into the caves of M. Bouquet and belonged to a bone-deposit of late geo- logical date. The partial search that I immediately made justified my predictions, and the government accorded me a sum sufficient for me to collect every specimen. I had the soil containing the bones sifted, and I was thus able to collect a large number of the bones, which are now in the collection of the ‘“‘ Faculté des Sciences,’ Unfortunately several of the bones were taken from me by some persons more alive to the marvellous than to the interests of science, VOL, XVIII,—PaRT I. B 2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 6, I still regret this loss—a loss the more felt as those who permitted themselves the pilfering did so out of mere curiosity, and I found it impossible to recover them. I am ignorant to what species these purloined specimens may have belonged. ; The discovery of the large cavern was soon followed by that of several others. I have specified them all in my work under the de- sienation of “fissure” and “ gut,” in consequence of their small size compared with the first cave*. The fissure was filled with bones of different animals; there were almost as many as in a grave-yard. We do not yet know the opening by which the bones were carried into the principal cave on the Bouquet property ; for that by which you now enter is in some degree artificial. The entrance was not, in fact, perceived until a mass of calcareous freestone, 35 metres thick, had been removed. Subsequently enlarged, and closed by a door, it now forms the only way into the principal cavern. These first points recognized, and the age of the Miocene lime- stone established, we soon comprehended that there was nothing in common between the formation of these cavities and their filling up. In fact these caves belong to the Tertiary period, whereas the earth (with rolled pebbles) containing the bones and the excrements as clearly belong to the Drift-period (terrains de transport anciens) or to the most recent geological timest. Later we perceived that these rolled pebbles and the fragments of rock were always accompanied by bone-remains, and after a great number of observations we recognized that the presence of the trans- ported materials was essential to the presence of the bones. In fact, where none of the former exist, none of the latter are met with; so that on entering a subterranean cavity which has not been explored, one can decide beforehand whether or not the remains of animals of geological antiquity exist there. In other caverns, on. the contrary, one can feel sure that there is every probability of finding organic remains, especially if a layer of stalagmite covers the pebbly loam. It is, nevertheless, well worth while to observe that the phenomenon of the bone-caves is accompanied by the same circumstances all the world over. The bones are to be referred, some to animals of extinct species, and others to races not to be distinguished from those now living; and these are, notwithstanding, mixed together indiscrimi- nately in the same soil. Finally, the last question which remains is not the least important. It is, to learn to what cause ought to be attributed the singular as- semblage together of so many bones, often accumulated in such large quantities that they are as plentiful as in a cemetery. What we have already said about the almost constant presence of bones in caves where there occur at the same time transported materials, leads to a strong presumption that these remains have been * “Recherches sur les cavernes 4 ossements de Lunel-Viel, Montpellier.” Boehm éditeur, 1839. vo i + At the period of the discovery of the bone-caves of Lunel-Viel none had been previously discovered in Tertiary formations ; since then we have found several in formations of that age. 1861. ] MARCEL DE SERRES—BONE-CAVES. 3 carried in, since they are always accompanied by alluvial deposits. If the Carnivora alone had been the cause of such phenomena, they ought to be found in all ossiferous caves, whereas it is far from being so. A very great number of them offer, i in fact, only herbivo- rous, without a trace of carnivorous animals, On the other hand, the condition of the cave-bones proves that they had been deprived of their flesh and integuments before they were carried into the caves. The numerous fissures connected with them, and the red earth with which these are filled, even the nar- rowest of them, prove in the clearest manner that the bones must have been transported into their present position merely as bare bones, and not otherwise. If, therefore, there are in some caves some bones which have been gnawed, that may have happened before they were swept into the caves. The excrements of Hyzenas are in no wise a proof that these animals lived in the caves where they are discovered. Their solidity and their rounded form would render their transport easily effected. How otherwise can we suppose that carnivorous animals of very unequal strength should live in common, and with a good mutual understanding, as must have happened with the lions, bears, wolves, foxes, otters, beavers, and so many others, which are found in the caverns of Lunel-Viel. It would be very easy to mention many other caves, even of less size, in which animals of habits not less dissimilar are met with; but the caves of the neighbourhood of Montpellier seem to us to suffice for the demonstration of a fact verified by so many observations. I will end this note with an observation of the illustrious physicist so recently lost to science. Humboldt observes that, when a pheno- menon is general and repeated under the same conditions, as has been the case in the filling of the longitudinal and vertical fissures of calcareous rocks, such a phenomenon must have been produced by a cause as general as the effects which group round it. Accord- ing to this double condition, which is presented in all caves where remains of animals of geological date are found, it is impossible to attribute it to any other cause than to violent inundations. . 2. On the PeTRoLeEUM-sPRiInGs in NortH AMERICA, By Axsranam Gessner, M.D., F.G.S. [ Abstract. ] Tae ample information on this subject already published renders it desirable to make use only of the subjoined portion of Dr. Gesner’s communication. The petroleum is obtained by borings, to a depth of from 150 to 500 feet. No reliable record of these borings, or the strata through which they pass, has yet been kept. As a general rule the sections may, however, be represented as—lIst. Soil, ferruginous clay, and boulders; 2nd. Sandstone and conglomerates; 3rd. Shale; 4th. Bituminous shale; and 5th. Oil, underlaid by an oil-bearing stratum B2 4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noves; of fire-clay, containing fragments of Stigmaria and other coal-plants. In the deeper sinkings, sandstones and bituminous shales are brought up by the borers; but in every instance the petroleum appears to be underlaid with a tight stratum of fire-clay. As soon as the oil- bearing stratum is reached, there is usually an escape of carburetted hydrogen gas, and it is discharged with such force that the boring- rods are often blown into the air, as if they had been discharged from a piece of ordnance. The gas is followed by a mixture of oil and gas, and finally by the oil itself, which is thrown in a jet upwards, sometimes to the height of 100 feet. The bore of the well is usually about 4 inches in diameter, being an iron tube let down as the boring proceeds. When the oil appears, the workmen, as soon as they can approach the spot, drive a wooden plug into the iron pipe, and thus prevent the flow of oil, until they are prepared to receive it. Finally, when the natural flow ceases, a pump is applied, and the raising of the petroleum proceeds. Some wells at the outset have produced no less than 4000 gallons of oil in twenty-four hours. At some sites the shallow wells have run out or been exhausted; but by sinking them deeper still greater supplies have been obtained, and which at present appear to be inexhaustible. It seems very certain, therefore, that the reservoirs of oil are fissures penetrating certain oil- bearing strata and the intervening deposits. The specific gravity of the petroleums varies from ‘795 to °881. In general they are of a dark-brown colour. A few wells have pro- duced oils quite clear and transparent ; and simple distillation renders them quite pure and suitable for lamps. The inflammability of the vapour of the mineral oil has given rise to accidents. In one case an oil, tapped by a bore at 330 feet, rose in a fountain 100 feet high, was soon afterwards ignited, and burned for two months before the workmen could plug the iron tube. After some observations on the antiquity of the use of mineral oil in North America and elsewhere, and on the present condition of the oil- and gas-springs and the associated sulphur- and brine-springs in the United States, the author stated that 50,000 gallons of mineral oil are daily raised for home use and for exportation. The oil-region comprises parts of Lower and Upper Canada, Ohio, Pennsylvania, Kentucky, Virginia, Tennessee, Arkansas, Texas, New Mexico, and California. It reaches from the 65th to the 128th degree of longi- tude west of Greenwich ; and there are outlying tracts besides. The oil is said to be derived from Silurian, Devonian, and Car- boniferous rocks. In some cases the oil may have originated during the slow and gradual passage of wood into coal, and in its final trans- formation into anthracite and graphite,—the hydrogen and some carbon and oxygen being disengaged, probably forming hydrocarbons including the oils. In other cases, animal matter may have been the source of the hydrocarbons. Other native asphalts and petroleums were referred to by the author, who concluded by observing that these products were most probably being continually produced by slow chemical changes in fossiliferous rocks. ~~ 1861. ] DAWSON—REPTILES IN THE COAL. 5 3. Notice of the Discovery of ApprrionaL Rematns of Lanp ANIMALS in the Coat-Measvres of the Sourn Jogeins, Nova Scoria. By J. W. Dawson, LL.D., F.G.S., Principal of McGill College. Iy the long range of rapidly wasting cliffs at the South Joggins, every successive year exposes new examples of erect trees and other fossils; and, as the removal of the fallen débris is equally rapid with the wasting of the cliff, it is only by repeated visits that the geologist can thoroughly appreciate the richness of this remarkable section, while every renewed exploration is certain to be rewarded by new facts and specimens. The present notice is intended to record the gleanings obtained in my last visit, in connexion with the presentation to the Society of a suite of specimens of the fossil Reptiles and other land-animals of the locality, which I desire to de- posit in the Museum of the Society, that they may be more fully studied by comparative anatomists, and may remain as types of the species, accessible to British geologists. In the bed which has hitherto alone afforded reptilian remains in its erect trees, two additional examples of these were exposed. One was on the beach, and in part removed by the sea. The other was in the cliff, but so far disengaged that a miner succeeded in bringing it down for me. In the first comparatively little was found. It afforded only a few shells of Pupa vetusta, and scattered bones of a full-grown individual of Dendrerpeton Acadianum. The second tree was more richly stored; and, being i situ, was very instructive as to the mode of occurrence of the remains. Like all the other trees in which reptilian bones have been found, it sprang immediately from the surface of the six-inch coal in Group XV. of my section*, which is also Coal No. 15 of Sir W. E. Logan’s section +. Its diameter at the base was 2 feet, and its height 6 feet, above which, however, an appearance of additional height was given by the usual funnel-shaped sinking of the overlying beds toward the cavity of the trunk. The bark is well preserved in the state of bituminous coal, and presents externally a longitudinally wrinkled surface without ribs or leaf-scars ; but within, on the “ligneous” surface, or that of the inner bark, there are broad flat ribs and transversely elongated scars. The appearances are precisely those which might be expected on an old trunk of my Sigillaria Brownz, to which species this tree may have very well belongedt. The contents of the trunk correspond with those of others pre- viously found. At the bottom is the usual layer of mineral charcoal, consisting of the fallen wood and bark of the tree itself. Above this, about 2 feet of its height are filled with a confused mass of vegetable fragments, consisting of Cordaites, Lepidodendron, Ulo- dendron, Lejidostrobus, Calamites, Trigonocarpum, stipes and fronds of Ferns, and mineral charcoal ; the whole imbedded in a sandy paste blackened by coaly matter. In and at the top of this mass occur the animal remains. The remainder of the trunk is occupied with * Quart. Journ. Geol. Soc. vol. ix. p. 58, and vol, x. p. 20. + Reports of Geol. Survey of Canada, 1845. t Quart. Journ. Geol. Soc. No. 68. p. 523. 6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 6, grey and buff sandstone, containing a few fragments of plants, but no remains of animals, Portions of six reptilian skeletons were obtained from this trunk. The most important of these is a large and nearly complete skeleton of Dendrerpeton Acadianum—by far the most perfect example, as I suppose, of any carboniferous reptile hitherto found. I shall not attempt to describe this specimen, and the new points of structure which it illustrates; but I send the specimen itself, in the hope that its _ details may be examined and described by the eminent naturalist by whom the species was originally named and characterized. Another specimen found in this trunk is a jaw of an animal about the size of Dendrerpeton Acadianum, but with fewer and larger teeth. I send this specimen, which may possibly indicate a new species. The re- maining skeletons were imperfect, and belonged to a small individual of Dendrerpeton Acadianum, two of Hylonomus Lyelli, and one of Hylonomus Wyman. The dislocated condition of these and other skeletons is probably due to the circumstance that, when they were introduced, the matter filling the trunk was a loose mass of fragments, into the crevices of which the bones dropped, on decay of the soft parts. Most of the skeletons lie at the sides of the trunk, as if the animals had before death crept close to the walls of their prison. At the time when the reptiles were introduced, the hollow trunk must have been a pit 4 feet in depth. A number of specimens of Pupa vetusta and Xylobius Sigillarie were found, but nothing throwing further light on these species. I found in this trunk, for the first time, indications of the presence of Insects. The remains observed were disjointed and crushed frag- ments, and as they did not include wings or elytra, I cannot give any decided opinion as to the orders to which they may have belonged. The most probable conjecture would be that they were Neuroptera or Orthoptera of large size. The most interesting fragment obtained is a compound eye, imbedded in coprolitic matter, along with obscure portions of limbs and abdominal segments. Its facets are perfectly preserved, and are lined with a brownish bituminous matter, simu- lating the original pigment. These remains are at least sufficient to prove that in Nova Scotia, as in Europe, Insects inhabited the coal-forests, and that they furnished a portion of the food of Den- drerpeton or its allies. I may mention here that in other coprolites quantities of segments of Xylobius occur, and that there are some little groups of bones of very small reptiles, which are probably co- prolitic. The beds on a level with the top of this erect tree are arenaceous sandstones, with numerous erect Calamites. I searched the surfaces of these beds in vain for bones or footprints of the Reptiles which must have traversed them, and which, but for the hollow erect trees, would apparently have left no trace of their existence. Onasurface of similar character, 60 feet higher, and separated by three coals with their accompaniments, and a very thick compact sandstone, I observed a series of footprints which may be those of Dendrerpeton or Hylonomus. The impressions are too obscure to show the toes di- 1861.} DAWSON—REPTILES IN THE COAL, 7 stinctly. They are half an inch in length, with a stride of about 2 inches. On neighbouring layers were pits resembling rain-marks, and trails or impressions of a kind which I have not before observed. They consist of rows of transverse depressions, about an inch in length and j of an inch in breadth. Lach trail consists of two of these rows running parallel to each other, and about 6 inches apart. Their direction curves abruptly, and they sometimes cross each other. From their position they were probably produced by a land or freshwater animal—possibly a large Crustacean or gigantic Annelide or Myriapod. In size and general appearance they slightly resemble the curious Climactichnites of Sir W. E. Logan, from the Potsdam Sandstone of Canada. I have long looked in vain for remains of land-animals in any other situation than the erect trees of the bed above referred to; but on my last visit I was much gratified by finding shells of Pupa vetusta in a bed 1217 feet below the former, in the upper part of No. 8 of my section, or about 15 feet below Coal No. 37 of Logan’s section. The bed in question is a grey and greyish-blue under-clay, full of Stigmarian rootlets, though without any coal or erect trees at its surface. It is 7 feet thick, with sandstone above and below. The shells occur very abundantly in a thickness of about two inches. They have been imbedded entire ; but most of them have been crushed and flattened by pressure. They occur in all stages of growth; but the most careful examination did not enable me to detect any new species. With them were a few fragments of bone, probably repti- lian. This discovery establishes the existence of Pupa vetusta in this locality during the deposition of twenty-one coal-seams, and the growth and burial of at least twenty forests; and from the oceur- rence of numerous specimens at both extremes of this range, without any other species, it would seem as if, for this locality at least, this was the only representative of the shell-bearing Pulmonates. I append a list of the specimens forwarded to the Museum of the Society, and which, with those formerly sent, constitute a complete collection of the air-breathing animals hitherto recognized in- the Coal-measures of Nova Scotia. | List of specimens of Reptiles, §c., from the Coal-formation of Nova Scotia, accompanying this paper. 1. Hylonomus Lyelli. A nearly complete skeleton, and the maxillary bone and teeth of another specimen. . H. aciedentatus. Maxillary bone, vertebre, ribs, scales, and foot. . H. Wymani. Lower jaw, vertebre and other bones, and scales. . Jaw of a Reptile, supposed to be new. . Skin and dermal plates of Hylonomus. . Dendrerpeton Acadianum, Owen. A nearly complete skeleton. . Pupa vetusta*. From a bed 1217 feet below that in which the species was originally recognized. “TO Ot He OO bo # I observe that Professor Owen proposes the name “ Dendropupa”’ (‘ Palxon- tology,’ 1860, p. 79) ; but I have retained Pupa for the present, not being satisfied 8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, 4. On a Votcantc PHENOMENON witnessed in MANILLA. By Joun G. Verren, Esq. [Extract of a Letter* to Dr. J. D. Hooker, F.R.S., F.G.S.] On the Ist ult. a portion of the River Pasig, on the banks of which the city of Manilla is situated, presented an extraordinary appearance, which continued with but shght interruption from 6to10 a.m. The oldest inhabitant never remembers having seen or heard of a similar phenomenon. The river, for the space of a quarter of a mile from east to west, and having at this point a depth of 15 to 18 feet, appeared in a state of violent fermentation, as if some commotion were taking place in parts invisible to the eye. Quantities of air-bubbles rose to the surface, until the river became covered with foam, and presented the appearance of simmering water. The temperature of the water where this appeared was 100° to 105° Fahr., that of the remainder of the river being 80°. The most remarkable circumstance was the effect produced on the bed of the river. Mounds of mud were raised several feet above the surface of the water, and appeared as if a huge bank of mud had been permanently thrown up in the midst of the river. The temperature of the soil thrown up was 60° to 65° only; but it smelt so offensively as to taint the atmosphere for a considerable distance in the immediate neighbourhood. After having been thus disturbed for the space of four hours, the bed subsided, and the river again resumed its ordinary appearance. — I trust this imperfect description may enable you to judge as to the cause of so curious a commotion. Here it is generally looked upon as being of volcanic origin. Novremser 20, 1861. Charles Sanderson, Esq., C.E., Engineer-in-Chief of the Bombay and Baroda Railway, Surat, Bombay; Ralph Tate, Esq., Teacher of Natural Science, Philosophical Institution, Belfast; James Ray Eddy, Esq., C.E., Carleton Grange, Skipton ; Henry Worms, Esq., of the Inner Temple, 272 Park Crescent, Portland Place; and Haddock that there is any good generic distinction ; though I admit that the form of the aperture suggests the possibility of affinity to Bulimus as well as to Pupa. Mr. J. G. Jeffreys, F.G.S., who considers the shell to be a true Pupa, has kindly directed my attention to traces of ridges observable on the columella of one spe- cimen, and which he regarded as corresponding with the screw-like plates in the young of Pupa wmbilicata and P. ringens. This appearance I have observed in, specimens now in my possession; and at one time I supposed that I had made out a distinct tooth; but, not finding this in other and less compressed indivi- duals, I concluded that it was an effect of pressure; in which, however, I may have been mistaken, as Mr. Jeffreys states that these processes have no connection with the teeth in adult specimens, and that even the toothless variety of P. wmbzli-. cata is furnished with them. '* Dated “Manilla, June 1861.” 1861. ] KEY—BOVEY DEPOSIT. 9 Dennys, Esq., 3 Percy Terrace, Lower Road, Islington, were elected Fellows. The following communications were read :— 1. On the Bovey Deposit. By J. H. Key, Esq. (Communicated by Sir C. Lyell, F.G.S. ) . [ Abridged. ] Introduction.—Singularly enough, as geologists approach our own: era the difficulty of determining the relative age of a particular stra- tum generally increases; and it is in the more modern tertiaries, or deposits succeeding to these, that the greatest amount of difficulty occurs. Among the strata not yet referred to any certain epoch, but broadly designated “tertiary,” are the clay-, sand- and lignite- beds, known to geologists as the “‘ Bovey deposit*.” Having been for the last ten years engaged in working and boring the various beds of clay, I may have become possessed of facts not generally known to geologists, bearing on the origin and nature of the deposit, and which may assist in some degree to fix its relative age. The physical features of the basin.—The Bovey basin is a depres- sion beneath the level of the surrounding country; its length, from Bovey-Tracey to about two miles south of Kingskerswell, is about 10 miles ; its breadth at the upper end about 24 miles, becoming much narrower towards its southern extremity. Two rivers, the Teign and the Bovey, both having their sources in the granite of Dartmoor, run into this basin, meet above Stover, and fall into the sea at Teignmouth. The Teign, the larger and more circuitous, for about 13 or 14 miles before entering the Bovey basin, flows through the slate; and the Bovey River, rising near the centre of the moor, crosses for a short distance the slate, and runs into the basin at its upper end. All the drainage of the basin flows to the estuary of the Teign through an opening between Buckland Point and Hackney, F about half a mile wide. The deposit, surrounded by hills forming the margin of the pasire presents to the eye for the most part a level plain; a large portion immediately above the point where the Teign meets the tide being of a very low flat character, subject to floodings at high spring-tides and heavy rains ; from this point it rises gradually, on the one hand, * The clays and lignites of Bovey-Tracey have been more or less fully described by Dr. Jeremiah Milles in the ‘ Philosophical Transactions’ for 1753; by James Parkinson and Robert Scammell (‘Organic Remains,’ p. 123, &e.) in 1811; C. Hatchett, Trans. Linn. Soc. vol. iv. p. 138, &.; and Phil. Trans. 1804, p. 390, &e.; J. Macculloch, Geol. Trans. 1814, vol ii. p. 18; Mr. Kingston, ‘ Mine- ralogy of Teignmouth’ Conybeare and Phillips, ‘Outlines of the Geology of England and Wales,’ p. 328, and p. 346. A résumé of the facts and opinions offered by the above-mentioned writers was given by Mr. E. W. Brayley in Moore’s ‘ History of Devonshire,’ 1829, vol. i p. 380, &. Further notices have been made by Mr. Godwin-Austen in 1834 and subsequently (Geol. Proceed. vol. ii. p. 103, and Geol. Trans. 2nd ser. vol. xi. p. 439, &e.); by Sir H. De la Beche in 1839 (Geol. Report Devon and Corn- wall, p. 246, &.) ; by Dr. Hooker in 1855 (Quart. Journ. Geol. Soc. vol. xi. p. 566) ; and b 7 Croker in 1856 (Quart. Journ. Geol. Soc. vol. xii. p. 354).—Enr- Q. J. 10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, towards Kingskerswell and Torquay, and on the other, towards the Bovey and Knighton Heaths, where the deposit attains its greatest elevation, 151 feet above the mean level of the sea; farther north it sinks again abruptly, before reaching the slate-hills of Bovey- Tracey, into the valley occupied by the Bovey Pottery. The excep- tions to the generally flat appearance of the lower portion of the deposit occur where the hills forming the border-line of the basin are composed of loose material, when it would appear asif portions had been washed into the depression over the deposit, breaking the general level; thisis observed at Stover, at Sandy Gate, and below Baker’s Hill. For more than a hundred years the Bovey basin has been worked for pipe and potter’s clay, sending off annually large quantities from its shipping port, Teignmouth, to all the principal sea-ports of the United Kingdom. In the northern part of the basin, near Bovey- Tracey, an extensive pottery has been established, excavating the ereater part of its fuel for many years from the adjoining beds of brown-coal or lignite; although at present, I believe, from exhaus- — tion of the beds near the surface, sea-borne coal is used to a consider- able extent. In penetrating beneath the soil of this deposit in any part, the borer meets with nothing harder than gravel or beds of lignite, with the exception of an occasional boulder near the surface; the whole basin being filled up with loose material, consisting of various kinds of clay, silt, sand, lignite, and gravel, deposited in beds, with con- siderable regularity. At one place it has been bored to a depth of 200 feet, and in many places 130 to 150 feet, without meeting rock. The strata of the Bovey Basin.—Commencing on Knighton Heath, and running down the eastern side of the basin, are three principal parallel beds of clay (used in commerce), resting on, separated, and covered by other parallel beds of muddy clay, silt, sand, and gravel, all having a western inclination or dip*. South of the Newton Railway Station the beds of fine clay thin out to a mere trace, but occur again at the Decoy, as a well-defined and regular deposit; but here the dip is changed from the west to the east, the pipe-clay now being found to the west, and the potter’s clay, accompanied by seams of lignite, to the east. Further south, the beds of fine clay thin out again, still keeping their eastern inclination; become again well defined at Aller, especially as regards the potter’s clay and lignite (the pipe-clay having here lost its distinctive qualities, being mixed up with sand and stained with ochreous matters); and onwards in the valley leading to Torquay traces of the clay may be found as far as the Atmospheric Engine-house, above the Torr Railway Station. As regards the strike of the strata on the western side of the deposit (its central and upper portion), not so much is known; no * On the plan of the Bovey basin presented to the Society (not published) the bed to the east, marked red, is the pipe-clay (called locally the ‘ white body ’’), the two western beds, marked green, potter’s clay (or the ‘black body’), and the parallel beds of coarse clay, sand, &c., marked brown. A bed of lignite, in some places well defined, but in others forming merely a trace, accompanies the middle bed of potter’s clay—the lignite marked black in the plan. 1861.] ; KEY—BOVEY DEPOSIT. 11 regular workings have been carried on there, as on the eastern side, the clay found by boring being, for the most part, unsuitable for commerce; it is highly stained with red matter, and gravelly. The little that is known tends to prove that the strike of the beds of clay, sand, and gravel, on the western side, corresponds in direction to an extended outline of the hills on that side, the dip of the beds being the same as at the Decoy, to the east. The north-western part of the basin is better known: here occur large deposits of “ Bovey-coal” or lignite,—an accumulation of tangled masses of vegetation, deposited in regular beds, of various thickness, separated by rough clays and sand. At the Bovey Pottery, where they have been worked extensively, the beds dip to the south- east, and the strike of the strata runs about south-west. The dip of the beds is about 11 inches in a fathom; and their vertical thick- ness is about 100 feet. The lower beds are those worked for fuel; the upper beds being very loose and irregular, and mixed with coarse clay and quartzose gravel. The whole is covered by a deep “ head ” of gravel, such as would be washed from disintegrated granite. Fig. 1.—Section of the Lignite-beds at the Bovey Pottery. (Taken by Dr. Croker in 1841.) Scale ith inch to a fathom. a. “ Head” of rough gravel. 6. Imperfect beds of Lignite, separated by thin seams of rough clay and sand. e. Yellowish sand, 9 feet thick, with bluish clay, sand, and pebbles at the bottom. d. Ten beds of Lignite, separated by thin seams of clay, mixed with vege- table matter. The beds dip to the South-east, with an inclination of 1 foot in 11. The order of deposition observed in this section corresponds with what would be expected to result were a river, bringing various kinds of sediment, to discharge itself into a deep lake. (See further on, page 17.) In the regularity of the ten lower beds of lignite, separated by thin seams of fine clay and vegetable matter, are discerned the characteristics of deposits gradually formed, in deep and comparatively still water, as the lake became filled up with sediment, and the water became shallower, and the current there- 12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, fore more rapid; the beds of lignite becoming more and more irre- gular, and separated by coarser and coarser materials. At length, as the sediment approached the surface, the lignite ceased to be de- posited; the specific gravity of the trees not being sufficient to with- stand the current ; and very rough granitic gravel was alone allowed to become fixed. Fig. 2 is a section across the beds of pipe- and potter’s clay, on the eastern side of the basin, near New Cross. It is constructed on data obtained from the inspection of deep and shallow pits from Knighton to Newton-marsh, from reports of the workmen, from borings, and from the superintendence of the Newton-marsh Clay- works. This section will nearly represent the stratification of the continuous clay-deposit from near Knighton, on the north, to the Newton Railway Station; with this difference, that at the com- mencement of the deposit the seams of fine clay are thin, somewhat irregular, and to some degree mixed with quartz-gravel. The dip is also greater than in the section; and in several places the clay- beds show the action, apparently, of running water, portions of the fine material having been evidently washed away, so that the fine clay runs down to a considerable depth almost perpendicularly. From Knighton southwards the beds of fine clay increase in thick- ness, purity, and regularity to below New Cross, where they begin to diminish in thickness, until lost south of the Newton Railway Station. In two or three places narrow bands of coarser clay, generally stained, run across the finer clay ; and in several places the pipe-clay forms two beds. Fig. 3 represents a section of the beds of clay, &c., at the Decoy*, and has been constructed from numerous observations made at the spot and in its vicinity during ten years. All the seams of clay shown in the section have been worked for considerable distances longitudi- nally, from 60 to 100 feet transversely, and to depths of from 30 to 90 feet. The inclination of the strata here is much greater generally than, and in the opposite direction to, that in the section fig. 2. It will be observed, however, that the superposition of the beds is almost identical with that in the last-mentioned section, taken in the upper part of the basin: the pipe-clay, it is true, is divided into three distinct beds, against two in section fig. 2; but the order of deposition is the same, and the description of one would suit the other. Taking the beds in order upwards, we shall have rough clays, pipe-clay, stiff clay, dark fine clay, rough muddy clays, pot- ter’s clay, and lignite. In section fig. 2, there are two beds of potter’s clay shown; at the Decoy also there is to the east a small second seam of fine clay resting on the one shown in fig. 3. Several seams of lignite, almost perpendicular in dip for the first 15 or 18 feet from the surface, and separated by thin divisions of dark clay and vegetable matter, lie immediately below the bed of potter’s clay in fig. 3. The pipe-clay at the Decoy has been worked Abate 90 feet deep, * This is the ‘‘ deep watercourse below Woolborough,” in Mr. Godwin-Austen’ s Memoir, Geol. Trans. 2nd ser. vol. vi. p. 451. ° ‘sureys yurd yyta Avpo our “8Z-eG\ FE ‘Aeyo UMorg, “QT ¢ TS ” ‘kepo-odig “$Z|'S ‘spoog pure soavory YIM ‘pues yaep ourg “ZT |" “pues pue Avpo Appnut jo spog “[[-¢ a ‘AvP JUS “S| & ‘Aejo Appuy “9T | & ‘Aepo Jo spaq uryy Aq ‘ow ‘spaag ‘soavoT YIM ‘pues yrep oun "2g | & ‘9sivO0 puB oy ‘pueg “GT |< poyedudos oj1usr] Jo sues [[VULG “F -soL1ag ‘Avjo Appnur ysnoy 1G] w ‘Avpo-odtg "FT cD “ABTO UMOAG OUT] " } deyo “kepo-odig ‘0G | 3. ‘Sep JUS “EL | 2. ‘Avpo Appr “6 YTS g szoyogq “Avpo OYA BUS “GL + # “Aepo yee “ZL) & "[OACIS JO, PCOH sD on a s 4 oo ff 8 Ff W SI SS Lf st bf 0 IZ eZerar SF IZ vz - ez 3 9 < ss eS SQ Z : Tas 5 - ‘MOYyL, B 07 yout yy opeag “Koay ay) 20 spag-hingg ay7 fo woNrg—g “OL = a , . nN 489M 94} 0} dip spoq oy, (‘pouo}toys st spaq osoryy Aq E aes ee pordnooo sovds oy) “Joavas puw ‘puvs ‘Avjo osavoo Jo spo “GI-8 - ‘kepo Appnyt ZZ) + ‘AvpO UMOIG OULT *L a ‘kepo-odig “1G 7 0G | oS ‘OPLUSTT JO survos YpLA ‘ATO UWMOA “9 S = ‘Kepo ory FUG “GL | & | “£epo Appuyl “¢ 3 ie ‘kepo Appuyw ‘Bt 9 LIL WS “F = “ABO Js pavyy “OT nl ‘Avo ounyz “e °, ‘Avpo-odig “CT | & ‘ABI Gk Avpo oy YUS “FL | ‘Joawas pur purg *] ‘Avpo uMOIg “ET ) * *JOABAT JO ,, PBITT,, “V we 16 a 8 L/ gf St w sa Ot 6 ra tts oF 7 cr : : “a Zsa . Fe P = rs - : oe - . v a ial oe a) lo Oy Ss “AA 14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, and bored to about 120 feet ; but the clay-seams gradually thin out, in depth, as shown in fig. 3. The pipe-clay and stiff clay in some places run down almost perpendicularly, as shown in bed 3 in fig. 3, representing the appearance of having been partially washed away by a stronger current than at first deposited the bed; and, wherever this occurs, the deposit lying on the bed so partially washed away is of very much rougher texture—generally fine or coarse sand or gravel. Here and there a smooth water-worn stone, generally of quartz, but sometimes slate, is found imbedded in the clay. Nodules of iron-pyrites, of all sizes, from that of small shot to that of an egg, are in some places abundant. Detached pieces of lignite, too, are very common—sometimes with the surface changed into mundic. The clay and accompanying beds at the Decoy rest against the Greensand hills surrounding this portion of the basin ; and the strike © of the beds forms a segment of a circle, somewhat conformable in direction to the shape of the hills. Fig. 4.—Section of Clays and Lignites at Aller. Scale 3th inch to a fathom. 1. “ Head” of gravel. 8. Three seams of lignite, separated by fine clay. 2. Sand. 9. Fine clay. 3. Muddy clay. 10. Rough clay. 4, Lignite. 11. Fine clay. 5. Clay. 12. Rough clay with gravel. 6. Lignite. 13. Rough sand and muddy clay. 7. Clay. The beds dip to the East. Fig. 4 shows a section* of the potter’s clay and lignite-beds at Aller. Here the lignite, separated by beds of clay, is more developed than at the Decoy. No fine pipe-clay has been found at Aller; but underlying the beds shown in the section, and occupying the posi- tion of the pipe-clay, are rough clays, highly stained with ochre, all having an eastern dip. . It will be observed in all the sections here given that the dip of the beds increases from the sides towards the centre of the basin ; and this I believe to be generally the case throughout the deposit. The clay-beds throughout the deposit show no sign of disturbance by slips or faults; they seem perfectly unaffected by any other power than that of water. * Constructed from numerous observations whilst superintending the works during several years. 1861.] | KEY—BOVEY DEPOSIT, | 15 Such is the manner in which the clays and other beds filling the basin are arranged; but, to complete the sketch, a description of the ** Head ” (seen in the various sections), covering the more regularly stratified beds, is necessary. a Lying unconformably on the upturned edges of the clay-beds, and becoming considerably deeper towards the centre of the basin (in some places 30 to 40 ft., in others not more than 3 feet deep), is an accumulation of clay, earthy matter, gravel, rolled stones, and boul- ders, with but little stratification. This is called the “ Head”*. In some places the gravel and boulders, in others the earth and clay, preponderate ; and in many places the “‘ Head” partakes of the cha- racter of the adjacent hills, particularly if they be of loose material. At the Decoy, for instance, the «‘ Head” is composed of flint-nodules, quartz, boulders, and gravel, mixed with clay and earthy matter, and containing also the fossils proper to the adjoining hills. In the upper portion of the basin, the “ Head” is composed of boulders of schorl, quartz, and slate, with sand and gravel. In the low marshes near Newton, the ‘“‘ Head” over the clay-beds is stratified in the following manner :—From the surface to the depth of 3 to 5 feet, loose silt, without shells; then from 3 inches to 2 feet of dark silt, containing a very few shells of the oyster and cockle, and a great number of the shells now common in the estuary below. Immediately under the silt containing shells, in one place, there is a narrow basin-shaped stratum of peat, from 3 to 18 inches thick, lying on which I found the rib and jaw of a Deer. Below the peat is coarse clay from 6 to 7 feet thick, in which are boulders of granite, slate, and quartz; and then the true stratified beds of clay. ; The shelly bed described above is not found in the higher portions of the basin, but only near where the River Teign runs into the salt water; indeed the shells are all found under high-water mark. Materials and probable mode of formation of the Bovey Deposit.— On submitting the pipe-clay to analysis it is found to contain aboutt 63 per cent. of silica, 27 to 29 per cent. of alumina, some oxide of iron, and a trace of lime. The stiff clay has considerably more silica, and in larger particles; the potter’s clay nearly the same amount of silica and alumina as the pipe-clay, with a little carbon, from the lignite, I suppose, to which it also owes its dark colour. The sand and silty beds on and under the clay are composed chiefly of minute pieces of quartz, with some schorl and slate; and in the finer beds of silt there are also numerous shining particles of mica. The greater part of the materials composing the Bovey deposit are, therefore, identical with the component parts of granite, or such * Some account of the “Head,” and of its local differences, is given by Mr. Godwin-Austen at pp. 438 & 440 of his Memoir, Geol. Trans. 2nd ser. vol. vi.— IT. + I say that the pipe-clay contains about 63 per cent. of silica, because all clays being mechanically, and not chemically, combined, samples of pipe- and potter’s clay are found to differ much in their relative proportions of silica and alumina. 16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, as would be expected to be brought to and deposited in a lake * by a river flowing over decomposed granite. A common variety of granite is frequent in Devonshire and Cornwall, containing— RE Nk eye eee os ae en a ar aaah ie 73°04 VIN es ASS eee tees ais eee 18°83 | Pomsives oS Nees Sa eee os ate. Oe 8:51 Mnonesia st FM! Ph Oar. alot Sade ad ae ee 0-83 PN peek. Eee rere arent SRO om CEES eae 0:44 Oxideiie arom | Poe A eR coe Ee ee 13 Wihaorte Welds. Goad: oS Ro a ee 0-18 By looking at the above-mentioned plan of the basin, it will be seen that the clay is continuously deposited in the valley leading to Torquay ; therefore, if a lake once existed, in order to deposit the clay, the current must have run in the direction of Kingskerswell and Torquay, and did not, as now, find an exit to the sea by the way of Teignmouth. In corroboration of this view appears the striking fact, that, were the opening in the chain of: hills surrounding the basin between the hills in the rear of Hackney and Buckland Point (now allowing the River Teign and other streams to escape to the sea by the way of Teignmouth) filled up, the water would accumulate until an ex- tensive lake would be formed, having its outline indicated by the dark line around the margin of the basin on the plan, and discharg- ing its surplus water at the point where now stands Lawe’s Bridge, taking the road over the railway above the Torr Station ; from this point the water of the lake would flow, with a rapid current, through a well-marked channel still existing for some distance, past the Torr Railway-station, and at the foot of the site of Torr Abbey, to the sea in Torbay. The height of this bridge above the mean level of the sea (as kindly communicated to me by Mr. Appleton, surveyor, of Torquay, and taken by him for the Torquay Water-supply) is 171 feet; but, on examining the nature of the ground around this bridge, it is found to be an accumulation of red brick-earth, evidently washed from the immediate neighbourhood,—no doubt choking up the ancient channel of the river for seme considerable depth, certainly for 18 or 20 feet, as seen in the cutting below the bridge. Deducting 20 from 171, we have 151 feet for the height of the surface of the lake above the mean level of the sea. Now this agrees remarkably well with the physical features of the basin. I refer to the fact, that the outline of the lake at that height nearly indicates the outline of the Bovey deposit, no marked member of the deposit being found above that line ¢; and’also that many of the hills forming the margin of * That the area of Bovey-Heathfield and Bellamarsh was once a lake was argued by Mr. Godwin-Austen in 1834 (Geol. Proceed. vol. ii. p. 103): the upper accumulation (‘‘ Head’’) alone, however, was supposed to be referable to such a condition; the lower sands and clays, which are destitute of chalk-flint detritus, not being included in that lacustrine series, but (at least those near Newton) referred to the Cretaceous series by Mr. Godwin-Austen, Geol. Trans. loc. cit. p. 451.—Ep. Q. J. G. S. + The highest part of the deposit is 151 feet above the mean level of the sea, on Knighton Heath. 1861.] | KEY—BOVEY DEPOSIT. 17 the basin present traces of a horizontal ridge at from 130 to 150 feet above the sea, particularly the older and firmer formations,— for instance, Buckland Point, Knowles, the hill over Kingskerswell Church, west of the road, and many others, indicating, it may be supposed, the line of wash near the surface of the lake around its margin, It is easy to conceive the chain of hills around the basin to have been unbroken at some former period, and the consequent existence of a lake, extending from Bovey-Tracey to near Torr, ramifying far up into the lateral valleys, receiving into it the rivers and streams that now run over its bed. Either by the advance of the sea from without, or, more probably, by the gradual opening of a channel between the hills behind Hackney and Buckland Point from within, by the action of the surface-wash of the lake (the waves of which must haye attained considerable power, driven by north or west winds on the point indicated), the lake grew shallower, until it ulti- mately disappeared. In order to prove beyond doubt that the surplus water of the lake discharged itself at the point mentioned (Lawe’s Bridge),it would have been desirable to find some beds of sand or gravel, indicating the bed of a river between Lawe’s Bridge and the sea; but the loose brick- earth forbids. Corroborative evidence, however, of the former chan- nel is found in the bed of peat * on the beach, under Torr Abbey ; showing, no doubt, that a small lake had existed here on the course of the river, and which, after the river had ceased to run in this direction, became filled with a growth of pzat. On the beach, too, near the peat, are spots of very white sandy clay, resembling that of the Bovey deposit, whiter, I think, than any which could be washed from the Red Sandstone cliff; and these may be small portions of a larger bed, deposited by the river before the sea had penetrated so far inland. The evidence offered by the strata of the Bovey deposit itself is, perhaps, the most conclusive as to the existence of this lake; the more prominent facts to be gathered from the plan and sections being these :— 1. That the Bovey deposit is composed of various beds almost identical with the component parts of granite. 2. That the strata run, for the most part, parallel with an ex- tended outline of the marginal hills, and dip from the sides towards the centre of the basin,—the nearer the centre, the greater being the dip. 3. That the finer material is deposited towards the sides, and the coarser towards the centre. 4. That where the basin contracts in width, the finer beds con- tract in thickness, and sometimes disappear ; on the contrary, where the basin widens the purest and most regular beds of clay are found, 5. That the northern part of the deposit is at first irregular, and composed of coarser substances than the central and lower portions. * Bones of Deer have been found in this peat. VOL, XVIII,— PART I, C 18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, 6. That on the eastern side of the basin the beds of fine material are more developed than on the western side. 7. And, lastly, that the various beds run in the direction of, and seem to point to, the River Bovey as the source from whence they were derived. The author then considers the probable conditions of a lake of the size of the Bovey basin, elongate, but contracted in the middle, fed by a rapid river entering the lake at its upper end, and having its tributaries in hills clothed with forest-trees, and consisting of de- composing granite, such as is seen at present on the south-western slopes of Dartmoor, and at the China-clay-works of St. Austell and St. Stephen’s, Cornwall, where the felspar of the granite has decom- posed into a soft white powder, and the quartz and mica form loose sand and gravel of all degrees of size, for a depth, in some places, of more than 40 fathoms. The materials brought by the river to the lake would (the author states) mainly consist of—first, clays of different degrees of fineness, derived from the decomposed felspar ; secondly, earthy matter, from the vegetable mould; thirdly, siliceous sand and gravel, of all de- grees of size; fourthly, vegetable matter, forest-trees and plants of various kinds, from the river, in time of flood or otherwise, under= mining its soft banks clothed with vegetation; and, lastly, stones and boulders of various kinds. The particular plan of deposition, and often redeposition, of these materials is then described by the author, and illustrated by a diagram-plan; and he remarks that the various strata, consequent on the fluctuating quantity of water discharged by the river, would not be deposited horizontally over the bottom of the lake, but would incline more or less from the sides towards the centre, or towards the current, the degree of inclination being regulated chiefly by the strength of the current. Where the lake became very narrow, the beds of sediment would be thin, and the dip great; and where the lake was wide, the dip would be comparatively small; the dip being probably caused by less material being allowed to permanently fix itself at the centre than at the sides; therefore the beds would have a tendency to thicken near the surface, and thin out below, causing the dip to increase towards the centre of the basin. The dip, too, would not be of the same angle throughout, but would be less towards the bottom; the section of such beds assuming a slightly concave form. Thus the lake would go on filling with sediment, the coarse irre- gular deposit of the delta advancing downwards, overlying the more regular parallel beds of the fine material beneath: the materials of the delta would be very thickly deposited towards the centre, and more thinly where the beds of fine material approach the surface, and it would thus form a coarse unstratified “ Head,” overlying the finer stratified deposits. Mr. Key observes that the strata of the Bovey basin, on coms parison, will be found to comply in every material circumstance with 1861.) | KEY—BOVEY DEPOSIT, 19 what would be expected under the conditions above given; and that though in the Bovey deposit we do not find a uniform arrangement of strata on each side of the basin, but a great development of fine material on one side, attended by a corresponding regularity,—and a paucity of clay and much irregularity on the other, yet, supposing that the rivers and streams of the ancient lake ran into it from similar situations to those now running into its bed, we could not expect the same degree of regularity as in the more simple form of the supposed lake and single river. Before the lake became drained by the bursting through, or wear- ing down, of the channel between Buckland Point and Hackney, the ** Head ” on the clay had probably run out over the greater por- tion of the higher part of the deposit, every little stream, of course, bringing its own formation from the hills; hence the flint, chert, and fossils from the Greensand. After the waters had retreated, the Teign, the Bovey, and other streams must have channelled out the loose material of the ‘“‘ Head” considerably ; and to this cause may be attributed the valley at the upper part of the basin, and ethers carrying small watercourses. The author proceeds to state his belief that the Bovey deposits were composed of detritus derived from the surrounding hills, and quietly deposited, with no more disturbance than the occasional flood: that if the relative level of sea and land has been disturbed, it has been over a large area, leaving the physical characters of the country comparatively unaltered ; because he does not observe similar deposits on the neighbouring hills; because the basin appears to have been always limited by the existing hills; because there are no slips or faults in the deposit; because the mode of deposition would account for the inclination of the beds, and for their local variations. Some of the beds have a dip of 45° or 50°, and the lignite at the Decoy (fig. 3) is almost perpendicular ; but this is only for about 15 or 18 feet; afterwards it takes an angle of 40° or 50°, The perpendi- cularity of these beds is accounted for by the author, by the supposi- tion that they have been bent outwards by the slipping or forcing out of the lower wedge-shaped beds, when in a soft state, pressed down by the weight of the “‘ Head.” Recurring, says the author, to the opinion I have heard expressed by some geologists, that the Bovey deposit is a portion of more widely spread beds that once existed over a large area, I can only say, it may be so; but up to the present time I have never seen the least sign of the clay and accompanying beds, either in the valley of the Dart, on the one hand, or that of the Exe, onthe other. On the northern slope of Dartmoor, it is true, near the village of Merton, there is a deposit much resembling that of the Bovey basin, both in regard to the quality of the clay and the manner in which it lies but the great similarity in general features of the Merton basin with that of Bovey explains the derivation of the clay-beds, and adds additional proof that my view of the Bovey beds is correct. The Merton clays are deposited in beds sloping at angles similar to those of Bovey; the deposit is entirely surrounded by hills, except at one ™’ where a c 20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [ Nov. 20, chasm of but short width has been worn away, affording a passage to the drainage of the basin into the Torridge. It is plain that a freshwater lake has existed here, in which clays, brought by streams from the northern slopes of Dartmoor, became deposited ; and that, by the wearing down of the chasm, the lake has drained itself, and the clays have become exposed in the same manner as are those of Bovey basin. In conclusion Mr. Key observes—How strange it is that, amid the proofs of teeming vegetation scattered throughout the Bovey deposit, not a fragment of bone or shell should indicate the existence of animal life! Besides Conifer (of which the mass of the lignite is supposed to be composed), numerous relics of dicotyledonous plants —leaves and seeds—have been collected by Mr. Key, chiefly from the clays at the Decoy; and original sketches of these remains accompanied the paper. Pyritous concretions, probably formed around some vegetable nuclei, occur abundantly, and are also illustrated in Mr. Key’s MSS. After some notes on the indications of an abundant flora, so well worth attentive and extended study, and the apparent absence of animal remains, the author remarks, that, with our present amount of knowledge, we can only suppose’ either that no animals existed around the old lake, or, what is more probable, that the conditions of the strata were inimical to the ~ preservation of animal remains, 2, On the VYoucanic Conss of Paterno and Morra (Sta. ANastasta), Erna. By Signor G. G, GrmMELano. {Communicated by Sir C. Lyell, F.R.S., F.G.8.] Tr base of that portion of the ancient basin of the Simeto which extends from Catania to the Carca di Paterno is formed of pleistocene clay, which is particularly exposed at the Siete della Motta and in the neighbourhood of the Valley of St. Biagio. The post-pliocene conglomerate, with beds of yellow sand and bands of clay, overlies it, and forms the upper part of the hills of Terre-forti, extending down their southern flanks as far as the broad plain of Catania, whilst the freshwater calcareous tuff, which is above it, completes for the neighbourhood of Paterné the series of sedimentary materials of the said basin, © This fertile district, in addition to having been exposed to the pyroxenic lava-streams from Etna, has been disturbed by the de- structive agency of volcanic cones. In the pleistocene period the intrusion of the basalt, coéval- with that of Aci-Castello, ravaged the district of Valcorrente; and at a subsequent period two centres of volcanic action existed at Paterné and at Motta (Santa Anastasia), of which the traces only now remain. These, however, offer such interesting phenomena, that I think it desirable to confine my remarks in this notice exclusively to them. Volcanic Cone of Paterné.—The beautiful city of Paterno, in the Province of Catania, is partly built on a mass of doleritic rock, which, -1861.] =. GEMMELLARO—vVOLCANIC CONES, ~ 21 according to Hoffmann, rises to the height of 620 métres above the level of the sea, and is distant about 12 miles from the existing axis of Etna. After a careful examination of it, the circumference being about a mile, we can make out the central nucleus, the lava, and the broken or fragmentary materials,—all of which are elements con- curring to the formation of a volcanic cone. The central doleritic nucleus rises up directly from below ; its hard crests, still rugged and angular, are exhibited at the rock of St. Mark, that of La Scala, and near the old Norman tower, and on the 8.W., W., and N.W. sides of the rock, which are entirely exposed and perpendicular, and are denuded of all the fragmentary materials which formed the corresponding flanks of the cone. This consists of a compact dolerite of a dark-ashy colour, tending to black, with conchoidal fracture and porphyritic structure, in which olivine occurs, varying in quantity in different portions of the same rock ; nor is it difficult to find augite and labradorite. Some blocks of this rock, broken away from the sides of the cliff, have fallen down on splitting at the surface, which shows itself with an earthy fracture ; whilst christianite in small crystals abounds in the vesicular hollows, as well as in the incomplete fractures, together with incrustations of blue phosphate of iron, which I have not found in the rock in situ and not decomposed. The character of this dolerite is that of large ovoidal masses laterally depressed, the larger diameter varying from 2 to 4 metres; they chiefly occur on the 8.W. side of the cliff, near the Rock of St. Peter; and here, as well as under the Norman Tower, it assumes a prismatic form, which in the former locality is in large irregular prisms from 1 to 3 métres, whilst in the latter they are smaller and more regular. On the N.W. side of the cliff the dolerite _ is impregnated with petroleum. In a kind of articulated junction between the crests of the nodular dolerite, there is found on the Rock of St. Peter a projecting mass of clay with pebbles of sandstone (grés), and another smaller one on the south side of the Rock, in the same matrix ; and these sediment- ary rocks, anterior in age to the volcanic, have been metamorphosed and transported, during the very act of the intrusion of the dolerite, at the commencement of this volcanic action. - The lava in this volcanic cone is easily distinguished. It comes out from the upper part of the cone, from the very spot where now stand the Church and Garden of the Capuchines, which is the most elevated portion of the Rock, and in which are found large quantities of scoriz and volcanic bombs. The lava, when issuing from the crater, flowed in two directions, the one due east, and the other S.W. This latter stream near its mouth of eruption is seen to bi- furcate into two branches, one of which forms the Rock of Calacala, and the other flows due south. The eastern stream extends as far as the Chiesa della Consolazione, in the neighbourhood of which it has been cut through by the road also called that of the Consolation. During the whole of this course, which is about 60 métres, it appears scoriated on the upper surface, to a varying depth of from 3 décim¢tres to a metre, while the rest of the mass is compact and of great thickness, 22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, and does not occur as one homogeneous mass, like the ordinary lavas of Etna, but in gigantic ovoidal masses, articulating one with another. It rests on the outer flank of the cone, formed principally of volcanic scorize which have been altered by the effect of the fumarole of the voleanie current, which, however, it is impossible to describe satis- factorily, or to trace to its termination, in consequence of the ground being in an advanced state of cultivation, and modified by the con- struction of the more outlying dwelling-houses of Paterno, which extend on that side of the hill to the extreme point, The other stream extending to the 8.W. is different. The branch which forms the Rock of Calacala—so called in Sicilian dialect on account of the great steepness of the lava—extends in length about 55 metres; it presents a front of about 25 metres, 1s very compact in the centre, and slightly scoriform on the lower surface, very much so on the upper; it has an average thickness of about 3 métres, has an inclination of 36°, and rests on the volcanic conglomerate, containing rounded pebbles of sandstone and clay which have been altered by the action of the fumaroles of the lava itself. This conglomerate forms part of the outer flank of the cone. The other branch, which flows to the south, has not pre- served its characteristic features so completely; but neither of these two branches of the volcanic stream reaches the base of the cone, nor can their continuation be traced in the plain below ; which proves that the lava did not extend beyond the side of the cone; and the base, which was formed of loose fragmentary materials, having been carried away by the action of water, it has partly fallen down, the upper portion of it still remaining 7 situ. This volcanic cone, even though it may have been denuded by the action of water, nevertheless still affords a large quantity of fragment- ary materials. At the Garden of the Capuchines, in which the crater formerly existed, the scoriz are of a black colour, with a slight reddish tinge, very cellular and fragile; there also occur metamorphosed pre- existing sedimentary rocks. Scorie are found in great abundance along the Strada della Consolazione, under one of the ridges of the Rock of St. Peter (and near the Church of St. Mark), which originally belonged to the inner side of the cone, being found in immediate proximity to the doleritic excrescence, and in a state of compact vol- canic agglomeration, owing to the pressure of the overlying materials which formed the outer flank; whilst the materials which are seen metamorphosed by an arm of the lava-stream near the Rock of Cala- cala, those of the Strada della Consolazione to the south of the rock, and those which are seen on the old road leading to the Salinelle, to the north of this same mass of rocks, are a portion of the fragmentary materials which formed the outer flank of the volcanic cone of Paterno, which are still liable to removal, and in great measure have been carried away by the action of rain-water and the River Simeto, which is constantly extending, with the materials which it carries along with it, the plain of Catania. The ‘rocky elements which constitute the fragmentary navies of this cone are as follows: viz., doleritic scoriz, more or less altered ; 1861.] | GEMMELLARO—VOLCANIC CONES. 23 clay in every state of metamorphism, passing even into thermantite ; and pebbles of sandstone (grés), some of which have been roasted and fall to pieces with the slightest touch, while others, on the contrary, have passed into the state of quartzite. The country around Paterno, is, from north to east, entirely covered with the pyroxenic lavas from Etna; whilst the alluvial soil which forms the plain of Catania is exposed to the south and shows a hori- zontal stratification, as the freshwater calcareous tuff, which overlies it, rests on the west side of the rock. This recent calcareous tuff contains many fossil plants and land-shells, amongst which can be made out Bulimus decollatus, Brug., Heliw vermiculata, L., Helix aspersa, Miill., &c.,—species which are still living and abundant in the neighbourhood. Volcanic Cone of Motta (Sta. Anastasia).—The village of Motta (Sta. Anastasia) is also built on the remains ofa volcanic cone. It is elevated about 813 Paris feet (Hoffmann) above the level of the sea, distant about thirteen miles from the present axis of Etna, and offers on a smaller scale the same phenomena as we have observed at Paterno. ; The sides of the Rock of Motta (Sta. Anastasia), from west to north, are in connection with the pre-existing sedimentary formations; but the village being almost entirely built on it, it is impossible to de- seribe it satisfactorily. The doleritic nucleus is almost perpendicular on the south side, the lower portion of which consists of large and irregular prisms, which from below upwards, for about 25 métres, converge to the centre, whilst in the upper portion the dolerite loses this character and becomes amorphous. To the 8.E. it is connected with great masses of conglomerate, of volcanic scorie, clay, and pebbles of sandstone (grés), altered like those of Paterné. On the east side, this nucleus is cut through by a road, which has exposed between the articulated joints of one of its outer ridges a great mass of clay, with sand and pebbles of grit, altered and contorted by the pressure of the doleritic nucleus, and which at the time of its intru- sion were also carried up. On the 8.W. side the same amorphous nucleus is also seen, and in connection with great masses of volcanic conglomerate which overlie it from the base up to the rugged crests. In this eruption the lava-stream also issued from the upper part of the cone. It issued from the side to the west of the Norman Tower, and flowed towards the 8. W., and can be traced as far as the Church della Immacolata. This lava, however, is less clearly made out than that of Paternd, being cut through and broken away in many places for the construction of the houses and roads of the upper part of the village ; it is nevertheless easily made out at the commence- ment, and its course can be traced, being very cellular on its upper surface, compact in the centre, and about 3 metres thick in some places. The fragmentary materials consist of scorie, clay, sand, and pebbles of sandstone (grés), altered by the igneous action of the volcanic rock, and which, being here and there in contact with the doleritic nucleus, constitute the foundations of the internal sides of the cone. The 24 PROCBEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, volcanic scorix near the Chiesa Madre and the Norman Tower, which © are close to the source of the lava-stream, are further proofs to en- able us to fix accurately the site of the crater, while the moveable materials which form its outer sides have been carried away by the action of waters. There can be no doubt that this doleritic rock offers a smaller number of phenomena than that of Paternd, in consequence of its smaller diameter and the ground being more changed ; but it is more interesting on account of the clear connection which the volcanic products show with the pre-existing sedimentary formation which has not been invaded by lavas from Etna. ‘The pleistocene clay and the post-pliocene conglomerate are closely connected together on the west and north-west sides, where no kind of alternation can be seen between these two rocks—either the volcanic or the sedimentary—as occurs in many other cases of extinct volcanos in the Val di Noto and in the Vallone della Pulicera, in which the stratification of the sedimentary deposit can be distinctly seen for a great distance; the clay and the conglomerate are perfectly horizontal. Conclusion.—F rom these observations we may conclude,—1st. That at Paterné and Motta (Sta. Anastasia) are the remains of two doleritic volcanic cones, because we there find the essential elements of volcanos, viz., a central nucleus, lava, and fragmentary materials. 2nd. That these voleanic phenomena were contemporaneous, and oc- curred during the post-pliocene period, previous to the deposit of the freshwater calcareous tuff of the neighbourhood of Paternd, because in the fragmentary materials of the two cones we find clay and pebbles of sandstone (grés)—pre-existing rocks, and no calcareous tuff. 3rd. These are cones of eruption and not of elevation, as some persons have lately endeavoured to prove, because the pre-existing sedimentary deposits of the neighbourhood do not show any modifi- cation in the direction of their strata. 4th. These eruptive cones are independent of Etna, because the doleritic nuclei have been brought up at once from below, and the lavas have issued from their terminal portions ; whereas in all the parasitical cones of Etna the streams follow the direction of the longitudinal fractures, which extend from the volcanic axis to the periphery ; and the lavas do not issue from. the upper portion of the parasitical cones, but from their bases, or at some greater distance. The bursting forth of lava from the throat or crater is a peculiarity of central eruptions, but not of those which are lateral or parasitic, 1861.) DAVIDSON—BRACHIOPODA, SALT-RANGE. 25 3. On some Carnonirerovs Bracuroropa collected in Inpta by A. Fremre, M.D., and W. Purvon, Esq., F.G.8. By T. Davinson, Esq., F.B.S., F.G.S. [Pxuates I. & II.] I. Brachiopoda of the Carboniferous Period, collected in the Punjab by A. Fleming, M.D., during the years 1848 and 1852. Dvunrine his geological survey of the Salt-range in the Punjab, Dr. A. Fleming had opportunities of collecting a considerable number of fossils, which he sent to England in 1849 and 1852, and of which a portion were at the time cursorily examined by M. De Verneuil, myself, and one or two other paleontologists. Some few of these fossils have been already recorded in a paper by Dr. Fleming, pub- lished in the 9th volume of the Quarterly Journal of the Geological Society (1853), also in the Journal of the Asiatic Society of Bengal for 1853, as well as in the same author’s excellent ‘ Report of the Geological Structure and Mineral Wealth of the Salt-range in the Punjab,’ printed at Lahore in 1854; and at the author’s request I have recently re-examined all the species of Brachiopoda of the Car- boniferous age which he had collected, with the view of completing in this respect the imperfect list published in 1853 *. It will not be necessary to dwell upon the geological features of the Carboniferous rocks of the district, as I could only repeat those details that have been made known in the report and papers above referred to. It will suffice for my present purpose to mention that the fossils occur in several beds differing mineralogically, some being erystalline and very hard, and others argillaceous: a few of the fossils occur in a magnesian limestone; but the same bed may be magnesian in one locality, and at a few miles distance be purely calcareous, Thus Dr. Fleming separates the Carboniferous rocks of the Salt- range into three divisions :— c. Upper Limestone. Brachiopoda and other fossils occur through- out the formation. b. Grey sandstone and shales, in which but few fossils have been found. : a. Lower Limestone, with calcarcous sandstone. This limestone generally abounds in large Brachiopoda and other fossils. It is also necessary to mention that the richest localities for Carboni- ferous fossils were Moosakhail, in the Salt-range proper, and Kafir Kote on the east bank of the Indus at about twenty-five miles below Kalabag, where the western prolongation of the Salt-range stretches down to the yery bank of the Indus; and Dr. Fleming informs me, moreover, that from these two localities the larger number of his fossils were procured, though of course they may also be found at intervening localities, such as Chederoo, Vurcha, Nulle, &e. Dr. Fleming assures me, likewise, that he is quite convinced that all the species about to be enumerated were derived from rocks of the Car- * The following are the species identified by M. De Verneuil and myself in 1853 :—Athyris Royssii, a Spirifera nearly related to S. lincata, Streptorhynchus Crenistria, Productus Cora, P, Flemingii, P. costatus, and P. Humboldtii, 26 PROCEEDINGS OF THE GEOLOGICAL society. = [ Noy. 20, boniferous period; and this I hasten to announce, because two of the species of Terebratula have puzzled me much, and raised some doubts in my mind as to their age; for they remind me more of what we should expect to find in the Jurassic or even Cretaceous, than in Carboniferous strata. Carboniferous Brachiopoda collected by Dr. Fleming in the Punjab. Terebratula (vel Waldheimia) Fle- | Rhynchonella Pleurodon, Phillips, sp. - mingii, Dav. Camarophoria Purdoni, Dav. —— biplicata, Brocchi (?). Var. | Streptorhynchus Crenistria, Phillips, problematica, Dav. sp. Himalayensis, Dav. Var. robustus, Hall, — subvesicularis, Dav. pectiniformis, Dav. Athyris Royssii, L’ Hveillé, sp. Orthis resupinata, Martin, sp, subtilita, Hall, sp. Var. grandis, | Productus striatus, Fischer, sp. Dav. longispinus, Sow. Retzia radialis, Phillips, sp. Var. | —— Cora, D’ Orbigny. Grandicosta, Dav. semireticulatus, Sow. Spirifera striata, Martin, sp. costatus, Sow. Moosakhailensis, Dav. —— Purdoni, Dav. lineata, Martin, sp. Var. Humboldtii, D’ Orbigny. Spiriferina octoplicata, Sow., sp. Strophalosia Morrisiana, King(?). Var, 1, TeREBRATULA (vel WatpHEIMIA) Freminett, Day. PI. I. figs, 1, 2. Shell variable in shape—ovate, longitudinally oval, or slightly pentagonal; valves almost equally deep and convex, but usually much depressed ; surface evenly smooth, without sinus or fold. Beak and foramen small and slightly separated from the hinge-line by a deltidium in two pieces; lateral ridges of the beak continued along the sides. Margin of the valves straight. Interior unknown. Of this species I have examined a number of specimens, which were all derived from a bed which first appears in the Nilawan ravine, and which Dr. Fleming considered to mark the commencement of the Carboniferous formation, which gradually increases in thickness as we proceed westwards towards the Indus. The shell could not, how- ever, be identified with any Terebratula of the Carboniferous age from any other part of the world, with which I am at present acquainted, while its affinities would on the contrary recall to our mind certain forms of the Jurassic period and more particularly those of the 7’. numsmalis group. The largest example measured 13 lines in length, 11 in width, and 8 in depth, and was proportionally much more convex than the other specimens. 2, TEREBRATULA BIPLICATA, Brocchi (?), var. PROBLEMATICA, Dav. Pi, 1, fi 3, Shell oblong, obscurely pentagonal; dorsal valve convex, rather deeper than the opposite one, and prominently biplicated; ventral valve flattened along the middle to a certain distance from the beak, where a median rounded rib with a sulcus on either side is produced and extends to the front. Beak’small, and truncated by a foramen of moderate size, Margins of the valves sinuous. Interior unknown. Length 20, width 8 lines, Of this species I am acquainted with but a single example, stated by Dr. Fleming to have been found by himself in the Carboniferous 1861.) _ DAVIDSON——BRACHIOPODA, SALT-RANGE. 27 Limestone of Moosakhail; and although the shell is silicified, like many of the other fossils from the Carboniferous Limestone in the Punjab, I cannot help repeating what I said with reference to the preceding species, viz. that it has much more the appearance of a Jurassic or Cretaceous form, e. g. of 7’. biplicata, Brocchi, than of any shell of the Carboniferous period with which I am acquainted. I would therefore call the attention of geologists and paleontolo- gists who may visit the district, to the two last-described shells, so as to ascertain whether they do really belong to the Carboniferous age as stated by Dr. Fleming, or whether they might not have been derived from some less ancient formation, 3. Teresratuta Himatayensis, Dav. PI. II. fig. 1. Shell ovate or ovato-pentagonal, longer than wide; valves almost equally and moderately convex, without sinus or fold; beak rather small, gently incurved, and truncated by a circular foramen, which slightly overlies the umbone of the opposite valve and thus conceals the deltidium to a greater or lesser extent. The surface of both valves is smooth up to within two or three lines of the margin, where a small number of rounded ribs are developed, of which four or five occupy the front, while two or three ornament each of the lateral portions of the valves; so that eleven of these short rounded ribs may be counted round the margin of each of the valves. The largest specimen I haye scen measured in length 11, width 9, depth 6 lines. This appears to be a common and characteristic species of the Carboniferous Limestone of the Punjab. All the specimens from Moosakhail are silicified. 4, TeREBRATULA sUBVEsICULARIS, Day. PI. I. fig. 4, Shell small, ovato-pentagonal, longer than wide; valves unequally convex, the ventral one being the deepest ; beak incurved, and trun- cated by a small oval-shaped foramen, which overlies the umbone of the opposite valve. Surface smooth to about half the length of the valves from the beak, while seven small ribs are developed near the margin: in the dorsal valve one or two of these occupy a slight mesial depression ; so that the frontal margin of the valve is usually triundate, from one or two of the central ribs being on a lower level than the lateral ones: in the ventral valve the ribs are somewhat similarly arranged. Dimensions generally small; an average-sized specimen measured 7 lines in length by 64 in breadth. This form does not appear rare in a darkish limestone in the neighbourhood of Moosakhail, and differs from 7. vesicularis and 1’. Himalayensis by the arrangement of its marginal ribs. 5, Atuyris Roysst1, L’Eveillé, sp. Pl. I. fig. 6, This characteristic and well-known species is very abundant at Moosakhail, and in several other localities in the Salt-range. It is identical in shape with our European specimens, and has been also ound in the black shales in the Chor Holi Pass by Capt. Strachey. 28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, 6. Aruyris suptiiira (Hall, sp.), var. granpis, Dav. PI. I. figs. 7, 8. Terebratula subtilita, Hall (?) in Howard Stansbury’s Exploration of the Valley of the Great Salt Lake of Utah, p. 409, pl. 2. figs. 1, 2; 1852. This appears to be a common species in the Punjab, having been found in several localities, but more abundantly at Moosakhail. It varies also considerably in shape and size; so that (as justly ob- served by Dr. Shumard while describing this shell from the Carbo- niferous strata of the Red River of Louisiana) we are very lable to multiply species from its varieties, unless a large number of speci- mens are under examination. Some of our Indian examples are exactly similar to those from Iowa, or from Pecos Village in New Mexico, whence the type of the species was obtained; while others are larger and more inflated or globose than any I ‘have hitherto seen from either Europe or America, although these last would agree very well with certain specimens described by Dr. Shumard from Washington county, Arkansas. ‘The largest Punjab specimen which has come under my observation measured in length 21, width 18, depth 17 lines. 7. Rerzra raprauis (Phillips, sp.), var. GRANpIcosrA, Dee by fig. 5. Shell longitudinally oval or ovate, with almost equally deep or convex valves; the beak is produced, and truncated by a small cir- cular foramen, which is slightly separated from the hinge-line by a small hinge-area; each valve is ornamented with about thirteen or more angular ribs, of which the central one is somewhat the largest, and corresponds to a groove of greater depth in the ventral valve. Our British specimens of 2. radialis are extremely variable in size and plication. In the typical form the ribs are smaller and more numerous than in the Punjab variety; while identical specimens of this last have been found in England, as well as in the Carboniferous rocks of Bolivia. Dr. Fleming states that he has found this shell rather abundantly near Moosakhail. 8. Sprrirera striata, Martin, sp. Pl. I. figs. 9, 10. Of this shell Dr. Fleming was able to procure but three or four fragmentary specimens, which could not be distinguished from simi- lar British examples of Martin’s species. It occurs at Nulle, Che- deroo, and several other localities. 9. SprrirerA Moosaxnartensis, Day. PI. II. fig. 2. Shell transversally subrhomboidal; valves almost equally deep or convex; hinge-line variable in length, sometimes not half as long as the breadth of the shell, while at times it is as long. Ventral area of moderate width; fissure wide and partially arched over by a pseudo-deltidium. Dorsal valve sublinear; beak small and mode- rately incurved. In the dorsal valve there exists a W ide, elevated angular fold, and in the ventral one a corresponding sinus. The whole surface of the shell is covered with numerous small ribs, which 1861.] DAVIDSON—BRACHTOPODA, SALT-RANGE, 29 cluster into fasciculi, seven or eight being collected into groups, which give to the valves the appearance of a double plication, many of the ‘smaller ribs being due to interpolation; while the whole surface and ribs are closely intersected by numerous sharp, projecting, concentric, undulating lamin, of which four or more may be counted in the breadth of a line. Dimensions very variable: a large example measured 26 lines in length by 39 in width and 18 or 19 in depth. Tt was not until after much hesitation that I have ventured to propose a new name for the Spzrifera under description. In external shape as well as by the grouping of its ribs, it bears much resemblance to several known species of Spirifera, and especially to that figured in Owen’s ‘ Geological Survey of Wisconsin and Minnesota’ (pl. 5. fig. 4) under the name of Spirifer fasciger, Keyserling?; but I partake of that author’s doubts while referring the shell in ques- tion to De Keyserling’s Russian species. It approaches also by its shape to certain examples of D’Orbigny’s Sp. Condor, Sp. cameratus, Hall, as well as to some exceptional British specimens of Spirifera striata; but in none of these do we perceive, nor does any author describe, the peculiar and beautifully regular, closely disposed, sharp, projecting, concentric, undulating lamin, which resemble so closely those of Sp. laminosa, and which give to the shell its beautiful sculp- tured appearance. Sp. Moosakhailensis is common in the Punjab, at Moosakhail, Chederoo, Kafir Kote, &e. 10. SprrrFera tineatA, Martin, sp., var. Pl. II. fig. 3. Martin’s shell varies considerably in shape, but has nowhere, to my knowledge, attained the large proportions of certain Punjab spe- cimens ; and indeed I was for some time uncertain whether these last did really belong to our well-known European species; but, after the attentive examination of some smaller Indian examples, I found these last to he undistinguishable from many specimens of Martin’s type. The peculiar arrangement of spinules, so well displayed in some Scottish examples of Sp. lineata, could also be observed here and there upon the Punjab silicified specimens. ‘The largest Indian example I have seen measured 3 inches 2 lines in length, by 3} in width and 1 inch 7 lines in depth. Another, identical with one from Derbyshire, measured in length 22, and in width 23 lines. It occurs at Chederoo and Moosakhail. This is the shell which in 1853 M. De Verneuil and myself considered to be nearly related to Sp. lineata, 11. Spretrerra ocrorricata, Sow., sp. Pl. I. figs. 12, 13. The Moosakhail specimens exactly resemble our British Carboni- ferous examples ; they show the same variations in shape and num- ber of ribs. 12, Rayncnonetta Prevropon, Phillips, sp. One or two examples, which appear to agree with our British type, have been found by Dr, Fleming at Moosakhail, 30 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Noy. 20, 18. CamaropHoriA Purpont, Dav. PI. II. fig. 4. Shell somewhat obscurely subrhomboidal or deltoid, wider than long. Valves almost equally convex, with a wide mesial fold of moderate elevation in the dorsal valve, and a corresponding sinus in the ventral one. The surface of each valve is ornamented with from eighteen to twenty-two angular ribs, of which from seven to eight occupy the fold, and from six to seven the sinus. The beak is small and much ineurved; so that the foramen, which is situated under the angular extremity of the beak, is but slightly seen. No marginal expansions could be perceived. This species does not appear to be rare in the Punjab; it occurs at Moosakhail, Vurcha, &c. 14, Srrerrornyncuvs Crenistria, Phillips, sp. Some very large examples, which entirely agree with our British specimens, have been found at Moosakhail, at Vurcha, and in other localities ; one in particular measured nearly 4 inches in length by about 5 in width and 13 in depth. The specimens are usually very irregular in their shape, from contortion and malformation, but agree in all their characters with Phillips’s type. 15, Streptoruyncuvs CrenisrriA (Phillips), var. ropustus, Hall. ela. tie, i, Orthis robusta, Hall, Report of the Geological Survey of the State of Iowa, p. 713, pl. 28. fig. 3; 1858. Shell somewhat marginally pentagonal and plano-convex ; hinge- line nearly as long as the width of the shell. Dorsal valve semi- circular and gibbous: ventral valve pentagonal and nearly flat; area triangular and wide, with a narrow pseudo-deltidium. Surface marked by small radiating striz with interspaces of almost equal width, while at variable distances from the beak finer interpolated striee occur between the larger ones. The valves are also crossed by numerous concentric lines or stria. A specimen from the Carboni- ferous Limestone of Vurcha measured 21 lines in length by 23 in breadth and 14 in depth. The Punjab examples of this variety of S. Crenistria so closely re- semble a specimen of Orthis robusta, Hall, from the Lower Coal- measures of St. Clair County, Illinois, in North America, that I am induced to consider them identical. 16. Srreproruyncuus prctintrormis, Day, Pl. I. fig. 17, Shell scallop-shaped; valves equally convex ; hinge-line sometimes less, rarely longer, than half the width of the shell, with projecting angular extremities. Ventral area triangular, usually higher than wide, and longitudinally divided by a narrow convex pseudo-delti- dium. The beak is pointed and tapering at its extremity, which is generally bent or twisted more to one than the other side. Dorsal valve pecten-shaped, very convex at the umbone, with small eared expansions, this valye being also slightly depressed along the middle. 1861. _ DAVIDSON BRACHIOPODA, SALT=-RANGE, 81 > The valves are ornamented with from twelve to fourteen angular ribs ; while the entire surface (area excepted) is covered with a great number of minute crenulated strie, which increase in number by the interpolation of smaller striz, especially close to the margin. The largest example I have seen measured 20 lines in length, by about the same in width and 14 in depth. This beautiful shell is not rare in the Carboniferous Limestone of Moosakhail, Chederoo, Nulle, and Kafir Kote; and appears to me to be quite distinct from any of its congeners. 17. Orruts resuprnata, Martin, sp. Pl. I. fig. 15. Of this well-known species one or two examples have been col- lected by Dr. Fleming in the Punjab. 18. Propvucrvs srriatvs, Fischer,sp. Pl. I. fig. 18. This European Carboniferous shell does not appear rare in a light- yellow limestone at Khond in the Punjab. 19, Propucrus Loneispinus, Sow. (=P. Freminer ejusd.), Pl. I. fig. 19. Two specimens exactly agreeing with Sowerby’s type have been found by Dr. Fleming, at Moosakhail in the Punjab, and at Srinug- gur in Kashmir; the specimen figured in my plate is the one iden- tified by M. De Verneuil and myself in 1853, 20. Propvctus Cora, D’Orbigny. Specimens identical with those of America and Europe have been found at Kafir Kote, Moosakhail, &e. 21. Propuctvs sEMIRETICULATUS, Sow. Of this species two or three specimens have been found in the Punjab by Dr. Fleming. 22. Propuctus costatus, Sow. PI. I. figs. 20, 21. This appears to be one of the most common species in the Carboni- ferous Limestones of the Punjab. It occurs at Moosakhail, Kafir Kote, &c., where it has sometimes attained large proportions, as may be seen from the specimen figured in my plate. The Indian ex- amples are exactly similar to those we find in Europe. 23. Propuctus Purpont, Dav. Pl. II. fig. 5. Shell longitudinally oval, broadest at two-thirds the length from the beak ; ventral valve moderately convex, flattened along the middle and longitudinally divided into two lobes by a deep sinus, which com- mences at the extremity of the beak and extends to the front. Beak and ears small; hinge-line very short, and generally not exceeding half the breadth of the shell. The dorsal valve is very much flat- tened until within a short distance from the margin, where it be- comes concave, and is divided by a mesial elevation, which commences close to the hinge-line and extends to the front, LExteriorly the 32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Noy. 20, surface of the ventral valve is entirely covered with minute, narrow, elongated tubercles, from which rise numerous small tubular spines, both the tubercles and spines becoming smaller and shorter as they approach the margin. ‘The dorsal valve is covered with small pits and tubercles, from which also rise slender spines, but apparently less abundantly than on the ventral one. A large specimen measures 2 inches 5 lines in length, by 2 inches 2 lines in breadth and 1 inch in depth. Of this interesting species I have seen several specimens from Chederoo and Moosakhail. 24, Propverus Humporprir, D’Orbigny. PI. II. fig. 6. Productus Humboldtii, D’Orb., Paléont. du Voyage dans l’ Amérique Méridionale, pl. 5. figs. 4,7; 1842. Shell marginally transverse, rotundate, quadrate; ventral valve moderately convex, with a wide shallow longitudinal sinus commen- cing at a short distance from the extremity of the beak and extend- ing to the front. Beak small and incurved ; hinge-line rather shorter than the greatest width of the shell. Dorsal valve almost flat for some distance, becoming slightly concaye close to the margin, and with a small mesial fold or elevation perceptible only close to the front, The surface of the ventral valve is covered with numerous small elongated tubercles arranged somewhat in quincunx, and from which rise short tubular spines, The largest of Dr. Fleming’s specimens measured 133 lines in length by 16 in width and 63 in depth. Dr. Fleming found his specimens at Kafir Kote on the west bank of the Indus. D’Or- bigny’s examples were obtained from Yarbichambi, on the Bolivian table-land of the Andes. I must, however, observe that several of the Indian examples bear so close a resemblance to some of our British specimens of P, scabriculus, that they could be with difficulty distinguished. 25, Srropwarosra Morrisrana, King (?), var. Pl. II. fig. 8. Among the fossils stated to have been procured at Moosakhail, I found two specimens of a shell which so closely resembled certain ex- amples of the Permian Strophalosia Morrisiana, that neither Messrs, Kirkby, Howse, nor myself were able to distinguish it. In shape it is nearly circular, with the same convexity of the ventral, and con- cavity of the dorsal valve, the same relative proportions of the dorsal and ventral areas, and, lastly, the presence of the same elongated adpressed spines which adorn the surface of the ventral valve in the Permian specimens; while the only difference consists in the appa- rent absence of those minute radiating raised strive observable in the perfect shell of King’s species: but it must also be remembered that this point of difference is only a negative one, and of slight value ; for some specimens of the species from Tunstall Hill do not show the character. The material at my command is not, however, suf- ficient. to enable me to positively affirm the identity; so that the 1861.] ==—s DAVIDSON——-BRACHTOPODA, SALT-RANGE. 33 safest plan will be for the present to consider the Punjab shell as a variety of S. Morrisiana*. Il. Brachiopoda of the Carboniferous Period, collected in India by W. Purdon, Esq., F.GS. At Mr. Purdon’s request I have examined the Brachiopoda collected by himself during his survey of the Punjab and N.E. Himalayan districts of India. Mr. Purdon’s collection contained many interesting and fine exam- ples of the following species t:— 1. Terebratula Himalayensis, Dav.; 2. Athyris Royssii, L’Eveillé ; 3. Athyris subtilita, Hall (?), var. ; 4. Spirifera Moosakhailensis, Dav.; 5. Sp. lineata, Martin, var.; 6. Rhynchonella Pleurodon, Phillips, var. ; 7. Camarophoria Purdoni, Day.; 8. Streptorhynchus Cremstria, Phillips; 9. Strept. pectiniformis, Day.; 10. Productus striatus, Fischer; 11. P. Cora, D’Orb.; 12. P. Purdoni, Dav. ; 13. P. costatus, Sow.; 14. P. Humboldtii, D’Orb.; 15. P. semireticulatus, Sow.; 16. Strophalosia Morrisiana, King (?), var.; 17. Aulosteges Dalhousie, Day. ; 18. Crania (sp. undeterminable). Having already described the sixteen first-named species in my preceding communication, all that remains for me to do, in order to complete the notice of what has been up to the present time dis- covered, is to describe the Aulosteges Dalhousti from the very inter- esting specimen found by Mr. Purdon in the Carboniferous (?) rocks of the Punjab. Avxosteces Datnousn, Day. Pi. II. fig. 7. Subtrigonal marginally, wider than long ; anterior angles rounded ; moderately indented in front ; hinge-line slightly exceeding half the width of the shell. Ventral valve convex, divided by a wide and deep mesial sulcus or sinus ; beak nearly straight, but inclining more to the one than the other side; area flat, irregularly triangular, forming an obtuse angle with the plane of the dorsal valve, and di- vided along the middle by a narrow convex pseudo-deltidium, the entire surface (area excepted) being closely covered with slender * Tn 1857 Messrs. Howse, Kirkby, and myself entertained the opinion that the British Permian S. Morrisiana should be considered identical with the S. lamellosa of Geinitz, or as nothing more than a variety of it; but although we are not yet prepared to abandon that view, it must be mentioned that Dr. Geinitz has ex- pressed a contrary opinion in his recently published work, ‘ Dyas oder Zechst.,’ etc., wherein he asserts that S. /amellosa and S. Morrisiana are entirely distinct species. It must not, however, be forgotten that S. /ame/losa appears to have been a very variable species, and to have suffered great modifications of general form, mode of growth, and of spine-arrangement, such as changes in physical condition would necessarily induce, and which should never be overlooked in taking philosophical views of species. ¢ It was not my intention to have alluded to the species collected in the Punjab by Mr. Purdon until the publication of that gentleman’s memoir upon the geo- logy of the district ; but, as I had also promised Dr. Fleming to describe those he found in the same localities, I thought it desirable to delay no longer the mention of those collected by Mr. Purdon, and to give him full credit for his discoveries. ; VOL. XVIII.——PART I. D 34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20, tubular spines, which appear to have exceeded in certain places 4 or 5 lines in length. The spines lie rather close to the surface of the valves, with their extremities directed towards the margins of the shell. The dorsal valve is convexo- concave, that is to say, gently convex until within a short distance of the margin, where the valve becomes concave or bent. The dorsal area is narrow and linear; and the entire surface of the valve appears to have been covered with slender spines. In the interior of the dorsal valve the cardinal process is trilobed ; and on either side may be seen some slight indications of dental sockets: a small longitudinal ridge, which first appears under the cardinal process, extends to rather more than half the length of the valve ; and on either side are situated two elongated-oval-shaped dendritic muscular scars, which are no doubt referable to the adductor or occlusor muscle. From the inner extremities of these depart the so-called reniform impressions, which extend by an outward oblique curve to near the margin, and, turning abruptly backwards and in- wards, terminate at some short distance from their first point of de- parture. The interior of the ventral valve could not be observed. An attentive examination of this interesting species has led me to consider that its affinities lie more with Helmersen’s subgenus Aulosteges than with King’s Strophalosia. Specifically speaking, it bears some resemblance to A. Wangenheimi (=A. variabilis, Helmer- sen); but it may, I think, be distinguished by its shape, larger dimensions, and internal details. The species composing the subgenera Aulosteges and Strophalosia, though represented in the Carboniferous period, appear in Europe to be more specially characteristic of the Permian epoch ; and it may therefore remain a question whether in the Punjab there does not exist, above all well-authenticated Carboniferous strata, some small bed representing the Permian age, and from which A. Dalhousw — and the variety of Stroph. Morrisiana we have described might have dropped and become mixed with shells of the Carboniferous period. We may also here remind the reader that another species of Stropha- losia (S. Gerardi, King) was some years ago discovered by Dr. Gerard in the Himalayan range at 17,000 feet above the sea. Of Aulosteges Dalhousi a single example has been hitherto pro- cured from the Carboniferous Limestone (?) of Moosakhail. In conclusion, we may observe that the total number of Car- boniferous Brachiopoda hitherto discovered by Dr. Fleming and Mr. Purdon in the Salt-range of the Punjab amounts to about twenty-eight species, of which thirteen at least are common to European rocks of the same period, although several of these have in India attained larger proportions. It is also very probable that further research among the Carboniferous deposits of the Punjab would bring to light several more species in addition to those here enumerated. 4 a eet “a R 3 ; 2 n.Geol. Soo. Vol XVII. Pl. if Quart..Jo of Whe FROM INDIA. De 2 BRACHIOF FOSSIL Tho! Davidson ddl. & a ‘RM, Quart Journ Geol. Sec. Vol. XVII PIT. Lrinted by TS. Rartre. 1861.] HISLOP—PLANT-BEDS OF INDIA. 35 EXPLANATION OF PLATES I. & II. Prats I. Specimens in Dr. Fleming’s collection, and in the Geological Society’s Museum. Fig. 1, 2. Terebratula (vel Waldheimia) Flemingii, Dav. 3. T. biplicata, Brocchi (?), var. problematica, Dav. 4. T. subvesicularis, Day. 5. Retzia radialis, Phil., var. Grandicosta, Dav. 6. Athyris Royssii, L’ Eyeillé. 7, 8. A. subtilita, Hall, var. grandis, Dav. 9, 10. Spirifera striata, Martin. 11-14. Spiriferina octoplicata, Sow. 15. Orthis resupinata, Martin. 16. Streptorhynchus Crenistria, Phil., var. robustus, Hall. 17. 8. pectiniformis, Dav. 18. Productus striatus, Fischer. 19. P. longispinus, Sow. 20, 21. P. costatus, Sow. Prats II. Specimens collected by W. Purdon, Esq., and now forming part of Fig. Mr. Davidson’s collection. 1. Terebratula Himalayensis, Dav. . Spirifera Moosakhailensis, Dav.: 2c, a young example, . 8. lineata, Martin, var. :3c, Crania (?). Camarophoria Purdont, Dav. Productus Purdoni, Dav, P. Humboldtii, D’ Orb. . Aulosteges Dalhousii, Dav. Strophalosia Morrisiana, King (?), var. WWD En A C9 36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 20. Supplemental Note on the Piant-Beartne SanpsTones of CENTRAL Inpv1a*. By the Rev. Srepnen Histor. (In a Letter to the Assistant-Secretary, dated Nagpur, July 19, 1861). [Read at the Evening-meeting, January 8, 1862; and, by Permission of the Council, printed in the February Number of the Journal. | ‘‘Recentiy I have obtained more Insect-remains ¢ from Kota, with a morsel of Sphenopteris in the limestone; also an Ichthyolite, probably Aichmodus Egertont. “‘ T think there are strong reasons for believing that the ichthyo- litic beds of Kotd are superior to our plant-sandstone and coal; and hence, if the former be Lower Jurassic, the latter must be older. “‘ In the sandstone at Sironcha, six miles further down the River Pranhita, there is an abundance of compressed stems identical with those at Silewada; so that there can be no doubt that the argil- laceous sandstone there is of the ‘ Damida group.’ This sandstone of Sironcha is stated by Mr. Wall to underlie almost immediately the Kota limestone.” After remarking that the genus Tcniopteris occurs both in the Rajmahal Beds of Bengal and in the “‘ Damuda Beds” of Nagpur, Mr. Hislop proceeds to state that the largest Taniopteris from Kampti (near Nagpur) is exceedingly like 7. lata and 7. multinervis of the Rajmahal Beds. The Teniopterides, thus closely approaching in form, prove, in his opinion, that the Damtda and the Rajmahal Beds cannot be widely separated. * See Quart. Journ. Geol. Soc. vol. xvii. p. 346 et seg. + The associated Estheria (loc. cit. p. 356) has been carefully examined, and appears to be different from that found at Mangali: both are new species; the latter, however, is very similar to an EHstheria found living in Palestine.—T. R. J. + An opinion coincident with Dr. Oldham’s: see Mem. Geol. Surv. India, i. p. 202.—T. R. J. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. POSTPONED PAPER. On the Lines of Drrrrst WarTER around the Britisu Isizs. By the Rey. R. Eversst, F.G.S. (Read June 19, 1861*,) [ Abridged. ] From two papers by Mr. Godwin-Austent we learn that the English Channel was, in all probability, a valley of depression. If, by the light thus afforded us, we examine the locality as laid down in a good chart, we shall see that as there is a valley of depression, so is there also an axis of depression, if the term may be used. We have in common use the term “axis of elevation ” to signify the line of greatest elevation in a mountain-range; and in a similar way we would employ the phrase “ axis of depression ” to mean the line of deepest water in a narrow sea. If we take a point (see Map) nearly south of Dungeness in Kent, orin north lat. about 50° 30’, and east long. rather less than 1°, and from this draw a straight line a little to the south of west, passing through the middle of the deep water, and meeting about north lat. 48° 20’, and west long. 8°20’, and another line of a similar kind pass- ing through the deepest water of the St. George’s Channel between Ireland and England, we find, tracing the course of our line, that it first passes between the two pits, called “‘ North Deep” and “ South Deep,” in the same longitudinal or axial direction as both of them ; it cuts the “‘ West Deep” in its deepest part, and nearly in the same longitudinal direction ; it passes through the “ Hurds Dyke” from end to end, and meets successively the projecting easternmost points of the lines of 40 to 50, 50 to 60, and 60 to 70 fathoms. Beyond this last, the lines of equal depth are but triflingly affected by the entrance to the Channel. See the Admiralty Charts. We would now wish to draw attention to the above-mentioned longitudinal pits, remarkable as they are for their great length, and for lying, all of them, nearly in the same direction. It has, I think, been suggested that a large river once passed * For the other papers read at the Evening-meeting, see Quart. Journ. Geol. Soe. vol. xvii. p. 533, + Quart. Journ. Geol. Soc. 1850-51 ; vol. vi. p. 69; vol. viii. p. 118, 38 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. through the bed of the Channel, when it was above the level of the sea; but the action of running water cannot be considered sufficient to have hollowed out troughs of this kind, with no exit or open passage at either end. We shouldrather wonder that they have not yet been filled up by the deposits that must have been poured into them. Here we have a long narrow cavity (“‘ Hurds Dyke ”’) sur- rounded by water of the depth of about 30 fathoms up to its sides, and having in its centre a depth of 72 fathoms, or about 240 feet more than its edges. It therefore seems probable, from what we know on the subject, that the remark of Sir Henry De la Beche respecting a similar pit (the “Silver Pit” off the coast of Lincoln- shire) would apply to these, viz. that they were the remains of ancient cracks or fissures in the earth. The chemical theory of volcanos, the subterranean solution of felspathic, calcareous, and other rocks by water, and the crumpling of strata* appear to account for the origin of cavities beneath the crust of the earth, and its consequent fissuring. From the point first taken, nearly to the south of Dungeness, the line of deepest water takes a north-easterly course to a little above lat. 52° N.; a winding course, like that of the English Channel, if observed only for a short distance, but in long distances deviating not much from a straight one. From the point last mentioned, in lat. 52° N., the line appears to turn in a direction somewhat to the west of the north; but beyond this it rapidly becomes shallower, indeed below 30 fathoms. It may be traced, however, with a depth of between 20 and 30 fathoms to a little north of lat. 53° N., and there ceases as a continuous line, though there are detached pits, such as the “ Silver Pit ”’ above alluded to, with a depth of from 40 to 50 fathoms. But, generally speaking, a bank here runs across the Channel all the way from England to Holland, so that a rise of 20 fathoms (120 feet) in the bed of the sea would enable us to walk across to Holland dryshod, all the way from the Wash to the Elbe. As the line of deepest water has now terminated in this locality, we must turn to another, and endeavour to recover it. ‘To the north- east of the Shetland Isles we meet with the 100-fathom line, which passes round the western coasts of Scotland and Ireland. North of the Shetlands it takes a bend to the east, and runs in a direction nearly west to east ; then sweeps round to the north, until it termi- nates its course in that direction almost in a point, and then runs away in a south-east direction, following the line of the coast of Norway. But during the short distance that it has run from west to east, it gives off a deep channel to the south; so that in an easterly direction from the north point of the Shetlands there is, after passing over the shoal water near the land, a channel of from 80 to 100 fathoms in depth, then a bank of from 60 to 70 fathoms, and beyond that the deep channel which runs conformably to the coast of Norway, to the depth of 200 fathoms or more. There is a deficiency of deep- sea soundings from about lat. 60°30’ to 59° 30’ ; but the channel we have mentioned, divided from the deep water on the coast of Norway, * See De la Beche, Mem. Geol. Surv. vol. i. p. 237. “EVEREST—POLYGONAL AREAS. 39 may be traced all the way, nearly ina southerly direction, at a depth of 70 to 80 fathoms, having on its eastern side the bank of 60 to 70 fathoms, which separates it from the Norway Sea. At about lat. 58° 40’, where the soundings are more regularly given on the charts, we find again the deep channel of from 80 to 100 fathoms, running in a direction nearly south, with a slight inclination to the east, having on either side a depth of 70 to 80 fathoms, and outside of that again a depth of 60 to 70 fathoms. Here we observe that it must have divided into two, after passing the northern point of the Shetlands, though the soundings are too imperfect to enable us to say where the division took place. We find, however, two channels of 70 to 80 fathoms in depth, with a bank between them. The easternmost or principal channel is continued to below lat. 58° at the depth of above 80 fathoms, and a little farther at the depth of above 70 fathoms. It continues at a depth of 50 to 60 fathoms to below 56° 30’, and there merges into a broad expanse of 40 fathoms depth. The westernmost or side channel appears to conform more to the line of the coast than the other. It gives off a branch into the Moray Firth, and another into the Firth of Forth. Lower down it runs conformably to the line of coast, and ends in about 54° 10! lat. in a rounded point at the depth of 30 fathoms,—unless indeed we suppose the detached pits, the “Silver Pit,’”’ the “Sole Pit,” the “Cole Pit,’ and the “ Outer Silver Pit,” to be continuations of it, which is probable. The first appears to branch aside in the direction of the “ Wash;”’ the second and third to continue in the direction of the channel which, as we saw, ends in lat. 54° 10’; and the last runs in a direction west to east, whence it may be traced in the chart all the way to the mouth of the Elbe. Now, take a central point, at the end of the principal or eastern channel, which we saw was in about lat. 56° 26’, and draw a straight line from that to the point which we have before taken in lat. 52° ; then produce the straight line so formed untilit meets the line drawn from the projecting angle of the 100-fathom line, west of the He- brides, towards the projecting angle of the same line which lies to the north-east of the Shetlands; from the first point draw a straight line to the next projecting point of the 100-fathom line ina 8.W. direction, which lies between lat. 53° and 54° N., off the west coast of Ireland; from this last point draw a straight line to the point we have before taken at the entrance of the British Channel, in lat. 48° 20’ N. and long. 8° 30’ W.: we have now completed an unequal-sided hexagonal figure, which may be said very nearly to represent the lines of deepest water round the British Isles. It is obvious, on referring to the Map, that, starting from the last-named point, in lat. 48° 20’ N., a similar process may be repeated for Ireland ; and we then get a pentagonal figure, the third side of which, running between the coasts of Ireland and Scotland, passes along a remarkable pit, 30 to 40 miles long, 3 to 4 miles broad, and 100 to 150 fathoms deep, or as much as 70 to 80 fathoms (420 to 480 feet) deeper than the water at its edges. See the Admiralty Charts. It may be objected, that in these two figures we have taken, on 40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. the western or oceanic faces, the 100-fathom line of equal depth, which is a different thing from a line or lines of greatest depth. To which we can only answer, that the 100-fathom line is the greatest depth for which the necessary soundings have been given to enable us to construct a continuous line for the whole distance. There are indications of a line of greatest depth outside of this, and which may be distinctly traced in the channel between the Ferroe Islands and the Orkneys, and between Rockall and the Hebrides; but, as the necessary soundings are not given for the southern part of its course, we do not insist on it. This form of an irregular polygon, usually the pentagonal or the hexagonal, is the form that bodies approximate to, more or less, in shrinking, either when cooling down from a great heat or when drying. Of the former process basaltic columns afford familiar ex- amples; and the same kind of thing may be seen in large surfaces of river-mud drying under the influence of a hot sun; and from what we know otherwise, the probable inference is that the con- traction or shrinking in question (from whence these large polygonal areas appear to have had their origin) has arisen from cooling, and the falling in of cavities occasioned by upheaval. The difference between the deep isolated pits and simple lines of depression appears to be this, that in the one case the strata are more unyielding than in the other. The area of the English Channel has been shown to be a valley of depression, from the terrestrial remains fished up in it, and the sunken forests on its edges. The same thing is known of that part of the German Ocean which is south of lat. 53°. There can then be no improbability in assigning a similar origin to the northern part of it. We have, therefore, two antagonistic forces in operation—the one an elevating and expanding force, the other depressing and contracting, both acting, if not in lines exactly straight, at least nearly so. If the bed of the English Channel, east of the Start Point, were upheaved 30 fathoms or 180 feet perpendicular, it would present the ap- pearance of a chain of lakes, similar to what is seen in the inland valley (the Great Glen) through which runs the Caledonian Canal. Does it not then appear probable that the latter valley has also had a similar origin, lying as it does between two lofty mountain-chains ? The furrow has run parallel to the ridges on either side of it, That it has been upheaved above the level of the sea by an after-process may be inferred from this, that the narrow trough at the western end of it (the Linnhe Loch), and the Moray Firth at its eastern entrance, have both the same maximum depth of water, viz. 100 to 120 fathoms. The line of 100 fathoms on the western face of the islands is the greatest depth at which numerous soundings are given, and thus yields better data for a continuous line. We will commence at its north-eastern end, to the north-east of the Shetland Isles, where it forms a remarkable projection into the deep water beyond. (1) From this point, it keeps a westerly direction until north of the Shetlands, and then bends somewhat to the south EVEREST—POLYGONAL AREAS. 41 in a line nearly straight, until off the Hebrides, (2) when it again makes a bend tothe south. It continues in this direction until about lat. 53° 20’, (3) when it again bends to the south, and continues nearly as a north and south line to a little above 49° 20’, (4) when it takes a sudden bend to the south-east, and runs in that direction all the way across the Bay of Biscay to the western foot of the Pyrenees. It will be observed that between these projecting points (see Map) the line bends inwards, like a slackened rope between Map of the British Isles, showing the 100-fathom line and the Hexagonal Area. FIRTA OF FORTH its points of support, and the cracks or rents we have been discuss- ing begin between the points of support at the deepest point of the curve. It will be observed also, that this 100-fathom line par- takes but little of the irregular shape of the coast; but that the shallower the water becomes, the more does the line of equal depth 42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. conform to the outline of the dry land opposite to it. May we not then explain these appearances by saying, that as the mass was upheaved from the bed of the ocean, the sides opened, in a degree, with the strain and shrank inwards or towards the land, so as. to produce (in the case of the channel to the north-east of the Shetlands, the northern entrance of the Irish Channel, and the entrance of the English Channel) a great crack or rent, which opened more and more as the mass rose into shallower water? This appearance in the last case, at the entrance of the English Channel, can be best studied in Maury’s small Chart of the North Atlantic. The relations of the strong projections or angles, and the weaker sides, of the half-hexagonal figure thus described are then treated of by the author ;—the analogous irregularly hexagonal outline of the Isle of Arran and of the Spanish Peninsula, and its 100-fathom line,—the absence of such a line of angles on the eastern side of England, where the strata are softer,—and the bearings that certain lines drawn across the British Isles from the projecting angles of the polygon appear to have on the strike, and other conditions of the strata—were described. After some remarks on the probable effect that shrinkage of the earth’s crust must have on the ejection of molten rock, the author observed that, in his opinion, the action of shrinking is the only one we know of that will afford any solution of the phenomena treated of in this paper, namely, long lines of depression accompanied by long lines of elevation, often, as in the case of the British Isles, Spain and Portugal, and elsewhere, belong- ing to parts of huge polygons broken up into small ones, as if the surface of the earth had once formed part of a basaltic causeway. 43 DONATIONS TO THE LIBRARY OF THE GEOLOGICAL SOCIETY. From July 1st to October 31st, 1861. I. TRANSACTIONS AND JOURNALS. Presented by the respective Societies and Editors. American Journal of Science and Arts. Second Series. Vol. xxxii. No, 94. July 1861. H. How.—Natro-boro-calcite and another Borate occurring in the Gypsum of Nova Scotia, 9. —. Gpyrolite occurring with Calcite in Apophyllite in the Trap of the Bay of Fundy, 13. L. Lesquereux.—The Coal-formations of the United States, 15. in a Guernsey County (Ohio) Meteor of May lst, , 30. E. B. ae note ol; its Geological Relations and Distribu- tion, 85. E. J. Brush.—Crystalline form of Hydrate of Magnesia from Texas in Pennsylvania, 94. The Tunnel of Mont Cenis, 101. G. Rose.—Deportment of Carbonate of Lime at a high temperature, 112. Geological Survey of Kentucky, 118. J. H. ReChicanay New Fossils from the Paleozoic Rocks of the Western States, 123. W. Haidinger.—Meteors, 135, Earthquake at Mendoza, 148, Assurance Magazine and Journal of the Institute of Actuaries. Vol. ix. Part 6. No. 46. July 1861. Atheneum Journal. Nos. 1758-1774. July—October 1861. Notices of Meetings of Scientific Societies, &c. E, Hull’s ‘The Coal-fields of Great Britain,’ noticed, 22. 44 DONATIONS. Atheneum Journal. Nos. 1758-1774 (continued). R. Chamber’s ‘Tce and Water,’ noticed, 58. T. Bell’s ‘ Mineral Veins,’ noticed, 191. Meeting of the British Association, 318, 348, 378, 411. ia and Geikie’s ‘Geological Map of Scotland,’ noticed, 322, ‘Our Black Diamonds,’ &¢., noticed, 401. Bengal Asiatic Society. New Series. No. 107. 1861, No. 2. T. G. Montgomerie.—Progress of the Kashmir Survey, 99. Berlin, Abhandlungen der kénig]. Akad. d. Wissensch. zu. Aus dem Jahre 1860. 1861. Beyrich.—Ueber Semnopithecus pentelicus, 1 (plate). Hensel.—Ueber Aipparion mediterraneum, 47 (4 plates). Questiones quas Academize Regie Scientiarum Borussicz Classis physica et mathematica certamini litterario in annum MDCCOLXIV. proponit, d&e. Zeitschrift der Deutschen geologischen Gesellschaft. Vol. xii. Parts 3and 4. 1860. Protokoll, 361, 517. Briefliche Mittheilungen, 373. H. v. Strombeck.—Ueber die Trias-Schichten mit Myophoria pes- anserts, Schlot., auf der Schafweide zu Lineberg, 381. Th. Kjerulf.—Ueber das Friktions-Phanomen, 389. M. Sars.—Ueber die in der norwegischen post-pliocainen oder gla- cialen Formation vorkommenden Mollusken, 409. A. Delesse.—Ueber das Vorkommen des Stickstoffes und der organi- schen Stoffe in der Erdrinde, 429. Fr. Pfaffi—Beitrage zur Theorie der Erdbeben, 451 (plate). ) H. B. Geinitz.—Zur Fauna des Rothliegenden und Zechsteins, 467. O. Speyer.—Ueber Tertiar-Conchylien von Sollingen bei Jerxheim im Herzogthum Braunschweig, 471 (plate). E. Weiss.—Ueber ein Megaphytum der Steinkohlen-Formation von Saarbriicken, 509. H. Wolf und Ferd. Roemer.—Nachricht von dem Vorkommen der Posidonomya Becheri in den Sudeten und in Mahren, 513. F. von Richthofen.—Bemerkungen tiber Ceylon, 523. . Ueber den Gebirgsbau an der Nordkuste von Formosa, 532. — Unger.—Der Schwefelkies-Bergbau auf der Insel Wollin, 546 late). Ge eataeeeee —Versuch, das geologische Alter einer Therme, der- jenigen von “ Wiesbaden,” zu bestimmen, 567. R. Andree.—Zur Kenntniss der Jurageschiebe von Stettin und Konigsberg, 578 (2 plates). Boston and Cambridge, U.S. American Academy of Arts and Sciences. Memoirs. Vol. i. Boston, 1785. Williams.—EKarthquakes of New England, 260. D. Jones.—West-River Mountain, and the appearance of there having been a volcano in it, 312. C, Alexander.—Account of Hruptions and present Appearance in West-River Mountain, 316. DONATIONS. 45 Boston and Cambridge, U.S. American Academy of Arts and Sciences. Memoirs. Vol.i. Boston, 1785 (continued). B. Lincoln.—Several Strata of Earth and Shells on the Banks of York River, Virginia ; Springs in Pennsylvania, &c., 372. J. Belknap.—Fossi substance containing vitriol and sulphur, 377. Vol. ii. Part 1. Boston, 1793. S. Tenny.—Medicinal Springs at Saratoga, a Y,, 43. S. Hitcheock.—Frogs found in the Earth, 6 Parsons.—Discoveries made in the Westen Country, 119, S. West.—A Letter concerning Gay Head, 147. W. Baylies.—Description of Gay Head, 150. R. Annan.—Account of a Skeleton of a large Animal found in Hudson’s River, 160. T. Edwards.—Description of a horn or bone lately found in the River Chemung or Tyoga, 164, ——. Vol... Part 2. Charlestown, 1804. B. de Witt.—Mineral productions of the State of New York, 73. O. Fisk.—Account of the Resuscitation of a Mouse, found in a torpid state enclosed in a fossil substance, 124. —. ——. —. NewSeries. Vol. i. Cambridge, 1833. C. T. Jackson and F. Alger.—Mineralogy and Geology of Nova Scotia, 217. ._ —. —. —. Vol. vi. Part 2. Cambridge and Boston, 1859. ——. ——. Proceedings. Vol. iv. From May 1857 to May 1860. 1860. 6 Se eae y of Japan compared with that of Asia, Europe, and America, 131, 171, 195, 411, 424. C. T. Jackson. —Analy sis of Bornite from Georgia, 196. P. Cleayeland, R. Brown, and A. Humboldt, Obituary Notices of, 226. C, T. Jackson.—Frozen Well in Brandon, Vermont, 269. S. 8. Lyon and 8. A. Casseday.—Synonymic list of the Paleozoic Echinodermata of North America, 282. — Shaw.—Granite as a Building Material, 353. —. —. —. Vol. v. Sheets 1-30. May 1860-April 1861. S. A. Casseda ‘aes 8. 8. Lyon.—Fossil Crinoidea from Indiana and Kentucky, F. H. Storer a C. W. Eliot.—Chromate of Chromium and Black Oxide of Manganese, 192. Breslau. Abhandlungen der Schlesischen Gesellschaft fiir vater- lindische Cultur. Philosophisch-historische Abtheilung. 1861. Heft I. 46 DONATIONS. Breslau. Abhandlungen der Schlesischen Gesellschaft fiir vater- lindische Cultur. Abtheilung fir Naturwissenschaften und Medicin. 1861. Hefte I. und II. H. R. Goeppert.—Ueber das Vorkommen von Lias-Pflanzen im Kaukasus und der Alborus-Kette, 189. ——. Ueber die Tertiarflora der Polargegenden, 195. . Acht und dreissigster Jahres-Bericht der Schlesischen Gesellschaft fiir vaterlindische Kultur. Arbeiten und Veriin- derungen der Ges. im J. 1860. 1861. — von Carnall.—Ueber die Lagerung der Steinkohlenflétze in Ober- schlesien, 28. C. Beinert.—Ueber die Geschiebe in den Conglomeratbanken der Grauwacke-Formation bei Schweidnitz, Seifersdorfund Gablau, 30. H. R. Goeppert.—Verzeichniss der Meteoriten der Mineralien- Sammlung der Schlesischen Gesellschaft, 32. Ueber Liasflora Russlands, 33. ——. Ueber die Kohlen Central-Russlands, 34. ——. Ueber die polare Tertiar-Flora, 34. British Association for the Advancement of Science, Report of the Thirtieth Meeting of the, held at Oxford, 1860. 1861. J. Anderson.—Excavations in Dura Den, 32. R. P. Greg.—Catalogues of Meteorites and Fireballs from a.p. 2 to A.D. 1860, 48. W. Vernon Harcourt.—Effect of long-continued Heat, illustrative of Geological Phenomena, 175. J. A. Brown.—Magnetic Rocks in South India, 24. 7 W.R. Birt.—Forms of certain Lunar Craters indicative of the - Operation of a peculiar degrading Force, 34. H. Hennessy.—Possibility of Studying the Harth’s Internal Structure from Phenomena observed on its Surface, 35. HI. Moseley.—The Cause of the Descent of Glaciers, 48. F. Anca.—Two newly discovered Ossiferous Caves in Sicily, 73. P. B. Brodie.—Stratigraphical Position of certain Species of Corals in the Lias, 73. J. A. Broun.—Velocity of Harthquake-shocks in the Laterite of India, 74. J.C. Clutterbuck.—The Course of the Thames from Lechlade to Windsor, as ruled by the Geological Formations over which it passes, 75. Daubeny.—The Elevation-theory of Volcanos, 75. J. B. P. Dennis.—On the Mode of Flight of the Pterodactyles of the Coprolite-bed near Cambridge, 76. J. Dingle.—Corrugation of Strata in the Vicinity of Mountain- ranges, 77. P. de M. G. Egerton.—The Ichthyolites of Farnell Road, 77. A New Form of Ichthyolite discovered by Mr. Peach, 78. A. Favre.—Circular Chains in the Savoy Alps, 78. A. Gages.—Some Transformations of Iron-pyrites in connexion with Organic Remains, 79. H. B. Geinitz.—The Silurian Formation in the district of Wilsdruff, 79. T. RH. owney.—Analysis of some Connemara Minerals, 71. ——. Composition of Jet, 72. DONATIONS. 47 British Association for the Advancement of Science, Report of the Thirtieth Meeting of the, held at Oxford, 1860 (continued). R. Harkness.—The Metamorphic Rocks of the North of Ireland, 79. Hector.—The Geology of Captain Palliser’s Expedition in British North America, 80 E. Hull.—The Blenheim Iron-ore ; and the Thickness of the Forma- tions below the Great Oolite at Stonesfield, Oxfordshire, 81. T. S. Hunt.—Some Points in Chemical Geology, 83. J. B. Jukes.—Igneous Rocks interstratified with the Carboniferous Limestones of the Basin of Limerick, 84. J. A. Knipe.—The Tynedale Coal-field and the Whin-sill of Cum- berland and Northumberland, 8&6. W. L. Lindsay.—The Eruption in May 1860 of the Kotliigja Volcano in Iceland, &6. W. Lister.—Some Reptilian Foot-prints from the New Red Sand- stone north of Wolverhampton, 87. C. Moore.—The Contents of Three Cubic Yards of Triassic Drift, 87. W. Molyneux.—Fossil Fish from the North Staffordshire Coal-fields, 88 J. Powrie.-—A Fossiliferous Deposit near Farnell, in Forfarshire, N.B., 89. J. Prestwich.—Some new facts in relation to the Section of the Cliffs at Mundesley, Norfolk, 90. W. Pengeliy.—The Chronological and Geographical Distribution of the Devonian Fossils of Devon and Cornwall, 91. G. N. Smith.—Three undescribed Bone-caves near Tenby, Pembroke- shire, 101. W. 8. Symonds.—The selection of a peculiar geological habitat by some of the rarer British Plants, 102. H. B. Tristram.—The Geological System of the Central Sahara of Algeria, 102. J. F. Whiteaves.—The Invertebrate Fauna of the Lower Oolites of Oxfordshire, 104. T. Wright.—The Avicula contorta beds and Lower Lias in the South of England, 108. J. Rae.—Icebergs and Ice-action as observed in the Hudson’s Bay and Straits, 174. Canadian Journal. New Series. No. 34. July 1861. C. Robb.—Petroleum ep of Western Canada, 314. E. Billings.—Devonian Fossils of Canada West, 329. E. J. Chapman.—Klaprothine or Lazulite, 363. E. Lartet.—Coexistence of Man with certain extinct Quadrupeds, 368. Chemical Society. Quarterly Journal. Vol. xiv. Parts 2 and 3. Nos. 54 and 55. July—October 1861. R. Adie and E. Frankland.—Ground-ice, 112. F. Field.—Some Minerals from Chile, 153. V. Harcourt.—Peroxides of Potassium and Sodium, 267. Christiania. Solennia Academica Universitatis Literarie Regie Fredericiane ante L. annos condite die 2 Septembris anni mpcccLxtI. celebranda indicit Senatus Academicus. 1861. 48 DONATIONS. Colonial Mining Journal (Melbourne). Vol. ii. Nos. 7 and 8. March and April 1861. P. Nisser.—Origin of the Metals in the Pleistocene detritus, 99, 111. H. Mackworth’s ‘ Pocket-metra,’ 115. J. Brady.—Bendigo Waterworks, 120 (map). Critic. Vol. xxii. Nos. 574-500. July—October 1861. Notices of Meetings of Scientific Societies, &c. H. W. Bristow’s ‘Glossary of Mineralogy,’ noticed, 423. Darmstadt, Notizblatt des Vereins fiir Erdkunde und verwandte Wissenschaften zu, und des Mittelrheimischen geologischen Vereins. Vol. iu. Nos. 32-40. 1860. Seibert.—Mineralogisch-geognostiche Notizen fir Excursionen in der Umgegend von Bensheim und Auerbach, 66. H. Tasche.—Zu den Sectionen Alsfeld und Allendorf, 69. —. Zur Section Giessen, 85. A. Gross.—Fossile Pflanzen im Taunusquarzit bei Ockstadt, 71. R. Ludwig.—Lagerungsverhaltnisse des Quarzites und Sericit- schiefers bei Bingen, Schloss Johannisberg und Rudesheim, 71. A. Gross.—Aus der Section Fauerbach-Usingen, 83. Seibert.—Versteinerungen aus der Section Worms (linke Rhein- seite), 85. R. Ludwig.—Kalk, Schiefer und Eisenstein von Walderbach ohnfern Stromberg, 86. Seibert.—Beobachtungen aus den Sectionen Erbach und Michelstadt, 87. R. Ludwig.—Kramenzel, Kieselschiefer und flotzleerer Sandstein bei Butzbach, 99. QO. Buchner’s ‘ Die Feuermeteore,’ 102. F. Scharffi—Die Quarzgange des Taunus, 115, 125. Seibert.—Die Buntsandsteinformation im Ostliche Theile der Section Erbach, 126. ——. ——. Vol.iu. Nos. 41-60. 1861. Seibert.—Die crystallinischen Gesteine des Odenwalds, 2. R. Ludwig.—Animalische Reste aus der westfilischen Steinkohlen- formation, 10. C. Koch.—Das Vorkommen von Schwefelkiesen und Pseudomor- phosen nach denselben in der Krammenzelformation, 12, 21. R. Ludwig.—Die Entstehung von Susswasserquellen bei Homburg am Taunus, 18. . Das Verhialtniss der Braunkohlenablagerung der Grube Jager- thal bei Zell zu den Vogelsberger Basalten, 29, 39. Die Braunkohlen von Wolfen in der Nahe von Halle, 55, 62. ——. Geologisches aus Russland, 65, ——. Die Mineralquellen zu Homburg vor der Hohe, 82, 89, 98, 107, 115 (plate). C. Koch.—Vitrioleier, 6. Seibert.—Knochenreste bei Heppenheim, 7. Aus der Section Worms, 23. ——, Aus der Section Hirschhorn, 152. ——. Versteinerungen aus dem Bensheim-Heppenheimer tertiaren Meersandstein, 118. DONATIONS. AY Darmstadt, Notizblatt des Vereins fiir Erdkunde und yerwandte Wissenschaften zu, und des Mittelrheinischen geologischen Vereins. Vol. iii. Nos. 41-60. 1861 (continued), Tasche.—Breccie aus Fischzithnen und Knochenstiicken bei Angers- bach, 118. A. Delesse’s ‘Ueber die Entstehung der sogenannten Massenge- steine,’ 24. Dijon. Mémoires de ]’Académie Imp. d. Sc., Arts et Belles-Lettres de Dijon, Deux. Ser. Vol. viii, 1861. A. Perrey.—Documents sur les Tremblements de Terre et les phé- noménes yolcaniques dans l’Archipel des Philippines, 85 Cau Dorpat. Archiv fiir die Naturkunde Liv-, Esth-, und Kurlands. Herausgegeben von der Dorpater Naturforscher-Gesellschaft. Zweiter Serie. Biologische Naturkunde. Vols.ii.andiii. 1860. Frankfurt. Abhandlungen, herausgegeben von der Senckenbergis- chen Naturforschenden Gesellschaft. Vol. ni. Part 2. 1861. Fr. Hassenberg.—Mineralogische Notizen, 255 (8 plates). P, A. Kesselmeyer.—Ueber den Ursprung der Meteorsteine, 313 (3 maps). O. Buchner.—Quellenverzeichniss zur Literatur der Meteoriten, 455. Geologist. Nos. 43-46. July—October 1861. R. N. Rubidge.—Metalliferous Saddles, 281. F. W. Hutton.—The Darwinian Theory, 288. W. Pengelly.—Deer’s Horns in Brixham Cave, 288, Foreign Correspondence, 289. Proceedings of Societies, 294, 364, 375, Notes and Queries, 306, 366, 383. Reviews, 313, 356, 399, 463. W. Pengelly.—The Devonian Age, 332. J. W. Salter.—Arenicolites in Bohemia, 347, F. Drake.—Human Remains in the Drift of Belvoir, 349. O. Fisher.—Fossil Deer’s Horn with marks of Human Operation at Clacton, 352. C. C. Blake.—Macrauchenia in Bolivia, 354, 8. J. Mackie.—Torbane Hill Mineral, 369. J. Anderson.—New Fossils in the Old Red, 385. A. Delesse.—Minerals of the Metallic Veins of Freiberg, 387, A. E. Reuss.— Clytia Leachit, 392. C. C. Blake.—Association of Human Remains with those of Extinct Animals, 395. S. J. Mackie.—The Lunar Seas, 409. T. Grindley.—The Darwinian Theory, 416. J. 1. W.—Human Remains in the Valley of the Trent, 415. W. Haidinger.—Meteorites, 420. G. E. Roberts.—Coal-field of Wyre Forest, 421 (plate). ee address to the Geological Section at Manchester, E. W. Binney.—Geology of Manchester, 443. R. Owen.—Plesiosaurus australis from New Zealand, 444. A. B. Wynne.—Geology of Knocksigowna, 445, W. Pengelly.—Encroachments of the Sea at Torbay, 447. J. Yates.—Excess of Water in the Region of New Zealand, 453, YoL, XVIII,—PART I, E 50 -DONATIONS. Geologist. Nos. 43-46 (continued). E. Hull.—Distribution of the Carboniferous Sediments, 454. W. Pengelly.—New Bone-cavern at Brixham, 456. | H. Seeley.—Elsworth Rock and Bluntisham Clay, 460, J. Hector.—Pleistocene Deposits of North America, 461, ‘Great Britain. Geological Survey. Annual Report of the Director- General for 1860. 1861. : Memoirs :— The Geology of the Warwickshire Coal-field and the Permian Rocks and Trias of the surrounding District. By H. H. Howell. 1859. The Geology of the Leicestershire Coal-field, and of the Country around Ashby-de-la-Zouch. By E. Hull. 1860. The Iron-ores of Great Britain :— Part 1. Iron-ores of the North and North-Midland Counties of England. By J. Percy, W. W. Smyth, and others. 1856. Part 2. Iron-ores of South Staffordshire. By Jukes, Dick, and others. 1858. | Part 3. Iron-ores of South Wales. By E. Rogers, Ratcliffe, Salter, and others. 1861 The Geology of the Country around Wigan. By E. Hull. 1860. The Geology of the Country around Nottingham. By W,T. Aveline. 1861. The Geology of Parts of Nottinghamshire, Yorkshire, and Derbyshire. By W. T. Aveline. With Lists of Fossils by J. W. Salter, F.G.S. 1861. The Geology of the Country around Prescot, Lancashire. By EH. Hull. 1860. The Geology of Parts of Oxfordshire and Berkshire. By E. Hull and W. Whitaker. With List of Fossils by R. Etheridge. 1861. The Geology of the Country around Woodstock, Oxfordshire. By EH. Hull. With List of Fossils by R. Etheridge. 1859, The Geology of Part of Leicestershire. By W. T. Aveline and H. H. Howell. With List of Fossils by R. Etheridge. 1860. The Geology of Part of Northamptonshire. By W. T. Aveline and R. Trench. With List of Fossils by R. Etheridge. 1860. | The Geology of Parts of Northamptonshire and Warwickshire. By W. T. Aveline.. With List of Fossils by R. Etheridge. 1861. The Geology of the Country around Altrincham, Cheshire. By E. Hull. 1861, Description of Horizontal Sections, Sheets 46, 47, and 52. By E. Hull and H. W. Bristow.. 1859. Description of Geological Map, Sheet No. 78. By A. C. Ramsay. The Geology of the Neighbourhood of Edinburgh. By H. H. Howell and A. Geikie. With Appendix and List of Fossils by J. W. Salter. London. 1861. Hamburg. Abhandlungen aus dem Gebiete der Naturwissenschaften, herausgegeben von dem naturwissenschaftlichen Verein in Ham- burg. Vol.iv. Part 2, 1860. Heidelberg, Verhandlung des naturhistorisch-medizinischen Vereins m. Vol w. Part & Bunsen.—Ueber Rubidium und Caesium, 128. Kirchhoff—Ueber den Spectral-Apparat, 129. . Blum,—Ueher cin Meteoreisen yon Darmstadt, 164, DONATIONS. 51 Institute of Actuaries. List of Members. 1861. Institution of Civil Engineers. Premiums. Session 1860-61. Leeds. Geological and Polytechnic Society of the West Riding of Yorkshire. Report of the Proceedings for 1860. 1861. J. Watson.—Geology of the Esk Valley, 91, R. Hunt.—Iron-ore Deposits of Lincolnshire, 97. R. Carter.—Colliery-ventilation, 110. BS i bids Wes Milner.—Explosions in Coal-pits and state of the Barometer, 9. J. Jebson.— Water-springs, and their relation to Manufactures, 122, ee ga pelative Changes of Land and Sea, Expansion of Strata, c., 150. —— Philosophical and Literary Society. Report for 1860-61. 1861. Liége. Mémoires de la Soc. Roy. des Sciences de Li¢ge. Vol. xvii. 1861, 7 T. Davidson et L. de Koninck.—Sur les Brachiopodes munis d’appen- dices spiraux, et sur leurs espéces découvertes dans les couches carboniféres des Iles Britanniques, 1 (2 plates). Literary Gazette. New Ser. Vol. vi. Nos. 143, 145, 146, 157; Vol. vii. Nos, 158-174. Notices of the Meetings of Scientific Societies, &c. Meeting of the British Association, 229, 252, 278, 302, 329. Liverpool Literary and Philosophical Society. Proceedings. No. 15. 1861, Hi. H. Higgins and C. Collingwood.—The Darwinian Theory, 42, 81, gn6.. . - G. H. Morton.—Coal-measures of Liverpool, 193, London, Edinburgh, and Dublin Philosophical Magazine. 4th Series. Vol. xxii, Nos. 144-147. July—October 1861. W. Thomson.—Underground Temperature, 23, 121. M. W. T. Scott.—The Symon-fault of Coalbrookdale, 77. J. Prestwich.—Cyrena fluminalis fossil at Kelsey Hill, 78. E. J. Chapman.—Klaprothine or Lazulite of North Carolina, 81. R. P. Greg.—New Falls of Meteoric Stones, 107. J. Tyndall.—Physical Basis of Solar Chemistry, 147, A. Fontan.—Bone-caves in the Languedoc, 164. J. Prestwich.—Flint Implements in the Drift. 165, J. G. Jeffreys.— Corbicula fluminalis geologically considered, 165. Holzmann.—Cerium compounds, 216, F. T. Gregory.—Geology of a part of Western Australia, 246. C. Moore.—Zones of the Lower Lias, 246, H. C. Salmon.—Granite-boulders in Rosewarne Mine, 324. J. W. Dawson.—Erect Sigillaria at the South Joggins, 325. —. Trigonocarpon Hookeri from Cape Breton, 326. W. SS Bcscnatenciod Chalk, 325, J. W. Salter.—Crustacea in the Coal-measures, 325, H, How,—Analysis of Gyrolite, 326, E2 52 DONATIONS. London Review. Vol. iii. Nos. 53-69. July—October 1861. Notices of Meetings of Scientific Societies, &e. What is Coal P 201. dritish Association, Geological Section, 344. Compressed Coal, 363. Longman’s Monthly List. No, 226. October 1861. Notes on Books, Vol. ii. No. 26. August 31, 1861. J. R. Greene’s ‘Manual of the Subkingdom Coelenterata,’ noticed, 157. Manchester Geological Society. Transactions. No.6. 1861. Ki. W. Binney and others.—Safety-lamps, 86, 105. Obituary Notice of Elias Hall, 92. I. W. Binney.—The Drift-deposits near Llandudno, 97; Hzematites of Ulverstone, &c., 102. ——. Coal; Sigillaria and its Roots, 110. Mechanics’ Magazine. NewSeries, Vol.vi. Nos, 132-148, July- October 1861. Notices of Scientific Meetings, &c. Tunnel through the Alps, 82. Gentilii—Causes of Earthquakes, 47. Oil-springs in America, 180. : British Association Meeting at Manchester, 147, 165. Milan. Atti del R. Istit. Lombardo di Sc., Lett. ed Arti. Vol. 1. Fase. 1-3 (in one). 1860. Belli.—Intorno a diverse particolariti della crosta terrestre, approssi- mativamente dedotte da alcuni calcoli sulla dissipazione del calor centrale della terra, 46. Memorie del R. Istit. Lombardo di Se., Let. ed Arti. Vol. vil. (2nd Series, Vol. ii.). Fasc. 2 and 3. 1860. Verga.—Della nuova fonte salso-jodica di Miradolo, 67. Montreal. Canadian Naturalist and Geologist. Vol. vi. Nos. 1-4. February—August 1861. R. Bell.—Occurrence of Freshwater Shells in some of the Post- tertiary Deposits of Canada, 42. A, Guyot.—Physical Geography of the Appalachian Mountain Sy- stem, 51. sig Sterry Hunt.—Some points of American Geology, 81. J. Barrande, W. Ik. Logan, and J. Hall.—The Taconic System, 106. J. W. Dawson.—Geology of Murray Bay, 138. Pre-carboniferous Flora of New Brunswick, Maine, and astern Canada, 161, T. Sterry Hunt.—Origin of some Magnesian and Aluminous Rocks, G. D. Gibb.—On Canadian Caverns, 184. Duke of Argyll.—Flint-drift and Human Remains, 190. W. KE. Logan.—Quebee Group and the Upper Copper-bearing Rocks of Lake Superior, 199. J. Phillips’s ‘ Life on the Earth,’ noticed, 207, DONATIONS. 53 Montreal. Canadian Naturalist and Geologist. Vol. vi. Nos. 1-4, February—August 1861 (continued). J. Sterry Hunt.—History of Petroleum or Rock-oil, 241. E. eee Becks and Fossils occurring near Phillipsburgh, Canada t, 310. How.—New Mineral (Cryptomorphate), 333. Munich. Sitzungsberichte der kénigl. Bayer, Akad. d. Wissensch. zu Miinchen. Yol.i. Parts 1-3. 1861. H. R. Goeppert.—Ueber die Kohlen von Malowka in Central-Russ- land, 199. —. Ueber die Verbreitune der Liasflora, 210. ——. Ueber einen bei Ortenberg gefundenen Psaronius, 211. A. Wagner.—Zur Feststellung des Artbegriffes, 316. —. Ueber die Auffindung von ZLophiodon in einer Bohnerzgrube bei Heidenheim, 358. Neweastle-on-Tyne. Rules of the Tyneside Naturalists’ Field- club. 1861. ——. Transactions of the Tyneside Naturalists’ Field-club. Vol. v. Part 1. 1861. New York, Agnals of the Lyceum of Natural History of. Vol. i. 1824, W. Cooper.—Remains of the Megatherium recently discovered in Georgia, 114. —. Discovery of a Skeleton of the Mastodon giganteum, 143. J. E. Dekay.—Organic Remains termed Bilobites from the Kaats- kill Mountains, 45. —. Structure of Trilobites, and description of an apparently new nus, 174. J. Delatield.—New localities of simple minerals along the North Coast of Lake Superior, &c., 79. E. James.—Identity of the supposed Pumice of the Missouri, with a variety of Amygdaloid found near the Rocky Mountains, 21. S. L. Mitchell.—Teeth of the Megatherium recently discovered in the United States, 58. J. Renwick.—Mineral from Andover Furnace, Sussex County, New Jersey, 37. On the Geological Position of the Trilobites found at Trenton Falls, 185. J. Torrey.—Locality of Yenite in the United States, 51. —. Columbite of Haddam, Connecticut; and notice of several other North American Minerals, 89. J. G. Totten. New supports for minerals subjected to the action of the blowpipe, 109. J. J. Bigsby.—Sketches of the Geology of the Island of Montreal, 198. J. Cozzens.—Iron-ores from the northern part of the State of New York, 378. J, E. Dekay.—Observations on a Fossil Crustaceous Animal (Ewy- pterus) from Westmoreland, One'da County, New York, 375. H. R. Schoolcraft.—Native Silver from Michigan, 247. J. Van Rensselaer.—Fossil Crustacea from New Jersey, 195, ——. Supplement to this notice, 249, rT" 54 DONATIONS. New York, Annals of the Lyceum of Natural History of. Vol. il 1828. W. Cooper.—Further discovery of Fossil Bones in Georgia, 267. J. F. Dana.—Analysis of the Copper-ore of Franconia, New Hamp- shire ; with remarks on Pyritous Copper, 253. J. E. Dekay.—Several multilocular Shells from the State of Delaware ; with observations on a second specimen of the genus Hurypterus, 273 (plate). —. Fossil Skull of the genus Bos, from the Banks of the Mississippi, 280. Mitchill, J. A. Smith, and Cooper.—Discovery of a Fossil Walrus in Virginia, 271. ——. Vol. iii. 1828-36. T. Thomson.—Chemical Examination of some Minerals, chiefly from America; with Notes by John Torrey, 9. W. Cooper.—Fossil Bones of the Megalonyx from Virginia, &e., 166. J; E. Dekay.—Remains of Extinct Reptiles from New Jersey; and on the occurrence of Coprolites in the same locality,154. ——. Fossil Jaw of a species of Gavial from West Jersey, 158, ——, Vol.v. No.2. 1850. —,; Vol.vi. Nos. 1-13. 1853-58. J. D. Dana.—Homeeomorphism of Mineral Species of the Tiimetric System, 37. T. Prime.—Three new Species of Pisidium, p. 64. ==, Voli vu: INOS; 1-9: “1859=60: T. Prime.—List of the known Species of Pistdiwm, with their Synonymy, 94. S. Smith.—Mollusea, Peconic and Gardiner’s Bays, Long Island, N. Y., 147; R. P. Stevens.—Taconic System, 276. Oriental Translation Committee. Report, &c. 1861. Palermo, Atti della Societa di Acclimazione e di Agriceltura in Sicilia. Vol.i. Nos. 1-4. 1861. Paris. Annales des Mines. 5°Sér. Vol. xix: 2° et 3° Livr. de 1861. Gruner et Lan.—Etat présent de la métallurgie du fer en Angleterre, 131. De Senarmont.—Extraits de minéralogie, 249, Callon.—Statistique minérale de l’empire d’Autriche, 285. Limpérani.i—Sur la découverte de gisements auriféres dans la pro- vince de Valdivia (Chili), 488. Gauldrée-Boilleau.u—Sur les gisements de cuivre nouvellement dé- converts au Canada, 489. De la Fosse.—Sur le traitement des minerais de fer & V’anthracite en Pennsylvanie, 490. Hocquard.—Sur la découverte d’un gisement de houille au Mon- ténégro, 495, DONATIONS, 55 Paris. Bulletin de la Société Géologique de France. Deux. Sér. Vol. xvii. Feuil. 53-57. 1861. Réunion extraordinaire a Besancon (Doubs), 819. —. —. Vol. xviii. Feuil. 22-43. 1861. Bureau.—Sur le terrain dévonien de la Basse-Loire, 337. De Verneuil et de Keyserling.—Coupes du versant méridional des Pyrénées (pl. vi.), 341 ; Ebray.—Sur les faunes des couches & oolithes ferrugineuses, 357. Bouriot et P. Marés.—Sur l’fge différentiel des roches qui constituent le massif d’Alger, 359, 365, Deshayes.—Distribution des mollusques acéphalés dans le bassin ter- tiaire de Paris, 370. Albert Gaudry.—Sur les Antilopes trouvées & Pikermi (Gréce) __ (pl. vii. viii. ix.), 388, eee oon & sa communication du 4 février dernier, 322, Ed. Suess.—Extrait d’une lettre &4 M. Deshayes sur la géologie de Vienne (Autriche), 407. Albert Gaudry et J. Barrande.—Sur la longévité inégale des animaux supérieurs et des animaux inférieurs dans les derniéres périodes géologiques, 408, 412. Melleville.—Description géologique de la montagne de Reims et des pays voisins, 417. _ | Emile Goubert.—Coupe dans les sables moyens, 4 Lisy-sur-Oureq Seine-et-Marne), 445. D’Archiac.—Observations critiques sur la distribution stratigraphique et la synonymie de quelques rhizopodes, 461. Daubrée.—Etudes et expériences synthétiques sur le métamorphisme et la formation des roches cristallines (Résumé), 468. Marcel de Serres.—Note additionnelle sur la troncature normale des coquilles fossiles, 499. Th. Ebray.—Stratigraphie du systéme oolithique in{érieur du départe- ment du Cher, 501. J. Barrande.—Sur deux ouvrages de MM. Koetting et Ed. Zeis, 517. Emile Goubert et Zittel—Sur le gisement et les fossiles de Glos a”: 520. D’Archiac.—Réponse & quelques observations critiques de M. Co- uand, 522. Albert Gaudry.—Sur les carnassiers fossiles de Pikermi (Gréce) (pl. x, et xi.), 527. cece ae des fossiles siluriens découverts dans le massif rhénan du Condros, 538. Delesse.—Etudes sur le métamorphisme des roches, 541. Nogués.—Sur le terrain crétacé de Tercis (Landes), 548, D’Archiac.—Sur quelques fossiles tertiaires et crétacés de l’Asie Mineure, 552. De Raincourt.—Sur les sables moyens de Verneuil (Marne), 564. D’Archiac.—Sur l’existence du second étage du lias prés d’Hirson Aisne), 567. E. Piette.—Sur un gite coquillier 4 Maubert (Ardennes), 572. E. Dumortier.—Sur le calcaire 4 Fucoides, base de l’oolithe inféri- eure dans le bassin du Rhone (pl. xii.), 579. Albert Gaudry.—Sur la Girafe et l’Helladotherium trouvés a Pikermi (Gréce) (pl. xiil.), 587, 56 DONATIONS, Paris. Bulletin de la Société Géologique de France. Deux. Ser. Vol. xvii. Feuil. 22-43. 1861 (continued). Jaubert et Ed. Hébert.—Sur la grande oolithe de la Provence, 599, 611. ; G. Cotteau.—Sur la famille des Salénidées, 614. Raulin.—Notice indicative des Pholadomyes tertiaires, 627. D’Archiac et De Roys.—Sur la faune tertiaire moyenne des environs de Béziers et de Narbonne, 630, 638. Jules Martin.—De 1’étage bathonien dans la Cote-d’Or (pl. xiv.), 640. Alph. Milne Edwards.—Sur les crustacés fossiles, 656. Paul Dalimier.—Sur la stratigraphie des terrains primaires dans la presqwile du Cotentin, 663. D’Archiac.—Sur les fossiles recueillis par feu M. de Boissy au plateau du Four (Loire-Inférieure), 666. Clarke.—Sur la formation carbonifére de l’Australie, 669, Ed. Jannettaz et Delanoue.—Sur la formation du cacholong dans les silex de Champigny, 673, 674. Edm. Pellat.—Sur l’existence aux environs d’Autun d’ossements de Sauriens dans une assise calcaire, 676. J. Fournet.—Sur les roches éruptives modernes du Lyonnais, 677. Naumann.—Sur les pseudomorphoses (extrait d’une lettre & M. Delesse), 678. ——. L’Acad.d. Sc. Comptes Rendus hebdom. 1861. Prem. Semestre. Vol. li. Nos. 21-25. Deux. Sér. Vol. lui. Nos, 1-11. Photographic Society. Journal, Nos. 111-114. July—Oct. 1861. Plymouth Institution and Devon and Cornwall Natural History Society. Annual Report and Transactions, 1860-61. 1861. Quarterly Journal of Microscopical Science. New Serics. Nos. 2,3, 4. April, June, October, 1861. Royal Asiatic Society of Great Britain and Ircland. Vol. xviii. Part.2, and Vol; xix. Part 1. 18645 Royal Astronomical Society. Memoirs. Vol. xxix. 1861. A. R. Clarke.—The Figure of the Earth, 25, Royal Geographical Society. Proceedings. Vol. v. No. 3. 1861. Royal Horticultural Society. Proceedings. Vol. i. Nos. 26-29. Royal Institution of Great Britain. Notices of the Proceedings, Part xi. 1860-61. M. Faraday.—Platinum, 321. H. D, Rogers.—Parallel Roads of Glen Roy, 341. ——, List of Members, &c., 1861. ——. Additions to Library (No. 4) from July 1860 to July 1861. Royal Society. Proceedings. Vol. xi. Nos. 44, 45, 46. Ii. Moseley.—Descent of Glaciers, 168. Kt. Mallet,—Wave-transit in rock-formations, 352, DONATIONS, 57 St. Louis. Academy of Science. Transactions. Vol. i. No. 4. 1860. A. H. Worthen.—Fossils from the Mountain-limestone of Illinois and Iowa, 569. H. A. Prout.—Paleozoic Bryozoa from the Western States, 571. B. F, Shumard.—Cretaceous Strata of Texas, 582. —. Cretaceous Fossils from Texas, 590. J. Marcou.—Geology of Kansas and Nebraska, 610. 8. S. Lyon.—Rocks of Kentucky, 612. B. F. Shumard.—Meteoric Iron from Texas, 622 (plate). -——. Paleozoic Fossils from Texas, 624. 8. 8. Lyon.—Blastoidea from Kentucky, 628 (plate). G. se Swallow.—Carboniferous and Devonian Fossils from Missouri, St. Petersburg. Bulletin de l’Acad. Imp. d. Se. de St. Pétersbourg. Vol. ii. Nos. 4-8. 1861. K. E. de Baer.—Sur une loi générale de la formation du lit des riviéres, 352. H,. Abich.—Sur un aérolithe tombé a Stavropol, 404, 433. —. Sur son voyage au Daghestan, 443. J. F. Brandt.—La paléontologie de la Russie méridionale, 501. —. Sur un squelette de Mastodon, 507 (plate), Vol. iii. Nos, 1-5. 1861. ~ G. de Helmersen.—Géologie de la vallée du cours inférieur de la Naroya, 12 (map and plate). J. F. Brandt.—La paléontologie de la Russie méridionale, 74. —. Sur l extinction de la vie animale dans la Baie de Balaklava, ar suite de la putréfaction d’une grande quantité de poissons, 84. J. Fritzsche.—Sur le Retén, 88. ——. Surun sel double de carbonate et de chlorure de Calcium, 285. H. R. Goeppert.—Sur les plantes du terrain liassique du Caucase et de l'Elbrous en Perse, 292. ; Mémoires de Acad. Imp. des Sciences de St. Pétersbourg. Vol. iii. Nos. 2-8. 1860. N. y. Kokscharow.—Die russischen Topase (3 plates). G. v. Helmersen.—Steinkohlenlager des Gouverments Tula. —. Jas Olonezer Bergrevier geologisch untersucht in den Jahren 1856-59 (map). N. y. Kokscharow.—Die russischen Epidot und Orthit (5 plates). Society of Arts. Journal. Vol. ix. Nos, 450-463, 465, 466. July— Oct. 1861. W. P. Jervis.—Mansfeld Copper-mines, 598, 603, 616, 627. Consular Information, 642; [Diamonds and Nitrate of Soda, San Domingo, &c. | 647, 760, 780, 793. New Paint from Antimony, 759. A. K, Irbister.—Discovery of Gold in the Valley of the Saskat- chewan, 759. . W. Vivian.—Structure of Metals, 782. Stuttgart. Wiirtembergische naturwissensch. Jahreshefte. Sieben- zehnter Jahrgang. Erstes, zweites und drittes Heft, 1861. O. Fraas.—Ueber Semionotus und einige Keuper-Conchylien, 81 (plate), 58 DONATIONS, Stuttgart. Wiirtembergische naturwissensch. Jahreshefte. Sieben- zehnter Jahrgang. LErstes, zweites und drittes Heft, 1861 (con- tinued). | A. Oppel.—Die Arten der Gattungen Glyphea und Pseudoglyphea, 108. O, Fraas.—Die Mammuths-Ausgrabungen zu Cannstatt im Jahre 1700, 112. A. Oppel.—Ueber die weissen und rothen Kalke von Vils in Tyrol, 129 (2 plates). C. Deffner.—Die Lagerungs-Verhiltinisse zwischen Schonbuch und Schurwald, 170 (map and plate). Vienna. Denkschriften der kais. Akad. der Wissensch. Math.- naturw. Classe. Vol. xix. 1861. Unger.—Sylloge plantarum fossilium. Sammlung fossiler Pflanzen,. besonders aus der Tertiiir-Formation, 1 (21 plates). Heckel und Kner.—Neue Beitrage zur Kenntniss der fossilen Fische Oesterreichs, 49 (10 plates). S. von Mohrenstern.—Ueber die Familie der Rissoiden, 71 (11 plates). Sitzungsberichte der kais. Akad. d. Wissensch. Math.-nat. Classe. Band xlii. Heft 1. Jahrgang 1861. Jinner. Erste Abtheilung (Mineralogie, Botanik, Zoologie, Anatomie, Geologie und Palaontologie). a KK. Reuss.—Ueber die fossile Gattung Acicularia, D’Archiac, 7 plate). , H. Emmrich.—Zur Kenntniss der siidbay’rischen Molasse, 13. A. Pokorny.—Ueber die Torfmoore Ungarns, 57 (map). — , 1 ——. Zweite Abtheiling (Mathematik, Physik, &c.). Heft 2. Februar. Erste and zweite Abtheil. F. Stoliczka.—Ueber die Gastropoden und Acephalen der Hierlatz- Schichten, 157 (7 plates). Washington. Smithsonian Institution. Smithsonian Contributions to Knowledge. Vol. xii. 1860. —-. . Annual Report for 1859. 1860. R. Mallet.—Harthquake phenomena, 408. Wiesbaden. Jahrbiicher des Vereins fiir Naturkunde im Herzogthum — Nassau. Heft xiv. 1859. W. Casselmann.—Ueber die Zusammensetzung der in der Niihe von Dillenburg vorkommenden Nickelerze, 424. ——. Ueber ein Graphitvorkommen in der Nahe von Montabaur, 432, Ei. Hildenbrand.—Analyse des Manganspathes von Oberneisen, 434. C. Hielt und R. Rohr.—Chemische Untersuchung des Mineral- wassers im Badehause, 436. A. Oker.—Chemische Analyse eines Spirifersandsteins von Kem- menar, Amts Nassau, 447, Berichte, &c., 450. = ee ee ee ee DONATIONS. 59 Zoological Society of London. Proceedings (Illustrated), 1861. Part 1. January—March. E. Vansittart Neale.—Typical Selection, 1. —. Proceedings for 1861. Part 2. March-June. 1861. — —, Transactions. Vol.iv. Part 7. Section]. 1861. II, PERIODICALS PURCHASED FOR THE LIBRARY. - Annals and Magazine of Natural History. 38rd Series, Vol. viii. Nos. 43-46. July—October, 1861. H. Seeley —New Echinoderms from the Upper Greensand, 16. J. F. Whiteaves.—Paleontology of the Coralline Oolites of Oxford, 142 (plate). W. K. Parker and T, R. Jones.—Nomenclature of the Foraminifera (Alveolina), 161. | H. C, Sorby.—The organic origin of the so-called “ Crystalloids” of the Chalk, 193. W. K. Parker and T. R. Jones.—Nomenclature of the Foramimfera Operculina and Nummulina), 229. Hi. J. Carter.—Structure of fossil Foraminifera from Scinde, 309. H. Faleoner.—Synonymy of Echinodon, Owen, 341. Edinburgh New Philosophical Journal. New Series. Nos. 27, 28. Vol. xiv. Nos.1,2. July and October 1861. W. King.—Certain species of Permian shells said to occur in the Carboniferous Rocks, 37. D. M. Holme.—Ancient glaciers of Chamouni, 46. A. Geikie.—Rise of the Coast of Frith within the Historical Period; 102 ff. How.—Natroborocalcite and another borate in the Gypsum of Nova Scotia, 112. -——. Gyrolite with Calcite in Apophyllite in the Trap of the Bay of Fundy, 117. D, Page’s ‘The Past and Present Life of the Globe,’ noticed, 129, A. Geikie.—Chronology of the Trap-rocks of Scotland, 143, A. Bryson.—Aqueous origin of Granite, 144. Obituary notice of the Rev. J. 8. Henslow, 169. ; R. Edmonds,—Earthquakes and extraordinary agitations of the sea, 203. bf Symonds.—The Drifts of the Severn, Avon, Wye, and Usk, T. Oldham.—Slate in India, 327. Institut, ’. I Section. Nos. 1434-1450. June—October, 1861. —. 2™ Section. Nos, 306-309. June—-September, 1861. Notices of Meetings of Scientific Societies, &c. 60 DONATIONS, Leonhard und Bronn’s Neues Jahrbuch fir Min., &c. Jahrg. 1861, drittes Heft. Giimbel.—Ueber das Alter der Miinchberger Gneiss-Parthie im Fichtelgebirge, 257. | C. F. Peters—Ein Beitrag zur Entwickelungsgeschichte des Azurits und Malachits von Moldava im Banate, 278. J. Barrande.—Ueber die geologischen und paliontologischen Er- scheinungen in Canada, 286. Quenstadt—Bemerkungen zum Archegosaurus, 294 (plate). C. v. Fellenberg.—Einige neuere Mineral-Vorkommnisse aus Ungarn und Siebenbirgen, 301. Letters ; Notices of Books, Minerals, Geology, Fossils, ——. Beilagen-Heft. Ueber die Ursachen der in den Jahren 1850 bis 1857 stattgefundenen Erd-Erzchiitterungen, und die Bezie- hungen derselben zu den Vulkanen und zur Atmosphire, von Dr. K. E. Klug. 1861. Paleontographica von H. von Meyer. Vol. vii. Parts 5 & 6. June and September, 1861. H. von Meyer.—Reptilien aus dem Stubensandstein des oberen Keu- pers, 253 (20 plates). III, GEOLOGICAL AND MISCELLANEOUS BOOKS. Names of Donors in Italies. Austin, T. On anew Genus of Echinoderm ; and Observations on the Genus Palechinus. 1860, On Lower Silurian Rocks in the South-east of Ireland; and on a Human Skeleton in an elevated Sea-margin. 1860. Becker, F.,und R. Ludwig. Geologische Specialkarte des Grossher- zogthums Hessen und der angriinzenden Landesgebiete im Maas- stabe vom 1:50000. Terausgegeben vom mittelrheinischen geo- logischen Verein. Section Dieburg (Darmstadt). rom the Middle Rhine Geological Society. Beke, O. T. On the Mountains forming the Eastern side of the Basin of the Nile, and the origin of the designation ‘‘ Mountains of the Moon,” as applied to them. 1861. Biden, W. D. Rules, Formule and Tables for the Valuation of Estates in possession or in reversion, with new rules and tables for ascertaining the correct market value or fair price to be given for Annuities, Reversions, Advowsons, and Next Presentations. 1816. Bosquet, J. Notice sur le genre Sandbergia, genre nouveau de mollusques gastéropodes de la famille Cerithiopside. 1861, ' ee ee ee ee ee ee ee ee ee a DONATIONS, 61 Bristow, H. W. th inch in diameter, and 4-th in thickness. The gently sigmoid and semitranslucent edges of the septa appear at the surface, and but seldom rise above it (except when the specimens are mechanically compressed, which is a common condition). The whorls (three in large specimens) are all visible in empty shells made transparent by water or Canada-balsam; they are proportionally wide for Nummulina (the outer whorl making half the width of the disk). The chambers are about half as long as wide, neatly curved, but subject to irregularity of growth. The lateral portions of the chambers, though very shallow, are continued over the surface towards the centre on each face, and are rather straighter in old specimens than in the young. 94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 8, This neat and delicate variety of Nummulina planulata, Lamarck, sp., has long been known in a clay containing much green sand, at Alum Bay, Isle of Wight (lower part of the bed ‘ No. 29’ of Mr. Prestwich’s Section, Quart. Journ. Geol. Soc. vol. 1. p. 257, pl. 9. fig. 1.); but it has not hitherto been described *. It is near to MM. d’Archiac and Haime’s ‘ Nummulites planulata, var. a,’ from Jette, Belgium t+; but the latter has a biconvex centre (opake when mounted in balsam), has narrower whorls (in the proportion of 1 to 4, instead of 13 to 4), and grows to a somewhat larger size. To distinguish our variety (which characterizes a well-marked geological zone), I propose to give it the name of Prestwichiana; and, as the small biconvex variety of Nwmmulina planulata passes binomially as N. variolaria, so this small depressed variety of the same species may be allowed to stand on a similar footing, and be known as WV. Prest- wichiana. In the sandy clay-bed at Alum Bay the shells of this little Nummu- lite are very numerous, and often well preserved, but not unfrequently much crushed by pressure. In many specimens, especially large ones, the chambers are occupied by iron-pyrites; and neat casts may be obtained by carefully dissolving the shell in weak dilute acid. In the clay at High Cliff the shells are not so numerous, are very much compressed, and so highly pyritized that they are readily destroyed by the atmosphere. — JaNnuARY 8, 1862. sharles Sturtirant Wood, Esq., Geological Survey of Otago, New Zealand; Robert Harris Valpy, Esq., Enborne, near Newbury ; and William Shepherd Horton, Esq., 10 Church Street, Liverpool, were elected Fellows. The following communications were read :— 1. On the Carsonirerovs Limestone of Oreton and Fartow, CLEE Hitis, Suropsuire. By Prof. Joan Morris, V.P.G.S., and Mr. Grorce EK. Rozerts. With a Description of a New Prericuruys ; by Sir Puruir pe M. G. Eenrron, Bart., M.P., F.R.S., F.G.S. [Pxate IIT. ] ConrTENTS. 1. Geographical Position of the Series. 2. Relation of the Yellow Sandstone to the Carboniferous Limestone. 3. Nature and Character of the Carboniferous Limestone. 4, Its Fossil Contents. § 1. Tux general physical and paleontological features of the small district referred to in these notes having been carefully and clearly * “ Nummulites levigatus and N. elegans”’ are incorrectly referred to as occur- ring in this bed, No. 29, op. cit. p. 257. t See ‘ Foss. de l’Inde,’ pp. 145, 144; and also Quart. Journ. Geol. Soc. vol. Vili. p. 333, note. es 1862.] MORRIS AND ROBERTS—CARBONIFEROUS LIMESTONE. 95 described by Sir Roderick Murchison in his classic work ‘The Silu- rian System,’ the additional facts which a visit paid to it during the past autumn enables us to record may be considered simply as a continuation of those previously observed. The thin beds of limestone which form the basement of the Titter- stone Clee Coal-field are well exposed in a marginal flexure of the strata north-eastward of the hill, at Oreton and Farlow, and also, at a somewhat higher level, around its southern abutments. Our observations upon the character of the beds and their fossil contents have been confined to the exposures in the first-named localities. The geographical relations of this limestone ridge with the near- lying millstone-grit and coal-measures, in their turn covered up by the sheets of erupted basalt which form the high summits of the Clee, are well seen from the igneous knoll of Kinlet, three miles to the eastward. § 2. Immediately below the summit of the ridge at Farlow, and on the northern side, is a quarry of yellow sandstone, from which recently a large quantity of stone has been obtained for the rebuild- ing of the church. It is a thick-bedded, fine-grained sandstone, having ripple-marked surfaces, and occasionally containing disseminated pebbles of quartz. The colour of the stone is a pale yellow, in places slightly stained by ferruginous oxidation. Remains of fossil Fishes were first de- tected in this quarry in 1856; these consisted of dermal plates of Pterichthys, or an allied genus; and from it was subsequently ob- tained by Mr. T. Baxter, F.G.S., the anterior portion of a Pterich- thys, of a new species, which is now in the collection of Sir Philip Egerton. It is described by Sir Philip at the end of this paper. Several other specimens (one nearly perfect) of this new species have lately been obtained by us from some large slabs of this yellow sandstone, as well as fragments of a larger Pterichthys, and de- tached scales of a small Holoptychius, probably of an undescribed species. A single plate of the well-known Holoptychius giganteus also rewarded our search. No remains of Testacea (with the ex- ception of fragments of Conulariw) nor of Plants have yet been de- tected in these beds. The measures lying between this Pterichthys-bearing sandstone, and the Old Red rocks which form a wide surface to the northward, are the following, given in descending order :—coarse yellow sand, without pebbles; yellow sand with loosely laid pebbles of quartz ; a thin bed of similar pebbles, compacted into a conglomerate; and fissile yellowish sandstones. The precise junction of this lowest bed with the red rocks having cornstone-bands is not at present to be seen, but a roadway now in progress of cutting will probably expose it. Above the Pterichthys-bed, a nearly similar series of alternating sands, with and without pebbles, lead up to compact pebbly sand- stones and coarse grits; and these are capped near the summit of the ridge by fissile yellow sandstones. About thirty feet of unknown ground lies between this and the beginning of the limestone series. 96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 8, Passing southward over the ridge, and at a point immediately below its summit, the upper beds of this sandstone series are observed, underlying and passing into the Carboniferous Limestone series above. This junction with the superincumbent limestone beds is clearly to be seen in a quarry 8. of the road, ina lne with the one we have been describing. The general relations of the series are seen in the following section. The strata dipping to the S.E. at an angle of 60°. , ‘ All the beds in this section, and more especially the oolitic lime- stone, are seen to increase in thickness as we trace them eastward from Farlow to Oreton. Many Cestraciont palatal teeth and Brachiopodous shells have been obtained from this opening into the limestone ridge, so graphi- cally described by Murchison. Half-a-mile eastward of it are the greater quarries of Oreton. There is evidence in the intermediate space of the limestone having been formerly worked ; for numerous hollows, from which stone has been got, make the irregularly undulating ground still more uneven. We are indebted to the Rey. J. Williams, of Farlow, for some valuable information relating to a recent exposure, in one of the deepest of the Oreton quarries, of the subterranean stream which has long been known as flowing parallel with the axis of the ridge. This “mole river ”’ loses itself in a hollow called the Foxholes, at the western extremity of the limestone, and, taking an N.N.K. course, reappears at the distance of a mile, about 300 yards from its con- fluence with the River Rea. Two of the quarrymen, who had struck upon it at the depth of about fifty feet from the surface, described it as a constant stream, occasionally greatly swollen by floods. An interesting account of an accidental stoppage at its inlet during one of the great floods of last year was furnished us by Mr. Williams. He stated, from his own observation, that two and a half acres of the hollow were covered to an average depth of fifteen feet by the dam- ming up of its course. Forty-eight hours sufficed to drain away this accumulation of water through its underground passage. From the data supplied by the careful observations of Mr. Williams, whose residence is above the stream, the lake thus formed must have con- tained one million six hundred and thirty-five thousand cubic feet of water; and the rate of its subsidence was not less than thirty- four thousand cubic feet per hour. It appears from this that the fissure through which the stream flows is of no insignificant dimen- sions. § 3. The quarries at Oreton are very extensively worked, and afford a good section of the general thickness and character of this limestone in its northern area. In the order of the beds, the deposits are a repetition, in greater thickness, of those exposed at Farlow. The variable character of this limestone, and its thinning out at each extremity, have been alluded to in ‘ The Silurian System,’ and are interesting as showing the different conditions, within a limited area, which obtained during its deposition. As a rule, the middle 97 MORRIS AND ROBERTS—CARBONIFEROUS LIMESTONE. 1862.] es are more fossiliferous than € seri and lower parts of the limeston , by the abundance 10n -sea condit the upper; and these indicate a deep “OUOJSPUBS OTISSTT ‘QUOIspUR pay PIO ‘souojsudog sedd q ‘sUOJSpURS Poy ‘pues mozjed poyeururery. ‘pues mood ut sopqqog "eID0eIg puR spuRg Or~oisdtoan ‘spoq-aiqqed Molex ° ‘speq-osesseg Jo |} ‘CHd-SAHLHOYAL| OYJ, “souojspuvs MOTTOX ° soTOISpUB MOT[OA “speq-a1qqed °6 ‘sorqqed pur spueg ‘oT ‘pues moped poyeutmmey *[T | ‘OULIT JO oyetI0G.1K0 | ‘(9903 OG) punors umouyUy ‘ZI | JO sUI0A pUe oUOJsoUTTT Jo sossvuT ATeUOMeIOUOD YITA ‘OUOSpURS MOTIAA “CT ‘SOYOUL Q JooF E ‘ Yyo99 Teyeyed osxey SuLUTeyUOD ‘oMOYSoUIT, OTJITOO Aaa “FT ‘qa0g GZ ‘aeds-oyeo Jo so—npou yyIM aa el a ‘SOTOUT Q yooy F ‘ (,, SeTquMP ,,) eUOysouNTT aytT00 Kang f ST ‘SOTOUL Z 400} F * Spuvq snoutdnatoy YIM ‘sXe puw yoor Apues yJoR -g] : ‘soyout F ‘Avjo youl LT ‘q003 T { Ayjoeys Axoa ‘ouojsounry Lory *Q1 ‘A'S ‘009 oqe ‘diqy ‘geez g {skevpo UMOIg “eT ‘SOYOUL Q JooFF ‘ vozodag yAIM ‘ouoysoUMT] [eptoutro LoL “OZ 700} Q SOFIA SuULIOYJVom ‘oUOYsoUNIT YsTyAep Jo sopnpou AreuorjeroU0D YIM ‘sXvyo Loas-yaVE “TZ ‘JO0FG + CUOJOUTI] JO Spoq UIT} UIT ‘spoq Apurg “ZZ ‘QUOISOUTT] SNOSOL|[ISAB JO SUOTJETOIOD YIM ‘souoysotut] Apues Jo spueq poppeq-uNy, “ez 1 8/L/ =] ere || E/ o 8 ANS AK PW ge ae a W ~ \ \ : ‘H'S'S ' "saUojsaUV'T snouafuogung MM Hanoy a3 oso huamoys ‘auysdouwyg ‘mopwny yo souojspuny monaz ay) ybnouyy uonooy the lar the imi in 1es are te by their structure s to those which have produced like beds VOL. XVIII.—PART I, ] feature of the ser ica ica 10n. The most important phys olitic limestone, which ind opodous shells, and the absence of large Lamellibranchiate f format of Brachi bivalves. bands of o agencies 0 98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Jan. 8, Carboniferous Limestones of Bristol and along the margins of the South-Wales Coal-field. Most of the larger palatal teeth le in the specular limestone, and in this the oolitic grains are associated with fragments of Brachio- pods, Bryozoa, and Crinoids. As the limestone-bands differ in character, some being more shelly than others, some oolitic, and a third group slightly argillaceous and sandy, they necessarily vary in commercial value, and are used for sundry purposes, among which lime-making and building-stone ap- pear to be chief. The thickest of the oolitic beds has been worked to a considerable extent for decorative purposes ; this is locally called ‘“‘jumbles,” but is elsewhere known as “ Clee Hill marble.” § 4. But, besides its economic value, this quarry is particularly interesting and important to the paleontologist, with regard to the fossil fauna of the period, in the comparative abundance of well- preserved ichthyic remains, chiefly Cestraciont teeth and fin-spines. We are indebted to Mr. Weaver Jones, of Cleobury Mortimer, for the preservation of some of the finer and more remarkable of these, - especially the great Deltodz, which probably belong to an undescribed species. The attention of another gentleman, Mr. E. Baugh, of Bewdley, has been directed of late years to the fossil contents of these limestones ; and with much assiduity he has collected every fragment of organism which could add.to our knowledge. The following genera are represented by palatal teeth :—Orodus (specimens of O. ramosus of unusual size are occasionally met with, —one of those we exhibit exceeds the largest figured by Agassiz), Helodus, Cochliodus, Cladodus, Psammodus, Deltodus (examples of a new species of this form of tooth, of great dimensions, which have been found several times of late, are here figured), and, more rarely, the cusped Pristicladodus Goughi. With these, fin-spines of great size are occasionally found asso- ciated. The form most commonly met with is that of a Ctenacanthus ; but the series of tubercles, more or less compressed, which are ar- ranged perpendicular to its length, do not agree with any published figure. Specimens, however, less ornamented, and which appear to be Ctenacanthus brevis, are also met with. . No other ichthyic remains, save a few undeterminable fragments, probably of dermal plates, have come under our notice. Zones of shells also occur in these limestones, both above and below the beds which contain the fish-fossils, but very rarely asso- ciated with them. ‘These are principally Brachiopods, of which Spirifere and Rhynchonelle are the most abundant. The species are but few in number; but an instructive series of intermediate forms —as, for example, those which appear to link together Spurzfer cus- pidatus and Sp. distans—may,be collected. Among the Rhynchonelle, R. pleurodon is found in great abundance at the bottom of-the series, though we have met with no instance of its occurrence in the previously laid sandstones. Terebratule are nearly, if not quite, absent ; and Discine are only represented by one species—D. nitida. 1862.] MORRIS AND ROBERTS—CARBONIFEROUS LIMESTONE. 99 Of Gasteropoda we have only seen Huomphalus pentangulatus. The Crustacea are as poorly represented ; one imperfect specimen of Phillipsia mucronata, from the lower beds, being our sole illustration. Bryozoan remains are numerous, though they appear to be con- fined within the narrow limits of the crinoidal band. Several species of Fenestella make a seeming confusion upon some surfaces in this bed, by the wildness and luxuriance of their growth; of these, the commonest are Fenestella plebeca and F. Morrisw. Associated with them is the elegantly sculptured Vincularia megastoma, and some other slightly branching Bryozoa. No well-defined remains of Crinoidew have been found, although one band of rock appears to be made up of the separated ossicula and pelvic plates of these animals, chiefly referable to Poteriocrinus gracilis, Cyathocrinus macrochewrus, and C. quinquangularis. The fish-remains tabulated below, and contrasted with those from the Mountain Limestone of other districts, though numerous, do not, as we believe, exhaust the series. Some of the smaller forms of Helodus and Psammodus, unrepresented in the Oreton column of the annexed Table, probably occur in those limestones, but we are unable at present to verify this assumption. In concluding our remarks, we have to express regret that the distance and the difficulty of removing the large collection liberally _ offered us for study by Mr. Weaver Jones prevent us now entering “upon other questions of interest connected with the relative value of the palzontological contents of this interesting locality; for we see in this, as in other instances, the possibility of giving decisions of value, by carefully elaborating the treasured-up systems of organic life preserved by a single district. Table showing the Geographical Range of the Fishes of the Mountain- Inmestone. [Note.—The materials of ‘this Table are derived from the following authori- ties: the British species from Agassiz and M ‘Coy ; the Belgian from De Koninek ; and the Russian from those cited by E. d’Hichwald in his ‘ Lethea, Rossica,’ 1861. The column for Ireland is chiefly made up from the Armagh specimens, and includes the new species with MS. unpublished names contained in the cabinet of the Earl of Enniskillen, upon which it is the intention of Professor Agassiz to publish papers ; and also those, from the Lower Carboniferous rocks, cited by M‘Coy. The column for North Britain refers to the Lower Carboni ferous rocks of Westmoreland, Northumberland, and Scotland.]_ Oreton Yorkshire { Ireland and Bristol. and (chiefly | North Farlow. BROS ETE Ronaahy Britain. Acrolepis Hopkinsii, M‘Coy ...| ...... | see. * Mcteropryemius ornatis, Ag...) 2.0.5. | sec. | vale * Carcharopsis prototypus, Ag...) ...... | sss % og a OT OUSSE ee (eee Were oe eee * semiornatus. Ae etree Tevet |! epatoe |. wade * Characodus angulatus, Ag.....:.| ...... | ceeee | eeeeee * SMMEMMSMAQ EE Maras tse) cctcdw) | sevace |” estes i Cheirodus pes-rane, M‘Coy ...| ...... | +++ * | Chomatodus cinctus, Ag......... * co ea Ma * % 100 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 8, Oreton Yorkshire | Ireland and Bristol. and (chiefly | North Farlow. ; Derbyshire.}| Armagh). Britain. ——— | | | t@eeeee fF eeeeee [f e8esee Chomatodus clavatus, M‘Coy... denticulatus, M‘Coy ...... —— linearis, Ag................... — obliquus, M‘Coy............ AT UNCAES; AG eee rcewesaceis BPRih Lesasitbigs ch Sem otigs teed tee os Cladacanthus paradoxus, 4g... Cladodus acutus, Ag. ............ basalis, Ag. ..............0++ CORICUS AG ieee —— levis, M'Coy ........ccse00s —— marginatus, Ag. .........+.. enn MN CTI AG. on cnlen nts oes See ———= mirabilis, AG. ........ce-0+0- —— striatus, Ag.............-...- Climaxodus imbricatus, M‘Coy ? Coccosteus carbonarius, M‘Coy Cochliodus contoftus, 4g. ...... THAPNUS (7) AG ri vied anes Btriatus (2); Ag... ccc..0s+9< HUB swtare etn cues en see Colonodus longidens, M‘Coy .. Copodus cornutus, Ag............ Talents, AQ, cs icvenacas-me —— lunulatus, Ag............... spatulatus, dg. ............ Cosmacanthus carbonarius, MC. | Cricacathus Jonesii, Ag.......... | Ctenacanthus arcuatus, Ag...... UEVAR, AG. fist noes ae see erenulatus, Ag. ...........- — distans, M‘Coy ............ heteropyrus, Aga.o..c<.00.0- VAN OR) AG Wo den cnike sone bates - —— tenuistriatus, Ag............ e@eeeee fb ceeeee | eeetee Cesedo f' vseslace «| ‘Sanens eeoceee F seeeee | eevee aeeeew ih | weaees fh) iaeisinteie @eceee Ff jfseoeeee | easeee Seacdec i vacesie | Meveme eacces fF jecVoeese if cesses *K OK OK OK OK K kK OK eeveee fF eceesee | 80sec e@ecess Ff ceesee jf bdeevee * OK XK @eooeee jf ee206¢08 j%|F 80sec * aK Ctenopetalus serratus, Ag. ...... ee subleevis, Ag............ Deltoptvehitis acutus, Ag. ...... —— gibberulus, dg. ............ Dimyleus Woodii, Ag............ Dipriacanthus falcatus, M‘Coy Stokesii, M‘Coy............. Erismacanthus Jonesii, M‘Coy Glossodes lingua-bovis, M‘Coy —— marginatus, M‘Coy ...... Gyracanthus tuberculatus, Aq. | Harpacodus dentatus, 4g. ...... Helodus appendiculatus, ‘Coy didymus, HQ. ..s0scgienn —— gibberulus, 4g. ............ —— levissimus, Ag. ..........:. mammillaris, Ag. ......... MUGS, LM C0 oc laseaia ten subteres, Ag... .acccdexeee —— turgidus, Ag. ............0.. * feeeee ff seeeee fF ecaetee * OK ewevee Nt -dweeeee Vy) |) Vises Peete vie i Meerven Vil) Malware Weje¢ ea) fi. Cs ee ee!” (i) ealaele.d w Ceiswie es) if awiaeae © 7h) / veee ws Sm mieaeny i)” gee... th) ob ieee ele Saiaets a ep Cee mee) (athe Jee sae Sesbe TT Veeedee ici “eee ae eeuape ii sense 9 ih Cen iae Sere ie aie awe easy | il) Jo caigiag ele KK OK OK kK OK OK KOK OK KOK X Sea eRe i) | Blaiwisinie'™ 101 \. Selelewiee * * ee ee ey 8p. Holoptychius Hibbertii, 4g... Homacanthus macrodus, M' Coy ‘ ‘ . . . . ‘ ‘ . . . . . . *K 1862.] Homacanthus microdus, M‘Coy Labodus planus, 4g. ............ prototypus, Ag. ............ Leptacanthus junceus, M‘Coy... ABISCHS AIOE. «525.0 eins en. - Jenkinsoni, M‘Coy......... Mesogomphus lingua, 4g. ...... Mylacodus quadratus, 4g. ...... Onchus falcatus, Ag. .........05. hamatus, Ag. .........:0.0- — plicatus, Ag. ...........668. MOR UB ES PON = oc cincstadeeton's SMG, (AG. vi... cannes ees Oracanthus confiuens, Ag........ LTS 0 —— minor, Ag. .. .......ceeeeee pustulosus, 4g. ............ Orodus angustus, Ag. ............ -catenatus, Ag............065- emmeins, Ag.. ........cks.s6 <3: — compressus, M‘Coy......... — gibbus, Ag. ...........0.00065 porosus, M‘Coy ........... ramosus, Ag. :...:...... aba Petalodus acuminatus, Ag....... Hastingsiz, Owen .......:. —— levissimus, 4g. ...........- marginalis, Ag. ............ sagittatus, Ag................ Petalorhynchus psittacinus, Ag. Petrodus petalliformis, M/‘Coy Pinacodus gelasinus, 4g. ...... Ponoplax, Ad... .2..622:..+5: Physonemus arcuatus, M‘Coy... putetes, Ag. .2)..5..2..2.0% Platycanthus isosceles, M‘Coy Pleurogomphus auriculatus, Ag. Peecilodus aliformis, M‘Coy ... — foveolatus, M‘Coy ......... MISE TAG iin nce’ aie ¥ 2% Ooliquus, Ag. ...022.i2 6.28. Polyrhizodus pusillus, ‘Coy... apCANS, AG’... 0.0scde cas. Pristodus falcatus, Ag............ Pristicladodus dentatus, M‘Coy Psammodus Goughii, M‘Coy... UU TU ORUS AG. 52.5.2 c0tecsane-- Psephodus magnus, 4g. ......... Rhizodus ferox, Owen............ Rhymodus transversus, Ag...... Streblodus Colei, Ag. ............ —— Hgertoni, Ag. ............... oblongus, Ag. .............4: Tomodus convexus, Ag. ......... ‘Xystrodus augustus, Ag.......... —— striatus, Ag.................. Oreton and Farlow. eeotoe coseee eecece eeccce eececoe eeccce e@oceee eescne @crcee eecces @oeeas eesece sercece eoveoe eeccae ecccee eeecee wocoee eeccee ecoccee eesoee @ooecee eoceece eoccees eorece ecccee coceees eossece eeceee eccece eoceee eeccee esccee eosece eeceee eecsee eeeeee eoeses eesees eeceee serene eo e886 faeces eeeeee aeesee weeeee eseeee secon cesses Seeses Bristol. eescee ceceee ecoses eevcee @encce @ecnes eeccee eeecee eecvne eeceee e@ccoee eorceoe e@eceee e@onacae aeccee eereee enscce neces vecsoe eecoe: eeotes eooesee coetee cecnes eescece ecccoe eoecee eecece eecece eecces @ecees eescece eoceee pacces eessse erases worese sevens Oeenes senses eeeeee eeeree Oereee MORRIS AND RUBERTS—CARBONIFEROUS LIMESTONE. HX KOK XK K HK KKK mK OK 3K * KK X erceee eereee * > *K * we as *K 102 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 8, Bexiorum.—(From De Koninck.) Russia.—(From E. d’Eichwald.) Helodus levissimus, Ag. Cladodus mirabilis, 4g. Orodus ramosus, 4g. Cochliodus contortus, Aq. Psammodus porosus, 4¢. Ctenoptychius denticulatus(?), Ag. rugosus, 4g. Dicrenodus Okensis, Rom. Helodus gibberulus, 4g. leevissimus, Aq. Hybodus polyprion (?), 4g. Panderi, Hichw. GERMANY. Psammodus rugosus, 4g. Nortu America.—(Lord Enniskillen.) Psammodus porosus, 4g. (Warsaw Leptacanthus remotus, Hichw. in I]linois.) Petalodus acuminatus, 4g. Psephodus magnus, 49. Peecilodus Rossicus, Keys. Cladodus. Psammodus porosus, Ag. For revising this list, and for much assistance in correcting the names of the species examined by M. Agassiz during his last visit to England in 1859, we are greatly indebted to the Earl of Ennis- killen and Sir Philip Egerton. In explanation of the changes in many names of genera and species referred to in the Table, we have been favoured by these gentlemen with the following notes :-— Found at Is now the Cochliodus magnus ...... Bristol Pe cescns os teeea anes Tomodus convexus. Cl MAGNUS Pic ienssudsesene Armagh, Richmond, and endaley stone iteaat Psephodus magnus. COR OCUCIIS He oA cto can JAMA OLIN he ake hoa el oe ce Deltoptychius acutus. OC QCUTUS bso aslo ee IBTIStOl dae eae ten sche ace ane D. gibberulus. CS ODOR GUS a... oud einiae WAMIN SONY (fone Ae eepanastee Streblodus oblongus. COHONGUS seco invieees~ Hook Point, Co. Wexford. S. Egertoni. CN ODLONGUS Ie soics vin oso on PAGING ENT. Ss deneincetonaderar S. Colez. VATA Sy eecte c oeiele cleeat se ie Aystrodus striatus. iL ae) CRS oe tea ti uring whe acai aetna iat vd angustus. Glossodes lingua-bovis Agassiz supposes to be the front tooth of Helo dus didymus; but he has taken the specimen to America. Helodus planus is now merged into Psephodus magnus. rudis is supposed by Agassiz to be a young tooth. . Orodus ramosus occurs also in Monmouthshire. Petalodus acuminatus and P. Hastingsi@ are said to be of the same species; if so, the name must remain P. Hastingsig. The localities for this species are Richmond in Yorkshire and Ticknall in Derbyshire. It is not found at Armagh. Petalodus radicans is now Polyrhizodus radicans; and Petalodus rectus is a young tooth of the same species. Petalodus psittacinus is now Petalorhynchus psittacinus. Pecilodus sublevis » Deltodus sublevis. P. parallelus is a second tooth of the above species. P. transversus is half a tooth of Pacilodus Jonesit. Pristodus falcatus is a new genus and species from Mr. Wood’s collection. Psammodus canaliculatus is now merged into Psammodus porosus and. rugosus. Psammodus rugosus. The type-specimen of the genus is from Hskey, Co. Sligo. P. cornutus is now subdivided into the following genera and species :— Characodus angulatus ...... Armagh. Labodus prototypus ...... Armagh. CL enneatus, 4.224 ae ‘ Mesogomphus lingua...... i ‘Copodus cornutus ............ Es Mylacodus quadratus...... i, Cy fomeainaiscn: 3: teecleseaemne 3 Mylax batoides ............ 5 CO Maal ats wissen se catese ey 2h Pinacodus gelasinus ...... Js C, mppntrle ne io. <0. evoumieae PY PEON GDI AR Nt. 2 iawn de zs Dimyleus Woodii... Richmond, Yorks. Pleurogomphus auriculatus __,, Labodus planus ............... Armagh. Rhymodus transversus ... i 1862.] MORRIS AND ROBERTS—CARBONIFEROUS LIMESTONE. 103 On a New Srecrzs of Prericuruys (PrTERICHTHYS MACROCEPHALUS, Egerton), from the Yettow SanpsToneE of Fartow, Co. Santor. By Sir Purmre pE Mapas Grey Eeerrton, Bart., M.P., F.R.S., B.G.S5 ke. [Puats III. Figs. 7, 8, 9.] Tue specimen of Pterichthys discovered by Mr. Baxter, F.G.8., in the yellow sandstone of Farlow is the smallest example of the genus which has come under my notice. Its total length, from the anterior margin of the head to the termination of the dorsal shield, is exactly one inch, of which the head occupies four-tenths. ‘The breadth of the shield is half an inch. The fish reclines on the ventral plates, thus presenting to view the upper surface of the body. The tail and left pectoral appendage are deficient; but the right arm is pre- served, and measures eight-tenths of an inch in length, or two-tenths | more than the carapace. See woodcut, fig. 1, and Pl. III. fig. 7. On comparing these dimensions with those of the other members of the genus, Fig. 1.—Outline of Mr. it appears that, although the small size of §_ Bawter’s Specomen of the body suggests a resemblance to the Pterichthys macro- Pterichthys Milleri of Cromarty, yet the cephalus from Far- disproportionate length of the pectoral ap- low.) (See Pl. T1U1: pendages (a feature of safe guidance in dis- _ fig. 7.) eriminating the species) assimilates it more closely to Pterichthys hydrophilus (Pam- i es \ phractus of Agassiz) found in the yellow (\ } sandstone of Dura Den in Scotland. It & differs, however, remarkably from this se) x species in the large proportionate size of the head. The breadth of this member ba in the Farlow species is just commensurate TS with its length, whereas in Pterichthys hydrophilus it is one-third greater. The form of the head is also very different in the two species; the outline in the former is nearly circular, whereas in the latter it is subtriangular, broad at the base, and contracting towards the snout. The length of the pectoral oars in the Pterichthys of Dura Den exceeds considerably that of these organs in any other species, being equal to that of the dorsal shield; but the English Pterichthys (the only one yet discovered on this side the Border) transcends in this respect that of Dura Den as much as the latter outstrips its con- geners ; for the arms project one-fourth beyond the posterior margin of the carapace. The plates of the cranium are not sufficiently per- fect for description. I may here remark that a specimen recently acquired by the Mu- seum of Practical Geology, from the Dura Den deposits, fully bears out the opinion advanced by the late Hugh Miller and myself in 1848, as to the identity of the genera Pterichthys and Pamphractus. Since the foregoing description of the solitary specimen of Pter- 104 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 8, whthys discovered by Mr. Baxter in the Farlow sandstone was penned, the researches of Mr. Roberts have brought to light from the same locality several additional specimens of the same species, which enable me to add the description of the ventral and thoracic plates. The former specimen is still so far unique that it is the only one yet discovered which gives a view of the dorsal surface, or reveals the proportions of the head, from which the specific title was derived. One of the more recently found specimens is quite a gem. The fish reclines upon its back, and thus presents to view the ventral plates, the thoracic plates, and their appendages; the head and tail are both wanting.- See woodcut, fig. 2, and Pl. III. fig. 8 & 9. Figs. 2 & 3.—Outlines of Specimens of Pterichthys macrocephalus from Farlow. (See Pl. II. figs. 8 & 9.) a In a former paper, read before the Geological Society in April 1848 (Quart. Journ. Geol. Soc. vol. iv. p. 302), the arrangement of the plates composing the integument of this genus was so fully described that it is needless to go over that ground again. I wish, however, to correct an error in the number of the ventral plates. Two plates are there enumerated as the posterior ventral plates, lettered hh on the outline-figures, ibid. p. 305, which (as shown by Pro- fessor M‘Coy) are not independent elements of the shield, but prolongations of the posterior ventro-lateral plates. I was led into this mistake by the semblance of a suture visible on most specimens, which proved to be the impression of the posterior mar- ginal rim which encircles the inner posterior edge of the dorsal plates, but traverses the inner surface of the posterior ventro- lateral plates in the direction of the supposed suture. The im- pression of this marginal rim is distinctly preserved in the Farlow specimens (figs. 1, 2,——I), and affords a secure datum for measuring the dimensions of the plates. The antero-posterior dimensions of the dorsal surface were taken from the front of the first dorsal plate to the posterior marginal rim; a similar measurement of the ventral surface, namely from the anterior margin of the shield to the impres- sion of the posterior marginal rim, exactly coincides with the former ; the width of the body and the length of the arms also correspond so exactly that the two specimens might have been derived from the same individual. The hinder prolongations of the posterior ventro-lateral plates extend in this, as in all other species, beyond the termination of the dorsal shield. In front of the anterior ventro-lateral plates *y ve ra i ia t Vol. XVI. Pl. III. J Quart. Journ. Geal. Soc eee &S Py Jsemetric lines of the Arenaceous & Argillaceous Strata. | Shaded portion shows the Garboraferous Arew. YY RRAVss w G G44 RRA S S RQ Sy \ S YY LY LL/ F ye BS SS s \ s s TW. Lowry, foulp* 1862. | HULL—CARBONIFEROUS STRATA. 127 On the 16th heavy rains fell, the weather having been quite clear and tranquil up to that time. On a second visit made on the 23rd of December, I ascertained the number of openings, marked by minor cones with funnel-shaped craters, that had been formed on the flank of the mountain were about twelve—ranged close together on a line from E.N.E. to W.S.W. at the distance of about 600 metres S.S.E. from the old lateral crater whence the lava-stream of 1794 proceeded which had poured down on Torre del Greco. Thus it appears that a fissure had on this occasion been formed in the side of the mountain, either on the prolongation of that of 1794, or parallel and close toit. The lavas produced by the two eruptions are also almost identical in mineral character, being very poor in leucite, but rich in augite crystals. On returning to Torre del Greco, I was surprised to find the prin- cipal fountains of the town overflowing with an excessive supply of water, as in general during eruptions the springs are rather apt to fail. Bubbles of carbonic acid gas were rising abundantly from the water. Many of the cracks which had been formed by the earth- quakes in the pavement of the streets of the town were seen, it is said, to emit small flames (of carburetted hydrogen?). It is certain that the shore beneath Torre del Greco was permanently elevated by above a metre—a long white line composed of mollusks and zoophytes attached to the rock, which only live under water, being now gene- rally raised that much above the sea-level, through a space of at least two kilometres. . The cone of Vesuvius continued to smoke at intervals for several days. On the 23rd of December ashes fell abundantly in the streets of Naples—a circumstance that has not occurred since 1822. 3. On Iso-p1AMEtRIc Linzs, as means of representing the DistRIBUTION of Sepimentary Cray and Sanpy Srrata, as distinguished from CatcaREous Srrata, with special reference to the CARBONIFEROUS Rocks of Brirary. By Epwarp Hutt, B.A., F.G.S., of the Geo- logical Survey of Great Britain. [Puare VII. ] ConTENTS. I. Introduction—Comparison of Argillaceo-arenaceous with Calcareous Sedi- ments, as to their range in Modern and Ancient Seas. Recent—Caribbean Sea, &e. Past—Oolites of Oxfordshire and Yorkshire. Permian Strata of England. Lower Carboniferous Strata of Belgium and Westphalia. Nature of Calcareous Deposits. Contemporaneity of the Deposits and Oscillation of the Land. Threefold arrangement of Groups with a calcareous centre. Iso-diametric aspect of Strata, Il. Carboniferous Land-surface of Central England—Existence of an old B. and W. Barrier. 128 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 5, 1. Region North of the Barrier.—South-easterly Attenuation of the Argil- laceo-arenaceous Strata.—North-westerly Attenuation of the Calcareous Strata. Distribution of the “Sedimentary” Strata and of the Limestones of the Car- boniferous Period :— : South Staffordshire. Anglesea. Warwickshire Coal-field. Notts, Derbyshire, and Yorkshire. Leicestershire Coal-field. Lancashire. North Staffordshire. Cumberland. Flintshire and Derbyshire. Scotiand. 2. Region South of the Barrier.—Easterly Attenuation of the Argillaceo-arena- ceous Strata.—Westerly Attenuation of the Calcareous Strata. 3. North Atlantic Continent.—Northerly Drift of Sediment during the Car- boniferous and Mesozoic times. ITI. Summary of Conclusions. [Note-—In the following pages the term “Sedimentary” is used to denote exclusively such inorganic strata as sandstones, clay, shales, &c., in opposition to Calcareous strata or limestones. | § 1.—Jntroduction.—A large and interesting field of inquiry is open to us in comparisons of the relative distribution of the calea- reous and the truly sedimentary members of different geological formations. We have, as it appears to me, been too much in the habit of classing limestones (whether coralline, crinoidal, shelly, or oolitic) as strictly sedimentary ; yet it will be found, by such comparisons as those alluded to, that the relation which is borne by sandstones and shales to limestones is one, not of similarity, but of contrast. In other words, that where we have a group of strata, as, for example, the Lower Carboniferous, composed partly of ‘“ sedi- mentary” and partly of calcareous members, it will generally be found that the one series is complemental of the other, and developed from opposite directions. This arises from the differences in the origin of the two classes of stratified rocks, the calcareous being essentially organic, and the “sedimentary ” essentially mechanical ; so that where the forces and agencies tending to the accumulation of the latter are in active operation, these very forces and agencies are in direct antagonism to the other, and, as a result, calcareous strata are either not formed or only sparingly*. (a.) Of these two ever-acting principles we have numerous ex- amples both in recent and in geologic periods. If we take as an illus- tration the Gulf of Mexico and the West Indian Islands, we find the sediment brought down by the Mississippi forming deposits of sand and clay which are spread along the coast and far out to sea by the Gulf-stream, while around the West Indian Islands coralline * That limestones are either directly or indirectly the production of animals is now so generally admitted that it seems scarcely necessary to cite authorities. Bischof in his work on Chemical Geology (vol. iii. p. 35) says, “So long as the formation of mechanical deposits was predominant, the organic action of the marine animals that separate limestone, or at least that of the corals, could not be exercised.” This passage (which did not come under my notice until these pages had been brought before the Geological Society) fully bears out the prin- ciple of opposition between the origin of the two classes of rocks, which I am now endeavouring to illustrate. See also Lieut. Nelson’s ‘Account of the Ber- muda Cora!-formations,’ Trans. Geol. Soc. 2nd series, vol. v. 1862. | HULL—CARBONIFEROUS STRATA. 129 limestones are being accumulated in a clear ocean*. If we take the North Atlantic, we find reason for believing, on the evidence of the deep-sea soundings, that the central area is composed of a fine cal- careous mud‘, the production of Foraminifera and other marine ani- mals, while along the shores of the American continent and those of Europe deposits of sand, gravel, and clay are in course of accumu- lation. If these regions were elevated into land, we should probably : find a formation composed in one direction of limestone, like chalk, and in the other of sandstones and shales, both classes of material being developed from opposite areas of dispersion. Indeed, the representative positions of the pelagic and littoral for- mations—the one calcareous, the other sedimentary—are very clearly stated by Sir C. Lyell, who sayst, “It has been ascertained by sound- ings in all parts of the world, that where new deposits are taking place in the sea, coarse sand and small pebbles commonly occur near the shore, while further from land and in deeper water finer sand and broken shells are spread over the bottom ; still further out, the finest mud and ooze are alone met with. Mr. Austen observes that this is the rule in every part of the English Channel.” I think, how- ever, that experience will bear us still further than this, and that we may regard the predominance of sedimentary strata as highly unfavourable to the development of calcareous, in the same group of rocks. (6.) The same general principle is in force over our globe at the present day, and probably has been from the times when calcareous strata, which are the representatives of marine life, first began to be formed. Wherever large rivers pour sediment into the ocean, or where currents take up and distribute this sediment over the sea-bed, there limestones will be very sparingly formed. On the other hand, where, from certain causes, such as the great distance from land, or the absence of such rivers and currents, the water of the sea is clear and free from mud within the temperate or tropical regions, there calca- reous matter will be accumulated. Of the strata at present forming, the great calcareous members are to be found occupying principally mid-oceanic regions, and their representative sedimentary members range themselves in the direction of the coasts. Still there may be frequent cases where the limestones may be formed along the coasts of large tracts of land, as on the shores of Australia and Southern India, but in every such case there is an absence or scarcity of sandy or muddy sediment§. Reverting to geologic periods, I have no wish here to repeat what has been frequently shown by Lyell, Darwin, Phillips, Godwin-Austen, and other writers, that calcareous forma- * For this illustration I am indebted to my friend Dr. J. Hector, lately Surgeon and Geologist to the exploring expedition under Capt. Palliser. t Capt. Maury’s ‘ Physical Geography of the Sea.’ A very interesting account of these soundings has been published by Dr. Wallich for private distribution. { ‘Principles of Geology,’ 8th edit. p. 770. § On this point Ehrenberg states “that he never saw corals grow where the sea was frequently rendered turbid by shifting sand, but on!y where it was clear and pure.” —Poggendorff’s Annalen. The same fact is stated by Mr. Jukes, Mr. Darwin, and other writers. VOL, XVIII.—PART I, K 130 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, tions of one region are represented by shales and sandstones in another; but the point I wish to urge particularly is that such con- temporaneous strata are necessarily developed from opposite direc- tions, and that the region over which one of these classes of strata is most fully represented is that in which the other has been most sparingly deposited. Thus the White Chalk of Europe is replaced “by sandstones, shales, and lignite in America®, in which there is very little calcareous matter. We may therefore believe that a clear ocean, uncontaminated by muddy sediment, overspread the greater part of Europe, while the waters of North America were charged with sedi- ment. The cause of the change of mineral character is here sufficiently evident. The animals which flourished in the clear waters of Europe, and by whose vital powers the soluble calcareous matter was con- verted into chalk, were incapable of living where the sea was turgid. In this case the animals were Corals, Sponges, Bryozoa, Cytheride, and Foraminifera. (c.) Confining our view to narrower limits, let us take for another illustration the Great Oolite as it occurs in Oxfordshire and on the east coast of Yorkshire. In Oxfordshire the most conspicuous member is the “ White Limestone” (not unlike hardened chalk), interposed between the Stonesfield Slate series} and the Forest-marble. The White Limestone is generally very free from any admixture of sand or clay, and is essentially organic in its composition. On the other hand, the Forest-marble and Stonestield Slate contain a large admix- ture of sedimentary ingredients ; but neither of them is as thick as the White Limestone. Yet, when traced to the coast-section of Scar- borough, a great change is found to have taken place in the relative development of these three members of the Great Oolite. The lowest and highest members have expanded by an accession of sedi- mentary materials. They are (as it seems to me) the “lower” and ‘‘upper sandstone and shale series,’ stated by Prof. Phillips to be 700 feet in thickness (but possibly more), while the central calea- reous member has become so thin and debased as to be scarcely re- cognizable. (d.) We may also instance the Permian Rocks of England. Thus we find the calcareous members attaining their maximum development of 500 feet according to Prof. Sedgwick, or 600 feet according to Mr. Kirkby, in Durham, dwindling to 440 feet in South Yorkshire; and when last exposed towards Nottingham, showing evident symptoms of debasement. Over these districts the Lower Permian strata are but sparingly represented, but as we proceed south-westward are found gradually to augment, tillin Warwickshire and Salop they attain their full thickness of 1500 or 2000 feet, the whole of which is formed of sandstones, shales, breccias, and conglomerates. It will be observed that the points of maximum development of the calcareous and sedi- * Lyell’s Manual of Elem. Geol., 5th edit. p. 255; Dr. Hector, Quart. Journ. Geol. Soc. vol. xvii. p. 412, &e. t In the Memoirs of the Geological Survey, 1858, the White Limestone is called ‘“‘the Upper Zone,” and the Stonesfield Slate “the Lower Zone” of the Great Oolite. ; | 1862. | HULI-——CARBONIFEROUS STRATA. 131 mentary elements are situated at opposite extremities of the area occupied by the Permian group. Fig. 1.—Comparative Sections in Oxfordshire and Yorkshire, showing the Changes in the Sedumentary and Calcarcous Members of the Great Oolhite, when traced from South to North. Scarborough. ' =----=---* li: ee DE eee ae Oxfordshire. pe ae Ss 1 Beit = . 3225 seas ee eM ere 3 t “heli Nala aE se eon EEE 8 —— sence een 1. Cornbrash. =1. Cornbrash. 2. Forest-marble. =2. Upper Sandstone and Shale. 3. eee aan or Upper Zone of camel lig Mt ate Oe 4. Stonesfield Slate, or Lower Zone. =4. Lower Sandstone and Shale. (e.) To take another example of development, from opposite direc- tions, of calcareous and sedimentary strata, we may select the Lower Carboniferous Rocks of Belgium and Westphalia, which present phe- nomena analogous to those of the same formations in our own country. In Belgium the Coal-measures rest upon a thin floor of sandstone representing the Millstone-grit. Below this is the Carboniferous Limestone in great thickness, which in turn rests on a thin series of shales. On tracing these strata north-eastward towards the vla- ley of the Rhine, they are found to undergo marked changes in their development, as shown by Sir R. Murchison and Prof. Sedgwickt. The limestone thins away, while the grits and shales proportionably expand. Thus it is found that the series which underlies the Coal- measures of Westphalia resembles the Lower Carboniferous series of Scotland, consisting of sandstones (Flotz-leerer Sandstein) and shales with Posidonomya Becheri, the limestone itself having disappeared*. These changes I consider to be intimately connected with those under- gone by the same formations in Britain, and to be due to the same general cause, namely, the northerly drift of sediment during the Carboniferous Period. Similar illustrations might be multiplied, did space permit; but, without here entering further into the general principle, I will merely state my belief that a comparison of the relative distribution of the calcareous as distinguished from the argillo-arenaceous, or sedimentary, strata of the Carboniferous, Devonian, and Upper Silu- rian formations would show, as a general rule, that the regions of maximum development of the one series are those of minimum de- * “Siluria” 2nd edit. p. 427. + Although there is a marked unconformity between the Lower and the Upper Carboniferous Rocks of Westphalia, I do not consider it, of itself, sufficient to account for the interchange of development between the arenaced-argillaceous and the calcareous strata. K 2 132 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, velopment of the other, and, consequently, that the relationship of the two classes of rocks is complemental. Fig. 2.—Section of the Carboniferous Rocks of Belgium and West- phalia, showing the augmentation rm the thickness of the “ Sedimen- tary’ Strata, and the simultaneous thinning-out of the Carboni- ferous Limestone towards the North-east. S.W. Belgium. The Rhine. Westphalia. N.E. a md oS MM SEES 1. Coal-measures. 2. Millstone-grit (Flotz-leerer Sandstein). 3. Carboniferous Limestone (absent in Westphalia). 4. Lower Shales, expanding in Westphalia. * Devonian Schists, &c. at the base of the Carboniferous Rocks. (f.) Ihave already hinted at the cause of this inherent distinction, but it may be as well to state it in more precise language. As lime- stones are by universal consent allowed to have resulted from the exuvie of living animals, they will be accumulated in greatest quantity wherever the conditions of life are most favourable. Now, the fact that limestones, when they occur in considerable thick- ness, are generally pure, and free from foreign matter, shows that one of the first requisites for liimestone-making animals is that they should inhabit waters free from mud or sand. Where the White Chalk is in greatest thickness, it is pure; the same is the case with the Oolite limestones, and with the Carboniferous Limestone of Derby- shire which is of enormous thickness and contains very few beds of shale ; but whenever these massive calcareous rocks begin to be split up by the admixture of shales or sandstones, they become im- poverished in mineral character and diminished in thickness*. The formations in which these phenomena. occur show us that the Mol- lusca are to some degree independent of such changes, as the remains of animals of this:class are often abundant in sandy and muddy deposits containing small quantities of lime; but, as a general state- ment, it may be affirmed that clear and unpolluted water was essen- tial to the full development of those delicately organized animals, the Foraminifera, Zoophyta, Polyzoa, and Crinoidea, which are, and have ever been, the most efficient elaborators of limestone rocks. It is almost superfluous to observe, that, in speaking of the neces- sity of pure water to the full development of the marine animals above named, carbonate of lime in solution is not understood as a source of impurity. This mineral must necessarily be present as the material from which the Zoophytes and other animals construct their * The limestones of the Culm of Devonshire, as compared with their repre- sentatives at Bristol, are illustrations of this principle. At Bristol, where it occurs in great force, the ‘limestone is pure and crystalline; but in Devonshire, where black shales are largely distributed amongst the beds of limestone, these latter are frequently of so poor a quality that ‘‘even in the richer portions there. is seldom more than a third or fourth part which is actually burnt for lime.” See Memoir of Sedgwick and Murchison, in Geol. Trans. 2nd ser. vol..v. p. 674 1862.]. | -HULL—CARBONIFEROUS STRATA, _/. 133 stony skeletons and habitations. Carbonate of lime, however, when — dissolved by the agency of free carbonic-acid gas, does not interfere with the transparency of the water ; and this transparency is the all- important condition to the organic growth of limestones. And not- withstanding that the amount of carbonate of lime in solution in the mid-ocean is often extremely minute, yet its solubility enables it to be carried to all parts of the ocean where no particle of sand or clay ean reach ; and thus it may be possible that all sedimentary forma- tions have had their contemporary calcareous representatives at some one or more parts of the globe. (g.) There is one objection which may be urged against this view of the relations of true sedimentary and the calcareous strata. In the cases just cited of the Carboniferous Rocks of Belgium and West- phalia, and of the Great Oolite of our own country, the development of the sandstones and shales from the one direction, and of the lime- stones from the opposite, are not strictly contemporaneous. Thus the lower and upper sandstone and shale of the Great Oolite, which are thickest in the North, are earlier and later than the “ white lime- stone,” which is most highly developed in the South. This, however, arises from the very slow progress of those changes in the character. of the land and sea which have conduced to the differences of the strata formed in each district. While the lower series of sandstones and shales were being formed over the Yorkshire area, the sea-bed _was gradually preparing for the future development of calcareous strata over the Oxfordshire area ; and while limestones were forming under Oxfordshire, the sea of Yorkshire was still sufficiently charged with sand and mud to prevent their full development in that quarter. Another change occurred: the Yorkshire sea again became charged with sand and mud, which so far extended its influence to Oxford- shire as to check the formation of pure limestone. In this instance, as in others, there was a series of oscillations as the two agencies alternately predominated ; but, while each in turn obtained the ascendency, the influence of the other never entirely ceased within certain limits. Thus, while sandstones and shales were accumulating in Yorkshire, sandy limestones and calcareous shales were forming in Oxfordshire, as the influence of the calcareous element was always more or less in force in the southern direction, when it was entirely overpowered by the ascendency of the sedi- mentary element in the north. And if we adopt the conclusion of Bischof, that it is impossible for any carbonate of lime to be preci- pitated at the bottom of the open sea by chemical action, but only by the intervention of organized beings, we must allow that these agencies, by whatever terms they may be designated, are not mere figures of speech, but real and ever-acting forces of nature. It is difficult to represent by means of a diagram what is here discussed ; but perhaps fig. 3, representing the Great Oolite of Yorkshire and Oxfordshire, may assist in rendering my meaning more clear*. (See also fig. 1, p. 131.) * T am aware that Dr. Wright, than whom there is no better authority, calls in question, on palzontological evidence, the parallelism here stated, which is, I 134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, Fig. 3.—Showing the Distribution of the Caleareous and “ Sedimen- tary” Strata of the Great Oolite. North Yorkshire. Bouton , ie Oxfordshire. AND paiisions t SAWOY T7 MEST ONE ¥ LIMESTONE and shale. § >» Regarding, then, the calcareous strata as differing in their origin and in their mode of distribution from the other stratified rocks with which they are associated, it appears to me that it is incorrect to class them together under the same term of “‘ sedimentary.” I there- fore prepose to eliminate the limestones from this category, and to place them as a distinct class of rocks, confining the term “sedi- mentary” to gravels, sandstones, shales, and clays, with their vari- ations. The presence of each class of rock in the same geological group is no argument in favour of their similarity. Whenever inter- stratifications occur, they may be regarded as occupying the neu- tral ground between their respective areas of dispersion ; and I have little doubt, could it be possible to trace the sources of the “sedi- mentary ” strata of any formation on the one hand, and of the lime- stones on the other, they would be found expanding in opposite di- rections, and, as it were, originating at opposite poles. The relation- ship here contended for will be rendered more clear in the case of the British Carboniferous Rocks by the iso-diametric lines presently to be described. (h.) Cause of the frequent occurrence of a Threefold Arrangement in Groups of Rocks, with a central Calcareous Member.—We cannot fail to have observed that many groups havea tendency to arrange them- selves into threefold divisions, the upper and lower being composed of sands or clays, the middle of limestone. This has been remarked as the result of his observations on the continent by Sir R. Murchi- son, and we have many examples in this country. Thus in the Upper Silurian Rocks there is a calcareous centre. ‘This is also the case in the Devonian group of Devon and Cornwall; in the Carboni- ferous, the Permian, the Triassic (when complete), and the Jurassic Rocks. Phenomena of so general a character cannot be accidental, but must be in accordance with the system of nature. May not the fol- lowing be the true explanation ? believe, in accordance with the order of succession determined by Prof. Phillips. Notwithstanding, however, the existence in the Scarborough Limestone of an Ammonite which is characteristic of the Inferior Oolite in Gloucestershire, I am strongly inclined to believe, on stratigraphical grounds, that there has been a “migration” of species; and that this is a case where identity of fossil remains does ot prove that the strata are contemporaneous, In either case, however, — the illustration is of equal value for my purpose. Limestone. 1862. | HULL—OCARBONIFEROUS STRATA, 135 We may consider a group of rocks as primarily representing three periods: the first of movement, the second of quiescence, the third of movement again. We have already seen that the formation of calcareous strata depends mainly on the absence of sandy or muddy matter in the sea, which we may believe would be most likely to occur during a long period of repose from oscillations of land, as every movement of that kind would tend to increase the quantity of sediment poured into the sea. Hence we have the following paral- lelism in the three stages :— Upper stage presenting movement resulting in sedimentary strata. Middle stage - quiescence ‘i calcareous strata. Lower stage “A movement i sedimentary strata. The movements of the introductory stage have generally been more powerful than those of the closing stage ; and thus, while we seldom or never find a Geological Epoch introduced with the forma- tion of limestones, we sometimes find limestones maintaining their position to the close, as in the case of the Clymenia-limestone of the Upper Devonian of the Rhine, and in the Upper Silurian Group of North America. The earliest stage is generally formed of sandstones and conglomerates, representing those physical changes which intro- duced the new epoch. (i.) Iso-diametric Iines.—We may regard all formations composed of sedimentary materials as exhibiting in cross-section a figure in- cluded by the arc of a curve and its chord (fig. 4). The end of the figure which tapers the more rapidly will represent the shore, the other the sea-deep ; and the form of the figure will be variously mo- dified by circumstances. The thickest or deepest portion will be not at the centre, but between the centre and the shore. Fig. 4.—Diagram representing the Primary Section of a Formation. Shore. e ad c Sea-surface. The Deep. 20 50 L0 30 Now, if we divide this figure by a series of lines (A, B, C, &c., and a, b, c, &c.), each decreasing by the same amount, and trace these lines over the region occupied by the formation, each will be a sort of stratigraphical contour; but, instead of representing equal altitudes, will show equal thicknesses. As such, these lines should properly be called iso-picthic; but this word is so difficult of pro- nunciation that I prefer the term iso-diametric, or simply isometric. Such lines are not intended to show the present or actual thickness of the strata, which may have been in part denuded, but the orginal development before denudation, and may thus be traced over areas where the whole has been swept away. In tracing out such lines, it is necessary to make accurate comparisons of sections scattered over the entire area, and of the original thickness of the strata which 136 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, are either partially or altogether denuded, estimated upon certain definite principles. Of such principles the development of calcareous and ‘ sedimentary”’ strata from opposite directions is one of the most important. It will be perceived that isometric lines may be used in repre- senting the thickness of an individual stratum, as well as of forma- tions, groups, or systems; and the chief point to be attended to in tracing them is that the caleareous elements be eliminated from the “* sedimentary.” In the case of ‘‘ sedimentary ” strata, a series of isometric lines, each representing an equal increase or diminution in thickness, will become nearer or wider apart as they approach or recede from the centre of maximum development. In the case of calcareous formations, the focus or centre of maxi- mum development will be at opposite points to that of the “ sedi- mentary” in the same group or system of rocks, and the isometric curves will intersect, gradually diminishing in force from their re- spective centres, just as a series of waves propagated from two centres of disturbance cross each other and gradually die away in opposite directions. (See Map, Pl. VII.) § IL. Carboniferous Land-surface of Central England.—Having, thus explained the nature of isometric lines, we proceed to consider their application to the Carboniferous Rocks of Britain. I believe. they will be found of essential service in bringing clearly and intel- ligibly before the eye several phenomena connected with the distri- bution of the sedimentary as compared with the calcareous portions of this group. It is necessary that a few words should be said in reference to a. point of interest in the physical geology of our island, which should be clearly understood before treating of the distribution of the Car- boniferous strata. I refer to the existence of a barrier of land which there are grounds for supposing to have stretched from Wales eastward, skirting the southern ends of the South Staffordshire and Warwickshire Coal-fields, and including the Cambrian Rocks of Charnwood Forest. The evidences for the existence of this land- surface I cannot here stop to point out in detail, having already done so elsewhere * ; suffice it to say that they are numerous and satis- factory, both on general physical grounds and from phenomena ob- served in the mines of the coal-fields on approaching its borders. This barrier (which possibly was an extension of the Scandinavian promontory on the one hand, as very clearly indicated by Mr. God- win-Austen, and thence stretched across the Irish Sea to embrace the Cambro-Silurian districts of Wicklow and Carlow on the other) divided the Carboniferous Rocks of South Wales, Somersetshire, and Dean Forest from the coal-tracts of Central and Northern England and Scotland (see Map); and, as we shall see, the strata on each side belong to two distinct systems of distribution, and are due to two different sets of oceanic currents. * «The Coal-fields of Great Britain,’ 2nd edit. p. 246 e¢ seq. 1862.] HULL—CARBONIFEROUS STRATA. 137 1. Reeron Norrs oF THE BARRIER. (a.) South-easterly attenuation of the <‘Sedumentary” Strata ; North-westerly attenuation of the Calcareous Strata—If we take a series of vertical sections of the various sandstones, grits, and shales of the Carboniferous Period, from the midland counties of Lei- cester, Warwick, and South Stafford, then through the adjoining districts to the north, and ultimately into Scotland, we shall find a constant accession of material along this course. Thus, I find that the increase from Leicestershire to Lancashire, along a line running north-west, is no less than 8000 feet of strata in a horizontal distance of 65 miles, which gives a slope of 1 in 43, or about 1° 30’, as the angle of increment of sediment in this distance ; the maximum thickness of the strata in Lancashire being 12,000 feet, and in Leicestershire 4000 feet. Tf, on the other hand, we make a similar series of sections of the limestones, from Derbyshire as a centre, either west, north-west, or north, we shall find that these calcareous strata constantly di- minish in thickness in these directions. In other words, the lme- stones become thin as the sandstones and shales become thick. We may thus regard Derbyshire as a focus of activity from whence the calcareous elements have been propagated with constantly diminishing intensity, at least in the directions here stated. What- ever be the extreme thickness of the Derbyshire limestone, it is apparently not less than 5000 feet, as determined by several mea- sured sections of the Geological Survey,—a bulk of calcareous matter truly astonishing when we regard it in its true aspect as the work of marine animals. Nowhere else in Britain does the formation attain such vertical dimensions ; but they may possibly be less than those which it reaches in the Rocky Mountains and elsewhere. Traced northwards into Northumberland and Scotland, the lime- stones, as is now well known, dwindle down in thickness as they become more and more mixed with transported sediment, and in Lancashire appear on the point of expiring. Traced southwards, the limestone ends against the shelving shore of the old land-surface of the barrier, as at Charnworth Forest (fig. 5) ; Fig. 5.—Section of the Carboniferous and Triassic Strata lying on the edge of the Cambrian Rocks of Charnwood Forest. Charnwood Forest. Grace Dieu. Be Ry A 22 SMe » a 3 ! - VY Vi ye Ps Me a Mh 1. Triassic Breccia. 3. Carboniferous Limestone. 2. Carboniferous Limestone-shale. 4, Cambrian slate and porphyry. or is altogether absent, as in South Staffordshire*, on account of this district having been above the sea, as shown by Mr. Jukes t. * Murchison, Proc. Geol. Soc. vol. ii. p- 407. + ‘Memoir on the South Staffordshire Coalfield,’ 2nd edit. 138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, From this old land, however, little or no sediment was given off, as the limestone attains a very great thickness, and is pure dolomite at a short distance from the present site of the Cambrian rocks *. Over Derbyshire the sea must have been remarkably clear ; but it became more muddy northward, till in Scotland the sediment was so abun- dant as to extinguish life in the Crinoids and Corals, by whose labours the limestone was formed. Hence we have a clear proof that the sources of the sediment were mm the north, In Yorkshire these variations in the relative distribution of the caleareous and non-calcareous strata of this group have long since been pointed out by Prof. Phillips. In a diagram appended to ‘The Geology of Yorkshire’ these variations are represented by an in~ genious design, “and prove,” as the author remarks, “that the agencies which resulted in the formation of the limestone acted with greatest effect from the south-east, while those which resulted in the deposition of sandstones and shales acted with greatest effect from the north-west.” _ He then proceeds to trace the range of the Lower Scar-limestone, showing that towards the south-east of its course between Ribbles- dale and Wharfdale it is 1000 feet in thickness. Northward at Pen-y-ghent itis about 600feet; at Kirkby Stephen even less. North of the line from Kettlewell to Bar Fellit becomes split up by beds of shale, grit, and coal, which continually augment northwards, until at length it assumes all the characters of the Lower Carboniferous group of Scotland. He then shows that the Yoredale series increases in thickness towards the north-west (that is, in the direction along which the limestone becomes attenuated), attaining at Bar Fell 1000 feet or more, and dwindling down to 300 feet under Great Whernside. These passages describe changes in the Lower Carboniferous series of Yorkshire, which are applicable on a much wider stage to Eng- land and Scotland, from the edge of the barrier northwards. Had Prof. Phillips extended his observations, and followed out the train of thought upon which he had entered, I can well understand what a fund of illustration and force of reasoning this subject would have received at his hands. The thickness of the Carboniferous Limestone over every part of Britain is indicated by the isometric lines on the Map. These thick- nesses have been obtained from the carefully measured sections of the Geological Survey—so far as it has extended,—and from the published works of various authors on the northern districts of Eng- land and in Scotland: the following are a few special instances. Thus, the thickness of the limestone in Coalbrook-Dale is 50 to 100 feet; in Denbighshire, 1000 to 1500 feet; in Flintshire, 1000 to 1500 feet; Anglesea, 360 feet; south side of the Lake District, 1500 feet ; Scottish Borders, 500 feet ; the Lothians, 162*feet; and Lanarkshire, less. In Fifeshire it is sometimes on the point of ex- pining. | * At Breedon Cloud, where its thickness is upwards of 1000 feet, with few or no bands of shale. 1862. | HULL—CARBONIFEROUS STRATA. 139 (6.) Distribution of the “Sedimentary” Strata of the Carboniferous Period.—The isometric lines on the Map will indicate better than any description the development of the grits, sandstones, and shales, from the north towards the south, collected from the most reliable sources. We shall commence with South Staffordshire. South Staffordshire.—As is well known, the Lower Carboniferous Rocks, including the Millstone-grit, are absent here, for the same reason that the limestone is absent, namely, that this was a district of land forming a portion of the northern side of the barrier at this period. As the land became submerged during the Coal-period, the sea gradually encroached, and spread the Coal-measures as far south us the Lickey. Notwithstanding the uneven nature of the Silurian sea-bottom on which the Coal-measures were spread, we feel certain that near Dudley there exists the full series of the Coal-formation, as proved by the fossil shells from the ironstones, which are iden- tical with those from the Lower Coal-measures of Coalbrook-Dale and Lancashire*. Here the combined thickness of the lower, middle, and upper Coal-measures (as determined by Mr. Jukes) is 1810 feet, which becomes considerably expanded north of Wolver- hampton. ‘This northerly expansion is remarkably exemplified in the case of the “ thick coal” of Dudley, which, forming at that place ° one solid seam 10 yards in thickness, becomes split up into nine distinct seams by the intercalation of 420 feet of strata over the northern area of the coal-field. In the Warwickshire Coal-field we find the Coal-series attaining, according to Mr. Howell?+, a combined thickness of 2950 feet, in addition to which the Millstone-grit and Limestone-shale is 500 feet. The main coal here also presents an example of the thinning of the strata towards the south; for, at the north side of the field, this seam is split into five beds by the intervention of 120 feet of strata. In the Leicestershire Coal-field, the Coal-series attains a thick- ness of about 2500 feet, while the Millstone-grit and Limestone-shale never exceeds 150 feet. The ‘‘ main coal” of Moira offers another illustration in addition to those mentioned above of southerly at- tenuation +. The three coal-fields of South Staffordshire, Warwickshire, and Leicestershire, presenting, as they do, a somewhat similar develop- ment of sedimentary strata, lie in the direction of the same series of isometric lines, and are to be compared with the coal-fields of North Staffordshire, Notts, and Derbyshire, immediately to the north of them. North Staffordshire.—The development of the strata in this coal- field, as compared with that in any of the three just described, is * The following are some of these, determined by Mr. Salter :—Discina nitida, Producta scabricula, Lingula elliptica——Mr. Jukes’s Memoir, 2nd edit. p. 27. The presence of these Lower Coal-measures is distinctly stated by Sir R. Mur- chison in his original description of this coal-field (Proc. Geol. Soe. vol. ii. p. 407). t ‘Memoir on the Warwickshire Coal-field,’”? Mem. Geol. Surv. 1859, ¢ Memoir by the Author, “ On the Geology of Ashby-de-la-Zouch,” &c., Mem. Geol. Surv. 1860. 140 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, great indeed. The three divisions of the Coal-measures attain a thickness of 6000 feet, in addition to which the Millstone-grit and Yoredale series are about 4000 feet, forming in all 10,000 feet of sedimentary strata, which is an increase of 6550 feet over the War- wickshire coal-field. The Carboniferous sands and clays appear to have been poured in greatest quantity along a tract of country running south-eastward through this district, causing the isometric lines to make a southerly bend when crossing it, and entitle this tract to be called “ the line of maximum accumulation ” *. Flintshire and Derbyshire.—The development of both the calea- reous and ‘sedimentary ” elements in these counties are probably nearly similar. The combined thickness of the upper, middle, and lower Coal-measures reaches 3000 feet ; and the Millstone-grit series from 800 to 1000; in all 3800 or 4000 feet. The Carboniferous Lime- stone varies from 1000 to 1500 feet +. Anglesea.—The thickness of the Carboniferous series in Anglesea (as determined by Prof. Ramsay) is as follows :—Coal-measures, 1300 feet; Millstone-grit, 200 feet ; Carboniferous Limestone (con- taining some beds of sandstone and shale), 450 feet +: separating the two elements we may say for the ‘“sedimentary,’”’ 1600 feet ; for the calcareous, 360 feet. The whole series, however, is not pre- sent, as the little coal-field has suffered from denudation, for which allowance must be made. Notts, Derbyshire, and Yorkshire.—Crossing the limestone anti- clinal into Derbyshire, we find the thickness of the strata in the neigh- bourhood of Alfreton as follows :—lower (or Gannister series), middle and upper measures, 3500 feet; Millstone-grit and Yoredale series, 600 feet ; in all 4100 feet. As we do not, however, throughout the whole of this great coal-field reach the top of the Carboniferous rocks, which haye either been denuded or are hidden beneath the Magnesian Limestone, several hundred feet ought to be added to the above, making the total thickness about 4500 feet, as compared with 2600 feet in Leicestershire. The thickness of these strata augments, though not rapidly, along their extension into Yorkshire. The development of the series in Durham varies from 3500 to 4000 feet. Lancashire.—In this county there is a greater development of Carboniferous sedimentary strata than in any district in England. The upper Coal-series of Manchester is 2000 feet in thickness ; the middle, 3200 feet ; and the lower, 2000 feet; the thickness of the Millstone-grit series is unascertained, but is at least 3000 feet ; and the Yoredale Rocks, 2000 feet ; in all 12,200 feet. This thickness is * T may here explain that it appears probable that the barrier of land was broken through to the south of Warwickshire, allowing the northern current, which brought the sediment, to escape through the opening. (See Map.) On this hypothesis we can explain the enormous accumulation of sediment along this line. The thicknesses of the strata are taken from several sections made by the Geological Survey. ; t These thicknesses are taken from the horizontal section by the Geological Survey. { Horizontal Sections, Sheet 40, with description. 1862. | HULL—CARBONIFEROUS STRATA. 141 greater than that of North Staffordshire by 2200 feet, and of War- wickshire by 8750 feet*. | 7 Cumberland.—It might have been expected, according to the principle of north-westerly expansion which I am now endeavouring to explain, that the sedimentary series of Cumberland should be even thicker than that of Lancashire, lying, as it does, to the north of this latter county. This, however, is not the case; and to account for the meagre development of the Carboniferous rocks there appeared to me for some time extremely difficult. I feel confident, however, it is only an apparent anomaly, and is capable of explanation. The proximity of the Cumbrian Mountains is evidently the primary cause of the thinness of the strata; and my friend, Mr. Salter, has sug- gested to me that a shallow sea and a shelving shore are sufficient to account for these phenomena. There is at least another explana- tion, and that is, that the Cumbrian Mountains having been islands in the Carboniferous sea, and rising in front of the current which brought the sediment, caused it to bend from its course, and by in- ereasing the velocity, prevented the deposition of the full supply near their coasts. Either of these explanations appears sufficient. Scotland.—From the position of the Carboniferous rocks which occupy the great depression between the Firths of Forth and Clyde, as compared with their representatives south of the border, and from the substitution of stratified shales, sandstones, &c., for lime- stones in the lower portion, it seems probable that, when the whole series was originally deposited, the sedimentary portion attained a development unsurpassed in any other district in Britain. In reality, however, we have no means of judging of the thickness of the Upper Coal-series, as it is incomplete, a vast quantity of strata having probably been removed by denudation from off the present coal-areas. The highest member of the Carboniferous series is the “ Flat- coal Group,” representing (as shown by Messrs. Howell and Geikie) a portion of the true Coal-measures of England, as being more recent than the Roslyn sandstones, the equivalent of the Millstone-grit*t. The thickness of this division is 1000 feet in the Lothians, and 840 feet in Lanarkshire, according to Mr. Ralph Mooret. The “ Flat- coal Group ” would appear from the fossil shells, which consist of various species of Anthracosia, to be the equivalent of the Middle Coal-series of England; and we have hitherto looked in vain for representatives of the Lower Coal-measures, or Gannister Beds, with their peculiar Lower Carboniferous Mollusca. The Millstone series is then, compared with that of Lancashire or Staffordshire, only 1500 feet, as is also the case with, the “‘ Edge-coal Group,” while the sedimentary strata of the Carboniferous Limestone have enor- mously expanded. It thus appears that there has been an increase * Most of these thicknesses have been determined by Mr. Binney, F.R.S., with the exception of the Millstone-grit and Yoredale series, which were partly mea- sured by myself. (See Mr. Binney’s papers in Trans. Geol. Soc. of Manchester, vol. i. t+ “ Memoir on the Geology of Edinburgh,” p. 105. 1861. + “Vertical Section,” 142 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 5, of sediment in the lower portion, and a decrease in the upper, as compared with the northern districts of England. — The following seems to be the corresponding series in both countries: Carboniferous Serves of England and Scotland. England (Lancashire). Scotland (Lothians). Feet. Feet. 1. Upper Coal-measures ......... 2,000 1. (Lost by denudation?) ...... — 2. Middle Coal-measures ...... 3,200 2. (Partially denuded ?) ......... 10006 3. Lower Coal-measures ......... 2,000 3. (Supposed to be absent) ...... — 4, Millstone-grit ...........:00.060 3,000 4. Roslyn Sandstone Group ... 1500 5. Yoredale Rocks .............+. 2,000 5. Edge-coal Group............... 900 6. Limestone (no “sedimentary” 6. Lower Carboniferous series KERHD)! tes coccen ee. quehe done 2,000 (shales and sandstones, 3000 ——— with little limestone) ... Total “sedimentary” strata... 12,200 Total ‘“ sedimentary” strata... 6400 It will thus be observed that, even allowing 2000 feet for the upper portion of the Scotch series, lost by denudation, the amount of “« sedimentary ” strata in Scotland could not reach that of Lancashire, notwithstanding the accession it receives in the horizon of the Car- boniferous Limestone. Future investigation will probably result in adding considerably to the thickness of strata, and in throwing some light on the equivalents of the Gannister Beds, which in the north of England form a most interesting and important group of strata*. Two other suppositions, however, may be advanced, one of which is that we have here a case of compensation not unfrequently to be observed ; and that, as the sedimentary strata have received so large an accession in the lowest member of the series, they have had a corresponding reduction in the upper portions of the system, as com- pared with England. But the supposition which I regard as the more probable is, that we may here have passed across the position of maximum accumulation, and may have reached the point where the beds begin to thin away in the direction of the old coast-line, as represented in fig. 4, page 1357. 2. Reeton Souru or THE BARRIER. We must now retrace our steps to the district south of the barrier, which includes the coal-fields of South Wales, Forest of Dean, Bristol and Somerset—Mr. Godwin-Austen’s hypothetical trough of the Thames Valley, and the culm series of Devonshire. The sedimentary strata of this region appear to have been derived not from the north-west, as in the case of the coal-fields north of the barrier, but from the west-south-west, as indicated by the isometric * Mr. Geikie has suggested to the author, as a possible explanation of the absence of the Gannister Beds or Lower Coal-measures of England, that the Scottish area was elevated into land during the period in question. + Taking the line A as the point of maximum accumulation, this may represent the Carboniferous series of Lancashire and Yorkshire, while the Scottish Coal- fields will be situated at b, and the English at B, @, D, E,—E being the vanishing ~ point towards the South-east of England. . Sd 1862. } HULL—CARBONIFEROUS STRATA. 143 lines. The variations of development of the Carboniferous rocks have been fully discussed by Sir H. De la Beche*, who shows that the greatest vertical thickness is attained in Glamorganshire of 12,000 feet or more, while east of Bristol the same beds are only 5500 feet, and in the Forest of Dean 3385 feet thick. To what extent the true Coal-measures once surmounted the culm- measures of Devonshire it is, of course, impossible. to say; but, from the position of these beds with reference to the Glamorganshire coal-field, from which they are separated by an anticlinal axis, there was probably a large amount of strata now lost by denudation. We must, with Sir R. Murchison+, regard the culm-measures themselves as the representatives of the Carboniferous Limestone, and probably the Yoredale series and Millstone-grit ; but, as there are only thin bands of limestone, with Posicdonomya Bechert, to represent the great limestone formation of Bristol and Chepstow, it is evident the “ sedi- mentary ” elements have predominated in Devonshire to the disad- vantage of the calcareous. These changes I have endeavoured to illustrate by means of the isometric curves. The Carboniferous series, therefore, to the north and to the south of the barrier belong to two different systems, not of time, but of circumstances. Their materials have been accumulated in nearly opposite directions. The sources of these materials have been differ- ent, and also the direction of the currents. That the Carboniferous series was connected by sea, round the western extremity of the barrier, is proved by identity of fossils in the limestones and Lower Coal-measures of the North of England, Central Ireland, and South Wales, d&c. In each of these districts Pecten papyraceus and Gonia- tites Listert occur in the Lower Coal-series. The calcareous member was more fully developed in the east than in the west, and extends from Somersetshire into France and Belgium, until, as already stated, it thins away on approaching the Rhine. 3. Norte ATLANTIC CoNnTINENT. Readers of the works of Sir C. Lyell will recollect how that author, in treating of the distribution of the Carboniferous rocks of North America, shows that the sedimentary materials increase in thickness and become coarser in texture as they approach the north-eastern seaboard. Thus in Nova Scotia these materials attain, according to Dr. Dawson, a thickness of 14,000 feet +, in which the limestones play a subordinate part, as they do in Scotland. From the flanks of the Alleghany range, westward and southward, into Central America, the “sedimentary” strata gradually thin away, while the calcareous as constantly augment in bulk, until, on reaching the Rocky Moun- tains, they attain magnificent proportions$, forming, as shown by Sir J. Richardson and Dr. Hector, the huge and rugged masses of the central range. The tendency of the calcareous and sedimentary elements of the system to become developed in opposite directions is therefore strongly marked over this Continent. * Memoirs of the Geological Survey, vol.i. t “Siluria,” 2nd edit. pp. 293--4. { “ Acadian Geology.” § Quart. Journ. Geol. Soc. vol. xvii. 144 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 5, From the north-easterly expansion of the sandstones and shales, as well as their increased coarseness in the direction of the North Atlantic, Sir C. Lyell has inferred the existence of a continent (occupying the position of this ocean), from the waste of which these strata have been derived. Mr. Godwin-Austen has also indicated its position*. The probability of ‘such a continent is reduced to certainty by the similarity and frequent identity of the Carbonife- rous flora of Europe and America, the land having formed a bridge for the migration of the plants from one country to another. We may suppose this land to have included Greenland, Iceland, and Scandinavia. Recollecting, then, the south-westerly attenuation of the American strata, and the south-easterly attenuation of the North-British, can it be doubted that the same continent was the parent of the coal-bearing strata of both countries? This being ad- mitted, we may also infer that the shores of this Atlantis were washed on the west side by a current running south-west, which drifted the sediment in that direction; and on the other by a cur- rent running south-east, which carried the sediment over the sub- merged portions of Scotland, England, and Ireland}. It may he assumed as a general principle, that all the oceanic currents north of the equator running west come from the north, and those running east come from the south. Hence we may infer that, during the Carboniferous Period, there was open sea in the arctic regions of the Western Hemisphere, generating an arctic current—a proposition borne out by the occurrence of plants and shells of this period as high as lat. 78°; and on the other hand we may infer land to have existed to the north of Europe, or at least of Britain, whose shores were swept by a current similar in its direction to the Gulf-stream. Throughout this long geological period did these currents carry the sands and clays southward ; and as the distance from the sources of these materials increased, so did the amount deposited diminish ; which to my mind is a satisfactory explanation of the thinning out of the strata in certain directions. I would here beg to remind the Society of a former communica- tion, in which it was attempted to be shown that the sedimentary strata of the Lower Mesozoic Formations undergo a similar diminu- tion of volume, when traced from the north-west towards the south- east of England. Now it is remarkable that the line of maximum development of the Carboniferous and the Mesozoic Rocks very nearly correspond in each case, stretching from Lancashire in the direction of London. So rapid does the attenuation of the Trias and the Lias appear to be, that I inferred that these formations would be found to terminate somewhere about the position of the Chalk escarp- * Tn his elaborate memoir “ On the possible Extension of the Coal-measures, &e.,” Quart. Journ. Geol. Soc. vol. xii. t I do not propose to touch on the subject of the derivation of the Carbo- niferous strata of Belgium and Germany ; but there can be little doubt of the northerly origin of the sedimentary strata, drifted by currents from land lying to the eastward of the Scandinavian Promontory. . t Brought to this country by Sir E. Belcher. « 1862.] --«-HULL——CARBONIFEROUS STRATA. 145 ment*. The whole series, therefore, may be considered as a system of wedges lying with their thin edges pointing towards the escarp- ment of the Chalk; and the absence of these formations under the Cretaceous Rocks at Harwich (for an account of which we are indebted to Mr. Prestwich) is, I submit, a proof of the soundness of the views here advanced. Ts it not therefore a remarkable circumstance, that the north has been the source for the supply of so many non-calcareous formations, including those of the Carboniferous, Triassic, Liassic, and Oolitic Periods, and that there has been a general “ northern drift,” re- peated at intervals from a period so far remote (at least as far as the commencement of the Carboniferous) until that immediately pre- ceding our own epoch? Such a series of events, when we consider the great physical changes which have occurred throughout this enormously long period, must, I think, be traced to some general law regulating the course of oceanic currents, and exhibits a remark- able uniformity in the operations of nature through long periods of geological history. The extent of the land which was capable of supplying so vast a quantity of material must have been very large, and, judging by the characters of some of the Carboniferous and more recent strata, seems to have been composed principally of granitoid or metamorphic rocks. Its southern limits may have reached the western and northern coasts of Scotland; and the Highland mountains may have formed outlying islets and headlands. § OL. Summary of Conclusions. (General.) 1. It appears, from the above considerations and examples, which further research will enable us to multiply, that calcareous strata are distinct from argillaceo-arenaceous, not only from differences of ori- gin (a fact now generally admitted), but also in the manner of their distribution ; so that limestones ought to be removed from the class of rocks termed “ sedimentary.” 2. That in any natural group or system of strata, consisting, on the one hand, of “ sedimentary ” strata, and on the other of calca- reous, it appears that the direction of the greatest vertical develop- ment of the one will be that of the smallest vertical development of poi In a word, where the one becomes thin, the other becomes thick. 3. That, on the principles here stated, the frequent occurrence of natural groups of rocks consisting of three members, the first and third “sedimentary,” the second (central) calcareous, admits of ex- planation. * “On the South-easterly Attenuation of the Lower Secondary Rocks, &c.,” Quart. Journ. Geol. Soe. vol. xvi. t In my work on ‘The Coal-fields of Great Britain,’ I have given a full exposition of these views, and a section showing the limits of the Carboniferous and Mesozoic Rocks over the South-east of England (pp. 253 e¢ seq., 2nd edit.). VOL, XVIII.—PART I. L 146 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, (Special.) 4, That a barrier, or tract of dry land, existed nearly across Cen- tral England, dividing the Carboniferous Rocks into two distinct regions. 5, That to the north of this barrier the “ sedimentary ”’ strata of the Carboniferous Period become attenuated from north-west to south, while the calcareous strata thin out from south to north, Derbyshire being the centre of greatest development. 6. That to the south of this barrier the ‘sedimentary ” strata become attenuated from west to east ; while the calcareous thin out from east to west. 7. That, while on the north side of the barrier there was a cur- rent bringing the sediment from the north, on the south side there was a current bringing sediment from the west. 8, That richly productive Coal-measures do not exist under the Eastern Counties. 14% DONATIONS TO THE LIBRARY OF THE GEOLOGICAL SOCIETY. From November 1st to December 31st, 1861. I. TRANSACTIONS AND JOURNALS. Presented by the respective Societies and Editors. Albany. Forty-second Annual Report of the Trustees of the New York State Library. Transmitted to the Legislature, April 3, 1860. 1860. From the New York State Inbrary, Albany. ——. Forty-third: April 9, 1861. 1861. Seventy-third Annual Report of the Regents of the Uni- versity of the State of New York. Made to the Legislature, January 13, 1860. 1860. ——. Seventy-fourth: made to the Legislature, January 17, 1861. 1861. ——. Twelfth Annual Report of the Regents of the University of the State of New York, on the condition of the State Cabinet of Natural “History and the Historical and Antiquarian Collection ae thereto, &c. Made to the Assembly, March 15, 1859. 1859. J. Hall.—Contributions to the Paleontology of New York (1855- 58), 7 (woodcuts). Thirteenth Annual Report of the Regents of the University 4 Oe State of New York. Made to the Senate, April 10, 1860. 1860. J. Hall.—Contributions to Paleontology (1858-59), 55 (woodcuts). ——. Fourteenth: made to the Assembly, April 10,1861. 1861. L, Lincklaen.—Guide to the Geology of New York, 17 (19 plates). J. Hajl.—Contributions to Paleontology (1859-60), 89. L 148 DONATIONS. American Journal of Science and Arts. Second Series. Vol. xxx. Nos. 95 and 96. September and November 1861. J. M. Ordway.— Waterglass, 153, 537. F. B. Meek and A. H. Worthen.—The age of the Goniatite-lime- stone at Rockford, Indiana, 167. . L. Lesquereux.—The Coal-formations of North America, 1953. G. H. Cooke.—The White Limestone at Sussex and Franklin Zinc- mines, New Jersey, 208. B. F. Shumard.—The Primordial Zone of Texas, with New Fossils, 213. E. Billings.—The Red Sandstone of Vermont, 252. S. W. Johnson.—Agricultural Chemistry, 235. F. B. Meek.—The Cretaceous and Carboniferous Rocks of Texas, 278. J. P. Lesley.—The North American Coal-measures, 281. T. S. Hunt.—The origin of some Magnesian and Aluminous Rocks, 286. J. M. Gillis:—Earthquake on the island of Penang, 297. Earthquake at Syracuse, New York, 297. Eckfeldt.—Natural dissemination of Gold, 297. J. Evans, Obituary Notice of, by C. T. Jackson, 311. L. Lesquereux.—Fossil Fruits in the lignite of Brandon, Vermont, 355. W. Fairbairn.—Address to the British Association, 363. C. W. Eliot and F. H. Storer.—Arsenic and Zine, 380. O. C. Marsh.—Gold of Nova Scotia, 395. J. L. Cassels.—Meteorite which fell in Hindostan in 1857, 401. Spectrum-analysis, 408 ; Ceesium and Rubidium, 409; Thallium, 411. . St.-Cl. Deville-—Reproduction of certain Crystalline Minerals, 415. J. Nicklés.—The so-called Semi-metals, 416. T. 8. Hunt.—On the “Taconic System,” 427. I, G. St. Hilaire.—On Species, 431. W. Haidinger.—Meteorites, 440. Assurance Magazine and Journal of the Institute of Actuaries, No. 47... Vol.x. Part1. October 1861. Atheneum Journal. Nos. 1775-1783. Notices of Meetings of Scientific Societies, &c. Swedish Expedition to Spitzbergen, 766. Eruption of Vesuvius, 884. . Berlin. Zeitschrift d. Deutsch. geol. Gesellschaft. Vol. xiii. Heft 1. 1861. — Proceedings, 1-5; Letters, 16-19. A. yon Strombeck.—Ueber den Gault und insbesondere die Gargas- Mergel (Aptien, d’Orb.) im nordwestlichen Deutschland, 20. R. Bunsen.—Ueber die Bildung des Granites, 61. A. Streng.—Zur mineralogischen und chemischen, Kenntniss der Melaphyre und Porphyrite des siidlichen Harzrandes, 64. . C, Rammelsberg.—Die isidomorn hie in Leucitform von Boh- misch- Wiesenthal, 96. M. Deiters.—Die Trachytdolerite des Siebengebirges, 99 (2 plates). Canadian Journal. New Series. Nos. 35 and 36. September— November 1861. T. S. Hunt.—Canadian Chloritoid, 484. DONATIONS. 149 - Canadian Journal. New Series. Nos. 35 and 36 (continued). | E. J, Chapman,—Freshwater Shells in the Upper Drift of Western Canada, 497. —. Minerals and Geology of Canada, 425, 500. ——. Lazulite, 455. _H. Milne-Edwards.—Molluses and Zoophytes at great sea-depths, 518. L. Semann.—Unity of geological phenomena in the planetary system of the sun, 525. Coal-deposits of British colonies in the South, 478. Mineralogical Notices, 526; Notices of Books, 528. Christiania. Del Kongelige Norske Frederiks Universitets Stiftelse Fremstillet i Anledning af dets Halvhundredaarfest af M. J. Monrad. Universitets-Program. 1861. —. Forhandlinger i Videnskabs-Selskabet i Christiania. Aar 1860. 1860. Sars.—Over de i vor Glacialformation indsluttede organiske Lev- ninger, 104, ——. Solennia Academica Universitatis Liter. Reg. Fredericane ante 50 annos conditz die 2 Sept. anni mpcccrx1. celebranda in- dicit Senatus Acad. 1861. Colliery Guardian, Vol.u. No. 52. December 28, 1861. W. W, Smyth.—Lectures on Mining, 433. Critic. Vol. xxiii. Nos. 591-599. Notices of the Meetings of Scientific Societies, &c. D. Page’s ‘The Past and Present Life of the Globe,’ noticed, 543, G. Rorison’s ‘The Three Barriers,’ noticed, 544. H. Miller’s ‘ Footprints of the Creator,’ noticed, 545. Geneya. Mémoires de la Soc. Phys. et d@Hist. Nat. de Genéve. Vol. xvi. ist Part. 1861. | E. Ritter—Recherches sur la figure de la terre, 165. Geologist. Vol.iv. Nos. 47 and 48. November and December 1861. S. J. Mackie.—Cervus tetracroceros? from Folkestone, 465. a F oberts.—Deep sinking for coal in the Wyre Forest Coal-field, C. C. Blake.—Distribution of Mastodon in South America, 469, J. Delbos.—Geology of Biarritz, 473. E. Hull.—Glacial Phenomena of Wastdale, Cumberland, 478. J. H. Macalister.—Fossils of North Bucks, 481. J. Plant—Human Remains in the Trent Valley, 495; E. Suess.—Large Carnivora of the Austrian Tertiaries, 496. paper of the Meeting of the German Association, 501. J. Whitaker and T. I’. Wilkinson.—The Burnley Coal-field, 508. T. A. Readwin.—Gold in Merionethshire, 511. H. Eley.—Accumulation of Earth in caves, 521. C. C. Blake.—Creation by law, 525. _ aaa of Foraminifera of Scinde, 366, 446 (3 lates). J. W. Salter.—New Paleozoic Star-fishes, 484 (plate). W. W. Stoddart.—A Microzoal Bed on the Carboniferous Limestone of Clifton, near Bristol, 486 (plate). J. R. Greene’s § Manual of the Ciesierie’ noticed, 493. H. Seeley.—The Fen-clay formation of Cambridgeshire, 503. M. F. Karrer.—The Foraminifera of the Vienna Tertiary Basin, 507. Institut, . le Section, Nos, 1451-1458 ; 2° Sect. Nos. 301, 310, dll, Notices of Meetings of Scientific Societies, &c. Leonhard und Bronn’s Neues Jahrbuch, Jahrgang 1861. IYV.Y. VI. Heft. F’, Scharff—Ueber die Bau-Weise der wiirfelférmigen Krystalle, 385 (38 plates). R. Blum.—Foyait, ein neues Gestein aus Siid-Portugal, 426. C. F. Peters.—Ueber Kalzit und die rhomboedrischen Karbonspathe im Allgemeine, 434. A. Knop.—Die Kupfererz-Lagerstiétten von Namaqualand und Da- maraland, 513. Gergens.—Entstehung von Schwefel-Krystallen in seiner Mineralien- Sammlung, 551. A. Delesse.—Die hydrologische Karte der Stadt Paris, 553. H. Fischer.—Ueber den Kinzigit, 641. C. F. Peters—Mineralogische Notizen, 655. H. B. Geinitz.— Ueber den Riesenhirsch des Dresdener Museums, 669. Gergens.—Ueber fossile Blutegel-Coccons bei Mainz, 670. Letters ; Notices of Books, Minerals, Geology, and Fossils, 156 DONATIONS. III. GEOLOGICAL AND MISCELLANEOUS BOOKS. Names of Donors in Italics. Barrande, J. Défense des Colonies. Groupe Probatoire ecompre- nant la Colonie Haidinger, la Colonie Krejéi et la Coulee Krejei. 1861. Bidder, G. P. Jun. The National Defences. 1861. From the In- stitution of Cwil Engmeers. Binkhorst, J. T. B. van den. Monographie des Gastéropodes et des Céphalopodes de la Craie Supérieure du Limbourg. 1861. Bland, T. On the Geographical Distribution of the genera and species of Land Shells of the West India Islands, with a Catalogue of the Species of each island. 1861. Capellini, G. Cenni geologici sul giacimento delle Ligniti della basa val di Magra. 1860. From J. G. Jeffreys, F.GS. Carpenter, P. P. Catalogue of the Reigen Collection of Mazatlan Mollusca. 1860. From the New York State-Library. Catalogue of upwards of fifty thousand volumes of ancient and modern books, English and Foreign, in all classes of literature and the fine arts, by Willis and Sotheran. 1862. From Messrs. Willis and Sotheran. Cheney, T. A. Illustrations of the Ancient Monuments in Western New York. 1860. From the New York State-Library. Deshayes, G. P. Description des Animaux sans Vertcbres découyerts dans le bassin de Paris, pour servir de supplément a la description des coquilles fossiles des environs de Paris. Livr. 25 et 26. 1861. Dewalque, M. G. Sur la constitution du Systéme Eifélien dans le bassin anthraxifere du Condros. 1861. : Esposizione Italiana. 1861. Classe VI. Mineralogia, Metallurgia, ed Armi. Consiglio dei Giurati. 1861. Hrom L. Horner, Hsq., Pres. GS. Favre, A. Notice sur la Réunion extraordinaire de la Société Géo- . logique de France 4 Saint-Jean-de-Maurienne (Savoie) le 1°. Septembre 1861. 1861. Gabb, W. M. Synopsis of the Mollusca of the Cretaceous Formation ; geographical and stratigraphical. 1861. Haast, J. Report of a Topographical and Geological Exploration of the western districts of the Nelson Province, New Zealand. 1861. DONATIONS. 157 Hall, J. Contributions to Palzeontology (1858-59). 1860. —. ——. (1859-60). 1861. | ——, ——. Descriptions of New Species of Fossils from the Upper Helderberg, Hamilton, and Chemung Groups. 1861. Hector, J. On the Geology of the country between Lake Superior and the Pacific Ocean (between the 48th and 54th parallels of latitude) visited by the Government Exploring Expedition, under the command of Capt. J. Palliser. (1857-1860). 1861. Heer, O. Recherches sur le Climat et la Végétation du Pays Ter- tiaire. Traduction de C. T. Gaudin. 1861. Hopkins, E. Fiery Globe and the Australian Gold-fields. 1861. : _ Horton, W.S. On the Geology of the Stonesfield Slate and its as- sociate formations. 1861. James, H. Abstracts of the Principal Lines of Spirit-levelling in Scotland; and Plates. 1861. From the Ordnance Survey of Great Britain. Kongliga Svenska Fregatten Eugenies Resa omkring Jorden under Befal af C. A. Virgin aren 1851-53. Haft 8. Fysik, I]. 1861. —. ——. Haft 9. Physique, 1. (French Translation). 1861. —. ——. Haft10. Zoologi, V. 1861. Haft 11. Botanik, II. 1861. From the Swedish Government. Lartet, E. Nouvelles recherches sur la co-existence de ’homme et des grands mammiferes fossiles réputés caractéristiques de la dernicre période géologique. 1861. Inneklaen, L. Guide to the Geology of New York and to the State Geological Cabinet. 1861. Lovén, S. Om nagra i Vettern och Venern Funna Crustaceer. 1860. Marcou, J. Notes on the Cretaceous and Carboniferous Rocks of Texas. 1861. Murchison, R. I. On the Inapplicability of the new term “ Dyas” to the “Permian” group of rocks as proposed by Dr. Geinitz. 1861. Odernheimer, Fr. Das Festland Australien. 1861. Owen, R. Paleontology, or a systematie summary of extinct animals and their geological relations. 2ndedit. 1861. Perthes, B. de. De Vhomme antédiluvien et de ses euvres. 1860. Reeve, L. Conchologia Iconica. Monographs of the genera T'rigonia, Scarabus, Myochama, Cymbium, Terebratula, Argonauta, Nautilus, Melana. 1860-61, 158 DONATIONS. Report of the Committee on the Decay of the Stone of the New Palace at Westminster. 1861. From Prof. J. Tennant, F.GS. Report on the Nova Scotia Gold-fields, by J. R. Hea and J. Howe. From Professor J. Tennant, F.GS. Sandberger, IF’, Die Conchylien des Mainzer Tertiirbeckens. Sechste Lieferung. Sars, M. Om Siphonodentalium vitreum en ny slegt og art af dentalidernes familie. 1861. Oversigt af Norges Echinodermer. 1861. Schvarcz, G. A Fajtakérdés Szinvonala hdrom éy elést. 1861. —~. A Gordgik geologiaja jobb napjaik ban. 1861. ——. Foldstani elméletek a Hellénségnél nagy sdndor koraig. — 1 Kotet. 1 Fuzet.:- 1861. —. ——. 1 Kotet. 2 Fuzet. 1861. ——. LaGéologie Antique et les Fragments du Clayoménien. 1861. ——. Lampsacusi Strato. Adalék a tudomdny_ torténet¢hez. 1¥Fuzet. 1861. Recherches sur les Théories Géologiques des Grecs. 1861. Towson, J. T. Icebergs in the Southern Ocean. 1859. Welhaven, I.S. Cantate ved det Norske Universitets Halvhundred- aarsfest den 2°*" September, 1861. Zirkel, F. De geognostica Tslandix constitute obschrannaes 1861. Presented by Sir C. Lyell, F.GS. THE QUARTERLY JOURNAL OF THE GEOLOGICAL SOCIETY OF LONDON. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Frsruary 26, 1862. SPECIAL GENERAL MEETING. It was Resolved that the Annual Contribution to be paid by both Resident and Non-resident Fellows elected after the 1st of March next shall be Two Pounds Two Shillings per annum: the Composition for future Annual Contributions being Twenty-one Pounds. ORDINARY GENERAL MEETING. George Charlton, Esq., Mining Engineer, Dukinfield, near Man- chester, and Julius Schvarez, Ph.D., Stuhlweissenburg, Hungary, were elected Fellows. The following communications were read :— 1. On the Drier contaamimg Recent SHELLS, in the neighbourhood of Wotyernamepton. By the Rev. Wiii1am Lister, F.G.S. (Abridged. ) Turse drift-deposits lie for the most part upon a nearly level surface of Lower Keuper Sandstone, overlooked eastward by a range of low Bunter and Permian hills, of which Show Hill and Bushbury Hill are the chief. Other exposures are upon Permian sandstone in the town of Wolverhampton, and upon the Coal-measures of the district - adjoining. Bushbury Hill is chiefly remarkable for the number of travelled blocks of granite and greenstone lying around its north- VOL. XVIII.—PART I. M 160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, western base—the side lying most open to bygone arctic and glacial influences. No boulder-clay nor drifted material of other kind is associated with these blocks upon the hills in this immediate neigh- bourhood. The drift at three localities, viz., Bushbury Junction, Oxley Manor, and Wobaston Big Meadow, had probably a parallelism in time of deposition and agency of formation ; though I cannot satisfy myself whether to regard them as the remains of a low terrace-line skirting the valley, or as the result of undercurrents, relaying the derived material in banks parallel with its strike. In the exposure of this drift at Bushbury Junction, where it is an apparently un- stratified bed of clay and sand, with an admixture of both rounded pebbles and angular flints, I have met with the followimg marine shells, which have been kindly determined for me by Mr. J. Gwyn Jeffreys, F.G.S.:—WNassa reticulata, Turritella communis, Purpura lapillus, Inttorina squalida, Astarte arctica, Cardium edule, Tellina solidula, and Cyprina Islandica. Rolled shells and other fossils derived from Liassic rocks accom- pany these, such as Gryphew, Ammonites, Cardime, and Belem- nites. I have also met with a fragment of Downton Sandstone (Upper Silurian), bearing a cast of Rhynchonella, together with pieces of coal, having rounded edges and striz upon their surfaces, and of unfossilized wood similarly rounded. At the exposure of this drift at Oxley Manor, half a mile N.W. of Bushbury, its physical character was that of a clay-bed resting upon sand. The following shells were met with in the clay, though the condition of all the imbedded remains was more fragmentary than at the first-named place :—Cardium echinatum, Tapes virginea, Venus striata, Modiola modiolus, and Turritella communis. In connexion with his determination of these and the before-mentioned species from Bushbury Junction, Mr. Jeffreys has favoured me with the following note :— “ All of these shells are much rolled and broken, and they appear to have been cast up by the tide on a pebbly beach. They indicate also the former presence of a gradually shelving tract of sand below the beach seawards, as well as of an intermediate belt of loose stones or shingle in the littoral zone. It is possible that these shells may have been carried off with the pebbles from a beach in the Arctic regions by an iceberg, which, after traversing a considerable distance in a glacial sea, may have stranded or melted, and deposited its load in the spot where the shells and pebbles have now been found. The pre- sent data are, however, insufficient to enable me to form any opinion on this point. All the species now inhabit the Arctic Sea. Two of them, Astarte arctica and Inttorina squalida, are not found living in our seas ; but all the rest are common British species. The period of this deposit in Staffordshire, whether original or derivative, may have been coeval with that of the Kelsey Hill formation, which has been lately described by Mr. Prestwich in the ‘ Quarterly Journal of the Geological Society*.’ Eight species enumerated in his paper also occur in the deposit under notice, which in its turn possesses four * Vol. xvii. p. 446. . 1862. | LISTER—SHELLS IN DRIFT. 161 (Astarte arctica, Cardium echinatum, Modiola modiolus, and Tapes virginea) wanting in the Kelsey Hill catalogue. The Cyrena, or Corbicula, is absent.” The third exposure of this line of drift-deposit is a partially strati- fied mound of sand and gravel, 88 yards long, 38 yards wide, and about 2 yards in height, situated in Wobaston Big Meadow, about a mile and a half north of Bushbury Junction. The long axis of this mound corresponds with the strike of the before-described beds, and with the direction of the valley, which is due N. and 8. This deposit has not at present yielded me any shells nor specimens of angular flints. The chief of its derived contents are the following :— pebbles of limestone, slate, quartzite, vein-quartz, black quartz, veined lydian-stone, a fragment of syenite, and a small Silurian coral (Cyathophyllum Loveni). The part cut into exhibits the fol- lowing section :— = 75) 2 LAD CIC sae aie a ae aan eae ae 0 Pebbles and sand (the pebbles vary in size, are largest at the top of the bed, and become gra- ueseeeiiaiier Pelow)...... 0... 2c cee ees 2 6 Bed of stratified sand, with a few small pebbles .. 1 6 Two other patches of drift, lymg at a somewhat higher level, occur in this immediate neighbourhood, and are probably related by coin- cidence of time and deposition. The first locality is that of Compton Holloway, in the parish of Tettenhall, where clay-deposits are seen to fill up eroded hollows of the Keuper Sandstone on the hill-sides west of the plain. These contain derived fossils from Liassic rocks, similar to those met with at Bushbury. A suite of them has been collected by Henry Hill, Esq., of Dunstall. Many like remains were found some years ago at Wightwick, another point at this higher level. Here, however, the clay contains angular flints, as at Bushbury, and the low hills are covered with scattered drift-pebbles. In drift-clay, at about the same level, near the Hospital in Wol- verhampton, Liassic Gryphew have been met with; and fossils of like age in a similar bed at the New Cemetery. I am indebted to Mr. Henry Beckett, F.G.S., for some notes respecting this easterly extension of the boulder-clay, as also for a notice of other exposures at Penn, from two to three miles south of Wolverhampton. At Upper Penn, the clay yielded pieces of wood and a broken tibia of Bos. I am also informed by Mr. George E. Roberts of a considerable exten- sion of these clays, with sandy layers, westerly ; for they are well exposed at Acleton, eight miles 8.W. of Bushbury, and there abound in Turritelle. A recent exposure in that district is at a spot half a mile north of Badger Hall. In conclusion, I would call attention to the deep and wide- stretching sand deposit described by Prof. Beete Jukes as lying in immense quantities around West Bromwich and upon the district east of Birmingham*. In the lower part of this sand, which in places * “The South Staffordshire Coal-field,” p. 325. M2 162 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, attains a thickness of 100 feet, marine shells identical with those found by myself at Bushbury and Oxley Manor have been detected by Mr. Beckett, at Mr. Sparrow’s colliery of Portobello. This fact is valuable as a determination of the relative position in which we shall be justified in placing these shell-bearing clays in the drift-deposits of Staffordshire. 2. On a Sexit Bounper in Littte Cumpra, WESTERN IstEs. By James Suits, Esq., F.R.S., F.G.8., of Jordan Hill. Sprit erratic blocks are of frequent occurrence in Switzerland. The only explanation of this phenomenon which I have met with is that of M. Charpentier, in his “ Essai sur les Glaciers.”” Speaking of the blocks, he says, ‘‘Quelques uns sont fendus, mais la direction des fentes prouve jusques a l’évidence que les ruptures sont le résultat d’une chute et nullement d’un choc horizontal” (p. 180). M. Char- pentier offers no conjecture as to the height from whence the blocks could have fallen; but where there is no superincumbent precipice of rock near, it must have been from one ofice. Indeed, I may say that I obtained proof that such was the case; for upon examining the frag- ments which lay at the foot of the escarpment of ice which terminates the Glacier of Grindelwald, I observed one which, from the freshness of the fracture, I concluded must have fallen very shortly before my visit, and obviously from the surface of the glacier. Such blocks occur occasionally in the basin of the Clyde, in situa- tions where there is no adjoining height from which they could have fallen,—a circumstance which I can only account for by supposing the former existence, in the same localities, of ice in the shape of glaciers, icebergs, or coast-ice. I may add that some of the split boulders are also scratched, exhibiting additional proofs of glacial action. To one of these blocks I wish to call the attention of the Society, on account of the peculiarity of the circumstances of its present position. There is on the west coast of Scotland a well-marked cliff and terrace, indicating an elevation of about forty feet above the present sea-level; and, from the amount of solid rock which has been removed by the washing action of the sea, we may form some con- ception of the prodigious lapse of time during which the sea-level was stationary at that height. This is nowhere better seen than in the Islands of Great and Little Cumbra. The larger island is composed cf red sandstone, traversed by trap-dykes ; the smaller one is composed entirely of trap. The trap of the dykes, from its greater hardness, has been worn away more slowly than the sandstone; hence their projection from the sandstone cliff; hence also the greater breadth of the terrace in Great Cumbra than in that of the trap of the smaller island. The terrace in Little Cumbra, formed by the wasting action of the sea at right angles with the coast-linc, has been subsequently ground down and scratched by a force acting parallel to it and the ancient cliff; and it is upon this that the blocks in question must have fallen. 1862. | SMITH——SPLIT BOULDERS. 163 The block is composed of trap, apparently the same as that of the island, but at such a distance from any neighbouring height as to preclude the supposition that it could have fallen from it. I see there- fore no other hypothesis by which we can account for its present position than that of supposing that it must have fallen from an escarpment of ice. We have thus two independent glacial phenomena which belong to a period subsequent to the formation of the forty-feet terrace, showing that the lengthened period of its formation belongs to the Glacial Epoch. Sketch of the Split Boulder on Latile Cumbra, Western Isles. i i‘ [N.B. In the foreground the shore shows glacial strie. | There is yet one circumstance connected with this locality which requires to be noticed. The scratched surface of the ancient terrace passes under the sea; and although it has been exposed to its wasting action for a length of time equivalent in duration to that of the present sea-level, the strie have not been obliterated. Here we have in juxtaposition two distinct cases of the effects of the wasting action of the sea. In the most ancient of these, or that when the cliff and terrace were formed, we have a removal of rock amounting to at least a hundred feet; in the second, or that of the present sea-level, the amount of wearing away of the same rock cannot exceed a small fraction of an inch. I am convinced that no decided change of level has taken place in the West of Scotland during the historic period; but there may have been small changes: and it is no objection to such a supposition that they have not been observed and recorded ; such changes of level either pass 164 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 26, unobserved, or are ascribed to the retiring or encroaching of the sea. We may suppose, therefore, that in times comparatively recent a small movement of elevation or depression of the land has taken place, sufficient to have brought the rocks in question within this wasting action of the sea. 3. On the Ick-worn Rocks of Scornanp. By T. F. Jamreson, Esq., F.G.S. ContTENTS. . Erosion of the rocks beneath the Drift. . Ice-action compared with torrent-action.—Case of the latter at Crinan. . Reasons for thinking the erosion of the rocks in Scotland to be due chiefly to land-ice, and not to water-borne ice. . Remarkable instances at Loch Treig and Glen Spean.—Boulders lifted up far above the parent rock.—Glen Roy. . Example of ice-action at Knapdale.—Motion uphill. . Probable solution of the phenomena.—Reference to Greenland. . Difficulty as to climate.—Fossil-evidence.—Probable period of elevation. . Proofs of great submergence subsequent to period of elevation. . Criteria for distinguishing action of land-ice from that of floating ice. . Denudation.—Probable geological date of the great land-glaciation of Scotland. § 1. At the bottom of all the Drift-beds there is in our northern latitudes a phenomenon which, if rightly understood, would dispel much of the obscurity that still envelopes the history of that period ; I mean that curious scoring and polishing of the rocky bed on which the Drift is found so frequently reposing. Saussure, in his Alpine journeys, had often remarked those rounded masses which he called roches moutonnées, and also did not omit to note the polishing of the rocky surface; curiously enough, however, although so familiar with glaciers, he did not refer these appearances to their true cause, but attributed this scoring of the rocks to the passage over them of boulders hurried along by arush of water. Colonel Imrie, also, and Sir James Hall, who in 1812 both described the same appearances in Scotland, sought to explain them in a similar manner. As this theory of their origin has found favour with several geologists, I am induced to describe here a case of some interest which came under my notice, and was peculiarly fitted to test the sufficiency of a powerful torrent, carrying with it great boulders and stony débris, to affect the rocks in the manner under consideration. § 2. In the county of Argyle an artificial channel was cut, a good many years ago, between the Sound of Jura and Loch Fyne, called the Crinan Canal; it is about 9 miles long, and lies in an E. and W. direction, or rather S.E. and N.W. Sloping up from the south side of this canal there is a range of hilly ground, where there are a few small lakes that have been converted into reservoirs for regu- lating the supply of water, and which are situated at a height of about 700 feet above the canal. Three of these lakes, each of them covering an area of about thirty acres, have been connected, and the depth of their waters increased by artificial embankments. But in © February 1859, owing to heavy floods or some other cause, the Coho SO GC AIS. He — 1862. | JAMIESON— GLACIATION OF SCOTLAND. 165 embankment of the uppermost of these three lakes gave way, and its water, rushing into the next one, caused it also to burst its bar- rier; and the contents of both, now descending suddenly into the lowermost lake, broke the embankment of it likewise; so that the contents of the whole three were at once let loose, and rushed down the steep channel of a mountain-stream with immense force. Owing, luckily, to the retired, barren nature of the locality, there were no houses in the way, nor much else that could sustain serious damage, except the canal, a great part of which was destroyed, and quite filled up with stones and gravel. It took an expenditure of several thou- sand pounds to repair the injury done to its channel, and the engi- neer who superintended the work told me that some of the boulders he had taken out of it weighed eleven tons. Here, then, was a great volume of water rushing violently down the flank of a hill, through a descent of about 700 feet, and carrying along with it stony débris and boulders of several tons weight. Having seen some account of the matter in the newspapers at the time, I was very glad when, in August 1860, I had an opportunity of examining the scene of the catastrophe. By this time the damage to the canal had been re- paired, but the channel of the hill-stream was very much as the torrent had left it. The rocks there consist of frequent alternations of clay-slate, greywacke-grit, and syenitic greenstone, covered occa- sionally by a variable thickness of stony earth or drift. This cover- ing the rush of water had in many places quite cleaned off, carrying the boulders and stony débris before it, and throwing them down in those spots where the force of the torrent began to fail. I saw many blocks that it had borne along, measuring 3 to 4 feet in length, and a few even from 8 to 11 feet. Onnone of these was there anything at all resembling the glacial polish and strie; neither were there any such markings on the smaller pebbles. Moreover, the débris was for the most part quite unmixed with clay or mud, and consisted either of clusters of large boulders, or masses of washed gravel,—the finer sediment having been carried away by the retiring water. This débris was therefore quite unlike our boulder-earth, and more resem- bled some of the coarser kinds of what I have elsewhere described as the upper rolled gravel that is so frequently met with covering the drift in almost all our river-valleys. I also examined the rocks along the bottom and sides of the ravine, to see how they were affected. Now, its direction is right down the hill-slope from 8.W. to N.E., with occasional windings, and such was the course of the torrent in descending it; but here there was a circumstance which added greatly to the.interest of the case. This was the occurrence of ' true glacial striz and scores, beautifully and extensively marked, and running obliquely across, and sometimes even at right angles to the direction of the ravine; so that there could be no risk of confound- ing them with any ruts made by the descending torrent, which by washing off the drift had finely exposed these markings, and they could be traced passing under banks of undisturbed drift. These glacial impressions, I may also mention, are not confined to this ravine, but are displayed over much of the neighbourhood, and will 166 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, be again referred to in a subsequent part of this paper. But in no ease could I discover the least indication of any such polish, or straight parallel scratching, due to the action of the torrent; I observed, however, in some ‘places on the surface of the greenstone, many round pits or dints, and short irregular scoops or furrows, seldom longer than a man’s finger, caused apparently by the bumping of the large boulders as they rolled along. These markings were irregular in their direction, like the scratching of poultry on a gravel walk, and quite unlike the long, rectilinear, parallel grooves and the polish which are ascribed to the action of ice. Here, then, it was evident that not only had this violent torrent no power to cause such markings, but, from the shortness of its duration, it had also failed in most places to obliterate the real glacial markings of a former period. Agassiz likewise mentions that the débdcle of the Dent du Midi— another example of a current of water charged with fragments of rocks—left no trace of this kind in any part of its course*. § 3. In 1837, the Swiss naturalist whom I have just mentioned com- municated to the Academy of Sciences at Paris some observations on the mode in which glaciers thus affect their rocky bed; and his force of character, together with the ardour he threw into the pursuit, effectually roused attention to the subject. In 1840 (nearly 30 years after Imrie and Hall wrote) he paid a visit to this country, and, in an extensive tour through Britain and Ireland, everywhere recognized in our rounded, scored rocks appearances precisely similar to those he had long studied among the glaciers. of his native country; and he did not hesitate to express his conviction that in Britain glaciers and large sheets of ice, “‘ resembling,” as he says, “‘ those now exist- ing in Greenland,” had formerly existed, to whose action these markings are due. The occurrence, however, of marine remains belonging to the Pleistocene period at various elevations, and even on the tops of considerable hills, together with a great mass of collateral evidence which went to show that this country had been to a great extent depressed beneath the sea during the Drift-period, led many to believe that the appearances referred by Agassiz to glacier-action might be better accounted for by the agency of floating ice; while the absence of alpine heights, and the comparative lowness of much of the country where these markings occurred, still further conduced to this opinion. 5 els When, therefore, I began the study of.the subject, it was rather with a disposition to refer these appearances to sea-borne ice; but a careful examination of such instances as have come under my notice * * The observations of Lyell on the Willey Slide in the White mountains of North America, and those of Dr. Hooker in the Himalaya, go to show that even land-slips do not mark the rocks over-which they pass in the same way that a glacier does. Pee ie + Although Charpentier, and perhaps others, had previously mentioned the erosive action of glaciers upon their rocky bed, yet Agassiz comprehended better than any the geological importance of the phenomenon; and he seems to have been the first to draw attention to the marked distinction that exists between the features of ice-worn and those of water-worn rocks. > 1862. ] JAMIESON—GLACIATION OF SCOTLAND. 167 has led me to believe that no modification of this agency will meet the requirements of the case, and that, in the great majority of instances, this grinding down of the rocks has, in Scotland at least, been caused by the long-continued movement of land-ice and gla- ciers ;—that, in short, when this abrasion took place, our country stood quite above the level of the sea, and probably formed part of an extensive northern continent; and that the submergence which led to the formation of the marine beds, with arctic shells, was a phenomenon subsequent to this great glaciation. One of the first things which convinced me that no icebergs run- ning aground, nor pack-ice driven by the winds, nor coast-ice lashed by the breakers, could explain the case, was the observation that it was always the land-side of the rocks—the exposure facing the highest mountains of the interior—that was most worn and polished, the side fronting the sea being in comparison much more rugged and angular. No instance occurred to me that could be explained by a motion of ice coming from the sea towards the land, while the boul- ders and scratched pebbles, when traced to their sources, also indicated a seaward transport. Thus, along the eastern border of Aberdeen- shire, the glacial strie and scores run from west to east; in my own neighbourhood at Ellon, the general direction is nearly due E. and W., or a few degrees to the N. of W. ; and a low tract of syenitic greenstone has yielded a profusion of large blocks which have been all carried towards the E., while the smaller scratched pebbles are of the kinds which would be got from rocks to the W., many of the varieties not occurring in anyother direction, and it is the western sides of the rocks that are most worn and scratched. Again, at Aberdeen, the surface of the granite, when newly uncovered, shows the glacial strie and grooves pointing a few degrees to the 8. of W., in the direction of the valley of the Dee, the rounded and polished faces of the rocks looking up the valley. On the southern shores of the Moray Frith, between Banff and Troup Head, I found glacial markings pointing S.E. and sometimes 8.W.; and along the shores of the Firth of Forth a mul- titude of instances have been recorded by Hall, Maclaren, Chambers, and Fleming, all indicating a movement from W. to E., and at Stir- ling from N.W. Such is the case in the low grounds along the east seaboard of the island. But when I went tostudy the facts on the west coast, I found it was no longer the same side of the rocks that had been ground down; itis there the east and north-east fronts that have suffered most abrasion, and the scores and strie that streak the rocky shores of the fiords of Argyleshire are just such as might be expected from the action of ice moving down from the mountains. The markings along these sea-lochs are often very striking, and have attracted the notice of Agassiz, Murchison, and Maclaren, who have all insisted on the fact of the rounded striated surfaces being invariably presented to the interior, and the rough jagged fronts to thesea. Prof. Nicol has also chronicled the direction of the striz, as noticed by Sir Roderick Murchison and himself, in several of the glens along the eastern, northern, and western scaboards of Ross 168 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, and Sutherland, all pointing to the same conclusion, viz., that they are due to the passage of ice down the glens. Another consideration that impresses me in favour of the theory that land-ice has caused these appearances, and which was also remarked by Forbes in Norway, arises from the fact that they be- come more extensively and clearly developed as we leave the low flat regions and approach the mountains. For instance, although there is good evidence that the greater portion of England was submerged during the Drift-period, yet it is only in the hilly tracts of Wales and the lake-district that we hear much of the rocks being striated and ice-worn; and in Scotland, although no part of the rocky floor of the country seems quite free from these markings, yet it is in the Highlands that they become so striking and intensely marked. But the instances I have mentioned above, being all purposely taken from localities close upon the present shores of Scotland, in my opinion go to prove that even in the low grounds this glacial erosion has radiated from the interior; and that not only in the mountain-giens has this. action been due to glaciers, but down to the present coast-line we must still ascribe it to an agent moving off the land, and not to sea-ice. The evidence required to distinguish glacier-action from the effects of an icy débdcle rushing down the glens, caused by the dislocation of sheets of ice owing to earthquake-shocks or movements of eleva- tion, is somewhat different from what I have brought forward in the preceding paragraphs. Here we have ice moving off the land in the same direction as a glacier, or nearly so; but in the one case the action would be transient, and in the other of vast duration. Now I think the amount of rock which has been worn away, even at the mouths of the sea-lochs of the W. Highlands, as at Loch Fyne and at the Kyles of Bute, opposite the steamboat-quay at Colintrive, by the glacial action, is far too great to be accounted for by the passage of even a succession of such débacles. The rounded outlines of the tough gneiss and syenite, which I there saw, denoted to my mind the long-continued grinding action of ice slowly moving over them ; for I think the rapid, hurried rush of a sludgy mass, even although repeated, would not produce such finely rounded contours: neither would the grooves and furrows be so persistent and rectilinear in their direction ; for the ice being in broken masses, and accompanied with water and melting snow, would have more freedom of movement than the rigid mass of a huge glacier or ice-stream filling the valley; and in the lower open grounds, where there were no heights to confine the torrent, the straight persistent direction of the scores is even more striking than in the glens and gorges, and to my mind still® more inexplicable by such a catastrophe or series of catastrophes. At Ellon, for example, on the east side of Aberdeenshire, there are no hills exceeding 600 feet in height within ten miles, and none exceed- ing 1000 feet within 20 miles; yet the scores on the rocks exposed in the railway-cuttings and quarries have a remarkably uniform direction, and run across hill and dale with a perfect indifference to the minor 1862. | _ JAMIESON—GLACIATION OF SCOTLAND. 169 contours of the surface. Now here, as in the basin of the Forth, no ordinary glacier-action will suffice for the explanation; yet the proof is clear that the action has come from the west or land side, and not from floating ice propelled inwards or parallel to the coast. § 4. In a paper in the 16th volume of the ‘Journal of the Geological Society,’ at pp. 368 and 370, I gave it as my opinion that at the commencement of the Drift-period this country had stood as high as at present, or perhaps much higher, with an extensive development of glaciers and land-ice, like that of Greenland; and I there described a case near Killiecrankie, in Perthshire, where the flank of a hill called Meal Uaine is rounded, scored, and in some places even polished, as if by the passage of ice down the valley; and I pointed out that, as the markings on the hill-top are about 1800 feet above the pre- sent bottom of the glen, it was evident that, were land-ice the cause, it must have been in a volume altogether extraordinary. My curiosity was greatly excited by what I there saw; and since then I have been so fortunate as to discover some other cases quite as remarkable, where the cause of the phenomena is more clearly indicated. One of the most complete of these was in the Lochaber district of Inverness-shire, so celebrated for its Parallel roads or terraces. High up among a cluster of hills forming the eastern extension of Ben Nevis, there is a mountain-pass, of a beautifully wild and savage character, where two streams take their rise, and flow in opposite directions. One of these runs to the N.W. down a very short glen, called the Larig Leachach, into Glen Spean. This Larig Leachach, or “ the Stony Larig,”’ is at its upper end very rocky; and some strata of quartz, that run vertically across the glen, show abundant traces of glacial action, the hardness of the rock having preserved even the finer striz and scratches: these markings are parallel to the direction of the stream, and the abrasion is most visible upon the faces of the rock looking up the hollow. Further down there is a great deal of moraine-matter—more indeed than is usually seen, owing, I imagine, to the precipices and high corries that overhung the ancient glacier, and had sent down much rocky débris upon its surface. The other stream, taking its rise at this mountain-pass, flows S.E. into the head of Loch Treig down a much longer glen, known simply as “the Larig.” Similar evidence of glacial action occurs along its course, but owing to the nature of the rock being different, and yielding more rapidly to the weather, the glacial impressions have not been so well retained. From this pass, therefore, we may sup- pose two ice-streams to have set out in opposite directions—one to the N.W., the other to the S.E. Two other glens, one of them larger than the Larig, contribute their streams to Loch Treig—a beautiful sheet of water, about six miles long, in a N. and S. direction, and scarcely a mile broad at its widest part. Itis enclosed by steep hills on both sides, and is so deep that I am told it was never known to be frozen over. Around its upper extremity there are many irregular hillocks of unstratified stony débris, full of boulders ; these are most numerous in the curve 170 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, of the hill at the south-eastern end of the lake. Near its outlet into Glen Spean, Loch Treig tapers to a narrow point, owing to the near Fig. 1.—Outline-map of a part of Inverness-shire, showing the Glacial Strie and the distribution of Moraine-matter on the Spean and elsewhere. pean; numerous, but Patch of syenite. el Boulders on the south side of the 8 not visited by the author Boulders of syenitic granite. Moraine-like matter. Direction of the strie. S oe AS la WIGL A207 ours, o e = oT ” Quen, DS % nd py ily Wik ree LTT = Mn << z — = “thing Ut 3 uO (hirer . %, 5 lh pS Zz B a pARi@ q aS om SS J " ° ws me Xs BOS | - es nZewes & So olink ake sonigs SN : ic > f TTT a & / 2 “t ep EACHey <, L | 7 Vopy al : lI 3 Ww fe ~~ | 3 Nl ny = uy] | iQ’ Sill : = \l g o. f RS — pBrje. N.B.—The syenitic area, finely dotted in the map, is mainly after Macculloch. The boundary of the syenite on the south side of the Spean is unknown to me, and even that on the north sideis in some parts conjectural. There is much granite in the hill to the N.E. of Craig Dhu; butit is of a different character from the other.—T. F. J. 1862. | JAMIESON—GLACIATION OF SCOTLAND. 171 approach of two mountains, each about 3000 feet high; so that a glacier filling the hollow of the lake would, in issuing out into Glen Spean, be very much compressed by the narrowness of the gorge, and therefore act more powerfully upon the rocks along which it had to force its way: here then, if anywhere, we ought to expect some tokens of its former presence. Accordingly we find that the tough micaceous gneiss, all around the outlet on both sides, has a character that attracts attention even at a great distance. Although the strata are highly inclined, and present their outcrop to the lake, yet, notwithstanding this disadvantageous position, they have been ground down into rounded flowing outlines like those of a feather-bed ; and these domes and bosses of rock are scored in many places with long rectilinear furrows, in the direction of the lake, spreading out to either side like a fan as they recede from the gorge, just as might be expected from the action of a glacier issuing from the narrow pass, and dilating as it got out into the more open ground. One bare, flat Fig. 2.—View of the North Entrance to Loch Treig, from the hill on the North side of Glen Spean. =—SSS= SS SS ——— responding in height with the lowest of the Glen Roy li (854 feet above the sea). oy lines surface of gneiss, about 30 yards long, is beautifully smoothed, and covered with parallel scratches, scores, and flutings, running straight from end to end. The preservation of these markings so distinctly is very singular: no vegetation or covering of any kind appears to have sheltered them from the weather, and yet the frosts and storms of many ages have failed to wipe them out. It is right, however, to mention that such cases are exceptional ; for in most places, although the rock has a smooth rounded outline, yet only a few of the ruder scores are visible, and often none at all. On the angle of the hill at the west side of the outlet, this worn character of the rock is very marked, up to a height of more than 1000 fect above the present 1. Gravel terraces, cor 172 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, surface of the lake, while glacial scores running horizontally along the faces of the rock were traced up to 1280 feet (by aneroid) *. Not that I can affirm this to be their upper limit; for on the moun- tain, at the opposite side of the gorge, 1 found the scoring fade away so gradually at these great heights, owing to the weathering of the rock, that I was unable to satisfy myself where it ended, perched boulders and rounded surfaces occurring much higher; and even up to the top, which I made out to be about 3055 feet above the sea, the gneiss, although it runs in nearly vertical stratification (dipping N.W. at an angle of about 70° or 80°), is nevertheless so free of any loose fragments on its surface, and the ends of the strata are often so rounded in outline, as to raise a suspicion that some denuding agent has flowed over it at a period geologically recent. This absence of fragments cannot be attributed to the effect of the rain or snow gradually carrying them down; for it so happens that some felspar- porphyry is occasionally interbedded with the gneiss: one such stratum passes over the highest point of the hill; and this porphyry, like similar beds lower down in the gorge, is covered with a quantity of its own angular débris which has not been carried off by the rains. If the gneiss, therefore, had disintegrated to any extent, its débris ought still to be found lying on its surface lke that of the porphyry. As I have already said, the evidences of glacial action are very plain up to rather more than 1000 feet above the lake, and 1800 feet above the sea; and near the angle of the mountain, between Loch Treig and Corry Laire, I found at this great height moraine- matter, consisting of débris of mica-schist, gneiss, quartz-rock, and felspar-porphyry, forming a loose heap of stony rubbish, which the rains, aided by the scraping of the sheep, had laid open to a depth of 12 or 15 feet. The stones were of all sizes, up to about 3 feet in length, and many of them glacially striated. This moraine-matter may be traced down the spur of the hill for a long way, increasing in breadth. Corry Laire, I have no doubt, has also been occupied by a glacier ; and, looking down, I observed in the bottom of the glen what appeared to be moutonnéed rocks, but had no time to visit them. Nowhere have I met with such impressive evidence of intense abrading force as these rocks present all about the outlet of Loch Treig. The rounded masses of tough gneiss are so extensive as to form hills several hundred feet high, and so smooth and bare that, over extensive areas, even the moss and heather have completely failed to get a footing on their surface. The amount of mineral matter that has been ground down testifies how lengthened the period must have been during which the abrasion had gone on; and the preservation of the scores and scratches on the present surface, * These aneroid measurements have, of course, no pretensions to accuracy, and their results are given merely as the best approximation I can offer; yet I believe they are nowhere so far from the truth as to disturb any of the con- clusions drawn from them. Indeed, where I have been able to check them by other data, they have turned out to be nearer the mark than might have been ex-. pected, being seldom 50 feet wrong. 1862. ] JAMIESON—-GLACIATION OF SCOTLAND. 173 since the disappearance of the ice, is an excellent proof of the tough, indestructible nature of the substance it had to work upon. Well might Agassiz say of it, “I do not believe that a locality exists, where the facts indicate in a more special manner the cause which has produced them.” The River Spean, which receives the drainage of Glen Treig, runs from E. to W. at right angles to the direction of the lake; and just opposite the gorge there is a mass of syenitic granite, forming some low rocks that extend for some distance eastward. Now it is an interesting fact, that this granite lying on the north side of Glen Spean is, as Agassiz observed, ‘‘ not only polished with that polish charac- teristic of glacier-action, but is, moreover, scratched transversely— that is to say, at right angles to the direction of the valley—by a cause which evidently proceeded from Loch Treig.” (Ed. Phil. Journ. Xxxill. p. 238.) As the existence of these transverse markings has been disputed, I am glad to be able to confirm the accuracy of the illustrious Swiss, and may mention that an instance of such marking is to be seen on the north side of the Loch Laggan road, about 200 yards west of the thirteenth milestone from Loch Laggan Inn. Pro- ceeding down Glen Spean, the strize (everywhere to be seen) are found gradually to curve round from N. and 8. until they finally assume a normal east and west direction parallel to the valley, and at right angles to their former course ; and along the road for four miles west- ward, as far as the Catholic Chapel, the rocks are seen to be ground down more especially upon their east side, and, where not too much weathered, still showing the glacial scormg. Here I have to men- tion an important fact that seems to have escaped the attention of previous visitors; and it is this, that from a point in Glen Spean opposite the gorge of Loch Treig, all along the road to Loch Laggan, glaciated rocks are to be found, showing the scores running parallel to the valley, but it is now no longer the east, but the west, side of the rocky masses that has sustained most abrasion; and far away, even for three miles to the east of Loch Laggan, I traced the same appearances. For beyond the Pass of Makoul, the low rocky emi- nences show evident traces of the passage of ice going out towards the valley of the Spey; as if at a point in Glen Spean, opposite the gorge of Loch Treig, there had been an immense accumulation, which had parted there and gone out in two great streams, one taking an eastward route by Loch Laggan to the Spey basin, while the other flowed west, down Glen Spean, to swell the mass of ice at the mouth of the great Caledonian Valley. The following are some striking facts that will help to give an idea of the depth and volume of this great ice-stream. Glen Spean is rather a wide glen, and, for some miles below the junction of the Treig, is bounded on its north side by a considerable hill called Craig Dhu, on whose flank the lowermost of the parallel lines of Glen Roy is clearly marked. The bottom of the valley is here about 400 or 500 feet above the level of the sea, while the line is 847 feet, accord- ing to the levelling of an engineer employed by Mr. Robert Chambers. The top of Craig Dhu, by aneroid measurement, I made out to be 174 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, | | about 2100 feet above the sea, or 1250 feet above the level of the line, and, say, 1600 feet above the bottom of the valley. Now I found the flank of this Craig Dhu strongly impressed with marks of glacial action up to within a hundred yards or so of the very top. Rounded shoulders of rock, scored and fluted horizontally, sometimes even polished, may be seen in many places all over the side of the hill ; and it is worthy of notice that these appearances are well displayed immediately above, below, and even on the very line itself. The highest well-marked scores observed by me were at a level of 300 — feet below the top of the hill, or (say) 1300 feet above the bottom of | the valley ; but transported boulders (blocs perchés) occur up to near the very summit. From the brow of Craig Dhu to the brow of Ben Chlinaig, on the opposite side of Glen Spean, is a distance of two miles Fig. 3.—Outline-section across Glen Spean. s. Col at the head Ben — { Craig Dhu, of Glen Glaster, Chlinaig. River Spean. 2100 feet. 1060 feet, oy or so; here, therefore, is a striking proof of what a volume of ice must have swept down this valley, if these scores were caused, as I believe they were, by this agency. The rock of the hill, wherever I saw it, consists of micaceous gneiss or mica-schist, dipping N.W. at a very high angle, with some thin dykes or beds of felspar-porphyry. Now, the cropping out of the ragged edges of the gneiss-strata obliquely to the east must have afforded tough morsels for the bite of even a glacier-stream moving westward ; but notwithstandiug this disadvantageous circum- stance of the edges being presented towards, and their backs away from the stream, it became evident to me, after a careful examina- tion of much of the hill all along its south flank, that from top to bottom the scoring agent had moved from east to west. ‘This was apparent not only from the greater rounding and polishing of the east faces, but a further proof was afforded by the movement of rock- masses: for instance, from a great dyke of white quartz a large angular block had been torn off and carried some yards to the west- ward ; also porphyry fragments indicated a similar direction of trans- port. But there was another most striking and convincing proof of this nature. The gneiss over the hill-top being quite bare, or covered only by a thin peel of turf, it was easily seen that no other rock was present; it will therefore be admitted to be a highly interesting fact when I state that large angular boulders of syenitic granite, precisely similar in mineral quality to the low mass of that rock which occurs in situ in the bottom of the valley to the eastward, opposite the gorge of Loch Treig, are scattered in great numbers all over the brow of the hill, resting on the bare upturned edges of the enciss, Which is shorn and rounded into smooth outlines ; and what 1862. ] _ JAMIESON—GLACIATION OF SCOTLAND. 175 is very remarkable, the largest and most angular blocks are more numerous high up on the very brow of the hill, at a level of from 130 to 400 feet from the top, than they are further down. Thus, one measuring 12 feet long, by 9 broad, and 6 high, lay 130 feet lower than the summit of the hill ; a few yards from it was another 9 x 6 x 4; and at a level of about 400 feet below the top, or 1700 feet above the sea, was a magnificent block, 15 feet long, by 10 broad, and 6 high: this was the largest, and, from its conspicuous position on the bare brow of the hill, may be seen at a great distance, being visible with the naked eye from the Bridge of Roy Inn, four miles off. This is another very striking example of boulders being carried up far above the source from whence they were derived; and I have little doubt that these granite blocks have come from the patch of that rock in the bottom of the valley to the eastward; for no mineral mass of the same kind is known elsewhere in the neighbourhood, nor did I see any of it on the sides of Loch Treig, where, by the by, there is an absence of these fragments also. It has been suggested by Mr. Darwin that such cases might be explained by supposing the boulders to have been frozen into coast-ice and carried upwards during a period of submergence, when the land was gradually sink- ing; and it is also found to be the case that even the sea-waves, un- aided by ice, can during a heavy swell throw up boulders upon the rocks out of deep water. But neither of these explanations will, I think, suffice for the phenomena on Craig Dhu ; for, in the first place, there are no water-rolled pebbles accompanying these boulders ; and in the second place, the repeated stranding of the blocks by coast-ice or a heavy surf would, as Darwin admits, have rounded and reduced them to smaller size the farther up they were carried, whereas we see here that those most conspicuous for size and angularity are highest up on the very brow of the hill. I may also point out that the submergence of an isolated hill, like Craig Dhu, would have left its top but a little round speck of an island, where coast-ice would have had no shelter and been readily driven away. The scoring also of the subjacent rock, if caused by the stranding of the boulders either by coast-ice or waves, would not have been so horizontal and so steadily in one direction ; we should have rather found scores run- ning uphill, from the blocks being driven on it by the surf. The extraordinary profusion of these granitic boulders all about the valley, the manner in which such immense blocks are piled up one over another on the surface of heaps of moraine-like débris, and the way they have been elbowed up the slope of the hill opposite the gorge of Loch Treig, together with the strong scoring and polish on the rocks,—all seem to me to speak an unmistakeable language ; for I know of no agency, except that of a great glacier-stream, that could have effected all this. The granite boulders have been carried westward past Craig Dhu, for I found some of them on the top of Bohuntine—a hill on the west side of Glen Roy, nearly 2000 feet high, and of a remarkably rounded outline, as if it had been moulded by the passage of ice. In an oppo- site direction they have been carried towards Loch Laggan, affording VOL, XVIII.—PaRT I, 176 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Feb. 26, || another proof of what I before stated, namely, that the ice-stream had parted and gone out both to EH. and W. I even found some of them to the east of that loch, near Makoul. On looking up Glen Spean from the top of one of the hills, I was struck by the greater wear and smoothness of the hill-slopes flanking the valley, below a level of about 2000 feet or so; and this moulding I could not help attributing to the same agency that had so power- fully scored the rocks of Craig Dhu. I have been induced to describe the foregoing case somewhat minutely, because not only is it interesting from the clear evidence it affords of the extent to which the ice had been developed, but it is further important as affording a good example of a movement from both S. and E., thus enabling us to get rid of the notion which has been so prevalent, that this great glacial action had come invari- ably from the N. and W. I have still to mention a circumstance perhaps even more singular than any I have described, showing the remarkable state of ice- development that had once existed in this region. Just below Craig Dhu there branches off from Glen Spean, in a N. and N.E. direction, the well-known little valley called Glen Roy, extending in that course to the watershed of the River Spey. Near the head of the Roy, the Glen is contracted and nearly closed by some rocky eminences which seem to form its natural termination, and beyond which there is a wide hollow opening into Strath Spey. Now the surface of these rocky eminences presents clear evidence of glacial action, being rounded off and scored, and also dotted with occasional perched boulders ; but I was not a little surprised to find it quite apparent that the ice had come from the 8.W. up Glen Roy, and gone out in a stream towards the wide valley of the Spey. My first thought was that glaciers might have descended from Glen Eggie and other little side-glens which branch off here; but, on examining the rocks at the junction of the Eggie and the Roy, I found the furrows on the well- moutonnéed mica-schist passing right across the mouth of Glen Eggie; and the strata, which are almost vertical in position, have been so blunted and rubbed on their south-west exposure as plainly to show that the movement came from that quarter ; and high up on the brow of the adjoining hill (which is an extension of that marked Tom Brahn on most of the maps, but known to the shepherds by the name of Craig Corrak) I saw several very large blocks and boulders that appeared to have been shifted or moved some distance by glacial action. In Glen Roy itself, owing to the great accumulations of stratified débris, the rock is not well exposed, and, where seen, is often of a rotten, shivery nature ; so that, although I had remark -d some striated boulders, I had not seen any ice-worn surfaces except on the top of Bohuntine Hill, where however I could detect no scores or scratches, although the rock was much ground down. But on returning down the glen my eye caught some suspicious-looking lumps of rock on the flank of Ben Erin that had been bared of their earthy covering by the water of a descending rivulet; and on scrambling up to examine 1862. ] JAMIESON—GLACIATION OF SCOTLAND. 177 them, I found a few clearly marked glacial scores running horizon- tally along, at a height a little below that of the lowest Glen Roy line, while the worn and rounded edges looked down the glen. The amount of rock exposed and thus marked was but small; and I should haye attached little importance to the latter circumstance had it not been for the fact already mentioned of the rocks at the head of the glen indicating the motion of ice coming up it, and passing out to N.E.: for this would seem to show that Glen Roy had at one time been filled with ice, which, unable to get out by way of Glen Spean, owing to the vast accumulation in that direction, had been obliged to discharge itself at the upper end into the more open outlet of the Spey basin. When we consider the narrow character of the great Caledonian Valley, bordered by lofty mountains and numerous side- glens, and choked up as it must have been at its mouth by the jost- ling of all these united ice-streams pressing out past Ben Nevis, and recollect that proof has been adduced of Glen Spean being filled with ice to the level of the top of Craig Dhu, which exceeds by 900 feet the summit-level of this pass into Strath Spey, the above singular fact becomes less mysterious. § 5. I have yet another example I should like to give, as further illustrating and confirming what I have already advanced. In Argyleshire there is an arm of the sea called Loch Fyne, whose upper branch stretches 25 miles from §.W. to N.E. far into the High- lands. The scored and polished rocks all along its shores; from In- verary down to Loch Gilp, plainly indicate the former passage of ice down the loch; their rounded, worn sides facing the interior, and the rough and more jagged outlines the sea. At Loch Gilp (which is a small inlet off the west side of the lake), a low tract, forming the bed of the Crinan Canal, runs across in an eastern direction to the Sound of Jura. The rocks along this hollow are likewise much worn and rounded, but chiefly on their eastern sides, and scored by glacial furrows pointing W., parallel to the canal, and indicating the course of an ice-current diverging from Loch Fyne. On looking at the map it will be seen that, if we produce the line of Upper Loch Fyne in a, south-west direction, it would run across Knapdale into Jura Sound, near Loch Killisport. Now, I find the gla- ciation of the rocks of Knapdale looks as if the stream of ice descend- ing Upper Loch Fyne (so great had been its volume, and so immense the wis a tergo impelling it onwards) had gone right out, over hill and dale, into the Sound of Jura. Let any one who wishes to satisfy himself of this examine first the course of the Crinan Canal, and he will find the masses of syenite, in the hollow beside the Dunartry locks, all worn and rounded on their south-eastern sides; and searching where the drift has recently been removed, he will find scores and polish indicating a motion to N.W. Let him then ascend the hill- slope from Cairnbaan, following the course of the ravine down which the torrent came when the reservoirs burst, and he will see the scores at the mouth of the stream running from E. 30° 8. to W. 30° N.; ascending the slope of the hill, he will find the scores turn- ing gradually to due E. and W., and, as he goes higher up, curving nw 2 178 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, more and more round to the N. of E., and, what will probably sur- prise him, as it certainly did me, he will see evidence that the agent which impressed these furrows moved obliquely uphill, mounting a slope of 700 or 800 feet; he will then find himself on a sort of table- land spotted with several small lakes, and along the rocky sides of these reservoir-lakes he will observe some of the most beautiful ex- amples of glaciation I have ever seen—long rectilinear grooves run- ning uninterruptedly onwards from N.E. to 8.W. for many yards, with all lesser degrees of scratching and polish. Let him then ascend over the ridges towards Cruach Lussa, and he will no longer Fig. 4.—Profile of the Ice-worn Knolls of Greenstone at the Crinan Canal. W. E. i Pnalitn. find these markings on their bare, weathered fronts; but he will notice the rounded snouts they present invariably to the N.E., and the more rugged outlines to the 8.W. Let him then continue all along until he gains the top of Cruach Lussa, the highest point in North Knapdale (and 1530 feet above the sea, according to the Admiralty chart), from whence, if the day be fine, he will have a view .of one of the most beautiful scenes in Scotland, which alone will recompense his toil if he be no geologist. § 6. The ice, therefore, descending by Loch Fyne, seems to have passed round and over this hilly ridge, just as the water of a river flows round and over a large boulder in its bed. It seems odd to talk of a glacier doing this ; but nothing short of ice, filling the valleys up to the brim, and covering the whole country in one great winding-sheet, will meet the requirements of the case. In short, we should have to describe it just in the way Rink speaks of Greenland, when he tells us that a spectator standing on the top of a mountain near the coast sees the various ice-streams “ approach and unite in an icy level occupying the whole of the eastern tract or area of the continent,” and which annually discharges its enormous excess in those great icebergs that infest Baffin’s Bay and the neigh- bouring seas. <“‘ To have a correct idea of the glacial accumulations in Greenland,” says that observant voyager, Dr. P. C. Sutherland, “‘ we must imagine a continent of ice flanked on its seaward side by a number of islands, and in every other direction lost to vision in one continuous and boundless plain. Through the spaces between these apparent islands the enormous glacial accumulations slowly seek their passage to the sea.”” In Melville Bay (lat. 75°), it presents to the sea one continuous wall of ice, unbroken by land for a space of 70 or 80 miles; and the average thickness, he tells us, is 1200 to 1500 feet, but in some of the valleys upwards of 2400 feet (Journ. of Geol. Soc. ix. p. 301). Somewhat similar, but much more 1862. ] JAMIESON—GLACIATION OF SCOTLAND. 179 extensive, is the ice-covering of the Antarctic Continent, where Sir James Ross traced a continuous vertical cliff of ice, more than 1000 feet thick, for 540 miles ; and detached portions were found 60 miles from its main edge, aground in 1560 feet of water. We see, therefore, that in certain parts of the globe land-ice attains a thickness at least as great as is required for the most extreme eases I have adduced in this paper, even allowing that the bottoms of the valleys had been as deep as they are at present when the ice reached the highest scores now found on the flanking hills, which is not at all likely ; for I believe that the grinding of the ice for many ages along the glens must have powerfully eroded its bed, and worn the bottoms of the valleys much deeper than they were at the commencement of the Glacial period, and in fact occasioned an amount of denudation of the surface which has been much too little allowed for. It may seem more probable to some, that the curious features in the erosion and scoring of Knapdale may be owing to the relative levels of the district having undergone considerable derangement since the time at which the rocks were so marked ; and indeed, when I first observed them, this seemed to myself the most likely explana- tion; for although I could not, after much careful examination, resist the evidence of the movement having been uphill over much of the ridge, I felt much puzzled by the fact of the rocky masses on the top towards Cruach Lussa being so uniformly worn on their north-east exposure, while those in the bottom of the Crinan valley were abraded on their east and south-east sides, indicating a move- ment diverging at right angles from Loch Fyne, where there is at present a wide opening to the sea. But after studying Lochaber, where the facts seem to me clearly to indicate the presence of land- ice in a volume quite as extraordinary as would account for the phe- nomena in Knapdale (allowing for erosion of the bed of Loch Fyne by the long passage of the ice, as I have above suggested), I am inclined to think that it is unnecessary to require any great local derangement of level. Those who would solve the facts I have adduced in this paper by means of floating ice have to show how the winds or currents that moved it could have radiated from the central heights of Scotland to all points of the compass, and in each district have always persisted so steadily in one direction ;—how, for example, from a point in the middle of Glen Spean, at the junction of the Treig, winds or currents could have set out in opposite directions, and in both cases at right angles to the line of movement in Glen Treig ;—how the movement on one side of Scotland should have been continually from W., and on the other from E., and on the north coast from §., and always from the land side ;—how blocks, 15 feet long, could have been by such an agency lifted up out of the bottom of a valley, and set down on the bare brow of a hill hundreds of feet above their source. The advocates of a débdcle have, on the other hand, to show how a sudden and transitory movement, even although repeated, could have lifted these blocks and have worn down ragged masses of tough gneiss at 180 _ PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, the mouths of the fiords of Argyleshire, and at Loch Treig, into smooth rounded domes, and scored the rocks in a direction so rigidly even ;—how, on the brow of a hill like Craig Dhu, at the height of 1200 feet above the bottom of a wide valley, it could impress hori- zontal scores and fluted hollows along the face of a shelving rock- surface. | § 7. Land-ice moving in a volume like that seen in Greenland or in the Antarctic Continent explains these and many other facts better, In my opinion, than any other theory yet proposed; and, so far as I can see, the only strong objection against it is the extraordinary climate for this latitude that it requires: but some such extraordinary climate is quite necessary to account for the fact of arctic quadrupeds, such as the Reindeer*, Musk-ox, the Lemming, and the Lagomys, having ranged into the south of England and the heart of Germany during the Drift-period; and one of these Lemmings (Myodes torquatus), whose remains were found by Dr. Hensel of Berlin in the Drift near Quedlinberg, is said to delight in so arctic a climate as seldom to ramble further south than the northern limit of the woods, and was found by Parry in latitude 82° N. We cannot suppose these ani- mals to have been mere stray wanderers; for in one of the Welsh caves, called Bosco’s Den, Dr. Falconer tells us, upwards of one thou- © sand antlers, mostly shed, and of young animals belonging to the Cervus Guettardi and C. priscus—species or varieties allied to the Reindeer—were found in the bottom of the cavern (Journ. of Geol. Soc. vol. xvi. p. 489). Such facts as these, together with boreal and even arctic shells (like the Cyprina Islandica and Natica clausa) inhabiting the Medi- terranean shores of Sicily, bespeak a climate perhaps as severe as, with a certain amount of elevation, would account for Greenland con- ditions in our latitude. “Not even on the verge of the arctic province,” says Edward Forbes, in his last work, “ are we to seek for the ana- logue of the fauna of the Drift, but within its strictest bounds ;” and yet this marine Drift to which he refers does not represent the time of severest cold, which was that of the great land-glaciation. We have therefore two sets of facts entirely different from each other, one from the organic, the other from the inorganic kingdom, and both alike demanding an arctic climate for their explanation. We cannot account for such a development of ice in this country without supposing the whole of the atmospheric moisture, or nearly so, to have fallen in a frozen or snowy condition, and to have had to find its way off the land in the shape of solid ice; and such a climate in the latitude of Scotland cannot with any probability be supposed without some great changes in the physical geography of the north- ern hemisphere ; for it comes to this, that the whole of Scotland must, during the period of greatest glaciation, have been within the snow-line, which renders the conclusion, I think, probable that our island must have then stood far higher above the sea-level than it does at present. Without supposing some such great elevation, * The recent discoveries of Lartet in the cave at Aurignac show that the ~ Reindeer inhabited even the Pyrenees. 1862, ] JAMIESON—GLACIATION OF SCOTLAND, 181 the case would certainly be very marvellous ; for even in Greenland, except at its nortuern extremity, the lower limit of the ice-covering, Rink tells us, is far above the coast-line, and it is only the larger glaciers that protrude into the sea; in the intermediate tracts, the snow and ice lying below the level of 2000 feet annually disappear before the heat of June. The whole of Norway, Sweden, and Lap- land appears to be ice-worn from the mountain-tops down to the sea, and a general view of the whole brings out the fact that the scores radiate from the central heights to all points of the compass. Along the coast of Norway they run to W. and N.W.; in Lapland, to N. and N.E.; in Sweden, to E. and 8.E.* The phenomena, as a whole, seem to be better explained by land- ice moving from the central plateaux downwards and outwards than by any other theoryy. In order, therefore, to account for this great glaciation of Britain and Scandinavia by land-ice, it is necessary, I think, to suppose that the elevation of these countries above the sea must have been much greater than at present. As regards Scotland, indeed, there can be little doubt of this, if we admit the markings I have described to have been caused by that agency ; for along all the wide mouths of its sea-lochs or fiords the glacial scoring everywhere - dives in full development underneath the present sea-level, and the same appears to be the fact in Norway and Sweden. Without sup- posing some such elevation, I do not see how a degree of cold at all like what seems to have prevailed can be accounted for, without sup- posing either the sun’s heat to have suffered some great diminution, or the position of the earth’s axis to have differed from what it is at present; and, even granting the elevation, the fact is very re- markable. $ 8. But, while apportioning to land-ice its due share in the events of the Drift-period, let us not forget the strong evidence which we possess of the great submergence that took place afterwards. No action of land-ice, for example, will account for the marine shells and chalk-flmts on Moel Tryfan, in Wales, at the height of 1392 feet ; and a mass of good evidence has been collected to show that this sub- mergence amounted to at least some hundreds of feet in various parts of England, Scotland, and Ireland, as well as in the Scandinavian * Tt is alleged, however, by Horbye and others, that in the midland region there is a remarkable exception to this rule. They state, indeed, that between lat. 62° and 633°, the erosive agent proceeding out of the relatively low ground of Sweden has marched wp/zi/ right over the Dovrefjeld! ‘Sans exception, toutes les stries qui se trouvent sur la frontiére mentionnée entre le 62™¢ et 633 dégré de latitude ont leur point de départ dans les contrées de la Suéde relativement plus basses.” (Horbye sur les Phénoménes ‘d’érosion en Norvége, p. 40.) And the author of the memoir quoted had traced this “ bwrinage erratique” to an elevation of 4590 Norwegian feet above the sea: he also quotes the authority of M. Durocher in support of this assertion as to the ascending movement of the erosive agent. . t “We generally find that the polished or opposing side (Stos-Sette) of the rocks is turned towards the principal plateaux of these countries. It is from these plateaux that the impelling power seems to have originated which deter- mined the direction of the bodies which scooped out the grooves.” (Bohtlink, Ed. New Phil. Journ. xxxi. p, 253.) 182 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 26, peninsula; sea-shells being found up to these heights imbedded in what look like marine strata. The mere presence of transported boulders, it is evident, can no longer be considered as a sufficient proof of sub- mergence if the existence of an extensive covering of land-ice be once admitted. For the transport of boulders floating ice is doubtless a very efficient cause, but equally so is land-ice ; each case, therefore, must rest on its own merits. The polishing and scoring of the rocks, however, will, I think, be found to have chiefly resulted from the latter cause, at least in this country ; but there are some curious cases for which probably few will be disposed to admit this explanation: such are the north-east strie at the extremity of the Island of Anglesea and on the Isle of Man, proceeding apparently from a cause exterior to these islands; also those parallel to the coast at Bray Head in Ireland, pointing N.E. However improbable it may seem, it will be well to bear in mind that it would be possible for land-ice to have caused these markings, supposing it to have been developed to an ex- tent sufficient to fill the bed of the Irish Channel. Without venturing to say that it did so, I merely point out that, had such been the case, it might have marked these rocks in the way we find them to be. The continental ice of Greenland fills areas more extraordinary. § 9. It is therefore very necessary that we should have some criterion — whereby we might be able to distinguish glacier-action from the action of floating ice. Mr. Darwin, in an excellent paper on the glaciers of Caernarvonshire, suggested that boss- or dome-formed rocks would probably serve as such. Another circumstance that, I think, should help us is the case of a deep hollow surrounded by a ridge on the side from whence the glacial agent has come. Such a ridge would evidently defend the hollow from the grounding of floating ice coming from that side, but would be of no avail against the erosion by a gla- cier. Now, such instances are frequent in Scotland. The well- rounded and scored gneiss which I have cited in the deep hollow of the east Kyle of Bute, opposite Colintrive, is one; that of the Gare- loch, described by Mr. Maclaren, is another ; the remarkable case of the reservoir-lakes of Knapdale may be mentioned as a third. Again, the steadiness of the direction of the striz would seem to be incon- sistent with the action of floating ice, unless in the case of deep- swimming icebergs in an open sea, moving under the steady influence of an ocean-current ; and how could these have grazed the bottoms of our intricate glens ? In the case of the Gareloch, Maclaren found that the bearing of the strie over a length of seven miles does not vary more than a point to the right or left of the axis of the}lake, and they are most clearly marked at the lower levels. Now, in Baffin’s Bay, Dr. Sutherland tells us the icebergs tumble about and butt against each other in great confusion, like houses in an earthquake, and also occasionally assume a rotatory motion from the pressure of ice-floes against them. Further, when an iceberg strikes against a sunken ridge, it will push the broken fragments of the rock over into the first deep hollow, and there leave them ; and, if grounded, it ‘would rock about by the action of the surf and thus cause irregular . curved markings unlike the straight ones that we always find. 1862.) - JAMIESON—GLACIATION OF SCOTLAND. 183 ~§ 10. In Scotland the whole débris resulting from the erosion of the rocks has often been swept clean off,—over most of the glens in the North and West Highlands such is the case to a remarkable Fig. 5.—Sketch-map of Scotland, showing the Direction of the Glacial Markings observed in different parts of the country. le [5 |4 =| A\ N.B.—The headless arrows indicate that the side from which the agent moved is not certain. —>— Direction of Glacial striz. Notz.—In this little map I have availed myself of the materials contained in a map of the middle region of Scotland which accompanied an excellent paper by Mr. C. Maclaren in the ‘ Edinburgh New Philosophical Journal’ for 1849, and likewise of various scattered notices by Murchison, Nicol, Milne-Home, Cham- bers, Forbes, and Smith of Jordan-hill. degree. Iwas much struck with this on the high barren ridge border- ing the Crinan Canal, where the reservoir-lakes are situated. The 184 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, upturned edges of the vertical strata there are in many places striated, and show great marks of erosion, as I have already mentioned ; and the interstratified beds of greenstone, which are very numerous, stand out like great Cyclopean walls, running for miles high above the softer slaty beds that have yielded more to the action of the ice. But almost the whole wreck of the strata has been carried off, as if the rocks had been swept bare with a great iron besom. Some of the protruding trap-dykes that attracted the notice of Macculloch in many parts of the Western Isles, and were referred by him, with hesitation, to the tedious operation of the atmosphere, are, I have no doubt, due to this erosion of the softer beds by the ice. The geological period to which this great glaciation of Scotland belongs was probably contemporaneous with the formation of those “‘ subaérial” beds on the borders of the English Chanrel, described by Mr. Godwin-Austen, and referred by him to the time succeeding the Norwich Crag. That, at least, it was not of much older date, I am led to think from the discoyery of some patches of what appears to be Red Crag in the low coast-district of Slains, in Aberdeenshire, that have partly escaped the denudation caused by the ice. In addition to the Mollusca recorded at p. 372 of the 16th vol. of the Quart. Journ. of the Geol. Soc., I have since found in these so-called ‘‘ Crag” beds of Slains what I believe to be fragments of the Voluta Lamberti, Nassa elegans, and Nucula Cobboldie—three shells eminently characteristic of the Crag-period. Nowhere, however, have I found in them any glacially striated stones ; and the absence of these I consider an im- portant fact, showing that glacial action had not then begun in the neighbourhood. If this development of land-ice coincided with an elevation of a great part of Europe, we may expect to find, to the south of the ice- covered region, traces of contemporaneous freshwater deposits, and remains of the continental fauna that flourished during the long period that the North was covered with ice. The valley of the English Channel and the southern portion of the German Ocean were then probably dry land, and may have been haunted by mam- malia of various kinds, and hence the quantity of Elephants’ teeth and bones they contain. Toa part of this period probably belongs the ‘‘ forest-bed ” underlying the boulder-clay of the Norfolk coast, and whose tree-stumps are rooted in the Norwich Crag. Marcu 5, 1862. George Ford Copeland, Esq., M.R.C.S., 5 Bay’s Hill Villas, Chel- tenham; William James Dunsford, Esq., 14 Taviton Street, Gordon Square; Charles Henry Gatty, Esq., F.L.S., Felbridge Park, Hast Grinstead, Sussex; and Alexander Henry Green, Esq., M.A., Fellow of Gonville and Caius College, Cambridge, were elected Fellows. The following communication was read :— * aya SUP hy bP a, one 2 eS i é : a; % Ns d r : " ' 5 y P ‘ ? 4 tb hy 4 , he j rie CR Ate ly cok tld 0A Le th MB in ell Geta é W mu Wh v8 gguove Val Tedlina & Como Aosta & Ivrea QUES rb of the map of Lar Ma. v Reuss & Lucerne Tinth 8 Zurich Rlane & Constance Aar S- Thauav of SWITZERLAN D Lago N°1. Glacier of the Rhone & Geneva o” mn in # Mot ANCIENT GLACIERS 6 SHR S Sketch tYy yyy! ZW) i 7 Yi MSs Y S RT, 4 ' WN WY \ Ye yy: iN Zips} \ JW. Lowry feulpt. | | il iin i ( 1862.] RAMSAY—GLACIAL ORIGIN OF LAKES. 185 On the Guactat Ortern of certain Laxes 7 SwiTZERLAND, THE Brack Forest, Great Britain, Swepen, Norra America, and elsewhere. By A. C. Ramsay, F.R.S., President of the Geological Society, de. [Puate VIII.) ConTENTS. Erroneous theories of the Transport The Lake of Lucerne. of Alpine Blocks: reasons for aban- The Lake of Zurich. doning them. The Wallen See. Old Distribution of the Great Alpine The Lake of Constance. Glaciers. The Italian Lakes. Connexion between Tarns and Gla- Summary with regard to the Alpine ciers. Lakes. Origin of the Great Alpine Lakes. Lakes of the Northern Hemisphere The Great Lakes :— generally. The Lake of Geneva. The Glacial Theory. The Lake of Thun. Erroneous Theories of the Transport of Alpine Blocks.—In the year 1859, in a series of papers by the members of the Alpine Club, I published a memoir in which I compared the old glaciers of North Wales with those of Switzerland; and in it, among other matters, I explained the glacial origin of certain rock-basins now holding lakes, on the watersheds and in the old glacier-valleys of both those countries ; and in a later edition of the same memoir, published as a separate book, with additions*, I extended these generalizations to many of the lakes in Sutherlandshire. In the same work I also expressed an opinion that the blocks of Monthey, in the valley of the Rhone, and the great erratic boulders that strew the southern flank of the Jura had been transported by icebergs derived from glaciers which descended in the Alpine valleys to the sea-level, during a period of submergence in which the low country that lies between the Jura and the Oberland was covered with erratic drift. There was nothing new in this latter opinion, for it had previously been held by several distinguished geologists, both English and con- tinental. Since then I have twice revisited Switzerland, and have seen good reason to change my opinion respecting the cause of the trans- port of erratic blocks to Monthey and the Jura, and of débris not remodelled by rivers, &c., that lies scattered over the lowlands of Switzerland, or that borders, or lies in great mounds well out in, the plain of Piedmont and Lombardy. I am now convinced, for example, that the vast circling moraine of Ivrea, noticed by Studer in 1844, was shed from a glacier, 105 miles in length, that filled the valley of Aosta to a height of more than 2000 feet, and protruded far into the plain; while on the north a still greater glacier, long ago described by Charpentier, flowed from the valley of the Rhone right across the low country until its end abutted on the Jura. As there are still many persons in England who doubt these conclusions, it ‘The Old Glaciers of North Wales.’ Longman & Co. a Quart. Journ: Geol: Soe-VoLXVIL. PL-Viit Sketch-map of Fart of the ANCIENT GLACIERS of SWITZERLAND. N°. Glacier of the Rhone & Geneva MihThaisen 2 z, A ., dar & Thun 2: - a . Reuss & Licerne 4 , . . Linthy & Zurich Mh 5. Rhine & Constance 6. 5 — 5, fago: Maggiore %, = : Val Tellina & Como WS 8 Aosta & Ivrea mi TRG Moraines m WAN wi = er < eutch. aS ob oligny Cc AAW! al yy, : WINS = clay PS ING = RAG GS ge? ORIN A WA : Ih WNW Ainiave it ' a Wi Borrbxa il 7 i ie i IW. ealtieehddiederen 22) Eee a ill aa eae ee ee 186 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, may not be beside the question to state the considerations that led me to reject the old theory. Reasons for abandoning the older theories.—I first began to doubt the correctness of my earlier opinions in the summer of 1860, while examining the country near Bonn, the banks of the Moselle, and the Eifel. Neither in the valleys nor on the wide table-lands on both sides of the Rhine and the Moselle is there any sign of glacial drift. Excepting alluvial débris in the valleys, the native rock is generally quite bare of transported detritus ; and the only marks of glaciation lie low on the sides of the Moselle, where the floating down of the river- ice has frequently rounded, polished, and striated the rocky banks in the direction of the flow. Boulders, transported from further up the stream, also sometimes le on the shores. But, in the absence of true drift, I considered that, had Switzerland been depressed at least 3000 feet, ‘until its mountains were washed by a sea that floated trans- ported blocks to the higher Jura, the table-lands of Rhenish Prussia and Westphalia would also possibly have been submerged, and more or less covered with glacial detritus. Further up the Rhine and in the Black Forest the same absence of marine drift prevails. There, looking eastward towards the Rhine, the mountains, chiefly of gneiss, are wonderfully scarred, telling the observer of the wasting effects of frost, ice, rain, and rivers, probably ever since the close of the Miocene period. In the valley of Oberweiler, between Mullheim and the watershed, I observed occasional heaps of moraine-like detritus, in which by diligent searching I found a few stones marked with the familiar glacial scratchings. In the interior towards Schonau and the Belchen, the rocks being generally soft and schistose, no very decided signs of old glaciers occur, and no part of the country shows symptoms of the presence of drift. Altogether the country looks as if it had stood in the air _ for so great a period that, even if glaciers were once present, they had disappeared so long that all the more prominent signs of degra- dation are now due to rain and running water. But further in the interior it is altogether different; for the signs of old glacier-ice are plentiful enough, and for miles round the Feldberg, which rises 4982 Baden feet above the sea, the sides of the valleys to the very summits of the mountains are often strikingly moutonnées, though the rounded forms are generally roughened and frequently half ruined with age. On these, striations, though rare, may occasionally be discovered (running in the direction of the valleys), although the rapid rate at which the rock weathers is much against their preservation. Moraines also are not uncommon. At the foot of the Feldberg, on the east, there is a beautiful circular lake, called the Feldsee, surrounded by tall cliffs of gneiss and granite in the shape known in Scotland as a corrie—a form eminently charac- teristic of all glacier-countries past or present. The outer side of the lake is dammed up by a perfectly symmetrical moraine, curving across the valley, and formed of sand, gravel, and of granite and gneiss, often in large boulders. It is now covered with pine- trees. The lake is deep, and the moraine rises from 25 to 40 feet 1862. ] _ RAMSAY—GLACIAL ORIGIN OF LAKES, Sa above the water. Outside the moraine lies a flat marsh, still retaining traces of having been a lake, once also dammed by a second and outer moraine, formed chiefly of large angular blocks of gneiss, piled irregularly on each other like the old moraine of Cwm Boch- lwyd, above Llyn Ogwen in Caernarvonshire. Quantities of moraine- matter strew the valley for two or three miles further down to the little marshy lake at Waldbauer, which is also dammed up by moraine-rubbish, in one place rudely stratified, like some of the old moraine-heaps on the Jura and parts of the great moraine of Ivrea; or like the heaps of glacier-débris that often border the lakes marshes, and flat peat-mosses, once lakes, that diversify the iowlands of Switzerland. At the upper end of the Alb Thal also, at the entrance of Menzenschwanden Alb, I saw four moraines curving across the valley, arranged concentrically one within another, like those at the end of the glacier of the Rhone; and for many miles in the Alb Valley, both above and below St. Blasien, roches moutonnées stand like islands through the alluvium, while it is also plain that the sides of the mountains above have been to a great height smoothed by ice. Nowhere however down to Allbruck, where the river joins the Rhine*, did I see any “ drift ;” and this village lying close on the north side of the Jura, it seemed impossible that the higher ground on the south side of that range, between the Lakes of Constance and Geneva, should have been submerged during any part of the Glacial period, while the country on the Rhine above Basel remained above the sea. I therefore saw that the theory that the Prerre a bot and its companion blocks had been floated from the Alps by marine ice- bergs was untenable ; and a later examination of a portion of the Jura, partly under the able guidance of Professor Desor, fully convinced me that the ice that descended the great valley of the Rhone had covered much of the low country and abutted on the south-eastern flank of the Jura. Old Distribution of the Great Alpine Glaciers.—At that period, then, of extreme cold, when the glaciers of the Alps flowed right across the Miocene basin of Switzerland, a glacier of vast thickness (No. 1 on the Map, Pl. VIII.), running from end to end of the upper valley of the Rhone, debouched upon the lowlands at what is now the eastern end of the Lake of Geneva, and spreading in a great fan-shaped mass extended to the south-west several miles down the Rhone below its present outflow from the lake, and north-east to the banks of the Aar, about half-way between Solothurn and Aarau. The length of this fan-shaped end of the glacier, from north-east to south-west, was about 130 miles, and its extreme breadth about 25 miles. Another great glacier (No. 5) descended in a direction opposite to the higher part of the Rhone glacier, through the upper valleys of the Rhine, and debouched upon a wide area that extends from Kaiserstuhl on the Rhine, far to the north-east. In the centre of this area lies the Lake of Constance. Between these, which were the largest glaciers on the north watershed of the Swiss Alps, several smaller, but still enormous, glaciers flowed in a north-westerly direction from the * Between Basel and the confluence of the Aar and the Rhine. 188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 5, mountains,—one down the Linth, through the area now occupied by the Lake of Zurich (No. 4), another down the Upper Reuss, across the area in which lie the Lakes of Lucerne, Zug, and others (No. 3), and a third down the valley of the Aar to Berne, through the country that now contains the Lakes of Brienz and Thun (No. 2). Accord- ing to this view (the result of the researches of the best Swiss geologists), the greater part of the Swiss Miocene area lay deep under - ice*, and I am inclined to think that the country between the great old glaciers of the Reuss, Aar, and Rhone was much more covered with ice than any map shows, the whole helping to swell the pro- digious glacier of the Rhone that abutted on the Jura. Connexion between Tarns and Glaciers—In ‘The Old Glaciers of North Wales’ I have shown that in all glacier-countries, whether past or present, there is an intimate connexion between tarns and glaciers. Some of these are dammed by old morainest, but the greater number lie in rock-basins, formed by the grinding of glacier- ice asit passed across the country, whether in valleys, on rough table- lands, or on the watersheds of passes. These lakes and pools are of all sizes, from a few yards in width, lying amid the mammillations of the roches moutonnées, to several miles in diameter. Sometimes in the convolutions of the strata (conjoined with preglacial denudation subsequent to the contortion of the beds), softer parts of the country may have been scooped out, leaving a hollow surrounded by a frame- work of harder rock ; but perhaps more generally they were formed by the greater thickness and weight, and consequently proportionally greater grinding pressure, of glacier-ice on particular areas, due to accidents to which it is now often difficult or impossible to find the clue. Trifling as this phenomenon at first sight may seem, I yet believe the manner of the formation of these lakes is of much importance to — the right understanding of the glacial theory, whether taken in con- nexion with the great extension of extinct glaciers in recognized glacier-regions, or, further, when viewed on a general continental scale; for the theory of the glacial origin of many rock-basins must, I feel convinced, be extended much beyond such mountain-districts as Switzerland, Wales, and the Highlands of Scotland, where they first attracted my attention {. | Origin of the Great Alpine Lakes. Subject stated.—From the con- sideration of the origin of mountain-lakes and tarns, the question easily arises,— What are the causes that have operated in the formation of the great lakes of Switzerland, such as those of Geneva, Zurich, and Constance, and, south of the Alps, of Maggiore, Lugano, Como, * The limits of the northern glaciers on the Map (PI. VIII.) are chiefly given from a MS. map compiled by M. Morlot. Those on the south are taken from a map by M. de Mortillet. Both were lent me by Sir Charles Lyell. a Quart. Journ. Geol. Soc. 1851, vol. viii. p. 371; and ‘Old Glaciers of North ales.’ { It is not to be supposed that I attribute the origin of all rock-basins to glacial action. Many le in the craters of extinct volcanos, some, no doubt, in areas of special subsidence, and others may be due to causes of which I know nothing. I now confine my remarks to certain lakes common in all highly glaciated regions such as I know. 1862. | RAMSAY—GLACIAL ORIGIN OF LAKES, 189 and others? To answer this with precision, it will be necessary, first, to examine seyeral other hypotheses that by some may be thought sufficient to account for them. It is well known that after the close of the Miocene epoch the rocks of the Alps were much disturbed,—a circumstance proved by the contortion of the Miocene strata, as for instance in the neigh- bourhood of Lucerne, where, on the Rigi (and in other conglomeratic mountains on the same strike), the strata are considered by the best Swiss geologists to be repeatedly folded and fairly inverted, so that the basement-beds form the top of the mountain instead of its bottom, thus, by reversal of dip, plunging under the Eocene and Cre- taceous strata of the mountains further south. The whole, as shown by the rapid truncated foldings and the escarpments of the hills, has since been much denuded, the denudation being of a kind and amount that, to effect it, proves the lapse of a long period of time. Wit- ness the outliers of Miocene strata in the upland valleys of the Jura. Among these disturbed and denuded strata of Miocene and of older dates, the Lakes of Geneva, Thun, Brienz, Lucerne, Zurich, Constance, the Wallen See, and the great lakes of North Italy he. A knowledge of the stratigraphical structure of the Alps, in my opinion, proves that these lakes do not lie among the strata in basins merely pro- duced by disturbance of the rocks, but in hollows due to denuding agencies that operated long after the complicated foldings of the Miocene and other strata were produced. First, none of these lakes lie in simple synclinal troughs. It is the rarest thing in nature to find an anticlinal or a synclinal curve from which some of the upper strata have not been removed by denudation. I never yet saw a synclinal curve of which it can be proved that the uppermost stratum in the basin is the highest layer of the formation that was originally deposited over the area before the curving and denudation of the country took place. The only approach to this may possibly be in the upper valleys of the Jura, where a part of the Miocene beds lie in basins separated by second- ary anticlinally curved strata, the tops of the anticlinal bends having been removed by denudation ; but these cases are surrounded with difficulties. ‘The lake-hollows in the Alps are, however, encircled by rocks, the strikes, dips, and contortions of which often exhibit denu- dation on an immense scale; and in no case is it possible to affirm, here we have a synclinal hollow of which the original uppermost beds remain. If these beds have disappeared to a great extent, then it is evident that denudation has followed disturbance. The frag- mentary state of the uppermost Miocene strata of the lowlands of Switzerland proves this denudation. Again, if it be argued that in the lake-areas these denudations have been produced by the waters of the lakes, it is replied that, though waves may form cliffs, neither running nor still water can scoop out deep trough-shaped hollows. Secondly, the same kind of argument applies to areas of mere watery erosion by rivers. Running water may scoop out a sloping valley or gorge, but (excepting little swallow-holes) it cannot form and deepen a profound hollow, so as to leave a rocky barrier all 190 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 5, round ; though it may fill with sediment one that had previously been formed. Thirdly, neither do most of the Swiss lakes lie in lines of dis- location. For many reasons I do not believe that any one of them among the high Alps or on their flanks can be proved to lie in lines of mere gaping fracture. Let us consider the nature of such fractures. In any country where the strata are comparatively little disturbed and lie nearly horizontally, if it be faulted, there is no reason why the fractures should be open. In the Oolites, for example, in the South of England, where faults are numerous, and in the New Red Sandstone of the central counties, there is generally a simple dis- placement of the strata up or down, on one side or the other; or, if the. disturbance go beyond this, it is that along the sloping line of fracture the beds on the downthrow side are turned up, and those on the opposite side bent down, by pressure and slipping combined. In more disturbed districts, ike the Welsh Coal-measures, the same phenomena are observable: witness, for instance, the numerous sec- tions from accurate observation, drawn on a true scale, by Sir Henry De la Beche, Sir William.Logan, and others. Experience both above ground and in mines proves the same. Most lodes are in frac- tures, and many lie in lines of fault. In metamorphic, excessively contorted, and greatly fractured districts like those of Devon, Corn- wall, and Wales, the cracks, whether bearing metals or not, vary from mere threads to a few fathoms in width. They are always filled with quartz or other foreign substances, frequently harder than the surrounding matrix. I have often traced lodes on the surface, in Wales, by the hard matter filling the crack standing in relief above the surface of the softer enclosmg rock. In lime-. stone rocks the cracks are usually partly filled with crystallized car- bonate of lime. Lines of fracture are not, therefore, for purposes of denudation, necessarily lines of weakness, unless it happen that on opposite sides of the fault hard and soft rocks come together, when of course the softer rocks will wear away more rapidly, and generally originate a straight valley. Again, in an excessively contorted ed such as the Alps, it is, I believe, impossible, in consequence of that contortion, that there should be gaping fractures now exposed to view. Assuming for the sake of argument the sudden violent contortion of the strata of any great tract of country, we shall see that the contorted rocks now exposed at the surface, even if broken, would be most unlikely to gape. The expression “elevation of mountains” conveys to the minds of many persons the idea that the elevation has been produced by some force acting from below, along a line in the case of a chain, and on a point of greater or less extent when the mountains lie in a cluster, as a whole, more or less dome-shaped. Such forces would stretch the strata ; and when they could no longer stand the tension, cracks would ensue, and many lines of valley are assumed to lie in such fractures. But in Wales, the Highlands of Scotland, and more notably in the Alps, the strata now visible have been compressed and crumpled, 1862.) , RAMSAY—GLACIAL ORIGIN OF LAKES. 191 not stretched, and they occupy a smaller horizontal space than they did previous to the formation of the chain. _ Let us suppose a set of strata of (say) 14,000 to 20,000 feet in thickness, like the rocks of North Wales, and let these be spread out horizontally over thousands of square miles. Let these strata, from any cause, be compressed from the right and left so as to be contorted, and occupy a smaller horizontal area than they did before disturbance. Then, at a great depth, where the super- incumbent strata pressed heavily on the lower beds, the latter would be crumpled up, cleavage would often supervene, and gaping frac- tures would be impossible; for, where mere fractures occurred, the walls of the cracks would be pressed more closely together. But nearer the surface, where there was less weight, and at it, where there was none, the beds would extend into larger curves than they did lower down; and where the limits of extensibility were passed, shattering might take place, and yawning chasms might ensue. In all violently contorted countries, however, as in the cleaved rocks ef North Wales, for instance, the present surface shows those origi- nally deep-seated contortions that since disturbance have been ex- posed by denudation; otherwise the rocks would not be cleaved. I therefore do not believe that in any country I have seen, such as Wales or Switzerland, there are any lakes now occupying yawning fractures, consequent in Switzerland on post-eocene or post-miocene disturbances. On the contrary, they lie in hollows of denudation, shortly to be explained, of later date than these disturbances. Fourthly, again, it may be supposed that the great lakes lie each in an area of special subsidence; but, in reply to this, it is evident that among the unnumbered lakes of Switzerland and the Italian Alps it would be easy to show a gradation in size, from the smallest tarn that lies in a rock-basin to the Lakes of Geneva and Constance. Neither do I see any reason why mere size should be considered the test of subsidence. Disallowing that test, we should require a great number of special subsidences, each in the form of a rock-basin, in contiguous areas. Between the Seidelhorn and Thun, for example, we should require one for the Todten See, several on the plateau on the north immediately under the Seidelhorn, one for the lake at the Grimsel, another for the drained lake at the Kirchet*, and another for the lakes of Brienz and Thun. In Sutherlandshire these areas of special subsidence would be required by the hundred, and in North America by the thousand. Signor Gastaldi, in a masterly memoir on the composition of the Miocene conglomerates of Piedmont?t, considers with reason that the large angular blocks of these strata, many of them far-trans- ported, and some of them foreign to the Alps and Apennines, have been deposited from ice-rafts; and thence he infers the exist- ence of glaciers during a part of the Miocene epoch. But, admitting this, it is evident that the distribution of the post-pliocene glaciers of * See the “Old Glaciers of Switzerland and North Wales.” t “Sugl elementi che compongono i conglomerati Mioceni del Piemonte.” Turin, 1861. VOL, XVIII.—PART I. 0 192 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Mar. 5, the Alps must, in all details, have been quite different from those of Miocene age, in consequence of the great disturbance that the Alpine rocks underwent after the close of the Miocene epoch, and the sub- sequent formation of numerous new valleys of denudation. Traces of the long lapse of time between the Miocene and the later Glacial epoch are in other countries but imperfectly preserved in the sub- divisions of the Crag, and of other minor formations of still later date. Of the finer gradations that unite these subdivisions few traces have been described. For long before, and during all these Crag epochs and the ages between them, of which we have little trace, and during all the time that elapsed from the close of the Crag until the period of extreme cold came into action, the Alps stood above the sea, and, suffering subaérial denudation, valleys were being formed and deepened. It is possible that, while the mild climates of the Lower Crag epochs endured, there may still have been glaciers in the higher Alps; but at whatever period the later glaciers com- menced, those who allow the extreme slowness of geological change will admit that the period was immense that elapsed during the gra- dual increase of the glaciers, until, in an epoch of intensest cold, the ice abutted on the Jura in one direction, in another spread far beyond the present area of the Lake of Constance, and on the south invaded the plains of Lombardy and Piedmont. During all that time weather and running water were at work modifying the form of the ground under review. But, as I have already ex- plained, these two agents were incapable of scooping out deep hol- lows surrounded on all sides by rocks, and it therefore follows that the lakes first appeared after the decline of the glaciers left the surface of the country exposed approximately as we now see it,— unless we admit, what seems to me impossible, that fractures, formed at the close of the Miocene epoch, remained filled with water until the great glaciers filled them with ice; or believe, with De Mor- tillet, that the valleys, and lake-hollows were charged with water- borne alluvial or diluvial débris before the glaciers ploughed it out *, Allowing the hypothesis of De Mortillet, the rock-basins mus? have been twice filled with water; but, according to my hypothesis, they did not exist as lakes till after the Hera of the glaciers. But the glacier map of ancient Switzerland shows that the areas now occupied by the great lakes, both north and south of the Alps, have all been covered with glaciers. No tertiary deposit of an age between the close of the Miocene and the commencement of the Glacial epoch lies between the Alps and the Jura; and, had the hollows of the lakes existed prior to the great Glacial epoch, we ought, but for some powerful wasting agent, probably in these hollows, still to find * See an admirable memoir by G. de Mortillet, “Des Anciens Glaciers du Versant Italien des Alpes.” Milan, 1860. ‘Though I had seen his map, I had not seen this memoir when I read my paper; and the passages in which it is mentioned have been added as these pages passed through the press. His theory leaves the difficulty of the first formation of the basins untouched, unless we believe (which I do not) that the Alpine valleys are lines of fracture. 1862. ] RAMSAY—GLACIAL ORIGIN OF LAKES, 193 _ some traces of freshwater deposits, perhaps of the age of part of the © Crag. No such relics exist. The Great Lakes. Lake of Geneva.—The Lake of Geneva is about 45 miles in length by about 12 in breadth, and its delta, once part of the lake, between Villeneuve and Bex, is 12 miles long. The © latter and a small part of the banks of the lake beyond the mouth of the river lie in the great Rhone valley, formed of older Tertiary and Secondary rocks. All the rest of the lake is surrounded by the low country formed of the various subdivisions of the Molasse and — Nagelfluh. The lake is 1230 feet above the level of the sea, and 984 feet deep towards the eastern end, according to the soundings of . De la Beche*. See fig. 1, p. 194. Geneva itself stands on superficial débris; but the solid rock first appears in the river-bed below Geneva, at Vernier, at the level . of 1197 feet above the sea—only 33 feet below the surface of the lake, or 951 feet above the deepest part of its bottom. Any one acquainted with the remainder of the physical geography of the country will therefore see that the water of the lake lies in a true rock-basin. The question thus arises, How was this basin formed? — ist. It does not le in a simple synclinal basin ; for, though the Lake of Geneva lies in the great synclinal hollow of the Miocene ~ strata between the Alps and the Jura, it is evident by an inspection of the country that the flexures of that formation are of far greater — antiquity than the lake. ‘These flexures have been denuded, and the © lake runs in a great degree across their strike. 2nd. For reasons already stated, it is, I believe, impossible to prove that the lake lies in an area of special subsidence, all the pro- | babilities being against this hypothesis. : 3rd. It is almost needless to say that the Lake of Geneva is too wide to le inamere line of fracture; and I know of no reason why the valley of the Rhone, where occupied by the delta, should be esteemed a line of fault or gaping fissure, any more than many other valleys in Switzerland, which many geologists will consider with me chiefly the result of the old and long-continued subaérial denudation of highly disturbed strata. I could enter on details to prove this point, but they belong rather to the rock-geology of Switzerland than to the matter in hand. Ath. Those who do not believe in the existence and excavating power of great and sudden cataclysmal floods will at once see that the area of the lake cannot be one of mere watery erosion ; for ordi- nary running water, and far less the still water of a deep lake, can- not scoop out a hollow nearly 1000 feet in depth. Now, if the Lake of Geneva do not lie in a synclinal trough, in an area of subsidence, in a line of fracture, nor in an area of mere aqueous erosion, we have only one other great moulding agency left by which to modify the form of the ground, namely, that of ice. When at its largest, the great glacier of the Rhone (No.1 of the Map, Pl. VIII.) debouched upon the Miocene beds where the eastern end of the Lake of Geneva now lies. The boulders on the Jura, near * Edinburgh Philosophical Journal, 1820, vol. ii. p. 107, and ue 2. ) 0 20] LO L 5 SS ZZ, ISS S S S It - is : ee | ) 00§ 096 816 096 VIL V66 O16 6 oor PIO 2Yp fo 207 ay) fo ssouyory 7, anyounduon,. ay, bumoys pun aef ysybug ur shupunog ynm “naouay fo ayn] oy) £0 wonoos—upuboug—e “SUy fo} Ae. FWY SAY T S77A40N Cem “yog 0 9d ‘H “uy vafy) sof ysybug un shuypunog yodiomad ayy Buumoys ‘naauay fo oxnry oun fo dnw-ompyng—tT “Siz 1862.] - RAMSAY—GLACIAL ORIGIN OF LAKES. 195 Neuchatel, at the point on the Map marked B, prove that this glacier was about 2200 feet thick where it abutted on the mountains; and, where it first flowed out upon the plain at the mouth of the valley of the Rhone, the ice, according to Charpentier, must have been at least 2780 feet thick *. Add to this the depth of the lake, 984 feet, and the total thickness of the ice must have been about 3764 feet at what is now the eastern part of the lake, fig.2+. I conceive, then, that this enormous mass of ice, pushing first north-west and then partly west, scooped out the hollow of the Lake of Geneva most deeply in its eastern part opposite Lausanne, where the thickness and weight of ice, and consequently its grinding power, were greatest. This weight de- creasing as it flowed towards the west, from the natural diminution of the glacier, possessed a diminishing eroding power, so that less matter was planed out in that direction, and thus a Jong rock-basin was formed, into which the waters of the Rhone and other streams flowed when the climate ameliorated and the glacier retired. Lake of Neuchatel.—The basins of the Lakes of Neuchatel, Bienne, and Morat were, I consider, hollowed out in a similar manner, dif- fermg in points of detail. Near the Lake of Neuchatel, on the flank of the Jura, the fan-shaped end of the Rhone glacier (No. 1) attained its greatest height, swelled in size and pressed on as it was by others that descended from the north snow-shed of the mountains between the Oldenhorn and the great snow-field above Grindelwald. Accord- ing to estimates based on the highest ice-stranded boulders, the ice rose 2203 feet above the present surface of the lake. The lake is now 1427 feet above the sea, and 480 feet deep; and the Lake of Bienne is 1425 feet above the sea, and 231 feet in depth. The bottom of the Lake of Neuchatel is thus 947 feet above the sea. Unless the gravel, therefore, on the banks of the Aar, immediately east of the latter, be over 480 feet deep, the hollow of the lake near its immediate bounds is a true rock-basin ; for on the north, south, and west it is surrounded by solid Secondary and Miocene rocks. Even if the rock does not rise close to the surface in the river near the lake, still, at Solothurn, strata in place come close to the river-bank on both ‘sides, the river being 1414 feet above the sea. Under any circumstances there must therefore be a long, deep trough between Solothurn and the rocks a little south-west of the Lake of Neuchatel. How was this basin formed? When the gla- cier, debouching from the valley of the Rhone, spread out like a fan and pressed forward till it abutted on the Jura, its onward progress was stopped by that mountain; and direct further advance being hindered, the ice spread north-east and south-west, to the right and left, and being as a whole thickest and heaviest above the area where the lake now hes, a greater quantity of the Miocene strata on which it rested must have been ploughed out there than further on towards the north-east and south-west ends of the glacier, towards which * The Lake of Geneva is 197 feet lower than the Lake of Neuchatel. The glacier first surmounted the hills between Lausanne and Vevay, and then flowed down the general slope northwards to the Jura. t This diagram is on a true scale both horizontally and vertically. 196 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, the ice, gradually declining in thickness, exercised less grinding power. In this manner I believe the troughs were formed in which he the three lakes near Neuchatel ; and when the ice finally retreated, the ordinary drainage of the country filled them with water, the cliffs on the south-eastern side of the Lake of Neuchatel and other changes of the form of the ground having since been produced or modified by watery erosion and the local deposition of silt and allu- vial gravel. The Lake of Thun.—The Lake of Thun is 1825 feet above the sea, and 776 feet deep. Its bottom is therefore 1049 feet above the sea. Itis about 10 miles in length, 14 broad, and its length chiefly cuts across the strike of rocks of Secondary and Miocene age. The Lake of Brienz (about the same size) is more remarkable ; for, while its level is 1850 feet above the sea, its depth is more than 2000 feet : so that its bottom is at least between 100 and 200 feet below the level of the sea. Before the formation of the alluvial plain between, these two lakes were probably united ; and whether or not this was the case, it is evident, from its great depth, that the Lake of Brienz lies in a true rock-basin. Even if below Thun the rocks do not crop nearer than Solothurn, the Lake of Thun still les in a rocky hollow more than 600 feet deep, both hollows having, I believe, been deep- ened by the great old glacier of the Aar (No. 2 in the Map), the ice of which was so thick, that above Brienz it overflowed into the valley of Sarnen by the Brunig, about 1460 feet above the Aar below Meyrin- gen, and sent off a branch which scooped out the hollows of the Lakes of Lungern and of Sarnen on its course towards Alpnach on the Lake of Lucerne. The Lake of Zug.—The Lake of Zug is about 9 miles long, from 1 to 21 wide, 1361 feet above the sea, and 1279 feet deep; and its bottom is therefore only 82 feet above the sea. The whole is surrounded by Miocene strata, the strike of which the lake cuts across, and its great depth clearly shows that it lies in a rock-basin. The Lake of Iucerne.—The Lake of the Four Cantons (Lucerne) ramifies among the mountains and extends its arms in various direc- tions. In its lower part, the branches that run N.E. to Kussnach and §.W. towards Gestad le partly in the strike of the Miocene and older strata; but for the most part it runs across the average strike of the Hocene and Secondary rocks, between banks, some- times precipitous, that rise in noble cliffs sometimes more than 2000 feet above the water. Its height is 1428 feet above the sea, and its recorded depth 853 feet; but the shape of the banks and the round number of 800 French feet make it likely that it may con- tain deeper gulfs than have yet been plumbed. If not, then its bottom is 575 feet above the sea; and those acquainted with the shape of the ground by Lucerne will easily be convinced that the lake lies in-an actual rock-basin. The steepness of the walls of this lake more resembles the sides of a rent than those of any of the basins yet described, and the re-entering angles of rock opposite curving bays have been cited as evidences of fracture, one side being supposed to fit into the other, But in most cliffy valleys of aqueous erosion there — 1862. ] RAMSAY—GLACIAL ORIGIN OF LAKES. 197 are necessarily such re-entering angles, from the common action of running water; and, in Switzerland, ere these valleys were filled with ice, they existed in some shape, and were drained by rivers that deepened them and gave them a general form preparatory to the flow of the ice that largely modified their outlines. I should no more consider the re-entering angles a sign of gaping fracture in these valleys than I would the bends of the Welsh valleys or of the tortuous Moseile. But even if at first sight one were inclined to believe the space between the opposite cliffs between Brunnen and Fluhlen to be an open fracture, if we take a moderate average slope for each side, say of 65°, and produce it below the water, we get a depth, ere the lines meet, of between 7000 and 8000 feet—a very improbable depth for the original hollow of the lake. But it may be said that the fracture has been much widened by degradation, the line of the break merely giving a line of weakness, along which the surface- drainage might widen the valley. If, however, we only take an angle for the sides of the lake giving a moderate depth, the necessity for a fracture does not exist, and we recur to some process of mere erosion for the scooping of the hollow in which the water les, that process having, I consider, been the long-continued grinding of the ice of the great glacier No. 3 of the Map. | The Lake of Zurich.—The Lake of Zurich runs from N.W. to8.E., across the average strike of the Miocene strata, which are much dis- turbed towards its eastern end. It is bounded by high hills, much searred by the weather, on which the different Miocene strata often stand out in successive horizontal steps. The Linth Canal and the Wallen See lie in an eastern prolongation of this valley, which is still further extended to the valley of the Upper Rhine at Sargans. The lake is about 25 English miles in length, by 21 wide in its broadest part. A great moraine partly dams it up at its outflow at Zurich; and asecond forms the shallowat Rapperswyl, where the lake is crossed by a long wooden bridge. ‘The general level of the water is 1341 feet above the sea, and only about 639 deep; and the bottom of the lake is therefore 702 feet above the sea. The limestone rocks at Baden, on the Limat, are 1226 feet above the sea; and the lake there- fore lies in a true rock-basin, though it is probable that the old mo- raine at Zurich accounts for the retention of the water of the lake at its precise level. The long hollow was in old times entirely filled by the great glacier (No. 4 in the Map, Pl. VIII.) which descended from the mountains between the Todi and the Trinserhorn, through the valley of the Linth, to Baden. The Wallen See-—The Wallen See lies in a deep valley, whose cliffy slopes of Secondary rocks rise from 2000 to 3000 feet, and in the Leistkamm 4500 feet above the surface of the lake. The lakeitself is 1591 feet above the sea; and from the great steepness of its banks it may be inferred that it is exceedingly deep, but none of the authorities I have consulted give its soundings. A large branch from the great Rhine glacier (No. 5 on the Map) joined that of the valley of Glarus and Zurich through this wide gorge, and ground out the hollow of the Wallen See. 2 198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, The Lake of Constance—The Lake of Constance, the largest sheet of water in Switzerland, is about 50 miles in length, by about 15 in breadth at its broadest part. It is entirely surrounded by Mio- cene strata, often considerably disturbed, and forming great hills to- wards the 8.E., which in a remarkable manner evince all the signs of long-continued erosion by running water,—convyeying the impres- sion that chiefly by that means all the deep valleys of the district have been worn since the close of the Miocene epoch. This lake lies 1298 feet above the sea; and, its depth being 912 feet, its bottom is only 386 feet above the sea. The falls of the Rhine are 1247 feet above the sea; and the lake therefore les in an unmistakeable rock- basin, the whole of which was once overflowed by the deep and broad- spreading glacier of the Upper Rhine valleys (No. 5 of the Map), which stretched far northward beyond the lake into Baden and Wurtemberg. Being of greatest thickness where it entered the region of the lake, by its enormous weight and grinding power it scooped out, in the soft rocks below, the wide hollow now filled with water. The Itahan Lakes.—If we now turn to the Italian side of the Alps, we shall find the same phenomena prevailing in the Lakes of Maggiore, Lugano, and Como, the only important lakes I have yet had an opportunity of seeing south of the great chain. To each of these the same reasoning applies, modified only in detail ; and I shall therefore briefly pass them over. The most westerly, the Lago Maggiore, lies in a winding valley, 40 miles long, excavated in gneissic and jurassic rocks, which rise on either side in lofty mountains. The surface of the lake is 685 feet above the level of the sea, and near the ‘Borromean Islands it has the enormous depth of 2625 feet; so that its bottom is 1940 feet lower than the sea-level. It must, therefore, be enclosed all round by rocks, unless we suppose the narrow passage at Arona, near its outlet, to be as deep as its deepest part, or that the alluvial deposits of the Ticino and the Po are more than 1940 feet deep— an assumption no one is likely to make. Of all the Alpine lakes, that of Lugano is the aie irregular in form,—in the language of M. Desor, stretching its arms like a great polyp among the mountains in all directions*. Its surface is 938 feet above the level of the sea, and its depth 515 feet. Its bottom is therefore only 410 feet above the sea-level, and the shape of the surrounding ground renders it oe to believe that it is not entirely surrounded by rocks. The Lake of Como, the hollow of which has been scooped out gene- — * See memoirs ‘‘ De la Physionomie des. Lacs Suisses”’ (extrait de la ‘Revue Suisse,’ 1860) and ‘‘ Quelques Considérations sur la Classification des Lacs, a propos des bassins du revers méridional des Alpes,” by E. Desor. The opinions of M. Desor and my own do not agree on the question of the origin of the lake-basins of the Alps. His views are well expounded in the above- named memoirs. It was in conversation with my friend, in 1860, that I first proposed what I consider the true solution of the question, and to this conver- sation I presume he alludes in the latter memoir, p. 13,—‘‘ On a prétendu que les lacs étaient l’effet de laffouillement des glaciers qui auraient labouré le sol sur lequel ils s’avangaient,”’ &c. \ c ——S rT ee — 1862. ] - RAMSAY—GLACIAL ORIGIN OF LAKES. 199 rally in the same set of rocks as the other two lakes, is 700 feet above the sea, and 1929 feet deep; and its bottom is therefore 1229 feet below the level of the sea. On the borders of these lakes the rounded rocks and the well-known glacier-stranded boulders, high on the mountain-sides, attest that these deep valleys were filled to the brim by a vast system of glaciers (Nos. 6 and 7 of the Map, Pl. VIII.) that flowed southerly from the snow-shed that runs from the eastern side of Monte Rosa, by the Rheinwald-horn, to the top of the valley of the Adda,—a system of glaciers so large that, like that of Aosta and Ivrea (No. 8 of the Map), further west, they protruded their ends and deposited their moraines far south on the plains of Piedmont and Lombardy. . The glacier of Ivrea (No. 8 on the Map), when it escaped from the valley of the Doire, deposited a moraine at its side, east of the town of Ivrea, rising in mere débris 1500 feet above the plain, and spreading out eastward in a succession of fan-shaped ridges miles in width. The vastness of this mass gives a fair idea of the huge size of the glacier, and of the great length of time it must have endured ; and just as this glacier hollowed out the little rock-basins in which lie the tarns that nestle among the large roches moutonnées be- tween the town and the moraine*, so, deep as the hollows of the great Lakes of Maggiore and Como are, I believe they also were scooped out by the grinding power of long-enduring ice, where, under favourable circumstances, the glaciers were confined between the mountains, and therefore thicker than the glacier of Ivrea where it debouched on the plain. Diagrams illustrative of this subject should be drawn on a true scale; otherwise, height, depth, and steepness being exaggerated, the argument becomes vitiated. I have not the data for giving an actual outline of the bottom of the Lago Mag- giore; but a line drawn from the upper end of the lake to the required depth near the Borromean Islands gives an angle only of about 3° in a distance of about 25 miles, and from thence to the lower end of the lake (12 or 13 miles) of about 5°. The depths of Maggiore and Como do not, in my opinion, militate against my view ; for, if the theory be true, depth is a mere indicator of time and vertical pressure in a narrow space. It is interesting, and confirmatory of this view, that the deepest part of the Lago Mag- giore is just at the point where the enormous glacier of the Val d’Ossola joimed the great ice-stream that was formed by the united glacier-drainage of the valleys above Bellinzona and Locarno. Where these glaciers united, there the lake begins ; and where the ice was on the largest scale near the Borromean Islands, there the lake is deepest. Summary with regard to the Alpine Lakes.—And now, in reviewing the subject of the origin of the lakes of Switzerland and North Italy, I would remark— Ist. That each of the great lakes (see Map) lies in an area once covered by a vast glacier. There is, therefore, a connexion between them which can scarcely be accidental. * There are other well-known lakes dammed up by the moraine of this great glacier. 200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, 2nd. I think the theory of an area of special subsidence for each lake untenable, seeing no more proof for it in the case of the larger lakes than for the hundreds of tarns in perfect rock-basins common to all glacier-countries, present or past, and the connexion of which with diminished or vanished glaciers I proved originally in ‘ The Old Glaciers of North Wales.’ In the Alps there is a gradation in size between the small mountain-tarns and the larger lakes. 3rd. None of them lie in lines of gaping fracture. If old fractures ran in the lines of the lakes or of other valleys, and gave a tendency to lines of drainage, they are nevertheless, in the deep-seated strata, exposed to us as close fractures now, and the valleys are valleys of erosion and true denudation. Ath. They are none of them in simple synclinal basins, formed by the mere disturbance of the strata after the close of the Miocene epoch: nor, 5th, Do they lie in hollows of common watery erosion; for run- ning water and the still water of deep lakes can neither of them ex- cavate profound basin-shaped hollows. So deeply did Playfair, the exponent of the Huttonian theory, feel this truth, that he was fain to liken the Lake of Geneva to the petty pools on the New Red Marl of Cheshire, and to suppose that the hollow of the lake had been formed by the dissolution and escape of salts contained in the strata below. 6th. But one other agency remains—that of ice, which, from the vast size of the glaciers, we are certain must have exercised a power- ful erosive agency. It required a solid body, grinding steadily and powerfully in direct and heavy contact with and across the rocks, to _ scoop out deep hollows, the situations of which might either be deter- mined by unequal hardness of the rocks, by extra weight of ice in special places, or by accidental circumstances, the clue to which is lost, from our inability perfectly to reconstruct the original forms of the glaciers. : ; 7th. It thus follows that, valleys having existed giving a direc- tion to the flow of the glaciers ere they protruded on the low coun- try between the Alps and the Jura, these valleys and parts of the plain, by the weight and grinding power of ice in motion, were modi- fied in form, part of that modification consisting in the excavation of the lake-basins under review. In connexion with this point, itis worthy of remark that glaciers, many of them very large in the modern sense of the term, on the south side of the Vallais (excepting those of Mont Blanc), and the large glaciers on the south side of the Oberland, all drain into the Lake of Geneva; those on the north of the last-named snow-field, also large glaciers, are drained through the Lakes of Brienz and Thun. These, among the largest existing glaciers of the Alps, are only the shrunken tributaries of the greater glaciers that in old times filled and scooped out the basins of the lakes. The rest of the lakes, as already stated, are in equally close connexion with the old snow-drainage of glacier-regions on the grandest scale,—all of them, excepting those of Neuchatel, Bienne, and Morat, lying in the direct 1862. ] RAMSAY—GLACIAL ORIGIN OF LAKES. 201 course of glaciers filling valleys that extend right into the heart of the mountains. 8th. Most of the lakes are broad or deep according to the size of the glaciers that flowed through the valleys in which they lie, this general result being modified according to the nature of the rock and the form of the ground over which the glacier passed. Thus, the long and broad Lake of Geneva, scooped in the Miocene lowlands, is 984 feet deep, and over its area once spread the broad glacier of the Rhone. Its great breadth and its depth evince the size of the glacier that over- flowed its hollow. The Lake of Constance, lying in the same strata, and equally large, is 935 feet deep, and was overspread by the equally magnificent glacier of the Upper Rhine. The Lakes of Maggiore and Como, deepest of all, lie in the narrow valleys of the harder Secondary rocks of the older Alps; and the bottom of the first is 1992 feet, and the latter 1043 feet, below the sea-level. Both of these le within the bounds of that prodigious system of glaciers that descended from the east side of the Pennine Alps and the great ranges north and south of the Val Tellina, and shed their moraines in the plains of Piedmont and Lombardy. The depth of the lakes corresponds to the vast size and vertical pressure of the glaciers. The circumstance that these lakes are deeper than the level of the sea does not affect the question, for we know nothing about the absolute height of the land during the Glacial period. The Lakes of Thun and Brienz form part of one great hollow, more than 2000 feet deep in its eastern part, or nearly 300 feet below the level of the sea. They lie in the course of the ancient glacier of the Aar, the top of which, as roches moutonnées and striations show, rose to the very crests of the mountains between Meyringen and the Grimsel. The Lake of the Four Cantons is imperfectly estimated at only 884 feet in depth; but here we must also take into account the great height and steep inclines of the mountains at its sides. The Lake of Zug, 1311 feet deep, lies in the course of the same great glacier, the gathering-grounds of which were the slopes that bound the tributaries of the Upper Reuss and the immense amphitheatre of the Urseren Thal, bounded by the Kroutlet, the Sustenhorn, the Galenstock, the St. Gothard, and the southern flanks of the Scheerhorn. The lesser depths (660 feet) of the Lake of Zurich were hollowed by the smaller but still large glacier that descended the valley of the Linth. This completes the evidence. Lakes of the Northern Hemisphere generally.—I shall now make a few remarks on the bearing of this subject on the glacial question generally. It is remarkable that in Europe and North America, goug north- ward, lakes become so exceedingly numerous, that I have been led to suppose the existence of some intimate connexion between their numbers and the northern latitudes in which they occur. Let any one examine the map of North America, and he will 202 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 5, find that, from the Atlantic coast to the St. Lawrence, through New Hampshire, Vermont, the north of the State of New York, Maine, Nova Scotia, New Brunswick, Gaspé, and Newfoundland, the whole continent is strewn with lakes. North of the St. Lawrence and the great lakes, as far as the Arctic Ocean, the same sprinkling of unnumbered lakes over the entire face of the country is even more remarkable; and it is a curious circumstance that a large part of this vast area is so low and undulating, that some of its lakes drain two ways—towards the North Sea and the Gulf of Mexico, or towards the North Sea and the North Atlantic. This vast country, about as far south as lat. 40°, shows, almost universally, marked signs of the strongest glacial action, in the moutonnée forms, polish, and constantly recurring striation of the rocks. JI have only seen a few of the above-mentioned lakes south of Lake Ontario; but I have closely questioned that able observer, Dr. Hector, who has examined the country north and west of the great American lakes, and he informs me that, though unable to account for it, he was struck with the cir- cumstance that so many (he thought he might say all) of the smaller lakes are in rock-basins. I connect this circumstance with the universal glaciation of the country, still evinced on the grandest pos- sible scale by every sign of ancient ice. These signs, I now believe, are far too universal and unvarying in their general directions to have been produced merely by floating ice, though in part of the glacial history of the continent floating ice has undoubtedly left large traces. But the lake-basins could only, I believe, have been scooped out by true continental glacier-ice, like that of Greenland ; for the lakes are universal in all the ice-worn region *. . On the eastern side of the Atlantic, Wales, Cumberland, many parts of Ireland, the North Highlands, and some of the Western Isles are also dotted with unnumbered lakes and tarns. All of these are well-glaciated countries, both high and low; and for Wales and many parts of Scotland, I can answer that by far the greater proportion of these lakes le in rock-basins of truly glacial origin +. . * Since this memoir was written, I have conversed on the subject with Sir Wm. Logan, Director of the Geological Survey of Canada, who not only agrees in my views with respect to the origin of American lakes in general, but also believes that the great American lake-basins may have been scooped out by the same means. They are all true rock-basins, in areas occupied by comparatively soft rocks surrounded by harder strata. Given sufficient time, I see no difficulty in this view, to which I inclined while writing this paper, but refrained from stating it, considering that most readers would think it too strong, and thus that in general opinion I might damage the whole theory. Sir William says that the arrangement of the strata proves that the great lakes do not lie in areas of special subsidence. t See ‘The Old Glaciers of North Wales.’ When I published my account of these glaciers, I was too timid to include the Lakes of Llanberis, Llyn Ogwen, Llyn Cwellyn, and some others of the larger lakes in this category. I now feel convinced that they are true rock-basins, and also that the shallower pools of Llyn Llegeirin, Llyn Felin-y-nant, and others in Anglesea had the same origin. The horizontal striations far up the side of Carnedd Dafydd, by Llyn Ogwen, were probably made by a glacier of immense thickness during the first great glacier-period, preceding the deposition of the stratified drift. 1862.] RAMSAY—GLACIAL ORIGIN OF LAKES. 203 Loch Lomond and Loch Katrine, probably, like the greater lakes of Switzerland, are of the same kind, being merely large cases of glacier-erosion, though in the case of the former it may be that the alluvial deposits on the banks of the Leven prevent its being in- vaded by the tide. Its islands are mere roches moutonnées *, In the lowlands of Scotland numerous examples of the same kind of rock-basins occur, some of them certain, others doubtful because of the surrounding drift, which indeed in some cases may be the sole eause of the retention of the water. Notable examples of both kinds occur in the lowlands of Fife and Kinross, and of true rock-basing in the Cleish and Ochil Hills, as for cae peg Loch Glow, Dow Loch, and the two Black Lochs, and more doubtfully Loch Lindores. I have not yet had an opportunity of visiting the Scandinavian peninsula, which, geologists are aware, is, through all its length and breadth, one of the most wonderfully glaciated countries in the world. On the west, descending from the great chain, striated roches moutonnées plunge right under the deep fiords; and on the east, in Sweden, all between the mountains and the Baltic, round the Gulfs of Bothnia and Finland, and up to the North Sea, the whole country is covered with a prodigious number of lakes, just like North America, the Lewes, and the North Highlands of Scotland. The intense glaciation which all of these countries have undergone, their similarity, and what I believe to be the intimate connexion of such erowded lakes with the movement of ice, induce me to believe that in Sweden also a great number of the lake-hollows must be true rock-basins scooped out by the passage of glacier-ice into the Baltic area. Furthermore, as the glaciated sides and bottoms of the Norwegian fiords and of the saltwater lochs of Scotland seem to prove, each of these arms of the sea is merely the prolongation of a valley down which a glacier flowed, and was itself filled with a glacier ; for the whole country was evidently, like the north of Green- land, moulded by ice. In parts of Scotland, some of these lochs being deeper in places than the neighbouring open sea, I incline to attribute this depth to the grinding power of the ice that of old flowed down the valleys, when possibly the land may have been higher than at present’. It may, however, only arise from unequal deposition of detritus. If the former view be admitted, raise the land so as to lay bare the surrounding ocean-bottom, and in some respects of levels and depth they become approximately the counterparts of the deeper narrow lakes of Switzerland and North Italy, glaciers bounded by mountains having flowed through both, and debouched upon the plains beyond. The Glacial Theory.—Furthermore, considering the vast areas over which the phenomena described are common in North America and Europe, I believe that this theory of the origin of lake-rock-basing * When the lake was low, I have seen in Loch Lomond ice-striated sur- aces of rock just above the water, the striations running in the direction of the length of the lake. t But this is not essential, unless the lochs are so aree that the ice must have been floated up before reaching the deeper parts. 204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5, is an important point, in addition to previous knowledge, towards the solution of the glacial theory; for I do not see that these hollows can in any way be accounted for by the hypothesis that they were scooped by floating ice*. An iceberg that could float over the mar- gin of a deep hollow would not touch the deeper recesses of the bottom. J am therefore constrained to return, at least in part, to the theory many years ago strongly advocated by Agassiz, that, in the period of extremest cold of the Glacial epoch, great part of North America, the north of the Continent of Europe, great part of Britain, Ireland, and the Western Islest, were covered by sheets of true glacier-ice in motion, which moulded the whole surface of the country, and in favourable places scooped out depressions that subsequently became lakes. This was effected by the great original glaciers (probably con- nected with the origin of the unstratified boulder-clay) referred to in my memoir on the glaciers of North Wales{, but the magnitude of which I did not then sufficiently estimate. The cold, however, con- tinued during the depression of North Wales and other districts beneath the sea, when they received the stratified erratic drift; and glaciers not only did not cease at this time of depression, but were again enlarged during the emergence of North Wales and other countries, so as to plough the drift out of many valleys. These enlarged glaciers, however, bore no comparison in size to the great original sheets of ice that converted the North of Europe and America into a country like North Greenland. The newer develop- ment of glaciers was strictly local. Amelioration of climate had already far advanced, and probably the gigantic glaciers of Old Switzerland were shrinking into the mountain-valleys. Finally, if this be true, I find it difficult to believe that the change of climate that put an end to this could be brought about by mere changes of physical geography§. The change is too large and too universal, having extended alike over the lowlands of the Northern and the Southern Hemispheres. The shrunken or vanished ice of mountain-ranges is indeed equally characteristic of the Himalaya, the Lebanon, the Alps, the Scandinavian chain, the great chains of North and South America, and of other minor ranges and clusters of mountains like those of Britain and Ireland, the Black Forest, and the Vosges. * I do not in any way ah to deny that much of the glaciation of the lower countries that came within the limits of the Drift was effected by floating ice on a large scale, which must have both polished and striated the rocks along which it ground. I have, with other authors, described this in various memoirs. But the two sets of phenomena are distinct. t The Lewes is covered by small lakes. t Quart. Journ. Geol. Soc. vol. xviii. p. 371. § It has been suggested to me by Dr. Sibson that the prodigious waste of the Alps by the gradual disintegration and diminution of the upper snow-fields, wit- nessed by the great moraines of North Italy and other phenomena, must have tended to lessen the glaciers. This is true, but, as he also believes, it is not of itself enough to account for the shrinking of the ice into the higher valleys where it is now alone found. 1862. ] HARKNESS—PERMIAN STRATA. 200 Marcu 19, 1862. Elliot Square, Esq., Gresham House, London; Ernest Shelley, Esq., Avington House, Winchester; Edward Romilly, Esq., 14 Stratton Street, Piccadilly ; The Right Hon. Edward Cardwell, Esq., M.P., 74 Eaton Square; George W. Stevenson, Esq., C.E., F.S.A., Halifax ; George W. Hemans, Esq., C.E., 32 Leinster Gardens, Bayswater; and Harvey Buchanan Holl, M.D., Woodgate, Malvern, were elected Fellows. The following communications were read :— 1. On the Sanpstonzs and their associated Deposits in the VALE of the Enrn, the CuMBERLAND Pratn, and the Souru-znast of Dum- FRIESSHIRE. By Professor R. Harxnuss, F.R.S.L. & E., F.G.S, ConTENTS. 1. Introduction 6. Country North of Penrith. 2. Section near Kirkby Stephen. 7. Sandstones of West Cumberland. 3. Section from Great Ormside to} 8. Sandstones of South-eastern Dum- Romanfell. friesshire. 4, Country between Great Ormside | 9. Organic remains. 10. St. Bees. and Penrith. 11. Scottish Permian Strata—their cha- 5. Section W. from Penrith to Hart- racter and age. side. 12. Conclusion. § 1. Tas memoir refers to an area which commences a little south of Kirkby Stephen, in Westmoreland, and extends N.N.W. for 50 miles, reaching the lower portions of the valleys of the Esk and Annan in Dumfriesshire. In an east and west direction, this area varies greatly in breadth; but, measured from Castle Carrock on the east, to the sea at Allenby on the west, the extent is about 30 miles. It occupies the whole of the Cumberland plain, except a small portion of the parish of Aikton; and, in Westmoreland, it occurs on both sides of the Vale of the Eden, The district under consideration exceeds 800 square miles. The strata which occur in this area consist of sandstones of two distinct positions and characters, separated from each other by a well-developed series of shaly beds, in some localities containing a considerable amount of gypsum; and calcareous layers are also some- times found associated with the shaly deposits. The arenaceous strata of Cumberland and Westmoreland have already attracted the attention of geologists. Those contiguous to the Penine chain are referred to by Dr. Buckland*. Those of the western side of the area have been alluded to by Prof. Sedgwick, and their boundaries in this portion of the north of England have been defined f. These deposits, as they occur at Kirkby Stephen, have been noticed by Prof. Phillips f. Mr. Binney has also described the nature and age of some of these * Geol. Trans., 2nd Series, vol. iv. p. 105 e¢ seg. + Ibid.vol. iv. p. 383 e seg. { Ibid. vol. iii. p. 9. 206 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 19, deposits in his memoir “ On the Permian Beds of the North-west of England *.” , In these several memoirs, detached localities are principally treated of. The object of this communication is not only to point out the several forms of rocks which occur in the area under consideration, but also to indicate the relative ages of the sandstones and the eypsiferous shales; and reference will also be made to the fossils which these latter afford. § 2. Section near Kirkby Stephen. (Fig. 1.) Wharton Park, immediately south of Kirkby Stephen, is the most southerly limit of the rocks referred to. Here the beds seen in the Eden consist of a breccia composed of angular fragments of light- grey limestone, cemented together by a fine-grained dark-red sand- stone. Fig. 1.—Section of Hden Valley, south of Kirkby Stephen, near Stenkrith Bridge. Length 1} mile. Railway- River W. Station. Eden. E. QERGSS SS : RX MSs . S N SV Vp GY 5. Upper sandstone. 3. Red clay (15 feet). 4. Upper breccia (60 feet). 2. Lower breccia. 1. Carboniferous rocks. This rock, locally termed ‘‘ hard brockram,” has a thickness in Wharton Park (from information received from a quarry-man) of 60 feet. Its aspect at Stenkrith Bridge, near this, has been described by Professors Sedgwick and Phillips, and also by Mr. Binney,—the latter pointing out the superposition of this “hard brockram” on an underlying mass of a softer nature, known as “‘ rotten brockram,” the latter resting on soft red sandstone. : The recent cuttings of the South Durham Railway, at the Kirkby Stephen Station, have exposed a section showing distinctly the rela- tions of the two “ brockrams.” The foundations of the bridge here rest upon the “rotten brockram,” dipping east at a low angle. Succeeding this is a series of red sandy clays, about 15 feet thick. Upon the sandy clays the “hard brockram” is seen extending to \ Stenkrith Bridge, and having a thickness of about 60 feet. These three deposits conform to each other; and a little below Stenkrith Mill, the “hard brockram” is overlain conformably by thin-bedded red sandstones. * Memoirs of the Literary and Philosophical Society of Manchester, vols. xii and xiv. fond 1862. ] HARKNESS—PERMIAN STRATA. 207 At the old saw-mill at Kirkby Stephen the “ hard brockrams” are also well seen, but they are much dwarfed in thickness, and show that they are rapidly thinning out. They repose on the sandy clays, which continue northward on the east side of the Eden, in the form of an escarpment; and at the Brewery, to the west, the “rotten brockram ” again occurs. Northward from this, no trace of the “hard brockram’”’ (which is an extensively used and durable building-stone) is seen. The lower or “ rotten brockram” has a different mineral nature from the “hard brockram ;”’ it consists of yellow limestone fragments, imbedded in a matrix of light-coloured sandstone; and it is more persistent in its occurrence. As it is seen in the "Bela Water and the neighbourhood of Brough, it has been described by Mr. Binney, who has also pointed out the great abundance of soft sandstones which are associated with it. Deposits of a like nature occupy the country north of Brough, the “rotten brockram” being seen west of Warcop; and to the east of this, under the western escarpments of Romanfell, the upper thin- bedded sandstones have been extensively worked. § 3. Section from Great Ormside to Romanfell. (Fig. 2.) The section showing most satisfactorily the sequence of the sand- stones and the accompanying strata in the north-west of England is one traversing the Vale of the Eden, from Great Ormside on the west to Romanfell on the east. Fig. 2.—-Section from Great Ormside to Romanfell. Length 5 miles. Hilton. Romanfell. N.E. mM 3 3 ee >) &E em S.W.~o Q f f { 7 56,1.8.9.10. 11 . Upper sandstones (700 feet). 4, Lower sandstones (2000 ft.). . Red clays (80 feet). 3. Carboniferous rocks. . Limestone (7 feet). 2. Old Red conglomerate (500 . Dark-coloured sandstone (6 feet). feet’). . Grey shale (3 feet). 1. Lower Silurian schists. . Thin-bedded red sandstone (50 ft. | . Plant-beds (20 feet). Professor Sedgwick notices the Se aby as they occur at Little Ormside, and at Burrels, a mile N.W. of Great Ormside *. * Geol. Trans. 2nd Series, vol. iv. p. 586. VOL, SVILE.— PART I. Vig series. =a on s10 6 Oe Se 7 “Fossilifer ous 208 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19, In Gill Beck, a small brook N.W. of Great Ormside, deposits appertaining to the Carboniferous rocks occur. Below these, in the brook, breccias are seen, succeeded by red sandstones, having an E.N. E. dip at 10°, inclining towards the Eden. East of this river, and west of the Appleby road, ridges of sand occur, as seen in the cutting of the Eden Valley Railway, resulting from soft decom- posing sandstones. At Coupland Mill, immediately east of the high road, in the course of the stream, red false- bedded flaggy sandstones manifest themselves. These have a dip and nature similar to the flagey beds which are wrought near Penrith. False bedding gives to these sandstones an apparent W.N.W. inclination, but the true dip is E.N.E. at a low angle. Kast from Coupland Mill is an extensive moor, called Brackenbar, along the western and northern margin of which ‘a stream, called Hilton Beck, flows. This stream exposes a beautiful section of the higher beds of the inferior sandstones and breccias. Above the false-bedded sandstones of Coupland Mill, a thick mass of soft deep- red-coloured sandy beds is seen. These are also greatly false- bedded, and have upon them strata of a harder nature, in which yellow breccias make their appearance in great profusion, conforming to the low E.N.E. dip of the sandstones. These breccias occur under the same circumstances as those seen in the Bela Water ; but they are rarely so thick as those of the latter, and the interstratified sandstones are usually less false-bedded. In their higher beds these sandstones become lighter in colour, and are conformably succeeded by some very interesting strata. These latter consist of cream-coloured, thin-bedded, arenaceous layers, with — thin, grey, shaly strata; and a few thin beds of limestone, well marked by their distinct jointings; the limestone is of a brownish colour in its interior, but weathers yellow. The strata, although well seen in the brook-course, are better exposed on the face of a small cliff seen below the Appleby guide-post on the south side of the stream. These yellow, thin-bedded strata have a thickness of about 20 feet. They have a remarkable resemblance to the marl-slate of Midderidge, Durham, and they afford fossils. The brook-course shows the following conformable succession above the yellow beds:—1st, very regular, thin-bedded, red sandstones, about 50 feet thick; 2nd, grey shale, imperfectly seen, having a thickness not exceeding 3 feet; 3rd, thin-bedded, soft, dark-red sandstones, 6 feet; 4th, a thin-bedded, compact, brownish-grey limestone, with drusy cavities filled with small crystals of cale-spar. The limestone becomes darker in colour, and semicrystalline in its upper layers ; and papery bands of black shale separate the strata. This limestone, which afforded no trace of fossils, does not pie to exceed 7 feet in thickness. A series of red clays overlies conformably the limestone. The thick- ness of this, which is probably 80 feet, cannot be exactly made out, as débris masks the junction of this clay with the upper sandstones. These latter, with associated clay-beds, form the bed of the brook to — beyond the village of Hilton, and they also dip E.N.E. at 10°. 1862. ] HARKNESS—PERMIAN STRATA. 209 At the smelt-mill, above the village, the dip of the upper sand- stones is reversed; but here they are contiguous to the great Penine fault. On the opposite or east side of the fault, Lower Silurian rocks are seen dipping N.N.W. at 50°; and on the west side of Romanfell these have upon them Old Red Sandstones, about 500 feet in thickness, dipping east, and passing regularly under the base of the Carboniferous series of Warcop Fell. The section from Great Ormside to Romanfell affords means for ascertaining the thickness of the inferior sandstones and breccias. The dip of these averages 10° E.N.E.; and the distance from their western margin to the spot in Hilton Beck where the yellow series occurs is about two miles, measured across the dip. This would give a thickness of nearly 2000 feet to the inferior strata. The next series, including the yellow sanastones below and the clays above, with the intervening deposits, has a thickness of about 160 feet ; and the upper sandstones are here about 700 feet in thickness. § 4. Reference has already been made to the occurrence of the breccias at Burrels. These are also seen on the east side of the Eden, immediately below Appleby; and at Bongate, an eastern extension of Appleby across the river, the false-bedded sandstones also occur. At Hungrigg, a mile E.N.K. from Appleby, the higher members of the breccia are seen, having here been extensively worked for their limestone fragments; and a short distance from this eastwards the clayey zone comes on. No traces of the breccias oceur north of Hungrigg; and with this thinning out of the coarse portion of the inferior series, we have a greater development of the sandstones proper. To the north of Hungrigg no section can be obtained comparable to that across the Eden from Ormside to Romanfell, but many ex- posures of rock are seen which exhibit the sequence of the several strata. At Long Marton, three miles north of Appleby, in the stream above the bridge, the inferior sandstone occurs, being the higher portion of the series. The clay-beds also were formerly wrought on the south side of the village, at Haa Plaister Sear, for the gypsum which they here afford; and the upper sandstones are seen in the streams between Dufton and Knock. At Stamphill,a mile N.W. of Long Marton, the red clays and gypsum were also formerly worked; and at Townhead, a quarter of a mile N.E. of Kirkby Thorpe, a good exposure of these now occurs, for here they are worked to a consi- derable extent. At this spot a mass of gypsum, called “ Haa Plaister,”’ about 9 feet thick, is seen resting on bluish clay, the gypsum itself being capped by about 7 yards of boulder-clay. The level country W. and N.W. from this affords no sections until we reach Cliburn, where the false-bedded flaggy sandstone has been noticed by Prof. Sedgwick*. From Cliburn this extends northward ; and, forming Whinfell, it here exhibits its normal false- bedded character well developed. East from Whinfell this sand- * Op. cit. p. 386. P2 210 PROCEEDINGS OF THE GEOLOGICAL socreTY. = [ Mar. 19, stone is seen at the bridge over the Eden, on the highway from Appleby to Penrith, to a slight extent. Near this is Crowdundle Beck, separating Cumberland from Westmoreland, in which we have a fine section of the argillaceous series. This extends from Acorn Bank to beyond Newbiggin, and is devoid of gypsum. It exhibits the same direction and angle of dip as at Hilton Beck, and is also succeeded by the upper sandstones, which are extensively worked at Crowdundle quarry. The same sandstone is also seen at Culgaith, and forms the escarpment known as Culgaith Peel; and immediately below it, on the opposite side of the Eden, the argillaceous series are well exhibited, forming Haa Plaister Scar, on the property of Winder- waith. 7 The section at Winderwaith is as follows:—The upper portion red clays, 12 feet thick, beneath which are greenish-grey clays with thin gypseous bands, 9 feet; red and grey clays and thin gypsum, 4 feet; a bed of fibrous gypsum, 2 inches,—the thickest seen, resting upon 6 inches of clay, passmg downwards into an argillaceous sandstone. Down the Eden on the east side, the argillaceous series forms a well-marked escarpment; and on the west side of the river the inferior sandstone is occasionally seen. The latter is, however, very well exhibited in the Eamont, a short distance above its junc- tion with the Eden, for about a mile and a half. In this section the false bedding is so abundant that on account of it no idea could be arrived at concerning the arrangement of the inferior sandstones. § 5. Section from the West of Penrith to Hartside. (Fig. 3.) West of Penrith, the junction between the Carboniferous rocks on the W. and the sandstone deposits on the E. is not apparent. Fig. 3.—Section from the West of Penrith to the Penine Chain. Distance 10 miles. W. Penrith Beacon. Langwathby. “Melmerby. Hartside. E. 7. Trap-rock. 3. Carboniferous rocks. 6. Upper sandstones. 2. Old Red conglomerate. 5. Red clay. 1. Silurian schists. 4, Lower sandstones (false-bedded, 5000 feet). At Newton Raigny and Catterlen, a purple grit of the Carboniferous series has been noticed by Prof. Sedgwick*. This grit is seen in the * Op. cit. note, p. 387. 1862. ] HARKNESS—PERMIAN STRATA. 211 Petterill, about half a mile below Newton; and there is reason for inferring that the red sandstone does not extend further than a mile west of Penrith. East of this place the sandstone is amply developed on Penrith Beacon Hill. Soft sandstones, nearly in the condition of sand, form the lowest beds here. Harder rocks succeed these, having . a false-bedded and flaggy nature, the false bedding inclining west- ward, and the beds haying sometimes a light colour. The same rocks occur at Cowrigg quarry, about a mile and a half E.from Penrith. Soft beds again succeed these, as seen on crossing over the Beacon Hill; and at Snittersgill, a mile and a half below Langwathby Bridge, on the west side of the Eden, the higher beds of the inferior sandstones occur with a false-bedded W. dip. On the east side of the river the ridge of the argillaceous strata is seen striking N.N.W., the road from Langwathby to Hartside crossing this between the village and Whinskill .Bridge, where the upper sandstones make their appearance with an E.N.E. dip at 10°. These continue to beyond Melmerby, and are well seen in the Rake Beck, three-quarters of a mile E. from this, where they come abruptly against a mass of trap occupying the line of the Penine fault. East of this, Lower Silurian rocks, overlain by Old Red Sandstones, passing upward to the Carboniferous series, occur. The rocks here have been alluded to by Dr. Buckland*. The section from Penrith to Hartside, with the exception of the traps, has a great affinity to that from Great Ormside to Roman- fell. In the former, however, there is a greater development of the inferior sandstones, and a total absence of the breccias, which are so abundant in the latter. The flaggy strata which occur between the soft sandstones are much more extensive in the former than in the latter, and equal the total thickness of the inferior sandstones as seen between Great Ormside and the plant-beds. Measured along the dip. which averages 10°, the lower sandstones of the Penrith section extend more than five miles; and from this it.would appear that the total thickness of this portion of the rocks here would be nearly 5000 feet. § 6. North from the line of the last section, numerous exhibitions of rocks appertaining to all the three groups are seen. The lower sandstones form the ridges which occur on the east of the Lancaster and Carlisle Railway, and are extensively marked on Bowscar and at Brownrigg in Plumton, where, in a quarry affording flags remark- ably like those of Corncockle and Dumfries, footprints similar to those of the Scotch localities have been found. Impressions of the same nature have been also noticed by Mr. Binney and the author on the flaggy beds near Penrith, but these are not so distinct as the impressions at Brownrigg. On Lazonby Fell the same flaggy beds, with the false-bedded westerly dip, are also very abundantly wrought, and, affording very superior flags, these are often sent to great distances. East from this range of hills we have also, in the Valley of the * Geol. Trans. 2nd Series, vol. iv. p. 112. 212 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 19, Eden, the inferior sandstones. They occur at Forge Mill, immedi- ately opposite to Lacy Caves, where they are intersected by a fel- stone dyke; at Scatterbeck, and in the brook near Lazonby village, they are also seen; they form Blaze Fell, and Great Barrock; and east from these we have them well exhibited in the Eden, immedi- ately above Armathwaite Mill, where they are intersected by the trap-dyke which runs from the Carboniferous rocks at Renwick, in a N.W. direction to Petterill Crooks, near the Wreay Station on the Lancaster and Carlisle Railway. East from Armathwaite, the in- ferior sandstones are found at Napestone, and amongst these are hard coarse flags like those of Templand quarry near Corncockle. Below Armathwaite Bridge the inferior sandstones are confined to the west side of the Eden. They are worked at Little Barrock quarry, near the Wreay Station ; but here they have a yellow colour, and no flaggy beds. : Their most N.E. exposure is in the course of a small stream flowing into the Petterill, known as Howgill Beck, on the west side of the Carlisle road, near Carleton Hill. Only a small portion of the higher beds appear here, consisting of red sandstones dipping W., succeeded by nearly horizontal layers passing conformably under the marls and gypsums of the argillaceous series, which here dip N. at a low angle. The western margin of the inferior sandstones also affords some sections. As occurring in Ive-gill, they have been described by Prof. Sedgwick*. Here the upper part of the stream is through these rocks, which dip N. at 20°. Below these, purple Carboniferous grits are seen; and closely con- tiguous to these grits the red sandstones exhibit reversed dips, and also a thin bed of breccia composed of fragments of the Carboniferous grits. The Carboniferous rocks extend down the stream to near High-head Castle, where the inferior red sandstones are again seen, and where their occurrence is mentioned by Prof. Sedgwick. Well- marked northern inclinations obtain here, and continue to near the junction of Raw Beck, below which the sandstones again appear, and continue with the same inclination to Stockdalewath, where, for a short distance, Carboniferous rocks again occur. ; The inferior sandstone, however, soon again makes its appearance, forming the brook-course to below the bridge at Througholme, where it passes conformably under the argillaceous series, which occurs about 200 yards below Througholme Bridge, dipping N. at 10°, and is about 100 feet in thickness. Below the argillaceous series, on the east side of the stream, Carboniferous rocks again appear, and extend south-eastward to Broadfield, where they were formerly worked for lime, as referred to by Prof. Sedgwickt. From Broadfield they extend still further in the same direction to Roughten Gill, a mile north of Southwaith Station, where they are wrought for the ironstone-nodules which they contain. * Geol. Trans. 2nd Series, vol. iv. p. 406. Tt Op. cit. p. 391. 1862. | . HARKNESS—PERMIAN STRATA. 213 The rocks seen in Ive-gill have the same general arrangement as that which obtains in the Valley of the Eden, the only difference being in the direction of the dip. This change from E.N.E. to N. is a gradual one, as is well shown in the strike and dip of the argilla- ceous series. Following the argillaceous series along its strike from Haa Plaister Scar, on the Eden, we find it exhibiting the following modifications :— At Langwathby it seems. to consist solely of red clays. At the farm of Lang Meg und her Daughters, near Lacy Caves, it consists of gypsum and clays, the former having been wrought here. About a mile and a half northwards, at Glassonby Beck, red clays alone occur; and at Ravens Beck, east of Kirk Oswald, where a good section is seen, the same features are manifested. In the river Croglin, between Dale and the Nunnery, argillaceous beds are the sole constituents of this series. Here, below the argillaceous strata, a fine section of the inferior sandstones is seen in the course of the Croglin, and, above these, the upper sandstones are worked at Sevie uarry. North of the Croglin, on the Armathwaite road, at Cross House, there are remains of a quarry in the argillaceous series, from whence gypsum was formerly obtained; but here the beds are thin, and not profitable, being irregular in their occurrence. The next locality which affords an exposure of the argillaceous series is the Haa Beck, at Ainstable. The strata here are only partially seen, but they seem exclusively clay-beds. On the west side of the Eden, at High Stand, gypsum is now extensively worked, the section of the quarry afford- ing the following beds :—The lowest (passed through in sinking a well below the floor of the quarry) consist of 8 feet of fine-grained purple sandstone, with thin layers of fibrous gypsum. Above these are three beds of gypsum, with a total thickness of 20 feet, the whole dipping N.E. at an angle of 5°. Similar gypseous strata are wrought at Carleton Hill, three miles N.W. from High Stand, near the Carlisle high-road. Here the gypsum is about 18 feet thick, irregular in its upper surface, and succeeded by indurated clay 3 feet in thickness, upon which rests a shaly sandstone 15 feet in depth. Here the strata have a low N. dip. On the east side of the argillaceous series, near High Stand, on the banks of the Eden, the upper sandstone is seen dipping N. at 20°. At Wetheral Pastures we have also this sandstone dipping in the same direction at an angle of 10°. At Corby the dip of this sand- stone is N.N.W.; and from thence it extends eastward to beyond Castle Carrock, where, in the Gelt, it is seen in close proximity to the Penine fault. From this the fault runs N. to Lanercost, occurring immediately below the bridge. From Lanercost its course is N.N.W.; and it is again seen at Penton Linns, on the Liddel, as described by Professor Sedgwick *. § 7. In the neighbourhood of Carlisle we see the upper sandstones in * Op. cit. note, p. 385. 214 PROCEEDINGS OF THE GEOLOGICAL society. [| Mar. 19, the course of the Caldew, both below and above Dalston, the dip here being N.N.W. at 10°.. No trace of the argillaceous series is seen in this river ; and the only evidence it affords of the inferior sandstones is at the bridge near Rose Castle, above which light-coloured rocks of Carboniferous age occur. West from the Caldew, in Chalk Beck, a good exposure of the upper sandstones and the argillaceous beds appears. The former, which dip N.W., have afforded the Romans materials for the construction of the western portion of Hadrian’s Wall; and the latter seem to repose upon a breccia, to the south of which occurs the fault sepa- rating the red sandstones from the Carboniferous rocks. The strata here, and also those which occur near this at Westward, have been described by Mr. Binney in the memoir before alluded to. West of these localities the wpper sandstones strike W.S.W., abut- ting directly against the Coal-measures of West Cumberland. At Maryport these upper sandstones are seen Jn near proximity to the Coal-measures. They are also well developed in the cliffs north of this place, where they exhibit the N.W. dip they usually assume in the west part of the Cumberland plain. On the English shore of the Solway these upper sandstones are not well seen; there is, however, every reason to infer that they occupy the whole of the flat area of N. Cumberland, except the por- tion covered by Lias referred to by Mr. Binney * (see fig. 4). The Seotch shore of the Solway, especially E. of Annan, affords these upper sandstones. They also, in Scotland, occupy the south- ern halves of the parishes of Canobie, Half Morton, and Kirkpatrick Fleming, the greater portion of the parish of Annan, the southern part of Cummertrees, and also the whole of Dornock and Graitney. The Scotch area of upper sandstone has for its northern boundary the same fault which in Cumberland separates it from the Carboni- ferous formation; but in Dumfriesshire this fault has a direction nearly E.N.E. and W.S.W. § 8. In Dumfriesshire, besides the fine section in the sk, 8. of Knotty Holm, the upper sandstones are seen in Half Morton, and at Cove, in Kirkpatrick, on the west side of the Caledonian Railway. They are also very extensively worked in the neighbourhood of Annan. Their general dip shows that they trough under the Solway, and become united with their equivalents on the south side of the Firth : see the section from Kirkpatrick to the Chalk Beck limestones showing their arrangement (fig. 4). Little has been said concerning the lithology of the inferior and the upper sandstones. There is a well-marked difference in this respect between them. In the former the particles are more angular, often exhibiting shining facets; the colour is also brighter than that of the upper sand- stones, and there is an absence of the interstratifying clay-beds which usually accompany the latter. These latter are more compact * Quart. Journ. Geol. Soc. vol. xv. p. 549. 1862. | HARKNESS—PERMIAN STRATA. 215 in their composition, and the faces of the strata exhibit features which are not seen on the lower series, consisting of beautiful rip- plings, desiccation-cracks, rain-pittings, and pseudomorphs of salt— features accompanying the upper sandstones throughout the area where they present themselves. Fig. 4.—Section across the Cumberland Plain to Dumfriesshire. Distance 15 miles. N. Cove. Solway Firth. Aikton. Chalk. 8. : | | i i 4 5 4 3 2 1 5. Lias. 3. Red clay. 4, Upper sandstone. 2. Breccia. 1. Carboniferous rocks. § 9. Organie Remains. Reference has been made to the occurrence of fossils in the yellow beds at Hilton Beck. The strata affording these form the lowest portion of the argillaceous series, and have, as before stated, a great affinity to the marl-slates of Midderidge. The remains consist prin- cipally of Plants, specimens of which were, through the kindness of Sir Charles Lyell, submitted to Professor Heer, who determined their general Coniferous character. The remains consist usually of leaves and wood, and in one instance of a cone. This, Sir Charles Lyell suggests, is of some importance, especially if the strata be Paleeozoic, since the absence of cones in Coal-strata induces botanists to regard the Conifere of the Carboniferous epoch as having a taaozd character, «cand, like a great majority of the Conifere of the southern hemisphere, as berry-bearing, and not cone-bearing.” Through the kindness of Mr. Wood of Richmond, I had an oppor- tunity of examining the marl-slate of Midderidge, and was furnished by him with fossil plants from this locality, which are remarkably like the fossils from the Hilton beds. Besides the remains of coni- ferous leaves, this locality affords ferns referable to Neuropteris and Sphenopteris. Of the latter, one form seems nearly akin to NS. erosa (Morris), a species from the Russian Permians*. Remains are found which appear allied to Weissites (Goppert), resembling that figured by Geinitz (‘ Die Versteinerungen des Zechsteingebirge und Rothhegenden oder des permischen Systemes in Sachsen,’ tab. vii. fig. 8). A form having the aspect of Caulerpites selaginoides (Sternb.) occurs here; and, with this, leaves identical with those of the Saxon Zechstein, as figured by Geinitz (tab. vii. figs.11, 12, 13), are found. Detached leaves, resembling Cupressites Ullmanni, Brongn., * See ‘Russia and the Ural Mountains,’ plate C. fig. 3. 216 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19, and others attached to stems akin to Voltzia Phillipsw (Lindley and Hutton), are also seen. These plant-remains are usually in the state of carbonaceous mark- ings; sometimes, however, they occur not embedded, but enclosed between the laminz ; and when in this condition, their preservation is very imperfect. A few traces of animals have also been found here, but, as yet, these have been seen only in the condition of casts. Crinoid stems, of small size, which seem identical with the casts of Cyathocrinus ramosus, are among them. Brachiopodous shells, which in size and general aspect resemble Terebratula elongata, Schloth., present themselves, and also other bivalves which are too imperfect to allow of their relations being determined. Although the fossils obtained at Hilton are as yet comparatively few, they conduce to the conclusion that the strata which afford them are at the base of the Zechstein portion of the Permians, and that the overlying beds, including the red clays, must be regarded as the representatives in the N.W. of England of the higher members of this formation ; while the thick mass of underlying sandstones and breccias is the equivalent of the Rothliegende, which attains its great- est development in this part of England. § 10. St. Bees.—Reference to strata which are seen on the north- east side of St. Bees Head, Whitehaven, and which have been long regarded as Permian, still further corroborates this conclusion. Here, at Barrow Mouth, reposing on purple sandstones of the Car- boniferous age, is a deposit of breccia only 3 feet in thickness, repre- senting the higher members of the inferior sandstone. Magnesian limestone, which is worked on the side of the hill, occurs above the breccia. This limestone, the base of which is not here seen, contains Permian Lamellibranchiata. On the shore it reposes on the breccia, and its thickness at this spot is about 11 feet, being much thinner than on the hill, and indicating a rapid thinning out. Red marls, with interstratified gypsum, about 30 feet in thickness, succeed the limestone, upon which the fine-grained red sandstones with interbedded clays of St. Bees Head occur,—these latter being wm every respect identical with the upper sandstones of Eastern and ' Northern Cumberland. The absence of the magnesian limestone, which we have seen is thinning out, would give us here the most common mode of occur- rence in this county of the argillaceous series and the upper sand- stones. These Permians of St. Bees have been described by Prof. Sedgwick *, and also by Mr. Binney in the memoir so frequently referred to. § 11. The Permians of Cumberland, especially their lower mem- bers, have an interesting bearing on the isolated Permian patches scattered over portions of the South of Scotland, and which, in Dum- friesshire, afford footprints. * Geol. Trans. 2nd Series, vol. iv. p. 399. 1862. | HARKNESS—PERMIAN STRATA. 217 In their mineral nature these Scottish Permians have a great affi- nity to the Rothliegende of the N.W. of England, and especially that portion which is seen in the Ormside and Hilton section. The Corncockle area exhibits the lowest beds of the Scotch equi- valents at several spots where these abut against the Lower Silurians. These lowest beds are breccias made up of fragments of the surround- ing Lower Silurians. One locality in this area, Dalton Hook, shows the inferior sandstones in proximity to the Carboniferous rocks. Here the breccias abound in limestone-fragments, have the aspect of the lower breccias of Burrels, and, like these latter, were formerly wrought for the limestone which they contain. Above the lower breccias the sandstones, with impressions as seen at Corncockle, occur; and any section taken across this part of Annandale would exhibit the arrangement seen in fig. 5, which is an extension of that given by Sir Wm. Jardine *. Fig. 5.—NSection across the Pernnan Strata of Annandale. Distance 8 miles. Muir. .-----Corncockle es We LLL Gy hee Yp—y hg typ, ZE Littl jp Ow ZL INTE SS SSS 3. Sandstone, with Fossil Footprints at Corncockle Muir. 2. Permian breccia. 1. Silurian rocks. The Annandale Permians do not show a full series of the Rothlie- gende: in order to see the other members, it is necessary to have recourse to the Nithsdale areas. The one which best exhibits this is seen in the district around Dumfries (fig. 6), extending from a Fig. 6.—Section of the Permian Strata of the southern part of the Valley of the Nith. W. E. Mabie Hills. River Nith. Craigs. Locher Moss. Forthorwald. > | Gy | : ae Yj OW Yj ' \ ts \ \ 4, Peat. 3. Permian breccia. 2, Sandstone with Footprints. 1. Lower Silurian rocks. * Ichnology of Annandale, p. 16. 218 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 19, mile E. of the Nith to about two miles W. thereof. In this section the lowest strata, well seen at Craig’s Quarry, are red sandstones with the same footprints as those of Corncockle, upon which, after passing through false-bedded sandstone, the thick mass of breccia forming a trough through which the Nith flows, and which extends to the Silu- rian hill W. of Dumfries, is seen. The sections of Annandale and Nithsdale collectively furnish the fol- lowing groups which compose the Permians of this part of Scotland :— first and lowest, breccias ; second, a thick series of sandstones, some of the strata of which are somewhat incoherent, and some flaggy, with footprints; and third and highest, a thick mass of breccias. This se- quence shows such an analogy to the inferior sandstones of Westmore- land as to justify the conclusion that in Scotland,so far as is yet known, the Rothliegende portion only of the Permians is exhibited. Another important circumstance connected with the Scottish Per- mians is the position of the footprints. Like those occurring in the neighbourhood of Penrith, which consist of Chelichnus Duncani, these impressicns appear to mark the middle portion of the Rothlie- gende—a position probably below that portion of the inferior sand- stone represented in the Hast of England, but which has very likely its equivalent in the well-developed Rothlhegende of Saxony. No allusion has been made to the geological age of the upper sandstones of the N.W. of England and the 8.E. of Dumfriesshire. Like similar strata in the 8.E. of Durham, they succeed the Zech- stein representatives of the Eden valley, and might therefore be regarded as Triassic. As Mr. Binney has noticed the occurrence of Liassic strata in North Cumberland, near the margins of the Solway Firth, which exhibit themselves in such a position as to lead to the conclusion that they repose in the trough formed by the upper sandstones, the Triassic age of these arenaceous deposits, with clay-beds, becomes highly probable *. Note.—In a memoir published in the 6th vol. of the Quart. Journ. of the Geol.Soc., having reference to the sandstones of the Vale of the Nith, I allude to them as appertaining to the same age as those of the Cumberland area, referring the whole to the Trias. This opinion I adopted in consequence of its being then a generally received one among geologists. Subsequently, in another memoir (vol. xii. p.266), I stated the reasons which induced me to alter this opinion, and to regard these deposits as belonging, for the most part, to the Per- mian age. 2. On the Dare of the Last Exevarton of Cenrrat Scornanp. By ArcnipaLtp Grrxiz, Esq., F.R.S.E., F:G.8., of the Geological Survey of Great Britain. Tat the central districts of Scotland, together with the greater part of the British Islands, have undergone a movement of upheaval within * Quart. Journ. Geol. Soc. vol. xv. p. 549. ' 1862. | GEIKIE—ELEVATION OF SCOTLAND. 219 a comparatively recent geological period is a fact which has long been familiar to the geologist. A line of raised beach, with shells of living species still in a perfect state of preservation, fringes many parts of the coast, at a height of from 15 or 20 to upwards of 40 feet above the present sea-level. This difference of elevation may point either to different periods of upheaval or to one great upward movement which varied in intensity in different parts of the island. For facts so well known it is only necessary to refer here to the papers of Mr. Smith of Jordan Hill, Mr. Maclaren, Mr. Chambers, and others who have described the evidence which different parts of the Scottish coast-line furnish as to arecent rise. The object of the present communication is to inquire how far we have data for ascer- taining the time at which at least the later stages of this rise took place. Ever since the publication, in 1838, of Mr. Smith’s great paper on the last changes of level in the British Islands*, the belief has been universal that no alteration of the relative position of sea and land has taken place within the last tivo thousand years, the coast-line being the same now as it was at the time of the Roman invasion. I shall have occasion, in a subsequent part of this paper, to examine the evidence on which such a belief is founded. With regard to the centuries prior to the Christian era, Mr. Smith remarks that probably no change of level has taken place within the human period}. For this statement, however, he adduces no other foundation than that mounds known as British tumuli, along with vitrified forts, exist close to the margin of the present high-water mark. The discovery of canoes in an elevated part of the old alluvium of the Clyde, and of other antiquities in that of the Forth, tended to throw some doubt on Mr. Smith’s assertion. Mr. Chambers, in his volume on ‘ Ancient Sea Margins’ (pp. 18-22), published in 1848, refers with hesitation to the possibility of these canoes having been in use prior to the last shift of the land, and the same view was entertained by other geo- logists; but in October 1850 he published an account of some anti- quities found in the Carse of Gowrie which he conceived to have been brought by an abnormal inundation within the historical period, and he then acknowledged his belief that those of Glasgow had been similarly imbedded, and that consequently they afforded no evidence in favour of a change of level since Scotland had been tenanted by manft. Such was the state of the question when, in the spring of last year (1861), I obtained evidence which seemed to show that a portion of the coast of the Firth of Forth had been elevated not only within the human period, but even since the first years of the Roman oceupation§. This observation involved so wide a departure from * Edin. New Phil. Journ. xxv. p. 385; and Mem. Wern. Soc. vol. viii. part i. t Mem. Wern. Soc. vol. viii. p. 58. t See Edin. New Phil. Journ. vol. xlix. p. 233. g Edin. New Phil. Journ., new series, vol. xiv. p. 107. Since this paper was written, more recent excavations have shown the existence of medieval 220 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19, preconceived opinions, and bore so closely on questions of the deepest moment regarding the antiquity of man, that I felt the necessity of examining other parts of the coast with the view of ascertaining how far the movement may have been general over the central districts of Scotland. It seemed to me advisable also to make a search through such archeological volumes as treat of our maritime antiquities, in | order to see whether any antiquary had detected proofs of physical changes. The results of these inquiries are now communicated to the Society. . The Firths of Clyde, Forth, and Tay are each bordered with a strip of flat land, varying in breadth from a few yards to several miles, and having a pretty uniform height of 20 or 25 feet above high-water-mark. This level terrace is the latest* and on the whole the most marked of the raised beaches. It must have been formed when the land was from 20 to 30 feet lower than at present, and evinces an upheaval which was nearly uniform over the whole of the central valley of Scotland. What, then, was the date of this upheaval ? P The discovery of human remains in the sands and clays of the raised beach affords the only ground for an answer to this question. From these strata canoes, stone hatchets, boat-hooks, anchors, pot- tery, and other works of art have been from time to time exhumed on both sides of the island. ‘These remains are usually claimed by the antiquary. He arranges them in his museum according as they belong to the Age of Stone, of Bronze, or of Iron. He speculates from them as to the character of the early races, and from the indi- cations which they may afford he compiles his prehistoric annals. But the geologist, too, has an interestin them. To him they are true fossils, as much as the footprint of a Reptile, the track of a Crustacean, or the tube of an Annelide. He deals with them as he deals with other evidence of the former presence of animal life. The circum- stance of their occurrence, the nature of the material in which they lie imbedded, the indications which they may afford of former di- versities of surface, whether of lake or river, land or sea, their association with the bones of animals now rare or extinct, and then pottery in the sands and silt of the section described by me as occurring at Leith. Attempts have been made to show that the deposit in which these fragments occur is merely artificial ground. Since this idea was suggested I have several times visited the sand-pit, both alone and in company with observers of greater experience than myself, and have been unable to alter the opmion I originally formed as to the true aqueous origin of the upper silt and sand. A hasty in- spection might lead one to confound these beds with an unconformable artificial earth which overlaps them, and to class together the contents of two very dif- ferent formations. The occurrence, however, of pottery, to which Mr. Franks of the British Museum can hardly assign a higher antiquity than 700 years, seems to show that the upper parts of this series of strata have been re-assorted in more recent times than I had supposed. But the subject requires further investigation, and until this is given, I am unwilling to depart from my original conclusion.—July 18, 1862. * here are occasional traces of a later terrace, as along the Clyde at Glasgow, — but these may for the present be disregarded. 1862. | GEIKIE—ELEVATION OF SCOTLAND. 221 their intrinsic character as illustrations of various stages in the onward march of human progress,—all these are points of view from which the geologist claims to study such remains. ‘The antiquities of man have thus a geological as well as an archeological interest. The day, indeed, is perhaps not far distant when archeology will form well-nigh as integral a part of geological science as palzonto- logy does now. ‘This conviction must, at least, be my apology for bringing before you some parts of a subject which is not usually held to come within the scope of the Geological Society. Along the margin of the Clyde at Glasgow, the raised beach ex- tends as a level terrace of varying width, its surface lying about 26 feet above high-water-mark. This plain, when sections are cut through it, is found to- consist of alluvial clay, silt, and sand, with layers of shells—the deposits of an ancient estuary. Its presence so high above the limits of even the extremest spring-tides or the highest recorded river-floods can only be accounted for by an actual upheaval of the land. No transient flood, of what magnitude soever, could deposit well-stratified lamine of fine silt and mud in regular succession to a height of 26 feet above the ordinary level of the estuary. The bed of the river, along with the surrounding country, must therefore have been raised; and hence any remains which may occur contemporaneously imbedded in these alluvial deposits must have been involved in the same upheaval. If it can be shown that human works of art lie beneath some of the undisturbed silt-beds, it will follow that the elevation has been witnessed by man. Human remains have been especially abundant in the alluvium of the Clyde. There is comparatively little variety, however, in their character, inasmuch as they have been almost entirely connected with the primitive navigation of the river. Within the last 80 or 90 years the hulls of no fewer than eighteen canoes have been exhumed, some of them even from under the very streets of the city*. The most important discoveries took place during the progress of those great excavations by which the harbour of Glasgow was widened and deepened. Twelve canoeswerethen obtained, the whole of which came under the notice of the antiquary, who in 1856, under the signature of J. B., communicated an account of them in the third volume of the work entitled ‘ Glasgow, Past and Present.’ With only one exception, they were all formed of single oak-trees. Two had evidently been scooped out by the action of fire; others had been hollowed with a rough implement, such as a stone axe; while several were cut beautifully smooth, evidently with metal tools. Hence a gradation could be traced, from a pattern of extreme rudeness to one showing considerable mechanical ingenuity. The average depth beneath the surface of the ground at which the whole were found was about 19 feet, or about 7 feet above the level of high watert. They all lay * For the details of the Glasgow canoes I am indebted to an interesting paper in ‘Glasgow, Past and Present,’ vol. ii., written, I believe, by that zealous anti- quary, Mr. Buchanan. +t The canoe found at an earlier date, on the site of the Tontine Hotel, lay about 21 or 22 feet above high-water-mark in the river. 222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19, at a distance of more than 100 yards back from the margin of the Clyde as it existed before the alterations began, and were chiefly im- bedded in a thick bed of finely laminated sand. Most of the Clyde canoes were formed out of single oak-stems ; but two of them were built of planks. Of these the more elaborately constructed was discovered on the property of Bankton, in 1853. A large oak had been cut longitudinally into a mere strip, as the back- bone of the boat, from which a long keel was formed underneath by being simply left standing out, while the back-bone was pared away, so that the keel appeared a mere longitudinal projection from the lower plane of the same strip. Strong transverse ribs were inserted for the skeleton of the back. These were clothed outside with deals about 8 inches broad, and they overlapped each other precisely as in modern clinker-work. The stern was formed of a thick triangular- shaped piece of oak, fitted-in exactly like those of our day. Again, the prow had a neat cutwater, rising about a foot above the gunwale, and giving it rather an imposing effect, not unlike, on a very small scale, the beak of an antique galley. The length of this curious vessel was 18 feet; width at the waist 5 feet, and at the stem 34 feet. When discovered, it was lying keel uppermost, with the prow pointing straight up the river. It had probably been capsized in a storm. The planks were fastened to the ribs, partly by singularly shaped oaken pins, and partly by what must have been nails of some kind of metal. The perforations where nails had been were uniformly square, and the marks of their broad heads driven home by smart blows deeply into the wood were very perceptible. None of the nails themselves were, however, to be seen; but several of the oaken pins were left. They were round, thicker than a man’s thumb, and ingeniously formed. The pin, after being rounded, had been sliced in two, and a triangular-shaped tongue inserted; so that, when driven into the deal, the pin would firmly hold its place*. In addition to these canoes, a polished celt of greenstone, a thin piece of lead perforated with nail-holes, and a plug of cork in the bottom of one of the vessels have also been discovered. Such are the remains of human workmanship which have been found in the elevated silt-beds of the Clyde. Do they of themselves afford any indication of the probable period during which this elevation was effected ? At the outset it must be borne in mind, that the occurrence of these canoes in the same upraised silt by no means proves them to be synchronous, nor even to have belonged to the same archeological period. The relative position in the silt from which they were exhumed could help us little in any attempt to ascertain their relative ages, unless they had been found vertically above each other. The varying depths of an estuary, its banks of silt and sand, the set of its currents and the influence of its tides in scouring out alluvium from some parts of its bottom and redepositing it in others are circumstances which require to be taken into account in all calculations as to the relative position of different parts of the bed of the stream in any * Glasgow, Past and Present, pp. 565-6. 1862. | GEIKIE—ELEVATION OF SCOTLAND. 223 former period. Hence mere coincidence of depth from the present surface of the ground, which is tolerably uniform in level, by no means necessarily proves contemporaneous deposition. Nor would such an inference follow even from the occurrence of the remains in distant parts of the very same stratum, A canoe might be cap- sized and sent to the bottom just beneath low-water-mark ; another might experience a similar fate on the following day, but in the middle of the channel. Both would become silted up on the floor of the estuary ; but as that floor would be perhaps 20 feet deeper in the centre than towards the margin of the river, the one canoe might actually be 20 feet deeper in the alluvium than the other; and on the upheaval of the alluvial deposits, if we were to argue merely from the depth at which the remains were imbedded, we should pro- nounce the canoe found at the one locality to be immensely older than the other, seeing that the fine mud of the estuary is deposited very slowly, and that it must therefore have taken a long period to form so great a thickness as 20 feet. Again, the tides and currents of the estuary, by changing their direction, might sweep away a con- ‘siderable mass of alluvium from the bottom, laying bare a canoe that may have foundered many centuries before. After the lapse of so long an interval, another vessel might go to the bottom in the same locality, and be there covered up with the older one, on the same general plane. These two vessels, found in such a position, would naturally be classed together as of the same age, and yet it is demonstrable that a very long period may have elapsed between the date of the one and that of the other. Such an association of these canoes, therefore, cannot be regarded as proving synchronous deposi- tion ; nor, on the other hand, can we affirm any difference of age from mere relative position, unless we see one canoe actually buried beneath another. Hence the only evidence that remains is that which may be afforded by the character of the antiquities. It is usual to speak of the canoes which have been from time to time exhumed in Scotland as of an extremely rude construction, and as the relics of a very bar- barous people. They are described along with the stone implements of the Stone Period, standing thus as far back in the past as the antiquary can place them*. Butitis manifest that most of the Glasgow canoes cannot be spoken of as works of extreme rudeness. One or two of them, indeed, were certainly primitive enough in their construction ; but the Bankton boat could not have been built by a race of savages. It is, indeed, impossible to avoid the conviction that the rough-hewn, fire-burnt oak-trunks must have belonged to an earlier time than that of the smoothly cut canoes, and that these again date further back than the regularly built boat of Bankton. The first class may be a relic of the Stone, the two latter of the Bronze Period, if, indeed, the boat came not within the Period of Iron. We seem to see, in the various stages of mechanical skill © shown in these primitive vessels, a record of the gradual progress of * See Dr. Wilson’s ‘ Prehistoric Annals of Scotland,’ chap. ii. Vor,

JunE 4, 1862. The Rey. David Honeyman, Antagonish, Nova Scotia, and Alex- ander Macdonald, Esq., Aberdeen, were elected Fellows. The following communications were read :— 348 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, 1. On the Diseurep Arrinity of the Mammatran Genus Plagiaulax, from the Purseck Beps. By Hvuex Fatconrer, M.D., F.RB.S., F.G.8., &e. Ont of the most accurate observers and original thinkers of our time has discoursed with emphatic eloquence on the imperfection of the geological record*. Besides what is yet to be discovered, so much has been irrecoverably lost that we may never hope to write more than disconnected pages of the paleo-biography of nature. The truth of the assertion comes home to the conviction of all; but so far from discouraging, it only renders us the more eager to pursue what we may attain. Every now and then, in paleontology, an unknown form is discovered of so unexpected a character, that our habitual train of ideas is diverted by it into a new avenue of thought. It may confirm a position which has before been merely conjectural, or but faintly shadowed out ; or it may shake the foundations of some cherished, but unsound, hypothesis. It is hailed with more especial satisfaction if it contribute to fill up any of the great gaps in our existing knowledge. The form itself is often presented to the first observer in such a mutilated or imperfect aspect, that at the best he can effect little beyond an approximative idea of the outline. From the same cause, or from a balanced conjunction of unusual charac- ters, he may fail in his first attempt at the interpretation ; but he has no reason to be ashamed of the failure, if he has devoted his powers fairly to the investigation; for a great part of the solid progress made in science is mainly effected by the later observer correcting the errors of those who have preceded him. Reproach can only be felt when we allow some bias unduly to influence our interpretation—when we strain facts to countenance a particular view. If the observer has guarded himself against this weakness, and with care used the proper means of investigation, whatever op- position his results may at first encounter, generally speaking, he may be at ease, in the assurance, that further research and future discovery will only confirm and extend them. If the conclusions are challenged, science is invariably benefited by the controversy. Different modes of analysis and different trains of ideas are brought into conflict; and landmarks are established for the warning and guidance of future observers. Among the mammalian forms brought to light through Mr. Beckles’s important researches in the Purbeck Beds, there was one which struck me with especial interest. I found in it a singular combination of characters :—the dentition modified by suppression to as great an ex- tent as in any existing form; strong analogies, in some respects, with known genera, while in others it diverged from them very widely. Early in 1857 I communicated to the Geological Society an account of the genus Plagiaulaw, which appeared in the 13th volume of the ‘ Quarterly Journal’ (p. 261). About the same time an abridged description of the form, illustrated by figures, was brought out in the Supplement to the 5th edition of Sir — * Darwin, ‘On the Origin of Species,’ p. 287. 1862. ] FALCONER—PLAGIAULAX. 349 Charles Lyell’s ‘ Manual of Geology’ (1857, p. 17). On both occa- sions I arrived at the conclusion that “‘ Plagiaulaw may be regarded in the natural system as a Marsupial form of Rodent*, constituting a peculiar type of the family to which Hypsiprymnus belongs,” although widely distinct from that genus. The only comment impugning this determination that has come under my notice, appeared in the Article “ Paleontology,” by Pro- fessor Owen, in the 8th edition of the ‘ Encyclopedia Britannica t,’ published in January 1859, and subsequently reproduced as a sepa- rate work{. ‘The two accounts differ in some unimportant particu- lars. I here cite the later in date, as presumably conveying the latest views of the author. The following are extracts :— «Two specimens exemplified the shape and proportions of the entire jaw of this species [Plagiaulax Becklesii]. The foremost tooth is a very large one, shaped like a canine, but implanted by a thick root in the fore part of the jaw, like the large lower incisor of a Shrew or Wombat. The three anterior teeth in place have com- pressed trenchant crowns, and rapidly augment in size from the first to the third. They are followed by sockets of two much smaller teeth, shown in other specimens to have subtuberculate crowns re- sembling those of Microlestes. The large front tooth of Plagiaulax is formed to pierce, retain, and kill; the succeeding teeth, like the carnassials of Carnivora, are, like the blades of shears, adapted to cut and divide soft substances, such as flesh. As in Carnivora, also, these sectorial teeth are succeeded by a few small tubercular ones. The jaw conforms to this character of the dentition. Itis short in proportion to its depth, and consequently robust, sending up a broad and high coronoid process, for the adequate grasp of a large temporal muscle ; and the condyle is placed below the level of the grinding teeth,—a character unknown in any herbivorous or mixed-feeding Mammal ; it is pedunculate, as in the predaceous Marsupialia, whilst the lever of the coronoid process is made the stronger by the condyle being carried further back from it than in any known carnivorous or herbivorous animal. The angle of the jaw makes no projection below the condyle, but is slightly bent inward, according to the Marsupial type.” “In the general shape and proportions of the large premolars and succeeding molars, Plagiaulax most resembles Thylacoleo (fig. 173, pm,1 and 2), a much larger extinct predaceous Marsupial from tertiary beds in Australia. But the sectorial teeth in Plagiaulaw are more deeply grooved; whenceits name. The single compressed premolar of the Kangaroo-rat is also grooved ; but it is differently shaped, and is succeeded by four square-crowned, double-ridged grinders, adapted * T leave the words as they originally stood ; but my meaning would have been more accurately conveyed by the expression ‘“‘ Rodent type of Marsupial,”—rodent being here used in the large sense, having reference to the plan of dentition, cha- racterized by two collateral incisors in the lower jaw, as typically shown in the placental series by the Rodentia and Cheiromys; and in the Marsupialia by Phascolomys, modified in the Macropodide and the Phalangistide by the opposi- tion, in the upper jaw, of several incisors. (See Cuvier, Oss. Foss., 4th edit. tom. v. p. 3.) t Vol. xvii. p. 161. t Paleontology, 2nd edit. p. 353. 350) PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, for vegetable food ; and the position of the condyle, the slenderness of the coronoid, and other characters of the lower jaw are in con- formity to thatregimen. In Thylacoleo the lower canine or canine- shaped incisor projected from the fore part of the jaw, close to the symphysis, and the corresponding tooth in Plagiaulax more closely resembles it in shape and direction than it does the procumbent in- cisor of Hypsiprymnus. From this genus Plagiaulaa differs by the obliquity of the grooves on its premolars; by having only two true molars in each ramus of the jaw, instead of four ; by the salient angle which the surfaces of the molar and premolar teeth form, instead of presenting a uniform level line; by the broader, higher, and more vertical coronoid; and by the very low position of the articular condyle. “The physiological deductions from the above-described charac- teristics of the lower jaw and teeth of Plagiaulax are, that it was a carnivorous Marsupial. It probably found its prey in the contem- porary small insectivorous Mammals and Lizards, supposing no her- bivorous form, like Stereognathus, to have co-existed during the Upper Oolitic period ”’*, We have here an opinion, professing to be founded on the high ground of a connected series of physiological correlations, that Pla- guaulax was a carnivorous Marsupial; while the same materials led me to infer that it was phytophagous. These diametrically opposed inferences recall, in some degree, the discussion, famous in its day, respecting the disputed affinities of Amphitherium. The question then was, whether the fossil was mammal or reptile; and the foun- dations of Paleontology were supposed to be concerned in the issue. In the present instance the area of the field of difference is less, but the interests involved are still important. Are the indications of paleontology, more especially in its great stronghold in the Mam- malia—the teeth and correlated organs—so unstable or so obscure, that of two paleontologists, the same dental and mandibular mate- rials shall lead the one to infer that the fossil form was a vegetable feeder, and the other that it was a predaceous carnivore? Or does this conflict of opinion arise from different methods having been fol- lowed by the observers in dealing with the evidence ? As the Geological Society gave to my original communication a place in its Journal, I feel bound, in the interest of science, either to support the opinion which I then advanced, or frankly to admit the correction, if | am found to be in error. Jam further impelled by my sense of self-respect, as an observer, to consider whether—apart from the conclusions—lI have fallen into such errors of observation and description as would necessarily be implied, should Professor Owen’s manner of viewing the objects prove correct; and if so, to explain the fallacious train of reasoning which led me astray ; for I cannot plead the excuse that the account was written in haste, or without due consideration. If the data, upon which the author of ‘ Paleontology’ professes * Paleontology, p. 353. I entertain strong doubts about the soundness of the deduction which makes Stereognathus to have been herbivorous. 1862. | FALCONER—PLAGIAULAX. 351 to rest his physiological deductions, were sound, the demonstration would be complete. They are put together with an exemplary show of harmony, and, with a single exception, every link in the chain is supplied. But there are, in the case, considerations of paramount import in an argument of this nature, that lead me to question their soundness, and to dissent from the conclusions. And first, as regards the admitted facts. Professor Owen agrees that the Purbeck remains establish two species of Plagiaulax ; and, as he has adopted two of the wood-cuts given in my original descrip- tion of these species, it is presumed that the correctness of the figures is not questioned. The marsupial nature of the forms is not dis- puted, nor is there any difference of opinion about the number or designation of the teeth. In both species there is a solitary incisor on each side of the lower jaw, in the fore part of the incisive border, closely followed, without the interposition of a canine, by a series either of three or of four premolars. The rami converge to a narrow point in front, so that the tooth occupies the entire width of the incisive border on each side ; and fig. 13, p. 280, of my former communication, representing the symphysial portion endwise, shows (what is confirmed by the other figures) that the two incisors were approximated and collateral, as in the rodent type, placental or marsupial. In P. minor, fig. 15, the tooth is procumbent. In the other and larger species, P. Becklesi, it is more robust, with a thicker root, and with a more decided curvature upwards, suggesting, at the first sight, some resemblance to the form of a canine. In both species the point is bevelled* ; and I failed to observe in either any mark of the play of an opposed upper tooth. What was the function of these incisors? Professor Owen’s opinion is expressed thus: ‘‘The large front tooth of Plagiaulax is formed to pierce, retain, and kill.” This conclusion arrived at, the other characters are naturally regarded in unison with it, until the genus is finally presented to us as a predaceous carnivore. It is therefore necessary to examine the evidence closely. Now, in solving a question of this kind, comparative anatomy supplies for our guidance fundamental principles, which govern the interpretation of mere form. Let us revert to the known marsupial genera, and see what light generalized observation upon them throws upon the ques- tion. In all the Carnivorous genera and species, fossil or recent, of which the dentition has been accurately determined, there are three or more incisors, followed by a canine, on each side of the jaw, above and below; and the empirically observed result is consistent with a rational interpretation of the arrangement, in reference to their food and the means of procuring it. On the other hand, in all the ex- isting strictly phytophagous genera, there is only a solitary incisor (being that next the axis) on either side of the lower jaw, and no canine; or if, as among the Phalangers, additional teeth are deve- loped, the outer incisors and canine are alike rudimentary. The pair * Not in the sense of being denuded of enamel by wear ; but the posterior sur- face is flattened near the apex, so as to yield a slightly bevelled point (op. cit. p- 268). 352 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, of developed incisors are approximated and placed collaterally, as in the placental Rodents; and commonly they are projected forwards with but a very slight upward inclination. They are unequally op- posed in the upper jaw by two or more incisors on either side. Why there should be this plurality of incisors above, and only two inva- riably occupying the same position below, is wholly unknown to us; but the constancy of the structure makes it certain that there must be a sufficient cause for itin nature; and we employ the generaliza- tion, empirically arrived at, with as much confidence as we do the law of necessary correlation*. In many critical cases, where the evidence is limited or defective, the empirical is even a safer guide than the rational law, since it is freer from the risk of errors of interpretation. Applied to the instance before us, it is manifest that the principle on which the incisors in Plagiaulaw are framed, in regard of number, order of suppression, collateral position, and re- lation to the premolars, corresponds exactly with the type of the Marsupial Herbivores, such as Halmaturus, Hypsiprymnus, and Phas- colarctus, and that it is wholly at variance with the Carnivorous type. Let us now test the opinion in its professed character as a physio- logical deduction. Throughout the Mammalia, where teeth perform the functions of canines, ‘to pierce, retain, and kill,” they are held well apart through the interposition of a line of incisors,—the end being obvious: the points of penetration are doubled, the grasp is strengthened by widening the base, and the dilacerating and killing powers are multiplied. To arrange them collaterally in the axis would be to place them at a disadvantage to the end to be attained. But when a gnawing power is required, the middle incisors are power- fully developed, and placed collaterally in the axis of the jaws, one on each side, above and below, as typically exemplified in the pla- cental Rodents and Cheiromys. Doubtless, a Rat when seized can inflict a smart wound on the hand: but the power is a secondary at- tribute, complementary to the main function. Regarded in this aspect, it 1s negatively stamped upon the incisors of Plagiaulax by their collateral position, that they are not constructed upon the Car- nivorous plan of design, nor in rational correlation thereto. It is obvious that this position of the teeth in Plagiaulax was not overlooked by the author of ‘ Paleontology ;’ for, on the first oc- casion, he describes the incisor of P. Becklesii as being “ very large, shaped like a canine, but implanted by a thick root in the fore-part of the jaw, like the large lower incisor of a Kangaroo or Wombat.” But the shape of the tooth prevailed in deciding him to pronounce it carnivorous. Now, the form differs in the two species: and I ask any Comparative Anatomist to look at fig. 15 of my former commu- nication (p. 281), and say whether the tooth there represented is formed to pierce, retain, and kill—being the attributes with which Professor Owen invests the incisor of P. Beckles. It is projected forwards with a slight upward inclination, somewhat asin the vege- * Cuvier, ‘ Discours Préliminaire,’ p. 51. af Encyclop. Brit., 8th edit. vol. xvii. p. 161. ‘‘Shrewand Wombat” are sub- ~ stituted in the ‘ Palzontology,’ p. 353. 1862. | FALCONER—PLAGIAULAX. 353 table-feeding Koala (Phascolarctus cinereus). The incisor of P. Becklesii* is undoubtedly curved more decidedly upward ; and, when viewed sidewise, it is not very unlike a canine. But the same may be said equally of the lower incisor of the Lemurine Aye-Aye (p. 368, fig.20,a). In this remarkable form, the affinities of which were so keenly disputed by the great French anatomists, Cuvier and Blain- ville, the solitary incisors are collateral, on the Rodent type; com- pressed laterally, and very deep at the base, they sweep upwards in a bold curve, being scooped vertically behind, to terminate in a sharp edge; so that, regarded sidewise, so far as vertical direction goes, they are more canine-like than in either species of Plagiaulax. But the resemblance goes no further. In the former the incisor, which is only partially invested with enamel, is continued backwards below the molars, the pulp-nucleus being persistent, and the chisel- shaped edge is constantly maintained by uset—conditions which are wanting in the latter. Should the construction of the skull and other parts of the skeleton of P. Becklesit be ever discovered, there is little doubt but that modifications will be detected throughout, in conformity with those of its incisors, as in the felicitous instance cited by Cuvier, of the secret relation between the upper canine- shaped incisors of the Camel and the bones of the tarsus: this ex- ceptional character does not remove the Camel from among the Ruminants, nor does the form of the incisor of P. Becklesu appear to me to be of sufficient weight to counterbalance the clear evidence of a phytophagous and rodent plan of construction. Professor Owen draws an argument, in confirmation of his view, from the dentition of Thylacoleo. The statement is :—*‘ In Thyla- coleo the lower canine, or canine-shaped incisor, projected from the fore-part of the jaw, close to the symphysis ; and the corresponding tooth in Plagiaulax more closely resembles it in shape and direction than it does the procumbent incisor of Hypsiprymnus”t. But, on referring to his detailed description of Thylacoleo, we find that the body of the tooth, of which the shape and direction are adduced as terms of comparison, together with the fore part of the symphy- sis and incisive border, is wanting §:—‘“ The symphysis (pl. 13. fig. 4, s) begins behind, at a vertical line dropped from a little in advance of the middle of the sectorial, » 4; it is of a wide and oval form. ‘To judge from the cast, but little of the jaw appears to have * Loc. cit., fig. 1. p. 278. + Blainville asserts that the incisors of the Aye-Aye are invested all round with a shell of enamel, and that the posterior facet 1s not the result of wear (Mémoire sur l’Aye-Aye, p. 23); while Dr. Sandwith, in his interesting ac- count of the habits of this animal, affirms that the facet is denuded, as in the _ Rodents (Zvol. Proc., Feb. 22,1859, p. 111). In a finely preserved cranium, for the transmission of which to London I am indebted to the great courtesy of M. Edouard Verreaux of Paris, it is distinctly seen that the coat of enamel is limited to a belt which sheathes only the anterior half of the incisors. { Paleontology, p. 353. § “Unfortunately, this morceau is much mutilated, the incisor being broken at its entrance into the alveolus; its form cannot therefore be precisely given ; but it is evident that it was curved upwards.’’—Stutchbury, Report on the Dis- covery of Gold in Australia, 1855, p. 53. 354 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, been broken away from the fore-part of the symphysis. The upper and fore-part shows the alveolus and base of a tooth (pl. 11. fig. 3, c) which has projected obliquely upward and forward. It is separated by an interspace of 3 lines from the sectorial, and would seem to be the sole tooth in advance of it. If the ramus be really produced at the upper part of the symphysis further than is indicated by the present cast, i may have contained one or more incisors, and the broken tooth in question may be the lower canine. If, however, this be really the foremost tooth of the jaw, it would appear to be one of a pair of large incisors, according to the Marsupial type exhibited by the Macropodide and Phalangistide”*. ‘* But in the lower jaw the carnassial is succeeded by two very small tubercular teeth, as in Plagiaulax ; and there is a socket close to the symphysis of the lower jaw of Thylacoleo, which indicates that the canine may have termi- nated the dental series there, and afforded an additional feature of resemblance to the Plagiaulax”’ +. In all this, it will be seen, the argument is within the domain of conjecture ; the tooth oscillates between canine and incisor ; and not merely so, but the principles which are followed as guides in this walk of investigation are set aside, to give place to the illusory in- dications of mutilated external form. If the tooth represented by a stump or socket proves to be a canine, the comparison will not hold; but if it be solitary with the position of an incisor, will it even then bear out Professor Owen’s hypothesis, that Thylacoleo, which he in- fers to have been one of “ the fellest and most destructive of preda- tory beasts t,’”’ may have had the laniary portion of its teeth in the lower jaw constructed on the type of the most meek and defenceless of herbivorous marsupials? Bearing in mind the sense in which the term “ type” is accepted among naturalists, [ must avow, that I have some difficulty in realizing the conception. But, should the unusual conjunction of characters assumed above be hereafter established, there are theoretical considerations which would prove to demonstra- tion that the types of construction are still absolutely distinct. For in the supposed case the outermost incisor would be the one deve- loped, the inner ones being suppressed; while, conversely, in the Macropodide it is the innermost incisor which is developed, the outer ones being suppressed. Morphologically, therefore, the types of con- struction would be radically different. If paleontological investiga- tions were conducted in this manner, there would be no limit to conjecture; the landmarks which we profess to follow would be disregarded, and disorder would face us everywhere. But, happily, seience furnishes unerring principles, which provide the corrective. I need hardly add that the argument drawn from T'hylacoleo has, in my view, no bearing on the incisors of Plagiaulax, and gives no » support to the carnivorous inference. Next, as regards the premolars. From their peculiar characters, and remarkable development, they furnish the most striking features * Phil. Trans., vol. cxlix. p. 318. t Paleontology, p. 432. t Phil. Trans., vol. cxlix. p. 319. 1862. | FALCONER—PLAGIAULAX. 355 in the dentition of the fossil genus. In P. Becklesii there are three, and in P. minor, four of these teeth, which diminish rapidly in size from the last to the first*. I here take the last as the most deter- _minate in form, and in its nature the most constant. I compared it rigorously with the corresponding tooth of Hypsiprymnus Gaimardi, and I affirm now, as I did in my original paper, that these homo- logous teeth, in the two genera, are identical in every essential point of form and construction. In proof, I refer to figures 5 and 6 of the representations above cited, the former showing the last premolar of Plagiaulax, the latter of Hypsiprymnus. The resemblance is so manifest and direct, that I never contemplated that it could be called in question ; but, as it has been questioned, it is necessary to descend to particulars. In both, the crown viewed from the side is of a quadrately oblong form, the length exceeding the height; in both, it is compressed and trenchant, the sides sloping uniformly from the base to a thin edge like a wedge; in both, the basal part of the tooth presents a smooth surface, above which the crown is traversed by a series of close-set, uniform, and exquisitely defined parallel grooves, sharply angular, and bounded by linear ridges ; in both, these grooves occupy both sides of the tooth; and in both, the channeled sides meet in a finely serrated edge. Not the least remarkable point in this striking list of agreements is the curious numerical coincidence, —these grooves being developed seven in number, alike in the homo- logous premolars of Pl. Beckleswi and of Hypsiprymnus Gaimard. As to the points of difference: in Plagiaulaw there are three or four of these teeth, while in Hypstprymnus there is but one; in the former, they are presented with the maximum of development, in the latter with the minumum ; in the former the grooves are diagonal, in the latter vertical. With this exception, and with some trivial de- tails of difference in the proportion of the length of crown to its height, and in the amount of the basal surface free from grooving, the last premolar in Hypstprymnus is identical in its characters with that of Plagiaulax. The two convey to my mind the impression of being typically alike. The objects strike Professor Owen in a very different light. His statement is that, ‘in the general shape and proportions of the large premolar and succeeding molars, Plagiaulaw most resembles Thyla- coleo, a much larger predaceous marsupial, from the tertiary beds in Australia. But the sectorial teeth in Plagiaulaw are more deeply grooved; whence its name. The single compressed premolar of the Kangaroo-rat is also grooved; but it is differently shaped,” &c. Now, apart from the inferences, here is a conflict of description, which can be settled by an appeal to the original specimens. I have described the large premolar as essentially alike in form, in the Kan- garoo-rat and in Plagiaulax. Professor Owen states that it is dif- ferently shaped in the two: if so, I invite him to show wherein the difference consists (I have failed to detect, and he as yet to indicate it),—bearing in mind that here it is not a question of slight difference, * See Quart. Journ. Geol. Soc., vol. xiii. pp. 278-281, figs. 1-15. VOL. XVIII.—PART I. 28 306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. June 4, such as a modification in the outline of the same organ in two nearly allied forms, but a difference of type—or of ordinal importance. Next as regards the assertion that in the general shape the large premolar of Plagiaulaw most resembles Thylacoleo. For convenience, - I separate the two terms of the comparison in the sentence. Pro- fessor Owen has figured and described the sectorial teeth of this large Marsupial, in his late memoir on the “ Fossil Mammalia of Australia”*. In Thylacoleo the inferior premolars are reduced to a single, but enormously large and massive, carnassial, with two small tubercular teeth behind it. This carnassial (figs. 16-19) consists of a long blade, high in front and lower behind, so that, if notched in the middle, the divisions would in some degree resemble the anterior and posterior lobes of the corresponding tooth in the placental Carnivorat; and the worn summit is distinctly concave lengthwise: conversely, in both species of Plagiaulax the cor- responding tooth is convex, and the outline of the whole series de- scribes a convex curve, of which the last premolar forms the most salient part. The base of the carnassial in T’hylacolco is “ slightly grooved vertically” on the inside (fig. 16). These indentations dis- appear about half-way up towards the edge, where the surface be- comes reticulately rugose, being precisely the reverse of what occurs in the last premolar of Hypseprymnus and Plagiaulax. Besides the difference of their position upon the tooth, the grooves of the car- nassial of Thylacoleo present the appearance of furrows, separating superficial undulations of the enamel. A transverse section of the basal part of the crown would yield a faintly crenated outline, wholly different from the salient and reentering angles of the close-set parallel grooves of Plagiaulaw and Hypsiprymnus. These undulations are exhibited chiefly, if not solely, on the inner side; their presence on the outer is not mentioned. Further, if the indentations on the premolar of Thylacoleo are to count for anything as significant of affinity, it should be with Hypsiprymnus rather than with Plagi- aulax, since the furrows are vertical in the two former. In fact, in the outline and proportions of the vertical section, the premolar of Thylacoleo differs less from Hypsiprymnus than it does from that of Plaguaulax. Ihave failed to realize the asserted resemblance be- tween Plagiaulax and Thylacoleo in the form of the last premolars ; and in the details of outline, section, curvature of edge, crenulation, surface-markings, &c., | am more impressed with the differences than with any one point of agreement. Let us now consider the inference as to the function of these teeth. It is expressed thus :—“ The large front tooth is formed to pierce, retain, and kill: the succeeding teeth are like the blades of shears, adapted to cut and divide soft substances like flesh,” &c. Professor Owen has elsewhere described the premolar of Hypsipr ymNUs as * Phil. Trans., vol. exlix. p. 318, pls. 11 and 13. + “The first molar is lunate, the cusps turning inwards, the anterior cusp rising at a salient angle, the edge is trenchant outwards ; the second molar is tri- angular with a large anterior cusp, and a slight ridge passing to a small depressed. posterior cusp.”’—Stutchbury, Joc. ct. 1862. | FALCONER—PLAGIAULAX. Bod trenchant *, and I have shown above that the tooth is essentially alike in Plagiaulax. If, therefore, the function is to be deduced with such facile certainty from the mere form, the premolar of Hypsiprymnus ought also to be carnivorous. But we know that the genus is so strictly herbivorous that the family to which it belongs has been regarded as representing in the Marsupialia the Ruminants of the Placental Mammals. With this fact before us, is it likely that the premolars of Plagiaulaw were applied to cut and divide flesh? Does the serrated edge indicate a flesh-cutting function ? The singular agreement between the two genera in their premolars, down even to the number of grooves, however trivial and unim- portant the character may appear to be, has, I confess, weighed greatly with me in forming my opinion. No special function has, as yet, been connected with the peculiarly grooved tooth of the living Kangaroo-rat. The agreement is therefore purely empirical ; but as the character, according to our present knowledge, is confined, among many hundred genera of Mammalia, to certain species of Hypsi- prymnus and to Plagiaulax, those who have faith in the constancy of the manifestations of nature will not lightly believe that it was common to these two genera alone without implying affinity; and when this is coupled with the obviously phytophagous type of the incisors, the conviction will be confirmed. I need hardly add that I regard the carnivorous deduction from the shape to be arbitrary and untenable. | William Hunter, a century ago, by a parity of reasoning, arrived at the conclusion that the Mastodon of North America, from the trenchant form of the transverse crown-ridges of its molar teeth, was an extinct, colossal, carnivorous animal, in short, a kind of predaceous flesh-eating Elephanty. The error in his case, as in the correspond- ing one of Leibnitz, was excusable, comparative anatomy having been then in its infancy. But it is not a little startling to see the same sort of unsound deduction reproduced, in regard of one of the most pigmy of Mammals, half a century after Cuvier, by his luminous demonstrations, had indicated the method by which such signal mis- takes might be avoided in future.—Oct. 15th. ] Professor Owen perceives another indication of resemblance be- tween Thylacoleo and Plagiaulax in the proportions of the large premolar to the succeeding molars. In both, there are but two molars, and in so far the agreement is clear; but no further. In Plagiaulux there are as many as four premolars; while in Thyla- coleo the enormous development of the solitary premolar or carnassial is effected at the expense of the rest of the premolars, which are suppressed, and of the tubercular teeth, which are dwarfed. In the former, as pointed out in my earlier description, “‘ the premolars are inordinately developed, while the true molars are dwarfed and rudi- mentary in proportion.” The operation of the well-known law of Anamorphosis or Balancement is visible in both. But examples of it are everywhere seen throughout animated nature, in the same * Odontography, vol. i. p. 389. + Phil. Trans. 1767, vol. lviii. p. 38. 2B 2 358 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, organ, without reference to affinity, as, for instance, among the Mammalia, in the canine of Machairodus and of the Musk-deer. Thylacoleo and Plagiaulaw may be regarded as being as wide apart among the Marsupials as the two former are among Placental Mammals. The solitary trenchant premolar in some of the species of Hypsiprymnus is said to attain a very large development. We have the authority of Professor Owen for the statement, that in two Potooroos of New Guinea its antero-posterior extent nearly equals that of the three succeeding molars*. If the teeth of Thylacoleo and Plagiaulaw had been on the same morphological plan of construc- tion, the agreement in the number of molars would clearly have carried weight; but, as such does not appear to be the case, the co- incidence ought not to overrule the other indications, more especially as the form of the crowns of the molars in the two genera is totally different. In Thylacoleo, the first tubercular tooth has the crown compressed, supporting two cusps on its axis, the anterior lobe being more or less conical, with a smaller lobe behind it, both on the usual carnivorous type of construction. The second tubercular is only known through its socket. In both species of Plagiaulax, the two molars present oblong crowns, supporting two opposed lines of mar- ginal eminences, separated by a depression. In my original descrip- tion, I referred to the fact that in Dromicia and Acrobata the molars are reduced from the ordinary number, four, to three. In Plaguaulax the suppression is carried still further, two only being developed. The agreement in. this respect between the latter and T'hylacoleo does not impress me with the idea of affinity, although admitting, as I do, that it ought to be duly weighed. I have entered in such detail upon the dental characters, because, by the consent of all observers, they are of paramount weight in the solution of a question of this nature. If the type be distinctly indi- cated by them to be herbivorous or carnivorous, the other charac- ters, however modified they may be, will ultimately be found to be in relation to the teeth. The author of ‘ Paleontology,’ having formed his opinion on the teeth, then examines the characters of the lower jaw and finds them in conformity. He adduces the shortness of the horizontal ramus in proportion to its depth as indicative of robustness; also the broad and high coronoid process, and the peduncu- late condyle placed below the level of the grinding teeth (above, p. 349). They are all regarded as proving a carnivorous type. They were not overlooked in my former communication :—“ The charac- ters of the jaw are so peculiar, and in some respects of so mixed and complex a nature, that they ought to be weighed with caution, in conjunction with the teeth, in forming any opinion of the affinities of Plaguaulax. The low position of the condyle is so pronounced, and the elevation of the coronoid above it so considerable, that, regarded per sé, Supposing no teeth had been discovered, they might have been considered to imply with some degree of certainty a predaceous ani- mal”+. But there were other characters, which, taken in conjunction * Odontography, vol. i. p. 389. + Quart. Journ. Geol. Soc., vol. xiii. p. 273. 1862.] FALCONER—PLAGIAULAX. 359 with the jaw, appeared to me to counterbalance these indications : namely, the moderate extent and low elevation of the coronoid above the grinding-plane of the teeth; the long neck and horizontal pro- jection of the condyle behind the coronoid ; the form of the condyle itself; and the absence of a stout angular process behind it. With one exception, I shall consider these mandibular characters briefly. And first, as regards the shortness of the horizontal ramus in pro- portion to its depth. I refer my reader to fig. 20 of the accompany- ing illustrations, representing the side view of the lower jaw of the Aye-Aye. A glance will satisfy him that the horizontal ramus is much deeper in proportion to the length in this form than it is in P. Becklesu. The fact is so obvious that I do not think it necessary to enter upon the metrical details. Commonly we connect the idea of robustness in the lower jaw with the form and section of the mandible presented by the Hyzena and Tiger. If the sections, figs. 2 and 3, p. 278, of my original paper are referred to, it will be seen that they are totally different. The jaw of Plagiaulaw in this respect also closely resembles that of the Aye-Aye™*. The coronoid process comes next for consideration. For the de- tails of my description of it, I refer my readers to p. 268 of my former paper. It is there stated that “in general form the coronoid pro- cess in Plagiaulax resembles more that of the predaceous marsupials, and of the Ursine Dasyurus especially, than that of the herbivorous families. It differs very markedly from the elevated strap-shaped coronoid of Hypsiprymnus and the other herbivorous marsupials. It is to be remarked, however, that it is less elevated, and its surface of less area, than in the predaceous genera, whether marsupial or pla- cental.”” Here, it will be observed, the comparison was restricted to marsupial forms, beyond which I did not then think it necessary to earry it. If extended to the Aye-Aye (fig. 20), additional light is thrown upon the character. In both, the anterior edge reclines at an angle of about 45°; in both, the summit is not much elevated above the grinding-plane of the teeth. The appearance of elevation, which is at first sight suggested by the coronoid of Plagiaulax, arises from the great depth of the sigmoid notch and the low position of the condyle. If fig. 1 of the illustrations of my former paper be re- ferred to, it will be seen that the process itself is not raised much above the summit of the premolars. There is a further agreement between the Aye-Aye and Plagiaulax in the amount of area occupied by the surface of the coronoid. This is partly disguised in the lower jaw of the former, by the broad neck of the condyle, and the shallow- ness of the lunate notch between it and the coronoid ; if the notch were deepened, as indicated by the dotted line, the resemblance would be complete. I do not, therefore, admit the force of Professor Owen’s remarks, as significant of carnivore affinities, that “ the lower * In the Koala (Phascolarctus cinereus), in which the procumbent incisors, as already observed (above, p. 353), are projected with an inclination resembling that of Plagiaulax minor, the horizontal rami of the lower jaw present great depth in proportion to the length, with a compressed section. (Waterhouse, ‘Mammalia,’ vol. i. p. 264.) But the ascending ramus, in that genus, is on a totally different plan of construction. 360 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, jaw is short in proportion to its depth, sending up a broad and high coronoid process for the adequate grasp of a large temporal muscle ”’ —seeing that all these characters are combined in an existing gliri- form Tiemur, which is not a carnivore. The descriptive terms applied to the coronoid would be suitable for that of a Tiger or Stoat, but they seem hardly enpaeai to the process of Plagiaulax. The author of ‘Paleontology’ lays stress on the low position of the condyle, and its long horizontal neck: “The condyle is placed below the level of the grinding-teeth,—a character unknown in any herbivorous or mixed-feeding Mammal; it is pedunculate, as in the predaceous Marsupialia; whilst the lever of the coronoid is made the stronger by the condyle being carried further back than in any known carnivorous animal.” But it is not a little remarkable that he is silent regarding the form of the condyle itself,—the most important of all the mandibular characters after the teeth; for the peduncle, on which he lays weight, is, like the fang of a tooth, but the stalk upon which the organ performing the function is borne. I think it necessary therefore to call attention to the remarks on the subject contained in my former paper. In the true Carnivorous type, the condyle shows more or less of a cylindrical or terete surface, having invariably a transverse direction, by which it is locked in the glenoid cavity of the upper jaw, thus constituting a pivot like that of a pair of scissors, which constrains the blades to a vertical motion. In Plagiaulax all these conditions are reversed, the condyle being convex, with its long diameter disposed subvertically ; ; regarded endwise, it is narrow in proportion to the height, and the outline is ovate or pyriform, the broad end being uppermost. ‘This is a form which is unknown among the Carnivora, but common in the Pla- cental Rodents, with the difference, however, that in the latter, the condyle having to work backwards and forwards in a groove, its articular surface is disposed longitudinally. In the common Norway Rat, the articular surface of the condyle is partly vertical, with the pyriform outline of Plagiaulax, but more compressed; and in one of the American Marmots (No. 2259, Mus. R. Coll. of Surgeons) it still more closely resembles that of the fossil genus. I cite these instances, to show the undercurrent of Rodent analogy which pervades the jaw of Plagiaulax throughout. But a more conclusive and irresistible case of correspondence can be adduced in the condyle of the Aye-Aye. In the words of the celebrated French anatomist who first settled the affinities of the genus, “ La forme générale de la machoire inférieure de ’Aye-Aye dénote une partie forte, large, ou mieux haute et tres comprimée; la branche horizontale beaucoup plus longue que la verticale, qui est presque dans la méme direction. Le condyle qui termine cette branche verticale, dans les autres animaux, est droite ici, et presque a l’extrémité postérieure de toute la machoire,” &c.* The condyle of the Aye-Aye has the same ovate form as that of "Plag i- aula, but reversed, the narrow end being uppermost (fig.20); thearti- cular surface is broader and somewhat flatter than in that genus, but the direction of the greater axis is the same, that is, longitudinal and * De Blainville, ‘Ostéographie: mémoire sur l’Aye-Aye,’ p. 19. 1862. | FALCONER—PLAGIAULAX. 361 subyertical*. The glenoid surface of the upper jaw is modified in correspondence—being broad and flat, and placed on an inclined plane that would intersect the tips of the nasals and the middle of the occipital foramen. Here, then, is a signal failure in the chain of physiological deductions requisite to prove that Plagiaulaw was a marsupial carnivore. Next, as regards the depressed position of the condyle—below the level of the grinding-teeth. The author of ‘ Paleontology’ states that it is a “‘character unknown among any herbivorous or mixed- feeding animal.” I again refer my reader to the figure (fig. 20) of the lower jaw of the Aye-Aye. In it, the articular surface of the condyle, although directed subvertically, or at the most diagonally, is wholly below the grinding-plane of the molars. It looks still more depressed in Plagiaulax Becklesiz; but this is, in part, owing to the inflected margin of the angle being broken off in the fossil, while it is entire and salient in the recent form, thus elevating the condyle above the lower plane of the ramus, and leading to an appearance of a greater amount of difference than exists in nature 7. For my reasoning as regards the signification of the long neck or pedicle of the condyle, I refer the reader to my former communication (op. cit. pp. 269 and 275). It is there stated that the low position of the condyle ‘‘is counterbalanced by another character, of which, so far as | am aware, there is no example among any of the predaceous genera, either placental or marsupial, recent or fossil, namely, the long neck and horizontal projection of the condyle behind the coronoid,” &c. ; and further on I added that the “ arrangement is equally without a parallel among the herbivorous or omnivorous tribes.” This latter remark was premature. I was then acquainted with the Aye-Aye only through the figures given by Blainville +, in which the lower jaw is shown in opposition with the skull, thus concealing the coro- noid, and its relation to the condyle. But if the accompanying figure (fig. 20) of the lower jaw detached be referred to, it will be seen that the condyle is not only below the level of the grinding-plane, but that it is projected a long way behind the posterior edge of the coro- noid, exactly as in Plagiavilax, and on the same plan of construction, —the sole difference being that the sigmoid notch is shallow in the Aye-Aye, and deeply excavated in Plagiaulaw. If the notch were deepened in the former, by removing the plate of bone behind and below the posterior edge of the coronoid, in the manner indicated by the dotted line (f), the resemblance would be complete. In order to place these facts of agreement beyond question, I give the following * “Tia machoire inférieure, comme celle des autres rongeurs, se meut évidem- ment au moyen d’un condyle longitudinal, de maniére 4 empécher tout mouve- ment horizontal, si ce n’est de l’arriére a l’avant et vice versd.” (Sandwith, Zoo- logical Proceedings, 1859, p. 113.) + In some of the families of the Rodentia the condyle is barely elevated above the grinding-plane of the molars. See Blainville ‘Ostéographie: genus Cavia,’ pl. 2. Figs. Cawia Cobaya and C. Capybara; genus Hystrix, pl. 2, and Sciurus maximus, pl. 1, while in others, e. g. Castor, both condyle and coronoid are well raised above the same plane. { Ostéographie: genus Lemur, pl. 5. 362 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, measurements of the relative proportions of the lower jaw in the Aye-Aye and P. Becklesn * :— Cheiromys Plagq. Madagasc. Becklesiz. ; inch. inch. Length of jaw from condyle to incisive border............ 2-3 2:0 From condyle to posterior edge of coronoid..............- 6 5 Height of jaw to summit of coronoid ..............-...++: 1:2 10 Height of ramus in front of first true molar............... "i ‘6 Height of ramus behind the incisor ..................240+- ‘65 45 Height from condyle to a line dropped verticaliy behind LetSteMOPar ys, tose weteec ee estat etka he acs fo bomen? 1-25 1:05 Height from the latter point to posterior edge of incisor atidiactemiens. 2.07 2 oe oan ee eae eee heh re) “79 From these proportions it will be seen that both in Chevromys and Plagiaulaxe the condyle projects behind the edge of the coronoid to the excessive extent of about one-fourth of the entire length of the ramus. Professor Owen meets the argument in my paper, by the assertion that the condyle of Plagiaulawx is ‘ pedunculate as in the predaceous marsupials.” If so, I invite him to adduce the instance, bearing in mind that the question here is one of degree. The lower jaw of a Tiger now before me measures 9-2 inches from the condyle to the incisive border, while the projection of the articular surface behind the fall of the coronoid does not exceed 7 of an inch, or one- thirteenth of the length of the jaw. In Dasyurus and Thylacinus + the condyle projects behind the coronoid, but nothing approaching the extent seen in the Aye-Aye and Plagiaulaw. As regards the functional effect of the condyle being carried so far back behind the edge of the coronoid, it is a plain question of animal mechanics, which the author of the ‘ Paleontology’ thus interprets: “Jt 1s pedunculate, as in the predaceous Marsupiaha, whilst the lever of the coronoid process is made stronger by the condyle being carried further back than in any known carnivorous or herbivorous animal.” As I regard it, a necessary effect would be to restrict the power of separating the jaws in front, essential to a predaceous animal having laniary teeth constructed to pierce, retain, and kill. And we have the direct proof in the Aye-Aye, that the same arrangement there is not applied to a carnivorous function #. * It must be borne in mind that fig. 1 of my previous communication (op. cit. p- 278), from which the measurements of P. Becklesti are taken, is magni= fied two diameters; the dimensions are therefore doubled. But this does not interfere with the ratios of proportion. Further, in the Aye-Aye the posterior margin of the coronoid is assumed to be continued down vertically, in order to get corresponding measurements. The dimensions of Cheiromys are of the natural size. Tt In the Ursine Dasyurus (No. 1900, Mus. R. Coll. of Surgeons) the length of the lower jaw is 4:2 inches, and the projection of the articular surface behind the deepest part of the sigmoid notch ‘4 inch., or about one-tenth of the entire length of the jaw. In Thylacinus (No. 1903 4 of the same collection) the pro- jection of the condyle is about one-eighth the length of the jaw. But in both these forms the posterior edge of the apex of the coronoid overhangs the condyle ; while both in P/. Becklesti and the Aye-Aye the articular surface of the condyle is removed about one-fourth of the length of the jaw behind the fall of the coronoid. + In the typical Carnivora the fulerum is a fixed point, the form of the glenoid 1862. ] FALCONER—PLAGIAULAX. 363 With reference to the angular process, I have nothing to add to what is set forth in my former communication. This process, which is a very constant character of the carnivorous jaw, is wanting as a salient apophysis in Plagiaulax, although well developed in the minute insectivorous Myrmecobius. I have one remark more to make in reference to the form of Pla- giaulax. Fig. 15 of my original description gives a representation of what remains of the lower jaw of P. minor, magnified. to a scale of four diameters. The entire length of the specimen, including the six molars and premolars, together with the procumbent incisor (according to the metrical line ¢), does not exceed °4 of an inch, of which the six cheek-teeth united make only about two and a half lines (-25 inch). I ask any zoologist or comparative anatomist to look at it, and say whether the dental apparatus of this extremely minute creature is competent to perform the duties required of a pre- daceous carnivore. Magnitude in this case is an important ingredient, as it necessarily involves measure of force. Could P. minor have preyed on small Mammals and Lizards? Is it not more probable that this pigmy form was itself an object of prey in the Purbeck Fauna? In the preceding observations I have gone seriatim into the ob- jections raised against the view which I advanced of the affinities of Plagiaulax. In the work referred to, every detail of external form was regarded in a light different from that in which it was viewed by me; every inference was controverted ; and the conclusion drawn from the whole was diametrically the converse arrived at by me. The verdict of Comparative Anatomists will decide which is right. I have reconsidered my first inferences, and tried to test their validity by the strongly contrasted and extreme view put forward by Professor Owen ; and the result has been to confirm the opinion that Plagiaulax did not belong to a carnivorous type of Marsupials. Re- garded morphologically, in the plan of its dental system,—rationally, through its condyle and correlated characters,—and empirically, by comparison with Hypsiprymnus and Cheiromys, it has led me, through every aspect, to this conclusion. Enough has been adduced in the fore- going pages to show that, to whatever family comparative anatomy may ultimately consign the genus, it must always be held to be a singularly modified form. I have directed attention to the numerous points of analogy between the lower jaw of Plagiaulax and that of the Aye-Aye, itself one of the rarest and most aberrant of existing cavity preventing protrusion or retraction of the lower jaw; and the muscular power being applied close to the condyle leaves the free part of the lever longer, or, in other words, admits of a wider separation of the jaws in front, for the canines and cutting-teeth to act. In the Aye-Aye and Rodents (e. g. Cavia and Hystriz) the fulcrum is moveable, the condyle playing on a flat glenoid surface ; the point of insertion of the muscular power is more advanced, leaving a short portion of the lever free, and thus restricting the aperture of the jaws. These conditions, combined with the oblique direction of the temporal muscle, implied by the reclining coronoid, conspire to produce the antero-posterior and lateral — motions required by the regimen of these forms. The same reasoning applies to Plagiaulax. 364 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, Mammala. They agree in the collateral position and upward direc- tion of their strong incisors; in the depth and shortness of the hori- zontal ramus; in the backward continuation of the ascending ramus in the same horizontal line with the body of the jaw, and in the ter- minal position of the condyle,—the two latter characters not being found, so far as is at present known, in any other Mammalia, fossil or recent. They agree further in the form and direction of the articular surface, in the reclinate coronoid, and in the backward projection of the condyle behind it. The two jaws are on the same plan of construction. Starting from the deep narrow incisors of the Aye-Aye, carried back below the molars, the great depth of its jaw, and the other associated characters, can be seen to be in necessary correlation. In Plagiaulax they are all presented in a less degree of development. The resemblance goes no further. I doubt if in the fossil genus the lower incisors were opposed in the upper jaw by only two chisel-shaped teeth as in the Aye-Aye. In all the other dental characters they are widely distinct. In Plagiaulax the force of the dental system is manifested in the great development of the premolars, of which there are none, at least in the adult state, in Cheiromys, but a vacant bar instead. In the latter there are three molars, in the former only two. While, therefore, admitting that the common construction of the jaw involves some trait of habit common to the two and essential to their existence, it does not im- press me with the idea of affinity. For the reasons which have led me to regard the nearest relationship of the fossil genus as being in the direction of Hypsiprymnus, I refer to my former communication assem, and to the preceding pages. Both genera appear to be Mar- supial: their incisors are on the same morphological plan, and their premolars are in the main identical, except in point of number. The Aye-Aye is a nocturnal animal, which uses its strong incisors as a nipping-apparatus, for breaking and detaching bark and wood in pursuit of the larve upon which, in part, it is said to feed. One of the live specimens procured by Sonnerat, on the first discovery of this form, lived in captivity two months fed on boiled rice *. The species of Hypsiprymnus are strictly vegetable-feeders. I shall adduce a celebrated case to show how little we should be authorized to pronounce with confidence on the nearest affinities of Plagiaulax from the small measure of evidence we now possess. The Aye-Aye (Chewromys Madagascariensis) was discovered by Sonnerat before 1782. The elder Geoffroy and Cuvier placed it among the Rodents. In 1816, Blainyille submitted the skull and teeth, together with the bones of the fore-arm, to a rigorous examination, and convincingly pronounced the Aye-Aye to be a Lemurine Quadrumane. * «Tl avécu prés de deux mois, n’ayant pour toute nourriture que du riz cuit ; il se servait, pour le manger, de ses deux doigts comme Jes Chinois, de baguettes.” (Sonnerat, quoted in Buffon, Supplement, tom. vii. p. 268.) The early account of the French traveller has been confirmed by the later and excellent observations of Dr. Sandwith, who fed his captive Aye-Aye upon bananas and dates, the latter of which he took to with great relish, gnawing the larve of insects out of the branches of trees, and feeding on them when he had the opportunity. (Sandwith, Zoological Proceedings, 1859, p. 113.) 1862. | FALCONER—PLAGIAULAX. 365 Notwithstanding the evidence supplied by the brain-case, teeth, and bones of the fore-arm, Cuvier persisted in regarding the animal to be a Rodent, and in the ‘Régne Animal,’ of 1829*, he places it between the Squirrels and Marmots. If, with such a full measure of evidence before him, the position of Chevromys in the natural system was so long erroneously contested by Cuvier, how little warranted should we be to pronounce dogmatically upon the food and habits of Plagiaulax from the slender evidence of the lower jaw! Supposing that Chetromys were only known to us through its mandible, what would now be its inferred position among the Mammalia? While, therefore, regarding Plagiaulax to have been of a phytophagous type in its affinities, we should not be justified in affirming that it may not have been a mixed-feeder; it may have fed on buds or fruits, like the Phalangers; or on roots like Hypsiprymnus; or on a mixed regimen of fruits and insects, like the Aye-Aye. But I maintain that every argument which has been adduced by the author of ‘ Palzontology’ to prove that Plaqiaulax was car- nivorous has been met in the preceding pages. The methods by which the opposite conclusions have been arrived at are as different as the results themselves. Professor Owen, in so far as his method is disclosed to us, has gone direct from the indications of form to the supposed function ; and he claims for the inferences, that they are physiological deductions. Comparative anatomists will decide how far they are entitled to the name. Mere external form must be handled with caution as an instrument of research; signal mistakes in Paleontology have been committed through too confident reliance upon it. On the other hand, the method which I have attempted to pursue was, first to ascertain upon what morphological plan the teeth of Plagiaulaw were constructed, and, having determined this, to supply the rest empirically by comparison with known forms, using at the same time rational analysis where it could be applied, e.g. to the condyle. The case is of sufficient interest and importance to test the sufficiency of the respective modes of analysis. In the general remarks appended to my former communication, I called attention to the contradictory bearing of the dental system of Plagiaulax upon the assumption that the earliest Mammals had the full complement of teeth. To that fact may now be added the fur- ther evidence of specialization, in the analogy of its mandible with that of the Aye-Aye, one of the most exceptional of Mammals. If we cast a glance over the instructive table given in Lyell’s ‘ Supple- ment’ (page 23), and reflect on the interpretation of the hiatus between the Upper Oolitic beds and the ‘Sables de Bracheux,’ how vast the interval in time by which they are separated, and how modern in comparison the earliest of Tertiary Mammals! If, on the other hand, Plagiaulax be regarded through the medium of the view advocated with such power by Darwin, through what a number of intermediate forms must not the genus have passed before it at- tained the specialized condition in which the fossils come before us! What a variety of Mammals may we not hope to disentomb from * Op. cit. p. 195. 366 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, Figs. 1-6.—Plagiaulax Becklesii (figs. 1-5), and Hypsiprymnus Gaimardi (fig. 6). Figs. 1 & 4 show the entire Right Ramus of the Lower Jaw of Plagi- aulax Becklesii, in two pveces, on reversed slabs of the same piece of matri#. (Magnified two diameters.) [Figs. 1 & 4 represent the same right ramus of the lower jaw seen on the opposite surfaces of a split stone, the two taken together affording data for a complete restoration of the jaw. | Fig. 1. a 6 e’. Outer side of the anterior portion of the right ramus of lower jaw; magnified two diameters. a 0, outer side. 00’ de’, im- pression of inner side. a. Incisor. 6c. Line of vertical fracture behind the premolars. d’. Impression in the matrix of the condyle. e’. Impression of top of coronoid process. . o’. Broken-off inflected fold of inner margin buried in the matrix. m. Place of the two molars. pm. Three premolars, the third or last divided by a crack. Fig. 2. f. Section of the anterior piece of the jaw at the fracture bc; «x, in- ner surface; y, outer. The notch at the top is formed by one of the sockets of the double-fanged true molar. Fig. 3. g. Section of the hinder piece near bc; «, inner surface; y, outer surface. Fig. 4. a’ d. Inner side of the posterior portion of the same lower jaw on the opposite slab of stone; dde, inner side; bah, cast and im- pression of outer side. a’. Outline of the incisor restored. bc. Line of vertical fracture. d. Condyle. e. Coronoid process. h. Impression of the three premolars on the matrix. i. Empty sockets of the two true molars. n. Orifice of dentary canal. o. Indication of the raised and inflected fold of the posterior inner margin. Fig. 5. &. Third or largest premolar, showing the seven diagonal grooves ; magnified 53 diameters. Fig. 6. 7. Corresponding premolar in the recent Australian Hypsiprymnus Gaimardi, showing the seven vertical grooves; magnified 33 diameters. 1862. | FALCONER—PLAGIAULAX. 367 Figs. 11, 12, & 13.—Plagiaulax Becklesii. Fragment consisting of the anterior portion of the Right Ramus of the Lower Jaw. Magnified 2 diameters. Fig. 11. Outer surface. Fig. 12. Inner surface. Fig. 13. Vertical view, seen from above. om a 9 - oS ae Leer a. Incisor. pm. Premolars. b. Symphysial harmonia. c. Mentary foramen. Fig. 15.—-Plagiaulax minor. Outside of the Right Ramus of the Lower Jaw; and the two Molars. Magnified. ——_-——4 @ Lee [All the teeth in this specimen are in place and well preserved. The hinder part of the jaw-bone, with the ascending ramus and posterior angle, are: broken away. 7 6. Right ramus of lower jaw, with all the teeth; magnified 4 diameters. a. Incisor with point broken off. a’, impression of same, showing that the inner side near the apex was hollowed out in a longitudinal direction. b. Offset of coronoid, the rest of which is wanting. m, m. The two true molars. pm. The four premolars. ce. The first molar; magnified 8 diameters. Upper figure, the crown. Lower figure, side-view. . d. Second molar; the crown and side-view. e. The length of the jaw, natural size. 368 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, Figs. 16-19.—Posterior half of a Carnassial Tooth (pm 4) from the left side of the Lower Jaw of Thylacoleo Carnifex. (Preserved in the Museum of the Royal College of Surgeons.) 17. Phan ina “see en ~ Fig. 16. Inner side. a, hinder end, showing the undulations of the enamel- surface on the base of the crown, and the rugosely reticulate surface below the summit. For comparison with figs. 5 & 6 (page 366); the same teeth in Plagiaulax and Hypsiprymnus. Fig. 17. Outer side. a, hinder end. Fig. 18. Top aspect, showing the undulations. a, hinder end. Fig. 19. Section, showing the broken edge of the middle of the crown. Fig. 20.—The Right Ramus of the Lower Jaw of the Aye-Aye (Cheiromys Madagascariensis); the outer aspect. Nat. size. a a. Incisor. e. Angle of Jaw. : b. Molar teeth. _ f. Conjectural dotted line. ce. Coronoid process. g. End-view of condyle. d. Condyle, having its articular surface below the grinding- plane of the Molars. 1862. | HEER—HEMPSTEAD PLANTS. 369 the buried Oolitic fauna, should Mr. Beckles resume his explorations, or another Beckles take his place ! The remote antiquity of the fossil as a mammalian genus must alone invest the discussion of its affinities with an interest which will prevent the question from resting in its present disputed state. Other paleontologists will examine the evidence, and give their verdict. Mr. Beckles’s specimens have long since passed out of my hands; and I have deferred my rejoinder in the expec- tation that they might ere now have found their way into some public collection, where I could have again submitted them to ex- amination and comparison ; but, as that has not yet taken place, I have thought it full time to reply, lest my silence should be construed into a tacit acquiescence in the carnivorous character attributed to Plagiaulax, which I do not accept—nor the reasoning on which it is founded. 2. On Certain Fossiz Piants from the Hempstead Beps of the Ist or Wieut. By the Rev. O. Heer, Ph.&M.D. With an IntrRo- puction, by W. Prnertty, Esq., F.G.S. (Communicated by W. PrencE.uy, Esq., F.G.S.) [Puate XVIII.) INTRODUCTION. GEOLOGIsTs are perhaps aware that not long since a systematic and careful exploration was made of the deposit of lignite, clay, and sand at Bovey Tracey in Devonshire, in the hope of determining its age; that a large number of fossil plants, of various kinds, were found, and all submitted to the Rev. Dr. O. Heer, Professor of Botany at Zurich; and that two papers, embodying the results of the inves- tigation, were recently presented to the Royal Society. From Professor Heer’s determinations, it appears that forty-nine species of fossil plants occur in the Bovey beds, of which twenty-nine are new to science, whilst the remaining twenty are well-known Miocene forms of Continental Europe; that, following the subdivi- sion of the Miocene beds adopted by some geologists on the Continent, sixteen of the twenty species occur in the Tongrian or lowest stage, nineteen in the Aquitanian, twelve in the Mayencian, five in the Helvetian, and eight in the Oeningian; that those common to the Aquitanian and any other stage are found, in almost every instance, in a greater number of localities in the former than in the latter, and in only one case (that of Vaccinium acheronticum, Ung.) in fewer ; and that the only one of the twenty species (Celastrus pseudoilea,, Ett.) not found in the Aquitanian stage occurs in the Tongrian be- low and the Mayencian above, but only in a single locality in each, and may therefore be looked for, sooner or later, in the Aquitanian also. Accordingly the Bovey deposit is considered to belong to this stage of the Lower Miocene. 370 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, This decision receives confirmation in the fact that the new species found at Bovey are closely allied to well-known Continental forms on this horizon. The most remarkable Bovey plant is Sequota Couttsie, Heer, a new species of fossil Conifer. Since its discovery at Bovey, Professor Heer has ascertained that it occurs also at Armissan, near Narbonne, in France. The work at Bovey was performed, under the superintendence of the author, by Mr. H. Keeping, of Freshwater in the Isle of Wight, well known as an efficient and reliable fossil-collector. It is probably unnecessary to add that he takes a lively interest in the problems which it is hoped his labours may help to solve, and readily under- stands the nature of the evidence required. In recognition of this, I wrote to him as soon as the chronology of the Bovey beds was settled, informing him that they were Lower Miocene, and probably on or very near the horizon of the Hempstead series, with which I knew him to be well acquainted. It may not be out of place to remark here, that I had come to this last conclusion on the principle that things which are contemporary with the same are contemporary with one another, and not from the fact that Bovey and Hempstead possessed any fossils i in common. In acknowledging my letter, Mr. Keeping stated that he had recently found Bovey fossils, especially Sequoia Couttsie, in the Hempstead beds. I immediately wrote, requesting him to devote some time, as soon as possible, to these beds on my account; to send me all the fossils he could find; to be very particular respecting their situations in the deposit; and directing him to “take his de- parture”’ from the Black and White Bands of Professor EK. Forbes*. In a few weeks he sent me a good series of fossil plants—seeds, cones, leaves, and twigs; amongst them certainly Sequora Couttsic and Folliculites Kaltennordheimensis. Being fully aware, however, that my opinion on such a point must necessarily be valueless, and believing the discovery, if fully established, to be one of considerable interest, I dispatched by far the greater number of the specimens to Professor Heer, requesting him to prepare a short paper on the fossils, if he thought the subject of sufficient importance, which I might present to this Society. Whilst waiting his reply, Mr. Keeping sent me, from the same beds, two fine portions of undoubted Palm-leaves, one of which I had no doubt was Sabal major, Ung.; the other, not so perfect, ap- peared to be also a decided Sabal, but less identifiable specifically. These were also forwarded to Professor Heer, from whom I have just received the accompanying paper, which I beg to present to the Society in his name, in the hope that some geologist may be induced to take up the subject and thoroughly examine it. ‘“‘ How im- portant,” says Professor Heer, ‘it would be to examine this (the Hempstead) flora as carefully as possible, and likewise that of the Bembridge series, and the pipe-clay of Alum Bay, where I collected last autumn a number of beautiful leaves! These floras would give * Tertiary Fluvio-marine Formation of the Isle of Wight, pp. 48, 44. 1862.] HEER—HEMPSTEAD PLANTS, 371 us important conclusions about the relation of the Miocene to the Kocene flora, and clearly show us the changes which have taken place in this land; for the forests particularly give the physiognomy of the country.”—W. P Fosstz Prants From Hempstead, Istz or WIGHT. Tue plants sent to me by Mr. Pengelly, from the Hempstead Series of the Isle of Wight, are of great interest, because the geological position of the deposit was exactly determined by the late Prof. KE. Forbes, and it is very important to know in what degree the flora of this division of the Tertiary formation is referable to that of the pipe-clay of Alum Bay and that of the lignite of Bovey Tracey. ~- The number of species is indeed very small, undoubtedly too small for an exact settlement of this question. However, they give us some important points of comparison. The plants sent to me belong to ten species. our of these (Sequoia Coutisiw, Andromeda reticulata, Nymphea Doris, and Carpolithes Websteri) have also been found at Bovey Tracey ; all these, except the Nymphea, are species which appear also in the Lower Miocene of the Continent. Melwmbium Buchii is known from Mount Promina, from the Paudeze, and Giinz- burg, localities belonging to the Lower Miocene, and is also accom- panied by Chara Eschert. We know, therefore, six species of the Lower Miocene (Tongrian and Aquitanian). Prof. E. Forbes says (in his ‘ Tertiary Fluvio-marine Formation of the Isle of Wight,’ p. 47), when speaking of Folliculites thalictroides Br., var., “ This form appears to be the same as that found in the Bem-= bridge and Headon series :”’ he certainly means the £. thalictroides, var. Websteri, Br.; but this, on account of its obtusely rounded end, must be separated as a species from FP’, thalictroides, and is identical with the Folliculites Kaltennordhemensis. If this species, indeed, appeared in the Bembridge beds, and not the F. thalictrordes, Br., Hempstead would have one species in common with the Bembridge series, Prof. Forbes mentions, besides, three species of Chara; but at present we cannot lay much stress upon these, as I shall show in my notice of Chara, because we must submit them to a new and careful examination. | Hempstead has no species in common with the pipe-clay of Alum Bay. As far as the deficient materials enable us to judge, the fossil flora of Hempstead has more reference to that of Bovey Tracey, and thereby to the Lower Miocene flora, than to the Eocene flora of the Bembridge series and Alum Bay, A further observation which these plants suggest concerns the local conditions which they announce. We perceive amongst them a Nelumbium and a Water-lily (Nymphea) ; also two species of Chara , which likewise lived in the water; and a plant nearly related to Cyperus, which undoubtedly grew on the bank, where an Andromeda had its place too. The s&eds of Nymphea Doris ave very numerous; and from the Nelumbium Buchit we have not only portions of leaves, but also numerous rhizomes with the fibres; we may therefore almost with certainty affirm that this plant really lived there, VOL, XYIII,—PARI I, 2¢ 3872 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, The Nelumbium and the Water-lily demand the presence of fresh water and exclude any idea of salt water; therefore one can easily explain the appearance of Paludina, Cyclas, Unio, and Planorbis at this place. Accordingly we admit the existence of a freshwater lake there, the Water-lilies and Lotos spreading their leaves over its waters, and the Sequoias, the Palms, and the Andromedas surround- ing its banks. The lake could not have been far from the sea, nor much above ity because these freshwater formations alternate with those of brackish water,—a circumstance which shows that the sea broke in at times, | and changed the fresh water into brackish, and finally into salt water ; so that the plants confirm the conclusions formed by Prof. Forbes from the animals. The exact sections in Forbes’s memoir give us very interesting indications of these events; and perhaps it may be possible, by a careful study of the plants these beds contain, to arrive at conclu- sions not only respecting the change of the freshwater and brackish formations, but also as to the seasons in which they took place. The “ Black Band” forms the basal stratum of the Hempstead series; and the next succeeding stratum shows us that already, in the beginning of the formation, a lake of fresh water existed there ; for it is particularly in this portion of the deposit that rhizomes and leaves of Nelwmbiwm are found, and with them the freshwater shells. An influx of salt water seems to have taken place before the forma- tion of the ‘‘ White Band,” as here there occur some brackish-water shells. During the formation of the “middle freshwater marl” of Forbes (op. cit. p. 42), the freshwater conditions were predominant, and the Water-lilies appear represented by a quantity of seeds, with Unio and Paludina. The “upper freshwater and estuary marls”’of Forbes are nearly always a freshwater formation; and we only get a true marine stratum in the “upper Corbula-bed.” It seems, therefore, that from the beginning to the end of the Hempstead Series there was a lake which received fresh Water from a river, but that from time to time it was supplied with salt water, which at last became predominant, by which the freshwater prs was nur planted by an exclusively marine one. To these general remarks I add the followin observations on the species. 1. Szqvora Courtsrm, Heer. Pl. XVIII. figs. 1-7. Heer, Fossil Flora of Bovey Tracey, Phil. Trans., pls. 8, 9, 10. Most of the specimens are from a bed 7 feet above the “ Black Band” of Forbes; but one specimen was found about 2 feet 6 inches from the top of the “second division” of Forbes (op. cit. p. 41). This species wholly agrees with that of Bovey Tracey. It has thin twigs (figs. 2, 4) which are covered with imbricated leaves. The leaves are alternate, acuminate, and mostly have a somewhat curved point; they are either pressed against the twigs (fig. 2), or spread in the upper part (fig. 4), like the Bovey plant. The cones are also of equal size, and formed by peltate, many-edged scales 1862.] HEER—-HEMPSTEAD PLANTS. 3873 (figs. 1, 26,3). The seeds (figs. 5, 6, 7) have flat wings and a curved nucleus, like that of the Bovey plant; and in this they differ from the seeds of Sequoia sempervirens. Prof. E. Forbes mentions from Hempstead ‘(Tert. Form. Isle of Wight, p. 47) Tasites (or Glyptostrobites) Puarisiensis, .Brongn. (Muscites syuamatus, Brongn. Végét. Foss. pl. 10. figs. 5, 7); he has certainly taken the plant in question for it. It appears, indeed, to be a species much resembling it. Brongniart says of his Muscites squamatus, < foliis rhomboideis obtusis ;” whilst our species has, on: the contrary, acuminate leaves. Our species appears, however, in France, viz. at Armissan near Narbonne, whence I have received some twigs. : _ 2. Cyprrires Forpest, sp.nov. Pl. XVIII. figs. 20, 21. The fruits are 2 millims. long and 14 millim. broad, oval, and fur- nished with a fine point. They occur ‘in great numbers together in the upper three feet of the “third division’ of Forbes. They are small black fruit, which are broadest in the middle, and equally, obtusely rounded at both ends, but provided with a small point at the top, which is the ead of the style. The side is flat, without an edge; therefore they were not triangular. Some- times there are two lines (fig. 21 g) above the middle, because it sprang up there; the edge is often split (fig. 21¢,f). The fruit agrees In size aad form with that of Cyperus Monti, L.; and it probably belongs to the genus Cyperus. The fruits of Scorpus are always tapered at the base and thickest above.the middle; those of Carew are beaded, whilst those of Cyperus are shaped like the fruits represented of the natural size in fig. 20, and magnified in fig. 21. They belong perhaps to Cyperus reticulatus (Heer, Flora Ter- tiaria Helvetiz, vol. i. p. 80; vol. iii. p. 165), whose ears resemble that of Cyperus Monti, L. ; but we have not found the fruits of this species. _ 3, Sapat mason, Ung., sp. (?) Only a portion of a leaf of the middle of the fan; it cannot be determined with certainty. The rays are 10-12 millims. in breadth, with a projecting edge in the middle; they have numerous longitu- dinal veins, and between every two there are four finer ones. Found seven feet above the “ Black Band.” 4, ANDROMEDA RETICULATA, Ett. Pl. XVIII. figs. 12, 18. Ettingshausen, Tertiire Flora von Hiring, p. 65; Heer, Fossil Flora of Boyey Tracey, Phil. Trans., pl. 17. figs. 10, 11. - From a bed seven feet above the “ Black Band.” These are coriaceous leaves, provided with a petiole, and gradu- ally tapering towards the base. They are distinguished by their reticulated venation (fig. 126). Like the leaves of this species from Bovey, the secondary veins project very little from the fine reticula- tion which covers the surface of the leaf. It is very like Andromeda protogea, Ung., but has a shorter petiole and a finer reticulation, 202 o74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, and is more tapered at the base; but it is still doubtful if these dif- ferences suffice toseparate them. The leaves figured by Ettingshau- sen in his ‘ Flora von Hiring,’ pl. 22, figs. 1-8, under the name of Andromeda protogea, belong, I think, to A. reticulata, ©. Nympoma Doris, Heer. Pl. XVIII. figs. 8-11. Heer, Fossil Flora of Bovey Tracey, Phil. Trans., pl, 19. figs. 32-37, The seeds appear in great numbers in the upper three feet of the ‘third division” of Forbes. These are probably the seeds which he mentions as Carpolithes ovulum, var. They are brilliantly black, short oval, at both ends obtusely rounded, 23—4 millims. long, and 2-34 millims. broad, agreeing in form and sculpture with those of Nympheea. In many of the speci- mens the fine stripes are to be seen with the aid of a lens, whilst in others they are rubbed out; they agree so well, however, in all other points’ with the rest that they cannot be ‘separated. It is undoubtedly the same species as that of Bovey; it differs from’ Nymphea Charpentieri (Heer, Flor. Tert. Helvet. pl. 155, fig. 20 6, c,d) and N. Arethuse, Br. (Carpolithes ovulum, Br.) by the somewhat broader and shorter seeds. The MW ymphea dololum*, Ludwig, is the N. Charpentiert, Heer. : 6. Netumsrum Bucur, Ett. , -Pl. XVIII. fig. 19. Bein gshausen, Flora des Monte Promina, p, 36, pl. 11, fig. 1; pl. 12 _ Heer, Flora Tertiaria Helvet. p. 31, pl. 107, figs, 2-5. Rhizomes and portions of leaves abundant, ’ ‘seven feet above the “‘ Black Band;” one rhizome in the eee three feet of the ‘third division,” Several large portions of leaves have ea found, but no entire leaves. They show us that the leaf was peltate, like that of Nelum- bum. Fig. 19. Pl. XVIII. represents a portion of a young leaf where the petiole was attached; its venation is very indistinct; one sees, however, that one of the principal veins was stronger than the others, which distinguishes Nelumbium Buchii from other species. Other portions belong to large, full-grown leaves, with well-preserved veins, but do not show either the edge or*the middle. The prin- cipal veins are forked, the forks forming’ acute ‘angles; they are forked again a little higher (Pl. XVIII. fig. 196, where asmall por- tion of a leaf is represented). Delicate veins unite the principal ones; and the areas they include are filled up with a fine reticula- tion. There is no doubt that the ee represented i in Pl. XVIII. fies. 19 ¢, d, e belong to: Nelumbium. - The rhizomes of this genus partly form knots, which are provided with a bunch of long fibres. They show, therefore, quite another structure than the rhizomes of Nymphea. ‘These rhizomes. occur in the same bed with the leaves of Nelumbiwm Buchii, and therefore confirm the explanation given * I received the sceds from M. Tasche of Salzhausen, 1862.] ee HEER—HEMPSTEAD PLANTS. 310 of them. The rhizomes are from 10 to 14 millims. thick, and at the knots 23 to 24 millims.; they represent brilliant brown or brownish black bands. ‘The large, thickened knots are provided with long and thin fibres, which bear finer fibrils. The fibres have fallen away in places, and scars appear, which are numerous and densely crowded. Fig. 19 d represents the lower end of the rhizome; fig. 19, a knot in the middle of it. These beautifully preserved rhizomes enable us to explain some enigmatical porticns which were formerly sent to me from Rochette and Ginzburg. In my ‘Flora Tertiaria’ I have represented in pl. xxi. fig. 13 a some fibres ranged in a circle, which at all events belong to Nelumbium. Rhizomes have been found at Ginzburg, which are as large as those of Hempstead. I took them formerly for Cyperites dubwus, A. Br. At Rochette and Ginzburg there appear with the roots, at the same place, the leaves of Nelwm- bium Buchii, which confirms their belonging to the same species. The Typha-like leaves mentioned by Prof, E. Forbes (op. cit, p. 44) are probably the rhizomes of our plant. 7. CarrotitaEs Wessterti, Brongniart. Carpolithes thalictroides, var., A. Brongn., Mémoires du Muséum, vol. vii. pl. 14. fig. 6. Folliculites = ee Zenker et Auct. Folliculites minutulus, J. D. Hooker, Quart. Journ. Geol, Soc., 1855, vol. xi. p. 567. Abundant at two feet below the “ White Band.” It wholly agrees with the specimens from Bovey, Kaltennordheim, the Wetterau, Rochette, and elsewhere. 8, CarpoLiTHEs GLoBuLvs, sp. nov. Pl. XVIII. figs. 14, 15, 16. Globose fruits (or seeds ?), 4 to 5 millim. in diameter, smooth somewhat depressed at both ends. . In the upper three feet of the “ third division ” of Forbes. They have a rather thick, coal-black rind, which easily peels o from the pyritized nucleus (fig. 166; magnified, fie Gi) a) aris we have golden-yellow grains, surrounded by a black rind. This gold-coloured nucleus has at one end asmall round aperture, or circular place (fig. 14); the other end has an impression (fig. 15), It is perhaps the fruit of a Palm. . Var. b. Natural size, figs. 17, 18; magnified, figs. 17 6, 18 6. Besides these globose, smooth fruits, there are at Hempstead, at the same place, short oval fruits (or seeds ?), which are densely and finely dotted. They are 6 millims. long, and 5 millims. broad. They have also a golden-yellow nucleus of pyrites, and a rather thick black rind, These fruits belong perhaps to another plant. 9, Cuara Escuent, A. Brongn. _ Heer, Flora Tert. Helvet. vol. i. p. 25, pl. iv. fig. 5. From the upper three feet of the “third division” of Prof. E. Forbes. I cannot distinguish these from the species which I described and 376 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4, figured in my ‘ Flora Tert. Helvet.’ They are very small, oval fruits, with 9 to 10 whorls ; these are partly flat, partly concave, where the spirals project more sharply. The coronula is formed by five very small warts or points. This differs totally from Chara medicaginula, Brongn., by its oval (not globose) fruits, and by the greater number of yhosla: ) Chara Eschert is abundant in our Lower and Upper Miocene, from the Aquitanian to the Oeningian stages, 10. Cara TUBERCULATA, Lyell, var. (?), It appears to be different from the real Ch. hideout Lyell (Manual of Elementary Geology, p. 210, fig. 189; and Salter, in Forbes’s Tert. Form. Isle of Wight, pl. 7. figs. 11, 12). The pieces I received (there were but a few, and not well preserved) are somewhat smaller, and have but eight or nine whorls; and they have also larger and fewer tubercles than the fruits of Ch, tuberculata. They may form another species, as these differences are also to be seen in Salter’s figures of Ch. tuberculata, var., from Hempstead (op. cit. pl. 7. fig. 13). Original specimens of Ch. tuberculata from Bem- bridge are wanting. Iam unable to decide this question with cer- tainty. We must have well-preserved fruits from the Hempstead and Bembridge series, _ Prof. Forbes mentions Chara helicteres, Brongn., and Ch. medica- ginula, Brongn. ; but Salter (op. cit., p. 159) seems to doubt the appearance of these species at Hempstead, and says that no specimen from this locality has been found in the collection. In pl. 7. figs.3—-5, ‘he only repeated the figures of Brongniart ; therefore we are not yet quite sure whether these two species appeared at Hempstead. Ac- cordingly we are obliged to omit these species of Chara in the com- parison of this locality. Postscrret.—I have just received several specimens of the Palm of Hempstead from Mr. Pengelly. They undoubtedly belong to Sabal major. Two of the specimens have still the end of the petiole and the base of the leaf. The rachis is 44 millims, broad at the base, very long, and gradually tapering (as the specimen figured in my ‘Flora Tertiaria,’ vol.i. pl. 36. fig. 2). The rays are attached on both sides; they wholly agree, in the insertion, form, and venation, with Sabal major, and indeed with the large form which Unger had called Flabellaria maxima (Chloris Protogzea, pl. 12). This species wholly differs from Flabellaria Lamanonis, Brongn., and therefore belongs to a Palm which extended over the whole of Europe in the Lower Miocene Period.—O. H. EXPLAN ATION OF PLATE XVIII, Illustrative of Plant-remains from the Hempstead Beds of the Isle of Wight. Fig. 1. Remains of Sequoia Couttsie. Fragments of cone. 2. ————. Fragments of twigs and of cone: 3. Sequoia Couttisie. Fragments of cone and twig. a Twig, . Wepre rts sea renee tnenere een O.Heer del. FOSSIL PLANTS FROM THE Quart. Journ. Geol Soo.Vol. XVILPLXVIL | Me Pte eee a > m, nae al < " ~ 4 > - Dates eee lave ete te re Str a pl eee Seay LR me SPOS ieee ee ree Aan ey re ener OO Kaye GATS eR ETES x Loxttny s eM ALES SRA EN ‘ WWest lth ° 4D BEDS OF THE ISLE OF WIGHT. | | | ng AT eS Quart. Journ. Geol Soo. Vol XVII. PLXVID. OHeer del, EAD BEDS OF THE ISLE OF WIGHT. FOSSIL PLANTS FROM THE HEMP¢ 4 ns te . H ¢' » . > 1862. ] .-- MORTON-—ICE-GROOVES. 377 Fig. 5, 6, 7. pei Couttsie. Seeds, 8, 9, 10, 11. Nymphea Doris. Seeds, natural size and magnified. 12a, 6, 13. “Andromeda reticulata. Leaves. 14, 15, 16a, 2, c. Carpolithes globulus, Natural size and magnified. 19a. Nelumbium Buchit. Young leaf. 19 4. —— ——. Portion of a large leaf. 19¢ ————. Rhizome, with knot and fibres. 19d. ————.._ Lower end of a rhizome 19 e. ————. ‘Transverse view of the fibres at a knot in the rhizome — 20, 21 a-g. Cyperites Forbes. 3. On @ractar ca See on the Signe eae LIVERPOOL. By G. H. Morton, Esq., F.G.S. Towarps the end of 1859, I gave an account to the Literary and Philosophical Society of Liverpool of certain indications of ice passing over and grooving the rocks in Toxteth Park. Since that time I have found the same appearances in two other places, and that a far greater interest is attached to the discovery than was at first anticipated ; it seems therefore desirable that the particulars should be made known through the Geological Society. Toxteth Park.—The first locality which was noticed is between Park Hill Road and the Dingle. It is near a quarry in the “‘ Pebble- beds ” of the *‘ Bunter” formation, where the strata dip 10° HK. The surface of the rock inclines 5° N.E. The direction of the striations is N.W. by N., or more correctly N. 42° W., allowing for variation. After the discovery, I employed a labourer to clear away some more of the “ Boulder-clay ” which originally covered the surface of the rock to the depth of about 9 feet, until at least 20 square yards were visible; and no doubt the appearances extend over a consider- able extent. The elevation is about 120 feet above the level of the sea. Boundary Lane, Kurkdale-—The second locality is in the brick- fields, about 50 yards north of Boundary Street, and 150 yards west of Gore Street, where 10 square yards of striated surface have been exposed for several years. The sandstone belongs to the base of the « Keuper” formation; the surface inclines about 5°, in the same direction as the grooves and furrows, N. 15° W. ‘The elevation above the sea is about 80 feet. New Road, Kirkdale.—tThe third locality is also in the brick-fields, about 600 yards S.W. of Kirkdale Gaol, and about the same distance from that last referred to, with which it may possibly communicate. The sandstone belongs to the base of the “ Keuper ;” and the striated surface Saposed 1 is fully 500 square yards, inclining throughout at an angle of 75°, in the direction of the stria, which is the same as in the contiguous example, N. 15° W. ‘The elevation above the sea is 80 feet, or perhaps a little less. At each of these places the sandstone is smooth, but with numerous longitudinal grooves and furrows of varying distinctness. The most 378 PROCEEDINGS OF THE GEOLOGICAL sociETY. [June 18, prominent are about an inch wide, and extend several yards in a perfectly straight line. In appearance they seem to have been caused by the passage of some heavy body across the rock; and as ice seems the only agent possible to produce the result, the grounding of icebergs in the ‘Glacial Sea” is probably the cause. Polished striated boulders and small stones are common in the overlying “ Boulder-clay,’”’ and shells very rare. Note.—Since making the above communication, I have found very distinct ice-grooves at Oxton, Cheshire, half a mile 8.E. from Flay- brick Hill. The direction of the striations is N. 30° W., and the gars is about 120 feet above high-water level. October 8, 1862, JUNE 18, 1862. John Cumming, Esq., 7 Montagu Place, Russell Square, and William Topley, Esq., of the Geological Survey of Great Britain, Colchester Villas, Lewisham Road, were elected Fellows. The following communications were read :— 1, On the Mover or Formation of some of the River-vatLEys wm the Sourn of Irrtanp. By J. Burrs Juxus, Esq., M.A., F.R.S., F.G.8., Local Director of the Geological Survey of Ireland, &c. [Puares XIX, & XX. ] ContTENTS. Introduction. B. Relations between the Actions of Part I. Physical Structure of the South Denudation and Disturbance in of Ireland. Former Extension of the Production of the Form of the the Upper Paleozoic Rocks. __ Surface of the Ground. Part II. The Existing River-valleys of C. Proposed Explanation of the the South of Ireland. Formation of the Transverse Val- 1. The River Shannon. leys. 2. The Rivers Barrow, Nore,and Suir. a. River Bandon. 3. The River Blackwater. b. River Lee. 4. The River Lee. c. River Blackwater. 5. The River Bandon. D. Application of this Explanation Part IIT. Formation of the Transverse to the Ravines of the Shannon and Ravines. of the Barrow, Nore, and Suir. A. The Ravines not caused by Dis- | Postscript. turbance. :; Introduction.—The determination of the methcd by which the sur- face of the land has been carved out of the subjacent rock into its present form is a geological problem which has not yet been solved, except in a very general way. The most important. contribution towards this solution is the paper by our President, Professor Ram- say, “ On the Denudation of South Wales and the adjacent Counties of England,” in the first volume of the ‘ Memoirs of the Geological Survey,’ in which the amount of denudation is proved by means of the accurate sections constructed by the Survey. 1862.] | JUKES—RIVER-VALLEYS, 379 When Sir Roderick Murchison became the Director-General of the Survey, and ordered that descriptions, or ‘‘ Explanations,” to accompany each sheet of the map, should be prepared, he pointed to the form of ground as one of the things to be described. I had often previously thought of examining this question, and was there- fore not sorry to find it brought directly before me in the course of my official duties as the Local Director of the Irish branch of the Survey, one of which duties is, of course, the editing of these “ Ex- planations.” The following notes on the formation of some of the river-valleys of the southern part of Ireland contain some conclu~ sions at which I have arrived in the course of the last few years, while engaged in that duty; and they are here offered as a contribution towards the solution of this problem. Part I.—Puysicat Structure oF THE SoutTH oF IRELAND. Ireland may be divided into two nearly equal parts by a line drawn from Dublin Bay to Galway Bay. This line would traverse a broad belt of low, very nearly level ground, the immediately subja- cent rock of which is almost entirely Carboniferous Limestone. It would run from the basin of the Liffey into that of the Barrow, and then crossing that of the Shannon between Lough Ree, the surface of which is about 125 feet above the sea, and Lough Derg, which is about 17 feet lower, would pass into that of Galway Bay, which, ex- cepting the Corrib, receives only a few marginal streams. The watershed between the basin of the Liffey and that of the Barrow cannot be higher in some parts than 279 feet above the sea, which is the height of the summit-level of the Grand Canal near Robertstown, about six miles west of Salins. One of the trigonome-~ trical points on the watershed, south of Robertstown, is only 290 feet above the sea. The watershed between the basin of the Barrow and that of the Shannon passes over ground, near Phillipstown, which is in some places not higher than 261 feet, the level of the Grand Canal there, one of the trigonometrical points on the watershed being only 295 feet. The great Bog of Allen, which is an ill-defined assemblage of large bogs, separated from éach other chiefly by gravel-mounds and esker-ridges, lies on the flat country about the watershed between the basins of the Barrow and the Boyne and the adjacent parts of those of the Liffey and the Shannon; so that there is a broad belt of land here, in the centre of Ireland, no part of which, except perhaps an occasional gravel-mound, exceeds 300 feet above the sea. The summit-level of the Royal Canal, which runs from Dublin to the Shannon above Lough Ree, derives its water from Lough Owel, the height of which is 327 feet above the sea. On the west of the Shannon basin, the watershed between it and Galway Bay is certainly not higher in some places than 300 feet above thesea; for this is the maximum height of the Great Midland 380 PROCEEDINGS OF THE GEOLOGICAL society. [June 18, and Western Railway about Woodlawn, which is the highest ground it crosses*. This great limestone plain, which stretches, thus unbroken, across the centre of Ireland, is interrupted towards the south by five chains of hills, which run along bearings more or less nearly N.E. and 8. W. When, however, we get as far south as Waterford, Tipperary, and Limerick, we meet with other ranges of hills, which run more nearly due E. and W. Of the first five ranges of hills, two are made of Coal-measures, resting conformably on the Carboniferous Limestone, and forming irregular table-lands, of which the summits rise to heights of about a thousand feet above the sea, and are generally near the edges of the escarpments which look down in-every direction on to the low lime-. stone ground around them. The other three ranges of hills are made of Lower (or Cambro-) Silurian rocks (with or without Old Red Sandstone), rising up from beneath the limestone, and attaining often to much greater elevations than the Coal-measures which rest upon it. The Old Red Sandstone, where it appears, always rests quite unconformably on the denuded edges of the Lower Silurian rocks, and passes up conformably into the base of the Carboniferous Limestone, through a narrow band of black shales. Of these three ranges of hills, the most eastern is the Wicklow and Wexford f range, made of Lower (or Cambro-) Silurian slates and traps, with a great mass of intrusive granite, and only coated by Old Red Sandstone towards its southern termination. Its loftiest point is Lugnaquilla (3039 feet), in county Wicklow. . The next of the three ranges consists of the hills called Slieve Bloom (1733 feet), the Devil’s Bit (1583 feet), and the Keeper (2278 feet), and their connecting ridges. They are all composed of Lower Silurian rocks, with an unconformable envelope of Old Red Sand- stone round their base, patches of the same rock being sometimes. left on the summits of the hills. The third range may be said to be formed of the Sheve Aughta (1243 feet), the Slieve Bernagh (1746 feet), and the Sheve Arra (1517 feet), which are of precisely similar constitution with the hills of the second range. Slieve Arra, indeed, is only separated from the Keeper group by a narrow limestone valley, not so wide, in fact, as the one which intervenes between Slieve Bernagh and Slieve Aughta. Of the two groups of high lands which are composed of Coal-mea- sures, the one lies between the Wicklow and Wexford hills on the east and those of the Slieve Bloom and Devil’s Bit on the west, being separated from them, and entirely surrounded, by a tract of low limestone ground, which spreads round them from the great plain on the north. The other Coal-measure high land is that which stretches * IT am indebted to Sir R. Griffith, Bart., for a confirmation of the correctness of the position and altitudes of these and some of the following watersheds. There is, in fact, no commonly received name for the whole of this range,— a peculiarity ‘which often pe it cuitculs to Peper ae of the mountain- ranges in Ireland. ae 1862.) JUKES—RIVER-VALLEYS. 881 from the county Cork, through Kerry and Limerick, into Clare. It is cut in two by the broad estuary of the Lower Shannon. Towards the northern part of Clare, a thin coating only of Coal-measures is is left on the high land, which is there formed of the Carboniferous Limestone,—hills of limestone, more than 1000 feet in height, form- ing the Barony of Burren, and looking down upon Galway Bay. These limestone and Coal-measure hills are separated from the Slieve Aughta and Slieve Bernagh by a low limestone tract, spreading from Galway, past Gort and Ennis, to the Lower Shannon, the water- shed of which is in the neighbourhood of Gort, and is in some places not higher than 150 feet above the sea. It is a branch of this low limestone country which runs out to Lough Derg by Scariff, between the Slieve Aughta and Slieve Bernagh hills. The part of the limestone plain lying on the east side of Lough Derg forms a similar country, and sends a branch down the Kilma-. stullagh valley, between the Slieve Arra and the Keeper group, to the. Shannon at O’Brien’s Bridge, and another smaller one through the Gap of Roscrea, between the Devil’s Bit range and the Slieve Bloom. This latter branch, which thus connects the limestone plains on each side of the central ridge of Slieve Bloom, is traversed by the main watershed of Ireland at a level not higher in some places than 360 feet above the sea. This part of the main watershed runs be- tween the basin of the Shannon and that of the Nore. To the south of the hills just described the limestone country again expands into a plain, in parts of Limerick and Tipperary, between the extension of the two Coal-measure high lands, embracing, however, several minor east and west ranges of lower rocks. The watershed on this plain, between the basin of the Shannon and that of the Suir River, is not higher in some parts, near the Limerick Junction Rail- way-station, than 330 feet above the sea. The most important of the east and west ranges that rise here- abouts is that of the Galty Mountains (8015 feet) and their sub- ordinate groups. These are surrounded by branches of the limestone plain, which meet about Castletown Roche, and conduct us into the valley of the Blackwater. The watershed between the basins of the Suir and Blackwater, in the western branch, is about Castle Harrison, near Charleville, at a height of about 374 feet; that in the eastern. branch is about the Caves of Mitchellstown, and is about 400 feet. above the sea. - The valley of the Blackwater River again enables us to cross Ireland wholly on the Carboniferous Limestone, in a nearly straight line from sea to sea, starting from Dungarvan Harbour, and ascending the Blackwater, past Cappoquin, Lismore, Fermoy, Mallow, and Mill- street, and then descending into the basin of the Flesk, and continuing out by Killarney and Killorglin into Castlemaine Harbour in Dingle Bay. Between Millstreet and Killarney, however, the limestone is’ entirely concealed for some miles by great accumulations of drift, pro- bably not less than 200 feet in thickness ; and the watershed between the Blackwater and the Flesk basins rises in consequence to a height of 550 feet at the lowest point. This is the greatest height for the 382 PROCEEDINGS OF THE GEOLOGICAL society, [June 18, lowest point of a watershed * anywhere, over any limestone ground, in the south of Ireland. | Thus far the Carboniferous Limestone is continuous from the great plain between Dublin and Galway, spreading round the hills of Lower Silurian and Old Red Sandstone rocks, and beneath the hills of Coal-measures. On the south side, however, of this limestone valley, which stretches from Dingle Bay to Dungarvan, the limestone is entirely cut off, and we meet with one continuous range of Old Red Sand- stone running from the headlands of Kerry, {near Valentia, out to Helvick Head, on the south side of Dungarvan Bay. All the Carboniferous Limestone to be found south of this long ridge consists of detached outliers, forming valleys and low grounds in the long synclinal hollows of the Old Red Sandstone. These, with their intervening anticlinal ridges, run along lines bearing, at first due E. and W., but gradually curving round as we go westwards, so as to run E.N.E. and W.S.W. The intervening ridges of Old Red Sandstone are of moderate height in Waterford and the eastern part of Cork, ranging from 400 to about 300 feet above the sea; while no parts of the limestone valleys rise to more than 200 feet, and their general level is less than 100 feet above the sea. As we proceed westward, however, towards Kerry, the ridges rise higher, and the limestone valleys become narrower and shallower, until the Old Red Sandstone alone, but bent into similar curves, forms the well-known mountainous district west and south of Killarney, between Dingle and Bantry Bays. All the hills, indeed, to the south-west of a line drawn from Wex- ford Harbour, past Cashel to Limerick, run from east to west; and most of them rise gently from the east, with their culminating points towards the west. Not only does the present surface of the ground rise higher towards the west, but the beds themselves that form these ridges, while they almost always dip at high angles either to the north or south, nevertheless rise imperceptibly towards the west, so that each bed gradually crops out towards the west, in the bottom of the synclinal or on the crest of the anticlinal folds, those folds being still apparent westwards, but in successively lower beds. We may ex- press this structure by saying that the axes of the curves are gently inclined, so as to sink towards the east, or rise towards the west. All the large open valleys of this south-western corner of Ireland, too, run E. and W. along the strike of the rocks, having been ex- cavated along the uppermost beds as they dip into the synclinal folds. The lateral, or north and south, valleys are narrow and precipitous, and either shallow and at high levels, or else deserve the name of glens or ravines, rather than that of valleys. As far south as the latitude of Cork, the Carboniferous Limestone is separated from the Old Red Sandstone only by the beds of black * Some definite term is wanted to express the lowest point of a watershed be- tween two adjacent basins of drainage, or that point which would first connect them if one or both had their present mouths completely blocked up. mii the phrase, ‘‘lowest connecting gap,” might be used to express this, : 1862. } JUKES—RIVER-VALLEYS. | 383 shale before mentioned. These may be called the Lower Limestone Shale; and they rarely exceed 200 feet in thickness. South of that latitude, however, beds of black argillaceous matter and of grey quartzose grit come in beneath the Lower Limestone Shale, forming the Carboniferous Slate of Sir R. Griffith, with the Coomhola Grits of the Survey, making a group which rapidly thickens towards the south, until it is 5000 or 6000 feet thick. This group there takes the place of the Carboniferous Limestone in the synclinals, the val- leys generally running along its softer upper parts, while the lower, or Coomhola Grit, portion of it forms the ridges, either alone or in conjunction with the Old Red Sandstone. (See Map, Pl. XIX.) A few instances occur, in the Carboniferous Slate country, of the highest*ground rising over a synclinal curve. Shehy Mountain (1797 feet), north of Dunmanway, is the most conspicuous of these; buta few other minor cases occur. Former eatension of the Upper Paleozoic Rocks.—It has been stated that, in the'district north of the Blackwater valley, the Carboniferous Limestone forms one continuous sheet, with the exception of those parts where the Lower Paleozoic rocks or the Old Red Sandstone appear through it. As the beds of the limestone always rise on all sides towards these protruded mounds, and are cut off successively as they approach them, no one can, I think, fail to recognize in these local protrusions the character of accidental holes of erosion in the once continuous sheet, and that the limestone beds formerly stretched horizontally across the areas where these holes occur. In other words, the limestone once spread continuously in horizontal beds over the spaces where we now find the hills of Sleve Bloom and the rest. When, moreover, we come to examine the isolated Coal-measure districts which rest on the limestone, and find them all made of pre- cisely similar beds, with similar fossils, and find also that wherever the uppermost bed of the limestone dips beneath the present surface of the ground, or wherever a hill rises to sufficient elevation above the limestone plain to take in the top bed of the limestone beneath its surface, the lowest beds of the Coal-measures always come in over that bed, with these invariable characters, we are similarly led to the conviction that the Coal-measures were formerly continuous over the whole of the limestone. Similar reasoning holds good for the former persistence of the limestone over the district south of the Blackwater Valley, inasmuch as we always find the limestone coming in wherever the uppermost bed of the Old Red Sandstone dips beneath the present surface, so as to allow of the whole of the black shales to sink beneath it also and the lowest bed of the limestone to appear in its natural po- sition. Where the Carboniferous Slate comes in with so great a thickness as if does in the south-west of Ireland, it of course precludes the appearance of the limestone, which could only come into the ground in one of two cases—either if that ground had been much loftier than it is, the folds of the rocks remaining the same, or if, the outline of the ground remaining the same, the dip of the beds had been more 384 PROCEEDINGS OF THE GEOLOGICAL socteTy. [June 18, steadily persistent in one direction, so as to bring the limestone down beneath its surface. ‘There is no reason to suppose that the limestone or Coal-measures would not have appeared if either of those two circumstances had occurred. I have, indeed, as the result of ten years’ examination and reflection, arrived ‘at the full belief that, wherever in the South‘of Ireland we now find Old Red Sandstone, the Carboniferous Limestone and Coal-measures once existed over it—and not only so, but that the upper rocks once spread far beyond the limits of the lower. i am, in fact, unable to escape the conviction that at the close of the Carboniferous Period one great plain of Coal-measures extended hori- zontally over all Ireland, with the exception perhaps of the loftier peaks of Connemara, Donegal, Down, and Wicklow, even if any parts of those mountains remained uncovered by the highest gee or haat beds. It is also quite clear that, from the base of the Old Red Sandstone to the highest bed of the Coal-measures, all the Upper Paleozoie rocks were originally horizontal, and that at the end of the Coal- measure Period they were all under water. It can be shown that all this vast series of beds was deposited on the slowly subsiding and rather irregular surface of a previously existing land, made of the Lower Paleozoic rocks, and that the de- pression commenced first on the south or south-west, and continued there for a long time, during the deposition of the great mass of the Old Red Sandstone, before it began to affect the centre of Ireland, where the Old Red Sandstone is comparatively thin or does not exist at all. It then went on again during the deposition of the Coomhola Grits and the chief part of the Carboniferous Slate, without much affecting any part north of the latitude of Cork. It was not until after the deposition of the Carboniferous Slate that the depression became more general, so as to allow of the regular deposition of the Lower Limestone Shale and Carboniferous Limestone. The partial nature of the earlier deposits, of course, necessitates a want of strict, parallelism between their beds and those which spread over and beyond them. The departure from strict parallelism, how- ever, would be too slight to be perceptible. In the wedge-shaped mass of the Carboniferous Slate, for instance, the angle included between the planes of the uppermost and lowermost beds would be less than 5°, since the distance between two planes inclined to each other at 5° will in the course of 18 miles exceed 8000 feet. (See Expla- nation to sheet 194, d&c., of the Maps of the Geological Survey of iit ) Part I1.—Tue Existine River-vatieys or THe Sour or IRELand. Having thus given a sketch of the form and structure of the country at the present day, and stated generally what they must have been towards the close of the Carboniferous Period, I now proceed to examine the relation between some of the chief river- valleys and the subjacent rocks. 1862. | , JUKES—RIVER-VALLEYS. 885 1. The River Shannon.—The Shannon, soon after issuing from the northern hills on to the limestone plain, forms the expansion called Lough Ree, from which it slowly winds over another part of the same plain, through great bogs, until it forms the similar expansion called Lough Derg. From the south end of Lough Derg it runs with a rather more rapid current past Killaloe, between the Slieve Arra and Slieve Bernagh hills, through a valley excavated out of the Lower Silurian and Old Red Sandstone rocks. Supposing a dam of 150 or 200 feet in height to be thrown across the narrowest part of the valley at Killaloe, the Shannon, instead of overtopping this dam, and thus seeking to pour down past Killaloe, would inevitably find a passage for its waters round the outside of the hills over the low limestone ground, either by Scariff to the Fergus, or by Nenagh and the Kilmastullagh valley to O’Brien’s Bridge. The Shannon, therefore, has certainly not excavated the valley at Killaloe since the limestone;ground attained to its present low level. Moreover, if these three modes of escape were all blocked up, the Shannon, after forming a great lake in the centre of Ireland, including Lough Derg, Lough Ree, and the adjacent country, together with a large part of the great bog of Allen, would find an exit for its waters down the valley of the Barrow, the Boyne, or the Liffey, or even into Galway Bay, rather than down its present course. It is, therefore, exceedingly difficult to understand how the ravine at Killaloe could haye been excavated either by the Shannon, or by any other waier, supposing it not to exist and the rest of the ground to have an out- line at all approximating to its present form and low level. 2. The Rivers Barrow, Nore, and Suir.—The Barrow issues from a glen on the northern flank of the Sheve Bloom Hills on to the lime- stone plain, where it is separated from some of the tributaries of the Shannon by elevations just sufficient to turn it to the eastward. Then, after winding round the northern termination of the Coal- measure hills of Carlow, it flows down, between them and the Silu- rian and Granitic hills of Wicklow, over low limestone ground as far as Gores Bridge. Here, however, it leaves the limestone plain, and traverses the Lower Silurian and Granite hills in a deep and some- times a wide valley until it flows into Waterford Harbour. Near a little place called St. Mullins, its waters become affected by the tide, whilst Granite hills, exceeding 1600 feet in height, rise on each side of it; and both above and below this, it cuts across the Granite and the aqueous and other rocks indifferently, without any regard either to their “lie” or their composition. The Nore and the Suir both flow from the Devil’s Bit range ; the Suir from Borrisnoe Mountain, and the Nore from the ground two miles north of it. They diverge, however, on entering the limestone plain,—the Suir flowing to the south by Cahir, and then, after a detour, past Clonmel to Waterford; while the Nore, after curving to the north, traverses the limestone plain to near Abbeyleix, and then cuts by a deep valley through the Coal-measure hills near Ballyragget and Freshford, from which it issues out on to the low limestone ground of Kilkenny. Passing over this, it makes for the high 386 PROCEEDINGS OF TME GEOLOGICAL SOCIETY, June 18, Silurian ground beyond Thomastown, cuts directly across the strike of the Old Red Sandstone, which rises from beneath the Limestone at that place, and then winds, in a deep and picturesque ravine with steep banks, between hills of slate and granite from 600 to 800 feet high. Itreceives the influence of the tide at Inistiogue, in the heart of these hills, and, passing through them, falls into the Barrow above New Ross, and flows with itinto Waterford Harbour. The Suir*, on the other hand, flows constantly over low limestone ground to the foot of the Knockmealdon Mountains, which deflect it into the lime- stone valley of Clonmel ; so that it only cuts across the rising beds of the Old Red Sandstone into the contorted Silurian rocks close to the town of Waterford itself, where those rocks seem to have formed originally lower ground than in other parts of their range. It has, however, immediately after leaving the limestone, steep banks of 250 feet on each side of it. In the case of each of these rivers, if the gorges by which they enter the Lower Paleozoic country were now to be blocked up to the level of the adjacent hills, or even to a height of only 300 or 350 feet above the level of the rivers, their pent-up waters would not flow over the dams so formed, but would be poured into the Shannon, either to the north of the Slieve Bloom, or out to Limerick along the line of the railway; or, if those passages were blocked up, they would escape down the basin of the Liffey or the Boyne, ‘This is proof that these gorges were not excavated by the rivers since the limestone ground attained its present low level, at all events. The origin of these gorges, as of that of the Shannon at Killa- loe, had been for a long time inexplicable to me. I think, however, that I have found traces of an explanation in the district that I shall now proceed to describe. 3. The River Blackwater.—I have already mentioned the narrow limestone valley that runs across Ireland, from Dungarvan to Dingle Bay, which is for the greater part of its course drained by the River Blackwatert. (See Map, Pl. XIX.) * Spenser, in his poetical description of the British rivers, in the ‘ Faéry Queen,’ after speaking of these three rivers as three brothers, * Which that great gyant Blomius begot Of the faire nymph Rheusa...” alluding probably to traditional tales now forgotten, thus proceeds to describe them :— + The first, the gentle Shure, that, making way By sweet Clonmell, adornes rich Waterford ; The next the stubborn Neure, whose waters gray By faire Kilkenny and Rosse ponte boord ; The third the goodly Barow, which doth hoord Great heaps of salmons in his deepe bosome : All which, long sundered, doe at last accord To ioyne in one ere to the sea they come ; So, flowing all from one, all one at last become.” Faéry Queene, B. iv. cap. xi. stanza xliii. The “ preat heaps of salmons” have, I fear, become almost as scarce in the Barrow since the days of Elizabeth, as the “‘gyants” were previously to that period. t It will be recollected that there are several other Blackwater Rivers in Ire- land—one, for instance, which falls into the Boyne. 1862.] | JUKES—RIVER-VALLEYS, 387 The Old Red Sandstone ridge which rises immediately to the south of this valley, invariably presents to it a steep slope with an undulating, but generally unbroken summit-ridge. The bottom of the limestone valley rises very slowly as we proceed from Dungarvan towards the interior of the country, until we arrive at its summit- elevation of 550 feet on the borders of county Kerry; and the average height of the summit of the ridge to the south of it increases in at least an equal ratio. The mean height of the ridge in Waterford is about 400 or 500 feet above the sea, with summit-elevations rising to 780 feet, while the highest parts of the limestone attain at one point only to so great an elevation as 200 feet. Between Fermoy and Mallow, where the summit-elevations of the limestone on the plain of Castletown Roche rise to 270 feet, the Old Red Sandstone attains, in the Nagle Mountains, to 13840 feet in height. Between Millstreet and Kil- larney, where the watershed of the Blackwater and Flesk Rivers occurs at 550 feet, the Old Red Sandstone is an unbroken moun- tainous ridge, with summits, such as Caherbarnagh and the Paps, between 2200 and 2300 feet high. Beyond this, where tke level of the limestone descends again to the Lower Lake of Killarney, the Old Red Sandstone forms the range of which Mangerton, the Reeks, and Carantuohill (3414 feet, and the loftiest peak in Ireland) are the summits, The crest of this ridge, between Cappoquin and Mangerton, is in a few places deeply indented by transverse valleys or gaps, of which the level-floored Pass of Glenflesk, leading from Killarney out into the Kenmare valley, is one of the most remarkable examples. The valley through which the Cork Railway runs from Mallow is the next greatest depression; and the valley south of Fermoy is the third. In Glenflesk a very little deeper cuttng towards Morley Bridge would divert the waters of the Flesk into the valley of the Roughty River, and allow of the drainage of some of the ground on the north of the ridge flowing right through it down to Kenmare. This deeper cutting, however, has not taken place; and the range preserves its character of a watershed between the rivers on the north and those on the south all the way from the headlands of Kerry to those south of Dungarvan Harbour, with the very remarkable exception of the Dromana gorge, south of Cappoquin, which I am now about to mention. The River Blackwater is first formed by brooks draining the high Coal-measure ground near King Williamstown, on the borders of Kerry, It runs due south to the foot of the high land near Caher- barnagh, which deflects it at right angles, to the east, down the narrow limestone valley before mentioned. It runs eastward down this, past Mallow, Fermoy, and Lismore, for a distance of fifty-five miles to Cappoquin, Beyond Cappoquin the valley is continued out to Dungarvan Harbour in the same straight line, with the same general low level, and with the same Old Red Sandstone ridges on both sides of it, Instead of following this obvious course, however, the River Blackwater turns suddenly at Cappoquin due south, crosses the lime- VOL, XVIII,—PART I, 2D 388 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, | ‘stone valley, and runs, by means of a deep and picturesque ravine, the sides of which rise steeply to heights of 300 or 400 feet, right across the Old Red Sandstone ridge, which is there a mile and a half broad. Having crossed the first ridge, it comes into another HE. -and W. limestone valley, that of the Tallow outlier, where it receives a large tributary from the west, called the Bride River. It crosses ‘that valley, and cuts through another Old Red Sandstone ridge by a ravine like that of Dromana, but larger, the ridge being 34 mules broad, and rising in one point, called Carnglass, to a height of 650 feet, not far from the river. (See sections, Pl. XX. figs. 1, 3 & 4). It then enters the smaller limestone valley of Clashmore, and cuts across another smaller Old Red. Sandstone ridge into a fourth limestone valley—that immediately above Youghal, and issues out into Youghal Bay through a fourth ridge of Old Red Sandstone, between cliffs 100 feet in height, and through ground that rises to more than ‘double that altitude. This latter ridge is the termination of the one that bounds the northern side of the Cork Valley. The section, Pl. XX. fig. 1, shows the form of the main limestone valley just above Cappoquin, before the river turns to leave it; ard the section, fig. 2, shows its form 43 miles below Cappoquin, at the part where the watershed occvrs between the brooks flowing towards the Dromana ravine and those flowing towards Dungarvan. The latter exhibits, of course, the greatest obstruction that now exists to the course of the Blackwater in the direction of Dungarvan, if the ravine at Dromana were to be blocked up. Figs. 3 and 4 show the ravines at Dromana, 3 miles 8. of Cappo- quin, and at Carnglass, 4 miles still further south, along the course which the Blackwater now follows. It is remarkable also that the tide now flows up these ravines as far as Cappoquin, and that the distance from Cappoquin by the valley to Dungarvan is only ten miles, while through the ravines to Youghal Harbour it is 15 miles. If a dam only 80 or 90 feet high were now to be constructed at ‘the ravine of Dromana, the River Blackwater, after forming a lake on the flat lands about Cappoquin and Lismore, would inevitably pour its waters along the valley into Dungarvan Bay, and excavate a bed for itself in that direction, instead of flowing over and eating away the dam at Dromana. ; | This then is proof that itis impossible for the River Blackwater to have formed the ravines across the Old Red Sandstone ranges since the limestone acquired its present low level, or indeed anything ‘at all approaching that level. 4, The River Lee.—The River Lee issues from Lough Gougane- barra, which has a height of 520 feet above the sea, and works its way through valleys and hills of Old Red Sandstone, and along one little outlying limestone valley, until it breaks forth into the large longitudinal limestone valley in which the city of Cork stands. It there receives from the west a large tributary called the Bride River (like that in the Tallow Valley), which has come in a straight course ‘from Crookstown, at the western end of this long limestone valley, ‘ 2 a eee ee OL Het oe sen et a Pleo SOY DUOUPL) Oy) ud uanwh syybray / ALLL FO. 0.2My aa } pn 10 asoyp) avo some, wy Ae ra eee = 5 608 a: PUPILS BY PIO POUL) a 7 bagcrece as eas ne “purjeat Jo yMog ayy wptsp “anonpunoy ngs rater Q | Mopnt OL neudypap | = é ; OpU : | : | Jo sKalpe,j—teany ey} JO suios jo uOMeULIOF TAs vubisniy ano, Lina) re i Mee eae ate md “ Sie aad i; : ‘ ae 5 % 097 as « ; * " ; oe ; Jo spout omy. uo reded ssexne ay erensnyr oy, CUASTURT SONU) maa aH agnhr auouupysraft pee : 2 Dpqvinny == aes g PER 209" | ypunply jo Ais.ne qonbopoas) Ip JO sameonuyo?) mmm ante appt ; ene” a ee ae ‘ a | soy parysygnd Vy U01f PANNPRT gy Ee ; wb ie | ‘CUO-ARALVM % Wao) in, jo sanimopg op Jo siird jo 03 4G —— — loess CLL 7 : ary fog . es AVW ‘TVOIDOTOAD 4 TO) <4 UMOASHOOD) 4, emai) \ W uinooayyog UMOQINAAN~ LZ ae : sa “ ) 4-29 5:00 6:14 7:03 2) 22h ee 0:48 0-16 0-74 0-74 El (2s 9-00 8:65 6:18 3°90 iean(protoxide) ............ 0-62 0:64 3°96 4-04 Manganese (protoxide) ...... 0:40 1:50 1:28 1-20 | Loss by ignition ............ 2°40 3°90 1:20 8:68 | 0H) ee 99-64 99-69 98:34 | 100-67 No. 1. ae Oceure in coarse gneiss, containing also orthoclase and oli- OClase. No. 2. Dip iilien.—Ocours in granite, in 34-inch plates, + inch in thickness. No. 3. Garvary Wood.—Associated with oligoclase, orthoclase, and molybdenite, in veins in gneiss. No. 4. Castlecaldwell—Associated with orthoclase and schorl in veins in gneiss. This mica is green, and is obviously the black mica much decomposed. Of these micas, No. 4 is evidently decomposing, and not to be considered in forming an opinion on the average composition of the black mica of Donegal. But the differences between No. 3 and Nos. 1 and 2 are too numerous to permit us to take the average of all. To enable us to form an opinion as to the probable composition of this remarkable mineral, I here add four analyses, of which three were made by myself :— Taste VITI.—Black Mica from other localities. No. 1. No. 2. No. 3. ‘ No. 4. a eens 35°55 35:50 39-70 37-40 MME es ed scnce can enessne 17:08 20°80 12°25 11:60 item (peroxide) ..............- 23°70 21-40 23°55 27°66 Pron (orotoxide)................ 3°55 774 0:96 12:43 Manganese (protoxide) ...... HES ho eee eae 1:00 LT hn 0°61 0°56 4-48 0:26 ae es 3.07 4-46 7-25 i UL7 a San ae eee 0°35 0-10 0:47 erent ces as poe pienae 9:45 9-00 7:30 9-20 Loss by ignition ............... 4°30 1:25 1:00 0-60 | 25) eS ee eae 99°61 100°81 97:96 | 99°15 _ No. 1. Ballyellin, co. Carlow.—(Haughton) Quart. Journ. Geol. Soc. vol. xii.p.175. No. 2. Canton.—(Haughton) Phil. Mag., April 1859, p. 259. No, 3, Jonesed, Sweden.—(Haughton) unpublished. No. 4. Petersberg, Wermland.—(Soltmann). 414 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, Rammelsberg (‘ Handbuch der Mineralchemie,’ 1860, p. 668) gives, in his list of magnesia-micas, three only that can be compared with the eight analyses just recorded—viz. Nos. 23, 24, and 25, although he does not hesitate to include in his list micas whose composition with respect to magnesia ranges from 3 to 30 per cent. Physically, it is evident that the eight micas, whose composition is given in the preceding Tables, are identical, notwithstanding the variation in their chemical composition. -5. White Mica.—This mineral, although not a constituent mineral of the granite of Donegal, occurs frequently in veins, and is always associated with orthoclase, sometimes with schorl and beryl. It is biaxial, and resembles the margarodite of Leinster already described in Part I. of these Researches. The following analyses show its composition :— Taste [X.— White Mica of Donegal. Now tl: No. 2 Mean DUCA Se. cnetse. melha awe aed 44-80 45:24 45:02 Alleria? 6. cide. aoa eted 29°76 35°64 38-99 Trromi@pexoxide)iy er yer cae 8:80 2:24 % PRUE PRISONS, Ate Wanda 0:45 0°51 0:48 Maomesia:. cians Acree 0-71 0-71 0-71 SXOe Fea es ae HERA le 0°32 0°54 0°43 Potash? Ac UA eee Sa 12-44 10°44 11-44 Irons(protoxde)) (iii Gedu |S abet ae 0-70 | 0-71 Manganese (protoxide) ...... 0-48 0:24 Loss by ignition ............... 2-00 4-00 3°00 Motelyay 201, .viitncs, 99:76 | 10026 | 100-01 No. 1. Castlecaldwell—F¥ound in veins of quartz and pink orthoclase, con- taining schorl and decomposing plates of black mica. Biaxial (72° 20’). The accompanying woodcut (fig. 1) shows the position of the plane of optical axes. Angle of plate=125°. No. 2. Near Ballygihen, in Dooish Mountain.—In veins in the granite, not associated with black mica; in plates ? inch wide, 4 inch thick. Bi- axial (62° 10’ to 65° 10’). Angle of plate=120°. Fig. 1.— White Mica from Fig. 2.— White Mica from Breezy Castlecaldwell, Donegal. Mountain, near Beleek. —_ OR TIC —AXES- In a specimen of speckled white mica from Breezy Mountain, near Beleek, I found the optical axes to form an angle of 63° 6’; and — also observed their plane to coincide with the shorter diagonal of the primary rhomb, whose angles were 120° and 60°. This is shown 1862. | HAUGHTON—GRAMITES OF IRELAND. 415 in the accompanying figure (fig. 2), in which also the internal lines of structure of the crystal are shown ; from which it seems possible that the optical plane may really bisect the acute angles of some of the component crystals, which would, in this case, have been rotated through 90°. In the specimens from Dooish, the plane of the optical axes is perpendicular to the side of the hexagonal plate of the mica, and therefore joins the acute angles of the primary rhomb. This optical peculiarity of the Breezy margarodite distinguishes it from the margarodite of the Lemster granite, in which the plane of the optical axes coincides with the long diagonal of the primary rhomb, joining its acute angles. From the preceding analyses the following atomic quotients may be calculated :— No. 1. No. 2. Mean. oc. ie 0995 | 1005 | 1000 | 3 Alumina Potten eeeeeceeceereeeees \ 0-682 0644. 0:664. 2 Tron (peroxide) ............... Soe LL ESTES se rs RMA acs a vescie de anceas : ' . JOP LL eee Uae oo vee ! iron (pratoxide) ...../..)::.... Manganese (protoxide) ...... TELS 1 0222 0-444 0°333 1 This result gives very accurately the well-known formula of mar- garodite— RO, 810, + 2(A1,0,, Si0,)+[HO]? The mean of four analyses of margarodite, from four distinct localities of the Leinster granite, gave me— SLLTGS SAS i San a ear 44-58 pI Ns ea, Ge a va Hron (peroxide), °<.0..0'../0% >: poe Lime pS ade Gy CHROMO Cnc GMO ROMO URCROLT Son Cae) 0:78 Minroniesta Or rE OY 0:76 “SLL ca Is a ie IA a 0-95 aries eo ry ee ER, ROT. 10°67 frou (protoxidey’ vee. 51). 0:07 toss byicmtion OY) 0)... 5°34 99:77 The two minerals are plainly identical, and form a well-marked feature of the granite of Leinster and of the granite-veins of Donegal. Margarodite is sometimes, as at Sheskina-roan and Dooish, found in the granite itself. 6. Hornblende.—The granite of Donegal varies much in texture and appearance, as might be expected from its gneissose character. It occasionally passes into a granitic syenite, composed of hornblende, oligoclase, and a little quartz and sphene. The composition of the 416 PROCEEDINGS OF THE*GEOLOGICAL SOCIETY. [June 18, felspar of this rock has been already given; that of its hornblende is as follows :— Hornblende of Donegal Syenitic Granite. Per-centage. Atoms, ELIGA 20). tcl ue mate eae AT DON Le olde eet 1050 ATV eee ee are DOO wParam nus as 108 protoxides Tron (peroxide) ...... 19°11 | of iron and } 551 | " manganese | THANE ibe Ma at erate Votes chs y TONGS rs a Nei 420 Miasniesiay cx share ae eZ Gye: 563 »1587 DOda Ma aus centette es OPIS Te oe heme 31 Potash cn cro Gee oo Ot sinteon eetoahe 22 Iron (protoxide) .... 0°94 Manganese (protoxide) 1-70 99°69 The rock, of which this hornblende is a constituent, has the follow- ing composition ; — Syemtic Granite of Donegal. UCB, Eee ore) Ginnie Seem ERO 58:04 Amana beast ear 16:08 ion) (Peroxide). ace 8:27 Pane RAO os entre biel 6-52 Ma oReStai i.) pions mack te 2°94 DGG a comune Maen eee 4-65 Bekah Testy ate 2°21 Tron (protoxide) .......... 0:45 Manganese (protoxide)...... 1:12 100°28 B. Accidental Minerals. 1. Sphene.—This mineral is very like the clove-brown sphene of Norway: it is found in the granite, when the latter becomes basic, containing much black mica and oligoclase; but it is principally found in a rock formed of a paste of quartz and felspar, that often lies between the granite and limestone of the metamorphic rocks of Donegal. This is especially observable at Anagarry and Barnesbeg, where this rock is so abundant as to become entitled to the name of sphene-rock ; and it cannot be distinguished from similar rocks from Norway. 2. Schorl.—This mineral accompanies orthoclase in veins, and is often curved and cracked, showing the wider openings of the fissures next the convex side, and filed with quartz, as if the curvature of the schorl, and the filling of its fissures with quartz, were the result of an action that took place after the deposition of the mineral. . 3. Beryl.—The only known locality for beryl in Donegal is She- 1862. | HAUGHTON—GRANITES OF IRELAND. 417 skina-roan, near Dunglow. It is green, with occasionally a shade of blue, and occurs both in reefs of quartz traversing the granite along its leading joints, and also in the granite itself, which, in this case, becomes very quartzose, and its black mica disappears, giving place to fine rhombs of margarodite. The beryl of Donegal has never, so far as I know, been analysed— a circumstance which may give some additional value to the follow- ing analysis :— Beryl, from Sheskina-roan, Oo. Donegal. Sp. gr.=2'686. Per-centage. Oxygen. Sie Goro 2 Pasi wats 34:02) 0.0. 4 emit... . 17°22 8:05 8-50 1 Iron (peroxide) .. 1°53 0:45 ne 0-43 Magnesia ...... 0:13 Ginema.-<. 5... .... Ss ie aaa arene SeGO 0 heap uk Matches... 0-90 99°47 This analysis gives very accurately the well-known formula of beryl— Be,0,, 28i0,+ AL0,, 28i0,. Mallet’s analysis of the beryl of Killiney, in the Leinster granite, is as follows :— Beryl of Leinster Granite. pales catty. chee, t . 66°13 AS TERE terete cast eet a 17:87 Hiren (peroxide) <0. i. te. 1:62 CFIC te i UE aang edie een lea 13:09 98°71 This mineral bears the closest resemblance to the beryl of Sheskina- roan in its chemical composition. 4. Garnet.—This mineral, in bright ruby-coloured crystals, is found in the granite of Glenties, Anagarry, and other localities. Form dodecahedral. 5. Molybdenite and Copper-pyrites.—These minerals are found in veins of granite, at Garvary Wood, near Castlecaldwell, associated with oligoclase and black mica. VI. Mineralogical Composition of the Grante of Donegal.—The granite of Donegal, as I have shown, is composed of four minerals, quartz, orthoclase, oligoclase, and black mica, with perhaps an un- known paste besides. It is now necessary to determine numerically its mineral composition, and to investigate the constitution of its paste. In order to do so, we must first fix the composition of each constituent. 1. Quartz.—This is assumed to be pure silica. 2. Orthoclase, Oligoclase, Black Mica.—I take the average com- position of the orthoclase and oligoclase already given; and for that 418 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, of the black mica, I assume the mean of Nos. 1 and 2 of Table VIL., which were procured from the granite of Glenveagh and Ballygihen, and resemble each other closely. Taste X.—Mean Composition of the Constituent Minerals of the Granite of Donegal, Quartz. | Orthoclase.| Oligoclase. |Black Mica.| Silica: |Cesareenaaiers aueescinten - 100-00 63-20 59-92 36:18 AVIDSTOWNTE WS. socapaaboneiee: So0ne-el['s dar sere 18-64 23°68 17-68 RROrs (WETORIGC) erence Mees an rear. 3 0-68 Tiy 26-75 tron (protoxide) . cc... 0. Aewaliwiee snc nfptteneneeiens 0:05 0°63 Protoxide of Manganese......) .:-.0.06. | ssesecees 0-16 0-95 Deine cis. sola eee eiaci ata cneidl «tater 2°75 5°30 0°54 Ma pmesiay «aio. ann daditteec scone! | aanetdes 0-11 0-13 4:65 hS{OLO Eee Ma IIS Man RIGRE (Miho. 3 deca 0°78 6:47 0°32 IPOfaS He jist: stp nes ba snoume walls haseaepilts 14-92 2:07 8-83 VEAEOIO Cos accctse ute heceniort onic iaciey Uae aieiae cca lO ga acer ee | eae 3°15 Potala heF osama 100-60 101-08 98:95 99°68 From the preceding Table we may readily calculate the follow- ing, which gives the proportion of oxygen belonging to the silica, peroxides, and protoxides of each constituent mineral, and which is necessary for the determination of the per-centage of the constituent minerals. Taste XI.—Oxygen-proportions of the Constituent Minerals of the Granite of Donegal. Quartz. |Orthoclase. | Oligoclase. |Black Mica. Silica con | eee coe 51-92 32°81 31-11 18°78 PeroxiGes 1c. See ee ale ees 8°91 11-41 16°28 Protoxides ous kee eee nee 3-55 3-61 3:94 Motalss:c.cateee cee 51:92 | 45:27 46-13 39-00 Let us take as an example of the mineralogical calculation the granite of Doocharry Bridge, No. [X., which is nearly in the centre of the granite axis, and represents well the average granite of Donegal. Its analysis and oxygen-proportions are as follows :— Granite of Doocharry Bridge. Per-centage. Oxygen. Sila. arin aerate UA: a, hone 37°51 Alma, cipal ee he TH 7-46 Tron (peroxide) .....-. Ge if | 5 ie Tron (protoxide) ...... 0:23 | Manganese (protoxide).. 0°32 AMINE és: eye a reli ate 1:68 9-50 Magnesia. .. x gis .i1 terete Oe 3B. (aks tea SOG ay Save. houses esate 3°51 | Potash) j:.)ccrhteieue trae 5°10 ) 1862. } HAUGHION—GRANITES OF IRELAND. 419 If, now, Q., Or., Ol., and M. denote the per-centages of quartz, ortho- clase, oligoclase, and mica in this granite, we have the following equations from the preceding oxygen-ratios :— 375100=5192 0.43281 Or.+3111 Ol.41878M....... (1) 74600= 891 Or.-+1141 O1.+1628 M....... (2) 25000= 355 Or.+ 361 01.4 394M. ...... (3) To which we may add the following :— 100=@.+ Or.4+- OL. Moo. ee eeee es (4) the reason of which is evident. From these four equations, the four unknown per-centages are to be determined. Eliminating M7. from (2) and (3), we find 1130800= 22689 Or.+138817 Ol. .......... (a.) Also, eliminating Q. from (1) and (4), we obtain 144100=1911 Or.4+ 2081 O1.43314M. ...... (b.) Again, eliminating M. between (6) and (3), we obtain the following equation in Or. and Ol. :— 2607600 =42357 Or. +37650 Ol... 2.6... 6. (G) Solving equations (a) and (c) for Or. and Ol., we obtain = Or. So 24:83, O1.= 41:88. Introducing these values of Or. and Ol. inte equation (2), we find M=3:16. And, finally, from (4) we obtain Q=30°63. The mineralogical composition, therefore, of the granite of Doo- charry Bridge is— Doocharry Bridge Gramie. GTP RS nae 30°63 AUS a eee 24°33 ABE hy ie lave Senin 41-88 LEDC 0 i a ee 3°16 100-00 The preceding calculation leaves little to be desired in point of accuracy, although it is open to the objection that it is somewhat laborious. I believe it to be superior in accuracy to the method of measurement used by Delesse. This distinguished geologist has VOL. XVII1.—PART I. 2 F 420 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, obtained the following proportions for three | granites, one from Egypt, and the other two from the Vosges :— Granite. Quartz. | Orthoclase.} Oligoclase. Black Mica. Red Granite of Egypt ...... 44. 43 9 4 Wosges, Tholy i. Sse sl Sire = ga O © ‘S$ = mos 3 & S Sry S \ oo? me NN) EES | .\iSSS a \ e op ; re : * This Section has been drawn for me by Mr. H. M. Jenkins, from data supplied by Mr. T. R. Jones. I have met with several other specimens, some of them of very considerable size, in the Wealden beds near Compton Bay, Isle of Wight. Of these I have secured seven speci- mens. ‘They are large trifid casts, each having the posterior portion more or less elongated, like the specimen indicated by the diagram, fig. 1, p. 396, Quart. Journ. Geol. Soe. vol. vill. One of them(fig. 2) I had raised from its natural posi- tion, as a mass attached to a thin bed of hard sand-rock, in reddish clay, on the shore at low water, between Brook Point and the Chine to the west of it (see section, fig. 1). The other specimens were found loose on the clay of the shore at low water, and were more or less worn by wave- action. These all have the usual three divergent, toe-like pro- jections, varying in propor- tional size in the several speci- mens, and radiating from a palmar mass ; but, in addition, the hinder portion forms a long tapering projection. In the largest (figs. 2 & 3), the whole length of the block is 3 feet 4 inches, but 3 feet 74 inches if measured along the curvature of the base; the breadth across the toes is 27 inches; across the “ heel,” just behind the central mass, 14 inches. The thickness, where the imprint of the toe (A) is represented by the natural cast, is 12 inches; where the pal- mar protuberance (C) has sunk into the pressed clay, 15 inches ; and where the hinder part of the foot, or the meta- podial portion, has impressed 1862. | BECKLES—REPTILIAN FOOTPRINTS. 445 the mud, the cast diminishes gradually in width and in thickness (B), as if this portion of the extremity of the animal had been ob- lique to the foot, at an angle of about 25°. It would thus appear that the foot of a large and heavy animal, walking on muddy ground, sank so deep as to bring the metapodium into contact with the ground; and the inclination of this part of the foot indicates an enormous Reptilian animal, walking with its legs bent and body near the ground. Figs. 2 & 3.—The Natural Cast of a Footprint from the Wealden Beds of the Isle of Wight. (About one-twelfth of the natural size.) Fig. 2. Lower surface. ~ The central prominence (C) in the trifid casts has nearly always a somewhat lateral position towards the largest of the outside toes, and it occupies about two-thirds or three-fourths of the entire breadth of the “palm.” The foot of Zguanodon appears to explain this. It has the distal extremity of the inner metatarsal, or that which supports the shortest toe, posterior to the extremities of the middle and outer metatarsals, so that in this case (and possibly in other Dinosaurs) the integument and flesh would here produce a pad cor- responding to what I may term the heel of the palm. I believe 446 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, that my largest specimen from the Isle of Wight exhibits traces of the impression of the skin in this region of the foot. The metapodial bones of the animal making the tracks here indi- cated must (if the posterior impression was due solely to those bones, and not partly also to the end of the tibia) have been about the size of the largest metatarsal (?) that I have seen from the Wealden beds (Isle of Wight). This was nearly twice the size of the corresponding element of the foot of the half-grown Iqua- nodon figured by Owen; and, judging from the vertebre with which the bone referred to was associated, I am inclined to be- lieve it to have belonged to a Cetiosaurus, or possibly to Pacilo- pleuron. Further, I possess phalangeal bones, recognized as be- longing to Iquanodon, that indicate an individual large enough to have produced such footprints as those under notice. With regard to the three-toed character of the imprints, it is certain that other Dinosaurians besides the Jguanodon had the same modification of structure* ; and we must not refer these pachydactylous trifids to that animal exclusively. Further, if these rough natural casts of footprints indicate with any exactitude the phalangeal propor- tions of the feet, we might seek to allocate the variously proportioned foot-bones of the different Dinosaurs to the differently shaped casts ; but this would be too hazardous a procedure, since the real shape of the foot could have been rarely preserved aright by the clammy mud from which the great brutes dragged their flopping feet. On the firmer ground alone, such as the sandstone on which Mr. Ross has lately found the imprints at Hastings}, could the exact outline of the foot be well preserved. Other natural casts of footprints I have found in the Wealden beds of Swanage Bay, at about 200 yards from the western end of the Wealden cliff there. They occur in two bands of sand-rock, usually about 1 foot thick, separated by about 20 feet of clay, and coming down to the sea-shore with the other beds. These casts are of the usual thick-toed trifidal shape, and of the usual size—about 15 inches long. One specimen of footprint (not a cast), remarkable for its small size (fig. 4), being only about 3 inches long and 3 inches broad, but distinctly trifid lke most of the others known, I met with on the shore of the Isle of Wight, about halfway between Brook and Brixton (see section, fig. 1). It was one of several, about 15 inches apart, on a sandstone band, at very low water. In the abstracts of my former papers, an ornithic relationship was arrived at as the general conclusion as to my views respecting the uniserial trifid footprints found in the Wealden, and my descrip- tions and remarks certainly gave it foundation; but in my manu- script, still in the possession of the Society, I also intimated that these bodies were probably connected with the Reptilian phalanges with which they are associated in the clay and sandstones of the * For instance, see the metapodium of Hyleosaurus, figured and described by Prof. Owen, Pal. Soc. Monograph, 1857, p. 18, pl. 11. + See the August Number of the Society’s J ournal (No. 71, p. 248). 1862. ] THORNTON-——ZANZIBAR. 447 Weald, and I wished to accept the trifids as representatives of the as yet unknown feet of the Dinosaurs. I find that Prof. Owen has referred to this view of the subject, both in his paper in the Society’s Journal, vol. xiv. p. 175, and in his ‘ Paleontology,’ 2nd edit. p. 293. Fig. 4.—Sketch of a Footprint from the Wealden Beds of the Isle of Wight. (Two-thirds of the natural size.) 9. On the Geotocy of ZanziBaR. By Ricuarp TuHornton, Esq. [From a Letter* to Sir R. I. Murchison, F.R.S., F.G.S8., &c.] Ovr route lay from Mombas to the 8.W., over the Shimba, thence N.W. to the Kadiaro, then S.W. to the Pare, then north to the Lake Yipe, thence through Dafeta to Kilema, where we made one attempt to ascend the Kilimandjaro, but had to turn back at an elevation of about 8000 feet. We then went round by the foot of the mountain to Madjami, thence we returned by Dafeta, Lake Yipe, Pare, and the north foot of Usambara, to Wanga on the coast, which we reached on the 101st day from Mombas. We did not succeed in reaching the top of the Kilimandjaro; but I have its altitude from six different stations, connected by tolerable triangles at distances varying from 15 to 50 miles. From these I believe the height of the Kilimandjaro to be about 20,000 feet. Its shape varies much as seen from different points of view; but, from all places we have seen it, its base rises very gradually from a great plain: the outline of the top, as seen from Madjami, is a great dome (but this face is nearly flat); as seen from the east it is * Dated Zanzibar, November 16, 1861. 448 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, conical, with the apex cut off, forming a little plain sloping some- what to the north. The southern slope of this cone is much steeper than the northern. Several miles to the N.E. of the top, a great conical peak rises to about 17,000 feet; and about fifty miles to the west of Kilimandjaro, a great conical mountain, named Méru, rises from the great plain of the Massai to an elevation of perhaps 18,000 feet. | As seen from the east, the snow forms only a thick cap to the Kilimandjaro, with a broad tongue creeping down the south slope; ' and, when the sun is high, several long streaks of snow are seen lying in small ravines descending from the cap. As seen from Madjami, the snow partially covers the 8.W. face of the dome (about one-fourth the height of the mountain), but several large bare patches of rock show out above the snow: the snow here seems to lie at its steepest possible angle; so that fresh snow, falling on this side, must at once slip down to the foot of the face of the dome. On one evening, at Madjami, we saw three such slips of snow in about an hour’s time. On the eastern peak a few patches of snow are seen when the sun is high. All parts of the mountain we saw are composed of lava of sub- aérial origm. From not reaching the top, and having seen only the S.E., S., and 8.W. parts of the mountain, I cannot speak with cer- tainty of its structure; but I think that the Kilimandjaro is the north-eastern part of an old subaérial volcano, the south-western and larger part having sunk down several thousand feet, and been partially broken up by faults. The great fault separating these two parts les about N.W. and 8.E., and forms a very steep, long, flat, south-western face to the mountain; and a high, very rugged mountain-mass lying a few miles to the north of Madjami may be the relics of the top of the original mountain. The commonest rocks to the south and south-west of the moun- tain are a vesicular porphyry, with crystals of glassy felspar, and a fine, hard, stony, slate-coloured lava, slightly vesicular, and some- times containing small black crystals. In the south-east of the mountain there is much of a similar stony lava, only generally more vesicular, and containing more of the small black crystals. Near the foot of the mountain is much highly vesicular brown lava ; and at the outer edge of the south-east slope several uniclinal ridges of metamorphosed sandstone project through the lavas, which here appear to have their original slope; the strike of these ridges is about N. and 8., and the dip E. at about 20°. The geological structure of the rest of the country through which we passed seemed to be very simple. The strike of the whole is about N. and S., and the dip easterly at various angles. Our route lay through a great plain (comparatively a plain, but in reality it rises and falls a little), which stretches far into the interior. It is bounded on the south by the northern ends of the ranges of Usam- bara, Pare, Ugono, Anusha, &c., and to the north by the southern | ends of the Endara and Bura, &c., and contains the mountains of Kadiaro, Kilimandjaro, Méru, &. Between the Kilimandjaro and 7 1862. | THORNTON—ZANZIBAR, 449 Ugono this plain is narrowed to a neck; but it again spreads out to the west as the Great Plain of the Massai. Commencing at the coast, we have first a band, from 3 to 5 miles wide, of coral-limestones and sandstone, &c., which is, I think, of an early tertiary age. This formation is, in common with the greater part of the country through which we passed, covered with red earth, in which I have not seen any fossils. Then comes rather higher ground, composed chiefly of yellow clay-shale; then the coast-range, which varies from 600 to 1300 feet high, consisting of flagstones and sandstones. In the former are many traces of fossils, and thin layers of carbonaceous matter; in these at Rabbai 1 found a few recognizable indications of a kind of Calamite (?), similar to those found in the coal-formation of the Zambesi. (The salt-water creeks of Mombas run with deep water at high tide into the foot of this coast-range.) The general dip of this sandstone-formation is slightly seawards ; but at Rabbai it is thrown by faults in various directions. The Shimba is about the highest part of this range, and presents a fine escarpment, about 800 feet high, towards the interior. On the face of this escarpment I found many blocks of silicified wood; but ap- parently the wood had been much decayed before being silicified. From hence, until halfway to the Kadiaro, we passed over low ridges of flagstones and shales, perfectly similar to those of the Zambesi coal-formation. The dip was to the east at about 5°. These end in a low escarpment, about 200 feet high, at the foot of which the great plain commences (but is not very level). As far as Kadiaro, where rock is seen on the surface, it is generally white sandstone, fre- quently containing deep circular cavities, in which we often found water. Beyond Kadiaro, metamorphism commences, ending to the south-west in many detached uniclinal ranges and hills of the meta- morphosed sandstone-formation, fronting and dipping from the north- east ends of the Pare and Ugono ranges. The high ranges bounding this plain to the north and south all appear to be uniclinal, dipping to the east. The Pare range is, I think, of old crystalline metamorphic rock, dipping to the east at a high angle. The Usambara range has, I think, a base of the same rock, capped by thick beds of the metamorphosed sandstone, dipping slightly to the east; and the Bura range, judging from its outline as seen from a distance, may have a similar structure. The eastern part of the Ugono range is of stratified rock; but the western is, I think, composed of syenite. The Anusha range appears to be of stratified rock, dipping to the east at a high angle. The Kadiaro is a high, narrow, precipitous mountain, composed of old crystalline metamorphic rock, in thick beds, dipping to the east at about 5°. We have not reached the axis of structure of Eastern Africa; but very far to the south-west from Kiléma are seen, on a clear day, three very high rugged mountains (as high as the Meru Mountain) with conical tops, which, if not volcanic (and I think their sides are too steep, and shapes too irregular, for ordinary volcanos), may be composed of the axial granite. * 450 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, 10. On a Srcrion at Junctron-Roap, Lerra. By Witiiam Carrutuers, Hsq., F.L.S. (Communicated by 8. P. Woodward, Hsq., F.G.S.) THE investigation of changes in the earth’s surface which have been effected since its occupation by man, or within the historic period, deservedly receives a large amount of attention in the present day. Any facts which will enable us to form an estimate of the time in which geological changes are produced are of the utmost value to science. Hence the importance of Mr. Leonard Horner’s investiga- tions in the Delta of the Nile, Mr. Geikie’s observations on the coast of the Forth, and similar recent contributions, if based on certain and incontrovertible data, can scarcely be over-estimated. But while the multiplication of such observations is desirable, the elimi- nation of erroneous data forming the bases of important deductions is no less so. And if the pottery raised from such a depth in the Nile sediment as to convince Mr. Horner that it was deposited there 14,000 years ago be Roman pottery, or if the Roman pottery of Mr. Geikie’s Forth section be of modern manufacture, it is of as much, if not of more value to science, that such received errors be corrected, than that new truths be added. In August last year I read Mr. Geikie’s paper, ‘“‘ On a Rise of the Coast of the Frith of Forth*.” Being in Edinburgh at the time, I visited the section which formed the basis of his hypothesis. With his sketch in my hand, I had no difficulty in recognizing the various beds he describes in his paper. But the story that the section pre- sented to me was very different from Mr. Geikie’s reading of it. The republication of his views during the past year, in popular Journals as well as before this Society +, has induced me to submit to you the grounds upon which I differ from him. I shall use Mr. Geikie’s section, copied in fig. 1, and alongside of it a copy of the section Fig. 1.—Seetion at Junction-Road, Lath. After Geikie. wy tebe, nit DNL ted, _-—-~ 7. Sand and shingle with shells. STEAL a << « ie eee a 1 pltannsieseadi Ae Oe ST e-es" =. 6, Brown sand, passing down- BN OE eMail I eee ee wards into re ae Ve hice ee Sgeibetent ht eemeen 5. Dark silt or sandy clay, with a Wabave LG ey ee oe kit Ae eee eu Oyster-shells, bones, pot- = eee Dae ie Siieee - SS tery, &c.: 6 feet. R eo ie 2 Ce SSS SS SS _ 4 Clay: 4 inches. f ey ee 2 *G8a-9 707 8 2 ot oogse SB HB OOO BO Ses 3, Graveland sand: 16 inches. 2. White sand, false-bedded: 6 feet. SG 99,% © “oS won 250508 oe 2/ 1. Gravel or shingle. h. Made earth. from my note-book, made on the spot, together with a section (fig. 2) of the same beds made carefully by a friend somewhat later, * Edinb. New Phil. Journ., New Series, vol. xiv. p. 107. t See the Memoir printed in the August number of this Journal, p. 218, &e. 1862. ] CARRUTHERS—SECTION NEAR LEITH. 451 when the operations of the workmen had exposed a greater extent of the beds. Fig. 2.—Section at Junction-Road, Levth. . Very recent overshot earth and sand. 56. Cultivated soil with cinders, coal, shells, &c. _ 5a. Clay passing upwards into cultivated soil. 4, Clay bed. 3. Gravel and sand. 2. Drift sand, false-bedded ; containing a medieval jar. 1. Gravel (resting on the Boulder-clay). The basement-bed (No. 1) is a very coarse gravel, evidently washed out of the Boulder-clay, on which I observed it rested. Bed No. 2 is a considerable thickness of fine, light-coloured, blown sand. It strikingly exhibits the false stratification characteristic of materials arranged by wind. ‘The whole of the flat on which Leith is built is covered with this sand. It comes out on the surface in the Links, where it is prevented from being blown about by a thin covering of turf. Dr. Paterson, of Leith, obtained, some months ago, from this sand a perfect jar, determined by Mr. Birch, of the British Museum, to be of medieval manufacture. It was found, 12 feet deep, in un- disturbed position in the bed, when digging the foundations of a house. Dr. Paterson read a paper on this interesting discovery to the Society of Scottish Antiquaries last winter. The place at which it was found is at a little distance from Mr. Geikie’s section; but the continuity of the bed between the two places has been deter- mined during drainage-operations which have been lately carried on in the district. This medieval jar, then, which is believed by Dr. Paterson to have been deposited in its place when the layer of sand was finally arranged, occurs in a bed much older than that contain- ing the supposed Roman pottery, and which, according to Mr. Geikie, was deposited when the Romans were in Britain. Beds 3 and 4 are, as described, strata of gravel and clay. Bed 5 is that in which the pottery was found. It is described by Mr. Geikie as “a dark silt, or sandy clay, well stratified, having thin lenticular interlaminations of sand, with occasional oyster-valves, a few stones, and fragments of bones and pottery.” It was formed as a littoral deposit like “the dark sandy mud which covers such ex- tensive flats between tide-marks at Leith.” ‘ Whatever,” he adds, “may be the contents of this bed of silt, they are undoubtedly of contemporaneous deposition.” Among the contents were fragments of pottery of two kinds, glazed and unglazed, and which Mr. M‘Cul- loch, the Curator of the Scottish Antiquarian Museum, “ stated he VOL. XVIII.—PART I. 24 452 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18, would have no hesitation in pronouncing to be Roman, if found near a Roman station.” Mr. Geikie accordingly concludes that “ the existence of Roman pottery in the silt shows us that the deposition of these upraised beds was going on during the Roman oceupation of Britain, and therefore that this rise (of 25 feet) has taken place since the time of the Romans.” The whole value of the section, as giving a key to the age of the deposit and a period within which an important change in the rela- tive level of land and water in the valley of the Forth took place, depends on this bed No. 5. I therefore carefully examined it, and satisfied myself that this was not an unaltered silt deposit, but that it had been a cultivated surface, and that its contents had been placed in it by the husbandman in the process of cultivation. I could discover no evidence of internal lamination ; indeed, having carefully examined it with this in view, I am satisfied that it does not exist. Moreover, the contents of the bed, viz. pottery, oyster- shells, and bones, small fragments of coal and coal-cinders, are scat- tered irregularly through the bed without the slightest approach to laminar arrangement. The occurrence of immense quantities of coal-cinders in the bed made me first doubt the antiquity Mr. Geikie gave to it; for, if the Romans, when in Britain, used mineral fuel, it certainly was not in the quantity needed to supply such a store of cinders as this supposed bed of littoral silt contains. The cinders also gave me the key to, as I believe, the true nature of the stratum. The section is at the foot of Bowling Green House garden, and this bed evidently at no far distant date formed part of the cultivated surface of the garden, its contents being obtained from the manure that was year after year dug into it. The base of the bed is clay of a lightish colour ; this gradually darkens upwards as it has been in- fluenced by tilling and by the organic matter thus introduced, until it becomes a rich dark soil within two feet of its surface. The two upper beds in Mr. Geikie’s section are recent deposits of materials obtained from digging the foundations of houses, as is evidenced by their character, as well as by the large board exhibited at the road- side, permitting “‘ Rubbish to be laid down here free.” The dif- ferent localities of the houses supplied the different kinds of over- shot,—some cartloads of sand having been deposited here, of earth there, or of gravel and sand in another place; but none covering more than a few yards. I have recently obtained a considerable number of objects care- fully collected from bed No. 5. Among them are a number of speci- mens of both the kinds of pottery obtained by Mr. Geikie. These I submitted to Mr. Birch, of the British Museum, who, after a minute examination of every specimen, declared that they were certainly not Roman, but might be the work of any period since the 14th century. I subsequently submitted them to Mr. Franks, also of the Museum, and, without being aware of Mr. Birch’s opinion, he con- firmed it, asserting that no portion of them was older than medieval, and that all of them might be comparatively recent. In addition to — this testimony it will be remarked that the edges of the fragments are invariably sharp, never rubbed as if they had been acted upon 1862. | DENISON—DEATH OF FISHES. 453 by moving water. This is also strikingly characteristic of the frag- ments of bones, which all apparently belong to an animal that still supplies a large proportion of the animal food of the country. But, besides these, I have obtained from the same bed more unequivocal testimony to the recent period at which it received its contents, by the discovery in it of fragments of tobacco-pipes. I neither showed . these fragments nor mentioned their occurrence to Messrs. Birch and Franks, so that their judgment was not in the least influenced by them. If additional evidence were needed to show the true nature of bed No. 5, these portions of tobacco-pipes surely finally settle the matter. Mr. Geikie asserts that, ‘‘ whatever may be the contents of this bed of silt, they are undoubtedly of contemporaneous deposi- tion ; in other words,” he adds, to make it more plain, “all the materials imbedded in the stratum were laid down at the same time with the stratum itself.” That is, according to his theory of the nature of the bed, either these tobacco-pipes on the Society’s table were the work of the Romans, or the valley of the Forth has.been raised 25 feet since the latter part of the 16th century, when it is generally believed Sir W. Raleigh introduced tobacco into this country. It cannot be doubted, it seems to me, that Mr. Geikie’s important inferences were based on a too hasty examination of the section, and were adopted the more readily because perhaps they fell in with opinions already held. 11. On the Deata of Fisnes during the Monsoon off the Coast of Inpra. By Sir W. Denison, Governor of Madras. [In a letter to Sir R. I. Murchison, F.R.S., F.G.S., &c., dated Potucamund, November Ist, 1861.] On steaming between Mangalore and Cananore, on the west coast of the Peninsula, I was sensible of a very offensive smell, which at last I found to proceed from the sea itself. When I landed at Ca- nanore, I found that the sea-breeze brought in a similar smell—a little modified in intensity, of course; and, on inquiry, I found that for some time after the 8.W. monsoon the sea was always very offensive,—that thousands of fish were thrown up on the shore dead. The cause of this was attributed to the mass of fresh water poured into the sea during the monsoon. In three months, 120 inches of rain, on an average, fall upon an area of, say, 60 miles in width, for the whole length of the coast-line, from each running mile of this coast; therefore there will be about 800,000,000 of gallons poured into the sea daily; but, as most of this will come out of the rivers, of course, at certain points, the quantity will be multiplied twofold. The natural consequence will be the destruction of all animal and vegetable life, which, being adapted for salt water, must die after a time in fresh water. There will, therefore, be layers of Shells covered by strata of sand and mud, Sea-weeds in various stages of decomposition, and Fish, small and great, deposited at the bottom of these seas. I saw thousands of dead fish floating, and there were, no doubt, thousands lying dead at the bottom. 2H 2 454 DONATIONS TO THE LIBRARY OF THE GEOLOGICAL SOCIETY. From April 1st to June 30th, 1862. I. TRANSACTIONS AND JOURNALS. Presented by the respective Societies and Editors. Abbeville, Mémoires de la Soc. Imp. d’Emulation d’, 1857-60. 1861. Boucher de Perthes.—De Vhomme antédiluvien et de ses ceuvres, 471. Cochet.—Hachettes diluviennes du Bassin de la Somme, 607. American Journal of Science and Arts. Second Series. Vol. xxxiii. Nos. 98, 99. March and May 1862. From Prof. B. Silliman, For. Mem. GN. A. A. Humphreys and H. L. Abbot’s ‘Report on the Physics and Hydraulics of the Mississippi River,’ noticed, 181. F, A. Genth.—Contributions to Mineralogy, 190. L. Lesquereux.—Plants of the Coal-formations of North America, 206. C. C. Parry.—Physiography of the Rocky Mountains, 231. ——. Profiles of ne Dean Beas 267. . ; T. S. Hunt.—Lower Silurian Glauconite, 277. | O. C. Marsh.—Saurian Vertebree from the Coal of Nova Seotia, 278. J. W. Dawson.—Pre-carboniferous Flora of New Brunswick, 278. J. Marcou.—Taconic and Lower Silurian Rocks of Vermont and Canada, 281. R. P. Greg.—Meteorites, 291. P. A. Kesselmeyer.—Meteor-stones, 292. A. Morlot. —Archeology and Geology, 297. F’. 8. Holmes’s ‘ Post-pliocene Fossils of South Carolina,’ noticed, 298. B. F. Shumard’s ‘Cretaceous Fossils from Texas,’ noticed, 300. F, V. Hayden.—Period of Elevation of the Rocky Mountains near the sources of the Missouri, 305. W. E. Logan.—The Quebec Group and the Upper Coppel eae Rocks of Lake Superior, 320. H. A. Newton.—Meteors in 1860, 344. D. M. Balch.—Orthite from Swampscot, Mass., 348. DONATIONS. 455 American Journal of Science and Arts. Vol. xxxiil. (continued). C. F. Chandler.—A new metal in the native Platinum of Rogue River, Oregon, 351. Winchell Some fossiliferous rocks in Michigan, and new Cepha- opods, 352. B. Se Ric emination of the age of the Red Sand-rock Series of Vermont, 370, 421. M. C. White.—Microscopic organisms in the Paleozoic Rocks of New York, 385. J. C. Ives’s ‘Report on the Colorado River of the West,’ noticed, 387. EK. Hitchcock and otliers’ ‘Report on the Geology of Vermont,’ &c., noticed, 416. E. Billings.—Date of publication of Obolella, 421. C. A. White and R. P. Whitfield—Some Paleeozoic Rocks of the Mississippi Valley, 422. H. B. Geinitz’s ‘ Dyas,’ noticed, 425. Artesian Wells at Passy, 488; Tunnel at Mt. Cenis, 489; Miscel- laneous, 449, Assurance Magazine. Vol. x. Part 3. No. 47. April 1862. Atheneum Journal. Nos. 1797-1809. Notices of Meetings of Scientific Societies, &c. L. Jenyns’s ‘ Memoir of the Rey. J. S. Henslow,’ noticed, 755. Australian Mail. Vol. iv. No. 38. June 12, 1862. Bath Royal Literary and Scientific Institute. 387th Annual Report, for the year 1861. 1862. Berlin. Monatsberichte der Konig.-Preuss. Akad. d. Wissenschaft. zu Berlin. Aus dem Jahre 1861. 1862. Beyrich.—Ueber die Versteinerungen der Vilser Kalksteins, 703. . Die Lias- und Jurabildungen in der Gegend von Fiissen, 719. Ehrenberg.—Mikroscopische Erdleben im Mexikanischen Golf bei Florida, 222; in Davisstrasse bei Island, 275; in Vorder-Indien, Ceylon, Nicobaren-Inseln, Java, Singapore, Lucon, China, Port Jackson, und Neu-Seeland, 886; im Stid-Ocean, 1085. —. Ueber die massenhaft jetzt lebenden oceanischen und die fossilen altesten Pteropoden, 434. Ewald.—Die Grenzgebilde zwischen die Trias- und Juraformation in der Provinz Sachsen, 1010. Rammelsberg.—Zusammensetzung des Stauroliths, 368. ——. Isomorphie der Sulfate von Kadmium, Didym, und Yttrium, 891. . Ueber einige nordamerikanische Meteoriten, 895. Rose, G.—Vorkommen yon krystallisirtem Quarz im Meteoreisen von Xiquipulco in Mexico, 406. . Zeitschrift der Deutschen geologischen Gesellschaft. Vol. x1. Heft 3. 1859. Proceedings, 340-346; Letters, 347-353. W. Keferstein.—Die Korallen der norddeutschen Tertiargebilde (2 plates), 354. Websky.— Ueber Uranophan, 384. C, Lyell.—Ueher fossile Menschenreste, 394, 456 DONATIONS. Berlin. Zeitschrift der Deutschen geologischen Gesellschaft. Vol. x1. Heft 3 (continued). Wedding.—Die Magneteisensteine von Schmiedeberg (2 maps), 399. C. Rammelsberg.—Ueber den Trachyt vom Drachenfels im Sieben- gebirge, 434. | . Ueber den Bianchetto der Solfatara von Pozzuoli, 446. Ch. Heusser und G. Claraz.—Ueber die wahre Lagerstatte der Dia- manten und anderer Hdelsteine in der Provinz Minas Geraes in Brasilien, 448. G. Rose.—Bemerkungen zur vorstehenden Abhandlung, 467. Karsten—Ueber einige Verstemerungen der Kreideformation aus Neu-Granada, 475. : Se ee Vole xn. ett 2. Leou: Proceedings, 169-184; Letters, 185-188. K. von Seebach.—Ueber den wahrscheinlichen Ursprung des soge- nannten tellurischen gediegenen Hisens von Gross-Kamsdorf in Thiiringen (plate), 189. R. Er Beschreibung der Umgegend von Brilon map), 208. C. nantaelihenet= tiebee die Zusammensetzung des Hiuyns und der Lava (Hauynophyr) von Melfi am Vulture, 273. A. Delesse.—Untersuchungen iiber die Pseudomorphosen, 277. Jeitteles.— Versuch einer Geschichte der Erdbeben in den Karpathen- BE Laat a bis zu Ende des achtzehnten Jahrhunderts, Ferd. Romer.—Ueber die Auffindung von Posidonomya Bechert im Grauwackengebirge der Sudeten, 350. H. Trautschold.—Ueber der Moskauer Jura, 353. Zerrenner.—Reclamation gegen Herrn Giebel, 357. ——. ——. Vol. xii. Hefte 2,3. 1861. Proceedings, 137-146, 347-360; Letters, 147, 148, 358-860. Heine.—Geognostische Untersuchung der Umgegend von Ibben- buren, 149 (map). 5 F. von Richthofen.—Ueber den geognostischen Bau der Umge- bungen von Nangasaki, 243. F, Senft.—Die Wanderungen und Wandelungen des kohlensauren Kalkes, 268. H. Trautschold.—Der Moskauer Jura, verglichen mit dem Westeuro- paischen, 361. P. v. Tschikatscheff.—Ueber den neuesten Ausbruch des Vesuvs, 453. G. G. Winkler.—Der Oberkeuper, nach Studien in den bayrischen Alpen, 459 (5 plates). 3 Berwickshire Naturalists’ Club. Proceedings. Vol. iv. No. 5. D. Milne-Holme.—Anniversary Address, 1861, p. 219. Bordeaux, Actes de la Société Linnéenne de. 37° Série. Vol. 111. Livr. 1-6. 1860-62. V. Raulin.—Description physique de Vile de Créte, 1, 70, 321. A. Leymerie.—Sur un aérolithe, tombé prés Montréjean (Haute- — Garonne), le Déc. 1859, 51. DONATIONS. 457 Bordeaux, Actes de la Société Linnéenne de. 1860-62 (continued). E. Jacquot.—Sur la terre végétale des montagnes de la Clape, prés de Narbonne, 318. A. Leymerie.—Notice géologique sur Amélie-les-Bains, 445. Brussels. Annuaire de l’Académie Royale des Sciences, des Lettres et des Beaux-Arts de Belgique. 1862. ——. Bulletins de l’Acad. Roy. des Sciences, &., de Belgique. 3d0eme Année, 2° Sér. Vol. xi. 1861. G. Dewalque.—Sur la constitution du systéme eifélien dans le bassin anthraxifére du Condros, 64. Du Bus.—Sur les découvertes faites dans les travaux de terrassement a Anvers, 511, H. Nyst.—Sur quelques recherches paléontologiques faites aux en- virons d’Anvers, 623. Vol. xu. 1861. P. J. Van Beneden.—Sur un mammifére nouveau du crag d’An- vers, 22. H. Nyst.—Sur un nouveau gite de fossiles se rapportant aux espéces faluniennes du midi de l’Kurope, découvert a Edeghem, prés d’Anvers, 29 (plate). ——. Dix espéces nouvelles de coquilles fossiles du crag noir d’Edeghem, prés d’Anvers, 188. Sur une nouvelle espéce du genre Pecten, trouvée dans le crag noir d’Anvers, ainsi que sur un gisement 4 échinodermes, bryozoaires et foraminiféres, 198 (plate). E. Dupont.—Sur les gites de fossiles du calcaire des bandes carboni- féres de Florennes et de Dinant, 298. ——. Mémoires couronnés et autres mémoires publiés par I’ Acad. Roy. des Se. &c. de Belgique. Collection in 8vo. Vol.xi. 1861. ——. ——. Vol. xi. 1862. A. Perrey.—Sur les tremblements de terre en 1858, avec suppléments pour les années antérieures. ——. Mémoires couronnés et mémoires des savants étrangers publiés par l’Acad. Roy. des Sc. &c. de Belgique. Vol. xxx. 1858-61. Mémoires de l’Académie Royale des Sciences, des Lettres et des Beaux-Arts de Belgique. Vol. xxxiii. 1861. F. Chapuis.—Nouvelles recherches sur les fossiles des terrains secon- daires de la province de Luxembourg (20 plates). Caen. Bulletin de la Société Linnéenne de Normandie. Vol. vi. Année 1860-61. 1862. KE. E.-Deslongchamps.—Sur la présence du genre Phorus dans le dévonien supérieur du Boulonnais, 144 (plate). 458 DONATIONS. Caen et Paris. Mémoires de la Société Linnéenne de Normandie. Vol. xii. Années 1860-61. 1862. HK. Deslongchamps.—Sur de nombreux ossements de mammiféres fossiles de la période géologique dite diluvienne trouvés aux environs de Caen (12 plates). De Ferry.—Sur V’étage Bajocien des environs de Macon (Sadne et Loire). Calcutta. Journal of the Asiatic Society of Bengal. New Series. No. 109. 1861, No. 4. ——. ——. No.110. 1862, No.1. Canadian Journal. New Series. No. 37. January 1862. E. J. Chapman.—Position of Lievrite in the Mineral Series, 42. E. Billings’s ‘ New Species of Lower Silurian Fossils,’ noticed, 71. A. Winchell’s ‘ First Report of the Geological Survey of Michigan,’ noticed, 73. A. Gesner.—Elevations and Depressions of the Earth in North America, 81. ——, ——. No. 38. March 1862. E. J. Chapman.—Minerals and Geology of Canada, 108. ap: Some points connected with the recent Eruption of Vesuvius, 5. J. W. Dawson.—Land-animals in the Coal-measures of Nova Scotia, 144. Produce of British Mines for the year 1860, 147. Newly formed Volcanic Island in the Caspian Sea, 147. _ EF. V. Hayden.—Primordial Sandstone of the Rocky Mountains, 149. ~~ Mineralogical Notices, 151. Canadian Naturalist and Geologist, and Proceedings of the Nat.-Hist. ae of Montreal. Vol. vii. Nos. 1, 2. Feb. and April 1862. T. Macfarlane.—Primitive formations in Canada and Norway, and their mineral wealth, 1. T. §. Hunt.—The “Taconic System ” of Emmons, 78. Chromic Iron-ore and Asbestus, 80. J. W. Dawson.—Flora of the White Mountains, in its geographical and geological relations, 81. ——. An Erect Sigillaria and a Carpolite from the J cee Nova Scotia, 106, T. Macfarlane.—Primitive Formations in Canada and N orway, and their mineral wealth, 1183. HE. Billngs.—Date of the publication of Odolella, 157. Chemical Society. Journal. Nos. 59-62. Vol. xv. Parts 3-6. _ March—June 1862. : Sup n weeee” R. Adie.—Ground-ice, 88. A. H. Churech.—Silica (orbicular), 107. F, Field.—Double Sulphides of Copper and Iron, 125. Colliery Guardian. Vol. iii. Nos. 66-78. Notices of Meetings of Scientific Societies, &e. J, J. Atkinson.—Gases in Coal-mines, and Ventilation, 265. DONATIONS. 459 Colliery Guardian. Vol. iii. (continued). H. T. Hind.—Mineral Ore of Canada, 287. W. W. Smyth.—Lectures on Mining, 287, 305, 325, 346, 364, 388, 428, 485. M. Fryar.—Faults and Disturbances in Coal-mines, 326. W. Barkus.—Working of Pillars in Coal-mines, 326. K. F. Boyd, — Gibsone, and N, Wood.—The Coal-formation along the Border, 403. M. W. T. Scott.—Lecture on Mine-surveying, 443. J. Tennant.—Lecture on Coals, 445. ———. Lecture on Clays and Coprolites, 485. Cossham.—Bristol Coal-field, 485. T. J. Taylor.—Archeology of the Coal-trade, 488, 503. M. Dunn,—..:.4..0e eee , J. F. BRanpT on a Mastodon from Nikolajew (N icolaieft), i in Stern Rn Ae el ee I RO MES Ve Sclavonia, D. StuR on the Neogene-tertiary Strata of Western .. 21 SracHe. On the Geology and Surface-features of Transylvania .. 5 Sroniczka, On some Fossil Bry 0208). ii .a.0 84 (G3 de sea ae 5 biti Stur, D. On the Neogene-tertiary Strata of Western Sclavonia .. 21 Suxrss, EH. The Ground beneath Vienna; its Origin, its Nature, and its Relation to the Public Health............0-ssccveeeeveuss 28 Surface-features of Transylvania, STACHE on the ................ 5 Tertiary (Neogene) Strata of Western Sclavonia, D.Stur on the .. 21 Val Trompia, Fr. von Haver on the Ammonites of..... Cd Bae 6 Vienna, i Sumss.on the Ground beneath... 2.0... csc eee 28 Voleanic Island 1m the Caspian Sea: j.n% a1: asl... dee J eee 1 TRANSLATIONS AND NOTICES OF GEOLOGICAL MEMOIRS. Newly formed Voucanic Istanp im the Caspian Sma. [Extract from a Report published in the ‘ Russian Naval Review,’ translated by Lieut. Litxe, and communicated by Sir R. I. Murcuison, V.P.G.8. ] On the 8th of August last, the steamer ‘ Turky,’ in going to Aster- abad, stopped (in the middle of the Caspian) at a distance of several fathoms from a newly formed island. We went to it in a boat and landed. The length of it is 23 fathoms, the breadth 12 fathoms, the height above the water 6 feet; the average depth of the sea at the distance of 5 to 6 fathoms off the island is also 6 feet. The ground is so loose yet, that the swell of the sea sweeps it away. Itis very dif- ficult to walk on the island, as the feet sink into the ground. The action of fire is to be observed all over the island. One may con- clude that a short time ago it was yet in a liquid state ; for the strong smell of petroleum indicates plainly a volcanic origin, and petroleum. is to be seen on the stones mixed up with the earth, the whole having cooled and being now comparatively hard. In passing on the lee side of the island we also perceived the smell of petroleum. It appears that this newly formed islet lies upon a continuation of the volcanic emanations which trend from the mud-eruptions near Kertch to the fires of Bakou, and in a line towards Asterabad. On the Orv Rep Sanpstone of Bonempa. By M. Joxzty. [Proceed. Imp. Geol. Instit. Vienna, February 25 and March 12, 1861.] TREE subdivisions may be distinguished in the Old Red Sandstone deposited along the southern or Bohemian margin of the Sudetian Mountains*. They are, in ascending order,—-A. Conglomerates, with a few intercalated layers of shale and sandstones, passing upwards into a deposit of shale 180 feet in thickness. This upper portion includes beds of bituminous shale, filled with remains of Fishes and Plants, together with local occurrences of black coal, argillaceous ironstone and sphzrosiderite, and (in a few cases) of traces of copper- ores. The vegetable-remains, as determined by Prof. Unger, stand * See also Quart. Journ. Geol. Soc. vol. xvi. Part ii. Miscell. p. 38. VOL. XVIII —-PART IT B Z GEOLOGICAL MEMOIRS. nearer to those from the Carboniferous beds of Waldenburg (Saxony) and of Radnitz (Bohemia) than to those hitherto known to oceur in the Old Red Sandstone.—B. Arkose-sandstones and a series of thinly stratified ribboned sandstones, with micaceous shales and beds of marly limestone. This subdivision, the most extended, and over- lying unconformably the strata of subdivision A, is but poor in organic remains, with the exception of silicified stems of Arauca- rites in the arkose-sandstones. A stem of Araucarites Schrollianus, Goepp., 24 feet in length and 31 feet in diameter, has been obtained for the Museum of the Imperial Geological Institute of Vienna. cy "ay ty @ W.West imp. U. =e Na GWest lith ad: nets C Veter eeu eee kL 184 | ee ee eS ee g _ Quart. Journ Geol. Soc. Vol. XVIULPLIV. a y (he I~ r ~s i b r: ° f i , H um \ "I GWest ith adnat, W.West ump eRe. ° a eS = a * os 21 i EP tS phil eente 8 ink hd oda : . . inept ; vile ——— ener ae preimage OLEH i A NENT DLE LOT 4 be tien \ J i 5 cache pt ee NP IO A NE ee a em re ee im a Ree aia NSLNEr Baa! Pale GWest lith.adnat. SOU. sy (¢ h Sue OW eli ( 1 D1 j | i t 3 4 . ey Re mst concn a . . 2. a” “2 ee i GWest lith.ad nat. WWest imp sigillaria vascularis. J ieee zee Sree 2 I EES IC LE — as re SCs SS ae ~ a ee “HEIL IS E/N, ‘Tle. eTe[n9 SPA uoIpuspoptde y TAX [OA 99S Toes) TNO P “A.TRNG) “Yet pe grasa) : a iW - West Tap, West ith ad nat Vi West tem Lepidodendron vasculare. ALPHABETICAL INDEX TO THE PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ The fossils referred to are described, and those of which the names are printed in italics are also figured. | Acanthophyton spinosum, 324. Alethopteris decurrens, 322. ingens, 322. from St. John, N.B., 322. Aller, section at, 14. Alpine blocks, transport of, 185. Alpine glaciers, distribution of, 187. Alpine lakes, origin of, 188 ; summary with regard to, 199. Alum Bay, Bracklesham beds at, 84; fossils from, 84; list of beds at, 84; section at, 89. America, Carboniferous rocks of, 142 ; - Crustacea from British North, 346 ; Flora of the Devonian period in North-eastern, 296 ; glacial origin of certain lakes in North, 185; petro- leum-springs in North, 3. Analysis of green colouring matter in the Bracklesham beds, 86. Andromeda reticulata, 373. Anglesea, Carboniferous rocks of, 140. Annandale, section at, 217. Anniversary Address, xxvii-liv. See also Murchison, Sir R..I.; Smyth, W.W.., Esq.; and Huxley, Prof. T.H. Annual Report, 1. Annularia acuminata, 312. Aporoxylon, 306. Araucarites Ouangondianum, 306. Asterophyllites acicularis, 310. latifolia, 311. longifolia, 311. — parvula, 311. sceutigera, 311. Athyris Royssit, 27. subtilita, 28. Aulosteges Dalhousit, 33. Australia, Mesozoic and Permian Faune in Eastern, 244. Award of the Wollaston Donation- fund, xxix; Medal, xxvii. Aye-aye, teeth of the, 359. Ayr, section in the valley of the, 439. Ayrshire, coal-measures of, 437. : Baggy Point, flint arrow-heads from, 114. Ballochmoyle Braes, section at, 441. Bandon, valley of the, 390, 393. Banffshire coast, metamorphic rocks of the, 331; section of the, 333. Barrow, Nore, and Suir, valleys of the, 385, 398. Barton Cliff, section of, 87. Basement-bed of the London Clay, 269. Beckles, 8. H., Esq., on some natural casts of reptilian footprints in the Wealden beds of the Isle of Wight and of Swanage, 4435. Bedford, flint implements in the gravel near, 1138. Bedwin district, geology of the, 260. Belgium, section in, 132. Berridale, section at, 337. Binney, E. W., Esq., on some fossil plants, showing structure, from the lower coal-measures of Lancashire, 106 ; on some upper coal-measures containing a bed of limestone at Catrine in Ayrshire, 437. Black Forest, glacial origin of certain lakes in the, 185. Blackwater, valley of the, 386. Blocks, transport of Alpine, 185. Bolton, J., Esq., on a deposit with in- sects, leaves, &c., near Ulverston, 274. Bone-cave at Wookey Hole, near Wells, Mr. Dawkins on a, 115. Bone-caves of Lunel- Viel, Prof. M. de Serres on the, 1. INDEX TO THE PROCEEDINGS. Bones from Wookey Hole, near Wells, 122. Boulder in Little Cumbra, Mr.J. Smith on a split, 162. Bovey deposit, formation of the, 18 ; Mr. J. H. Key on the, 9; materials of the, 15; strata of the, 10. Bovey Pottery, section at the, 11. Brachiopoda from India, 25. age Bay, 73; list of beds at, A, Bracklesham beds, analysis of green colouring matter in, 86. Bracklesham beds at Alum Bay, 84; Bracklesham Bay, 73; Bramshaw, 80; Brook, 82; Bury Cross, 76; Corfe, 83; Fort Gomer, 77; High Cliff, 86; Hunting Bridge, 79; Mixen Rocks, 76; Netley, 79; Poole, 83; Rowner Fort, 77; Shepherd’s Gutter,80; Stubbington, 77; White Cliff Bay, 67; correla- tion of the fossiliferous localities of the, 92; list of fossils of the, 70; near Selsea, 76 ; of the Isle of Wight Basin, the Rev. O. Fisher on the, 65; New Forest, 79; pebble-beds of the, 90; western range of the, 83. Bramshaw, Bracklesham beds at, 80. Bridge of Allan, Old Red Sandstone of the, 254; section at the, 256. Britain, Carboniferous rocks of, 127 ; glacial origin of certain lakes in, 185. British Isles, lines of deepest water around the, 37; map of the, 41. British North America, Crustacea from, 346. Brook, Bracklesham beds at, 82. Bury Cross, Bracklesham beds at, 76. Bushbury, drift with shells near, 160. Calamites cannzformis, 310. mornatus, 310. Transitionis, 309. Callander, section at, 256. Camarophoria Purdon, 30. Canada, Devonian plants from, 298. Canoes in the alluvium of the Clyde, 221. Carboniferous Brachiopodafrom India, Mr. Davidson on, 25. Carboniferous Limestone, fossil fishes of the, 99; of Oreton and Farlow, Prof. Morris and Mr. Roberts on the, 94; section of the, 97. Carboniferous rocks, Mr. Hull on the iso-diametric lines of the, 127. Carboniferous rocks of America, 142 ; Anglesea, 140; Cumberland, 141 ; Derbyshire, 140; Flintshire, 140 ; Gloucestershire, 142; Lancashire, 140; Leicestershire, 139; Notts, 140; Scotland, 141; Somersetshire, 142 ; South Wales, 142; Stafford- shiré, 1389; Warwickshire, 139 ; Yorkshire, 140. Carboniferous strata near Paisley, crustacean from the, 421. Cardiocarpum cornutum, 324. obliquum, 324. Carpolithes globulus, 375. Websteri, 375. Carruthers, W., Esq., on a section in Junction-road, Leith, 450. Catrine, Ayrshire, coal-measures at, 437, Cave at Wookey Hole, near Wells, 115. Caves of Lunel-Viel, 1. Chalk, surface-deposits on the, 265. Chara Escheri, 375. tuberculata, 376. Charnwood Forest, section in, 137. Cheiromys Madagascariensis, 368 ; teeth of, 359. Chemical composition of the granites of Donegal, 408. Chirbury, crustacean track from, 34:7, Chiton from near Settle, 236 ; Chiton ?, 235. Burrowianus, 234, coloratus, 235. Chitons from the Mountain-limestone, Mr. Kirkby on, 233. Clarke, Rev. W. B., on the occurrence of Mesozoic and Permian Faunee in Eastern Australia, 244. Cleavage- and joint-planes in the gra- nite of Donegal, 404. Clee Hills, Carboniferous Limestone of the, 94. Clyde, alluvium of the, 221. Coal-field, Labyrinthodonts from the Edinburgh, 291. Coal-measures of Ayrshire, Mr. Binney on the, 437. Coal-measures of British North Ame- rica, Crustacea from the, 346. Coal-measures of Lancashire, Mr. Binney on some fossil plants from the, 106. Coal-measures of Nova Scotia, Dr. J. W. Dawson on reptiles from the, 5; Prof. Owen on Reptilia from the, 238. Coast of India, death of fishes off the, 453. Compton Bay to Atherfield, section from, 444, Constance, lake of, 198. Cordaites angustifolia, 318. —— Robb, 316. INDEX TO THE PROCEEDINGS. Cordaites (?) from British North Ame- rica, 318. Corfe, Bracklesham beds at, 83. Cork and Waterford, geological map of, 389. Council, Report of the, i. Courtney Bay, section at, 300. Crinan, ice-action at, 165. Crustacea, a new genus of Silurian, 347. Crustacea from the Coal-measures and Devonian rocks of British North America, Mr. Salter on, 346. Crustacean from the Carboniferous strata near Paisley, Prof. Huxley on a, 420. Crustacean track in the Llandeilo flags, Mr. Salter on a, 347. Cumberland, Carboniferous rocks of, 141; geology of West, 214. Cumberland Plain, Permian strata in, 205; section at, 215. Cumbra, Mr. J. Smith on a split boul- der in, 162. Cyclopteris Brownii, 320. Halliana, 318. incerta, 320. — Jacksoni, 319. obtusa, 319. —— valida, 319. —— varia, 319. Cyperites Forbesi, 373. Dadoxylon Ouangondianum, 306. : Hallii, 306. Dayidson, T., Esq., on some Carboni- ferous Brachiopoda collected in India by A. Fleming, M.D., and W. Purdon, Hsq., F.G.S8., 25. Dawkins, W. B., Esq., on a hyena- den at Wookey Hole, near Wells, 115. Dawson, Dr. J. W., notice of the discovery of additional remains of land-animals in the coal-measures of the South Joggins, Nova Scotia, 5 ; on the flora of the Devonian period in North-eastern America, 296; Reptilia discovered by, 238. Death of fishes during the monsoon, Sir W. Denison on the, 453. Decoy, near Bovey, section at the, 13. Dendrerpeton Acadianwn, 242. Denison, Sir W., on the death of fishes during the monsoon off the coast of India, 453. Depth of water around the British Isles, 37. Derbyshire, Carboniferous rocks of, 140. Devonian flora, 296 ; character of the, 328. Devonian period in North-eastern America, flora of the, 296; fauna of the, 5, 238. Devonian plants from Canada, 299; Maine, 298 ; New Brunswick, 299 ; New York, 297. Devonian rocks of British North Ame- rica, Crustacea from the, 346. Devonshire, flint arrow-heads from Baggy Point, 114. Diagram-section of a formation, 135. Didymophyllum reniforme, 309. Diplopterus, 435. Diprotodon australis (?), 423. —— minor, 423. Diprotodon, Prof. Huxley on, 422. Donations to the Library, xii, 43, 147, 278, 454; Museum, ix. | Donegal, granites of, 403. Drift-beds of Scotland, 165; Wolver- hampton, 159. Drift-period, climate of the, 180 ; fauna of the, 113, 160, 180. Drift with recent shells, the Rev. W. Lister on, 159. Dumfriesshire, geology of South-east- ern, 214; Permian strata in, 205. Eden, Prof. Harkness on Permian strata in the Vale of the, 205. Edinburgh coal-field, Labyrinthodonts from the, 291. Egerton, Sir P. de M. G., Bart., on a new species of Pterichthys (P. ma- crocephalus) from the yellow sand- stone of Farlow, Shropshire, 1038. Elevation of Central Scotland, Mr. Geikie on the, 218. Eocene beds, westerly thinning of the Lower, Mr. Whitaker on the, 258. Eocene fossils from the Isle of Wight, Prof. Sandberger on, 330. Erosion of rocks in Scotland, cause of the, 167. Eruption of Vesuvius, Prof. Palmieri on the, 186; M. Tchihatcheff on the, 126. Etna, volcanic cones of, 20. Eurypterus, Mr. Salter on, 346. Everest, Rev. R., on the lines of deepest water around the British Isles, 37. Falconer, Dr. H., on the disputed affi- nity of the mammalian genus Plagi- aulax, from the Purbeck beds, 348. Farlow, Shropshire, Carboniferous Limestone of, 94; section at, 97; Sir P. Egerton on a new species of Pterichthys from, 1038. Fifeshire, geological sketch-map of, 429; Old Red Sandstones of, 427. INDEX TO THE PROCEEDINGS. Fisher, Rev. O., on the Bracklesham beds of the Isle of Wight Basin, 65. Fishes, death of, 453. Fleming, Dr., Brachiopoda collected in India by, 25. Flint arrow-heads (?) from North Devon, Mr. Whitley on, 114. Flint implements at Wookey Hole, 117; in the gravel near Bedford, 113. Flintshire, Carboniferous rocks of, 140. Flora of the Devonian period in North- eastern America, Dr. Dawson on the, 296. Footprints from the Wealden, 247, 443. Formation, diagram-section of a, 135. Fort Gomer, Bracklesham beds at, 77. Forth, alluvium of the, 225. Fossil fishes of the Carboniferous Limestone, 99. Fossil plants from the Isle of Wight, 369; lower coal-measures of Lan- cashire, Mr. Binney on, 106. Fossils from Alum Bay, 84; High Cliff, 88; Hunting Bridge, 79; the Bedford gravel, 113; the Isle of Wight, 330; Wookey Hole, near Wells, 122 ; Mesozoic and Permian, in BH. Australia, 244; of the Brack- lesham beds, list of the, 70; Old Red Sandstone, 258; Old Red Sand- stones of Fifeshire, 483; Permian, at Hilton Beck, Cumberland, 215. Gamrie to Cullen, section from, 333. Geikie, A., Esq., on the date of the last elevation of Central Scotland, 218. Gemmellaro, Signor G. G., on the vol- canic cones of Paternd and Motta (Sta. Anastasia), Etna, 20. Geneva, lake of, 193. Geological map of Cork and Water- ford, 389; of part of Fifeshire, 429. Geological structure of the Southern Grampians, Prof. Nicol on the, 443. Geology of the gold-fields of Nova Scotia, 342; Zanzibar, Mr. Thorn- ton on the, 447. Gesner, Dr. A., on the petroleum- springs in North America, 3. Gilmerton ironstone, Labyrinthodont from the, 291. Glacial origin of certain lakes, Prof. Ramsay on the, 185. Glacial striz in Scotland, direction of, 167, 183. Glacial surface-markings near Liver- pool, Mr. Morton on, 377 Glacial theory of lakes, 203. Glaciation of Scotland, Mr, b amieson on the, 164, Glaciers and tarns, connexion of, 188. Glaciers, distribution of Alpine, 187. pe Roy, terraces of, 171; Spean, 171. Gloucestershire, Carboniferous rocks of, 142. Glyptolemus, 434. Glyptolepis, 435. Glyptopomus, 435. Godwin-Austen, R. A. C., Esq., reply on receiving the Wollaston Medal, XXViil. Gold-fields of Nova Scotia, the Rev. D. Honeyman on the, 342. Granites of Donegal, chemical compo- sition of the, 408; cleayage- and joint-planes of the, 404; geological relations of the, 406; minerals of the, 410; the Rev. S. Haughton on the, 403. Gravel, flint implements in the, 113. Great Oolite, distribution of the strata of the, 134. Great Ormside, section at, 206. Greywethers, age of the, 271. Harkness, Prof. R., on the metamor- phic rocks of the Banffshire coast, the Scarabins, and a portion of East Sutherland, 331; on the position of the Pteraspis-beds,.and on the se- quence of the strata of the Old Red Sandstone series of South Perth- shire, 253; on the sandstones and their associated deposits in the Vale of the Eden, the Cumberland Plain, - and the South-east of Dumfriesshire, 205. Hartside, section at, 210. Hastings, footprint of Iguanodon at, 247. Haughton, Rev. §., experimental re- searches on the granites of Donegal, 403. Headley Heath, sands of, 273. Heer, Prof. O., on certain fossil plants from the Hempstead beds of the Isle of Wight, with an introduction by W. Pengelly, Esq., 369. Hempstead beds, fossil plants from the, 369. Herault, bone-caves in, 1. High Cliff, Bracklesham beds at, 86; fossils from, 88 ; list of beds Hh 88; section of, 87, 89. Hislop, Rev. S., supplemental note on the plant- bearing sandstones of Central India, 36, 113. Holoptychius, 433. Honeyman, Rev. D., on the geology of the gold-fields of Nova Scotia, 342. INDEX TO THE PROCEEDINGS. Horner, L., Esq. (President), letter to Sir R. I. Murchison, xxix. Hull, B., Esq., on iso-diametric lines, as means of representing the distri- bution of sedimentary clay and sandy strata, as distinguished from calcareous strata, with special refer- ence to the Carboniferous rocks of Britain, 127. Human remains in the alluvium of the Clyde, 221; Forth, 225. Hunting Bridge, Bracklesham beds at, £9: Husley, Prof. T. H. (Secretary), anni- versary address, Feb. 21, 1862 :— results of paleontology, xl; con- temporaneity of strata, xli; works on paleontology, xli; Bronn’s ‘Untersuchungen, xlii; Pictet’s ‘Traité de Paléontologie,’ xli; geological terms, xlii; geological record, xliii ; contemporaneous for- mations, xliv; De la Beche’s ‘ Re- searches in Theoretical Geology,’ xly ; views of Prof. Forbes on con- temporaneity, xlv; percentage of species common to contemporaneous formations, xlvy; synchronism of strata, xlvi; succession of life, xlvi; positive and negative evidence, xlvii; extinct orders, xlviii; persistent types, xlix; changes of life in the Protozoa, 1; in the Ccelenterata, li ; in the Mollusca, li; in the Annu- losa, li; in the Vertebrata, li; pro- gressive modification,lii; ossification of the skeleton, liii ; conclusion, liv. Huxley, Prof. T. H., on a stalk-eyed Crustacean from the Carboniferous strata near Paisley, 420; on new Labyrinthodonts from the Edin- burgh coal-field, 291; on the pre- molar teeth of Diprotodon, and on a new species of that genus, 422. Hyzna-denat Wookey Hole, Mr. Daw- kins on a, 115; section of the, 115. Hylerpeton Dawsoni, 241. Hylonomus aciedentatus, 239. Lyelli, 238, 242. —— Wymanmi, 240. Hymenophyllites curtilobus, 321. Gersdorffii, 322. obtusilobus, 322. Hypsiprymnus Gaimardi, 366. Hypsiprymuus, teeth of, 353. Ice-action at Knapdale, 177; in Scot- land, 164. Iguanodon-footprint at Hastings, Mr. Tylor on, 247. India, death of fishes off the coast of, 453; plant-bearing sandstones of Central, 36. Insects in a deposit near Ulverston, 274: Inverness-shire, map of part of, 170. Treland, river-valleys in the south of, 378. Isle of Wight Basin, Bracklesham beds of the, 651. Isle of Wight, reptilian footprints from the, 443; Prof. O. Heer on fossil plants from the, 369; Upper Eocene fossils of the, 330. Tso-diametric lines, Mr. Hull on, 127. Italian lakes, 198. Jamieson, T. F'., Esq., on the ice-worn rocks of Scotland, 164. Jeffreys, J. G., Esq., list of shells found in the gravel near Bedford, 113; on some fossil shells from the drift near Bushbury, 160. Joggins, Reptilia from the coal-mea- sures of the South, 5, 2388. Jones, T. R., Esq., note on Nummu- lina planulata, Lam., sp., var. Prest- wichiana, Jones, 93. Jukes, J. B., Esq., on the mode of formation of some of the river- valleys in the south of Ireland, 378. Junction-road, Leith, section at, 450, 451. Key, J. H., Esq., on the Bovey de- posit, 9. Kirkby, J. W., Esq., on some remains of Chiton from the mountain-lime- stone of Yorkshire, 238. Kirkby Stephen, section near, 206. Kirkdale, glacial markings at, 377. Knapdale, ice-action at, 177. Labyrinthodonts from the Edinburgh coal-field, Prof. Huxley on, 291. Lake of Constance, 198; Geneva, 193 ; Lucerne, 196; Neuchatel,195; Thun, 196; Zug, 196; Zurich, 197. Lakes, glacial theory of, 203. Lakes in Switzerland, &c., Prof. Ram- say on the glacial origin of, 185. Lakes, Italian, 198; of the northern hemisphere, 201. Lancashire, Carboniferousrocks of, 140; fossil plants from the coal-measures of, 106. wah in a deposit near Ulverston, 274. Lee, valley of the, 388, 395. Leicestershire, Carboniferous rocks of, 139. Leith, section at, 450, 451. Lepidodendron Chemungense, 313, INDEX TO THE PROCEEDINGS. Lepidodendron corrugatum, 313. Gaspianwm, 312. Lepidostrobus globosus, 314. Richardsoni, 314. Leptophleum rhombicum, 316. Library Committee, report of the, v. Limestone in the coal-measures of Ayrshire, Mr. Binney on, 437. Lindale Cote Mines, sections at, 275, 276. List of Devonian plants from New Brunswick, 304; fossil fishes of the Carboniferous Limestone, 99; fossils of the Bracklesham beds of Bracklesham Bay, 74; Alum Bay, 84; High Cliff, 88; Hunting Bridge, 79; White Cliff Bay, 70; shells from the gravel near Bedford, 118 ; specimens from the coal-formation of Nova Scotia, ‘7. Lister, the Rev. W., on the drift con- taining recent shells in the neigh- bourhood of Wolverhampton, 159. Little River, section at, 300. Liveing, Prof., analysis of green colour- ing matter in the Bracklesham beds, 86. Liverpool, glacial near, 377. Llandeilo flags, crustacean track in the, 34:7. Loch Treig, 171. London Basin, Mr. Whitaker on the, 269; section across the, 260; west- ern end of the, 258. London Clay, 270; basement-bed of the, 269. Loxomma Alimanni, 291. Lucerne, lake of, 196. Lunel-Viel, bone-caves of, 1. Lycopodites Matthewi, 314. Vanuxemiu, 314. Maine, Devonian flora of, 298. Manilla, voleanic phenomenon witness- ed in, 8. Map of a part of Nova Scotia, 343 ; lake of Geneva, 194; part of Fife- shire, 429. Marcel de Serres, Prof., on the bone- caves of Lunel-Viel, Herault, 1. Megaphyton (?) from Perry, Maine,318. Mesozoic and Permian faune in E. Australia, the Rev. W. B. Clarke on, 244: Metamorphic rocks of the Banffshire coast, &c., Prof. Harkness on the, 331. Minerals of the granite of Donegal, 410. . Mispec River, section at, 300. surface-markings Mixen Rocks, Bracklesham beds of the, 76. mint death of fishes during the, 453. Morris, Prof. J., and G. E. Roberts, Esq.,on the Carboniferous Limestone of Oreton and Farlow, Clee Hills, Shropshire; with a description of a new Pterichthys, by Sir P. de M. G. Egerton, Bart., 94. Morton, G. H., Esq., on glacial sur- face-markings on the sandstone near Liverpool, 377. Motta, volcanic cone of, 23. Mountain-limestone of Yorkshire, Chi- tons from the, 233. Murchison, Sir R. I. (Vice-President), address on presenting the W ollaston- medal to Mr. Godwin- Austen, xxvii; and to Professor Huxley on handing to him the residue of the Wollaston- fund for Prof. Heer, xxix; obituary notice of Dr. Fitton, xxx. Museum Committee, report of the, iii. Nelumbium Buchii, 374. Netley, Bracklesham beds at, 79. Netley Heath, sands of, 273. Neuchatel, lake of, 195. Neuropteris polymorpha, 320. serratula, 320. New Brunswick, Devonian plants from, 299 ; section at Courtney Bay, 300; section from Little River to Mispec River, 300. New Cross, near Bovey, section near,13. eo Forest, Bracklesham beds of the, : 9. New York, Devonian flora of, 297. Nicol, Prof. J., on the geological structure of the Southern Gram- pians, 443. Nith, section across the valley of the, 217. Nore, valley of the, 385, 398. North America, petroleum-springsin,3. Northern hemisphere, lakes of the, 201. Nottinghamshire, Carboniferous rocks of, 140. Nova Scotia, gold-fields of, 342. , map of, 343. , Reptilia from the coal-measures of, 5, 238. Nummulina planulata, var. Prest- wichiana, 93. Nymphea Doris, 374. Old Red Sandstone, sequence of, in 8S. Perthshire, 253. Old Red Sandstones of Fifeshire, Mr. . Powrie on the, 427. INDEX TO THE PROCEEDINGS. Oolite, distribution of the strata of the Great, 134. Oreton and Farlow, Prof. Morris and Mr. Roberts on the Carboniferous Limestone of, 94. Orthis resupinata, 31. Outliers, tertiary, 260. Owen, Prof. R., description of speci- mens of fossil Reptilia discovered in the coal-measures of the South Jog- gins, Nova Scotia, by Dr. J. W. Dawson, F.GS., &c., 238. Oxfordshire, section in, 131. Paisley, crustacean from the Carboni- ferous strata near, 420. Paleozoic rocks of the South of Ire- land, 383. ; Palmieri, Signor L., on some volcanic phenomena lately observed at Torre del Greco and Resina, 126. Paterné, volcanic cone of, 20. Pebble-beds of the Bracklesham series, 90. Pecopteris,sp.from St. John, N.B.,322. decurrens, 322. ingens, 322. Peltocaris, Mr. Salter on, 347. Pengelly, W., Esq., on certain fossil plants from the Hempstead beds of the Isle of Wight (Introduction), 369. Penrith, geology of the country near, 211; section at, 210. Permian fossils in Cumberland, 215 ; E. Australia, the Rev. W. B. Clarke on, 244. Permian strata in the Vale of the Eden, &c., Prof. Harkness on, 205. Perthshire, Old Red Sandstone of, 253. Petroleum-springs in North America, Dr. A. Gesner on, 3. Phaneropleuron, 434. Pholidogaster pisciformis, 294. Pinnularia dispalans, 312. Plagiaulax Becklesti, 366, 367. — minor, 367. Plagiaulax, Dr. Falconer on the affi- nities of, 348. Plant-bearing sandstones of Central India, Rey. S. Hislop on the, 36. Plants from the coal-measures of Lan- cashire, 106. Platygnathus, 435. Polygonal areas of the lines of deepest water around the British Isles, 37. Poole, Bracklesham beds at, 83. Powrie, J., Esq., on the Old Red Sand- stones of Fifeshire, 427. Prestwich, J., Esq., section of White Cliff Bay, 69. Productus Cora, 31. costatus, 31. — Flemingi, 31. —— Humboldtii, 32. longispinus, 31. —— Purdoni, 31. semireticulatus, 31. striatus, 31. Psilophyton elegans, 315. glabrum, 315. prineceps, 315. Pteraspis-beds, Prof. Harkness on the position of the, 253. Pterichthys from Dura Den, 435. macrocephalus, 108. Punjab, Brachiopoda from the, 25. Purbeck beds, Plagiaulax from the, 348. Purdon, W., Esq., Brachiopoda col- lected in India by, 25. Pygocephalus (?), 421. Ramsay, Prof. A. C., on the glacial origin of certain lakes in Switzer- land, the Black Forest, Great Bri- tain, Sweden, North America, and elsewhere, 185. Ravines, formation of transverse, 390. Report, Annual, i; of the Council, i; Library and Museum Committee, iii. Reptilia from the coal-measures of Nova Scotia, 5, 238. Reptilian footprints-in the Wealden beds of the Isle of Wight and Swan- age, Mr. Beckles on, 443. Resina, volcanic phenomena at, 126. Retzia radialis, 28. Rhachiopteris cyclopteroides, 323. pinnata, 323. —— punctata, 323. striata, 323. tenuistriata, 323. Rhynchonella pleurodon, 29. River-valleys of the South of Ireland, Mr. Jukes on the, 378. Roberts, G. H., Esq., and Prof. J. Morris, on the Carboniferous Lime- stone of Oreton and Farlow, Clee Hills, Shropshire, 94. Romanfell, section at, 207. Roman wall, near the Clyde, 230. Rowner Fort, Bracklesham beds at, 77. Sabal major, 373. St. Bee’s Head, Permian strata at, 216. Salter, J. W., Esq., on a crustacean track in the Llandeilo flags of Chir- bury, Shropshire, 347; on Pelto- caris, a new genus of Silurian Crus- tacea, 347 ; on some fossil Crustacea from the Coal-measures and Devo- nian rocks of British North America, INDEX TO THE PROCEEDINGS. 346; on some species of Eurypterus and allied forms, 346. Sandberger, Prof. F., on Upper Eocene fossils from the Isle of Wight, 330. Sta. Anastasia, volcanic cone of, 28. Scarabins, metamorphic rocks of the, 331; section of the, 337. Scotland, Carboniferous rocks of, 141 ; denudation of, 183; glaciation of, 164; last elevation of Central, 218; Permian strata in, 216 ; sketch-map of, 183; split boulders in the West- ern Isles of, 162. Section across Glen Spean, 174; the Cumberland Plain to Dumfriesshire, 215; London Basin, 260; Permian strata of Annandale, 217; at Aller, near Bovey, 14; Ballochmoyle Braes, 441; Courtney Bay, New Bruns- wick, 300; Farlow, Shropshire, 97 ; Junction-road, Leith, 450, 451; Lindale Cote Mines, near Ulver- ston, 275, 276; the Bovey Pottery, 11; Decoy, near Bovey, 13; (dia- gram) of a formation, 1385; from Berridale to Strath Naver, 337; Bridge of Allan to Callander, 256 ; Compton Bay to Atherfield, 444 ; Great Ormside to Romanfell, 207 ; Little River to Mispec River, New Brunswick, 300; the west of Pen- rith to Hartside, 210; in Belgium and Westphalia, 132; Charnwood Forest, 137; the Valley of the Ayr, 439; near Kirkby Stephen, 206; New Cross, near Bovey, 13; of drift near Bushbury, 161; High Cliff and Barton Cliff, 87; Lake of Ge- neva, 194; the Banffshire coast, 333 ; the hyzena-den at Wookey Hole,115; Permian strata of the valley of the Nith, 217; Wealden along the coast of Sussex, 250; White Cliff Bay, 69. Sections, comparative, in Oxfordshire and Yorkshire, 181; of Alum Bay and High Cliff, 89. Sediments, relations of, 128. Selaginites formosus, 316. Selsea, Bracklesham beds near, 76. Sequoia Couttsia, 372. Serres, Prof. Marcel de, note on the bone-caves of Lunel- Viel, Herault,1. Shannon, valley of the, 385, 398. Shells in the gravel near Bedford, Mr. Jeffreys on, 113 ; near Wolverhamp- ton, Mr. Jeffreys on, 159. Shells in drift, 113, 159, 180. Shepherd’s Gutter, Bracklesham beds at, 80. Shropshire, Carboniferous Limestone of, 94; crustacean track from Chir- bury, 347. Sigillaria palpebra, 307. simplicitas, 308. Vanuxemit, 307. Silurian Crustacea, Mr. Salter on, 3477. Sketches of flint implements from Wookey Hole, 118. Sketch-map of Nova Scotia, 343. Sketch of footprint of the Iguanodon, 248; natural casts of footprints, 445, 447; red sandstone in trap- rock, Ayrshire, 440; the split boul- der on Little Cumbra, 163. Smith, James, Hsq., on a split boulder in Little Cumbra, Western Isles, 162. Smyth, W. W., Esq., Notices of de- ceased Fellows :—Sir Arthur de Ca- pell Broke, Bart., xxxv ; the Rev. J. B. Piggot Dennis, xxxv; General Sir C. W. Pasley, xxxv; the Rev. J.S. Henslow, xxxv; J.J. Forrester, Esq., xxxvii; W. Hutton, Hsq., xxxvii; J. MacAdam, Hsq., xxxvii; Prof. E. Hodgkinson, xxxvii; T. W. Atkinson, Hsqg., xxxix; Sir Charles Fellows, xxxix; M. L. A. Necker de Saussure, xxxix. Somersetshire, Carboniferous rocks of, 142. Southern Grampians, geological struc- ture of the, 443. South Joggins, reptiles from the, 5. South Wales, Carboniferous rocks of, 142. _Sphenophyllum antiquum, 312. Sphenopteris Harttit, 321. Hitchcockiana, 321. — Heeninghausi, 320. marginata, 321. Spirifera lineata, 29. Moosakhailensis, 28. striata, 28. Spiriferina octoplicata, 29. Springs, petroleum-, in North America, 3 Staffordshire, Carboniferous rocks of, 139. Stigmaria exigua, 308. ficoides, 308. Strath Naver, section at, 337. Streptorhynchus crenistria, 30. — crenistria, var. robustus, 30. pectiniformis, 30. Strophalosia Morrisiana, 32. Stubbington, Bracklesham beds at, 77; list of beds at, 77. Suir, valley of the, 385, 398. INDEX TO THE PROCEEDINGS. Surface-deposits on the Chalk, 265. Surface-markings on the sandstone near Liverpool, 377. i Sussex, section of the Wealden along the coast of, 250. Sutherland, metamorphic rocks of, 331. Swanage, reptilian footprints from, 443, Sweden, glacial origin of certain lakes in, 185. Switzerland, glacial origin of certain lakes in, 185. Syringodendron gracile, 308. Syringoxylon mirabile, 305. Table of the distribution of Carboni- ferous fish, 99; Devonian plants, 326. Tables of cleavage- and joint-planes in the granite of Donegal, 404. Tarns and glaciers, connexion of, 188. Tchihatcheff, M. P. de, on the recent eruption of Vesuvius in December 1861, 126. Teeth of Diprotodon, 422. Terebratula biplicata, 26. Himalayensis, 27. subvesicularis, 27. (Waldheimia) Flemingi, 26. Tertiary outliers, 260. Thanet Sand, 266. Theory (glacial) of lakes, 203. Thornton, R., Hsq., on the geology of Zanzibar, 447. Thun, lake of, 196. Thylacoleo carnifex, 368. , teeth of, 353. Torre del Greco, volcanic phenomena at, 126. Torrent-action at Crinan, 165. Toxteth Park, glacial markings at, 377. Transport of Alpine blocks, 185. Trichomanites(?), from St.John, N.B., 322. Trigonocarpum racemosum, 324: Tylor, A., Esq., on the footprint of an Iguanodon, lately found at Hastings, 247. Ulverston, Mr. Bolton on a deposit near, 274; sections near, 275, 276. Uphantenia Chemungensis, 325. Valleys in the South of Ireland, 378. Veitch, J. G., Esq., on a volcanic phe- nomenon witnessed in Manilla, 8. Vesuvius, recent eruption of, 126. View of Loch Treig, 171. Volcanic cones of Etna, Signor Gem- mellaro on, 20. Volcanic phenomena at Torre del Greco, 126; in Manilla, Mr. J. G. Veitch on, 8. Wallen See, 197. ; Warwickshire, Carboniferous rocks of, 139. Water around the British Isles, lines of deepest, 37. Waterford, geological map of, 389. Wealden, footprints from the, 247, 443 ; section of the, 250, 44.4. Wells, hyzena-denat W ookey Hole, 115. Western end of the London Basin, Mr. W. Whitaker on the, 258. Westphalia, section in, 132. Whales in the alluvium of the Forth, skeletons of, 225. Whitaker, W., Esq., on the western end of the London Basin, on the westerly thmning of the Lower Hocene beds in that basin, and on the greywethers of Wiltshire, 258. White Cliff Bay, Bracklesham beds at, 67; section of, 69. Whitley, N., Esq., on some flint arrow- heads (?) from near Baggy Point, North Devon, 114. Wiltshire, greywethers of, 258. Wollaston Donation-fund, award of the, xxix; Medal, xxvii. Wolverhampton, drift with recent shells near, 159. Wookey Hole, bones from, 122; flint implements from, 117; hyzena-den at, 115. Woolwich and Reading beds, 267. Wyatt, J., Esq., on some further dis- coveries of flmt implements in the gravel near Bedford, 113. Yorkshire, Carboniferous rocks of, 140; remains of Chiton from the Mountain-limestone of, 233 ; section in, 131. Zauzibar, geology of, 447. Zug, lake of, 196. Zurich, lake of, 197. THE END. Printed by Taylor and Francis, Red Lion Court, Fleet Street. SUEY ER Sry iG Sa ys ty: Balt. As Se ney a Nc -- Wiis phy ” ate ve." ee AAD ae | > . hs ee 4 4 Ak sat p a ge as HE “ + SMITHSONIAN INSTITUTION LIBRARIES TEIN 3 9088 01350 1622